Occurrence of Nonpegmatite Beryllium in the United States

GEOLOGICAL SURVEY PROFESSIONAL PAPER 318

This report concerns work done on behalf of the U.S. Atomic Energy Commission and is published with the permission of the Commission Occurrence of Nonpegmatite Beryllium in the United States

By LAWRENCE A. WARNER, WILLIAM T. HOLSER, VERL R. WILMARTH and EUGENE N. CAMERON

GEOLOGICAL SURVEY PROFESSIONAL PAPER 318

This report concerns work done on behalf of the U. S. Atomic Energy Commission and is published with the permission of the Commission

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1959 UNITED STATES DEPARTMENT OF THE INTERIOR FRED A. SEATON, Secretary

GEOLOGICAL SURVEY Thomas B. Nolan, Director

The TJ. S. Geological Survey has cataloged this publication as follows: Warner, Lawrence Alien, 1914- Occurrence of nonpegmatite beryllium in the United States, by Lawrence A. Warner [and others] Washington, U. S. Govt. Print. Off. 1959. viii, 198 p. illus., maps, tables. 30 cm. (U. S. Geological Survey. Professional paper 318) Part of illustrative matter in pocket. "This report concerns work done on behalf of the U. S. Atomic Energy Commission and Is published with the permission of the Com­ mission." Bibliography: p. 186-195. 1. Beryllium. i. Title. (Series) [QE75.P9 no. 318] ' GS 59-196

For sale by the Superintendent of Documents, U. S. Government Printing Office Washington 25, D. C. - Price $2.25 (paper cover) CONTENTS

Page Pag« Abstract...-----_--_--___-__-_-_-____----_--_- __ 1 Commercial possibilities and suggestions for prospecting.. 59 Introduction. ____..______1 Description of localities ______61 Nature and purpose of report______1 Nevada and California, by E. N. Cameron and L. A. Recovery, properties, and uses of beryllium. ______2 Warner ______. 61 Production of beryllium ore______2 Nevada ______63 Acknowledgments______4 Elko County. - ______... _ 63 Field investigations.______4 Star mine, Harrison Pass ______63 Previous work______4 Good Hope barite mine, Tuscarora Present work..______4 Range ______._. ______63 Scope of investigations______4 Humboldt County 64 Field methods______5 Golconda manganese-tungsten deposit- 64 Determination of beryllium______5 North workings ______64 Spectrographic analysis______5 South workings.. ______64 Gravimetric and volumetric analysis______6 Occurrence and distribution of Colorimetric and fluorimetric analysis.______6 beryllium.. ______65 Mineralogic methods.______7 Lander County__-__--__----__-.___-_-__ 65 Beryl______7 Barite deposits, Battle Mountain area.. 65 Helvite group.______7 California-Nevada Barite Co. Other minerals-.______-___-______7 65 Radiometric methods______8 Barium Products Corp., Ltd., Mineralogy of beryllium______8 mine...... --_--______.______66 Crystal chemistry of beryllium minerals______8 Lincoln County__-__-----_-----_-----___ 66 Beryllium as an essential constituent in minerals..__ 10 Tern Piute district...... __ ___ ... 66 Beryllium as an accessory constituent in minerals. __ 12 Mineral County____-__- ______66 Sulfides.._____-_-___.______16 Rawhide district ____ .______..__ 66 Oxides______16 Nevada Scheelite mine.. ______67 Halides______.______16 Hooper No. 2 mine ______68 Carbonates______16 Yankee Girl mine______Phosphates______16 Desert Scheelite and Gunmetal mines, Neosilicates- ______16 Pilot Mountains______.____ 68 Ring and chain silicates______18 Desert Scheelite mine..... ______68 Sheet silicates.______18 Gunmetal mine ______69 Framework silicates.______19 Manganese-tungsten deposit at Soda- Beryllium in igneous rocks.,______20 ville... __ . _ _. ______69 United States localities..______20 Andalusite deposits near Thorne. _____ 70 Foreign localities______20 Green Talc naine______70 Distribution of beryllium in igneous rocks..______22 Mine near Green Talc mine. _____ 70 Mode of occurrence______-_-___ 24 Nye County ____ _._-___-______-___ 70 Beryllium in sedimentary rocks..______25 Gabbs area ______70 Clastic deposits...______25 Victory tungsten deposits ______71 Chemical and residual deposits.______26 Brucite and magnesite deposits. __ 71 Coal deposits...______28 Pershing County __ 71 Beryllium in metamorphic rocks...... ______29 Rocks in the West Humboldt Range ..~ 71 Beryllium in pyrometasomatic and related deposits____ 29 Limerick Canyon area... ______71 Previous and present investigations ______29 Panther Canyon area ______72 Characteristics of beryllium-bearing deposits.______33 Rocky Canyon-Wrights Canyon Related occurrences...... ______34 area. ______74 Beryllium in vein deposits______35 Results of sampling______76 Quartz-tungsten veins...... ______35 Tungsten area, Mill City district ___ 76 Quartz-gold veins..______35 Sutton beds of local usage ______76 Manganese-lead-zinc veins______38 George beds of local usage ______77 Other veins.______39 Other rocks sampled ______77 Beryllium in hot-spring deposits.______39 Rose Creek mine.__-______79 Association of beryllium with other elements.______40 Ragged Top area. ______81 Genesis of beryllium deposits...... ^...______58 Champion dumortierite mine______82 m IV CONTENTS

Page Page Description of localities Continued Description of localities Continued Nevada and California Continued New Mexico Continued Nevada Continued Dona Ana County. ______113 White Pine County..______83 Organ district-______113 Cherry Creek district______83 Grant County ______114 Happy claims______83 Burro Mountains district-______114 Cherry Creek mine______83 Carpenter district______114 Snake Range______84 Grandview mine______.__..___-_ 116 Sacramento Pass mine______84 Other mines______116 Dirty Shirt mine______84 Central district (including Fierro, Hanover, San Pedro mine.______85 and Santa Rita districts)______116 Minerva district______. 85 Pinos Altos district-______--_-____ 118 California______85 Hidalgo County.-______118 Inyo County______85 Apache No. 2 district_-_--__-_----_--__- 118 Tungsten Hills district______85 Hachita district (including Eurekr and Deep Canyon area______86 Sylvanite districts)______119 Little Sister mine______86 Lordsburg district.______120 Aeroplane (Moonlight) mine. 87 San Simon district______---____---_--__- 120 Round Valley area______87 Lincoln County______. ______121 Results of sampling.______91 Capitan district_____-__-______-__-_-__ 121 Pine Creek district______91 Gallinas district.______121 Pine Creek tungsten mine______91 Luna County______121 Tailings from mill of Tungstar Tres Hermanas district.______121 mine______92 Victorio district____--___--__-_---___--- 122 Yaney tungsten prospect, Bishop dis­ Geology. ______.____-.-______-. 122 trict______92 Tungsten and beryllium deposits_ _ 122 San Bernardino and Kern Counties.______92 Quartz veins______------_ 123 Atolia district______92 Pyrometasomatic deposits ______123 Union mine...______93 Otero County-_____-______--____-__-__-_- 125 Flatiron-Spanish vein system___ 93 San Miguel County ______125 Arizona, by W. T. Holser______93 Rociada district______-_---_------___-_- 125 Cochise County____-______-______93 Willow Creek district__-_.__--______125 Dragoon Mountains______93 Sandoval County______-_-_---______---_ 125 Courtland-Gleeson district______96 Cochiti district.______-___-__-__-__-__ 125 Gordon mine______96 Santa Fe County..______125 Abril mine______97 New Placers district______125 Little Dragoon Mountains______97 Old Placers district.______127 Tungsten King mine.______98 Sierra County-______128 Bluebird mine______98 Apache No. 1 district.____--___-_____._- 128 Johnson Camp area______101 Cuchillo Negro district.______128 Tombstone district______101 Iron Mountain district.______129 Socorro County______--____--____--_ 129 Mohave County ______101 Jones Camp district_____-___-__-___-_-_- 129 Boriana district______101 Taos County..______---_.__-_-__--_- 129 San Francisco district__---_----_-______102 Red River district--....--.-______129 Pima County______103 Trans-Pecos Region, Texas and New Mexico, by Empire district______-----_--______103 W. T. Holser__--_-_._---______.__._-_--_--. 130 Helvetia district_-___-_-----_-______103 Introduction ______130 Hma district______103 Intrusive igneous bodies and contact zon?s__-_ 131 Santa Cruz County__-__-__---__---______105 Syenitic rocks______-_-______-____-__ 131 Patagonia district_____---_-__-______105 Granitic rocks______._--_____-____---- 131 Yavapai County______106 Metamorphic rocks.______135 Boulder Creek area______106 Wind Mountain area___--______-_---_-_- 135 New Mexico, by W. T. Holser______107 Geology.______-______135 Catron County______107 Structure and metamorphism.______135 Black Range district-__-_____--______107 Igneous rocks.______.___-______--- 137 Colfax County___-______109 Occurrence of beryllium.______-_-_--- 138 Cimarromito district___-_____-______109 Cave Peak area______--_-__-__-__--- 140 Elizabethtown district______109 Geology __-______---______--_--___ 140 Raton volcanic region.______110 Igneous rocks____----__--_-__------140 Geology... ______110 Metamorphic rocks.______--_--___- 141 Occurrence of beryllium.______112 Occurrence of beryllium.______141 CONTENTS

Page Page Description of localities Continued Description of localities Continued Utah, by L. A. Warner and V. R. Wilmarth__.__ 143 Colorado, by L. A. Warner and V. R. Wilmarth-_ 159 Juab and Utah Counties ______143 Boulder County-- ___-_- -___ 161 Tintic district.______143 Coal deposits______161 West Tintic district______144 Chaffee County______161 Topaz Mountain, Thomas Range, by J. C. Calumet mine______161 Olson______144 Geneva claim.______162 Salt Lake County______145 Monarch district______162 Little Cottonwood district-______145 Mount Antero area, by J. W. Adams...-.- 163 Tooele County.-______145 Ouray Peak_... _..__ ___ 163 Ophir district-______145 Sedalia mine______-______163 Sheeprock Mountains.______145 Winfield district______.... 164 Montana, by L. A. Warner and V. R. Wilmarth.__. 148 Clear Creek County______164 Cascade and Judith Basin Counties ______148 Georgetown district______164 Little Belt Mountains-______148 Conejos County--- _____ 164 Deer Lodge County..______149 Platoro-Summitville district______164 Georgetown district, by W. T. Holser. _ _ _. 149 Costilla County______164 Mill Creek area______150 Grayback district.. ______164 Granite County, by W. t. Holser______151 La Veta area.. ______165 Garnet district.._-_-______-__-______151 Custer County... .______165 Philipsburg district.______151 Querida district ______165 Red Lion district.__--___-_--______151 Dolores County--..- _-__ 165 Jefferson County._-______-_--_-___-_--_-___ 152 Rico district------______165 Basin district______152 Fremont County .______166 Elkhorn district.______152 Florence-Canon City area______166 Lewis and Clark County____---_____--_____ 152 Garfield County-. - _--- _-_---- 166 Marysville district----.------.. 152 Rifie and Silt areja______166 Spring Hill mine__-_____--____-______- 153 Gunnison County ______166 Madison County______153 Crested Butte district______166 Silver Star district.---..------.-----.-- 153 Gold Brick district______166 Meagher County.______153 Iron Hill area______.. 166 Gordon Butte._-____-__-_---______-___- 153 Geology.. ______..._.___.._ 166 Powell County______-_____-_.___ 153 Occurrence of beryllium.______169 Ophir district.______153 Commercial possibilities.-..--.------170 Priest Pass area.______153 Italian Mountain area______170 Silver Bow County______154 Snowmass Mountain area_____-____-_---- 171 Butte district.______154 Tincup district-______172 Highland district-______154 Tomichi district..______172 Toll Mountain area.______155 Hinsdale County______173 Sweet Grass County______155 Labe City district______173 Haystack stock______155 Huerfano County... _..______173 Wyoming, by L. A. Warner and V, R. Wilmarth__ 155 Walsenburg area, by W. T. Holser 173 Albany County______155 Lake County...______.. ____ 173 Centennial district.______155 Climax mine----.--.--... ______173 Iron Mountain.______155 La Plata County_.. ___ -___ 174 Rambler mine__-______157 Durango area______174 Strong mine_____-_--__-_-______- 157 Las Animas County______174 Carbon County.:....______157 Morley area, by W. T. Holser _____ 174 Encampment district______157 Mineral County. ______174 Hanna district______157 Creede district______--_____---_-----__- 174 Rawlins area_____-_--__-_--__-__-______157 Wagon Wheel Gap______174 Fremont County_____.______158 Montezuma County______-_____--__-----___ 174 Fort Washakie area______158 Rush Basin______. 174 Laramie County______158 Silver Crown district______158 Ouray County_ ___- 174 Natrona County______158 Ouray district______-______-__-_--_-_- 174 Casper Mountain__--______158 Red Mountain district______175 Garfield Peak...______158 Upper Uncompahgre district-_____-_-___- 175 Platte County______158 Park County______176 Halleck Creek area____-______158 Tarryall district..---______176 Welcome mine______159 Pitkin County______176 Sweetwater County____-______159 Redstone area______176 Leucite Hills_-______-_____--___---__-_- 159 Saguache County_--_------___--_---_---_-_- 176 Superior district____----__-_--___--__--- 159 Bonanza district_____--______-__----_--- 176 VI CONTENTS

Page Page Description of localities Continued Description of localities Continued Colorado Continued Central United States Continued San Juan County______176 Arkansas Continued Eureka-Animas Forks district ______176 Little Rock area______181 Mineral Point and Poughkeepsie Gulch dis- Bryant and Bauxite areas, by W. T. Folser, 181 tricts______---__--______177 Tri-State lead-zinc district ______181 Silvertori district______177 Eastern United States, by W. T. Holser._____._ 181 San Miguel County______178 Sanford, York County, Maine______. 182 Ophir district.______178 Carroll County, New Hampshire______182 Summit County_____^.______178 Iron Mountain. ____------__-_----- 182 Breckenridge district____.______178 Red Hill_____-_-___------~ 183 Montezuma district__-______-______178 Sussex County, New Jersey______183 Upper Blue River district.______178 Beemerville area______183 Teller County______179 Franklin district______183 Cripple Creek district-______179 Central United States, by L. A. Warner and V. R. Irish Creek district, Rockbridge County, Vir­ Wilmarth______179 ginia ______185 Arkansas ______179 Selected references.-.------______186 Magnet Cove_____-______179 Index ______-___-_--__-____-----_--_ 197

ILLUSTRATIONS

[Plates are in pocket] PLATE 1. Intrusive igneous rocks of part of the Trans-Pecos Region, Tex. and N. Mex. 2. Geologic map and section of western area, Wind Mountain, Otero County, N. Mex. 3. Geologic map of southern area, Wind Mountain, Otero County, N. Mex. 4. Geologic map of eastern area, Wind Mountain, Otero County, N. Mex. 5. Geologic map of Cave Peak, Culberson County, Tex. FIGURE 1. Production, imports, and consumption of beryl in the United States, and total world production.. ______3 2. Index map of localities listed in table 16__-______-.______-______-___------__-_-----_. 41 3. Schematic diagram showing occurrence and distribution of principal beryllium-bearing minerals-______. 58 4. Index map showing localities sampled in Nevada and California.______--_--_-__-__._____. 62 5. Geologic map of part of the Rawhide district, Mineral County, Nev__-_--__---_------_------. 67 6. Geologic map of part of the Desert Scheelite mine, Mineral County, Nev_.______--______--_-__--_--_. 69 7. Geologic map of part of Limerick Canyon, West Humboidt Range, Pershing County, Nev______72 8. Geologic map of a part of Panther Canyon area, Rye Patch, Nev______-______-__----_--_____. 73 9. Sketch of part of north wall, South fork of Panther Canyon, Pershing County, Nev______73 10. Geologic map of part of Rocky Canyon and vicinity, West Humboidt Range, Pershing County, Nev___-.-__. 74 11. Geologic map of vicinity of Oreana tungsten mine, Pershing County, Nev______75 12. Geologic map of part of Tungsten area near Mill City, Pershing County, Nev_-__---_--_------78 13. Geologic map of the Rose Creek mine and vicinity, Pershing County, NeY___-__-__--_-_-_-_--_------_--_. 79 14. Geologic map of the Rose Creek mine workings, Pershing County, Nev______80 15. Geologic map of tactite body near Ragged Top mine, Pershing County, Nev_.______-_--_-_-__-__-__-_-. 82 16. Sketch cross section of glory hole, Little Sister mine, Tungsten Hills, Calif., showing rock units sampled..-.-. 86 17. Geologic map showing glory hole level and inclined shaft level of the Round Valley mine, Inyo County, Calif- 88 18. Geologic map of the lower eastern adit, Round Valley mine, Tungsten Hills, Inyo County, Calif _-_-.____. 89 19. Geologic map of the Round Valley mine, Inyo County, Calif___----__---_------90 20. Geologic map of part of Pine Creek mine area, Inyo County, Calif______92 21. Index map of localities sampled in Arizona.______-______-___---_-_---_------_----_-- 94 22. Index map of beryllium occurrences in Dragoon Mountains, Cochise County, Ariz______95 23. Map showing localities sampled in the Little Dragoon Mountains, Cochise County, Ariz____---___-__-_-____ 99 24. Geology of the Tungsten King claims, Cochise County, Ariz______.__-_---_-_-_-_____--_____- 100 25. Mines of the San Francisco district, Mohave County, Ariz______.____-__-__-______-_-__-_ 102 26. Geologic map of part of the Helvetia district, Pima County, Ariz_____--______------_---_----_-_- 104 27. Index map to locations of samples from the Pima district, Pima County, Ariz-______-_-__.-____-_--. 105 28. Geologic map of Boulder Creek area, Yavapai County, Ariz______.___-__--__-_-_-___-_--_- 106 29. Index map showing localities sampled in New Mexico___---___-_____-_-___---__--__-----_------_---- 108 30. Sketch map of localities sampled in the Cimarroncito district, Colfax County, N. Mex______-_-_-____--_--_- 109 31. Map of post-Cretaceous volcanic rocks of the Raton region, New Mexico______111 CONTENTS Vn

Page FIGURE 32. Map of volcanic rocks of southeastern Colfax County, N. Mex______-_____-_-_-----___--___-__-______-._ 112 33. Geologic map of part of the Carpenter district, Grant County, N. Mex______115 34. Index map showing localities sampled in the Apache No. 2 district, Hidalgo County, N. Mex______119 35. Tungsten and beryllium deposits in the Victorio district, Luna County, N. Mex______124 36. Geologic map of the New Placers and part of the Old Placers districts, Santa Fe County, N, Mex______126 37. Index map of the Apache mining district, Sierra County, N. Mex______128 38. Geologic map of Wind Mountain, Otero County, N. Mex______.--_____-____-_-______136 39. Index map of Utah, showing localities sampled______144 40. Geologic index map showing locations of areas investigated in Sheeprock Mountains, Utah __.__.______.__ 146 41. Geologic sketch map showing occurrence of beryl in Hard-to-Beat Canyon, Sheeprock Mountains, Utah______147 42. Geologic sketch map of northwest contact of granite stock, Sheeprock Mountains, Utah.______148 43. Index map of Montana, showing localities sampled______149 44. Sketches showing geology in road cut on U. S. Highway 89, in T. 12 N., R. 8 E., about 10 miles south of Neihart, Mont______150 45. Index and sketch maps of contact zone near Mount Haggin, Anaconda Range, Deer Lodge County, Mont___-._ 150 46. Index map of Wyoming, showing localities sampled_---___---___------_-_--__------156 47. Geologic map of Iron Mountain magnetite deposit, Albany County, Wyo______157 48. Geologic sketch map of part of Halleck Creek area, Platte County, Wyo______158 49. Index map of Colorado, showing localities sampled______-_--_-__-_----__--___--____-_-______160 50. Geologic map of Calumet mine, Chaffee County, Colo______.-._____-_---_----_-_-__-______-______161 51. Geologic sketch map of area near head of Taylor Gulch, Chaffee County, Colo______162 52. Geologic sketch map of vicinity of Star of the West workings, Grayback district, Costilla County, Colo _____ 165 53. Geologic map of Iron Hill area, Gunnison County, Colo__------_-_---_------_.___-______.__ 167 54. Geologic sketch maps of parts of Italian Mountain area, Gunnison County, Colo.______170 55. Geologic sketch map of tactite zone near head of Yule Creek, Snowmass Mountain area, Gunnison County, Colo__ 171 56. Geologic sketch map of part of northern Tomichi district, Gunnison County, Colo___--_- ______172 57. Index map showing localities sampled in the Central United States.______179 58. Geologic map of Magnet Cove, Ark., showing localities sampled____--__-----__----____- ______180 59. Geologic sketch map of area in vicinity of Cove Creek bridge, Magnet Cove, Ark ______181 60. Index map showing nonpegmatite beryllium occurrences investigated in the Eastern United States______182

TABLES

TABLE 1. Comparison of quinalizarin, quinizarin, and morin methods for determination of beryllium in rocks and minerals. _ 6 2. Minerals in which beryllium is an essential constituent______-_-___-___--_----_-_---_----_------____ 10 3. Minerals in which beryllium may be an accessory constituent______--_____------__---_--_------13 4. Garnet analyzed for beryllia____-____-______-._____-__--_---__- 17 5. Analyses of idocrase for beryllia-______-___-_-_-__---_--_--___---_-_- 17 6. Beryllia content of 14 samples of feldspar______19 7. Beryllia content of igneous rocks of the United States, as published______----_-______-______20 8. Beryllia content of igneous rocks of the United States, as analyzed for this study ______21 9. Beryllia content of igneous rocks from foreign localities______-__-_---_---__------__--_------__- 23 10. Beryllia content of sedimentary rocks other than coal in the United States______27 11. Beryllia in ash of coals of the United States______28 12. Beryllia in pyrometasomatic rocks from Germany, Norway, and Sweden-______29 13. Beryllia content of some pyrometasomatic and related deposits of the United States.______30 14. Beryllia in some veins and related deposits in the United States______-___-_--____--______--__--_--_- 36 15. Spectrographic analyses for other elements in samples analyzed for beryllium ______42 16. Other Spectrographic analyses from the files of the U. S. Geological Survey._____-______~______-_ 54 17. Beryllia in samples from Harrison Pass area.______.______-____-___----____------__---- 63 18. Beryllia in samples from north workings, Golconda manganese-tungsten deposit-__-_____----_____-___---___- 64 19. Beryllia in samples from south workings, Golconda manganese-tungsten deposit-______65 20. Beryllia in samples from the California-Nevada Barite Co. mine______-______--___-_--____-__----____- 66 21. Beryllia in mill products from the Tern Piute district______--____---___---_----_-_- ______66 22. Beryllia in samples from the Nevada Scheelite mine.______-_____--__--_--.___-______68 23. Beryllia in samples from the Hooper No. 2 mine______-____-__-----__---_- ______68 24. Beryllia in samples from the Yankee Girl mine-______-___-__-_-___-_-_-----_-__------__-__------68 25. Beryllia in samples from the Desert Scheelite mine-___-____--_----_-_------.-. ______69 26. Beryllia in samples from the Green Talc mine--______-___-___-_-____--_-_------_--_------__- 70 27. Beryllia in samples from inner contact zone, Panther Canyon area.------73 28. Beryllia in samples from outer contact, zone, Panther Canyon area.---.-.-______74 VIII CONTENTS

Page TABLE 29. Beryllia in samples from the Rocky Canyon-Wrights Canyon area______74 30. Beryllia in samples from the Button beds of local usage______76 31. Beryllia in samples from the George beds of local usage______77 32. Beryllia in samples from Humboldt Hill and Stank Hill______78 33. Beryllia in samples from the Rose Creek mine______81 34. Beryllia in samples from the Ragged Top area______81 35. Beryllia in samples from the Champion mine______83 36. Beryllia in samples from the Happy claims______-____---_------_-_-______-_-----______-_-__-- 83 37. Beryllia in samples from the Dirty Shirt mine______85 38. Beryllia in samples from the Minerva district..-______85 39. Beryllia in samples from the Little Sister mine______87 40. Beryllia in samples from the Aeroplane mine______-______-_-_------__--__-_-- 87 41. Beryllia in samples from the Round Valley mine______91 42. Beryllia in samples from the Pine Creek mine______92 43. Beryllia in samples from the Yaney prospect______92 44. Beryllia in samples from the Union mine______93 45. Beryllia and tungsten in samples from the Little Dragoon Mountains. ______97 46. Beryllia in mill tailings from the San Francisco district______-_----_-__----____ 103 47. Beryllia in samples from the Helvetia district______103 48. Beryllia in samples from the Pima district______----___-_-______105 49. Beryllia in samples from the Elizabethtown district______110 50. Correlation of volcanic rocks and related units in the Raton region______110 51. Beryllium and other elements in volcanic rocks of the Raton region______113 52. Average mineralogical composition of volcanic rocks of the Raton region______113 53. Beryllia in samples from the Organ district____-______--_-___--____----_------_-___------114 54. Beryllia in samples from the Carpenter district______116 55. Beryllia in samples from the Central district-______-_____-___--_-__--_-_-_-__-_--_-_-- 117 56. Beryllia and tungsten in samples from the Victorio district-______122 57. Beryllia in samples from the New Placers district______127 58. Beryllia in samples from the Red River district.______130 59. Beryllia in intrusive rocks and contact zones of part of the Trans-Pecos Region ______132 60. Analyses of zirconium silicates.______138 61. Beryllia in samples from Wind Mountain______139 62. Analyses of hornfels from Cave Peak______141 63. Beryllia in samples from Cave Peak______142 64. Beryllia in samples of granite and aplite from Hard-to-Beat Canyon.______. ______147 65. Beryllia in minerals from contact zone, Mill Creek area, Montana______151 66. Beryllia in samples from mine dumps at Butte, Mout______154 67. Beryllia in samples from Washoe Reduction Works, Anaconda, Mont--______154 68. Beryllia in samples from Halleck Creek area______159 69. Beryllia in samples from Iron Hill, Colo______169 70. Distribution of beryllia in rock types at Iron Hill, Colo______169 71. Beryllia in samples from the Tincup district------______172 72. Beryllia in samples from the Lake City district______173 73. Beryllia in samples of mill products from Climax, Colo______174 74. Beryllia in samples from the Red Mountain district______175 75. Beryllia in samples from the Tarryall district-___-____-______176 76. Beryllia in samples from the Eureka-Animas Forks district------177 77. Beryllia in samples from the Golden Cycle mill______179 78. Beryllia in samples from Magnet Cove, Ark______180 79. Beryllia and niobium in samples from Iron Mountain, N. H______183 80. Beryllium in samples from the Beemerville area, New Jersey______188 81. Beryllia in mill products from the Franklin district______-______184 82. Beryllia in minerals from the Franklin district______~__-______-----_------__- 185 THE OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES

By LAWRENCE A. WARNER, WILLIAM T. HOLSER, VERL R. WILMARTH, and EUGENE N. CAMERON

ABSTRACT portion of the pyrometasomatic deposits contained detectable The demand for beryllium in industry increased rapidly dur­ quantities of beryllium; the richest are the deposits at Iron ing and after World War II, establishing a trend that is likely Mountain, N. Mex. In the feldspathoidal rocks beryllium was to continue. Production of beryl from pegmatites, the only found only as an accessory constituent in rock minerals* present source of beryllium, has lagged far behind annual con­ Some of the vein deposits investigated have promise F.S pos­ sumption in the United States, and even with heavy imports, sible sources, but sampling was not sufficiently detailed to fur­ an adequate domestic supply has not been assured. This con­ nish a basis for calculating reserves. In places the ber7llium dition has directed attention to nonpegmatite deposits. During content compares favorably with that of beryl pegmatites. Min­ the period 1948-50 the U. S. Geological Survey conducted a pro­ ing of these deposits will depend on an increase in price of gram of field, laboratory, and library research to determine the beryllium, improved beneficiation methods, and utilization of occurrence and distribution of beryllium in nonpegmatite rocks coproducts and byproducts. and mineral deposits, and to appraise the extent to which these might furnish beryllium ore. Although no deposits of present INTRODUCTION commercial value were found, the investigation has set criteria that will be of value in future prospecting. NATURE AND PURPOSE OE REPORT The average beryllia content of the lithosphere is about 0.001 Technological developments during the past d?oxygen salts, which constitute the bulk of metal­ has come to assume great strategic importance. Spe­ liferous ores. Because of its small ionic radius, resulting low cial alloys containing beryllium are in wide demand in coordination number, and strongly electro-positive character, modern industry and their use is restricted chief y by crystal structures that will permit high concentrations of beryl­ lium in minerals are comparatively rare. It forms only a few the short supply and relatively high cost of beryllium stable minerals of its own, such as beryl, helvite, chrysoberyl, metal. and phenakite. In other silicates, including the common Beryl-bearing pegmatites, so far as known in mid- rock minerals, it may replace elements such as silicon and 1956, constitute the only commercial source of beryllium. aluminum to a slight extent. Under special conditions, as when Because high-grade domestic reserves are small, the it fills normally empty lattice positions in idocrase, it may be present in appreciable quantity. United States has been forced to import most of the As an accessory constituent in rock minerals, beryllium is beryl it uses. Recently attention has been focused on somewhat more common in granitic and feldspathoidal rocks rocks other than pegmatite as potential sources of than in other igneous rocks. Its principal occurrence is in beryl beryllium. During the past century many beryllium- in granitic pegmatites. Other than in pegmatites, beryllium bearing minerals have been reported from a variety of minerals are found chiefly in quartz-tungsten veins and pyro- metasomatic deposits. Small amounts also occur in other types rocks and mineral deposits. Only a few of these min­ of veins, particularly quartz-gold and manganese veins. In most erals are common and many are exceedingly rare. of these occurrences beryllium is found with fluorite; in pyro- However, beryllium is evidently much more widely dis­ metasomatic deposits it sometimes occurs with fluorine-rich tributed in the rocks of the earth than had been as­ beryllian idocrase. sumed previously, a discovery that suggests the possi­ Many sedimentary rocks contain small quantities of beryl­ lium, particularly those formed by residual concentration, as bility of locating new sources of supply. the metal hydrolyzes in a manner similar to aluminum. For A program of field, laboratory, and library research the most part, however, beryllium tends to be dissipated by to formulate workable criteria that might be us?.d in processes of weathering and sedimentation. Under simple meta- the search for beryllium ore in nonpegmatite rock? was morphic conditions, beryllium is not easily mobilized, and there­ begun in 1948 by the U. S. Geological Survey on be­ fore it is not concentrated in metamorphic rocks other than pyrometasomatic deposits. half of the Division of Raw Materials of the TJ. S. Pyrometasomatic deposits and feldspathoidal rocks were sam­ Atomic Energy Commission. It had as its objectives pled at many localities in the United States. Only a small pro- (1) to obtain information on the distribution, grade, 467945 59 2 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES and size of domestic deposits of beryllium in nonpeg- Beryllium has the lowest atomic weight of any element matite rocks, (2) to determine the types of rocks and that is crystalline at normal temperatures and, there­ mineral deposits most likely to contain beryllium, and fore, absorbs few X-rays; this makes it useful as win­ (3) to suggest favorable areas for prospecting. The dows on X-ray tubes. Because beryllium also has a low results of these investigations are set forth in this absorption cross section for neutrons, it is comparable report. to deuterium and graphite as a moderator and reflector During the early stages of the fieldwork, all types in atomic piles (Smyth, 1945, p. 62). of rocks and mineral deposits were regarded as poten­ Besides slowing neutrons without absorbing them, tial sources of beryllium, and materials of wide vari­ beryllium produces neutrons more easily than any ety were sampled and tested spectrographically. Spe­ other element, when excited with gamma or other radia­ cial attention was given to those types that were tion (Russell and others, 1948). The reaction is as thought to be most promising on the basis of earlier follows: investigations. Much of the material regarded as Be9+7>1.65 mev - Be8+n; beryllium bearing in this report is too low in grade to 10-w sec be commercial by present standards. However, the Be8 > 2 He2. consistent presence of beryllium in certain types of de­ It is used as a neutron source in laboratories and in neu­ posits, even though in very small amounts, seems to tron logging of wells. mark these for further study, and its consistent absence Beryllium imparts to its alloys lightness, hardness, in certain other types of material seems to exclude strength, and resistance to heat and corrosicn. When these. alloyed with aluminum, magnesium, and zinc, it forms a protective coating of beryllium oxide on the surface RECOVERY, PROPERTIES, AND USES OF BERYLLIUM of the metal. Beryllium-aluminuni alloys ha^e promise Beryllium was discovered in 1798 in beryl by L. N. in high strength-high temperature applications where Vanquelin, and in 1828 Wohler and Bussey succeeded lightness is important (Raynor, 1946) . Beryllium-cop­ in isolating the metal (Parsons, 1909, p. 77). Proc­ per, one of the most useful alloys of beryllium (Yar- esses for the preparation of beryllium, except on a lab­ ham, 1945; Williams, 1946), combines high electrical oratory scale, were not developed until late in the conductivity with high strength and is used extensively 1920's. Since then the price of the metal has decreased in current-carrying springs, in telephone equipment, and from $200 to an average of less than $100 per pound. in pressure gages, as well as in bushings, cams, and Beryllium metal is produced by the Beryllium Corpo­ sleeves. A beryllium-copper alloy with nonsparking ration of America at Reading, Pa., the Brush Beryl­ qualities is used in the explosive and petroleum indus­ lium Company of Cleveland, Ohio, and the Clifton tries where dangerous dust or vapor condition** exist. A Products Company of Painesville, Ohio. Details of beryllium-copper-cobalt alloy that combines high elec­ beryllium metallurgy are given by Kroll (1945) and trical conductivity with heat resistance ha^1 recently Kawecki (1946). become important in the manufacture of electrical Beryllium is a metallic element belonging to the alka­ equipment. line-earth family, which constitutes group 2 of the peri­ Because beryllium oxide melts at 2,570° C and is re­ odic table of Mendeleeff. It has many properties in sistant to corrosion, it has been used to some extent in common with other members of this group, which in­ crucibles and electric furnace parts. Beryllium nitrate cludes magnesium, calcium, strontium, barium, and added to thorium nitrate solution is used in the manu­ radium. It also closely resembles aluminum in chemi­ facture of gas mantles, to strengthen the oxid^ skeleton. cal behavior. Beryllium stearate is used in printing inks, beryllium Pure beryllium is rather brittle but can be hammered, nitride in making C13, and other beryllium salts are forged, rolled, and polished. It may be alloyed with used in pharmaceutical preparations. If be:ryl is sub­ many other elements, of which copper and aluminum stituted for feldspar in the manufacture of porcelain, are the two most commonly used. Its hardness, depend­ the product has high electrical resistance and low ther­ ing on the amount of impurities, ranges from 6 to 7 on mal expansion, properties that are necessary in airplane the Mohs scale. It is one of the lightest metals, the spark plugs. Emerald and aquamarine, transparent va­ specific gravity being 1.85, as compared to 1.75 for mag­ rieties of beryl, are highly valued as gem stones. nesium and 2.7 for aluminum. Other valuable prop­ PRODUCTION OF BERYLLIUM erties of the metal are a high modulus of elasticity, a low electrical conductivity as compared with common In mid-1956 the only known commercial source of metals, and a high resistance to heat and corrosion. beryllium is beryl, mined from granite pegmatites and INTRODUCTION recovered by hand sorting. In 1951 the world produc­ beryl than it has consumed, but current trends indicate tion of beryl concentrates totaled about 50,000 tons. that this surplus may be reduced in the future unless Nearly all of this amount was produced between 1930 domestic production is increased. and 1951 and more than two-thirds from 1940 to 1951. Known reserves of coarse beryl ore are small, and any Foreign production is chiefly in Brazil and Argentina, marked increase in supply must come from deposits of though India and Australia have at times contributed a milling type. The U. S. Bureau of Mines has experi­ substantial amounts. In the United States, the Black mented with methods of beneficiating low-grade Hryl Hills region of South Dakota is the main producing ore and results are encouraging (Lamb, 1947; Sneddon area. Beryl has been mined also in New England, Colo­ and Gibbs, 1947; Kennedy and O'Meara, 1948). Fatty- rado, Virginia, North Carolina, Arizona, and New acid reagents are used in a flotation process to sepr.rate Mexico. beryl from other minerals. High recovery has been The status of the United States with respect to beryl obtained from ores containing more th'an 0.35 percent supply is summarized diagrammatically in figure 1. BeO, and fair recovery from ores containing less than Domestic production and imports of beryl in relation that amount, some as little as 0.08 percent. Helvite re­ to world supply are shown for the period 1936-51. The sponds to similar treatment. Feldspar, mica, and cf,her dependence of the United States upon foreign sources is minerals may be recovered as coproducts. clearly indicated. Since 1940 the United States has Quantitative spectrographic analyses for beryllium produced and imported, on the average, somewhat more were made under contract to the U. S. Geological Sur-

7000-

6000-

World production

5000-

4000- cn z o

3000- I en

2000-

1000-

U.S. production

1936 1937 1938 1939 1940 1941 1942 1943 1944 1945 1946 1947 1948 1949 1950 1951 FIGURE 1. Production, imports, and consumption of beryl in the United States, and total world production. OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES vey by the Saratoga Laboratories, Inc., and the Strock studies indicated the presence of small amounts of Laboratories, Inc., of Saratoga Springs, N. Y., and by beryllium in English and German coals (1933). Earlier, the National Spectrographic Laboratories of Cleveland, Washington (1931) had pointed out the possibility Ohio; check samples were also analyzed by the Geo­ that beryllium had been overlooked in many chemical logical Survey. All semiquantitative spectrographic analyses of rocks, particularly nepheline syenites. and chemical analyses were made in the laboratories of Other studies were made by Tolmacev and Filippov the Geological Survey. (1934), Zilbermintz and Rusanov (1936), Szelenyi (1937), Oftedal (1939), Sahama (1945a), and Rankama ACKNOWLEDGMENTS (1946). In the United States Sandell and Goldich (1943) Without exception we found owners and operators studied the minor elements in igneous rocks, including of mining properties cooperative in making available the beryllium content of nine samples of granitic rocks. samples and geological information. The officials of During World War II the U. S. Geological Survey the American Smelting and Refining Co., Tucson, collected a large number of samples from mines and Ariz., the Coronado Copper and Zinc Co., Johnson, mills throughout the country, most of wlich were Ariz., and the New Jersey Zinc Co., Franklin, N. J., analyzed spectrographically for beryllium and other made available some of their own analyses for beryl­ rare elements (Kaiser and others, 1954). lium and other elements. L. H. Bauer of the New References to the occurrence of beryllium-bearing Jersey Zinc Company, James Gilluly of the U. S. minerals are numerous in geological literature. Beryl Geological Survey, D. M. Henderson of the University and phenakite have been reported from quartz veins of Illinois, F. A. Hildebrand of the University of at many localities throughout the world, and Hlvite has Chicago, V. C. Kelley of the University of New Mexico, been noted in several manganif erous veins and in con­ R. G. Knickerbocker of the U. S. Bureau of Mines, E. S. tact metamorphic deposits. Some idocrase ar i allanite Larsen, Jr., of Harvard University, M. D. Lyons of have been found to contain beryllium, and minor Beryl Ores Co., J. H. C. Martens of the New Jersey amounts have been reported in garnets, micas, and Bureau of Mineral Research, and officials of Climax many other minerals. Before the present work, the Molybdenum Co., the Anaconda Copper Mining Co., only nonpegmatite beryllium deposits in tl ^ United and the Utah Copper Co. generously supplied samples States that had been studied in detail were those at and specimens from localities that we were unable to Iron Mountain, N. Mex. (Jahns, 1944a, 1944b; Glass visit in the field. Messrs. D. M. Henderson, C. T. Gris- and others, 1944), where minerals of the heMte group wold of Albuquerque, N. Mex., and D. S. Tedford of occur rather abundantly in unusual tactite deposits. Columbus, N. Mex., were particularly helpful in sup­ Information concerning the occurrence of beryllium plying unpublished results of their geologic mapping. was summarized by Fleisclier and Cameron (1946), We are grateful to the University of Colorado, Cor­ who suggested that in addition to pegmatites; potential nell University, the University of Wisconsin, and the New Mexico Bureau of Mines and Mineral Resources sources of beryllium include contact-me^amorphic zones, alkalic intrusive rocks, coals, and bauxite de­ for the facilities lent us. posits. FIELD INVESTIGATIONS PRESENT WOBK SCOPE OF INVESTIGATIONS PREVIOUS WOBK With the aid of clues to the occurrence of beryllium Most information about the occurrence of beryllium in suggested by earlier investigations, a field program was rocks has come from geochemical studies of trace ele­ planned which would enable investigation of as many ments. The pioneer work on the geochemistry of beryl­ favorable areas as possible. Time did not permit lium was that of Goldschmidt and Peters (1932), who sampling of all the localities that were considered, but concluded from their spectrographic studies of many those sampled are sufficiently numerous and widespread rocks that the beryllium content of granites and sye­ to be considered representative. Fieldwork was done nites tends to be noticeably greater than that of olivine- during August-November 1948 and June-Peptember bearing and other mafic rocks, and that beryllium is 1949. A total of 23 man-months was spent in actual found commonly in the contact metamorphic products field work in connection with this program. of calcium-rich sedimentary rocks, notably in such In August 1948, alkalic intrusive rocks of Tertiary minerals as idocrase and axinite. They noted the ap­ age in western Texas and southern New Mexico were parent similarity of beryllium to aluminum in the proc­ investigated by Holser and Wilmarth. During Sep­ esses of weathering and sedimentation, and their later tember, October, and November, 1948, field ^ork was DETEEMINATION OF BEEYLLIUM continued in Colorado, Wyoming, Arkansas, and the Three general methods of sampling were employed. Tri-State lead-zinc region by Warner and Wilmarth. Grab sampling, which consists of gathering pieces of In the winter of 1948-49 samples collected in 1948 were material at random, was used at large mine dumps and analyzed for beryllium and studied mineralogically. mill tailings ponds. Channel sampling, which consists The results were used to plan fieldwork for 1949. of cutting continuous strips of rock along preferred The program was expanded in 1949 in order to in­ lines, was done mainly in mine openings. Because of vestigate areas in Nevada, California, Utah, Montana, the time consumed in this method, it was employed in and Arizona, as well as to continue activities in areas relatively few places. Chip sampling, in which chips previously studied, and three parties consisting of two are taken along preferred lines, was used in sampling men each were actively engaged in fieldwork. Holser large exposures. and W. I. Finch returned to western Texas for de­ In active mining districts, samples of the mill prod­ tailed mapping of two alkalic intrusive bodies, and ucts were obtained wherever possible, as well as sam­ investigated many localities in Arizona and New Mex­ ples of ore and waste rock from the operating mines. ico, spending 2 months in the field. Work in Colo­ At abandoned mines, an attempt was made to obtain rado and Wyoming was carried on during July and representative samples of the different types of material August by Wilmarth and P. L. Cloke. Cameron and observed on the dumps. An effort was made ir sam­ J. H. Macleod spent 6 weeks investigating a number pling rock types to include all significant varieties noted of mining districts in Nevada, California, and Utah. in the field. Many hand specimens of rocks and min­ The fieldwork was concluded by Warner and Wilmarth erals were collected for laboratory study in event the who investigated several mining districts in central bulk samples proved to contain beryllium. Montana and near Salt Lake City, Utah, in Septem­ The field program was designed to obtain informa­ ber 1949. Several localities in New England were tion concerning the beryllium content of a variety of visited by Holser in May 1950. During the winter of rocks and mineral deposits throughout the United 1949-50 analytical and mineralogical work was con­ States in the shortest possible time. The amount of tinued, and compilation of results begun. time that could be devoted to detailed geologic mapping

FIEIiP METHODS was therefore small. For the most part, when geologic maps were not available for areas where samples were In planning the field program, a choice had to be obtained, sketch maps were made showing the mor* pro­ made between sampling a few localities in great detail nounced geologic and cultural features. Topography or a larger number of areas somewhat superficially; and geology of areas at Wind Mountain in the Cornu- the latter alternative was chosen. This imposed many das Mountains, Otero County, N. Mex., and Cave Peak difficulties in obtaining representative samples. Some in the Sierra Diablo, Culberson County, Tex., were of the deposits selected for sampling are large and ex­ mapped in detail by planetable. tremely variable. Literally hundreds of samples might be needed at each deposit to obtain a reliable estimate DETERMINATION OF BERYLLIUM of the beryllium content. Many of the localities visited are so isolated that only a few samples could be removed SPECTKOGKAPHIC ANALYSIS conveniently. In deposits consisting of alternating lay­ ers of many types of material, a composite sample of The spectrographic method appears to be the most the whole would be of little value in determining the reliable for quantitative determination of small beryllium-bearing type; yet sampling each layer indi­ amounts of beryllium in rocks and minerals. A gen­ vidually requires much time and care. It is doubtful eral discussion of the method is given by Peer (1943), that beryllium-bearing minerals are evenly distributed and the application of the method to ore samples has through the containing rock masses. A sample taken been investigated by Marks and Jones (1948). The at a point where the concentration of such minerals is lower limit of accurate spectrographic determinations relatively high might indicate a potential ore body, is in the range 0.005 to 0.0001 percent BeO. The equip­ whereas one taken a short distance away might contain ment required is expensive and complicated, and trained no beryllium even though the differences between the two materials might not be distinguishable in the field. technicians are needed to interpret the results. Sp°ctro- Both would give an erroneous impression of the average graphic analyses of samples collected in the present in­ contents. For these reasons, many of the samples that vestigation were made in part by the Geological Survey were analyzed probably were not truly representative, laboratories, and in part by the National Spectro­ and future sampling in the same localities may give sig­ graphic Laboratories, Cleveland, Ohio, and Stroclr Lab­ nificantly different results. oratories, Inc., Saratoga Springs, N. Y. 6 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES GRAVIMETRIC AND VOLUMETRIC ANALYSIS fluorescent compounds in solution. Many of the reac­ tions are very sensitive and thus applicable to analysis Beryllium as a trace constituent in rocks and min­ for beryllium. A comprehensive treatment of the sub­ erals cannot be determined quantitatively by gravimetric ject is given by Sandell (1944). Several metals, includ­ or volumetric methods of analysis, as the lower limit ing zinc, lithium, the rare earths, thorium, and calcium, for BeO of these methods is approximately 0.01 per­ react with certain of the reagents commonly employed cent. Beryllium will generally be precipitated with in colorimetric tests for beryllium. Other elements such aluminum unless special precautions are taken, and in as iron, magnesium, manganese, and alumirum form many analyses it has been calculated with that metal. flocculent hydroxides that cloud the solution and ab­ The problem of separating beryllium and aluminum has sorb beryllium and the color reagent. Procedures for been a challenge to analytical chemists for many years, dealing with interfering ions differ according to the as is indicated by the extensive literature on the sub­ method of analysis employed, but in general they may ject. Special techniques must be employed also in the either be eliminated from the solution or rendered harm­ removal of iron, lest some beryllium be lost in the proc­ less by adding appropriate reagents. Special methods ess. Any quantitative separation of beryllium should for removal of iron from the test solution hav*. been de­ be verified by spectrographic analysis of residues. scribed by Hillebrand and Lundell (1929, p. 110-111) A gravimetric method for determining beryllium in and Sandell (1949, p. 93). rocks and minerals containing a few hundreds of 1 per­ The two types of color reagent that have been most cent of the metal was developed by Stevens and Carron used in beryllium determination are morin and the (1946). The new method separates beryllium from anthraquinones. Of the latter, quinizarin (1-4-dihy- aluminum by a sodium carbonate fusion of their phos­ droxyanthraquinone) and quinalizarin (1-2-5-8-tetra- phates and leaching with water. Various methods for hydroxyanthraquinone) are the most popular. Quini- removal of iron were studied, and the cupferron method zarin-2-sulfonic acid (l-4-dihydroxyanthracuinone-2- was found to be most satisfactory. sulfonic acid) has also been used (Cucci and others, 1949). Quantitative methods for each of the reagents COLORIMETRIC AND FLUORIMETRIC ANALYSIS have been rather carefully worked out. Comparative Colorimetric analysis is based on the reactions of cer­ characteristics of the methods are shown in tr.ble 1 and tain elements with dye reagents to produce colored or detailed procedures are given in the publications cited.

TABLE 1. Comparison of quinalizarin, quinizarin, and morin methods for determination of beryllium in rocks and minerals Quinalizarin Quinizarin Morin Visual reaction _____ Blue lake______Red fluorescent solution ______Yellow-green fluorescent solution. Light conditions _ _ _ _ Daylight ______Ultraviolet (3,650 A) ______Ultraviolet or sunlight. pH condition...._ -0.5N NaOH______-0.3N NaOH (pH 11.5)____:_ 0.01 to 0.1N NaOH. Sensitivity 1...-.--- 0.5 ppm Be______0.05 ppm Be______-_____ 0.001 ppm Be. Interfering ions_____ Zn, Mg, Zr, Th, rare earths______Li______-______-______Li, Ca, Zn, Sc. Remarks______Least sensitive, best at high pH__ Most specific, color stable, tested Most sensitive, least specific, worst on all ores. at high pH, color fade?, tested on all rocks. References______Sandell, 1944, p. 153-154; Feigl, Rienacker, 1932; White and Lowe, Sandell, 1944, p. 152-J53; 1940a, 1939, p. 119-121; Fischer, 1928. 1941; Fletcher, White, and 1940b, 1949. Sheftel, 1946; Zermatten, 1933; Fletcher and White, 1946; Underwood and others, 1947.8 1 Stated In terms of minimum parts per million Be in test solution. 2 Underwood, A. L., Neuman, W. F., and Carlson, A. B.f 1947, Determination of small amounts of beryllium by fluorescence measurement: 17. S. Atomic Energy Oomm., MDDC 941,17 p. The morin reaction is the most sensitive of the three therefore it is probably of greater use in testing of ores tests and, unlike other fluorescent methods, the fluores­ and all types of rocks than are other reagents. The cence may be observed in daylight. A disadvantage quinalizarin test, like most other colorimetric methods, is the large number of interfering ions that must be is of much lower sensitivity than fluorimetric reactions. eliminated. Though apparently suitable for rocks, this However, only simple laboratory equipment ir required method may have application in testing ores. Quini­ in the procedure and most interfering ions may be elim­ zarin gives a less sensitive fluorescent test than morin inated without difficulty. and requires the use of an ultraviolet lamp. Its chief Several other reagents have been found to give color advantage is that few ions interfere with the test, and reactions with beryllium but have not been adapted for DETERMINATION OF BERYLLIUM trace analysis of rocks and minerals (Kolthoff, 1928; EnBLVITE GROUP Feigl, 1939, p. 121; Kulcsar, 1943; Aldridge and Lid- In some districts, such as the Victorio Mountains and dell, 1948; Underwood and Neuman, 1949; Kassel and Carpenter districts, New Mexico, the Silverton district, Neuman, 1950). Most of the reagents used in colori- Colorado, the Butte district, Montana, and the Rock- metric and fluorimetric analysis for beryllium may also port area, Massachusetts, minerals of the helvite group be used in making qualitative spot tests. Reasonable commonly may be recognized by their crystal form precautions must be observed, even in qualitative work, and color. In the Iron Mountain district, New Mexico, in ridding the test solutions of ions which may interfere and at places in some of the other districts just men­ with the results, and quantitative determinations may tioned, helvite is easily confused with garnet cf the be carried out with slightly more effort. same shade of yellow or red. Some danalite and garnet in the Iron Mountain district were so intimately inter- MINEBAZ.OGIC METHODS grown that identification was especially difficult (Jahns, 1944a, p. 57-58). A stain test developed by Beryllium, in rocks may be determined by finding Gruner (1944) has proved useful if helvite is admixed the amounts of beryllium minerals present and their with garnet. beryllium contents. Commonly the BeO content of the The proportion of helvite is determined by methods mineral or minerals is determined by one of the meth­ similar to those used for beryl. If the gangue is gf met, ods discussed above, though optical determinations are the volume proportions nearly equal the weight propor­ possible for some species. For accurate results the tions. The theoretical BeO content of helvite ranges average of several determinations must be taken. Min­ only from 12.5 to 13.5 percent (Glass and others, 1944, eral percentages by volume are determined by petro- p. 182). In the absence of a chemical analysis, a value graphic methods. Techniques employed with the more of 12.8 ±0.9 percent BeO may be assumed. More than common beryllium minerals are discussed below. one mineral of the helvite group may be found in the BERYL. same deposit,1 and this possibility must be considered in evaluating the beryllium content. Beryl crystals, if large, generally may be recognized Mineralogical calculation of beryllium has bee^ ap­ by their crystal form, hardness, and color; some beryl, plied by Glass (Jahns, 1944a, p. 63, 77) to the Iron however, is white and easily confused with quartz or Mountain helvite deposit. feldspar. Beryl in small crystals or fragments in a ground sample may be recognized microscopically, but OTHER MINERALS identification is not always certain, for quartz and Other beryllium minerals have not been found in apatite have similar optical properties and crystal form. sufficient quantity to make their quantitative deter­ Once beryl has been recognized, its proportion in the mination important. Beryllium-bearing mineralr such rock may be found by one of the ordinary methods as idocrase, garnet, axinite, aegirite, and nepl 'vline of volume, area, line, point, or grain counting, subject have a content of beryllium that ranges from more to the statistical restrictions of the method employed than 3 percent BeO to below the limit of detection. (Krumbein and Petti John, 1938, p. 465-^89). Because Correlation between physical properties and beryllium the specific gravity of beryl is about that of its usual content is uncertain for these minerals, and no data gangue, quartz, its volume proportion is approximately have been gathered on their probable ranges of Hryl- equal to its weight proportion. lium content within a given deposit or rock type. The beryllia content of beryl ranges from 10 to 14 The two minerals of highest extraneous beryllium percent, varying inversely with the alkali content. The content are allanite and idocrase, both of which con­ alkali content of the beryl may be determined by meas­ tain such a diversity of elements that correlation of uring the ordinary refractive index by the immersion physical properties with beryllium content is extrrnely method and referring to an empirical curve (Winchell, difficult. Gadeke (1938) has achieved some success in 1951, p. 464). In pegmatites the beryllium content of correlating the optical properties of idocrase with its beryl may vary within a single pegmatite, or even highly variable composition. However, some half- within a single unit (Cameron and others, 1949, p. 69). dozen types of isomorphous substitution were found to No such variation has yet been discovered in veins, have a marked effect on the optical properties, rnd a but relatively few analyses of vein beryl are available. reliable criterion for determining the presence cf be­ Mineralogical calculation of beryllium in beryl de­ ryllium seems improbable. If either idocrase ci? al- posits has so far been applied only to pegmatites (Han- * Iron Mountain, N. Mex. (Jahns, 1944a, p. 56-58) ; Bartlett, N. H. (Glass and others, 1944, p. 185) ; and Cornwall, England (Mlers and ley and others, 1950, p. 12). Prior, 1892, p. 11). 8 OCCURRENCE OF NONPEGMATTTE BERYLLIUM IN THE UNITED STATES lanite occurs in a deposit containing helvite or beryl, there are several disadvantages. Initial expense would it may be expected to be beryllium-bearing. In each be moderate but operating expense would include the of the three helvite deposits where idocrase has been maintenance of a supply of Sb124, which hrs a rather found and analyzed, it contained at least 0.2 percent short half-life. Safety and waste-disposal of the source BeO. In such deposits a mineral count of beryl or required to detect small amounts of BeO would be helvite will give a BeO content below the true value. problems. A mineral count of all the recognizable beryllium MINERALOGY OP BERYLLIUM minerals may miss a substantial quantity of beryllium occurring in fine-grained or unknown species. This CRYSTAL CHEMISTRY OF BERYLLIUM MTKrERALS was the experience of Glass and Lemke with the Iron Most beryllium minerals are silicates, many of which Mountain, N. Mex., tactite (Jahns, 1944a, p. 77-78), are structurally complex. The commonly associated ele­ and of Holser with the Victorio Mountains, N. Mex., ments are aluminum and the metals of the alkali and tactite during the present investigation. However, the alkaline-earth groups, together with fluorine, water, and beryllium content determined from beryl or helvite the hydroxyl ion. With few exceptions, iron and mag­ counts could be of more economic significance than that nesium are rare constituents. Other mineral groups, in­ given by chemical or spectrographic methods if the cluding oxides, carbonates, phosphates, and borates, are trace quantities of beryllium in the minerals associated sparsely represented, but sulfides, halides, r,nd related with the beryl or helvite were not recoverable. compounds are notably lacking. The tendency for beryllium to affiliate itself with the silicates and oxygen RADIOMETRIC METHODS salts in preference to the sulfides and halider is best ex­ Beryllium is an efficient producer of neutrons when plained by the marked difference in crystal chemistry excited by high-energy gamma radiation. It shares of these compounds. Full treatment of this subject is this property with H2 and several other atoms, but beyond the scope of this report. However, the prin­ the energy threshold for the beryllium reaction happens ciples involved are thought to have an important bear­ to be lower than for any other element. The reaction ing upon the nature and occurrence of beryllium min­ was experimentally applied to the mechanical sorting erals and thus to merit the following brief discussion. of beryl (Gaudin and others, 1950), and the data ob­ Beryllium has a relatively small ionic radius, is tained in these experiments allow a preliminary calcu­ strongly electropositive, and is found only in tetra- lation of the sensitivity of the reaction for the assay of hedral coordination in crystal structures. As a result beryllium in rocks. of these properties, it favors combination rith anions The gamma-ray sources used in the published experi­ that are not easily polarized, forming crystal bonds of ments were a Van de Graaf generator and radium the ionic or semi-ionic type. Stable combinations of (Gaudin and others, 1950, p. 496). The recently avail­ beryllium with sulfur, which is readily polarized, are able artificially radioactive antimony may be more de­ not to be expected. Similarly, chlorine, bromine, and sirable for field determination of beryllium, despite its iodine form structures which, except for the alkali chlo­ short half-life. It decays according to the following rides, tend to approximate the sulfide type and are not equation: likely to contain beryllium. Fluorine vigorously resists Sb124 -» Te124-f&. 4 i.7 Mev polarization but, because of its large ionic size does not favor tetrahedral coordination with beryllium. The The gamma radiation is of sufficient energy to excite most stable combination of beryllium is with oxygen, beryllium, giving 2.105 neutrons per curie per gram of which is not readily polarized and, which, though com­ beryllium at 1 cm. (Russell and others, 1948). Sb124 parable in size to fluorine, will permit bonds of semi- possesses an advantage over Ra226 in the analysis of nat­ ionic type involving some electron sharing. Such bonds ural materials, because it gives only a very small num­ result in relatively close packing of four cxygen ions ber of neutrons from H2. The neutrons may be slowed around the small beryllium ion and permit the required in a moderator, such as paraffin, and detected by stand­ spacing of beryllium ions in the structure. The oxide, ard procedures. Preliminary calculations, including al­ bromellite, though rare, is thus a stable mineral com­ lowance for efficiency and background, indicate a limit pound. of detection of O.OOX (percent BeO times curies of The silicate minerals are most favorable for beryl­ Sb124). lium occurrence. The complex structural arrangement This method has some promise for semiportable field and chemical composition of these minerals give greater equipment, as it would be highly specific, independent opportunity for meeting the four-fold coordination re­ of the state of beryllium, fast, and simple. However, quirement of beryllium. Even here many combinations MINERALOGY OF BERYLLIUM 9 which fit the ordinary laws of valency are structurally the interchange of ions is subject to the condition that incompatible. Whereas beryllium is known only in the positive and negative charges must balance. tetrahedral coordination in oxyminerals, aluminum, Excess charges may be balanced by adding ions to the iron, magnesium, and other elements are capable of structure. Such complex substitutions are well known either four-fold or six-fold coordination. Such ele­ in amphiboles, micas, and clay minerals. As an ex­ ments therefore have a considerable advantage over ample, Rankama and Sahama (1950, p. 126) theorize beryllium in meeting structural requirements in silicate that the small content of lanthanum sometimes f ^esent minerals. Even if beryllium were present in concentra­ in'potassium feldspar is a result of the substitution of tion equal to that of these elements, a condition which La3+ for K+ simultaneously with Be2+ for Si4*. Not only is rare in nature, it would be at a loss in competing with must the combined charges of the substituting ionr bring them for positions in crystal lattices. about electrical neutrality in the structure but their Though oxysalts of beryllium occur as minerals, they sizes and coordination numbers must be such that they are not common. In the oxyradicals, oxygen atoms are will fit into the spaces provided by the ions replaced. closely grouped around small atoms such as carbon, ni­ The difficulty of finding proper combinations is im­ trogen, and phosphorus; and bonds within the radicals measurably increased when the disparity of valences is are mainly covalent. Because the bonds between beryl­ greater, so despite the greater difference in ionic size, lium and oxygen are mainly ionic, the beryllate radical Be2+ is more likely to substitute for Si4* than for S6+, is unstable in nature and not found in minerals. Bonds Cr6*, or P5+. between beryllium ions and the large oxyradicals are Presumably beryllium ions or atoms may fill inter­ of a weak ionic type and the resulting beryllium nitrate, stices of proper size in certain crystal lattices without carbonate, and phosphate also have poor stability under actually substituting for other ions. In this connection natural conditions. the small ionic radius for beryllium would seem a dis­ In the presence of water, especially at low tempera­ tinct advantage. However, the difficulties inherent in tures, hydrogen has considerable influence on the rela­ isomorphous substitution would not be entirely obviated tions of beryllium and oxygen. The hydroxyl ion is in this process, and it is doubtful that significant deformed by the charge of the beryllium ion and, ac­ amounts of beryllium could be thus accommodated ex­ cording to the theory developed by Wickman (1944), cept in minerals where vacant oxygen tetrahedra exist,, the resulting deformation may allow formation of hy­ as in idocrase. droxyl bonds and precipitation of beryllium hydroxide. On the whole, isomorphism does not promise to pro­ This is thought to be of considerable importance in the vide minerals of even moderately high beryllium con­ occurrence of beryllium in sedimentary rocks. tent except under special conditions. Undoubtedly it Many minerals contain beryllium in solid solution, is a means by which much beryllium is dissipated r,mong though rarely in significant amounts. That ionic size, silicate minerals as a trace constituent. rather than valency, is the controlling factor in isomor- Throughout the foregoing discussion the matter of phous substitution is now commonly accepted. Thus ion concentration, or availability, has been largely ne­ beryllium may replace ions or atoms of comparable size glected. As pointed out by Osborn (1950), tin, con­ in crystal structures but is not likely to replace those of centration of a given element in a particular geologic substantially different ionic radius. Because of the dis­ environment has much to do with the amount cf that crepancy in ionic size, the substitution of beryllium element contained in the minerals that form. In the for most of the more common metals is not to be ex­ early stages of basaltic magma crystallization the con­ pected in appreciable amount. The best possibilities centration of beryllium is low, and it is not a serious for substitution are with ions such as Cr6*, P5+, S6*, and competitor to the more common cations which are more Si4+, which are of about the same size as Be2+. Not readily incorporated into the structures of the ferro- only are these ions, except that of silicon, compara­ magnesian silicates and plagioclase. It thus tends to tively rare, but all have valences ranging from four to be concentrated in the late magmatic residue where op­ portunities for the formation of minerals in which six, whereas the valence of beryllium is only two. beryllium is a necessary constituent reach their maxi­ Other ions of some of these elements have lower val­ mum. Silicate minerals that form during the late mag­ ences, but their radii are considerably larger than that matic and early hydrothermal stages of igneous activity of the beryllium ion. Although difference in valence probably remove most of the beryllium. Sulfur, the does not prohibit substitution, the ions of higher charge oxyradicals, and to some extent the halogens tend to be will in general be somewhat more stable in the struc­ concentrated in later hydrothermal fluids and combine ture than beryllium (Goldschmidt, 1934, p. 385); also with metals to form the common ore and gangue min- 10 OCCURRENCE OF NONPEGMATITE BERYLLIUM EST THE UNITED STATES erals. Not only are the structures of these minerals un­ physical and chemical conditions in nature, i? not ade­ favorable to beryllium occurrence, but the concentration quate to explain these rare occurrences. Beryl, helvite, of beryllium in the ore fluid probably is low, most of bertrandite, chrysoberyl, and phenakite are not only it having gone into previously formed minerals. Pauc­ the most common minerals of beryllium, but actually ac­ ity of beryllium in ore deposits that formed at moderate count for nearly all mineralogical occurrences as well or low temperature is, therefore, to be expected. as all probable ores of beryllium. All can occur in de­ Theoretical considerations thus indicate that, because posits other than pegmatites. of the peculiar structural and chemical properties of The chrysoberyl (BeAl2O4) structure is similar to beryllium, minerals in which beryllium is a necessary that of fayalite and has been described by Bragg and constituent are few. These minerals are most likely to Brown (1926). Although the possibility of isomorphic occur in rocks believed to have formed during the tran­ variation in the aluminum or beryllium content is sug­ sition from magmatic to hydrothermal activity. The gested by artificial melt studies (Geller and others, 1946, number of potential beryllium ore minerals is, there­ p. 289), the only variation found in natural cl rysoberyl fore, not large and their geologic environments are has been the substitution of small amounts of ferric iron restricted. These principles, though not without ex­ for aluminum, and ferrous iron for beryllium (Palache ception, are in accord with, and tend to substantiate, and others, 1944, v. 1, p. 719). Chrysoberyl occurs in conclusions previously drawn from field observations. some pegmatites and in at least one it constitutes beryl­ BERYLLIUM AS AN ESSENTIAL CONSTITUENT IN lium ore (Hanley and others, 1950, p. 103). It is found MINERALS also in aluminous schists commonly associated with peg­ Minerals in which beryllium is an essential constituent matites, as in the Ural Mountains (Fersman, 1929, p. are described in table 2. Although the list is an im­ 94) and in New York (Palache and others, 1944, v. 1, posing one, many of these minerals are rare, and some p. 721). None was found during the present investiga­ are found in only one or two localities. Knowledge of tion.

TABLE 2. Minerals in which beryllium is an essential constituent [Key to abbreviations: isom. isometric; tetr. tetragonal; hex. hexagonal; trig. trigonal; orth. orthorhombic; mono. monoclinie; H hardness Moh scale; G specific gravity; F fusibility; Cl cleavage form; N index of refraction; N0 index of refraction for the ordinary ray; Ne index of refraction for the extraordinary ray; Ns index of refraction for the intermediate ray; B birefringence; 2V optic axial angle] Mineral Chemical competition Percent BeO Description Occurrence Aminoffite _ _ _ Ca8Be3Al(OH) 3Si8028- 4H2O_ 6.2 Tetr., pyramidal; vitreous; color­ Pyrometasomatic, with mag­ less; H, 5.5; G, 2.9; No, 1.64; Ne, netite; very rare. 1.637; B, 0.010. Barylite_. BaBe_Si2O7______15. 4-15. 8 Orth., platy; greasy; white; insol­ Pyrometasomatic, New Jer­ uble; Cl, 001, 100; H, 6-7; G, 4.0; sey; very rare. F, 7; Ny, 1.68-1.70; B, 0.013; ( + )2V, 65° to ( )2V, 65°. Bavenite_____ Ca4BeAl2Si9O28.H2O______3.0- 7.7 Orth., fibrous, prismatic; white; H, Granitic pegmatite, Italy; 5.5; G, 2.7; Ny, 1.58-1.59; B, very rare. 0.004-0.0007; (-)2V, 47°. Bertrandite____ Be4Si2O7(OH)2______39.6-42.6 Orth., tabular, prismatic; vitreous; Granitic pegmatite and feld- colorless, yellow; insoluble; Cl, spathie veins; widely dis­ 001, 110, 100; H, 6; G, 2.6; F, 7; tributed in small amounts. Ny, 1.61; B, 0.023; ( + )2V, 74°. BeryL Be3Al2(SiO3)6 ____----- 10. 0-14. 0 Hex., prismatic (vert, striae), vit­ Granitic pegmatite, high reous; green (rarely white, pink, temperature veins; widely g?Uow); insoluble; Cl, 001 (poor); distributed. Alters to kao- , 7.5-8; G, 2.6-2.8; N0, 1.57- linite. 1.60; Ne, 1.56-1.59; B, 0.004-0.008. BeryUonite___ NaBePO4_ 19.8 Orth., short prismatic; vitreous; Granitic pegmatite, Maine ; colorless, white, yellow; soluble; rare. Cl, 001, 100; H, 5.5-6; G, 2.8; F, 5; Ny, 1.56; B, 0.01; (-)2V, 67°. Bityite._____ Ca4(Li,Be)4Al8 - 2. 3- 8. 1 Pseudohex., minute r>lates; white; Granitic pegmatite, Mada­ [(Si,Al)4010]3(OH)20. insoluble; Cl, 001; H, 5.5; G, 3.0; gascar; rare. F, easy; Ny, 1.63; B, 0.02; ( )2V, small. Bromellite___ BeO. 100.0 Hex., prismatic; white; insoluble; Pyromstasomatic, Sweden; Cl, 1010; H, 9; G, 3.0; N0, 1.72; very rare. Ne, 1.73. Chkalo vite___ NaBeSi2O0 12.7 Orth., colorless; H 6; G, 2.7; soluble; Syenitic pegmatite, U.S.S.R; Cl; Ny, 1.55; (+) 2V, 78°. very rare. Chrysoberyl.___ BeAl_O4 ______16. 9-19. 7 Orth., tabular, twinned crystals; Granitic pegmatite, schist, vitreous; green, yellow, brown, placers; uncommon. red; Cl, 110; H, 8-9; G; 3.7; F, 7; Ny, 1.75; B, 0.009; 2V, variable. MINERALOGY OF BERYLLIUM 11

TABLE 2. Minerals in which beryllium is an essential constituent Continued Key to abbreviations: isom. isometric; tetr. tetragonal; hex. hexagonal; trig. trigonal; orth. orthorhombic; mono. monoclinic; H hardness Moh scale; Q~speciflo gravity; F fusibility; Cl cleavage form; N index of refraction; N0 index of refraction for the ordinary ray; N« index of refraction for the extraordinary ray; N» index of refraction for the intermediate ray; B birefringence; 2V optic axial angle] Mineral Chemical composition Percent BeO Description Occurrence f* Epididymite___ HNaBeSi3O8______10.6 Orth., basal plates-; vitreous; white; Syenitic pegmatite, Green- nearly insoluble; Cl, 001 and 010; land; rare. H, 5.5; G, 2.6; F, 3; Ny, 1.54; B, 0.002; (+) 2V, 23°. Euclase_____ BeAlSiO4(OH). 16. 9 Mono., prismatis; vitreous; color­ Granitic pegmatite, "chlorite less, green, blue, white; insoluble; schists, placers; rare. Cl, 010; H, 7.5; G, 3.0-4.0; F, 5.5; Ny, 1.655; B, 0.02; (+) 2V, 50°. Eudidymite__ HNaBeSi3O8.______10.6-11.1 Mono., basal plates; vitreous; white; Zircon syenitic pegmatite, nearly insoluble; Cl, 001; H, 6; Norway; rare. G, 2.5; F, 3; Ny, 1.55; B, 0.006; (+) 2V, 30°. Gadolinite ___ Be2Y2FeSi2Oio- 5. 5-13. 2 Mono., prismatic; vitreous; black, Granitic pegmatite, gener- greenish, brown; gels HC1; Cl, ally with fluorite; rncom- none; H, 7; G, 4.0-4.6; Ny, 1.78; mon. B, 0.01; (+), 2V, 85°. Hambergite._ Be2(OH)BO3 36.7 Orth., prismatic; vitreous; gray- Granitic and syenitic pegma- white; insoluble except in HF; tites, Norway and Mada- Cl, 010 and 100; H, 7.5; G, 2.3; gascar; very rare. F, 7; Ny, 1.59; B, 0.074; (+) 2V, 87°. Harstigite___ (Ca,Mn) 7Be4(Si2O7) 3(OH,F)4~ 11.2 Orth.,. \MUfj shortOAJ.UJ. V prismatic;jJi A£)JJJ.-*_J1X/ y vitreous;V -LUJ.OUU.C3j Pyrometasomatic,J. J J. \J JJLJ.U \JOHJ\J J. Sweden; colorless; soluble in HC1 after ig- very rare, nition; Cl, none; H, 5.5; G, 3; Ny, 1.68; B, 0.005; (+) 2V, 526. HELVITE GROUP Helvite. 10.5-15.0 Isom., tetrahedrons, spherical masses; Pyrometasomatic deposits; vitreous to resinous; yellow, red, rhodonite veins, granitic brown; gels in HC1; Cl, 111 (poor); and syenitic pegrratites; H, 6; G, 3.2-3.4; F, 3; N, 1.73-1.75. uncommon. Danalite____ Fe^BesSisO^.S..--..-____ 12.7-13.8 Isom., octahedrons, massive; red, Granitic pegmatite, pyro- brown; H, 6; G, 3.3-3.5; F, 3; metasomatic deposits; N, 1.75-1.77. rare. Genthelvite___. Zri4Be3Si3Oi2.S___ 12. 6 Isom., rose red, brown; H, 6; G, 3.6; Pegmatite, Colorado; very N, 1.75. rare. Herderite_____. CaBePOi(OH,F) 15. 0-15. 8 Mono., prismatic; vitreous; yellow­ Pegmatites, Maine; very ish to greenish: soluble in acid; rare. Cl, 110 (poor); H, 5; G, 3.0; F, diffi­ cult; Ny, 1.61; B, 0.029; (-)2V, 74°. Kolbeckite(?) Hydrous Be, Ca, Al, Si phos­ 8.7 Mono., short prisms; blue to gray; Quartz- wolframite vein, Ger- phate, poorly defined. Cl, 010; H, 3.5-4.0; G, 2.4. many; very rare. Leucophanite (Ca,Na)2Be Si_(O,OH,F) 7__ 10. 0-12. 4 Orth., basal plates, massive, col­ Syenite pegmatite, Norway; umnar; vitreous; white, green, very rare. yeyellow; insoluble; Cl, 001, 010; H[, 4; G, 3; F, 6; Ny, 1.59; B, 0.027; (-)2V, 39°. Meliphanite__ (Ca, Na)2Be(Si, A1)2(O, F)7_ 9.8-14.0 Tetr., obtuse pyramidal or platy; Syenite pegmatites, Norway; vitreous; yellow to reddish; insol­ very rare. uble; Cl, 001; H, 5-5.5; G, 3; fuses with intumescence; N0, 1.61; Ne, 1.59. Milarite 5.0 Hex., prismatic; vitreous; pale green, Granite, Switzerland; very colorless; insoluble; no cleavage; rare. H, 5.5-6; G, 2.6; F, 3; N0, Ne, 1.53; B, 0.001-0.003. Phenakite 44. 0-45. 6 Trig., rhombohedral or prismatic; Granitic pegmatites, high vitreous; colorless, yellow, rose, temperature veins; rare. brown; insoluble; Cl, 1120; H, 7.5-8; G, 3.0; F, 7; N0, 1.654; Ne, 1.670. Rhodizite (Na, K)2Li4Al4Be3B10O27(?) - _ _ 9. 0-15. 1 Isom., dodecahedrons; translucent; Pegmatite, U.S.S.R., Mada­ white or yellow; insoluble; Cl, 111 gascar; very rare. (poor); H, 8; G, 3.4; F, 7; N, 1.69. Swedenborgite NaBeiSbO? ______35. 3 Hex., short prismatic; colorless; yel­ Pyrometasomatic deposit, low; insoluble; Cl, 0001; H, 8; G, Sweden; very rare. 4.3; N-, 1.77, Ne, 1.77; B, 0.002. Tengerite. _ , _ _ Hydrous Y, Ca, Be carbonate _ 9. 8 Fibrous, powdery; dull; white; sol­ Granitic pegmatite as alter­ uble with effervescence; G, 3.1; ation product of gadoli- Ny, 1.57-1.63;B, 0.02-0.03; (-)2V, nite, Texas; very rare. large. Trimerite 17. 1 Mono., tubular prisms; pink; soluble Pyrometasomatic, Sweden; in HC1; Cl, 0001; H, 6-7; G, 3.5; very rare. F, 6; Ny, 1.72; B, 0.01; (-)2V, 83°. 12 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES The phenakite (Be2SiO4) structure according to Beryl is the most common beryllium mineral in beryl­ Bragg and Zachariasen (1930) consists of linked tetra- lium-bearing veins. The vein occurrences are tabulated hedra with silicon and beryllium at their centers. The and discussed by Holser (1953, p. 604) and by Adams structure is similar to that of willemite and a small (1953, p. 114-117). Beryl also occurs less commonly as amount of willemite is needed as a seeding agent in pro­ an accessory mineral in granitic rocks and in schists, ducing synthetic phenakite (Morgan and Hummel, generally associated with pegmatites. The known oc­ 1949, p. 252). Phenakite occurs in small quantities in currences in nonpegmatite rocks of the United States pegmatites, but rarely is found in those containing are discussed in this report. chrysoberyl. It is an associate of beryl in a few granites Helvite and its isomorph ((Mn, Fe, Zn) 4Be3Si3Oi2S) containing segregations of aplite and occurs rarely in have a three-dimensional framework of oxygen tetra- beryl-bearing quartz veins. None was discovered in the hedra similar to that of sodalite. Beryllium occupies current investigation, but it has previously been de­ the position normally given to aluminum in such struc­ scribed from veins at Irish Creek, Va. (Koschmann and tures, and this allows the presence of the divalent others, 1942, p. 281-282) and Mount Antero, Colo. metals in place of sodium (Barth, 1926, p. 4C). (Switzer, 1939, p. 789). The chemical composition and physical properties of Beryl (Be3Al2 (SiO3 )6) is uncommon among silicates the helvite group are summarized by Glass, Jahns, and as an example of a sixfold ring structure of four-co­ Stevens (1944), who list many helvite localities. In ordinated silica groups (Bragg and West, 1926). The addition to the pegmatite occurrences at Amelia, Va., groups are tied together by beryllium in four-coordina­ Cheyenne Canyon, Colo., Eockport, Mass., Langesund- tion and aluminum in six-coordination. fiord, Norway, Miass, U. S. S. E., and Mount Francisco, Beryl is variable in composition, ranging from 10 to western Australia, helvite has been found in pegmatites 14 percent BeO (the formula content is 14 percent). at Eincon, Calif. (Murdoch and Webb, 1948. p. 170), Alkalies and alkaline earths, principally sodium, con­ Walrus Island, Northwest Territory, Canada (Hoff- stitute as much as 4 percent of many beryls, and con­ man, 1901, p. 15), and Ipe', Minas Gerais, Brr.zil (writ­ stitutional water may amount to 2.7 percent. The de­ ten communication, E. E. Swoboda). In corrmon with crease of beryllium content might be structurally cor­ phenakite and beryl, minerals of the helvite group are related with either the addition of an alkali atom to the found rarely in small rather fine-grained segregations empty position in the center of each silicate ring, or in granite (Fischer, 1942). Most helvite occurs in veins with the substitution of hydroxyl for oxygen in part and pyrometasomatic deposits. Occurrences in the of the ring itself. Both systems have been found in United States are described in detail in this report. other silicates; 2 sufficient analyses are not yet available to determine which is more important. BERYLLIUM AS AN ACCESSORY CONSTITUENT IN Theoretically, the type and amount of substitution in MINERALS beryl should be closely related to the mode of occur­ The minerals that are known to contain beryllium as rence. Beryl formed as a late magmatic product should an accessory constituent are listed in table 3^ together contain less beryllium than that formed earlier, because with some of their physical properties and their modes of increase in alkali content of the magma as differen­ of occurrences. The range of beryllium content re­ tiation progresses. The abundance of water in the pre­ ported for these minerals is also indicated, although the forming fluid should result in a further reduction of accuracy of most of the figures is difficult or impossible beryllium in vein beryl. Accordingly, the alkali con­ of evaluation. Aside from the usual analytical diffi­ tent of beryl might be expected to increase during peg- culties, most reports in the literature give no informa­ matization and, in general, the beryllium content of tion about what precautions were observed against in­ beryl should be higher in igneous rocks than in vein clusions of other beryllium minerals. Indeed, even deposits. The few analysis of nonpegmatite beryl show, with detailed microscopic examination of tie sample, however, that the average BeO content does not appear one cannot be certain of its nature, as only a few mi­ to be appreciably different from that of beryl in peg­ nute grains would be necessary to give the small matites. The optical data on nonpegmatite beryl indi­ amounts of beryllium detected by spectrographic cates that the index is higher, and therefore the beryl­ analysis. lium content probably lower in tungsten-bearing veins The recovery of beryllium by known hydrometal- than in molybdenum- and tin-bearing veins (Adams, lurgical or similar methods from most minerals in 1953, p. 117). which beryllium is dispersed as an isomorphous con­ stituent is not possible, but some recovery mry be pos­ 2 Na in amphibole: Warren (1929, p. 42) ; OH in garnet: McConnell (1942, p. 458-460). sible from very low grade material containing inclu- MINERALOGY OF BERYLLIUM 13 TABLE 3. Minerals in which beryllium may be an accessory .constituent {Key to abbreviations: isom. isometric; tetr. tetragonal; hex. hexagonal; trig. trigonal; orth. orthorhombic; mono. monoclinic; trie. triclinic; H hardness Moh scale; Q specific gravity; F fusibility; Ol cleavage form; N index of refraction; N0 index of refraction for the ordinary ray; N« index of refraction for the extraordinary ray; Ny index of refraction for the intermediate ray; B birefringence; 2V optic axial angle] Approximate maximum Mineral Chemical composition percent BeO Occurrence Amphibole group: Arfvedsonite. Na3 (Fe,Mg)4FeSi8O22(OH) 2 ____ 0. OX Mono., prismatic; vitreous; black Alkalic igneous reel's; un­ to deep green; insoluble; Cl 110; common. H 6; G 3.5; F 2; Ny 1.69; B 0.015; (-)2V variable. Glaucophane. 001 Mono., prismatic; vitreous; blue; Schists; uncommon. insoluble; Cl 110; H 6; G 3.0-3.1; Ny 1.63; B .019; (-) 2V small. Hornblende__ Ca2 (Mg,Fe)5Si8O22 (OH) 2_ 006 Mono., prismatic; vitreous; green to Igneous and metaraorphic black; Cl 110; H 5.6; G 2.9- rocks; very common. 3.4; Ny 1.61-1.71; B 0.02-0.03; (~)2V large. Apatite_____ Caio(F,Cl,OH) 2 (PO4-As04)6---- 01 Hex., prismatic; vitreous; green, Widely distributed igneous white; soluble; H 5; G 3.2; rocks, pegmatites and sedi­ Cl 0001 imperfect; N0 1.60- mentary and metamorphie 1.77; Ne 1.58-1.77; B 0.002- rocks; common. 0.01. Axinite_____ H (Fe, Mn) Ca2 Al2BSi4O16. Trie., wedge-shaped; vitreous; Pyrometasomatic and high- brown, blue, gray; insoluble; Cl temperature veins; un­ 112, 010, 130; H 7; G 3.3; common. F 2; Ny 1.68-1.69; B 0.01; (_)2V 70°-90°. Cassiterite_____ SnO2_ tr Tetr., short prismatic or pyramidal; High-temperature veins and adamantine; brown or black; Cl pegmatites, placers; com­ 110; H 6-7; G 6.8-7.1; N0 mon. 1.99; Ne 2.09. Chevkinite___ (Ga,Fe)(Ce,Y,Di)i(Si,Ti)sOio_ 1.9 Mono., vitreous; red-brown, black; Granitic pegmatite; rare. gels with HC1; Cl none; H 5; G 13-4.6; F 4; Ny 1.88-1.97; B low, may be amorphous and isotropic. Chlorite....__ (Mg,Fe,Al)5-6(Si,Al)4Oio(OH)8- tr Mono., lamellar; pearly; green; Cl Schists and hydrothermally 001; H 1-2; G 2.6-2.8; Ny altered rocks; eomiron. 1.58; B 0.003-0.007; (+)2V small. Clay minerals: Illite series_ K5(Al,Mg) 2 (SiJAl)4010(OH) 2. 008 Mono., minute lamellae; white; Soils; very common. «H2O. Kaolinite Al2Si2O5(OH)4 ..---_-_-.. 005 Trie., minute pseudohexagonal plates, Hydrothermally altered group. vermicular groups common; white; rocks, soils; common. H 2; G 2.6; F 7; Ny 1.56; B 0.006; (-)2V 20°-55°. Montmoril- . 01 Mono., minute lamellae; Cl 001; Altered tuff, hydrothermally lonite nH2O. H 1.5; G 2.5-2.6; F 5 with altered rocks, soils; com­ series. swelling; Ny 1.50-1.60; B 0.025; mon. ( )2V variable. Clinohumite_.._ Mg»[Mg(F,OH)]j ______1.7 Mono., complex crystals; vitreous; Pyrometasomatic; rare. yellow, red; gels in HC1; Cl 001; H 6; G 3.2; F 7; Ny 1.65; B 0.03; (+) 2V large. Epidote group: Epidote____ Ca2- (Al,Fe, Mn) 02-Al(AlSi3) O9_. tr Mono., prismatic or acicular; vit­ Pyrometasomatic, metamor­ reous; green to black; partially phosed limestones; com­ decomposed by HC1; Cl 001; mon. H 6-7; G 3.3-3.5; F 3 (swells); Ny 1.72-1.82; B 0.006-0.07; 2V large. Allanite..___. (CaJ Ce) 20-Fe2OH.Al.(Al,Si3)09_ 5.5 Mono., tabular or acicular; subme- Accessory in acidic iecneous tallic; brown to black; gels in HC1; rocks, gneiss, schist, mag­ no distinct cleavage; H 6; G 4; netite iron ores; uncom­ F 2.5 (swells); Ny 1.65-1.78; mon. All beryllium ma­ B variable; ( )2V large. terial from graniti". peg­ matite; rare. EudiaUte...... _ (Na,Ca) 6ZrSi6Oi8OH. 005 Hex., rhombohedral; pink; gels in Nepheline syenite pegma­ HC1; Cl 001; H 5; G 2.8-3.1; tite; rare. F 2.5; uniaxial+or ; No, Ne 1.59-1.64; B 0.(KM).01. Euxenite______(Y,Ca,Ce,U,Th)(Cb,Ta,Ti) 2O8__ 05 Orth., massive; brilliant; brownish Pegmatite; rare. black; insoluble; Cl none; H 6.5; G i.8; F 7; isotropic (from alteration); N 2.06-2.26. 14 OCCUERENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES

TABLE 3. Minerals in which beryllium may be an accessory constituent Continued [Key to abbreviations: isom. isometric; tetr. tetragonal; hex. hexagonal; trig. trigonal; orth. orthorhombic; mono. monoclinic; trie. triclinic; H hardr<\ss Moh scale; G specific gravity; F fusibility; Cl cleavage formpN index of refraction; No index of refraction for the ordinary ray; Ne index of refraction for the extraordinary ray, N_ index of refraction for the intermediate ray; B birefringence; 2V optic axial angle] Approximate maximum Mineral Chemical composition percent BeO Description Occurrence Feldspar group: Microcline KAlSisOg.. 0.04 Trie., short prismatic crystals; vitre­ Granitic rocks, pegmatite, (microper- ous: white; Cl 001, 010; H 6; metamorphic rocks; very thite). G 2.55; F 5; Ny 1.52; common. B 0.007; (-) 2V large. Plagioclase_ NaAlSi3O8_ .01 Trie., tabular or prismatic; vitreous; Igneous rocks and pegma­ white; Ci 001, 010; H 6; tite, metamorphic rocks G 2.6-2.76; F 5; Ny 1.53- very common. All beryl- 1.58; B 0.01; 2V large. lian material is albite from pegmatite. Fergusonite. ... (Y,Er,Ce,Fe) (Cb,Te,Ti)O4_ .74 Tetr., prismatic or pyramidal; sub- Pegmatite; rare. metallic; brown; soluble in H2S04 ; Cl 111; H 6; G 5.8; F 7; isotropic (from alteration); N 2.0^2.19. Fluorite_____ CaF2_ .OOOX Isom., cubic; vitreous; white, purple; Accessory in igneous rocks soluble in H2SO4; Cl 111; H <±; and pegmatites; wide­ G 3.2; F 3; N 1.43. spread in vein? and pyro- metasomatic deposits; common. Garnet Ca3(Al,Fe)2Si3Ol2 . .2 Isom., dodecahedronal; vitreous; red, Pyrometasomatic; common. (grossularite- brown, yellow, green; Cl none; andradite). H 6.7; G 3.1-3.4; F 3; N 1.74-1.79. Gersdorffite. _ _ _ Ni AsS tr Isom., massive, metallic, silver- white; Sulfide veins; rar^. Cl none; H 5.5; G 5.6-6.2. Homilite____ 3. 0 Mono., basal plates; black; H -5; Syenitic pegmatites, Nor­ G 3.36; F 2; geis in HCi; Ny way; very rare; beryllian 1.73;B 0.023;l+ ) 2V 80°. variety highly altered. Hyalotekite__ (Pb,Ba,Ca) 9B_(SiO3),2 .. . 75 Orth. (?); vitreous; white; insoluble Pyrometasomatic deposits, in HC1; Cl 2 at 90°; H 5; Sweden; very r-Me. G 3.8; F 3; Ny 1.96; B 0.003; (+) 2V small. Idocrase Caifl(,Al,Mg) 13Si18(O,OH,F)76- 4.0 Tetr., prismatic; vitreous; brown, Pyrometasomatic deposits; (.vesuvianite). green, blue; decomposed by HGi; common. Cl 110 (poor); H 6.5; G 3.4; F 3; N 1.71-1.174; Ne 1.70- 1.73; B 0.001-0.006 (may be biaxial, small 2V). Maucherite_ ___ Ni3As______tr Tetr., square tabular crystals; metal­ Sulfide veins; rare. lic; reddish white; Cl none; H 5; G 7.8; F easy. Mica group: Biotite. _. K(Mg,Fe) s(AlSi3)010 COH)2_ .OX Mono., tabular; pearly; black; de­ Igneous and metamorphic composed by H2SO4; Cl 001; rocks very common. H 2.5-3; 'G 2.8-3.4; F 5; (Beryllium-bearing sam­ Ny 1.56-1.69; B 0.040-0. 060; ples obtained from gran­ ite, pegmatite, and re­ lated rocks.) Lepidolite__ KLi2AiSi4O10(OH)2_ .OX Mono., tabular; pearly; violet, yel­ Granitic pegmatites and tin low; attacked by acids; Cl 001; veins; common. H 2.4-4.0; G 2.8-3.3; F 1.5- 2.5; Ny 1.55; B 0.02; (-) 2V 42°. Muscovite. _ _ KAl2 (AJSi3) OJO(OH)2 . .OX Mono., tabular; pearly; colorless, Granite, gneiss, schist, peg­ brown; insoluble in acids; Cl 001 ; matite, hypothermal veins; H 2.5-3; G 2.7-3; F 6; Ny very common. 1.58; B 0.036; (-) 2V 47°. Microlite. _____ (Na,Ca)2Ta_O6(O,OH,F). 2. 97 (?) Isom., octahedral; vitreous, brown, Granitic pegmatite; very blaak; decomposed by H2SO4j rare. H 5.5; G 5.5; F 7; N-1.93. Nepheline___ NaAlSiO4_... .____. .OX Hex., tabular, prismatic; vitreous to Sodic syenites; common. greasy; colorless; Cl 1010; H 5.5-6; G-2.6; F 4; N0 1.54-1,55; Ne 1.53-1.54; B 0.003-0.005. Niccolite_____ NiAs______tr Hex., massive; metallic; pale red; Sulfide veins; common. Cl none; H 5; G 7.3-7.7. Pyrophyllite__ Al2Si4Oio(OH)2 _ .0008 Mono., lamellar; pearly; white; Metamorphic rocks; un­ Cl 001; H 1; G 2~.8; F 6; common. N, 1.59; B 0.048. MINERALOGY OF BERYLLIUM 15 TABLE 3. Minerals in which beryllium may be an accessory constituent Continued Key to abbreviations: isom.~isometric; tetr. tetragonal; hex. hexagonal; trig. trigonal; orth. orthorhombic; mono. monoclinic; trie. tridlnic; H hardness Mch scale! G specific gravity; F fusibility; Cl cleavage form; N index of refraction; N0 index of refraction for the ordinary ray; Ne index of refraction for the extrao-dinary ray; N, index of refraction for the intermediate ray; B birefringence; 2V optic axial angle] Approximate maximum Mineral Chemical composition percent BeO Description Occurrence Pyroxene group: Aegirite. _ _ _ _ (Na,Ca) (Mg,Fe) 0.1 Mono., long prism, vitreous; green; Syenitic rocks and related slightly soluble; Cl 110; H 6; deposits; common. G 3.5; F 2; Ny 1.77-1.82; B 0.05; (-)2V large. Diopside___ Ca(Mg,Fe,Mn,Zn)Si2O6- 01 Mono., prismatic; vitreous; green; Pyrometasomatic, metamor- Cl 110; H 5-6; G 3.2-3.3; phic, and igneous rocks; F 5; Ny 1.67; B 0.03; (+)2V very common. 58°. Rhodonite _ _ _ Mn2Si2O6 - 002 Trie., basal plates; vitreous; pink; Ore deposits of manganese, Cl 100, 010, 001; H 5.5-6.5; iron, copper, generally G 3.7; F 4; Ny 1.68-1.74; with rhodochrosite. B .01-.02; (+)2V large. Samarskite___ (Y.Er,Ce,U,Ca,Fe,Pb,Th) Orth., prismatic, tabular, massive; Granite pegmatite; rare. (Cb,Ta,Ti,Sn)206 vitreous; black or brown; insolu­ ble; Cl 010; H 5-6; 6 5.675.8; F 5; isotropic (from alteration); N 2.10-2.25; also strongly biref. (Unaltered) Steenstrupine... (Ca,NaJCe)6(OH)Si3Oi2(?)----. 1.9 Hex., rhombohe.dral; dull; brown; Syenitic pegmatite; very H 4; G 3.3; uniaxial negative. rare. Stilbite__ . _ _ _ NaCa5(AluSi29) Ogo.SO H2O___ .7 Mono., tabular; pearly; white; de­ Cavities in basalt; corrmon. composed by HC1; Cl 010; H i; Beryllian variety (fore- G 2.1-2.2; F 2; Ny 1.49; B site) in pegmatite; very .011; (-)2V 30°-50°. rare. Thorite_____ ThSiO4_____...______. 1 Tetr., prisms with pyramids; vitreous; Pegmatite and syenite; rare. brown; insoluble; Cl 110; H 5; G 5.2-5.4; F 6; NO 1.8, com­ monly isotropic from alteration, with N 1.7. Tilleyite____ Ca5(CO3)2Si207-___-___._ tr Mono., colorless; Cl 100, 101 (?); Metamorphosed limestone, G 2.84; Ny 1.63; B 0.04; (+) California; rare. 2V large. Tourmaline__ Na(Mg,Fe,Li)9B3Si6027(OH) 4___ .OX Trig., prismatic; vitreous; black, Widely distributed in meta- brown, green, red; insoluble; Cl morphic rocks, pegma­ poor; H 7; G 2.9-3.2; F i-6; tites, and high tempera­ No 1.64-1.67; N6 1.62-1.64; ture veins; common. B 0.02-0.03. TriphyUite_.. Li(Fe"Mn")PO4 .. --.-.__ .01 Orth., prismatic; vitreous; greenish Granitic pegmatites; corn- gray; soluble; Cl 001; 010, 110; mon. H 5; G 3.4-3.6; F 1.5-2; Ny 1.67-1.70; B 0.004-0.010; 2V variable. Uraninite____ U02.-.---___-.__.__..__ .01 Isom., octahedral, massive jsubmetal- Veins and granitic pegma­ lic; black; soluble in HNOaj H tites; rare. 5.5; G 9; F 7. Variscite____ (Al,Fe)PO4.2H2O______.01 Orth., pyramidal or prismatic; green; Sedimentary rocks. soluble; Cl 010; H 4; G 2.5- 2.9; F 7; Ny 1.56-1.59; B 0.02-0.03; 2V variable. Wavellite_... (A1(OH) 3(PO4)2.5H2O___.___ 1. Orth., fibrous; pearly; white, green; Secondary mineral in bedded soluble in HsSO* and in NaOH; ores; rare. Cl 110, Oil, 010; H 4; G 2.3; F 7; Ny 1.53; B 0.02-0.03; (+)2V 72°. Willemite____ Zn2SiO4...______.005 Hex., prismatic; resinous; white, Zinc deposits; uncommon. green, red: soluble; Cl 0001,1120; H 5.5; 6 3.9-4.1; F 4; No 1.70, Ne 1.72. Yttrotantalite.. (Fe,Y,U,Ca)(Cb,Ta,Zr)O4 _____ .58 Orth., prismatic; sub metallic; black; Granitic pegmatite; rar3. insoluble; H 5; G 5.5-5.9; F 7; isotropic from alteration, N 2.15. Zircon___.... ZrSiO*...______.___.._. 14(?) Tetr., prismatic; adamantine; brown; Accessory mineral in igneous Cl 110 imperfect; H 7.5; rocks, especially in gran­ G 4.7; No 1.94, N. 1.98; B ite, syenite and diorite; 0.04-0.06. common. Beryllian vari­ ety (alvite) in granitic pegmatites; very rare. 16 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES sions of beryllium minerals. The possibilities of fche HALIDES occurrence of beryllium in various minerals as a guest Fluorite samples from several veins contain as much element, and the importance of these minerals as pos­ as O.OOX percent BeO by spectrographic analysis, al­ sible sources of beryllium are discussed below. though none of the samples analyzed were from known beryllium mineral localities. The fact thr.t fluorine SUIiFII>ES does not favor tetrahedral coordination with beryllium Beryllium is not likely to be precipated in sulfide suggests that beryllium in fluorite will be of small lattices. However, it has been detected spectrograph- amount and restricted occurrence. However, the geo­ ically in gersdorffite, niccolite, and maucherite (Haw- logical occurrence of beryllium may be related to the ley, Lewis, and Wark, 1951, p. 154). The manner of presence of fluorine, as fluorite is a common constituent occurrence of the beryllium is not known. Helvite and in many beryllium-bearing tactites, veins, and pegma­ other beryllium-bearing minerals occur in sulfide de­ tites. posits, and minute inclusions of these minerals in the CARBONATES sulfides are a possibility. Although rhodochrosite from Kapnik, Hungary, and OXIDES calcite from Franklin, 1ST. J., are reported to contain traces of beryllium (Goldschmidt and Peters, 1932, In the Franklin district, New Jersey, beryllium was p. 368), the difficulty of accommodation of beryllium reportedly discovered in franklinite concentrates in in the lattice suggests that the maximum amount is 1944 (L. H. Bauer, written communication). Spectro- extremely small. At Franklin, 1ST. J., a district from graphic analyses of carefully selected samples of which several beryllium minerals are known, only 1 of franklinite taken at the Franklin and Sterling mills 10 samples of dolomitic marble contained more than during the present investigation showed less than the detectable minimum of 0.0005 percent BQ,O (L. H. 0.0004 percent BeO, the lower limit of sensitivity. Bauer, written communication). Traces of beryllium have been detected in cassiterite from pegmatites and hydrothermal veins (Borovick PHOSPHATES and Gotman, 1939; Larionov and Tolmacev, 1937). The substitution of beryllium for phosphorus is a The beryllium content of uraninite and other radio­ possibility on the basis of comparable ionic size but ad­ active oxides was determined by Oftedal (1939) who justment of valence is difficult. Although No?kolds and found that most uraninite contains less than 0.01 per­ Mitchell (1948) and Goldschmidt and Peter? (1932, p. cent beryllium. Most of the uraninite samples from 367) did not find beryllium in apatite fro^i igneous the Colorado Plateau contain from 0.0001 to 0.0005 rock, Schroeder. (1931) found beryllium only in apa­ percent beryllium, however the uraninite from the Bed tite, among all the rock minerals which re spectro- Bluff area, Gila County, Ariz., contains as much as graphed qualitatively. Apatite from beryl-bearing 0.005 percent beryllium (Thomas W. Stern, oral com­ pegmatite in the Newry and Eumford ar^a, Maine, munication). The distribution of beryllium in the contained 0.002 percent BeO. In the present investiga­ uraninite structure is not known. tion one specimen of arsenian apatite (svaHte) from Bauxites containing as much as 0.018 percent beryl­ Franklin, 1ST. J., was found to contain 0.0")! percent lium and beryllium hydroxides readily form under BeO; in three others it was absent. The principal similar conditions of surface temperatures and hydro­ mineral of phosphate rock is a member of the apatite gen-ion concentrations. It is not known whether the family, but phosphate rock in the United Plates con­ small proportion of beryllium in the bauxite can be tains no more beryllium than the shale with which it accommodated in the lattice of the finely crystalline, occurs. Apparently apatite group mineral^ can con­ hydrous aluminum minerals or whether it forms dis­ tain only traces of beryllium. Wavellite, however, has crete crystals of its own. An even more likely possi­ been found to contain as much as 0.1 percent BeO bility is adsorption of the beryllium hydroxide to the (Preuss and Gliszczynski, 1951). surface of aluminum minerals. Detailed study of beryllium-rich bauxite might solve this problem. NEO SILICATES In general, the occurrence of beryllium in oxide In minerals of the garnet group a large number of minerals is unlikely because of structural difficulties trace elements have been detected, particularly the rare- and none may be regarded as a potential source of earth metals, which enter by means of the substitution beryllium. Y3+A13+ for Mn2+Si4+ (Jaffe, 1951, p. 133). Beryllium MINERALOGY OF BERYLLIUM 17 has been detected in only a few varieties of garnet; peculiar structure, despite the difference in ionic sizes. typical examples are given in table 4. All known va­ At the lower temperature at which supergene willemite rieties of garnet containing appreciable beryllium are forms by alteration of sphalerite (Pough, 1941, p. 98), members of the grossularite-andradite series and are the presence of beryllium in the solutions seems un­ from pyrometatasomatic deposits. Helvite or other be­ likely. Beryllium in willemite is apparently confined ryllium minerals occur in three of these deposits (Iron to that of high-temperature origin, as at Franklin, Mountain, N. Mex., Wykertown, N. J., Victorio Moun­ N.J. tains, N. Mex.) and within a few miles of a fourth Idocrase contains beryllium more consistently than (Aarvold, Norway: Goldschmidt, 1911, p. 30); beryl­ any other silicate in which beryllium is not an essential lium occurs in idocrase at all four. Samples from many constituent, and of all such minerals that occur ontside of the garnet-rich pyrometasomatic deposits in the of pegmatites it contains the largest amount of beryl­ western United States were analyzed for beryllium in lium (see table 5). the present investigation; of these more than 90 percent did not contain a detectable amount of BeO (0.0004 TABLE 5. Analyses of idocrase for beryllia BeO percent); the maximum content was only 0.002 percent Locality (percent) Reported by- BeO. Many of these samples were nearly pure garnet. Franklin, N. J______3.95____. _ _ C. S. Hurlbut, yoritten Beryllium was not detected in spessartite from beryl- communicati ")n. and helvite-bearing pegamatites (Glass, 1935, p. 765). 1951. Iron Mountain, N. Mex__ 1.09______Glass and otherr. 1944. Apparently, no more than traces of beryllium can be Turnback Lake, North 1.07. ___ Meen, 1939. expected in garnets except in helvite-bearing pyrometa­ West Territory, Canada. Victorio Mountains, N. .2____. Holser, 1953. somatic deposits. Mex. Graubunden, Switzerland- .09 ______Zilbermintz and Roschkova, 1933.* TABLE 4. Garnet analyzed for beryllia Mill Creek area, Montana. .OX____ (2). Aarvold, Norway__ ___ .OX______Goldschmidt ard Composition _ Locality Percent BeO Reference Peters, 1932. Grossularite___ Iron 0. 08-0. 19 Glass and Breitenbrunn, Germany._ ,OX______Do. Mountain, others, Julia mine, U. S. S. R. (?)_ <.01_ ___ Zilbermintz and N. Mex. 1944, Roschkova, 1933. p. 173. Johnson, Ariz______.005_____ (2). Andradite (And.w Wykertown, 0. OX-0. OOX Milton and Woodstock, Me______Present... (3). GrsePysAlsSpi). N. J. David- Amherst, N. H______tr______(3). son, 1950, Carro de los Muertos, Small tr___ (3). p. 504. Chihuahua, Mexico. Grossularite_ __ Victorio 0. 007 Holser, Guffey, Colo______None_____ (3). Mountains, 1953, Ternares mine, Durango, None.-... (3). N. Mex. p. 603. Mexico. Manganian Aarvold, 0. OOX Goldschmidt 1 The several complete analyses of material from this locality are of an int0rgrovro grossularite. Norway. and mixture of idocrase and diopside. 2 Spectrographic analysis by A. A. Chodos. Peters, ' Spectrographic analysis by George Steiger. 1932, p. 369. Spessartite____ Mill Creek, <0. OOOX (») The structure of idocrase is similar to that of garnet Mont. and has been described by Warren and Modell (1931) Grossularite_____ Franklin, N. J, <0. 0004 (») 1 Spectrographic analysis by A. A. Chodos. and Machatschki (1930). A study of the distribution of beryllium in idocrase has shown that perhaps a third of Spectrographic lines of beryllium were reported in beryllium in idocrase replaces silicon in tetrahedrr,, and willemite concentrate from Franklin, N. J. (L. H. the rest enters normally unoccupied tetrahedral posi­ Bauer, written communication). In the present work, tions. Valence is balanced by loss of aluminuir and willemite was carefully picked from composite samples some loss of calcium from the structure. Berrllian of average willemite concentrates. The material from idocrase is consistently high in fluorine content, but Franklin, which is characteristically green, contained there is no correlation with B, Ti, Zn, Mn, Cu, Na, K, 0.004: percent BeO; material from Sterling Hill, which or other minor constituents. is characteristically pale red, contained 0.005 percent With few exceptions idocrase is found only in allo- BeO. No beryllium was detected spectrographically chemical metamorphic rocks (those which have received in willemite from Northern Rhodesia (L. H. Bauer, additions of material while being changed by heat and written communication). pressure). Within this general category, however, two The structure of willemite is nearly identical to that general types of occurrence are common. In or^, as of phenakite, zinc being in rare tetrahedral coordina­ exemplified by some of the occurrences in Switzerland tion with oxygen (Bragg and Zachariasen, 1930). A and the Ural Mountains, idocrase is found at the con­ small quantity of beryllium substitutes for zinc in this tact of mafic intrusive rocks (usually serpentimzed) 18 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES and limestone. A number of samples of this type ing differentiation of sodium-rich magmas, from which of occurrence are among those of table 5 in which no these minerals are late to crystallize. beryllium was detected. The second type of occurrence Rhodonite is associated with beryllium minerals at is in limestone near the contact of granitic rocks and is several places, including Franklin, N. J., Butte, Mont., probably more common. All examples of idocrase con­ and the Sunnyside mine, near Eureka, Colo. An analy­ taining 0.1 or more percent of BeO are from the second sis of rhodonite from Franklin, shows 0.002 percent type of occurrence (table 5). Several of these occur­ of BeO. Samples of vein material in which rhodonite rences are from localities at which helvite or other is the principal gangue were taken from the Butte dis­ beryllium minerals have also been found, and at all trict during the present study. The BeO content in such places fluorite is an associate of the idocrase. these samples ranged from 0.0005 to 0.007, and in most of the samples helvite was observed. Sample^ from the KING AND CHAIN SILICATES Sunnyside mine showed little helvite and contained Tourmaline from pegmatites has been reported to an average of less than 0.001 percent of I>O. One contain as much as O.OX percent BeO (Goldschmidt sample from Bill Young mine contained 0-0016 per­ and Peters, 1932), but even that from beryl pegmatites cent BeO; no helvite was identified. Beryllium was commonly contains much less.3 Tourmaline from hypo- not detected in samples of other rhodonite veins at thermal veins has not been analyzed separately, but localities in the San Juan region, Colorado, from tourmaline-quartz vein material from the Lordsburg which no beryllium minerals have been reported. district, New Mexico, contained less than 0.0004 percent Manganese-bearing members of the epidote group BeO (table 14). have been reported to contain traces of beryllium Beryllium occurs in soda-rich pyroxenes and amphi- (Glass and others, 1944, p. 177). The ordinary pistacite boles more commonly than in the normal members of variety has not been analyzed separately for beryllium, these groups. Goldschmidt and Peters (1932, p. 366) but a large number of epidote-rich tactites1 analyzed reported 0.1 percent BeO in aegirite, and O.X percent in in the present investigation contain a maximum of arfvedsonite and barkevikite. One sample of aegirite 0.0008 percent BeO (table 15), but in 75 percent of from Wind Mountain, N. Mex., contained only O.OOOX them BeO was below the limit of detection. Allanite, percent BeO. The foregoing are all from pegmatitic which is structurally and chemically related to the f acies of nepheline syenite intrusive rocks, but zincian- epidote group, is repqrted to contain as much as 5.52 manganoan diopside from Franklin, N. J., was found percent BeO (Dana, 1892, p. 526). All allr.nites con­ also to contain 0.01 and diopside-hedenbergite from taining more than 0.5 percent BeO were higl ly altered Mill Creek, Mont., contained O.OOX percent BeO. and all were from pegmatites. Beryllium was not de­ Goldschmidt and Peters (1932, p. 367) list two am- tected in the unaltered allanite of hydrothermal origin phiboles of metasomatic origin containing O.OOX per­ at Wykertown, N". H. (Milton and Davidson, 1950, p. cent BeO and one enstatite in which beryllium was not 504). detected. An augite which contained less than 0.001 SHEET SILICATES percent BeO was from basalt, and a pyroxene in which beryllium was not detected was from eclogite. Nock- Complex substitutions of various ions in she^t silicates olds and Mitchell (1948) analyzed the hornblendes and are common, and opportunities for the occurrence of pyroxenes from a series of Scottish igneous rocks rang­ beryllium are numerous. Micas from pegmatites have ing nearly continuously in composition from dunite been found to contain a maximum of O.OX percent BeO through granodiorite. One hornblende sample con­ (Goldschmidt and Peters, 1932, p. 366), but no beryl­ tained a questionable 0.003 percent BeO, which was the lium was found in micas from a series of igneous rocks limit of sensitivity, and the rest showed no BeO. Bray (Nockolds and Mitchell, 1948, p. 564-565). Fluorine- (1942b, p. 794) did not detect any beryllium in five phlogopite has been synthesized as much as one-fourth samples of hornblende from granodiorite. In syn­ of the silicon being replaced by berylliuir (that is, thetic fluo-amphiboles, beryllium has been substituted K2Mg6BeSi7O2oF4=about 3 percent BeO) (Eitel, for silicon to the extent of 12 percent of the tetrahedral Hatch, and Humphrey, 1950). This is an example of groups (about 3 percent BeO) in both lime- and soda- replacement of A1+3A1+3 by Be2+Si4+ in tetrahedral coor­ rich varieties (Comeforo, Hatch, and Eitel, 1950). The dination, a process which may be important in other presence of beryllium in pyroxenes and amphiboles alumino-silicates. Another replacement observed was is probably due largely to beryllium concentration dur- A1A1 by BaBe2. Such replacements in syrthetic flu- orine-nmscovite are more restricted. Data on natural 8 Average of 0.006 percent BeO in blue, green and pink tourmaline from the Newry and Rumford area, Maine; analyses by J. D. Fletcher. micas do not yet indicate any preference of beryllium MINERALOGY OF BERYLLIUM 19 for those of a particular mode of occurrence or of a par­ contrast markedly with calcic plagioclase, in which ticular composition. beryllium has not been detected. Nockolds and Mitchell A large number of representative samples of clay (1948) tested 11 potsassium feldspar samples and 9 minerals were analyzed spectographically for beryllium plagioclase (A^g-An^) samples from a variety of by Wheeler and Burkhardt (1950). All of the mont- igneous rocks; all contained less than 0.003 percent of morillonites that originated through surface or sub­ BeO, the limit of sensitivity. Bray (1942b, p. 790) was marine alteration of tuffaceous rocks were found to not able to detect beryllium spectrographically in 17 contain berylliiun, the maximum content being 0.01 samples of feldspar from either pegmatites or related percent BeO. Beryllium was found in nearly all of the igneous rocks near Jamestown, Colo. Substitution of kaolinite-group samples that were of hydrothermal ori­ beryllium in feldspars is stable when the beryllium is gin (maximum 0.008 percent BeO), but could not be in tetrahedral positions in place of silicon or aluminum detected in most of those of residual origin. Illite (Schiebold,1931). formed by soil alteration contained a maximum of 0.008 Available data on nepheline (Tolmacev and Filippov, percent BeO. None was detected in attapulgite. None 1934; Goldschmidt and Peters, 1932, p. 366) indicate of these clays appear directly related to bauxite de­ that beryllium may have about the same solubil'ty in posits formed by alteration of syenitic igneous rocks. the nepheline lattice as in that of the alkali feldspar. Szelenyi (1937) reported that some clays contain about However, nepheline seems to have a higher average the same amount of beryllium as the associated bauxite beryllium content than feldspar minerals. Most of the (0.005 to 0.01 percent BeO), although others contain analyzed nepheline and feldspar minerals are from peg­ less. In addition to the mechanisms proposed above matites. A lower beryllium content for these minerals for other silicates, a new .interpretation of the mont- in finer grained intrusive rocks may be surmised from morillonite structure (McConnell, 1950) suggests the spectrographic analyses of igneous rocks. Feldsrmth- further possibility of replacing Si4Oi0 by BeSi3H2Oio oids other than nepheline have not been analyzed for in the tetrahedra. beryllium. Chlorite (Glass and others, 1944, p. 177), pyrophyl- Analytical data for the amphiboles, micas, feldspars, lite (Wheeler and Burkhardt, 1950, p. 80), and apoph- and feldspathoids show approximately the same maxi­ yllite (Goldschmidt and Peters, 1932, p. 367) have been mum beryllium content for each, this suggests th"t be­ reported to contain small amounts of beryllium. ryllium substitution is controlled by a feature coinmon to these minerals. This common feature is the presence FRAMEWORK SILICATES of four-coordinated aluminum, permitting the substi­ Beryllium is found in small quantities in feldspars tution of BeSi for A1A1. Silicates of this typ% in­ (table 6). cluding all the framework silicates except quarts, all Although the maximum beryllium content recorded the sheet silicates, and hornblende in the chain silicate for albite is higher than that for the potassium feld­ group, should have comparable solid solubilities for spars, a few determinations show the averages not to be beryllium. Therefore, when formed in environments significantly different. The alkali feldspars as a group of similar beryllium concentration, these minerals

TABLE 6. Beryllia content of 14 samples of feldspar BeO Mineral Pock locality (percent) Reference Microcline microperthite_ Granite pegmatite______Risey, Norway______--__-_ <0. OOOX Goldschmidt and Peters> 1932, p. 366. Do_-_---____--_-_-_- __do______.____ Pikes Peak, Colo.______.OOX Do. Do_---___---_----. Pegmatite(?)____.-.__ U. S. S. R.(?)______.04 Filippov and Tolmacev, 1935. Soda microcline. ______Syenite pegmatite ______Langesundfiord, Norway _ _ _ _ . OOX Goldschmidt and F3ters, 1932, p. 366. ______Laven, .OOX Do. Microcline______Perthite zone, granite Ridge pegmatite, Red Hill, .003 0) pegmatite. Maine. Perthite______do______.__do______.003 0) Microcline______Granite pegmatite. _____ Rumford, Maine-____---_-_ .003 0) Albite ______Tactite ______. __ Mill Creek, Mont______.OX Do ______Granite pegmatite. _____ Ne wry and Rumford, Maine- .002 Do ______do______do______.006 Do ______do______Kragero, Norway ______.01 Goldschmidt and Peters, 1932, p. 366. Labradorite. ______Anorthosite. Sogon, Norway. <. OOX Do. Bytownite. ______do_____ <. OOOX Do. i Spectrographic analysis by J. D. Fletcher; specimens collected by V. E. Shainin. * Spectrographic analysis by A. A. Ohodos. 20 OCCURRENCE OF NONPEGMATTTE BERYLLIUM IN THE UNITED STATES should contain comparable quantities of beryllium. table 7, many qualitative determinations 1 ave been However, a wide range is to be expected, owing to the made most with negative results. Spectrogro.phic tests variety of geologic environments in which the minerals of a representative suite of igneous rocks from the crystallize. Spanish Peaks region, Colorado, showed negative re­ sults for beryllium, but the limit of detection was about BERYLLIUM IN IGNEOUS ROCKS 0.02 percent Be (Knopf, 1936, p. 1779). Spectrographic UNITED STATES LOCALITIES analyses of 425 miscellaneous rocks and ores were tabu­ The few data on the beryllium content of igneous lated by Freeman (1942, p. 777, 778) and only one, a rocks in the United States are summarized in table 7". weathered granite, contained more than the detectable Some of these analyses, originally stated in terms of limit of 0.001 percent Be. Bray (1942a, p. 431; 1942b, percent beryllium, were converted to percent BeO in p. 784,785) reported qualitative spectrographic analyses order to facilitate comparisons with results of the of 19 samples of Precambrian granites, 9 samples of present investigation. Most of the original analyses Tertiary granodiorite, and 7 samples of Tertiary quartz were stated to only one significant figure; consequently, monzonite, all from Colorado, and 9 samples of granite the converted result gives an impression of greater and 2 of granodiorite from Massachusetts. None accuracy than was intended by the analyst. showed beryllium, but the sensitivity of the tests is not Besides the semiquantitative determinations listed in stated.

TABLE 7. Beryllia content of igneous rocks of the United States, as published BeO SiO2 Rock Locality (percent) (percent) Reference Obsidian______,_ Yellowstone Park, Wyo______.__ 0.01 75 Goldschmidt and Peters, 1932, p. 365. Nepheline syenite______Magnet Cove, Ark______. OOX 49. 7 Do. Granite porphyry,______Babyhead, Llano County, Tex_____ . 004 75. 20 Sandell and Goldich, 1943, p. 169. Granite-__-_-__----______-___ Graniteville, Mo. ______.003 76. 81 Do. Granodiorite__---____-____-_. Bear Mountain, Gillespie County, . 003 76. 77 Do. Tex. Granite -____---______Granite Mountain, Burnet County, .002 73. 02 Do. Tex. Rhyolite..______.______Devils Track River, Cook County, .002 73. 6 Do. Minn. Granite ______Cassaday quarry, Llano County, .001 72. 15 Do. Tex. Albite-nepheline syenite.______Litchfield, Maine______-__ .001 60. 39 Goldschmidt and Peters, 1932, p. 365. Quartz monzonite______Town Mountain, Llano County, .0008 68. 15 Sandell and Goldich, 194f; p. 169. Tex. Granitic rocks 1______Minnesota______-______. 0008 Do. Granite______-___.._-_____ Malmo, Aitkin County, Minn______.0006 71. 19 Do. Diabase..____._____-____ Minnesota(?)______. 0005 52. 70 Sandell, 1949, p. 91. Do______-__Do------______-___..- . 0003 46. 88 Do. Quartz monzonite______Bagdad, Ariz__.______<,. 0004 64. 49 Anderson, 1950a, p. 617-18. Dunite.______Jackson County, N. C-.__--_---__ . OOOX _ ___ Goldschmidt and Peters, 1932, p. 363. i Composite of five samples. Many igneous rocks in the United States were ana­ samples it was 0.001 percent BeO or less. TH table in­ lyzed spectrographically for beryllium (table 8). dicates that those rocks that contain more than 0.001 Though a variety of rock types was included in the percent BeO are mainly of silicic or alkalio varieties, present sampling, particular attention was paid to silicic whereas those of less than this amount are fc^ the most and alkalic intrusive rocks, for experience of previous part the more mafic types. Notable exceptions to this workers appeared to indicate that these are most likely generalization occur in the Iron Hill rocks, where un- to contain beryllium. The composite alkalic intrusive compaghrite (melilite-diopside rock) and pyroxenite, rocks at Iron Hill, Colo., northeastern New Mexico, which are low in silica and alkalis, contain r>ost of the Magnet Cove, Ark., and in Trans-Pecos Texas, were beryllium, whereas nepheline syenite and scda syenite sampled extensively and account for the many rare and show abnormally low beryllium content. uncommon rock types included in the table. With the exception of granite, less emphasis was directed to the FOREIGN LOCALITIES more common igneous rocks of the Western States. Gra­ Spectrographic analyses of many igneous rocks from nodiorite and other intermediate types are poorly rep­ localities outside the United States are included in the resented. reports of Goldschmidt and Peters (1932), Kodolico The lower limit of beryllium determination for some (1943), Eodolico and Pieruccini (1943), Y^ager and samples was as high as 0.004 percent BeO but for most Mitchell (1943), Sahama (1945a; 1945b), and Nockolds BERYLLIUM IN IGNEOUS ROCKS 21 and Mitchell (1948). Beryllium was among the minor miscellaneous foreign sources are summarized in table 9. elements determined or looked for in many of the sam­ The results compare favorably with those obtained for ples. Data for these samples and for a few others from igneous rocks in the United States (table 8).

TABLE 8. Beryllia content of igneous rocks of the United States, as analyzed for this study

Number Percent BeO Rock Form Locality Associated of metals analyses i High Low A verage

Feldspathoidal: Melanocratic: 1 <0.001 Analcite gabbro Plug do...... 1 2.002 Dike ___ . _ - Fe ... - 1 <001 Gordon Butte, Meagher County, Mont __ .. None.- ... .. 1 <0001 Madupite . ____ Sheet . do - 1 <001 Malignite (some nepheline- Dike Tip 10 0.03 0.001 .016 syenite pegmatite). Leucocratic: Nepheline syenite ____ Dike Fe . 4 .002 <001 .001 Do Plug(?)...... Al »1 2. OOOX Do do- 31 2. OOOX Do Be .0050 Do...... do. . do do 6 .0074 <001 .005 Do Sill...... - 1 .0066 Do 2 .OOX .OOX .OOX Do. Sill ..... do 81 2. OOOX Do...... do do «2 .002 .OOOX .001 Analcite-nepheline syenite _ PlUg(?)- ... - Little Wind Mtn., Otero County, N. Mex _ .... -do 1 .002 Nepheline-sodalite syenite. Ring dike ___ Red Hill, Carroll County, N. H- ...... do 1 s.OOOX Nepheline syenite pegmatite Dikes ____ ... Be 3 .0074 <001 .003 (see also malignite) . Pulaskite. _ . __ Stock.. AL- .... 2 .OOOX <001 2. OOOX Leucite syenite porphyry. _ Dike ____ - do... 2 Sills. 5 .007 .001 2.003 Do...... Dikes ­ do «3 .002 .OOOX .001 Do do ?5 .001 <001 K.001 Sheet- .... -do 1 <001 Ijolite -do ..... 8 .001 <001 <001 Do. (altered) ______do- do ...... do 2 <0001 <0001 <0001 Do Dike __ ..... do. 2 .007 do...... do .... 7 .0098 <001 .0037 Do. (altered)..--...... do -do...... do ..... 13 .0041 <.001 .0019 -do-. Fe 1 <001 Wyomingite ______Sheet. Leucite Hills, Sweetwater County, Wyo _____ None. -_ 1 <001

Syenitic: Porphyritic syenite...... Plug...... Cornuda Mtn., Otero County, N. Mex...... None.. 2 .002 .0008 s.OOl Do ...... Sills... _ ...... do ... - 1 <004 Do. . .do 1 <.001 Do Plug do 1 2.001 Do do- ..... do 1 s.004 Ring dike(?)_ ..... do...... 1 '.002 Do Cu, W 1 2.0004 Do...... Cu, Au 2 K.0004 Do....-. . Ring dike (?) Red Hill, Carroll County, N. H ______.. 1 2 < OOOX Soda syenite _ . - ...... Dike do 3 <0005 «X»5 <0005 Sill(?) ..... do.. 1 2<001

Granitic: Batholith.. __ Bartlett, N. H... __ .... _ ...... Fe, Be ___ ~ 82 .0032 .0017 .0025 Do. Stock __ . __ Fe, Ti _ ..... 1 <001 Do. .. __ .do _ ...... »1 .018 Do...... do.. 1 '.0002 Do. . .. Batholith _ .. Be, Sn, Li.... 105 .0009 Do...... W...... 2 .0078 <0001 .0004 Do...... do.. W... 1 .0015 Do...... _ ...... do.. ... W...... 1 .0007 Do .. ... -do...... W __ __ . 1 <0001 Do do...... Rocky Canyon, Humboldt Range, Nev ...... None.. 2 .0011 .001 .001 -do.. Be, U ... 4 .0052 .0024 .0037 Granite porphyry...... Dike - Limerick Canyon, Humboldt Range, Nev...... None.. ___ 1 <0001 Rhyolite porphyry ...... do. Vietorio Mts., Luna County, N. Mex ___ ...... Be, W _ ..... 1 .002 Do...... do-.. W ______. 1 <001 Rhyolite breccia...... Plug...... do...... do ... 1 <001 See footnotes at end of table. 22 OCCURRENCE OF NONPEGMATTTE BERYLLIUM IN THE UNITED STATES

TABLE 8. Beryllia content of igneous rocks of the United States, as analyzed for this study Continued

Number I'ercent BeO Rock Form Locality Associated of metals analyses 1 High Lov Average

Granitic Continued "1 0.0005 Aplite (altered)...... Dike Be, U 1 .0098 Aplite ...... do...... do .... .do.. 3 0.0019 O.OC1 .0019 Do do W ___ 1 <0002' Do...... do...... 1 .0007 Do ...... do...... do.. 3 .0015 .OH .001? Do...... do _ ...... W_ 1 .0011 Do. - ..do. -...... do 1 .0008 County, Nev. do...... 0007 <.orn .000% Stock(?)._. . W _ ...... 1 .0001

Intermediate: Dike Zn, Pb, Cu... 1 s.0004 Do ...... Stock ...... W 1 <0001 County, Nev. Do...... do.. W .... . 1 .ooia Do...... do ...... W .. 1 .0034 1 *<.0004 Do...... 182 .0016 nri.1 .0015 Do ...... do.. 1 .OOlfr Do...... do.. . W 1 <.0001 Do...... do...... W 1 < 0001 do W 1 .0044 Do. .do W 1 <.0001 Do...... -do... .. W.. 1 <0001 »1 .0004 _ do- Fe, TL ... 1 <-001

Mafic: Gabbro ______Dike ...... Co...... »1 *<001 Do...... do... Fe, TL...... 1 <001 do...... < nnfu <.' *<.001 Stock do 10 .0033 <.

> Unless otherwise noted, all analyses are of samples collected during this investi­ 7 Material collected by the Mine, Mill, and Smelter Survey, U. S. Geological gation. Survey. * Determined on plates exposed for general scanning, and not for precise determina­ 8 Material collected by D. M. Henderson, University of Illinois. tion of BeO. ' Material collected by J. W. Adams, U. S. Geological Survey. 8 Material collected by Mackenzie Gordon, U. 8. Geological Survey. 10 Material collected by 3. J. Norton, U. S. Geological Survey. * Composite. 11 Material collected by C. S. Ross, U. S. Geological Survey. * Material collected by A. S. Wilkerson, New Jersey Bureau of Mineral Research. ij Material collected by 3. R. Cooper, U. S. Geological Survey. * Material collected by Fred Hildebrand, University of Chicago. DISTRIBUTION OF BERYLLIUM IN IGNEOUS BOOKS Since then other estimates have been made, somewhat The average BeO content of various types of igneous increasing the amounts for both granite and average rock is important to a basic understanding of beryllium igneous rock and substantially reducing the figure for geochemistry. Furthermore, this information may in­ feldspathoidal rocks. However, recent estimates by dicate what kinds of rock are favorable for beryllium Sandell (1952, p. 212-213), based on fluorimetric deter­ prospecting, and what amounts may be considered sig­ minations of beryllium in composite samples of igneous nificant in a given rock type. Goldschmidt and Peters rocks from various localities, agree essentially with the (1932, p. 370) made the first detailed estimate of the values given by Goldschmidt and Peters for granite, consent of beryllium in igneous rocks, as follows: gabbro, and average igneous rock. BeO The analyses by Goldschmidt are not strict];T compa­ Rock type (percent) rable with those of some later analysts because his are Average igneous rock______0.0005 given only in powers of ten, although the figures given Nepheline syenite ______.01 Granite ______.001 by others may not be precise. On the other hand, the Gabbro______1.0003 greater accuracy of the more recent determinations 1 Added later (Goldschmidt, Hauptmann, and Peters, 1933, p. 364). has been offset by discovery of a wider range in beryl- BERYLLIUM IN IGNEOUS BOCKS 23

TABLE 9.- -Beryllia content of igneous rocks from foreign localities BeO content, in percent Number of Rock Loeality samples High Low Average Reported by

FELDSPATHOIDAL Melanocratic types__ _ Portugal _____ 2 0. OX 0. OOX 0. 01 Goldschmidt and Peters (1932). Do______Fennoscandia. 1 ______<. 001 Do. Leucocratic types______Greenland-__. 1 ox Do. Do______Portugal____- 2 01 . 001 . 005 Do. Do______Fennoscandia. 7 01 <. 001 .003 Do. Zilbermintz and Roschkova (1933). Do______Hungary. ______2 001 .001 . 001 Goldschmidt and Peters (1932). Do______Brazil______2 OOX . OOX .OOX Do. Do______Southern Russia. 1 <.01 Zilbermintz and Roschkova (1933), Do______Canada. ______2 <. 001 <. 001 <. 001 Goldschmidt and Peters (1932). Mixture. ______World. ______22 .001 Goldschmidt and Peters (193.).

SYENITIC Syenite ______Fennoscandia. 1 0. 001 Goldschmidt and Peters (1932). Do______do_.__-_. 1 19 . 0006 Sahama (1945a). Trachyte ______Italy__ 2 0. 0030 0. 0022 .0026 Rodolico and Pieruccini (194S).

GBANITIC Granite_*.______Italy______2 0. 0033 0. 0021 0. 0027 Pieruccini (19431. Do______Germany.. ___-_--____. 1 14 . 002 Goldschmidt and Peters (1932). Do.___-___.____ Italy______. 2 .0018 . 00046 . 0011 Pieruccini (1943). Do______Germany.. ______5 .OOX <. 001 .001 Goldschmidt and Peters (1932). Do______Fennoscandia ______i 54 .001 Sahama (1945b). Do______do______. 2 .OOX . 001 .OOX Goldschmidt and Peters (1932). Do.______do______. i 42 . 0003 . 0003 .0003 Sahama (1945b). Do______Scotland.-______._. 3 <. 001 <. 001 <. 001 Nockolds and Mitchell (1948). Do______Fennoscandia- ______5 . 0003 <. 0003 <. 0003 Sahama (1945b). Granophyre. ______Greenland- ______2 <. 003 <. 003 <. 003 Wager and Mitchell (1943). Aplite. ______Scotland ______1 <. 001 Nockolds and Mitchell (1948). Obsidian ______Various ______3 . 001 . 001 . 001 Goldschmidt and Peters (1932). Granodiorite and Scotland______-_-____. 9 <. 001 <. 001 <. 001 Nockolds and Mitchell (1948). adamellite. Tonalite ______Germany-Fennoscandia. 3 .001 <. 001 <. 001 Goldschmidt and Peters (193f\ Do______Scotland. ______1 <. 001 Nockolds and Mitchell (1948).

MAFIC Diorite ______Italy______. 1 0. 0011 Pieruccini (1943). Do___. ______9 <0. 001 <0. 001 <. 001 Nockolds and Mitchell (1948). » 11 ______. 0003 Goldschmidt and others (1933). Do______... 7 <. 003 <. 003 <. 003 Zilbermintz and Roschkova (1933). Do 6 <. 001 <. 001 <. 001 Nockolds and Mitchell (1948). Do______:____ 124 ______<. 0001 Sahama (1945a). Diabase ______Germany ______. 3 <. 001 <. 001 <. 001 Goldschmidt and Peters (19357. Basalt.. ______.___ _ _do ______.. . 1 __ __ <. 001 Do. ' 2 <. 001 <. 001 <. 001 Nockolds and Mitchell (1948). Dunite______do____.__. ______1 <. 001 Do. "Ultrabasics" __ _ ..___ Fennoscandia ____ <. 0001 Sahama (1945a). 1 Mixture. Hum content for a given rock than was previously ex­ sampled in detail. The average value of 0.01 percent pected. An attempt has been made to adjust the aver­ BeO given originally by Goldschmidt and Peters for age BeO contents for igneous rock types to fit the data nepheline syenite seems much too high, as the only obtained in the present investigation; the following analyses in their data that exceeded the figure were the values are suggested: very extraordinary "sodalite-eudialyte rock" (alkalic BeO syenite) and "pedrosite" (alkalic hornblendite). Their Rock type (percent) revised figure of 0.003 percent BeO (Goldschmidt, Average igneous rock______0.001 Feldspathoidal rocks______.0025 Hauptmann, and Peters, 1933, p. 364) is close to that Granitic rocks______.002 proposed by us. The analytical data of Goldschmidt Syenitic rocks______.001 and Peters on rocks from Magnet Cove, Ark., compare Intermediate rocks______.0007 favorably with our results. (See tables 7 and 8.) "iliey Mafic and ultramafic rocks______.0001 report 0.004 percent BeO in nepheline syenite from that The present study has provided much information locality, whereas the present investigation disclosed a concerning the presence of beryllium in alkalic intru­ maximum of 0.002 percent BeO and an average of about sive rocks in the United States, as most of these were 0.001 percent. 24 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES The average beryllium content of feldspathoidal able do not differ noticeably in BeO content from the rocks gives little weight to the less abundant mafic vari­ average for the corresponding intrusive rocks. eties. However, the average beryllium content of the The beryllia content of the average igneous rock was mafic varieties probably exceeds the total average by as calculated by the method of Knopf (1916, p. 620) and, much as 0.001 percent BeO. At Iron Hill, Colo., Wind like the figures on which it is based, must be considered Mountain, N. Mex., and Alter-Pedrosa, Portugal, the as tentative. The value of 0.001 percent BeO thus highest contents were all in pyroxene- or amphibole- obtained is intermediate with respect to averages rang­ rich rocks, but in southern Norway the highest was in ing from 0.0005 to 0.002 percent BeO given by others laurdalite, a type of nepheline syenite commonly poor (Goldschmidt and Peters, 1932, p. 371; Noddack and in minerals of the pyroxene and amphibole groups. In Noddack, 1934, p. 173; Sandell and GoldicK 1943, p. comparing the chemical analyses and modes so far 181; Sandell, 1952, p. 213). available, no consistent correlation between beryllium In comparing the new averages for the various rock content and mineralogy is apparent. The tendency for types with that of the average igneous rock, the writers higher BeO content in the mafic types may be attrib­ confirmed their earlier conclusion that beryllium is con­ uted to the admittance of larger amounts of beryllium centrated in granites and feldspathoidal rock, but the into the lattice of aegirite than into other minerals of difference in average BeO content for granite and feldspathoidal rocks (see table 3) and to the tendency feldspathoidal rocks is much less than formerly sup­ for pyroxene and amphiboles to crystallize last in many posed. The formation of granite and feldspathoidal alkalic intrusive bodies (Fersman, 1929, p. 22-27). rocks is attended by a concentration of alkalies and The granites analyzed in connection with the present volatile components, and apparently beryllium tends investigation (see table 8) average somewhat higher to be concentrated in the process. In feldspathoidal in beryllium content than those of Goldschmidt and rock the process of differentiation apparently is such Peters (table 9) or Sandell and Goldich (table 7), that beryllium tends to be concentrated in the more being about 0.004 percent BeO. However, many of mafic f acies. the samples probably are not representative: those from Sheeprock Mountains, Utah, and Mount Antero, Colo., MODE OF OCCTTBBENCE are from areas known to be rich in beryl, and others are At most localities where beryllium has been detected from small granitic intrusive bodies in metal-mining in igneous rocks the beryllium-bearing miner?! or min­ districts of the western United States. Although such erals have not been determined. The occurrence of rocks probably do not contribute greatly to the world beryl and phenakite as miarolitic fillings, schlieren, average for granitic rocks, they should serve to raise segregations, and individual grains in granite at Mount the beryllium content somewhat above the minimal Antero, Colo., and in the Sheeprock Mountains, Utah, values obtained for other granites. The value of 3 suggest that these minerals may be present in other ppm beryllium (about 0.0008 percent BeO) suggested beryllium-bearing granites. Microscopic beryl in by Sandell (1952, p. 212) for the average granite thus granite was described by Hartley (1902, p. 285). may be too low, and the 0.002 percent BeO suggested The theoretical upper limits for BeO content in by Goldschmidt, Hauptmann, and Peters (1933, p. 364) igneous rocks containing no beryllium minerals (that is taken as a suitable compromise for the present. Re­ is, beryl, helvite, etc.) may be approximated by total­ sults of our analyses seem to indicate that granitic rocks ling the maxima (see table 3) for the various mineral associated with major ore deposits have higher than species in the rock. For an average granite this would average beryllium content. Nonfeldspathoidal syenites be about 0.02 percent BeO, with mica as the principal appear to contain less beryllium than granites, although carrier. However, most of the analyzed rod" minerals they have not been sampled extensively. Quantitative are of specimens from pegmatites and are therefore data on granodiorites are lacking. most likely to be saturated with beryllium, b"it also are The new analyses contribute little to the knowledge more likely to contain inclusions of beryl and other of beryllium content of the more mafic rocks, except to beryllium minerals. The grade of beryl ore in confirm that they most commonly contain less than pegmatite zones (Hanley and others, 1950, p. 11) sug­ 0.001 percent BeO. The only high value was obtained gests that the average BeO content of most pegmatites from a pyroxenite associated with the alkalic intrusive does not greatly exceed 0.02 percent, or that of an at Iron Hill, Colo. The average value given is that of average granite. Possibly the beryllium in sime gran­ Goldschmidt, modified by the determinations of ites containing this amount of BeO may be present in Sahama. part as minute crystals of beryl or phenakite. Analyses of extrusive rocks are few, but those avail­ In feldspathoidal rocks beryllium may be present as BERYLLIUM IN SEDIMENTARY ROCKS 25 an accessory constituent in minerals, mainly in aegirite. laboratory experiments that largely decomposed feld­ Goldschmidt and Peters (1932, p. 366) give the follow­ spars and many other silicates (Norton, 1939, p. 11). ing analytical data on minerals from a nepheline-sye- Danalite has been found altered to phenakite, side- nite pegmatite at Laven, Langesundsf iord, Norway: rite, sphalerite, and pyrite (Palache, 1907, p. 25S/-254), BeO but no other alterations of the helvite group minerals Mineral (percent) have been recorded. Aegirite______.______0.1 Aside from the rare presence of bertrandite, reten­ Nepheline______.______. OX tion of beryllium in the alteration product is uncertain. Soda-microcline______. OOX Lepidomelane . OOX Although Kerr's analysis of the kaolinite-rich product showed 0.24 percent BeO, he assumed in his calculations The theoretical maximum beryllium content for an that this was owing to contamination by beryl (1946b, average nepheline syenite is approximately 0.04 per­ p. 439-440). Probably most beryllium minerals do not cent BeO. Even in the pegmatitic phase of these rocks, weather chemically except under extraordinary circum­ beryllium minerals are rare. Furthermore, pegmatite stances. Many of the silicate minerals in which beryl­ is not so common in f eldspathoidal rocks as in granitic lium is a minor constituent, such as feldspar, nepheline, rocks. Detailed analytical work on the feldspathoidal and micas, decompose easily under surface conditions. rocks from Wind Mountain, N. Mex., indicates that all The decomposition involves an intermediate dissolved the beryllium is present in rock minerals, and that it state (Correns and Engelhardt, 1938) in which there is nearly as abundant in the parent rock as in pegma­ is a breakdown of the oxygen tetrahedra, accompanied tite. The highest contents were found in the malignite by the release of colloidal silica and beryllium. (aegirite-rich) facies of the pegmatitic rocks and in the The specific gravity of most beryllium minerals, aegirite-rich hornf els associated with it. which is 2.6 to 2.9, is so close to that of quartz that no BERYLLIUM IN SEDIMENTARY ROCKS mechanical concentration can be expected in sandy sedi­ ments. Instead, the beryllium minerals that may have CLASTIC DEPOSITS been localized originally, as in granitic pegmatites, The concentration of beryllium in clastic sedimen­ tend to be dispersed. Close to a rich source of beryl, a sufficient concentration may be present to mske re­ tary rocks depends largely upon the effect of weathering on the beryllium-bearing minerals and the extent to covery profitable; removal of other minerals in solu­ tion or suspension may improve the grade. Such placer which gravity may have concentrated these minerals. beryl has been reported from Minas Gerais, Brazil The weathering of beryllium minerals has not been (Moraes, 1933, p. 291) where it is associated with dia­ studied as such, but some information was obtained on chemical weathering of beryllium minerals through mond and tourmaline. Beryl has poor cleavage and a hardness of T and study of hydrothermally altered beryl and danalite. therefore might be expected to persist in sediments. Altered beryl from pegmatites in Brazil (Kerr, Freise(1931) conducted experiments to show c'nanti- 1946b) and Korea (Iwase and Ukai, 1944) shows an tatively the relative resistances of various minerals to increase in water and a decrease in silica, alkalies, and abrasion. Part of his results, showing the resistance specific gravity. In these and other studies of altered of beryl in comparison to other silicates, are tabulated beryl, the effect of alteration on beryllium content is below: not certain. Generally some beryllium is lost, although Abrasion resistance in the Korean material a slight gain perhaps due to Mineral (Hematite-100) secondary bertrandite was noted. Quartz______245 Some investigators are of the opinion that the water Beryl______270-465 in beryl analyses is due to included alteration products Chrysoberyl 300 (Caglioti and Zambonini, 1928; Folinsbee, 1941, p. 488). Idocrase__ 330 Grossularite-andradite 320-420 However, the fact that beryl loses water slowly and ir­ reversibly at 800°C (Alien and Clement, 1908, p. 115- The many treatises on the mineralogy of sediments do 116) indicates that the water is probably held in the not mention beryl, but this may be due to several fac­ beryl structure rather than in the structure of an alter­ tors: (1) beryl is in the light fraction, whereas the ation product. According to Kerr (1946b, p. 436) and heavy fraction is usually of greater interest to the Waldschmidt and Adams (1942, p. 34), kaolinite and petrographer, (2) because of dispersion the number of muscovite are products of highly altered beryl. At beryl grains will be very small except near a very rich temperatures as high as 300 °C, beryl was stable in source, and (3) grains of beryl may be mistaken for

467945 59 3 26 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES apatite and possibly for quartz. Some rarer but more grained unidentified minerals; the mode of occurrence easily distinguished beryllium minerals such as euclase of the beryllium is unknown. (Spencer, 1924) and gadolinite (Hutton, 1950, p. 662) have been found in clastic sediments. In finer sediments, small amounts of beryllium may The chemistry of solution, transportation, and dep­ occur in micas and clays. Together with some material osition of beryllium in connection with processes of absorbed from solution, these probably account for the weathering and sedimentation has been only partly small amount of beryllium found in shales. Gold- worked out. The tendency for beryllium to follow schmidt and Peters (1932, p. 367) found 0.001 percent aluminum in these processes applies only where the two BeO in a composite sample of 36 shales. metals are in solution in surface waters, and it is due to A detailed study of beryllium in some Italian sedi­ their precipitation as hydroxides under alkaline condi­ ments was made by Pieruccini (1943; see also Carobbi tions. A similar tendency in relation to iron and man­ and Pieruccini, 1941), the results of which are sum­ ganese might be expected. Apparently, little beryllium marized below: is transported in surface waters under prevailing con­ Num­ BeO ditions of temperature and pH. Its concentration in ber of Percent sam­ sediments of chemical origin is, therefore, unlikely and Rock ples High Low Average is more to be expected in residual deposits; such as Sandstone. 8 0. 00070 0. 00030 0. 00045 laterites, in which aluminum, iron, and manganese are Shale___. 4 . 00056 . 00030 . 00050 Limestone. 4 . 00056 . 00036 . 00039 concentrated. Strock (1941b, p. 860) found 0.001 ppm of beryl­ Pieruccini found that in coarser sediments most of lium in the waters of Saratoga Springs, N. Y.; the the beryllium is in the cement and that the amount is beryllium probably is nonmagmatic in origin. In dis­ larger where the cement is argillaceous. Some of the cussing the presence of zirconium in the same water, he marls he tested have comparatively high beryllium con­ postulated that it was in solution as the complex zirco- tent; in others the cementing calcite is low in beryllium, nocarbonate ion (ZrO(CO2) 2)~2, and says (p. 868), thus reducing the BeO content of the rock. He em­ "Beryllium should form an even more stable complex phasizes the role of source rocks in the beryllium con­ anion than ZrO, and the fact that BeCO8 is formed only tent of sediments. Although no minerals of mafic ig­ in presence of excess CO2 and its known tendency to neous rocks were found in the sediments that were low form soluble double salts are undoubtedly manifesta­ in beryllium, the presence of elements such as copper, tions of its tendency to form such stable complex cobalt, nickel, and platinum in the samples suggests anions." Although this might be admitted as a possible these rocks as a probable source of the sediments. mode of transport of beryllium in natural waters, it is Few clastic sediments were sampled in the present in­ difficult to share Strock's conviction without experi­ vestigation, but many sedimentary rocks have been mental evidence for even the zirconium analogy. analyzed in connection with other investigations of the Apparently, beryllium has not been detected in sea Geological Survey. Unfortunately, the lower limit of water, but by analogy with aluminum, the expected beryllium determination in this work was 0.001 percent amount would be only 10~8 percent BeO, whfch is well BeO, and as the analyses did not detect beryllium in the below the limit of detection. Beryllium wrs not de­ majority of samples (see table 10), they give only a tected in limestones analyzed in the present investiga­ rough indication of beryllium content. A large propor­ tion (see table 10) nor in a series of flints and other sili­ tion of the samples are from phosphatic formations and ceous precipitates studied by Miropolsky and Borovick associated oil shales. The oil shales contain a little more (1944). Marine sediments which may be partly clastic beryllium than the phosphate rock, indicating that and partly chemical were found to contain < 0.001 per­ beryllium does not tend to substitute for phosphorous cent BeO in some deep sea cores from the Challenger in these sediments. expedition (Goldschmidt and Peters, 1932, p. 367), and A maximum of 0.004 percent BeO was found in each an average of 0.0037 percent BeO was found in three of two shale specimens of Devonian age sampled: the cores from the Mediterranean (Landergren, 1948a). Helms formation north of Van Horn, Tex., and the Beryllium might be expected in bauxite an^ clay de­ Chattanooga shale from Tennessee. The former con­ posits because of its association with aluminum and tains veinlets of gypsum, limonite, and several fine­ with alkalic igneous rocks from which such deposits BERYLLIUM IN SEDIMENTARY ROCKS 27 TABLE 10. Beryllia content of sedimentary rocks, other than coal, in the United States

Number BeO content * Sediment Age Formation Locality of samples' High Low Average

aands tones

»1 0.007 Maury, Meridan. Do...... »1 .004 Do...... »19 <0.001 <0.001 <.001 Tertiary «*7 <001 <001 <001 Do...... do...... «4 <001 <001 <.001 >3 <001 <001 <.001 ... ..do...... *1 <001 Sand (gold placer) _____ .... .do...... 819 <.001 <001 <001 Sand (titanium placers)...... do...... 2 <001 <001 <001 .... .do...... >3 <.001 <001 <001 ... ..do...... »«3 <001 <001 <001 .... . do...... «1 .0004

Shales

Pennsylvanian . Stigler- ...... »3 0.001 <0.001 <0.001 Do . «1 <.001 «1 flfU «5 .002 «<.001 (2) .001 Maury, Meridan. Do. ._- Permian 84 <.001 <.001 <.001 Do .... .do...... do...... »2 <.001 <.001 <001 Do >4 .0001 <0001 .0001 "Wlitfvi n*%/4 Tftf»lrQnTi nAiinHfls T'ftnti >9 .003 «<.001(8) <001 Do 826 .001 *<.001 (19) <.001 Siltstone and shale. ____ Canutillo- ... Franklin Mountains. £1 Paso County. *3 <.001 <.001 <001

Limestones

1 <0.000- Do...... 1 <,000<

Miscellaneous

Residual manganese... *1 0.05 Do...... 31 .03 Do...... «1 .02 Do ...... Batesville district, Pike County, Ark. .... *6 0.01 0.008 .01 Do...... *2 , -02 .01 .01 County, Va. Do...... do.- ...... *3 .01 .006 fWV7 «13 .01 .006 .009 ings). 322 .001 <.001(17) <" 001 37 <001 <001 <001 ?...... ? .. 7 .001 *<.001(6) <001 Do ...... ? ?- .-...... »11 <001 <.001 <001

i Samples collected in the present investigation, unless otherwise noted. < Concentrate or tailings sample only. 1 BeO determined on plates exposed for general scanning, not for determination ' Number in parentheses indicates the number of analyses in which beryllium of BeO alone. was not detected. > Samples collected by the Mine, Mill, and Smelter Survey, IT. S. Geological Survey. 28 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES commonly are derived. Samples of bauxite from vari­ In the Embreeville district, Tennessee, rapid weather­ ous localities have been analyzed for beryllium with ing of the Shady dolomite of Cambrian ag^ has pro­ disappointing results, as indicated below: duced minable concentrations of iron, manganese, zinc, Locality Percent BeO Reference and lead (Secrist, 1924, p. 141-145). Samples taken at Jamaica. ______0.05 0) the Embree mill by the U. S. Geological Surrey in 1943 Arkansas..______. OOOX to 0. 0006 0) and Goldschmidt and showed as much as 0.08 percent BeO in the tailings and Peters (1932, p. an average of 0.03 percent. Although analyses of the 367). Hungary______. 005 to 0. 01 Szelenyi (1937). unweathered Shady dolomite are not available, the high Yugoslavia______. 0038 Minguzzi (1943). beryllium content of the ore suggests that beryllium has France..______. OOX Goldschmidt and Peters (1932. p. been concentrated with the other elemerts during 367). weathering. Haiti. 0008 Goldich and Bergquist (1947, COAIi DEPOSITS p. 76). Dominican Republic- .0006 Do. That beryllium tends to be concentrated in certain Dutch Guiana_____ .001 0) plants was discovered by Sestini (1888), wl o believed 1 Unpublished analyses from the files of the U. S. Geological Survey. that beryllium replaced magnesium in the pTant tissue. Many of the kaolinites analyzed by Wheeler and Apparently, there has been no further investigation of Burkhardt (1950) are also of low beryllium content. beryllium enrichment in plants during growth. Numer­ Comparison of beryllium content of the Arkansas baux­ ous analyses of coal ash indicate that beryllium tends ites and kaolinites with that of the nepheline syenites to be concentrated during plant decomposition and coal and pulaskites similar to those from which they were formation. Goldschmidt (1937, p. 669) estimated derived (see table 8), indicates that the beryllium was beryllium to be enriched by a factor of about 50 in the concentrated much less than aluminum, contrary to average coal. The details of the enrichment process theoretical expectation. Data are as yet too few, how­ are discussed by Haberlandt (1944) who, I? analogy ever, to support any conclusion regarding beryllium with germanium, concludes that beryllium and other concentration in bauxites and residual clays. trace elements were concentrated in coal as stable Landergren (1943,1948b) determined the beryllium organic complexes similar to porphyrin (pyrrolidine). contents of several hundred iron ores of all types, most­ The first comprehensive study of trace elements in ly from Sweden, but including samples from elsewhere coal was by Goldschmidt and Peters (1933), who found in Europe and the United States. The lateritic iron a maximum of 0.1 percent BeO (average 0.07" percent) ores of Northern Ireland were all below the limit of in ashes of coal from England and Germany. Zilber- sensitivity 0.001 percent BeO. Finnish bog iron ores, mintz and Rusanov (1936) studied ashes of more than which are more strictly precipitates, were also mostly 600 coal samples from Russia and found 38 with more below the limit. Oolitic and other marine types aver­ than 0.001 percent BeO; 3 contained more than 0.01 aged 0.001 percent BeO. Goldschmidt and Peters percent, and 1 contained 0.04 percent BeO. Similar (1932, p. 368) did not detect beryllium in the few sam­ investigations conducted by Nazarenko (1937) in Rus­ ples of iron ore they analyzed, including the Clinton, sia, Lopez de Azcona and Puig (1947) in Spain, Reyn­ N. Y., material. A sample of limonite from New Zea­ olds (1948) in the United Kingdom, and Uzamasa land was reported to contain 0.01 percent BeO; in an­ (1949) in Japan and Manchuria revealed small other, beryllium was not detected (Becker and Gad- amounts of beryllium in the ashes of coals from these dum, 1937). countries. A summary of the literature on trace con­ Although Goldschmidt and Peters (1932, p. 368) did stituents in coal was compiled by Gibson and Selvig not detect beryllium in several samples of residual man­ (1944). ganese ore, the manganese deposits sampled by the U. S. The beryllium content of 21 samples f ron a number Geological Survey during World War II showed an of Colorado, Wyoming, Virginia, and Wes* Virginia average of about 0.01 percent BeO (see table 10). In coal fields are given in table 11. most of these deposits the manganese came from quartz- TABLE 11. Beryllia in ash of coals of the United States ites and dolomites of early Paleozoic age, but they may Numba of BeO content (percent) have undergone more than one cycle of concentration Formation Location samples Age ' High Low Average (Stose and Miser, 1922, p. 52-55). Available analyses Late Cretaceous- Mesaverde. 9 0.0025 <0.0006 0.0013 Do.. ------do Wyoming 2 .001 .0008 .0009 indicate no separation of beryllium between concen­ Do . Vennejo .... Colorado- 3 .0017 .0008 .0011 Do. Laramie--. do - 2 .0008 <0.0006 .0004 trates and tailings during milling of the manganese ore. West Virginia-­ 1 .014 Do... . Virginia-- 3 .01 .0014 .004 The beryllium mineral is not known. Do . West Virginia.. 1 .006 BERYLLIUM IN METAMOBPHIC ROCKS 29 Ashes of eastern coals of Carboniferous age average in pyrometasomatic deposits at Lupikko, Finland 0.008 percent BeO. Ashes of western coals of Cretace­ (Trustedt, 1907), Schwarzenburg, Germany (Peck, ous age, however, average about 0.001 percent BeO, 1904), Bartlett, N. H. (Huntington, 1880), and Casa which corresponds to the average content of shales or La Plata, Argentina (Fischer, 1925; 1926). Gold­ of igneous rocks. The reason for the different BeO schmidt and Peters (1932) devoted a great deal of their contents in coals of Carboniferous and Cretaceous age study of the geochemistry of beryllium to this type of and the manner of occurrence of the beryllium in the rock. Landergren (1948b) determined beryllium in coal is not known. several pyrometasomatic deposits in Sweden. The ana­ Beryllium has been looked for but not found in a lytical results for European localities are given in table number of marine plants (Cornu, 1919), but traces have 12. The discovery of idocrase of high beryllian content been found in algae (Lagrane and Tchakirian, 1939). There seems to be little concentration of beryllium dur­ TABLE 12. Beryllia in pyrometasomatic rocks from Gernany, ing the formation of petroleum, as only traces have Norway, and Sweden [All analyses of rocks from Sweden from Landergren (1948b)t> others from Gold­ been found in petroleum ashes (Katchenkov, 1948). schmidt and Peters (1932)] Number BeO (percent) BERYLLIUM IN METAMORPHIC ROCKS o/7 Description Locality samples High Average Only isochemical metamorphic rocks (those which Skarn2-magnetite _ Nordmark region, 6 0.03 0. 01 Sweden. have not received metasomatic additions of material Banded quartz- Skinnskatteberg 12 .03 .01 while being changed by heat and pressure) are included hematite, skarn- region, Sweden. magnetite, sul- under this heading. Some calc-silicate rocks which may fides. belong in this category are discussed with the pyrometa- Quartz-magn etite, Silvberg-Sater 6 .03 .01 skarn-hematite_ region, Sweden. somatic deposits, with which they are associated. Meta­ Grossularite a- Thale-Friedrichs- 1 .01 morphic rocks as thus defined would be expected to show diopside-wollas- brunn, Germany. little difference in composition from the sedimentary or tonite hornfels. igneous rocks from which they were derived. Local Grossularite 3- Braulage, Ger- .01 diopside-an- many. concentrations of beryllium by the processes of meta­ orthite hornfels. morphic differentiation are conceivable but probably Skarn-magnetite, Persberg region, .02 .007 cummingtonite. Sweden. rare. Calcite-magnetite, Norberg region, 17 .03 .007 Analyses for beryllium have been made of a large quartz-hematite, Sweden. actinolite-skarn- number of schists and gneisses from a wide range of magnetite, metamorphic facies, principally in Finland (Sahama, others. Skarn-magnetite. _ Uppland region, 12 .02 .006 1945a, p. 38-39), Sweden (Landergren, 1948b, p. 77-78), Sweden. and Greenland (Wager and Mitchell, 1943, p. 286-287). Calcite-magnetite. Stallberg, Sweden. .008 . 006 Diopside-skarn- Garpenberg region, .02 .004 In more than 80 percent of these rocks the content was magnetite. Sweden. below the limits of detection; which ranged from 0.003 Skarn-magnetite, Sodermanland re- . 008 . 004 quartz-magne- gion, Sweden. to 0.0003 percent BeO. Of those in which beryllium tite. was detected, quartz-biotite schist from the Striberg Amphibole skarn, Nora-Viker re- 4 .03 . 004 cummingtonite gion, Sweden. iron district in Sweden contained 0.011 percent BeO, skarn, quartz- but the rest were below 0.005 percent. No rocks of this amphibole skarn. Anorthite-cordi- Thale-Friedrichs- 1 __.. .001 type were sampled during the present investigation; a erite hornfels. brunn, Ger­ few recent analyses of metamorphic rocks by the Geo­ many. Anorthite-diopside Aarvold-Grorud, 1 ___ .001 logical Survey show little or no BeO. hornfels. Norway. Grossularite-diop- Aro, Norway _ 1 _.--.- .001 side hornfels. BERYLLIUM IN PYROMETASOMATIC AND RELATED Skarn-magnetite... Grythyttan re­ 4 <. 003 <. 003 DEPOSITS gion, Sweden. Manganoan oli- Ljusnarsberg re- 9 <. 003 <. 003 PREVIOUS AJTD PRESENT INVESTIGATIONS, vine, magnetite, gion, Sweden. mica, others. Pyrometasomatic deposits containing beryllium were Skarn-magnetite, Norrbarke region, 3 <. 003 <. 003 quartz-skarn- Sweden. first described by Goldschmidt (1911) in his monu­ magnetite. mental work on the metamorphic rocks of the region Anorthite-hyper- Aarvold, Norway. 1 _.__- <. 001 sthene hornfels. around Oslo, Norway. Helvite is associated with gar­ Andradite skarn. _ Grua, Norway 2 <. 001 <. 001 net, idocrase, diopside, magnetite, fluorite, and other i A total of 150 analyses, mostly of gangue from pyrometasomatic iron deposits. Some metamorphosed quartz-iron sediments included where associated with sll'eates. minerals in these deposits, which were regarded as hav­ Minimum content 0.003 percent BeO at all localities. * Skarn is a type of tactlte, generally rich in andradite and hedenbergite. ing little commercial value. Helvite was also reported a Grossularite or idoerase or both. 30 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES at Franklin, N. J. (Palache and Bauer, 1930, p. 31) and fluorite, in a tactite having a finely banded struc­ raised hopes that idocrase in other deposits might be ture of diffusion-replacement origin ("ribbon rock"). similarly rich in beryllium; however, Zilbermintz and Other tactites rich in magnetite, fluorite, g^ossularite, Koschkova (1933) showed that beryllian idocrase occurs idocrase, and other silicates contain less beryllium. only rarely. Although the deposit at Iron Mountain ir not ore at Interest in pyrometasomatic beryllium was revived present, it has focused attention on tactite deposits as by the discovery of helvite at Iron Mountain, N. Mex. potential sources of beryllium. The present investiga­ (Strock, 1941a). In a detailed survey of this deposit, tion included sampling of a large number of pyrometa­ Jahns (1944a; 1944b) found that beryllium occurred somatic deposits in the western United States. The in greatest amount as helvite associated with magnetite results are summarized in table 13, along with some

TABLE 13. Beryllia content of some pyrometasomatic and related deposits of the United States

Number BeO content Locality of Mineralogy * Associated metals * Associated intrusive samples' rocks* High Low Average

Bartlett, CarroU County, N. H __ . >2 1.6 1.0 1.5 Fe, Be...... Grani«.. chalcopyrite, fluorite, quartz. <<) 3.6 .4 .7 Do... . <<) .85 .1 .2 helvite, fluorite, chlorite. Magnet Cove, Hot Springs County, 1 .028 Fe.._._ ...... Nepheline syenite. Ark. Star mine, Elko County, Nev...... 3 .056 .0044 .027 W...... Biotiti granite, quartz calcite, scheelite. morsonite. 1 .022 DioriK biotite. Dragoon Mts., Oocbise County, Arlz.. . 4 .01 004 ».02 Pb, Zn....-_...... GranlX sphalerite. Victorio Mts. district, Luna County, 10 .1 .003 .02 W, Be...... RhyoMte porphyry. N. Mex. idocrase (0.2), fluorite. Victory tungsten deposits, Mammoth 1 .014 W ...... Qrancdiorite. Range, Nye County, Nev. ene(?). 1 .011 Quart T monzonite. Carpenter district, Grant County, N. 9 .02 <001 .01 Pb, Zn ... Di. Mex. garnet, chlorite, helvite. Qallinas district, Lincoln County, N. «1 «.008 Fe...... Syeni '<> porphyry. Mex. 6 .024 .0032 .0078 W...... Qrani^ to diorite. scheelite, pyrite. Oapitan district, Lincoln County, N. «1 «.005 Fe...... "ApliX" Mex. Wind Mtn., Otero County, N. Mex __ 10 .026 <.001 .005 Be...... Nephraline syenite peg­ wollastonite, garnet. matites. Cave Peak, Oulberson County, Tex .... 3 .0006 <004 <004 W, Be...... Grani*

Number BeO content Locality of Mineralogy > Associated metals' Associated ir<;ruslve samples ' rocks' High Low Average

891 KO. 001 Cu chalcopyrite, pyrite. Control mines, Oracle, Pima County, 81 K.001 Hornblende cUorite. Ariz. copyrite, galena, sphalerite. Greenhorn Mts., Kern County, Calif- 83 <0.001 <0.001 K.001 W, Mo . Granodiorite. lastonite, scheelite, pyrrhotite. 83 <.001 <.001 K.001 W, Pb, Ag. epidote, scheelite, pyrite, fluorite. Tungsten Hills, Inyo County, Calif.--. 27 .0045 <.0001 <.001 W. Granite, quartz mon- lite. zonite. Calumet mine, Chaffee County, Colo ... 7 <.001 <001 <.001 Fe Granodiorite. kaolinite, calcite, quartz, pyrite. Monarch mining district, Chaflee 6 <001 <001 <.001 Au County, Colo. pyrite, limonite. 3 <.001 <.001 <001 Au County, Colo. magnetite. Italian Mtn., Gunnison County, Colo.. 11 .0013 <.0001 <.001 Au ...... Quartz monz-mite. idocrase. Snowmass Mtn. area, Gunnison 8 <.001 <.001 <.001 Granite County, Colo. quartz, calcite, diopside. Tomichi Mining district, Gunnison 19 <.001 <.001 <001 Pb, Zn, Ag.. County, Colo. chalcopyrite, galena, sphalerite. 1 <.001 Pb, Zn Do. County, Colo. chlorite. Breckenridge mining district, Summit 3 <.001 <.001 <.001 Quartz monz-mite por­ County, Colo. phyry. >4 <.001 <.001 K.001 Cu ...... rite, pyrrhotite, fluorite, magnetite. Georgetown district, Deer Lodge 7 <.001 <.001 <.001 Granodiorite, County, Mont. blende, epidote. Garnet district, Granite County, Mont. 2 <00l <.001 <001 Do. Philipsburg district, Granite County, 3 <.001 <.001 <.001 Do. Mont. serpentine. Red Lion district, Granite County, 2 <.001 <.001 <001 Quartz, limonite, sericite, dolomite _ Au Do. Mont. 891 Zn.. sphalerite, willemite. 83 <.001 <.001 KOOl gopite, calcite. 83 <001 <.001 K001 Utah Counties, Utah. diopside, tremolite, quartz, scheelite. granodioriti. 85 <001 <.001 K.001 Utah. dote, garnet, diopside. Little Cottonwood mining district, 82 <.001 <.001 K.001 Ag, Cu, Pb-- ~ Do. Salt Lake County, Utah. K.001 Ph AIT Utah. porphyre d'vQS. Garfleld Peak, Natrona County, Wyo 1 <001 Latite. 5 .002 «><.0004 (1) 1.0009 donite, garnet. Mt. Silver Heels, Como, Colo... ___ 3 .0010 .0004 .0008 AU Do. 3 .001 .0005 «.0007 Pb, Zn. Granite (?). N. Mex. sphalerite. 82 .0005 <; 0001 K.0005 Cu, Zn magnetite, chalcopyrite. phyries. 6 .0013 <.0001 .0005 biotite, garnet. 2 .0008 <.0003 0.0004 Pb, Zn Granodiorite, N. Mex. sphalerite. 1 .0004 Cu pyrite. 2 <;.ooo4 <" OfWU 1 <" OfWU Cu Tombstone, Cochise County, Ariz ... 4 .0007 <.0004 K.0004 Garnet, calcite, tremolite, idocrase Ag, Pb, Cu, Mn_. Granodiorite 4 <.0004 <.0004 6 <" mfii W .... wollastonite. 9 .002 <.0004 K.0004 Cu - porphyries and aplites. Mineral Hill and Twin Buttes districts, 14 .001 <.0004 «<.0004 Garnet, quartz, epidote, pyrite.. Zn, Pb, Cu, W .... Granodiorite granite. Pima County, Ariz. 9 <.0004 <.0004 K.0004 Ariz. sphalerite. granite porphyry. See footnotes at end of table. 32 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES

TABLE 13. Beryllia content of some pyrometasomatic and related deposits of the United States Continued

Number BeO content Locality of Mineralogy4 Associated metals 2 Associated intrusive samples ' recks 2 High Low Average

Cimarroncito district, Colfax County, 4 <0.0004 <0.0004 5<0.0004 Garnet, diopside, hematite, horn­ Cu - Quartz nronzonite. N. Mex. blende, pyrite, chalcopyrite. Elizabethtown, Colfax County, N. Mex. 3 <.0004 <0004 5<0004 Diopside, hornblende, seapolite(?) Au ... - Monzoni a porphyry. Do...... -.-_. . 3 .0004 10 <.0004 (2) »<0004 Fe Do. Organ Mts., Dona Ana County, 9 .0004 i° <.0004 (8) 5 < 0004 Garnet, quartz, hematite, sphalerite, Cu, Ag, Pb. Monzoni'o to quartz N. Mex. altaite. monzorfte. Eureka district, Grant County, N. Mex. 7 <0004 <.0004 8<0004 Cu, Mo, W __ Monzoni'r}. 1 « < 0004 Fe.-- Quartz ironzonite. 10 .0008 10 <0004 (8) 5 < 0004 Garnet, hedenbergite, epidote, mag­ Zn. Do. netite, ilvaite, pyrite, sphalerite. Pinos Altos, Grant County, N. Mex. - . 2 <0004 <0004 «<0004 Calcite, sphalerite, pyrite, chalco­ Granodicrite. pyrite. Santa Rita, Grant County, N. Mex . 10 .001 <.0004 5 < 0004 Epidote, garnet, pyrite, chalcopyrite, Cu, Zn ..... Quartz nronzonite. magnetite. Apache Hills, Hidalgo County, 4 <.0004 <0004 «<0004 Garnet, epidote, pyrite. Cu, W -..--- Quartz monzonite por­ N. Mex. phyry. Peloncillo Mts., Hidalgo County, 3 <.0004 <0004 5 < 0004 Pb, Zn._ ... . Monzonite porphyry. N. Mex. Jones Camp district, N. Mex _ - _ - _ «1 5 < 0004 Fe-.. ... Diabase. Tres Hermanas Mts., Luna County, 2 <0004 <0004 5 < 0004 Zn. . .. Granite porphyry. N. Mex. Ortiz district, Santa Fe County, N. Mex. 2 <0004 <.0004 «<0004 Cu . Syenite. San Pedro district, Santa Fe County, 11 <.0004 <0004 5<0004 Garnet, calcite, hornblende, epidote ... Cu,W.. _ ... Do. N. Mex. Potosi district, Humboldt County, Nev. 85 .0003 <0001 .0003 W, Cu, Au, As . Granodiorite. Rawhide district, Mineral County, Nev 12 .0028 <0001 .0002 W '- Granite. Ouray mining district, Ouray County, 2 .0002 .0002 .0002 Garnet, magnetite, epidote, quartz, AJI Quartz monzonite. Colo. limonite. Beaver-Tarryall mining district, Park 7 .0001 .001 .0001 Garnet, epidote, magnetite, quartz, Au - ... Do. County, Colo. calcite, phlogopite. Geneva claims, Chafiee County, Colo.. 3 <0001 <0001 <0001 Molybdenite, garnet, pyrite, galena, Mo. _ - ___ - Granite. calcite. Georgetown area, Clear Creek County, 1 <0001 None Do. Colo. Gold Brick mining district, Gunnison 2 <0001 <0001 <0001 Garnet, magnetite, quartz, pyrite, Au - _ -. Diorite ?nd granite. County, Colo. chalcopyrite. Tincnp mining district, Gunnison 3 <0001 <0001 <0001 Magnetite, garnet, specularite, epi­ Fe. Quartz c"iorite. County, Colo. dote. Rush Basin area, Montezuma County, 1 <0001 Garnet, specularite, epidote, quartz ... None. . - Monzon'te. Colo. Montezuma mining district, Summit 2 <0001 <0001 <0001 Garnet, epidote, quartz, sulfldes...... Au...... Quartz nonzonite. County, Colo. Toll Mountain area, Deer Lodge 1 <.0001 Garnet, diopside, hedenbergite _ None . . Granite. County, Mont. Neihart-Yogo Peak area, Cascade 3 <0001 <0001 <0001 Pyroxene, epidote, garnet, calcite, Lamproihyre. County, Mont. prehnite, thomsonite, orthoclase, idocrase, magnetite, wollastonite, sphene, eudialite, merwinite. Elkhorn mining district, Jefferson 3 <0001 <0001 <0001 Epidote, garnet, pyrrhotite, calcite, Pb, Zn...... Granite. County, Mont. scapolite. Spring Hills mine, Lewis and Clark 1 <0001 Garnet, ollvine, scapoHte, titanite, Au ...... Diorite. Counties, Mont. epidote. Silver Star mining district, Madison 2 <0001 <0001 <0001 Hedenbergite, garnet, epidote, horn­ All Granite. County, Mont. blende, calcite, magnetite, pyrrho­ tite. Ophir mining district, Powell County, 1 <0001 Garnet, epidote, calcite Au ...... -. Quartz monzonite. Mont. Priests Pass area, Powell County, 1 <.0001 Au ...... Do. Mont. Highland mining district, Silver Bow 2 <0001 <0001 <0001 Garnet, epidote, magnetite, diopside, Diorite and quartz County, Mont. actinolite, pyrite, chalcopyrite. monzcnite. Haystack Stock, Sweet Grass County, 1 <0001 Garnet, epidote, quartz, actinolite None _ .-.. . Quartz monzonite. Mont.

1 Samples collected by the U. S. Geological Survey during the present investigation, o Samples collected by V. C. Kelley, U. S. Geological Survey. unless otherwise noted. ' Samples furnished through courtesy of the New Jersey Zinc Co. * Minerals, metals, and intrusive rocks spacially associated in the mineral deposit, »Samples collected by Mine, Mill, and Smelter Survey, U. S. Geo'ogical Survey. not necessarily related in time or genesis. Known beryllium-bearing minerals in Tailings or slag samples only. italics, their maximum beryllium content for that deposit in parentheses. » Numbers in parentheses indicate number of samples having a BeO content 3 Samples collected by D. M. Henderson, University of Illinois. below limit of sensitivity. * Data from Jahns (1944a, p. , 76). i' Six of the samples collected by J. R. Cooper, U. S. Geological Survey, ' Determinations on plates for general scanning, not for precise determination o i* Sample collected by Elliot Gillerman, U. S. Geological Survey. BeO alone. BERYLLIUM IN PYBOMETASOMATIC AND BELATED DEPOSITS 33 earlier determinations from the files of the U. S. Geo­ marmorization of limestone but before intense reiolace- logical Survey. The minerals, metals, and intrusive ment. According to Osborne (1932, p. 221-222), ido­ rocks of each deposit are also tabulated, although in crase may be "generated during retrogressive meta- most places they probably are unrelated in origin and morphism with which was associated a change pro­ time of deposition to the beryllium. moted by falling temperature, and at pressures under Extensive sampling shows that only a small number which grossular was not stable. . . The data available of pyrometasomatic deposits contain more than 0.001 concerning the various grades suggest that while this percent BeO, the average for the earth's crust. Only mineral may occur with grossular and wollastonite, it 15 percent of the United States deposits sampled con­ is also stable in a lower grade where these two minerals tain more than 0.005 percent BeO. The Swedish de­ fail to develop." The nature of the implied pressure posits are of somewhat better grade. In most of the change is not discussed. Tilley (1927, p. 375) sug­ pyrometasomatic deposits that have been analyzed gested that both idocrase and grossularite might form throughout the world, beryllium was not detected. at lower temperatures than normal when subjected to the shearing stresses of regional metamorphism. CHARACTERISTICS OP BERYLLIUM-BEARING A further reason for the association of beryllium and DEPOSITS idocrase may be due to fluorine. Fluorine-rich idocrase Some of the common minerals in the beryllium-bear­ and fluorite are common minerals in beryllium-bearing ing pyrometasomatic rocks are helvite, idocrase, garnet deposits and thus may be a clue to the occurrence of (mostly andradite), magnetite, fluorite, scheelite, and helvite or other beryllium minerals. Although the ido- diopside-hedenbergite. Theoretically, these minerals crase-fluorite association is not found in all pyrometa­ may form in any metamorphic temperature and pres­ somatic deposits containing beryllium, the Darwin, sure facies from "pyroxene hornfels" down to "epidote Calif., deposit is the only one sampled at which these amphibolite" (Turner, 1948, p. 70-90). Paragenetic minerals were found without beryllium. Idocraso with­ data from the few deposits studied in detail indicate out fluorite or beryllium was found at several localities. that deposition of helvite is possible through this en­ In the Carlingford district, Ireland, are several varie­ tire range of temperature. ties of idocrase, some associated with simple isochem- ically metamorphosed limestones, and others associated Idocrase commonly is associated with helvite in with "pneumatolytic" alteration around pegmatites. beryllium-bearing tactites. (See table 13; also tables Regarding the associations, Osborne (1932, p. 222) says, 12 and 13 of Glass, Jahns, and Stevens, 1944). Be­ "Where pneumatalytic metamporhism operates in an cause grossularite and idocrase are similar in structure aureole, fluorine, if available, enters the constitution of and composition, although idocrase is slightly poorer vesuvianite, but it is suggested here that vesu^ianite in aluminum, one might wonder why beryllium occurs which is due entirely to diaphoretic changes * * * will in idocrase-bearing tactites in preference to grossula- be fluorine free." The implication that fluorine-rich rite-bearing tactites. Idocrase in normal metamor­ idocrase and associated products are of pneumatolytic phosed limestones may form in equilibrium with gross­ origin may be valid. In the absence of experimental ularite and diopsicle, grossularite and calcite, or diop- data the nature of the beryIlium-fluorine relations in side and calcite (wollastonite may take the place of pyrometasomatic deposits remains conjectural. calcite at higher temperatures), but only if the com­ Magnetite and scheelite are commonly found in de­ position of the rock is less aluminous than grossularite posits containing beryllium minerals. In most of the de­ itself (Turner, 1948, p. 91). Holser (1953, p. 607) has posits, however, helvite formed later than magnetite, noted in Victorio Mountains, N. Mex., that helvite mainly in open cavities. At Iron Mountain, N. Mex., forms in rocks having relative low alumina content. scheelite is also earlier than helvite. The heMte in At Rose Creek, Nev., beryllium occurs without the tactite in the Victorio Mountains may be exceptional aluminum garnet (grossularite), the principal minerals (Holser, 1953, p. 606) in that it appears to be contem­ being diopside, actinolite, and feldspar. Thus, among poraneous with the other silicates and to have formed metamorphosed limestones, beryllium is more likely to at relatively high temperature. Scheelite is present but be found in those that were originally low in argilla­ magnetite is not. ceous material and to which little alumina has been Most of the Nevada and California scheelite-l taring added in the metamorphic process. tactite deposits sampled during the present investiga­ Actually, the nature of equilibrium relations be­ tion contain more beryllium than the average pyrometa- tween idocrase and grossularite is in some doubt. Kerr somatic deposit (see table 13). As yet the beryllium- (1946a, p. 58) observes that both minerals form after bearing minerals in these deposits and their petitions 467945 59 4 34 OCCURRENCE OP NONPEGMATITE BERYLLIUM IN THE UNITED STATES in the mineral sequence are not known. The relation as granite or nepheline syenite and associated pyro­ between beryllium and iron or tungsten, although not metasomatic deposits. Actually beryllium-bearing clearly defined, is in marked contrast to the negative pyrometasomatic deposits are more commonly associ­ correlation of beryllium with copper, zinc, or lead. ated with rocks of intermediate composition, such as Landergren (1948b) found little correlation between granodiorite and monzonite. Though some 1 ^ryIlium type of ore and beryllium content in the pyrometaso- is found in the contact zone of feldspathoidal intrusive matic iron deposits of Sweden. In the United States, rocks, the tactite zones adjacent to these roc^s gener­ however, beryllium was not found in deposits contain­ ally are small and poorly developed. ing magnetite with olivine or derived serpentine like those at Fierro, N. Mex. The lack of beryllium can BELATED OCCURRENCES hardly be due to an excess of magnesium, as magnesium- Helvite at the Grandview mine, Carpenter district, rich pyroxene or amphibole is a common associate of New Mexico (Weissenborn, 1948), is nearly all found beryllium-bearing pyrometasomatic deposits and may as sharp, tiny tetrahedra on quartz and fluorit?. crystals occur in such a deposit to the exclusion of garnet. The in vugs and in veins. In some places the qi^artz was fact that olivine normally forms at higher temperatures coated with chalcedony before deposition of th^ helvite. than pyroxene or amphibole may account for the ap­ Although a small amount of garnet and other silicates parent lack of correlation between olivine and beryllium are found replacing the limestone in the Grandview in these deposits. mine, the manner of occurrence suggests that tl ^. helvite Jahns (1944b, p. 179-189) suggests that the banded is a low-temperature mineral, more closely related to and orbicular structures observed at Iron Mountain, N. vein filling than to pyrometasomatism. Mex., may be a clue to the presence of beryllium in tac- The zinc deposits at Franklin and Sterling Hill, N. J., tite. He notes that similar tactite were previously de­ bear little relation to any other deposits in the world, scribed from Seward, Alaska, and Pitkaranta, Finland. with the possible exception of those at Langl an, Swe­ The former was tested and found to contain beryllium. den (Palaehe, 1929b). The rare mineral barylite has In the latter area, helvite occurs in intimate association been found at only these two New Jersey localities. with idocrase andfluorite (Trustedt, 1907); theidocrase Brown idocrase, similar to that in which a large amount has been found to contain 0.18 percent BeO (Zilber- of beryllium has been found, is of rare occurrence in mintz and Rosehkova, 1933, p. 253). None of the beryl­ the Franklin mine, and the blue variety (cyprine), lium-bearing tactite sampled in the present investiga­ which contains a small amount of berylliunr, is even tion showed banding of this type, but banded and or­ rarer. Palaehe (1929a, p. 10-11) believed that these bicular structures are common in magnetite-serpentine minerals were a product of pneumatolytic action rocks that lack beryllium, as at Philipsburg, Mont., and around intruded late pegmatites. No beryl has been in the Quitman Mountains, Tex. found in the pegmatites, or elsewhere in the- district. Jahns (1944b, p. 196-204) postulates that the banded A large amount of beryllium at low concentration is beryllium-bearing tactite is of hydrothermal origin, in contained in the great masses of willemite ar«i associ­ contrast to massive tactites of simpler mineralogy, which ated zincian-manganian diopside. The pegmatites were may be pneumatolytic. He infers that the latter are formed after deposition of willemite and may have less likely to contain beryllium. The helvite deposit in reconcentrated a little beryllium in their vicinity. It the Victorio Mountains, N. Mex., is massive and of sim­ is a mystery why some of the beryllium does not occur ple mineralogical composition. The difficulty of dis­ as helvite, especially because of the excess of manga­ tinguishing the actions of liquid and gaseous solutions nese, zinc, and iron. at high temperature does not exclude the possibility Beryl is found in mica and amphibole schiHs at the that even this deposit may be hydrothermal. Whatever Izumrudnie (emerald) district of the southern Urals the details of their origin, such massive tactite cannot (Fersman, 1929, p. 74-116); Habachtal, Salzfrirg, Aus­ be excluded as possible sources of beryllium. tria (Koenigsberger, 1913); Leydsdorp, South Africa Results of analyses show that simple metamorphic (Le Grange, 1930); Keene, N. H. (Olson, 1942, p. 372); hornfels, quartzite, and marbles that surround tactite and the Black Hills, S. Dak. (Page and others, 1953, deposits are notably lacking in beryllium. It must be p. 46). At all of the localities for which detailed geo­ presumed to have been added to the tactite, along with logic description is available, the beryl is near granitic other constituents, by solution probably derived from pegmatites that are beryl-bearing. At the Tungsten an igneous source. The commonly held theories of mag- King mine, Arizona, beryl occurs in the chlorite schist matic differentiation imply that beryllium should be in the hanging wall of the quartz-beryl-tung^ten vein. concentrated with late products of differentiation, such More remarkable are two similar occurrences in which BERYLLIUM DST VEIN DEPOSITS 35 the beryl is in marble (Just, 1926; Chhibber, 1945). walls; and at Mount Antero, Colo., and Irish Creek, Studies of these deposits indicate that the beryllium has Va., it immediately follows the formation of some of been added to the wall rock from the pegmatite or vein the quartz. In a few places, as at Hill City, S. Dak., (see also Stoll, 1945). Apparently, this mode of oc­ and Irish Creek, Va., the beryl-bearing quartz veins currence is rare for beryl, as most beryl pegmatites do contain cassiterite instead of tungsten minerals. Stu­ not introduce beryllium into the wall rock even in trace dies of foreign deposits (Tetyaev, 1918; Turner, 1919) amounts. In most of the deposits mentioned, the beryl where both tin and tungsten occur in the veins indicate in the wall rock is much less abundant than in the as­ that cassiterite may be later in the mineral sequence sociated pegmatites. With the exception of the Urals than tungsten minerals. At Irish Creek, cassiterite deposits, which are quite large, they are of little eco­ and beryl are nearly contemporaneous (Koschnann, nomic importance unless the beryl is of gem quality. Glass, and Vhay, 1942, p. 280). The occurrence of beryllium in quartz veins cortain- BERYLLIUM IN VEIN DEPOSITS ing tin and tungsten suggests that it might also H ex­ Beryllium minerals, chiefly beryl or helvite, have been pected in molybdenum deposits. Molybdenite is a found sparsely disseminated in certain types of veins. major constituent in a beryl-bearing vein at Mount An­ Such veins generally contain ores of useful metals and tero, Colo., and at the Black Pearl mine, Yavapai are thus well suited to recovery of beryllium as a by­ County, Ariz., and the two minerals occur togetHr in product. The published descriptions of beryl-bearing several veins in Asia. However, most of the molyb­ veins are tabulated and discussed by Holser (1953, p. denite deposits in the United States that have been 604-605 and Adams, 1953). More than 100 high-tem­ tested contain little beryllium, including those at Cli­ perature veins in the western United States were sam­ max, Colo., Red River, N. Mex., and Bunker Hill, Ariz. pled and analyzed for beryllium. Previously, a large Although the content of beryllium probably varies number of vein samples collected by the U. S. Geologi­ markedly throughout a given vein, as is true for tung­ cal Survey had been analyzed qualitatively. These sten, it appears to average O.OX percent BeO for those analytical data are summarized in table 14. Analyses tungsten veins in which beryllium is present. In two for several miscellaneous deposits that are not strictly veins sampled in detail (Tungsten King mine, Little veinlike are included in the table. Dragoon district, Arizona, and Eloi claim, Victorio Those veins in which beryllium minerals have been Mountains, New Mexico), there is no correlation be­ noted, as well as those in which beryllium was found by tween tungsten and beryllium content, although most sampling, fall largely into three groups: quartz-tung­ samples high in beryllium content also contained ap­ sten veins; quartz-gold veins; and manganese-lead-zinc preciable tungsten. The vein system at the Tungsten veins. King mine extends for several thousand feet but has QUARTZ-TUNGSTEN VEINS been sampled for beryllium over only a small ps.rt of Beryllium appears to be more common in quartz- its length. tungsten veins than in other kinds of veins, the asso­ Some veinlike bodies that are otherwise similar to ciation having been noted at a dozen or more localities those described above contain feldspar (Norman, 1945 ; throughout the world. In some deposits, as exemplified Carne, 1911, p. 58,67) and are probably transitional be­ by the Boriana mine, Moliave County, Ariz. (Hobbs, tween the quartz-tungsten-beryllium veins and quartz- 1944, p. 254), the quartz veins contain fluorite, wol­ rich parts of pegmatites. Several of the quartz-tung­ framite, and sulfides. Generally, beryllium occurs in sten-beryllium veins appear to be related to neighbor­ beryl, which is found only in small amounts. In some ing pegmatites. veins of this type the beryl may be altered to phenakite QUARTZ-GOLD VEINS or bertrandite, but no helvite has been noted. In the Tungsten King mine, Arizona, beryl occurs in a Samples of gold ores from the epithermal veins in scheelite-bearing vein. However, scheelite veins in Ne­ the Oatman district, Mohave County, Ariz., and the vada and California sampled during the present inves­ hypothermal veins in the Bald Mountain district, tigation contain little or no beryllium; this indicates Lawrence County, S. Dak., contain about 0.01 percent that beryllium and tungsten are not invariably asso­ BeO (see table 14). In both districts (Wilson, Cun- ciated. ningham, and Butler, 1934, p. 80-115; Connolly, 1927, Beryl occurs early in the mineral sequence in the few p. 60-94) the gangue includes carbonates and fluorite. instances where it has been studied. At the Victorio The beryllium-bearing mineral has not been deter­ Mountains, N. Mex., deposits, it forms a selvage on the mined. 36 OCCURRENCE OP NONPEGMATITE BERYLLIUM IN THE UNITED STATES

TABLE 14. Beryllia in some veins and related deposits in the United States

Number Percent BeO Locality of sam­ Mineralogy » Principal metals ples i High Low Average

7 0.02 0.005 0.02 W. Mount Antero, Chaffee County, Colo.: California si .016 Me. mine. Providence Mts., San Bernardino County, Calif.: 2 .01 .01 «.01 W. Scbeelite Ray mine. Little Dragoon Mts., CocMse County, Ariz.: 4 .052 .0008 .01 Quartz, scheelite, beryl, chlorite. _ __ ...... W. Tungsten King mine. 457 .03 7<.001(3) t.Ol An. Bald Mtn. district, Lawrence County, 8. Dak _ . «4 .02 .01 t.Ol Quartz, dolomite, glauconite, pyrite, gold, ar- An. senopyrite, sylvanite, fluorite. Thomas Range, Juab County, Utah: Bell Hill 1 s.OOX Fluorite, clay, hematite, calcite ______F. mine. Vanee County, N. 0.: Hamme mine ______««3 .008 004 8.007 W. Warren and Lyman, Grafton County, N. H. __ «2 .006 006 «.006 Zn Pb. Apache district, Sierra County, N. Mex.: Mid­ 2 .01 <.0004 6.005 Quartz, bornite, garnet, epidote. __ ...... On. night mine. Red River, Taos County, N. Mex.: Questa mine 5 .004 .0005 .004 Quartz, calcite, molybdenite ______Mo. Butte district, Silver Bow County, Mont ____ ttK7 .0005 .003 Pb, Zn. pyrite, helvite. Black Range, Catron County, N. Mex.: Taylor 1 «.002 Sn Creek mine. Burro Mts., Grant County, N. Mex.: Long Lost 1 «.002 F. Brother claim. Creede district, Mineral County, Colo __ .. 2 .002 .002 5.002 Ag, An, Pb, Za. Terlingua district, Brewster County, Tex__ _ . <4 .005 <.001(3) ».002 Hg-. Holden, Chelan County, Wash.. ______««3 .001 '.001(1) «.001 On, Zn, An. Sundance area, Crook County, Wyo ______2 .OOX .OOOX 5.001 F. Mother Lode district, Eldorado, Calaveras, and ««23 .002 <.001 «.001 Quartz, gold, ferrodolomite, sericite, albite, An. Amador Counties, Calif. pyrite. Little Dragoon Mts., Cochise County, Ariz.: Blue­ »3 .0019 .0005 .001 Quartz, muscovite ("greisen"), huebnerite, W. bird mine. scheelite, taofite, beryl. Encampment district, Carbon County, Wyo. . _ . 2 .002 <.0001 .001 Chalcopyrite, pyrite, bornite, covellite, siderite, CL-. quartz, malachite, azurite. 2 <.001 <.001 <.001 Cu. limonite. Juneau, Alaska: Alaska-Juneau mine ______««1 «<.001 An, Ag, Pb. Metaline district, Pend Oreille County, Wash..... *28 <.001 <.001 «<001 Sphalerite, galena... ______Zn Pb. Northport district, Stevens County, Wash.: Van <1 8<.001 Galena, sphalerite, tetrahedrite ...... Zn Pb. Stone mine. Republic district, Ferry County, Wash.: Knob *1 «<.001 Quartz, tetrahedrite, pyrite, chalcopyrite ...... Ar. Hill mine. Mehama, Marion County, Ore______«3 <.001 <.001 «<.001 Zn Glen County, Calif.: Gray Eagle mine __ ... *5 <001 <.001 «<.001 Chromite .. ____ _ . _ Or. Guernerville, Sonoma County, Calif.: Mount 462 <.001 <.001 «<.001 Chalcedony, cinnabar, pyrite ...... Hf. Jackson mine. San Luis Obispo County, Calif.: Costro mine. _ . 4«2 <.001 <.001 5<.001 Or. Rociada, San Miguel County, N. Mex.: Azure 1 «<.0004 Ca. Chief mine. Willow Creek, San Miguel County, N. Mex.: 1 «<.0004 Zn, Pb. Pecos mine. line, pyrite, sphalerite, galena, chalcopyrite. Cherry Creek district, White Pine County, Nev 10 .0009 <.0001 .0003 W. Wauconda district, Okanagan County, Wash __ 44 .0003 <.0001 «.0002 Ar, Douglas County, Ore.: Bonanza mine ______*3 .0004 <.0001 «.0002 Hg. Clark Fork district, Banner County, Idaho: *4 .0003 <.0001 «.0002 PI. Whitedelf mine. Tincup district, Gunnison County, Colo _____ 6 .0013 <.0001 .0002 M->, W, An. quartz, pyrite. Gallinas district, Lincoln County, N. Mex.: Red »1 .0002 F. Cloud mine. Oroville district, Okanogan County, Wash ____ <4 .0002 <" nnni «.0001 PI , On. Marshall Lake district, Idaho County, Idaho. __ <4 .0004 <.0001 .0001 An, Ag. Monarch district, Chaffee County, Colo... ___ 3 .0004 <.0001 .0001 ....do..-...... Mi>. flfiflV <.ooox 6.0001 PI , Zn. clay, pyrite, chalcopyrite. Beaverhead County, Mont.: Poison Lake mine _ 1 »<.ooox F. spar, calcite. St. Peters Dome district, El Paso County, Colo.: 1 «<.ooox F, Pb, Zn. Sheffield claim. kasolite. Querida area, Ouster County, Colo ______1 .OOOX Ag. pyrargyrite. Mountain Pass, San Bernardino County, Calif .... 103 <.ooox <.ooox «<.ooox Ce, etc. Lake City district, Hinsdale County, Colo ...... 8 .0002 »<.0001(6) <0001 See footnotes at end of table. BERYLLIUM IN VEIN DEPOSITS 37

TABLE 14. Beryllia in some veins and related deposits in the United States Continued

Number Percent BeO Locality of sam­ Mineralogy1 Principal rentals ples i High Low Average

8 <0.0001 <0.0001

TABLE 14. Beryllia in some veins and related deposits in the United States Continued

Number Percent BeO Locality of sam­ Mineralogy > P -'ncipal metals ples ' High Low Average

Little Missouri R., Pike County, Ark... _ . __ .. <16 <0.001 <0.001 s <0. 001 Hg. «12 <001 <.001 «<001 Ar ««20 <001 <.001 «<001 Or, Fe. «7 <001 <.001 «<001 ZB, Pb. Mascot, Ktiox County, Term ...... _ 4«6 <001 <.001 «<001 ZB. Gratz, Owen County, Ky ____ . ______«6 <001 <.001 «<001 Zn, Pb. «12 <001 <.001 «<001 Cr Sanford Lake, Essex County, N. Y... ______««1 «<001 Ilmenite, magnetite ______. __ TI Fe, V. «11 <001 <.001 «<001 Cr copyrite. Virgilina, Halifax County, Va.: Red Bank mine... ««1 «.001 Ar Spottsylvania County, Va.: Valzinoo mine ____ «4 <001 <.001 «<001 PI , Zn. galena. i«l «<.00l Cr, Finley, Caldwell County, N. C...... _ ..... «2 <001 <.001 «<00l Ti. ««1 «<001 Ar-Ag. Kershaw, Lancaster County, S. C.: Haile mine.... ««1 «<.001 Ar Ag. Orange County, Vt.: Elizabeth mine ...... «3 <001 <.001 »<00l Cr, «1 «<001 PI , Zn. Marysvale, Piute County, Utah: Freedom No. 2 1 .001 «.ooox Fluorite, pyrite, wad, uranophane, autunlte, U. claim. pitchblende. 1 .0007 None. Canyon. Elko County, Nev.: Good Hope mine...... 1 .0007 Br, Climax, Lake County, Colo.: Climax mill ...... 10 .0006 .0001 .0006 M->, W. chalcopyrite, cassiterite. Animas Forks district, San Juan County, Colo .... 12 .0021 <.0001 .0006 Rhodonite, galena, sphalerite, pyrite, quartz Ar Ag. 5 .0017 <0001 .0006 W. 2 .0007 .0005 .0006 Ar, Sambo mine. 4 .0011 .0001 .0005 M-t, Bi, Au. 7 .0008 <.0001 .0005 W. Nev. Mineral Point district, San Juan County, Colo .... 4 .0016 <.0001 .0004 Galena, sphalerite, rhodonite, rhodochrosite, Ar Hg. pyrite. 1 *<.0004 Au, Mo. Deep mine. 4 <0004 <0004 «<.0004 W, Cu. American mine. Lordsburg, Hidalgo County, N. Mex.: Eighty- 3 <0004 <.0004 «<0004 Quartz, muscovite, hematite, chalcopyrite, Cr, flve mine. tourmaline.

i All samples collected during the present investigation by the U. 8. Geological * Mill concentrates or tailings only. Survey, unless otherwise stated. f Number in parentheses indicates number of samples having BeO content below »Mineral association in the vein, not necessarily related to time or origin. Listed the limit of sensitivity. in approximate order of abundance; known beryllium minerals in italics. * Samples collected by J. B. Cooper, TT. S. Geological Survey. * Samples collected by J. W. Adams, U. 8. Geological Survey. * Samples collected by U. 8. Bureau of Mines. 4 Samples collected by Mine, Mill, and Smelter Survey, U. S. Geological Survey. 1° Samples collected by J. C. Olson, U. S. Geological Survey. > Beryllium determinations on plates exposed for general scanning, not for quanti­ tative beryllium determinations.

A quartz vein cutting limestone at the Midnight MANGANESE-LEAD-ZINC VEINS mine in the Apache district, Sierra County, N. Mex., Originally described from Kapnik, Hungr.ry (Szabo, may be related to this type (Harley, 1934, p. 85). Ore 1882), beryllium-bearing veins of this type are found in from the vein, which contains gold and silver in ad­ the United States at the Sunny side mine, Colorado dition to bornite and other copper sulfides, was found (Burbank, 1933a, p. 521), and Butte, Mont, (Hewett, to contain 0.01 percent BeO. 1937). Khodonite, rhodochrosite, and other manganese The few veins of this type that we sampled showed little or no beryllium and there is little indication that minerals occur with quartz, helvite, and sulfides, with beryllium is at all common in quartz-gold veins. No helvite last in the mineral sequence. veins of this type are reported to contain tungsten, From mineral associations and structure relations we although at Bald Mountain, S. Dak., tungsten deposits infer that, the manganese-helvite veins are o* somewhat nearby are believed to be related in origin (Connolly, lower temperature than the tungsten-be^yl veins. 1927, p. 95-97). However, only veins that are rich in manganese contain BERYLLIUM IN HOT-SPRING DEPOSITS 39 helvite, in which manganese is an essential constituent. beryllium content of the crust; in particular the Be to We know of no vein deposit in which beryl and helvite Al ratio has not increased. are found. During the present investigation samples were taken OTHER VEINS from three tufa deposits that were presumably formed by hot springs no longer active. Data for these sr.mples The helvite-bearing vugs and veins of the Carpenter district, Grant County, N. Mex., are probably similar are tabulated below: BeO to manganese-lead-zinc vein deposits; the helvite seems Location Material (frcenf)1 to have no genetic relation to silicate minerals. Some Golconda, Humboldt Manganese-iron-tungsten- 0.016 County, Nev. rich tufa. rhodonite was found in the Grandview mine, although Do___-______Calcareous tufa (overly- <. 0001 not directly in association with the helvite. Fluorite, ing above-mentioned tufa). which is prevalent at the Grandview mine, is found Sodaville, Mineral County, Manganese-tungsten ore. . 007 also at the Sunnyside mine, Colorado, and at several Nev. of the mines in the Butte district, Montana. Cove Creek, Hot Springs Tufa______.003 County, Ark. The veins in Colombia (Oppenheim, 1948), from Ouray,Ouray County, Colo_ __do_.______.08 which most of the world's emeralds are mined, are 1 Analyses by U. S. Geological Survey. unique. Small fractures in limestones and shales are filled with calcite, dolomite, beryl, parasite, pyrite, The relatively large amount of BeO in the material quartz, and rarely barite and fluorite. from Golconda, Nev., presumably is due to deposition of beryllium with the manganese, iron, and tungsten. The BERYLLIUM IN HOT-SPRING DEPOSITS beryllium mineral in the deposit is not known; but as the tungsten has been adsorbed in amounts of as much Beryllium has not been mentioned in the many de­ as 6 percent in very fine grained masses of cryptomelane tailed reports on the chemistry of volcanoes or those and psilomelane without forming minerals of it" own on the volcanic f umarole and hot-spring areas of Yel- (Kerr, 1946a, p. 78-79; 1940, p. 1377-1387), the beryl­ lowstone and Katmai, but it may not have been specifi­ lium may have been similarly adsorbed. Shallow veins cally looked for. Using enrichment procedures, Ku- are associated with the tufa deposits, and a very close roda (1939, 1940) was able to detect a maximum of connection between hot springs, fumarolic, and ep ; ther­ about 0.000001 percent BeO in waters of a large num­ mal deposits seems well established. Deposits s'milar ber of the Japanese acid-sulfate hot springs. Beryl­ to those at Golconda are quite rare, and by analogy, lium was reported or its presence inferred in mineral the similar and much lower grade beryllium deposits springs studied by Mazade (1852), Bechamp (1866), cannot be expected to be important as a source of beryl­ and Fresenius (1933), but there is no indication of lium. If the beryllium is adsorbed in the manganese what proportion of these waters are juvenile. Detailed minerals, the recovery problems would be even greater geochemical data given by Strock (1941b) indicate that than they are for tungsten. the waters of Saratoga Springs which contain more Though of doubtful commercial value, the deposit of beryllium than yet measured in any other mineral Golconda may provide important information regard­ water are entirely meteoric, although the source of the ing the origin of beryllium in hot springs. Scheeli te de­ beryllium itself is not postulated. posits occur in the vicinity of Golconda, and Kerr points Beryllium has been noted at several localities in out that underlying scheelite or wolframite veinr may material deposited by hot springs. At Steamboat possibly have been the source of tungsten in the spring Springs, Nov., calcareous sinter and siliceous mud, both waters. In line with this reasoning, beryl-bearing of recent origin and rich in pyrite and stibnite, con­ tungsten veins or helvite-bearing tactites conceivably tained 0.0002 to 0.0008 percent BeO (Brannock, and may have furnished beryllium. The scheelite deposits others, 1948, p. 224). Ferruginous and calcareous ma­ of this region probably are related to Cretaceous intru­ terial from two hot springs in Sandoval County, N. sive rocks, whereas the hot-spring deposits are thought Mex., contained less than 0.0005 percent BeO, except for to be of Pleistocene age. The thermal waters may have one sample of ferruginous material that contained O.OOX leached tungsten and beryllium from the earlier deep- percent.4 Sediments in a carbonate mineral spring in seated deposits and carried these elements to tho sur­ Germany were found to contain 0.0016 percent BeO face. Beryllium-bearing hot springs may thus serve as (Rezek and Tomic, 1942). None of these deposits a guide to deposits of relatively high beryllium content represent appreciable enrichment over the average at depth. Sampling of all tactites and high-tempera­ ture veins in the vicinity of such springs seems war­ * Analyses by A. T. Myers, U. S. Geological Survey, of material col­ lected by C. S. Eoss. ranted. 40 OCCURRENCE OP NONPEGMATTTE BERYLLIUM IN THE UNITED STATES ASSOCIATION OF BERYLLIUM WITH OTHER ELEMENTS metric analyses for tungsten of samples from the Little A large proportion of the samples analyzed for beryl­ Dragoon Mountains, Ariz., and Victorio Mountains, lium in the present investigation were also analyzed N. Mex., showed no significant relation to beryllium de­ spectrographically for other elements. All samples terminations. Some correlation between beryllium and analyzed are included, whether or not they contained zirconium was noted in the f eldspathoidal rocks of the any beryllium. The data are compiled in table 15, by Raton volcanic region, New Mexico, and the Trans- States, districts, and sample number. Pecos Region of New Mexico and Texas. Many other spectrographic analyses for beryllium are Geochemical relations between beryllium and certain in the files of the U. S. Geological Survey, most having other elements, particularly tin, tungsten, aiH fluorine, been made during World War II in the countrywide are suggested by the mineral associations noted in beryl­ sampling of mine, mill, and smelter products. The lium occurrences in veins and pyrometasomatic deposits (see tables 13 and 14), although they are not without spectrographic data for those samples that showed more than 0.001 percent BeO are given in table 16. The exceptions. The apparent association of beryllium and fluorine is particularly striking. Fluorite occurs in two- analyses that showed 0.001 percent BeO or less have thirds of all the beryl-bearing quartz veins so far re­ been summarized in tables 8, 10, 11, 13, and 14. The ported throughout the world and in most of the helvite- localities sampled are shown in figure 2. bearing veins and pyrometasomatic deposits. Idocrase The older analyses of table 16 may be of a lower order where associated with helvite contains abnormal of accuracy than those of table 15. Reanalysis for amounts of fluorine as well as beryllium. T e average beryllium of several of the older samples indicates that fluorine content of igneous rocks is 0.04 percent in gab- the earlier determinations may be high by a factor of bro, 0.085 percent in granite, and 0.103 percent in as much as four. Resampling at some localities also nepheline syenite (Koritnig, 1951, p. 111). These fig­ suggests that some of the older samples may have been ures show an approximate straight-line correlation with contaminated in an unknown fashion with as much as the corresponding averages for beryllia, there being ap­ 0.2 percent BeO. However, reanalyses of samples of proximately 30 times as much fluorine as beryllia in tactite from Nevada were in agreement with earlier igneous rocks, plus an additional 0.03 percert. fluorine. results. Lindgren (1933, p. 179) postulated a relation between The reliability of determinations for elements other fluorite distribution and magmatic differertiation in than beryllium has not been tested, but inaccuracies may the western United States. He noted that intrusive have been introduced by contamination in grinding. rocks of intermediate composition near the Pacific Most of the samples were processed in a routine man­ Coast are succeeded by silicic intrusive rocks farther ner by commercial crushing and grinding equipment. east, and finally by a belt of alkalic intrusive^ along the Sandell (1947) has shown that even when reasonable Rocky Mountain front. Fluorite is most al 'indant in precautions are taken by hand grinding in a Plattner the rocks and mineral deposits along the eastern mar­ mortar, as much as 0.028 percent iron is added to quartz gin of the Rocky Mountains, particularly in tte southern and feldspar. Recent tests conducted by Myers and part. A corresponding concentration of beryllium in Barnett (1953) of the U. S. Geological Survey with this zone might be expected because of the association standard grinding equipment showed additions of as of fluorine and beryllium in igneous rocks and mineral much as 1.5 percent iron and 0.1 percent manganese in deposits. While the beryllium-bearing deposits of Iron routine processing of these minerals. Mountain and the Victorio Mountains, N. Mex., may be Correlations between beryllium and other elements cited in support of this thesis, the virtual absence of are not apparent from the data provided in the tables. beryllium elsewhere along the Rocky Mountain front Unfortunately, the list of elements for which spectro­ and its presence in tactite deposits in Nevada and Cal­ graphic determinations are available does not include some of those most likely to be correlated with beryl­ ifornia are opposed. Although the fluorite deposits of lium. In igneous and metamorphic rocks, for exam­ the Southern Rocky Mountains are believed to have a ple, two of the elements most important in determining genetic relation to intruded igneous bodies nearby the mineralogy are silicon and aluminum, and few de­ (Rothrock, Johnson, and Hahn, 1946, p. 21), the min­ terminations of these have been made in samples tested eralogy of many of them suggests a relatively low tem­ for beryllium. Analyses for fluorine, with which a cor­ perature origin that would not be favorable for depo­ relation might be expected, are also lacking. Gravi­ sition of beryllium. ASSOCIATION OP BERYLLIUM WITH OTHER ELEMENTS 41

FIGUBB 2. Index map of localities listed in table 16. Alabama Georgia South Dakota 1. Bakerhill lignite 11. Cave Springs district, Callahan mine 19. Keystone district 2. Bock Bun district, Emerson mine 12. Cartersville district 20. Maitland district Michigan 21. Trojan and Lead districts Arizona Tennessee 13. Houghton district 3. San Francisco district 22. Bumpass Cove district, Embree mine Missouri 23. Central Tennessee black shales Arkansas 14. Rocky Creek mine Texas 4. Batesville 5. Fletcher mine Nevada 24. Terlingua district 6. Glenwood district 15. Tern Piute district 7. St. Joe district Utah New Hampshire 25. South Temple Mountain California 16. Grafton County lead-zinc mines Virginia 8. Elsinore lignite * 17. Ore Hill mine 9. Mother Lode district 26. Appalachian district 10. Providence Mountains district, Scheelite North Carolina 27. Southwest Virginia district, Glade 1 foun­ Bay mine 18. Hamme mine tain mine 42 OCCURRENCE OP NONPEGMATITE BERYLLIUM IN THE UNITED STATES

TABLE 15. Spectrographic analyses, in percent, for other [Analysts, F, Janet D. Fletcher; M, Z. J. Murata; C, A. A. Chodos. nd, not detennined; leMers (....) looked Ana­ Locality and sample lyst BeO Sb As Ba Bi B Cd CaO Cr Co Cu Ga Ge In FeaOj

ARIZONA (see fig. 21)

Cochise County: Courtland-Qleeson district: 1 329^551. ___ - __ ...... F O.OOX O.OX xo O.OOX O.OOOX O.OX O.OOX nd 3-6 ?, 552 . _ ... _ .. F .OOX 6-10 .OOX .OOX X.O .OOX XO Gordon and Abril mines: 3 39Q_S43 F 0.04 .OOX .ox O.OX YO .OOX .OOX .ox .OOX 3-6 4 647A F .007 .OOX nnv xo .OOOX .ox .OOX 3-6 6 KiQ F 004 finmr 6-10 .OOX .OOX .OOX .OOX 6-10 ft 550 F .02 .OOOX .OX .ox 6-10 .OOX .ox .X .OOX nd 6-10 Little Dragoon Mts.: 7 329-449 F .0007 nv 3-5 .OOX .OOX .X .OOX 3-« 8 A.F.n F .0007 .OX 6-10 .OOX .OOX .X .OOX 3-6 9 451 .. __ ... F .0007 .OX 6-10 .OOX .OOX .ox .OOX 3-6 10 458..-.-...... F .0007 .OX O.OOX 1-3 .OOX .ox nd 1-3 Tombstone district: 11 329-539 __ .. F O.X O.OX .OOX .OOOX .ox 3-6 .OOX .OOX .X nd 1-3 1? 540 _ ...... F .OOX .OOX XO .OOX .ox .OOX nd 1-3 13 544 F .OOX .OOOX XO .OOX .OOX nd 1-3 yn .ox 14 546 F .0007 .OX .OOX .ox .OOX .OOX .ox .OOX 1-3 Pima County: Empire district: 16 329-524 _ ..... _ ...... F .OOX ftftTT XO .OOX .OOOX .OOX .OOOX 1-3 16 528- F .OOX XO .OOX .OOOX .ox .OOX nd XO 17 526 F .OOX .ox XO .OOX .OOX .ox .OOOX nd XO 18 527 F .OOX .X xo .OOX .OOX .X .OOX XO Helvetia district: 19 329-510 F xo .OOX .OOOX .X .OOOX 3-6 W 512 ...... F .0004 6-10 .OOX .OOX X .OOX 3-6 21 514 ...... F .002 .OOX 6-10 .OOX .OOOX .X .OOX 3-6 Wi 515 F .0004 .ox XO .OOOX .X .OOX nd 3-6 y& 516 _ ...... F nATT .OOX 6-10 .OOX .X .OOOX 3-6 24 517.. F .OOX 6-10 .OOX .X .OOX O.OOX nd 3-6 26 520 F 6-10 .OOX .OOX X .OOX XO 2ft 521 F 6-10 .OOX .OOX X .OOX XO SI7 523 F .0004 .OOX 6-10 .OOX .OOOX X .OOOX .OOX nd 3-6 Pima County: Pima district: 28 329-490 F .OOOX XO .OOOX .ox .OOX nd XO ?9 491 _ . ___ ...... F .OOX .OOX 6-10 .OOOX .X .OOX nd XO 30 494. __ . __ . ____ ..... F nmc .OOX 6-10 .OOOX .OOX .X .OOX nd XO 31 ddfi F .001 nmr nmr 6-10 .OOX nflOY .OOX .OOX nd 3-6 32 497 ...... F .001 .OOX 6-10 .OOOX .X .OOX nd XO 33 dost F .OOX 6-10 .OOOX .OOOX .OOX ,oox nd 3-6 34 499 . I...... F .OX XO .OOOX .ox .OOX nd XO 35 601 ...... F .OOX .OOX XO .OOX .OOX .OOX O.OOX nd 3-6 36 502...... F ...... OOX ...... OOOX ...... 3-0.6 .OOOX .OOX nd 1-3 37 503 F ...... OOX .OOOX .3-0.6 .OOOX .OOX nd 1-3 38 506 ______F .0004 .OOX 6-10 .OOOX .OOX .OOX ox nd XO 39 607 F .OOX XO .OOX .OOX .OOX .OOX nd XO 40 508 F .OOX nmr 6-10 .OOX .OOX .X nd 3-6 41 609 F .ox mr .ox 6-10 .OOX .OOX .X nd 3-6 Santa Cruz County: Patagonia district: 42 329-628 ______... F .OOX XO .OOOX .OOX .X .OOX nd XO 43 629 ...... F .OOX .X .ox 6-10 .OOX .OOX X nd XO 44 531 _ ..... ____ .. F .OOX .OOX 6-10 .OOX .OOX .ox .OOOX nd 3-6 45 . 632 F .OOX XO .OOX .ox .OOX nd XO 4fi 533- ______.. F .OOX OY .ox 6-10 .OOX .OOX .X nd 3-6 47 535 F .OOX .OOX XO .OOX .OOX .X .OOX nd XO 48 536 F .OOX .OOX 6-10 .OOX .OOOX .ox .OOX nd XO 49 837 F nft"5T .OOX 6-10 .OOX .OOOX .ox .OOX nd 6-10 50 538 F .OOX 6-10 .OOOX .OOX .ox .OOX nd XO ASSOCIATION OF BERYLLIUM WITH OTHER ELEMENTS 43 elements in samples analyzed for beryllium for but not found; asterisk (*) percent of element rather than oxide. Major, more than 1 percent].

La Pb MgO Mn Mo Ni Nb Ag NajO Sr Ta Sn Ti w u eU eUsO V Y Zn Zr

1 O.OOX 0.3-0.6 O.X O.OOX nd nd O.OOX O.X nc 0.001 nd O.OOX o.y O.OX 2 .ooox .3-0.6 .X .oox nd nd .oox nd .001 nd .oox .ox .OX

3 .X .1-0.3 X O.OOX .oox O.OOX nd .ox O.OOX .ox nd nc .ox X .OOX 4 .oox .1-0.3 .X .oox .oox .ooox nd .ox ...... ox ...... nd ...... nd .oox .ox .OOX 5 ...... 3-0.6 .X .oox nd .ox .ox nd .oox .X .OOX 6 .oox .6-1 .X .oox ...... ooox nd .ox .ox O.OX nd nc .oox X .OOX 7 .6-1 .X .oox .ooox .ooox nd .ox .X .ox nc .001 nc .oox .y .ox 8 .6-1 .X .oox .ooox .ooox nd -OX .X .ox nd .001 nd .oox .X .oox 9 .6-1 .X nd .X nc .003 nc .oox .ooox .ooox .ox .ox .oox .07".or .ox 10 .3-0.6 .X .oox .oox nd .oox nd .001 nd .oox

11 X .03-0.06 xo .oox .oox .ox nd .ox ny nd .003 nd .oox X .oox 12 .oox .1-0.3 .ox .oox nd .oox .X nd .001 nd .ox .ox 13 O.OX .ox .1-0.3 .ox nd .X nd .004 nd .oox .ox .ox .07" .ox 14 .ox .ox .1-0.3 .ox ----_-_ .oox - .ooox nd .ox nd nd .ox .ox

15 .ooox .6-1.0 .X nriy nd .oox nd nd .oox .oox 16 .1-0.3 .X .oox nd .oox .ox nd nd .ox .oox 17 .ooox .3-0.6 .X .oox .oox nd .oox .ox .X nd nd .ox .oox 18 .oox .1-0.3 .X .oox .oox .oox nd .oox .ox .X nd .001 nd .ox .oox 19 .6-1 .X .oox ...... ooox nd .oox .oox .oox nd .001 nd .oox .X .oox 20 .ox .6-1 .X .ox .oox .oox nd .oox nd .001 nd .oox O.OX .or .ox 21 3-6 .X .oox .oox .ooox nd .oox .X nd .001 nd .oox .ox 22 .ox .6-1 .X .oox .oox .ooox nd .oox .ox nd .003 nd .oox .or .ox 23 .6-1 .X .oox .oox .oox nd .oox ny nd j .001 nd .oox .oox 24 .3-0.6 .X flflY .oox .ooox nd .oox .oox .ox .X nd .001 nd .oox .oox 25 .6-1 .X .oox ...... oox nd .oox ...... oox nd .001 nd .oox .or .oox 26 .6-1 .X .oox .oox .ooox nd .oox .oox .ox nd .001 nd .oox .or .oox 27 .6-1 X .oox .oox .oox nd .oox .oox .oox .ox nd .001 nd .oox .or .oox

28 .1-.3 .X .oox nd .oox .oox .oox .ox nd nd nd .oox .oox 29 .ox .1-0.3 .X .ox .oox .ooox nd .oox .oox .ox .ox nd nd nd .oox .or .oox 30 .oox .6-1 .X .oox .oox .oox nd .oox .oox .ox nd .002 nd .oox .oox 31 .ooox 1-3 .X nmr nd .ox nd .001 nd .oox .oox 32 .3 .X .oox. .oox .oox nd .oox .oox .ox .ox nd nd .oox .or .oox 33 .3 .X .oox .oox .ooox nd .oox .oox .ox .ox nd nd .oox X .oox 34 .1-0.3 .X .oox .oox nd .oox .oox .oox nd .001 nd .oox .oox 85 .6-1 .X .oox nd .oox nd .001 nd .oox ] .ox 36 .X .ox .oox nd .oox ny nrt nd 37 .X .ox .oox nd .oox .ox .X nd .001 nd 38 .X .X my nd .oox nd nd .oox .oox 39 .X .X Any nd .oox ...... oox nd .001 nd .oox .oox 40 .X .6-1 X .oox .ooox .oox nd .oox .ox nd nd nd .oox X .oox 41 X .6-1 .X .oox .oox .oox nd .oox .ox nd nd nd .oox ...... X .oox

42 .X .06-0.1 .X .oox .oox .oox nd .oox .oox .ox nd .001 nd .oox .X .oox 43 xo .1-0.3 X .oox .oox .ox nd .oox .ox .X nd .001 nd xo .oox 44 .X .1-0.3 X .oox .ooox .ooox nd .oox .ox .ox nd nd nd .oox ...... X .oox 45 .X .06-0.1 .X .oox .oox ...... ooox nd .oox ...... ox nd .001 nd .ox .or .oox 46 X .1-0.3 X .ox .oox .oox nd .oox .ox .X nd .001 nd X .oox 47 X .1-0.3 .X .oox .oox .ooox nd .oox .ox .X nd .001 nd .oox .X .oox 48 .ox .1-0.3 .X .oox .oox .ooox nd .oox .ox nd nd .ox ..... - .X .oox 49 .X .1-0.3 X .oox .oox .oox nd .oox .X nd nd .X .ox 50 .X .03-0.06 .X .oox .oox .ooox nd .oox .oox .ox nd .001 nd .ox .X .oox 44 OCCURRENCE OP NONPEGMATITE BERYLLIUM IN THE UNITED STATES

TABLE 15. Spectrographic analyses, in percent, for other [Analysts, F, Janet D. Fletcher; M, K. I. Murata; C, A. A. Chodos. nd, not determined; leachrs (__) looke

Ana­ Locality and sample lyst BeO Sb As Ba Bi B Cd CaO Or Co Cu Ga Ge In FeaOs

NEW MEXICO (see fig. 29)

Catron County, Black Range district: 51 329-711 F 0.002 n nnv 0.1-0.3 O.OOX O.OOX O.OOX 3-6 Colfex County: Cimarroncito district: 5?, 329-376 ______. F nv 6-10 .OOX .ox .OOX 6-10 53 377 F .OX O.OX 6-10 .OOX O.OOX X 10 54 378 . _ - _ . __ .... F .OX .OOX .OOOX .X .OOX XO 55 382 .. ___ .. ___ - F XO .OOOX onnv .X .OOX XO Colfax County: Elizabethtown district: 56 329-262 _ ...... F .OX O.OOX 3-6 .OOOX 1-3 57 263 F .OX .OOX .OOX .OOOX .OOOX .OOX 1-3 68 267. F nv .OOX .OOX .OOX 6-10 59 271 F .0004 nv OOX oe .OOX .OX .OOX XO 60 272 F ...... OOX ...... 3-0.6 .OOX ...... OOX ...... nd XO 61 273 F .OX .OOX 6-10 .OOX .OOOX .OOX nd 3.0 6?, 274 F nnv nnv .OOOX .OOX nd vn 63 275 F nv 6-10 .OOX .OOX .OOX nd 3-6 Baton volcanic region: 64 329-360 F .002 nv nnnv .OOX .OOX nd 1-3 65 361. F nn9 nv .OOOX .OOX .OOX nd 1-3 66 364 __ ...... F nn9 nv .OOX .OOX .OOX nd 1-3 67 365 F .002 nv OOX .OOOX oov oov nd 1-3 68 367. F .X n /> .ox .OOX .OOX .OOX nd 3-6 69 369 . ___ .... F .007 nv .OOOX .OOX .OOX nd 1-3 70 372 F nv .OOX .OOX .OOX .OOX nd 3 71 373 _____ F .OX 1 O .OOOX .OOX .OOX nd 1-3 Dona Ana County: Organ district: 329-790 F nv nnv nd .OOX .OOX .ox nd XO 73 791 F .0004 nnv nd XO .OOOX .OOOX .X nd XO 74 793...... F .OX nd vn nnv nnnv oov .OOX nd 6-10 75 794 F nnv .ox nd vn .OOOX .X .OOX nd XO 76 796 F .ox nd .OOX .OOOX .ox .OOX nd 1-3 77 797 F 00V fiV nd O.OX .ox .X nd 3-6 78 797a ...... F nnv nv nd .OOX .OOOX .ox .OOX nd XO 79 799 _ . __ ...... F nv nd .OOX .OOX nd 3-6 80 802. __ ...... _ - F nnv nd 6-10 .ox nd .3-0.6 Grant County: Burro Mountains: 81 329-318 F .002 .X XO .OOOX .OOX nd .1-0.3 82 319 F 001 nnv nnv 6-10 nnv OOX .OOX nd 3-6 Carpenter district: 83 329-735-6 F .01 nnv ftV .ox nnv OOOX nv nd Central district: 84 329-276 F nv XO.O .OOOX .OOX nd 3-6 85 277 F .0008 .OX .OOX .OX .OOOX .OOX .OOX nd 3 86 280 F nv 6-10 .OOX .OOX .OOX .OOOX nd XO 87 281. . _ .. _ ... F nv nv vn .OOX .ox .OOX nd vn 88 284.. _ ...... F .0004 nv .OX Vft .OOX nnv .ox .OOX nd XO 89 286 _ ...... F nnv .OX vn .OOX .OOOX .ox nd XO 90 287 F nnv .ox .OOX .OOX .OOX nd XO 91 288... __ ...... F nv nv 6-10 .ox .OOX nnv nd 1-3 9? 289 ______. ___ . F *.OOOX nnnv nnv .OOOX .OOX O.OX nd X 93 291..- . _ .... F nnv .OOX 6-10 .OOX nnv nv oov nd XO 94 292...... F OOX nnv 6-10 nnv nnv .X .OOX nd XO 95 293 F nv nv 6-10 .OOX nnv .X .OOX nd 6-10 96 294 F .0004 nv nv OJS .OX nnnv oov oov nd 1-3 97 295 F OOX nv nov .OOX nov nd 6-10 98 296 _ ...... F .001 OOX .OOX nnv .ox nd 1-3 99 297 F oov nv XO .OOX nd .OX 100 301 F OOX XO .OOX .OOX nv nd XO 101 302 F .OOX vn .OOX .OOX nd XO 102 303 F nnv vn .OOX .OOOX nv nd vn 103 305 ...... F ...... OX ...... OOX ...... 1-3 .OOOX .OOX .OOX ...... nd 1-3 104 306 F .OX .OOX 3-6 .OOOX .OOX .X .OOX nd XO 105 308 F nv nnv XO nnv nv nd 6-10 106 730 F .001 OOV ox ox Oft nv nd 3 107 732 F .0008 .OOX 6 .OOOX .OOX .ox nd 3-6 108 734 . F .OOOX 6-10 .OOOX .ox nd 3-6 109 807 F .002 .OOOX 6-10 .OOX .ox nd 3-6 ASSOCIATION OF BERYLLIUM WITH OTHER ELEMENTS 45 elements in samples analyzed for beryllium Continued for bnt not found; asterisk (*) percent of element rather than oxide. Major, more than 1 percent].

La Pb MgO Mn Mo Ni Nb Ag NaaO Sr Ta Sn Ti w II eU eUjOg V Y Zn Zr

51 O.OX O.OOX O.OX O.X O.OOX n< O.OOX O.X O.OX ..... nd 0.00 nd O.OOX O.OX O.OX

52 .3-0.6 .X .oox nc .ox .X nd .OX .oox 53 .oox .3-0.6 .OX O.OOX .oox O.OOX nc .ox nv nd .001 nc .OX .oox 54 .3-0.6 .X .oox .ooox nc .ox .ox nd .001 nd .OOX .oox 55 ------.6-1.0 .OX .oox .oox .ooox nd .ox nv nd nd .OOX .oox

n~v 56 .oox 0.6-1 .OX .X .oox nd OTT .oox 57 3-6 .X .oox .oox .ooox nd .OX nd .002 nd .OX .ox 58 .6-1 .X .oox nd .ox nd .001 nc .OX O.OX .oox 59 .6-1 .X .oox nd .ox nc .OOX .oox 60 ...... 3-0.6 .OX .oox .oox ...... nd .oox .X O.OX nd nd .OOX .oox .ox 61 .6-1 .X .oox nd .ox nd .001 nd .OX .ox 62 .ox .6-1 .X .oox .oox .ooox nd .ox .X nd .001 nc .OX .ox .oox 63 .OX .ooox .6-1 .X .oox .oox nd .ox .X nd .ox .oox

64 .ox .3-0.6 .X .oox O.OX . ..-. nd .ox .003 .005 nd .oox .ox 65 .ox .oox .1-0.3 .X .oox .ox nd .ox .003 .007 nd .ox 66 .ox .oox .3-0.6 .X .oox .ox nd .ox .002 .007 nd .oox .ox 67 .ox .oox .1-0.3 .X .oox .ox .ooox nd .ox .002 .006 nc .ox 68 .ox 3-6 .ox .oox nd .ox nd .002 nd .ox .oox 69 .ox .oox .1-0.3 .X .oox .ox nd .ox .004 .010 nd .oox .ox .X 70 .ox 1-3 .ox .oox nd .ox nd .001 nd .ox .ox 71 .3-0.6 .ox .ooox nd .ox nd .003 nd .oox .oox

72 .ox .1-0.3 .X .oox .oox ...... ooox nd .oox .oox .oox nd .001 nc .oox .ox .oox 73 .oox .3 .X .oox .ooox nd .oox .oox .oox nd .002 nc .oox .ox .oox 74 .oox .6-1 .X .oox nd .ox .oox .X .ox nd .001 nc .oox .ox .oox 75 .ox .3-0.6 .X .oox .oox .ooox nd .oox nd nd .oox .X .oox 76 .oox 1-3 .X .oox nd .ox .X .ox nd .001 nd .ox .X .oox 77 .ox .1-0.3 .X .oox .oox nd .ox .ox nd nd .oox X. .oox 78 .ox 6-10 .X .oox .oox nd .ox .ox nd nd .oox .X .oox 79 .ooox .6-1 .X .oox .ooox nd .ox .X nd .002 nd .oox .ox 80 x-xo 0 .ox .ooox ...... oox nd .ox

81 .oox .X .X .oox .ooox nd .ox nd .001 nd .oox .ox 82 .6-1 .ox .ox .oox nd .ox ...... oox .OX .X nd nd .ox .oox .oox 83 X .6-1 .X .oox .oox .oox nd .oox nv nd nd X. .oox

84 .ox .6-1 x.o .oox .ooox nd .ox flATT nd nd .oox .ox .oox 85 .oox .3-0.6 .X .oox nd .ox nd .003 nd .ox .ox .ox 86 ...... 3-0.6 .X .oox .oox .ooox nd .ox ftTT nd nd .oox .ox .oox ft"V" 87 .ooox .1-0.3 .X .oox .oox .ooox nd .oox nd nd .oox .oox .ox .ox 88 .ox .6-1 X .oox .oox .ooox nd .ox nd .001 nd .oox .oox .X .oox 89 .ooox .OX .X .oox nd .oox .oox nd nd .oox .ox .oox 90 ...... 3-0.6 .X ...... oox ...... nd .oox .oox nd nd .oox .ox .ox 91 .ooox .6-1 .ox .oox .ooox nd .ox nd .002 nd .ox .ox 92 .ox .X xo .oox nd .ox .oox .ox nd nd .oox .X 93 .ooox .6-1 .X .oox .oox nd .ox .X nd .001 nd .oox .oox .X .ox 94 .ox .6-1 .X .oox .ooox nd .oox nd .001 nd .oox .oox .ox 95 1-3 .ox .oox .oox ...... ooox nd .ox nd .002 nd .ox .oox 96 .ooox 3-6 .X .oox .oox nd .ox nd .002 nd .ox .ox .oox 97 .6-1 .X .oox .ooox nd .ox X nd .001 nd .ox .oox 98 .oox .1-0.3 X .oox .ooox nd .ox .oox nd .001 nd X .oox 99 .ooox .OX .ox nd .ox .oox nd nd .oox 100 ...... ooox .3-0.6 .X .oox .oox ...... ooox nd .ox .X nd .001 nd .oox ...... X .oox 101 .ooox .6-1 .X .oox .oox .ooox nd .ox .oox nd nd .ox .oox A"V 102 .6-1 .X .oox nd .ox nd nd .X .oox 103 .6-1 .ox .oox nd .ox nd .003 nd .oox .oox .ox ft"V" 104 6-10 .X .oox nd .ooox nd .001 nd .oox 105 .6-1 .X .oox nd .oox .ox nd .001 nd .oox .X .oox 106 .ox .6 .X .ooox .oox nd .oox .oox nd nd xo 107 - .X .6 .X ...... oox ... .ooox nd .ox .oox nd nd 108 .ox .3-0.6 X .ooox nd .oox nd nd nd .oox ...... X .oox 109 .X .1-0.3 .X .oox nd .oox nd nd nd .oox X .oox 46 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES

TABLE 15. 8pectrographic analyses, in percent, for other [Analysts, F, Janet D. Fletcher; M, K. J. Murata; O, A. A. Ohodos. nd, not determined; lead-^s (__) looked

Ana­ Locality and sample lyst BeO Sb As Ba Bi B Cd CaO Cr Co Cu Qa Ge In FejOi

NEW MEXICO Oontlnaed

Grant County Continued Pinos Altos district: 110 329-738... F O.OOX O.OX O.OX 1-3 O.OOX O.OOX O.X nd XO 111 740... .. _ F O.OX .OOX .OOX .ox 3-6 .OOOX .ooox .ox nd XO Hidalgo County: Apache No. 2 district: 112 329-752...... _ ...... F .OX xo .OOOX .OOX .X nd 3-6 113 755 . F ftft-V- xo .OOOX .ooox .ox nd XO 114 781 F nnv 6-10 .OOX .OOX nd XO 115 783... F .OX xo .ooox .OOX .X O.OOX nd 3-6 Hidalgo County: Hachita district: 116 329-740a ___ . ______. F ox 1-3 .ooox .ooox .ox .OOX nd 6-10 117 741 - F .OOX 3-6 .OOX .OOX nd XO 118 742 F mr .ox 3-6 .ooox .ooox .ox nd XO 110 743 F .OOX .6-1 .ooox .OOX nd XO 120 744...... -. .. F nv XO .OOX .OOX nd 1-3 121 745 ...... F nv XO .ooox .OOX nd 3-6 122 746 F nnv XO .OOX .ox x-xo nd XO 123 747 F .OOX XO .OOX .OOX .X nd 3-6 124 749 F ftTT 6-10 .ox .OOX .ox .OOX nd 1-3 125 750 F .OOX 6-10 .ooox .OOX .X nd XO 126 751 F 6-10 .OOX .OOX nd 1-3 Lordsburg district: 127 329-121 F .OOX .OOX O.OOX .1-0.3 .ooox .X .... nd 1-3 128 422 . F nnv nnv 1-3 .ooox .ooox .X nd 1-3 129 423 F nnv 6-10 .ooox .OOX X nd XO San Simon district: 130 329-127 F nnv .ox XO .OOX .ooox .OOX .OOX nd 3-« 131 429 . F .OX .OOX XO .OOX .OOX .ox nd 3-6 132 433 F .OOX XO .OOX .ooox .X nd XO Lincoln County: Capitan district: 133 329-810 F 0.005 .ox ...... OOX ...... 3-6 .ooox .OOX - nd 1-3 Gallinas district: 134 329-308 --.- F .008 ..OOX 3-6 .ooox .ooox .OOX nd XO Luna County: Tres Hermanas district: 135 329-759 __ .... F ftHTT .X XO .ooox .OOX nd 3 136 760 F nmr .ox XO .OOX .ooox .OOX nd 1-3 Victorio Mountains: 137 329-890 F .02 .ox .ox .ooox XO .OOX .ox .ooox O.OOX nd 1-3 138 392 F .003 .OOX .ox .ooox XO .OOX ...... OOX .OOX nd .6-1 139 393 F .004 .OOX .OOX .ooox XO .ooox .OOX nd .3-0.6 140 399 F .1 .ox .ox .X XO .ooox .OOX .ox .ooox .OOX nd XO 141 400 F .02 ...... ox .OOX .ooox XO .ooox .ox nd .8-0.6 142 401 F .2 .OOX .ox 6-10 .OOX .OOX nd XO 143 402 F .005 .OOX .ox .ooox XO .ooox .OOX nd .6-1 144 403 F .002 .ox .OOX 1-3 .ooox .OOX .OOX 1-3 145 408 _ ..... F .03 .OOX .ox .ooox .ox XO .OOX .ooox .ox .ooox .ox XO 146 411 F .006 .OOX .OOX XO .OOX .ox .OOX .ox ...... 6-10 147 415 ...... F .08 .OOX .X XO .OOX .ooox .OOX .OOX .ox 3-6 148 394.. F .005 ...... OOX .OOX .OOX XO .ooox .ox .3-0.6 149 416.. ____ ...... F .02 .ox .OOX .OOX XO .ooox .OOX .ooox .OOX ...... 1-9 150 417 - _ F .005 .ox .OOX 3-6 .OOX .ooox .OOX .ooox 1-3 151 418 F .008 .OOX XO .OOX .ooox .OOX .ooox .OOX XO 152 420 F .002 ------.OOX .ox ...... XO .ooox .ooox .ox .OOX .ox XO San Miguel County: Eociada district: 153 329-384 ...... F ftftV .OOX 6-10 .OOX .OOX X .OOX XO Willow Creek district: 154 329-385A...... F .OOX .ox .OOX .ox .3-0.6 .ooox .ox .OOX ...... 3 Santa Fe County: New Placers district: 155 329-323...... F .ox 6-10 .OOX .OOX X .OOX 6-10 156 324...... F .ox .OOX XO .OOX .OOX .X .OOX 1-3 157 325 ...... F .ox .OOX XO .ox .ox .OOX ------3-6 158 326 ...... F ------.OOX ...... OOX ...... XO .OOX .ox .OOX 6-10 159 828 F .ox .OOX XO .OOX .ox .X .OOX 3-6 160 333 F .ox .OOX 6-10 .OOX .OOX .X .OOX 3-6 161 334...... F .ox 6-10 .OOX .OOX .X .OOX 3-6 ASSOCIATION OF BERYLLIUM WITH OTHER ELEMENTS 47 elements in samples analyzed for beryllium Continued for bat not found; asterisk (*) percent of element ratber tban oxide. Major, more tban 1 percent]

La Pb MgO Mn Mo Ni Nb Ag Na2O Sr Ta Sn Ti w u eU eUaOs V Y Zn JTr

110 O.OX 0.1-0.3 O.X O.OOX O.OOX nc O.OOOX O.OX nd 0.001 nd X O.OOX 111 X .3-0.6 .X .OOX .OOX nd .OOX - -- .OOX nd 001 nd X .OOX

112 .6-1 .X .OOX nd .ox .X nd O.OOX .OOX 113 .6 .X O.OOX .OOX .ox .X nd .001 nd .OOX .OOX 114 .OOX .3 .OX .OOX .ox .ox n< .OOX O.OOX .ox .OOX 115 .6 .X .OOX .ooox nc .ox .ox nd .001 nd .OOX .OOX

116 .OOX .3-0.6 .OX ...... ooox ...... nc .ox .X O.X nd .006 nc .ox .OOX 117 .ox .6 X .ooox .OOX nd .ox .ox .X .OOX 118 .ox .6-1 X .ooox .OOX nc .ox .ox .OOX X .OOX 119 X .6-1 X-XO .ox nc .OOX .ox .X .OOX 120 .OOX 1-3 .X .OOX nd .ox .X nmr .ox 121 .ooox .1-0.3 .X .ooox .ox .X nd .002 nc .OOX .OOX 122 .ooox .6-1 .X .ox .OOX nc .ox .X nd .002 nd .OOX .ox .OOX 123 3 .X .OOX .ooox nc .ox nc .001 nc .OOX .ox .OOX 124 .ooox 1-3 .OX .ox .OOX .ox .X nd .003 nc .ox .OOX .oox 125 .1-0.3 .X .OOX .OOX .ooox nd .ox .ox nc .001 nd .OOX .OOX 126 3-6 .OX .OOX nd .ox .X nd .001 nd .OOX .OOX .ox

127 x-xo .1-0.3 .OX .OOX .OOX ...... OOX nc .OOX .X nc .001 nc .OOX .ox .OOX 128 .ox .6 .X .OOX .OOX .OOX nd .ox .X nd .001 nd .OOX .ox .OOX 129 .X .6-1 .X .OOX .OOX .OOX nc .OOX .ox .ox nd .002 nd .ox .OOX

130 X 1-3 .ox .OOX .OOX nd .ox .X .ox .ox .OOX 131 O.OX .X 3 .ox .OOX .OOX nd .ox .X nd .002 nd .OOX .X .OOX 132 .ooox .3 .ox .OOX .OOX nc .ox ------.ox nd nd .OOX .ox .OOX

133 6-10 .ox .OOX nd .OOX .ox nd nd nd .OOX .OOX

134 .OOX 1-3 .ox .OOX .OOX fWlTT nd nd nd .ox .OOX .OOX

135 1-3 .ox .OOX nd .OOX O.OOX .ox nd nd .OOX .OOX .OOX 136 .6 .ox nmr nd .ox nd .001 nd .OOX .OOX .OOX

137 .ox 6-10 X .ooox .oooox O.X .OOX .ox .ox .02 nd nd .003 .OOX .X .OOX 138 .OOX 6-10 X .ooox .oooox .X .ox .ox .ox nd nd .OOX .X .OOX 139 .OOX 6-10 .X .oooox .X .OOX .OOX .ox nd nd .OOX .ox .OOX 140 .X 1-3 X .OOX .ooox .ooox nmr .ox .ox .ox nd nd .OOX X .OOX 141 .ox XO X .oooox nmr nftv nd nd .OOX .ox 142 .X 1-3 .ox .OOX .OOX .ooox .X .OOX .OOX .ox .08 nd nd .001 .ox .OOX .X .OOX 143 .ox XO X .ooox .ooox .X .OOX .OOX .OOX nd nd .001 .OOX ftV 144 .ox .6-1 .X .ooox .ooox 4-7 .OX .OOX .ox nd nd .005 .OOX .ox .ox .OOX 145 .X 3-6 X .OOX .ooox .OOX .X .OOX .ox .X .ox nd nd .ox X .OOX 146 .OX .ooox 1-3 X .ooox .oooox .OOX .ox .X .04 nd nd .001 .OOX .OOX .ox .OOX 147 .OOX .X 3-6 X .OOX .ooox .ooox .OOX .ox .X .06 nd nd .002 .ox .ox .OOX 148 .ooox XO .X .ooox ...... oooox .X .ox .OOX .ox nd nd .001 .OOX .ox .OOX 149 .OOX 1-3 .X .OOX .ooox .ooox .X .OOX .OOX .OOX .X nd nd .OOX .ox 160 .OOX 1-3 .X .OOX .OOX .oooox .X .OOX .OOX .OOX .2 nd nd .OOX .ooox .ox 151 .OOX 3-6 .X .OOX .oooox .X .OOX .OOX .ox nd nd ...... OOX .ox .OOX 152 .X .6-1 X .ooox .ooox nmr .ox .X nd nd .OOX .OOX .X .ox

153 3-6 X .OOX .OOX ------.OOX nd .OX .X nd .001 nd .ox .OOX

154 x-xo .1-0.3 .X .OOX .OOX .X nd nd nd XO .OOX

155 .1-0.3 .X .ox .OOX .OOX nd .ox nd .001 nd .OOX .OOX 156 .OX .6-1 .X .OOX .OOX ...... ooox nd .ox .X nd .004 nd .OOX .OOX 157 .3-0.6 .X .OOX nd .ox nd .001 nd .OOX .OOX 158 .1-0.3 .X .OOX nd .OOX ...... ox ..... nd .001 nd .OOX .OOX 159 .6-1 .X .ox .OOX ...... ooox nd .ox .X nd .001 nd .OOX .OOX 160 .OX .3-0.6 .X .OOX .OOX .OOX nd .ox nd .003 nd .OOX .OOX 161 .1-0.3 .X .OOX .OOX .OOX nd .OOX .ox nd .001 nd .OOX .OOX 48 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES

TABLE 15. Spectrographic analyses, in percent, for other [Analysts, F, Janet D. Fleteher; M, K. J. Murata; O, A. A. Ohodos. nd, not determined; leaders ( ) looked

Ana­ Locality and sample lyst BeO Sb As Ba Bi B Od OaO Or Co Cu Qa Qe In FeaOi

NEW MEXICO Continued

Santa Fe County Continued New Placers district Continued 162 329-336... _ . __ . ___ ..... F O.OX XO O.OOX O.OOX O.X O.OOX 3-6 1«3 340...... _ . _ ... F mr XO .OOX .X .OOX 3-6 164 341...... ___ ... F .OOX XO .OOX X .OOX 6-10 165 342...... _ ..... F nv XO .OOX .OOX .X .OOX XO Ififl 345-...... F 0.0004 3-6 .OOX .ooox .ox .OOX 1-3 Old Placers district: 167 329-349...... _ .... F 3-6 .OOX .OOX .OOX 1-3 168 350...... F 3-6 .ooox .ooox .OOX .OOX 3-6 169 352...... _ ...... F .OOX XO .OOX .ox .OOX 3-6 "vn 170 356 ...... F mr .OOX .ooox .ox .OOX 3-6 171 359...... F nv i-s .ooox .OOX .OOX 1-3 Sierra County: Cuchillo Negro district: 329-700... -....-...... F .001 O.OX nnv n mr O.OX 3-6 .OOX .OOX .X ... nd 1-3 173 701...... F .0007 .OOX O.OOOX 6-10 .OOX .ooox .OOX .OOX ...... nd 1-3 174 702-. . ... F .0005 nv 1-3 .OOX .OOX .ox .OOX ...... nd 3-6 175 708 . .. __ .. _ . F .004 nv 3-6 .ooox .ox ...... nd 3 Apache No. 1 district: 176 329-705 . F nv 3-6 .OOX .ox nd 1-3 177 706...... F .01 .OX .3-0.6 .OOX .X ...... nd .6-1 Socorro County, Jones Camp: 17ft 329-809 F nftV 3-6 .OOX .OOX .ox nd 3-6 TRANS-PECOS REGION (see pi. 1) Wind Mountain: 179 329-129 __ ...... __ ... M .0051 nnV X.O .ooox X.O 180 135...... __ .... F .006 nnv .ooox 1-3 .ooox .ooox .OOX ...... nd XO 136 ... F .003 nnv .ooox "Vft .OOX .ooox . nd .6-1 145. _ F <.001 nnv .ooox "Vft .ooox .ooox ...... nd .3-0.6 183 145A- ...... M .OOOX nnv nd nd nd .X nd nd .OOX nd nd nd *Major 1S4 145B...... M *.OOX nd nd nd nd nd *Major nd nd .OOX nd nd nd *Major 185 611C...... M .0050 .OOX .OOX .ooox .OOX ...... nd X 186 622 _ .... _ . . F .001 mr .OOX XO .OX .OOX .OOX .OOX nd nd 1-3 187 631...... _ ...... F .OOX XO .OOOX .ooox nd nd .1-0.3 188 649 . F .004 mr 1 .ooox .OOX .ox nd nd 1-3 189 652... _ -_-._. _ . __ F .004 .OOX 1 .ox .OOX .ox nd nd 1-3 Cave Peak: 190 329-077...... F .01 .ox .OOX 3-6 .OOX .OOX .OOX nd nd XO 078- . .. F oru nv .OOX .6-1 .OOX .ooox .OOX ...... nd 3-6 193 079-...... F .01 .OX .OOX 3-6 .OOX .ooox .OOX .OOX ...... nd 6-10 193 680 _ ... __ ...... __ ... F .0005 mr .OOX XO .OOX .OOX .OOX nd 1-3 Other localities: 194 329-601. _ F .001 nv .3-0.6 .ooox .OOX .OOX ...... nd 1-3 195 603 F .004 .OX .ooox .6-1 .OOX .OOX .OOX ...... nd 3-6 196 609 F .002 .OX 6-10 .ooox .OOX .ox .OOX ...... nd 3-6 107 610 . _ ..... F .0008 nv .3-0.6 .ox .OOX .OOX ...... nd 1-3 198 650 ...... M .0066 .OOX .OOX .X .ooox .OOX X.O 199 653 . . F .002 mr 1-3 .ooox .ooox .OOX .OOX ...... nd 1-3 son 688 F .002 mr 1-3 .OOX .OOX .OOX ...... nd 3-6

MONTANA (see fig. 67)

Anaconda mill and smelter products: 201 328-952- ___ . ... F .OX .3-0.6 .ooox .X 3-6 203 963. _ ...... _ ...... __ .. F onru nv nnv .1-0.3 .OOX .ooox .ox .OOX 3 208 966.. __ . _____ .. ___ .. F .OX 1-3 .ooox .ox 1-3 204 973- __ __ ...... F .OX ,ox .6-1 .OOX .OOX XO .OOX XO 205 074 F .001 vn .ox 1-3 206 975 ...... __ ..... F .001 A.V nnv OJS .OOX .ox .6-1 207 976A...... F .0004 .ox .OOX XO .ox .ox .3 208 975B __ ...... __ .. ... _ . F .ox nmr XO .ox .ox .3-0.6 209 977 F nnv .3-0.6 .OOX .OOX .ox 3-6 ?10 981 _ _ .. __ . _ .. F .OOX .6-1 .ox .OOX .OOX XO 211 988 ...... F mr nv on & nmr .OOX XO XO 212 989 ...... F .X .OOX .ox .OX .1-0.3 .OOX .ooox .X .ox O.OX O.OX 3 ASSOCIATION OF BERYLLIUM WITH. OTHER ELEMENTS 49 elements in samples analyzed for beryllium Continued or but not found; asterisk (*) percent of element rather than oxide. Major, more than 1 percent]

La Pb MgO Mn Mo Nl Nb Ag Na2O Sr Ta Sn Ti w U eU eUsOs V Y Zn Zr

162 0.3-0.6 O.X O.OOX nd O.OX O.OX nd 0.001 nd O.OOX O.OOX 163 .3-0.6 .X .oox O.OOOX nd .ox .ox nd .002 nd oox .oox 164 .3-0.6 .X .oox .oox nd .ox .ox ud .001 nd .oox .oox 165 .3-0.6 .X .oox .ooox nd .ox .ox nc .001 nd .oox .oox 166 O.OX .6-1 .OX .oox nd .ox .X nd .003 nd .oox O.OOX .ox

167 .6-1 .ox .oox nd .ox .X nd .003 nd .oox .oox .ox 168 .OX .6-1 .ox .oox nd .ox .X nd .002 nd .oox .oox .ox 169 .OX .3-0.6 .X .oox .ooox nd .ox .X nd .001 nd .oox .oox 170 .3-0.6 .X .oox nd .ox .X nd nd .ox .oox 171 .3-0.6 .ox .ooox nd .ox nd .001 nd .oox .oox

172 x-xo .3-0.6 .X O.OX .oox .ox nd .oox .ox O.OX nd nd .oox xo .oox 173 .X .6-1 .X .oox .ooox nd .ox o.oox .X nd --.---- nd .oox .X .oox 174 X .6-1 .X .oox .ooox nd .ox .X nd nd .ox .X .oox 17S .3-0.6 x-xo .ooox .ooox nd .ox .oox nd nd .ox

176 .ox .6-1 .X .oox .oox nd .ox .X nd .002 nd .oox .oox 177 .ox .1 .ox .oox .ox nd .oox .ox nd nd

178 3-6 .ox .oox .oox nd .oox .X nd nd nd .ox .oox

179 .X .ox .OX X.O .oox 0.53 nd .ox .ox .ox .X nd nd .X I^ajor 180 .OX .ox <.l .X .oox .ox .oooox 7-10 .ox .oox .ox nd nd nd nd .ox .ox 181 .oox 1-3 .ox <1 .ox .ox nd nd nd nd .oox .oox .ox 182 1-3 .ox <1 .ox .ox nd nd nd nd .oox .oox .ox 183 .ox .oox *.X .X nd nd .ox nd *Major .oox nd .oox .X nd nd nd nd nd .oox nd .X 184 .X .oox * OX Major nd nd .X nd .X_ nd nd nd nd nd nd .X nd Major 185 .ox .oox .X .X .02 nd .oox .X nd nd nd .ox .OX 186 .ooox 1-3 .OX .OOX .OOX ------.X .ox ...... oox .X nd nd nd .OX .oox .OX 187 XO .ox .OX mr nd nd nd .OOX 188 .ox .ooox .1-0.3 .X .OOX .oox .oox 7-10 .oox .X nd nd nd .oox .oox .OX 189 .ox .ooox .1-0.3 .X .OOX .ox .ox 4-7 .oox .ox nd nd nd .oox .ox .ox

190 .ox .X .3-0.6 .X .OOX .oox .ox .OOOX 1 .ox .ooox .X nd nd nd nd .oox .ox .OX .ox 191 .ox .ox .1-0.3 .ox .OOX .ox .ooox <1 .oox .ooox .ox nd nd nd nd .ox .ox .ox 192 .ox .X 1-3 .X .OOX .oox .oox .oooox 4-7 .ox .ooox .ox nd nd nd nd .oox .ox .X .ox 193 .6-1 .oox .ooox nd .ox nd .001 nd .oox .oox .ox

194 .1-0.3 .ox .ooox nd .oox nd nd nd .oox .ox 195 .ox .3-0.6 .X nd .ox .X nd .005 nd .X 196 .oox .ooox 1-3 .X .oox .oox .oox 4-7 .ox .X nd nd nd .ox .ox .ox 197 .oox .ooox . 1-0. 3 .X .oox .ox .oox 7-10 .oox .X nd nd nd .oox .oox .ox 198 .ox .oox .X .X .03 nd .oox .X nd nd nd nd .ox .ox 199 .oox .ooox .3-0.6 .ox .oox .ooox .oox 4-7 .ox .X nd nd nd .OOX .oox .ox 200 .oox .3-0.6 .ox .oox nd .ox .X nd nd nd .OOX .oox .ox

201 .ox .3-0.6 .X .ooox .ooox nd .oox .X nd nd .002 nd .oox .oox .ox 202 .ox XO .X .oox .oox nd .oox .X nd nd .003 nd .oox .oox .X .ox 203 .ox .6-1 X .ooox nd .oox .ox nd nd nd .ox .oox 204 .ox 6-10 .X .oox .ox ...... ox nd .oox .ox nd nd .001 nd .X .ox 205 .ox .oox 6-10 X .oox .ooox nd .ox .X nd nd .004 nd .oox .ox .ox 206 .ox XO X .oox .ooox nd .oox .X nd nd .002 nd .oox .ox .oox 207 .ox .6-1 .ox .oox .ox .ooox nd .X .ox nd nd .008 nd .X .ox .ox .ox 208 .ox .6-1 .ox .oox .ox .ooox nd .X .ox nd nd .010 nd .X .ox .ox .ox 209 .ox X .oox .oox nd .ox nd nd nd .ox .oox 210 .ox 6-10 .X .oox .oox nd .oox .X nd nd .014 nd .X .ox .ox 211 .ox .1-0.3 .X .oox .ox nd .oox .ox nd nd .002 nd .oox .oox .X .ox 212 X 6-10 .X .ooox .ox nd .ox nd nd .001 nd xo 50 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES

TABLE 15, Spectrographic analyses, in percent, for other [Analysts, F, Janet D. Fletcher; M, K. J. Murata; C, A. A. Ghodos. nd, not determined; leaders ( ) looked

Ana­ Locality and sample lyst BeO Sb As Ba Bi B Cd CaO Cr Co Cu Ga Qe In FejOj

WYOMING (see flg. 46)

Carbon County, Hanna district: 213 328-248 - M 0.0003 nd nd nd nd nd nd nd nd nd nd .002 nd nd Sweetwater County, Superior district: 214 328-245 - .. _ M fWVU nd nd nd nd nd nd nd nd nd nd .004 nd nd COLORADO (see flg. 49)

Boulder County, Lafayette area: 21fi 328-357 M nd nd nd nd nd nd nd nd nd nd .004 nd nd 21fi 358 M .0003 nd nd nd nd nd nd nd nd nd nd .003 nd nd Chaflee County: Monarch district: 217 328-020 F O.OOOX XO O.OOX O.OOOX O.OOX O.OOX nd XO 218 021 F .OOX XO .OOX .OOOX .OOX .OOX nd XO Sedalia mine: 219 328-602 F .0004 .OX XO .OOX .OOX .OOX nd 3-6 Conejos County: Platoro Summitville district: m 328-694 ___ ... _ . __ . _ F .OX O.OX .6-1 .OOOX .OOX .OX nd 1-3 221 595 __ ...... - ...... F .X .3-0.6 .OOX .OOOX .OX .OOX nd 3-6 222 597 _ . _ . _ F .OX O.OOX <1 .OOX .OOX .X .ox nd 3-6 223 598- ___ - _____ - ..... F .X .OOX <1 .OOOX .ox .OOX ------nd 3-6 Costilla County, La Veta area: 224 328-164 M * 0004 nd nd nd nd nd nd nd nd nd nd .004 nd nd Fremont County, Florence- Canon City area: 22S 328-171 M *.0006 nd nd nd nd nd nd nd nd nd nd .004 nd nd 226 172 __ ... _ ...... M * IWI9 nd nd nd nd nd nd nd nd nd nd .004 nd nd Qarfleld County, Rifle- Silt area: 227 328-83 ...... M *.0009 nd nd nd nd nd nd nd nd nd nd .004 nd nd 223

La Pb MgO Mn Mo Ni Nb Ag NaiO Sr Ta Sn Tl w U eU eU»0« V Y Zn Zr

213 nd nd nd nd nd nd nd nd nd nd nd nd nd nc <0.001 nt 0.02 ad ad nd

214 nd nd nd nd nd nd nd nd nd nd nd nd nc nc <001 nd .008 nd nd nd

21$ nd nd nd nd nd nd nd nd nd nd nd nd nd nd <001 nd .01 nd nd nd 216 nd nd nd ndr nd nd nd nd ad nd nd nd nd nd <001 nd .01 nd nd nd 217 O.OOX 1-3 O.X O.OOX O.OX O.X nd nd nd nd .OOX O.OOX 0.03* O.OOX 218 O.OOX .OOOX 1-3 .X .OOX .OX .X nd nd nd nd .OX .OOX .oy .OOX

219 .OX .OOX 6-10 .X .OOX nd .OX .X nd nd nd nd .OOX .OX .OX

220 X .X O.OOX nd .OOX .ox nd nd nd .001 X .OOX 221 .OOX .OOX 1-3 .ox .OOX .OOOX nd .OOX .X nd nd nd .002 .OX .OOX .OX 222 .ox 1-3 .ox ...... OOX ...... OOX nd .X .X nd nd nd .002 .OX .OX 223 .OOX .ox <1 .ox .OOOX .OOX nd .OX .X nd nd nd .002 .OOX .OX

224 nd nd nd nd nd nd nd nd nd nd nd nd nd nd <001 nd .01 nd nd nd

225 nd nd nd nd nd nd nd nd nd nd nd nd nd nd .001 nd .007 nd nd nd 226 nd nd nd nd nd nd nd nd nd nd nd nd nd nd .001 nd .001 nd nd nd

227 nd nd nd nd nd nd nd nd nd nd nd nd nd nd <001 nd .02 nd nd nd 228 nd nd nd nd nd nd nd nd nd nd nd nd nd nd .001 nd .01 nd nd nd 229 nd nd nd nd nd nd nd nd nd nd nd nd nd nd .002 nd .008 nd nd nd

210 .OX 3-6 .X .OOOX a ox 4-7 .X X nd nd nd nd .OOX .OOX .oy .OOX 211 .OX 6 .X .OOOX 4-7 .X .X nd nd nd nd .OOX .OOX .oy .OX 212 .OX 6 .X .OOOX .OX 2-4 .X X nd nd nd nd .OX .OOX .oy .OOX 213 .OX 6 .X .OOX IW <1 .ox X nd nd nd nd .OX .OOX .OX 214 .OOX .1-0.3 .OX .OOOX 4-7 .X .X nd nd nd nd .OX .OX .OX 215 .OOX ...... 1-0.3 .OX ...... OOOX ...... 7 .ox .X nd nd nd nd .OOX .OX 216 .OOX 6 .X .OOOX <1 .ox .X nd nd nd nd .ox .OX .OX 217 .OX 3-6 .X .OOX .OX <1 .X X nd nd nd nd .ox .OX .OX 218 .OX .OOOX .1-0.3 .OX O.OOX .OOX .ox 1-2 .ox X nd nd nd nd .ox .OX .X 219 .OX 6-10 X .ox .ox 1-2 flTT X nd nd nd nd .ox .OOX .OX 220 .OX 3-6 .X .OOOX .ox nd .X X nd nd nd .003 .ox .ox 221 .OX 3-6 .X .OOOX .ox nd .X X nd nd nd .004 .ox .ox 222 .OX 3-6 .X .OOOX .ox nd .ox X nd nd nd .003 .ox .ox 223 .OOX 1-3 .X .OOOX .ox nd .ox X nd nd nd .002 .ox .OOX .ox 224 .OOX 1-3 .X .ox nd .ox .X nd nd nd .002 .ox .ox 225 .OOX 1-3 .X .OOX nd .ox .X nd nd nd .002 .ox .OOX .ox 226 1-3 .X .OOX nd .OOX .X nd nd nd .ox .OOX .ox 227 .ox .OOOX 6-10 .X .OOX .OOX .ox nd .ox .OOX X nd nd nd .ox .ox .X 228 .ox .OOOX 6-10 .ox .OOX .ox nd .ox X nd nd nd .005 .ox .ox .ox 229 .OOX 3-6 .X nd .ox X nd nd nd .002 .ox .ox .X 230 .ox 6-10 .X .ox nd .X .X nd nd nd .003 .ox .OOX .ox 231 .ox 3-6 .ox OOOX .ox nd .X X nd nd nd .001 .ox .OOX .ox 232 .ox .OOOX 3-6 .ox ftflTT IW nd .X X nd nd nd .ox .OOX .ox 233 .ox 3-6 .ox .OOX nd .X .X nd nd nd .ox .ox .ox 234 .ox 3-6 .X .OOX .ox nd .X .OOX .X nd nd nd .003 .ox .OOX .OOX

235 3-6 .X .OOX ...... <1.0 .ox ...... OOX .X nd nd nd nd .ox .OOX .OOX

236 1-3 .X .OOX .OOX .ox nd nd nd nd .OOX .OOX

237 .OOX XO .X .OOX nd .ox nd nd nd .OOX X .OOX 238 .OOOX XO .X .OOX nd .OOX .X nd nd nd .002 .ox .OOX .X .ox 239 .OOX .OOX 1-3 .X .OOX nd .ox .X nd nd nd .002 .ox .OOX .03T .OOX 240 X .3-0.6 XO .ox .OOOX ...... OOX nd .X .X nd nd nd .002 .OOOX X .OOX 241 xo <1 .ox .OOX .OOOX .ox nd .ox nd nd nd .OOX X 52 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES

TABLE 15. Spectrographic analyses, in perwnt, for other [Analysts, F. Janet D. Fletcher; M. K. J. Murata; 0. A. A. Ohodes. nd, not determined; leaders ( ) looked

Ana­ Locality and sample lyst BeO Sb As Ba Bi B Cd CaO Cr Co Cu Qa Qe In Fe2O3

C OL O R AD O Continued

Huerfano County, Walsenburg: ?42 329-251- __ _ ... _ ... F 0.002 O.OX n nmr 6-10 O.OX O.OOX O.OX O.OOX nd 3 243 252. __ ...... ____ .... _ F .0008 .OOX 6-10 .OX .oox .oox .oox nd 3 La Plata County, Durango area: 244 328-158 M .0003 nd nd nd nd nd nd nd nd nd nd .004 0.006 nd nd 245 159...... ____ - __ - M .0006 nd nd nd nd nd nd nd nd nd nd .005 .007 nd nd ?46 161 . M nd nd nd nd nd nd nd nd nd nd .004 nd nd 247 163...... __ ...... M .0003 nd nd nd nd nd nd nd nd nd nd .005 nd nd Las Animas County, Morley area: 248 329-254.. __ ... _ .. __ ...... F fl"5T nnTT 3-6 rnr .OOX .OOX .oox nd 3 249 257 F OT nmr 3-6 .OX .OOOX .OOX .oox nd 1-3 Mineral County, Creede district: 250 328-590.. _ ...... ____ .... F .002 fiftTT O.OX .1-0.3 .OOOX .OX nd 1-3 251 592 _ . _ ..... __ ...... F .002 .OX .ox .1-0.3 .ooox .OX nd 6-1 Park County, Tarryal district: ?,52 328-603- ______.. ____ .... F .001 .ox O.OOX 6-10 .oox .OX .OX .oox nd XO 253 608 ______. _ . __ ...... F .0004 .ox XO .ox .OOOX .OX .oox nd 3-6 254 612. ___ ...... _ . __ F .001 .ox nmr nd .1-0.3 .ox .OOX .OOX .oox nd 3-6 255 614.. ._ F .oox nd XO .oox .OOX .oox nd nd Pitkin County, Redstone area: 256 328-092 M *.0005 nd nd nd nd nd nd nd nd nd .004 nd nd Summit County, Breckenridge dis- tiict: 2f>7 328-099... __ - _ ... . . _ ... F .OX XO .OOX .OOOX .OOX .oox nd XO Tri-State lead-zinc district: 258 328-325 F .OOX nd XO .OOX .OX nd .3-0.6 259 327 ...... - F .OOX nd XO .OOX .OOX nd .3-0.6

ARKANSAS

Hot Springs County, Magnet Cove: WO 328-293 __ .... _ __ ..... F .01 .OX nn~sr XO fWTT .OOOX .OOX .ooox nd 3 2fi1 299. __ . F .002 .X XO .ooox .OOX .OOOX .ooox nd XO 262 311 F .001 .OX XO .oox .OOX .oox .oox nd XO 263 318 F .001 flTT .6-1 .oox .ooox .oox nd 1-3 Saline County: 264 329-842...... C *.OOX .oox nd .ox nd 265 843 C *.OOX Amr nd .ox nd 266 844...... C *.ooox fifl"5T nd .oox .ox nd

NEW JERSEY

Sussex County: Beemerville area: 2fi7 329-826 _-.. C *.oox .ox nd .ooox .oox nd 268 827 C .oox .ox nd .OOX .ooox .ox nd 2fi9 828 . C .002 .ox nd .ooox .ox nd 270 829 __ . _ . ___ .. __ . C *.ooox .ox nd .oox .ooox .ox nd 271 830 . C *.ooox .ox nd .ooox .ox nd Franklin district: 272 329-819B...... M .01 .ox XO .OOX .ooox XO 273 832 C .003 HOY nd .oox 3-6 274 837 C .001 .oox nd .oox .oox 3-6

NEW HAMPSHIRE

Carroll County: Bartlett mine: 275 329-865 _____ . ______M (Wf> nAV .oox X.O Red Hill area: 276 329-812 _____ .. C .ooox nmr nd .ooox .oox nd 277 813 _ . _____ . C .oox nd .ooox .ooox .oox nd ASSOCIATION OF BERYLLIUM WITH OTHER ELEMENTS 53 elements in samples analyzed for beryllium Continued for bat not found; asterisk (*) percent of element rather than oxide. Major, more than 1 percent]

La Pb MgO Mn Mo Ni Nb Ag NajO Sr Ta Sn Ti w u eU eUsOs V Y Zn Zr

242 3-6 O.OX O.OOX nd O.OX X nd 0.001 nd O.OX O.OX 243 6-10 .OX .OX nd .X X nd .001 nd .OX .OX

244 nd nd nd nd nd nd nd nd nd nd nd nd nd nd .001 nd .02 nd n

248 3-6 .OX .OX nd .OX nd X nd nd .OX .OOX 249 O.OOOX .6-1 .OX O.OOX .OOX nd .X nd O.X nd .001 nd .OOX .OOX 250 X <1 .X .OOOX O.OX nd O.OX .ox nd nd nd X .OOX 251 .X <1 .X .OOX nd .OOX .X nd nd .002 nd .X .OOX 252 6-10 .X .OOX .OOX .OOOX nd .OX nd nd nd nd .OX a oox .OX 253 XO .X .OOX .OOX nd .OX .X nd nd nd nd .OX .OX 254 a ox 1-3 .OX .OOX nd .OOX .X nd nd nd nd .OX .OOX .OX 255 XO .X nd .OOX .ox nd nd nd nd .OX .OOX 256 nd nd nd nd nd nd nd nd nd nd nd nd nd nd .001 nd .02 nd n

257 .OOX .OOOX 1-3 .X .OOX 2-4 .OOX .X nd nd .002 nd .OOX .OOX .OX 258 .OX nd .OX nd .OOX .ox nd nd .001 nd .OOX .OOX X 259 .OOOX nd .ox nd .OOX .OOX nd nd nd nd .OOX .OOX X

260 .OX 1-3 .ox .OOX .OX nd .OX .X nd nd nd nd .ox .OX .OX 261 .OX .OOOX XO .X .OOX .OOX nd .OX .ox nd nd nd nd .ox .OX .OOX 262 1-3 .ox .OOX .OOX nd .OX .X nd nd nd nd .X .OX .OX 263 .OOX .OOOX <.l .ox .OOX .OOX .OX nd .ox .ox nd nd nd nd .OOX .OOX .OX 264 .OX .OOX nd .X nd nd .ox nd nd nd nd .X 265 .OX .OOX nd .X .OOX nd nd .ox nd nd nd nd .ox .X 265 .OX nd .X nd nd .OOX nd nd nd nd .ox .X

267 .OOX nd .X nd nd .X nd nd nd nd .X 268 .OX nd .X nd nd .X nd .X nd nd nd .ox .X 269 .OX nd .X .01 nd .X nd .X nd nd nd .ox .X 270 nd .ox nd nd .ox nd .X nd nd nd .ox .ex 271 .ox nd .X nd nd .X nd .X nd nd nd .ox .ox 272 X.O XO .OOX nd nd .ox .OOX nd nd nd X .OOX 273 nd X .OOX .OOX nd .OOX nd .ox nd ::::::: .ox _ __._ nd nd nd X .OOX 274 .ox nd X .OOX nd .OOX nd .ox nd .ox nd nd nd X .OOX

275 .ox .OOX .OX .ox .02 nd .OOOX nd nd nd .OX .ox 276 .OOX nd .ox nd .OOOX .OOX nd .X nd nd nd .ox 277 .OOX nd .ox nd nd .OOX nd nd nd nd .ox 54 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES

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1 Arkansas: California: Arizona: )1 4 ft 1 i 43-CE-l...... 002 1 .001 1 nna <003 .01 1933-42. 2...... do...... do .002 .001 .001 .01 <003 .01 4 _ ...... do... do.- .002 .001 008 <003 .01 6...... do __ ...... Gold tailings, .002 .001 .001 .01 <003 .01 before 1938. 7 ...... do- ... do _ .002 .001 .01 <003 .01 San Bernardino County, Provi­ dence Mts.: 12-SR1-6 ____ . .01 .05 .03 .003 .005 .19 .003 .04 .08 12-SR2-7 ..... do...... do .01 .05 .02 .003 .005 1.63 .003 .04 .02 Georgia: Bartow County, Car- tersville district: 76-AP-1A . .008 .04 .003 .02 .006 .003 .04 IB...... do...... do ...... 008 .05 .002 .02 .008 .003 .03 no 10...... do...... do...... 006 .05 (VY> .001 .02 .003 :::::: feon ID .....do...... do .... .008 .05 003 .02 .001 .02 .003 .04 76-AU-9B _ . do...... - .006 04 .002 .02 .001 .01 .003 .01 t* 9A do...... do ...... 007 .03 002 .02 .001 .01 .003 .02 7A._ ...... -do do .008 .04 .003 .01 .001 .008 .003 .02 ...... gH 7B...... do . do ...... 008 .04 .002 .02 .001 .008 .003 .03 70...... do. ~-~ do...... 008 .04 fU19 .02 .001 .008 .003 .02 ^ 7D...... do ...... do .. .008 .04 .003 .02 .001 .008 .003 .02 ...... o 7E...... do...... do ...... 008 .05 .003 .02 .001 .008 .003 .02 *l 7F...... do ... .do ...... 008 .06 .003 .02 .01 .003 .02 8A- -do ... ..do ... .01 .07 .004 .001 .02 .003 .02 M 8B...... do do .006 .04 .002 .02 .001 .02 .003 .01 » J< 10 ..do...... do...... - .01 .08 .006 .04 .001 .03 .003 .03 11...... do. do ...... 01 .08 nm 03 .03 .003 .02 S 12 . do ...... do .01 .05 .003 .03 .03 .003 .03 s 76-Br-2 ...... do...... 006 fU .003 .03 .001 .03 .003 .03 9 76-D-6A ...... do...... 006 04 AAO .02 .001 .02 .003 .03 6B...... do. do...... 007 .05 .003 .02 .001 .02 .003 .03 ^ 76-PF-3-4 ...... do .01 .04 .002 .04 .02 .003 .04 £jj 76-8-5 _ ...... do ...... 01 .06 .003 .01 .03 .003 .03 s Polk County, Cave Springs district: 13-C-2. _ ... do. .02 .2 .02 .1 .01 .003 .02 .08 ffi Michigan: Houghton district, Ed Copper Bange: ts 115-QUI-3 ...... 002 .001 .002 .02 .001 <.003 .001 ...... | centrate. Missouri: Shannon County: z 23-ROC-44 ... .05 .08 .01 .002 .02 .005 .001 .05 .005 .003 .05 01 a Nevada: Lincoln County, Tem-Piute district: 49-DGW-20 ...... 002 >1.0 .05 .01 .1 .01 004 .003 .02 >1 .003 .008 fide float tails. 21 ___ . do...... _ do .003 ... >1.0 .06 .01 .002 ...... 1 .01 .005 .003 03 >1 .003 .01 22 __ ...... do ...... 01 .05 .001 .05 .001 .08 .03 .003 .04 23 do ... __ . Scheelite cone __ .001 .5 .003 .001 .3 .01 0.003 .002 .03 >1 .003 .08

See footnotes at end of table. 56 OCCURRENCE OF NONPEQMATITE BERYLLIUM IN THE UNITED STATES

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Q ASSOCIATION OF BERYLLIUM WITH OTHER ELEMENTS 57

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Oilshale___.... * do______SouthernTemole fromcentrate residualclay. p "c CD ffi W mine. .1 s t 1CD > ^ ^ 1 § ac 1 T 1 1 I S | S PH o ° -s S a a S|I 293-P4-44'..... 7-GMC-l...... 11.. . 154-S100-2«....__.__ Terlinguadistrict: 9-SB-l...... palachiandistrict: 13-RM-3...... SouthwestVirginia ifil 1C County,BlandAp­ County:Jackson i County,Brewster County:Emery SmythCounty, « s s? P-H 2 o district: Virginia: S Texas: Utah:

a03 a*M 467945 5£ 58 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES GENESIS OF BERYLLIUM DEPOSITS to hydrothermal conditions. Except for local occur­ The physicochemical conditions under which the rences in granite, beryllium minerals are rare in igneous beryllium-bearing minerals originate have not been de­ rocks other than pegmatites; probably most of the termined, with few exceptions. However, some idea/ beryllium in such rocks is contained in silicate structures of the conditions may be surmised from the relative as a guest ion.^ This tendency appears to be particu­ abundance of these minerals in certain geologic envi­ larly marked in the feldspathoidal intrusive rocks, ronments and their virtual absence in others. The pre­ which do not as a rule give rise to extensive pegmatites ceding discussions emphasize that with few exceptions and ore deposits. Most veins containing beryllium min­ beryllium minerals occur in silicic and alkalic igneous erals are of high-temperature origin and may form rocks, especially pegmatites, in pyrometasomatic de­ about the same time as pegmatites and pyrometasomatic posits, and in high- to medium-temperature veins. deposits. Beryllium deposits thus are mainly the products of The reasons for deposition of beryllium in pegma­ igneous activity, rather than of sedimentary and meta- tites or veins at some localities and in pyroni etasomatic morphic processes. Figure 3 shows the distribution deposits at others are not clear. In the Victorio Moun­ tains, N. Mex., beryl crystallized in an open vein about

IGNEOUS ROCKS the same time that helvite replaced limestone nearby. Most pyrometasomatic deposits do not have any direct ___ FELDSPAR, relation to pegmatites or even to neighboring igneous rocks. In pyrometasomatism the ease and pervasive­ ness of replacement implies high concentration of water and other volatiles. Although a moderate concentra­ CHRYS08ERYL tion of volatiles appears necessary for the growth of large crystals in pegmatites, detailed studies of their structure and composition suggest that they are formed from an equivalent body of magmatic material, with only minor and later hydrothermal alteration (Cam- eron and others, 1949, p. 97-106). According to this view, preexisting fissures are required for emplacement FIGUBE 3. Schematic diagram showing occurrence and distribution of of pegmatites, whereas pyrometasomatism may be ac­ principal beryllium-bearing minerals. complished through rock pores without recourse to of the common beryllium-bearing minerals among the larger openings. Veins are regarded usually as fissure various types of major occurrence. Such a diagram fillings. In a general way, structural conditions may cannot, of course, be quantitative with regard to the thus influence to some extent the modal occurrence of amount of any mineral; thus, the arrangement of col­ beryllium in that commonly beryl appear? to prefer umns is not necessarily significant. fissure deposits and helvite to favor replacement bodies. Theoretical considerations discussed by Osborn Structural features presumably have little to do, how­ (1950) lead to the conclusion that beryllium should be ever, with the presence or absence of beryllium in the concentrated in the late aqueo-igneous residue of a deposits. magma, as a result of fractional crystallization, along Whether beryllium appears at a given locality pri­ with Si, F, Li, Na, K, and rare earths. These elements, marily in pegmatites, in veins, or in pyroir etasomatic together with water, generally are not removed in pro­ deposits is concerned also with relations of the pegma­ portion to their abundance in the magma during the tite melt and the hydrothermal fluid. Petrologists do crystallization of olivine, pyroxene, amphibole, and not agree on whether the two fluids exist as separate plagioclase, which constitute the bulk of earlier min­ phases in the rest magma or are parts of a single water- erals in igneous rocks. Their proportions in the re­ silicate system. Objections by Morey (19*9) to the maining liquid, therefore, tend to increase progressively hypothesis of immiscible fluids as postulated from theo­ with crystallization, which is controlled largely by the retical studies by Neumann (1948) and the qualitative concentration and stereochemical properties of the ions. experiments of Smith (1948), seem to have been re­ Temperature is regarded as more important than moved by recent quantitative experiments proving im- pressure. miscibility in systems similar to magmas (Tuttle and Distribution of beryllium in igneous rocks and min­ Friedman, 1948). It remains to be proved that such eral deposits suggests that much of it is deposited in immiscibility did in fact exist in the natural processes beryl and helvite during the transition from magmatic of pegmatite and vein formation. COMMERCIAL POSSIBILITIES AND SUGGESTIONS FOR PROSPECTING 59 In practice, the distinction between quartz-rich peg­ in the late silicic and alkalic differentiates of igneous matites and quartz veins is actually somewhat arbitrary; magmas is based on averages of many analyses rather in this investigation those bodies with an appreciable than on specific examples. In some igneous rock series amount of feldspar were considered as pegmatites. whose trace elements have been analyzed in detail Many examples of gradation between the two have been (Nockolds and Mitchell, 1948; Wager and MitcHll, described (see compilations by Tolman, 1931, and Fur- 1943), the amount of beryllium concentrated in the f nal nival, 1939) and the beryl-bearing veins of Mount An- differentiates (granophyre and aplite) is too small to tero, Colo., Hill City, S. Dak., Irish Creek, Va., and be detected by qualitative spectrography. Although several foreign localities are all described as being analytical data indicate that granitic and syenitic rocks closely related to neighboring pegmatites. Fersman are on the average richer in beryllium than mafic ro".ks, (1940, p. 37-39) emphasized the genetic relation of many some granodiorites and other intermediate types con­ quartz veins to pegmatites, and recent structural studies tain appreciable quantities of beryllium. These dis­ of pegmatites have shown that many quartz-rich (and crepancies may be due, of course, to differences* in sometimes beryl-bearing) fracture fillings are continu­ beryllium content of the magmas involved, but it is ous and contemporaneous with the quartz core or other not certain that beryllium is inevitably concentrated in inner zone of the associated pegmatite (Cameron and the late magmatic products. others, 1949, p. 70-83, 105-106). These associations At Mount Antero, Colo., and Bagdad, Ariz., rather suggest that some beryl-bearing quartz veins have an complete gradation is found from a granite so ricl in origin similar to pegmatites, if they are not actually beryllium that it occurs as grains of beryl, through be~yl- continuations of neighboring pegmatites. They were bearing schlieren, vugs, and small veins to conventional probably formed at high temperatures from "magma- pegmatites. Such deposits have not been sufficiently like liquid" (Jahns, 1948). studied to determine the relations between beryl and The temperatures of formation of pegmatites, pyro- other rock minerals. However, in the Sheeprock Moun­ metasomatic deposits, and hypothermal veins probably tains, Utah, beryl replaces feldspar in an albite granite are similar. The prevalence of helvite and idocrase in and appears to have been introduced in connection vith pyrometasomatic deposits in contrast to beryl in peg­ albitization of the granite. matites and veins is, therefore, probably due to chemical The concentration of beryllium in pegmatites nay environment rather than to temperature. In syenitic have been exaggerated. Moderately rich beryl pegma­ pegmatites, helvite or rare aluminum-poor beryllium tite ore contains only about 1 percent beryl, or about 0.1 minerals occur, whereas, in pyrometasomatic deposits in percent BeO (Hartley and others, 1950, p. 11). This aluminous schists the mineral is beryl. Such occur­ does not take into account beryl that is too fine grained rences are rare, however, as most pegmatites are gran­ for hand sorting or that lies in unmined zones. If one itic and most pyrometasomatism is in calcareous rocks. considers that only a small percentage of pegmatites Where the ratio of aluminum to calcium, sodium, and contain enough beryl to be mineable, it is apparent that potassium, is greater than one, some aluminum is avail­ the overall average beryllium content of pegmatites able to form beryl; otherwise helvite may form (Holser, may not be appreciably higher than that of the average 1953, p. 608). granitic or feldspathoidal rock. A somewhat wider range in temperature of formation Many sedimentary rocks and residual deposits con­ is noted for helvite than for beryl. In pyrometasomatic tain some beryllium and beryllium shows some tendency deposits helvite is generally late in the mineral sequence, to follow aluminum in sedimentary processes. For the often lining vugs. The manganese-rich veins in which most part, however, beryllium probably tends moro to it occurs apparently formed at a lower temperature be dissipated than concentrated by processes of weatl ^r- than the beryl-bearing quartz-tungsten veins. The as­ ing and sedimentation. Little information is available sociation of a nearly pure manganoan member of the concerning the beryllium content of metamorphic rocks, helvite series with sphalerite in veinlike deposits in the but there is no indication that beryllium tends tc be Carpenter district, New Mexico, in contrast to the oc­ concentrated by processes of dynamic and regional meta- currence of zinc-rich genthelvite in the pegmatites at morphism. St. Peters Dome, Colo. (Genth, 1892), suggests that at least this helvite-bearing vein was formed at a tem­ COMMERCIAL POSSIBILITIES AND SUGGESTIONS FOR perature far enough below that of pegmatites to de­ PROSPECTING crease considerably the solubility of zinc in the helvite The deposits of beryllium in nonpegmatite rocks that lattice. are most likely to be of commercial interest fall into The thesis that beryllium tends to be concentrated two categories: beryl in high-temperature veins and 60 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES igneous rocks, and helvite in pyrometasomatic deposits. tonnage of ore for tungsten, gold, lead, or other metals. Beryllian idocrase commonly occurs with helvite, The possibility is indicated by recovery r,t Climax, though it is probably never high enough in beryllium Colo., of cassiterite from molybdenum ore containing content to make its separation profitable. Its effect, only a trace of tin (Gustavson and Umhau, 1951, p. therefore, is to make some of the beryllium contained 1195). in the deposit economically unrecoverable. Other sili­ Where a large proportion of the beryllium is dissem­ cates which contain beryllium, such as garnet and epi- inated in minor amounts through the principal rock dote in pyrometasomatic deposits, and micas and feld­ minerals, instead of occurring as beryl or lelvite, the spars in igneous rocks, have a similar but lesser effect. problems are much greater. High temperatures or The best nonpegmatite beryllium deposit yet discov­ very strong acids are required to decompose silicates ered is that at Iron Mountain, N. Mex., where a small such as idocrase, nepheline, and garnet and release their tonnage of high-grade tactite ranges from 0.5 to 3.5 beryllium. Eecovery of beryllium from such minerals percent BeO, with an average of less than 1.0 percent, does not seem likely at present. Even for minerals mostly in helvite. The low-grade material ranges more susceptible to chemical treatment, such as the from 0.1 to 0.85 percent BeO, with an average of 0.3 cryptomelane of Golconda, Nev., recovery would be percent, but only a small part of this beryllium occurs relatively expensive. Traces of beryllium in minerals in helvite (Jahns, 1944a, p. 59). Vein deposits in might be recovered as a byproduct in smelling to re­ Arizona and New Mexico contain from 0.01 to 0.1 per­ lease other metals. However, most smeHers treat cent BeO, presumably all in beryl. These grades com­ mainly sulfide ores, which are unlikely to certain beryl­ pare very favorably with those of beryl pegmatites, lium. Sampling of many zinc, lead, and copper smelt­ where the zones mined for beryl range from 2 percent ers by the Mine, Mill, and Smelter Survey showed no down to less than 0.1 percent beryl, or about 0.2 to 0.01 beryllium in any of the products. Nonsulfide ores, such percent BeO. as bauxite, have a remote possibility of producing beryl­ Despite the fact that several thousand tons of high- lium, but bauxites from the United States apparently grade material are indicated at Iron Mountain, the contain very little. deposit has not been mined, principally because it is The lack of a reliable method of beryllium analysis, fine grained. In inner pegmatite zones, some of the with the attendant problem of separating ore from beryl crystals which are several feet long are easily waste during mining, is an important economic factor. hand sorted, or selectively mined, to give a concentrate Although some pegmatite beryl is difficult tc recognize, above the marketable minimum of 8 percent BeO. the problem is greatly increased when the material is Such treatment is impossible with the fine-grained ma­ fine grained. At Iron Mountain, N. Mex., much of the terial of all nonpegmatite beryllium deposits. Flota­ helvite-danalite cannot be distinguished from garnet tion of both beryl and helvite ores has been moderately except by a stain test. Some or all of the beryllium in­ successful on a laboratory scale (Lamb, 1947; Sned- dicated by chemical or spectographic analyses may be don and Gibbs, 1947; Kennedy and O'Meara, 1948). contained in rock minerals as a guest element rather However, when metallurgical concentration becomes than in beryllium minerals. Microscopic mineralogical widely applied to fine-grained beryl, the nonpegmatite analysis is therefore recommended as offerirg the most deposits that could be worked would still have to com­ realistic estimate of recoverable beryllium. Occasional pete with pegmatite deposits, many of which also con­ control determinations of total beryllium content might tain beryl too fine grained for recovery by sorting. be made by spectrography. In the Black Hills pegmatites, no deposits have been The importance of nonpegmatite beryllium deposits mined exclusively for beryl, it having been recovered is exemplified in the Soviet Union. According to as a byproduct of mica, feldspar, or lithium-mineral Scherbakov (1936) the Izumrudnie (emerald) mines of mining (Page and others, 1953, p. 52). Similarly, the Southern Urals have greater possibilities than all byproduct recovery of fluorite and magnetite may make the other regions of the Soviet Union as a source of it possible to mine the Iron Mountain tactite at a profit. beryllium. Although associated with berylliferous peg­ Prospecting for nonpegmatite beryllium should be matites, the principal deposits are in the s irrounding only part of a general prospecting program, as the schists and slates. The second most important are the beryllium can probably be recovered only in conjunc­ Sherlovoi Mountain deposits in Zabaikal, v^nere beryl tion with some other metal or mineral. Actually the occurs in quartz veins and greisen zones in granite. Al­ greatest hope is probably in byproduct recovery of though none of the deposits thus far discovered in the beryllium from high-temperature veins or pyrometa­ United States is exactly analogous to these, the possi­ somatic deposits that are presently producing a large bilities for discovery are not exhausted. LOCALITIES IN NEVADA AND CALIFORNIA 61

Most prospecting for nonpegmatite beryllium prob­ logical Survey in 1943 and was not revisited. Cameron ably will be confined to pyrometasomatic deposits and found it necessary to return to other work before com­ high-temperature veins. The relationship of beryllium pletion of the laboratory investigations. The analytical and fluorine minerals has been noted in many of these data were compiled by Warner, who also wrote parts deposits, and the association of idocrase and fluorite in of the descriptions. The descriptions of deposits are pyrometasomatic deposits is thought to be a reliable based partly on observations made during the sampling, guide to beryllium occurrence. A similar relation but free use was made of information in the literature between beryllium and tungsten is suggested by the and of unpublished reports and maps compiled by ^ar- widespread occurrence of beryllium in tungsten-bearing ious geologists of the U. S. Geological Survey during tactites and veins. World War II. In general, mineralogical criteria appear to be some­ Of the more than 300 samples that were collected and what more reliable than structural features, though the analyzed spectrographically for BeO, the larger num­ latter may also be clues to beryllium occurrence. Some ber are from tungsten deposits in which scheelite is beryllium-bearing tactites show a peculiar banded the dominant tungsten mineral. The field itinerary, structure, called "ribbon rock" at Iron Mountain, N. therefore, conforms in a general way to the tungsten Mex. Material of this type was not found during the arcs in the Basin and Range province as shown by F"err present investigation in any of the beryllium-bearing (1946a, pi. 1). A variety of other materials, how­ tactites. Similar banded magnetites were completely ever, was sampled in Nevada, including the manganese free of beryllium. The absence of this structure, there­ and tungsten-bearing hot-spring deposits at Golccnda fore, does not preclude the possibility of the occurrence and Sodaville, the barite deposits at Good Hope and of beryllium in tactites; that all "ribbon rock" contains near Battle Mountain, andalusite deposits near Thcrne, beryllium remains to be proved. Most pyrometaso­ brucite-magnesite deposits at Gabbs, and a dumortierite matic deposits that contain beryllium are found near deposit near Oreana. Samples of igneous rocks and the contact of limestone and granodiorite or granite. contact-metamorphosed sedimentary rocks in and ad­ However, beryllium-bearing tactites, like other pyro­ jacent to the ore deposits were obtained in nearly all metasomatic deposits, commonly being controlled by districts visited in which contact metamorphic tungs­ fractures or high-porosity limestone, may not be closely ten deposits occur. related to contacts. At Iron Mountain and Victorio The' analytical results suggest that in this region Mountains, N. Mex., intrusive rocks are relatively in­ beryllium occurs in greater concentrations in the tungs­ conspicuous. ten-bearing tactite than in the other deposits sampled. As beryllium comes into greater use and the present Of the 4 samples containing more than 0.01 percent resources are exhausted, it will become increasingly BeO, 3 were from tactite deposits at the Star, Victory, necessary to find new resources by scientific means. For and Rose Creek mines; they contained 0.056 percent, this purpose a really basic understanding of the geo­ 0.044 percent, and 0.024 percent of BeO, respectively. chemistry of beryllium is necessary, especially an un­ Samples containing more than 0.001 percent BeO were derstanding of the relations among beryllium-bearing obtained from all tactite deposits, though the average minerals, and the physical and chemical conditions of for some deposits particularly at the Desert, Gun- their deposition. Further investigations of the natural metal, and Ragged Top mines and deposits in the Paw- occurrences should be supplemented by experiments un­ hide district is considerably less than this amount. der controlled laboratory conditions. The BeO content of samples from tactite in the Mill City district, Nevada, and the Tungsten Hills district, DESCRIPTION OF LOCALITIES California, were relatively low in comparison to the NEVADA AND CALIFORNIA importance of these districts as tungsten producers. In general there is no apparent correlation between By E. N. CAMERON and L. A. WARNER the amounts of tungsten and beryllium in the tactite Sampling of nonpegmatite rocks and mineral de­ deposits. posits in Nevada and central California was undertaken The beryllium content of the tungsten-bearing by Cameron, assisted by J. H. McLeod, during July and tactite is in marked contrast to that of associated horn- August 1949. In the short time available only a few of fels, marble, and quartzite. Though many samples of the many mining districts of the region could be ex­ these rocks were obtained, none contained BeO in ercess amined. Locations of the 27 districts and areas selected of 0.001 percent. The beryllium contents of igneous for investigation are shown on figure 4. One of these, rocks associated with the tactite is also low, the few the Tern Piute district, had been sampled by the Geo­ exceptions being for samples obtained adjacent to con- 62 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES

120'

NEVADA strict having sample containing Blko Count- ore than 0.005 percent beryllia 1 1. Star mine, Harrison Pass 2. Good Hope mine Humboldt Cornty 3. Golconda deposit Lander County 4. Battle Mountain barite drnosits Lincoln Courty 5. Tern Piute district Mineral Courty 6. Rawhide district 7. Desert Seheelite and Gunmetal mines 8. Sodaville district 9. Thorne andalusite deposits Nye County 10. Victory Tungsten deposits 11. Gabbs magnesite and bruc'te Pershing County 12. Limerick Canyon area 13. Panther Canyon area 14. Rocky Canyon-Wrignts Canyon area 15. Tungsten area 16. Rose Creek mine 17. Ragged Top mine 18. Champion dumortierite nine White Pine County 19. Cherry Creek district 20. Sacramento Pass mine 21. Dirty Shirt mine 22. San Pedro mine 23. Minerva district CAIiIFOBHIA Inyo Count1" 24. Tungsten HiUs district 25. Pine Creek district 26. Yaney prospect San Bernardiuo and Kern Counties 27. Atolia district

FIGURE 4. Index map showing localities sampled in Nevada and California. tacts with tactite, where endomorphism might be ex­ less than 0.0001 percent. The paucity of beryllium in pected. These relations imply that beryllium was in­ these veins, in contrast to its relative almidance in troduced by ore-forming solutions which gave rise to pyrometasomatic deposits nearby, apparently is more the tungsten-bearing tactites, the two metals being de­ marked in the Basin and Eange province tl *n in other rived from a common magmatic source. areas where beryl is not uncommon in quartz-tungsten Several scheelite vein deposits were sampled in the veins. The beryllium-bearing hot-spring deposits of Snake Range and Cherry Creek district, Nevada, and in Pleistocene age at Golconda and Sodaville, Nev., must the Atolia district, California. None of the samples con­ be regarded as extraordinary. These are ccherous de­ tained more than 0.001 percent BeO and most contained posits containing relatively large amounts of manga- LOCALITIES IN NEVADA 63 nese and tungsten. A sample from the deposit at Gol- Samples were taken of the metamorphosed rocks of conda contained 0.016 percent BeO, and one from Soda- the contact aureole, as well as of the tactite deposits. ville contained 0.0075 percent. Sample descriptions and analytical results are given in the table 17. NEVADA TABLE 17. Beryllia in samples from Harrison Pass area EUKO COUNTY BeO Sample Description (percent) STAB MIKE, HARRISON PASS NOETH OPEN CUT The deposits of the Star mine are in the Ruby Range 329-1039 Chip sample of aplitic granite 10 to 30 ft from tactite_____-______0. 0002 on both sides of Harrison Pass Creek Canyon, about . 1040 Chip sample of tactite______._ . 0044 2 miles east of the pass. They are readily accessible by 1041 Chip sample altered aplitic granite im­ mediately adjacent to tactite____-__-_ . 0098 road from Elko by way of Jiggs, thence by the road over 1042 Silicated marble 0 to 3 ft from tactite_ __ <. 0001 Harrison Pass. The area is described briefly by Hess and Larsen (1921, p. 305); the deposits were mapped SOUTH SHAFT QBE BODY 329-1043 Chip sample of tactite body, north end of by M. R. Klepper and P. Joralemon of the U. S. south stope at its base______. 029 Geological Survey in 1943. 1044 Chip sample .from tactite body, top of south stope--_-__---_-_---___--___- . 056 The Ruby Range consists largely of a stock of biotite 1045 Chip sample of silicated marble adjacent to tactite, bottom of north stope____ <. 0001 granite and quartz monzonite that intrudes limestone 1046 Chip sample of silicated marble adjacent and quartzite of Paleozoic age. The contact east of to tactite, base of shaft______<. 0001 1047 Chip sample of granite outcrop adjacent Harrison Pass is very irregular; and many dikes and to tactite, north of shaft______. 0078 apophyses of aplitic granite cut the sediments, which CONTACT-METAMORPHOSED BOCKS have been metamorphosed to silicated marble and horn- 329-1048 Chip sample of recrystallized marble, 0 to fels. Scheelite-bearing tactite occurs intermittently 15 ft from contact.______<. 0001 1049 Chip sample of blue and gray marble, along the contact. Four ore bodies have been mined partly silicified, 15 to 70 ft from con- on the property of the Star mine and several others have tact______<. 0001 1051 Chip sample of blue and gray silicified been prospected. The principal workings, which are in limestone, 150 to 170 ft from contact. _ <. 0001 the Main, North, and South ore lodes, were inaccessible 329-1054 Chip sample across beds of idocrase- bearing(?) marble, 345 to 365 ft along in 1949. The No. 7 ore body and the ore bodies in the road from contact______<. 0001 North opencut and the South shaft were examined 1055 Chip sample of interbedded pure and sili­ cated marble, 656 to 681 ft from con- briefly. tact______<. 0001 The North opencut exposes a tactite body along the 1057 Chip sample across beds of bluish-gray, fine- to medium-grained marble, 1,053 irregular boundary between granite and marble. The to 1,233 ft along road from contact__ . 0008 body is 1 inch to 30 inches thick, not more than 20 feet 1059 Chip sample across beds of blue-black limestone, 1,520 to 1,540 ft along road long, and probably contains no more than 200 tons of from contact_-_--_---__---_--__---_ . 0008 rock. The tactite consists of garnet, diopside, epidote, 1061 Chip sample of silicated marble and horn­ fels, south slope of Harrison Pass Creek quartz, and calcite. Canyon, between No. 7 ore body and Main ore body..______<. 0001 The South shaft ore body is a tactite mass about 200 1063 Chip sample of porphyritic granite, sum­ feet in strike length and 1 to 4 feet wide. A vertical mit of Harrison Pass______<. 0001 shaft, 43 feet deep, has been sunk near the middle of The analytical data clearly indicate that beryllium is the outcrop. From the bottom of the shaft a drift ex­ contained in the tactite bodies and in the granite imme­ tends along the base of two stopes; the south stope is diately adj acent to them. It appears to be lacking in the blind, the north stope extends to the surface. The other rocks of the contact aureole and in the interior tactite body appears to be cut off at depth either by a of the granite stock. Presumably the solutions that fault or by a change in strike of the contact of the formed the tactite bodies and related tungsten ores were granite and marble. Reserves are no more than a few those which brought in beryllium. The beryllium-bear­ hundred tons. ing mineral or minerals have not been identified. If A belt about 1,500 feet wide along the irregular east­ most of the beryllium is in helvite, some byproduct re­ ern margin of the granite stock consists of marble, sili­ covery may be possible in connection with future min­ cate-bearing marble, and calc-silicate hornfels. The ing of tungsten in the area. beds range from fractions of an inch to 3 feet in thick­ ness. Garnet, diopside, and epidote are the principal GOOD HOPE BARITE MINE, TUSCARORA RANGE minerals, but actinolite, idocrase, and tremolite char­ The Good Hope mine is on one of a series of Hrite acterize some beds. vein deposits in the Tuscarora Range. The mine is 64 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES reached by a road leading north to Lynn from U. S. eastern end of the hill and underground workings of Highway 40 at Carlin, Nev. At 7.4 miles from U. S. unknown extent. 40 and just south of the mouth of Maggie Creek Can­ In the northwest workings, two parts of the stopes yon, a mine road turns westward. The mine is about were sampled. The section exposed in the stopes is as 1.3 miles from this point on the northeast side of a follows, from top to bottom: small canyon. 4. Thin layer of gravels. The deposit, as exposed in the main and upper work­ 3. Coarse rubble (fanglomerate?) cemented by calcareous tufa; ing, is an irregular vein of massive, fine- to coarse­ as thick as 6 feet. This is the cap of the deposit. 2. Rubble tufa with manganese oxides and ocher, 1 to 3 feet grained, white barite that apparently occupies a shat­ thick. Apparently this zone was mined for rcanganese. tered zone in partly silicified interbedded limestone, 1. Rubble poorly cemented by tufa. Thickness more than 3 shale, and sandstone. The vein strikes N. 38° W. and feet; bottom is not exposed. Contains som* manganese dips 70° to 80° E. The lower working consists of a oxides and ocher, but much less than zone 2. 41-foot drift along the vein, which is 4 to 5 feet wide, At Bed Springs Hill, in the opencuts near the north and an adit that extends northward from the mouth end, the beds dip gently westward and are as follows, of the drift. A chip sample (329-1071) of the vein from top to bottom: from the upper working contain 0.0007 percent BeO. 5. Thin layer of gravels. 4. Calcareous tufa caprock, as thick as 5 feet. The lower 12 HUMBOLDT COUNTY inches in places is manganese rich. 3. Layer rich in manganese oxide and ocher, ranging along GOLCONDA MANGANESE-TUNGSTEN DEPOSIT strike from iron-rich to manganese-rich; 9 to 18 inches thick. The Golconda manganese-tungsten deposit is in the 2. Gray shale rubble as much as 2 feet thick. Low in man­ Edna Mountains about 3 miles east of Golconda. The ganese and iron content. mine is a short distance north of U. S. Highway 40 1. Soft shale of Triassic age, forming the surface upon which zones 2 to 5 were laid down. Manganifer^us and fer­ and immediately east of the road to the Getchell mine. ruginous. This material has been mined to a depth of at The deposit has been described by Kerr (1940; 1946a, least 10 feet in the opencut. p. 171-173). It was mined for manganese during Descriptions and analytical data for samples from World War I and for tungsten during World War II. the north workings are given in table 18. The deposit consists of layers of manganiferous ocher and calcareous tufa, with some rubble derived from un­ TABLE 18. Beryllia in samples from north workings, Golconda derlying Triassic sedimentary rocks, and is capped by manganese-tungsten deposit BeO tufa and fanglomerate. The ore bodies extend north­ Sample Description (percent) ward along the slopes for about a mile. Toward the BED SPRINGS HILL east they rest directly on the beveled edges of the Trias­ 329-1073 Chip sample, calcareous tufa, zone 4 _ _ _ _ 0. 0008 sic sedimentary rocks, but toward the west an increas­ 1074 Chip sample, manganese-rich material, base of zone 4._-__-_-______.0026 ing thickness of sedimentary rocks intervenes between 1075 Channel sample, manganese-rich material, the deposits and the bedrock surface. A typical pedi­ zone 3-__-___-_--_---_---_-_-_----- . 0045 1076 Channel sample, ocher-rich materif', ment-alluvial fan relation is indicated. The tungsten- zone 3______-_--_-_--_------__ . 0037 bearing manganese oxides and ferruginous ocher, to­ 1077 Channel sample, zone 1______.0016 1078 Chip sample, small lens of ocherous tufa gether with the tufa, were deposited by hot springs in zone !____.______.0058 thought to have been most active during the Pleistocene epoch. Fissure veins in the underlying Triassic sedi­ NORTHWEST WORKINGS mentary rocks contain ore material similar to that in 329-1079 Chip sample, zone 3______.0007 1080 Channel sample, zone 2______.0058 the overlying ocherous deposits. 1081 Channel sample, zone 1 ______. 001 For the present purpose the workings are divided into two groups: the north workings, which consist SOtTTH WORKINGS largely of opencuts and stopes, and the south workings, The south workings consist of three larpre opencuts which are a series of large opencuts. arranged roughly along a line trending northeast for about 2,000 feet. The northeastern cut is at out 600 feet NORTH WORKINGS long and 200 feet in maximum width; the middle one The workings of this group may be subdivided into measures about 700 feet by 700 feet. The southeastern the northwest workings, which are a series of adits that cut was not measured. It is the largest and deepest of lead to gently inclined stopes, and the Bed Springs the three cuts, but its walls are not accessible for Hill workings, which consist of opencuts around the sampling. LOCALITIES IN NEVADA 65 In the northeastern cut the section is as follows, from tungsten-bearing material. According to Kerr (1P40, the top down: p. 1385-1387), warm spring waters rose along fissures 4. Tufa cap, more than 3 feet thick. in the Triassic rocks, the outflow resulting in beds of 3 Manganese-rich layer, thickness greater than 4 feet; bottom calcareous tufa, together with tungsten-bearing lirao- not exposed. Mined in underground workings of unknown nitic and manganiferous material. He concludes that extent. iron and manganese were precipitated as gel products, 2. Shale rubble, at least 4 feet in maximum thickness. This which adsorbed tungstic oxide from the solution?, a material is highly variable. In part it appears nearly barren of iron and manganese oxides, in part it is rich in process which could just as well result in the presence one or the other. of beryllium. Tungsten occurs in hydrated ferric oxide, 1. Shales of Triassic age containing manganese and iron oxides. psilomelane, and hollandite; the beryllium-bearing In the middle cut samples were obtained from the minerals are not known. east wall and the southwest wall. Along the east wall The thickness and composition of the layers in the the section is as follows, from the top downward: Golconda deposits are extremely variable along strike and dip. Only detailed exploration and sampling 4. Fanglomerate, 6 to 8 feet thick; rests on the uneven top of of a layer of compact calcereous tufa. would serve as a basis for estimating reserves. 3. Calcareous tufa, 3 to 7 feet thick, bottom gently undulating. 2. Manganifereous fangloinerate, 9 inches to 2}£ feet thick. LANDER COUNTY 1. Ferruginous fanglomerate, thickness more than 4 feet; bot­ BARITE DEPOSITS, BATTLE MOUNTAIN AREA tom concealed. Along the southwest wall the section is as follows: Many barite deposits, some of commercial impor­ tance, are found in northern Lander County, northern 5. Fangloinerate, a maximum of 4 feet in thickness. 4. Manganese-bearing, fractured tufa, 3 to 4 feet thick. Eureka County, and west-central Elko County, espe­ 3. Manganese-rich tufa, 2 to 3 feet thick, forming a series of cially in the Tuscarora and Shoshone Ranges. Tlie lenses in the tufa cap. The largest lens is about 30 feet barite deposits are of two general types: vein deposits long. of white barite, in some areas associated with metallif­ 2. Manganese-free tufa, 4 to 4}£ feet thick. erous deposits; and bedded gray barite generally con­ 1. Crossbedded green and brown gravels, containing ocherous layers and manganiferous layers as thick as 2 inches. sidered to have formed by replacement of limestone. The veins have supplied small tonnages of barite, some Data for samples from the south workings are given of exceptional purity. The bedded deposits contain in table 19. large tonnages of barite ranging from 80 to 93 percent barium sulfate and are the main producers. Samples TABLE 19. Beryllia in samples from south workings, Golconda manganese-tungsten deposit from deposits of the latter type were obtained from BeO mines of the California-Nevada Barite Co. and the Sample Description (percent) Barium Products Corp., Ltd. NOETHEASTEEN CUT 329-1084 Channel sample, zone 3-______0. 0023 1085 Channel sample, manganese-rich rubble, CALIFORNIA-NEVADA BARITE CO. MINE zone 2, southeast wall of cut-______.0023 1087 Chip sample, ocherous material overlying The California-Nevada Barite Co. mine is reached by shale rubble of zone 2, southeast wall about 2 miles of steep but well-graded gravel road that of cut.______.016 1086 Composite channel sample, zone !______.0024 turns south from U. S. Highway 40 at a point 12.9 miles east of the junction of TJ. S. Highway 40 and MIDDLE CUT, EAST WALL 329-1088 Chip sample, zone 3______<. 0001 State Highway 8A. The mine is near the crest of the 1089 Composite channel sample, zone 2___.__ .0035 northwest spur of the Shoshone Range. 1099 Composite channel sample, zone !______. 0002 The workings are a series of opencuts extending for MIDDLE CUT, SOUTHWEST WALL about 2,200 feet along the eastern side of the ridge. 329-1092 Chip sample, zone 4______. .0027 The principal workings are in the southern 900 feet 1094 Chip sample, zone 1______. 005 and consist of five opencuts and several minor open­ ings. The workings are in a belt 300 feet wide that OCCUEEENCE AND DISTRIBUTION OF BERTLLIUM trends about N. 20° W. The mine is owned and oper­ Analytical data indicate that beryllium in the Gol­ ated by the California-Nevada Barite Co., subsidiary conda deposit is contained mainly in the manganiferous of the Glidden Co. ocher, which has been mined for its tungsten content, The deposit consists of beds of barite, with an ag­ rather than in the tufa caprock or the underlying gregate thickness of at least 40 feet, interbedded vith Triassic sediments. Presumably, the beryllium is thin beds of chert, silicified limestone, and shale. The genetically related to solutions which deposited the barite beds mostly range from an inch to a foot in 467945 59 6 66 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES thickness and appear to be thickest and least inter­ recrystallized. Shales are altered to hornfels and sand­ rupted by chert partings in the southern 900 feet. The stones to quartzite. West of the south stock are thick structure of the deposit is highly complex. The barite tactite bodies in bands parallel to the bedding; little beds in general appear to be dipping to the east at tactite has been found near the north stock. moderate angles, but there is local folding and much Minerals observed in the tactite and listed in approx­ faulting. Table 20 gives the beryllia content of samples. imate order of abundance are: garnet, quartz, actino- lite, calcite, fluorite, pyrite, pyrrhotite, diopside, sphal­ TABLE 20. Beryllia in samples from the California-Nevada erite, scheelite, chlorite, hematite, clinozoisite, epidote, Barite Co. mine BeO molybdenite, and powellite. Most of the scheelite oc­ Sample Description (percent) 329-1064 Chip sample, bed by bed of about 15 ft curs in garnet tactite but some rich deposits have been of chert beds immediately above main found in small masses of calcite-fluorite-sphalerite rock barite zone______<0. 0001 1065 Chip sample, bed by bed across main formed in marble remnants adjoining tactite bodies. barite zone; represents about 30 ft of Products of the mill at Hiko were sampled for the beds______<. 0001 1066 Chip sample, bed by bed, of 5 ft of inter- Mine, Mill and Smelter Survey in 1943. Data for these bedded barite and chert immediately samples are given in table 21. beneath footwall of main barite zone__ . 001

BABIUM PRODUCTS CORP., LTD., MINE TABLE 21. Beryllia in mill products from the Tern Piute

The Barium Products Corp., Ltd., mine is 26 miles Sample Description BeO (percent) south of Battle Mountain in Lander County, by way 49-DGW-20 Grab sample of scheelite tailings, and of State Highway 8A. A good gravel road leads from sulfide float tails (lS(42-43 produc­ tion)-.______---.______.__ 0. 002 the highway about a mile to the mine. The workings 21 Same (1940-42 production)______.003 consist of an opencut about 260 feet long, 210 feet wide, 22 Grab sample of test run on scheelite mill tailings____-___-_----___------__- . 001 and 20 feet in maximum depth. The deposit is a 23 Scheelite concentrate (composite of warped and moderately faulted westward-dipping samples collected by company) ______. 001 sheet that extends from the crest of a low hill down MINERAL, COUNTY the northwest slope for about 280 feet. The deposit is probably about 375 feet in strike length. RAWHIDE DISTRICT The barite is similar to that at the Calif ornia- Tactite deposits containing scheelite occur in the Nevada Barite Co.'s mine. It overlies thin-bedded southern part of the Sand Springs Range about 4 miles chert. The overlying beds are not exposed. east of the old mining camp of Eawliide. T^ e deposits A bed-by-bed chip sample (329-1072) taken across are in sees. 1 and 12, T. 13 N., E. 32 E., near the south a 20-foot thickness of barite, beginning a few feet above border of the Carson Sink quadrangle. TJ^ deposits the footwall contains 0.0007 percent BeO. can be reached by a graded road that turn? off U. S. Highway 50 about 35 miles east of Fallen, on the east LINCOLN COUNTY slope of the Sand Springs Eange just below the sum­ TEM PIUTE DISTRICT mit, or by graded roads leading northeasterly for about Scheelite-bearing tactite deposits occur at the north 45 miles from the town of Hawthorne. The deposits end of the Tern Piute Range in the west-central part were mapped by E. F. Stopper and others of the U. S. of Lincoln County, Nev., about 85 miles west of Cal- Geological Survey in 1944. The geology of the area iente. The district is reached by 40 miles of desert and locations of the mines are shown on figure 5. road from U. S. Highway 93 at Crystal, near Hiko. The Nevada Scheelite, Hooper No. 2 and Yankee Girl The principal mines of the district are the Lincoln and mines were visited and sampled. the Schofield, the former accounting for most of the The tungsten deposits are tactite bodies in meta­ production. A mill at Hiko processes the ore. The morphosed limestone and hornfels at or iier.r the mar­ deposits were explored by the U. S. Bureau of Mines gins of a body of granite about a mile wide in outcrop. in 1942 and 1944 (Binyon, Holmes, and Johnson, 1950), The limestone is part of a thick sequence of folded and and were mapped and described by D. W. Lemmon faulted sediments and meta volcanic rocks that were in­ (written communication). truded by granite. The main limestone unit is esti­ The district comprises steeply dipping limestone, mated by Stopper (written communication) to be 400 shales, and sandstones of Paleozoic age which have been to 750 feet thick. Other limestone units ar^ thin beds intruded by two small granite stocks and several nar­ included in hornfels that overlies the main limestone row basalt dikes. For a distance of 700 feet from the unit. The productive deposits are along the west and granite contacts the limestone is bleached and in places north margins of the granite where for some thousands LOCALITIES IN NEVADA 67

EXPLANATION

T. Lower metavolcenic rocks

N.

Contact Dashed where approximately located or inferred

Fault Dashed where approximately located or inferred; dotted where conceaM

-of5 Strike and dip of bed* -4° Strike of vertical bed*

B Sheft

v«Vv-.:: '\: ft:-:': R. 32 E. Geology by R. F. Stopper, April 1944 R. 33 E. 1000 0 2000 Feet I__ i I______I______I FIGURE 5. Geologic map of part of the Rawhide district, Mineral County, Nev. of feet it is in contact with the main limestone or with beds at the mine strike northeast and dip from vertical the overlying hornfels. Tactite bodies, however, occur to steeply southeast. A tactite body 2 to 50 feet -ride only at intervals along the contact; elsewhere limestone occurs along the contact in an irregular zone about or marble is directly against the granite. The tactite 1,800 feet long. In the northern and southern parts of bodies range in thickness from a few inches to 50 feet. the zone, the contact between limestone and granite is The fresh tactite consists of andradite garnet with vari­ nearly vertical and mainly concordant with bedding ous proportions of calcite, quartz, amphibole, epidote, in the limestone. In the middle part of the zone, the pyroxene, wollastonite, pyrite, magnetite, scheelite, and contact strikes northwest and dips 30° to 40° ] TE., chalcopyrite. cutting sharply across the bedding. This part of the NEVADA SCHEELITE MINE contact is believed by Stopper to follow a pregranite The Nevada Scheelite mine consists of an inclined fault along which the beds northeast of the fault h-we shaft leading to levels at 100, 200, and 300 feet, to­ been offset about 350 feet to the northwest. The tactite gether with a series of stopes between the levels. The body is thickest along the middle part of the contact mine is on the west side of the granite stock near a and is absent in places to the north and south, granite sharp bend in the contact (see fig. 5). The limestone being directly against marble. The tactite in this mine 68 OCCURRENCE OF NONPEGMAT1TE BERYLLIUM IN THE UNITED STATES is in large part oxidized. Oxidation is marked on the the drifts is connected with the surface by a shaft. A 200- and 100-foot levels and extends in places below the 25-foot inclined winze leads from the floor of the east- 300-foot level, which is probably about its lower limit. southeast drift to a small stope. Samples of tactite, granite, and marble were obtained. The mine is along the contact of the granite with the No systematic variation in any of these rocks was noted. hornfels that overlies the main limestone unit. Inclu­ The marble is in marked contrast to that associated with sions of limestone that have been metamorphosed to tac­ tactite in other contact metamorphic deposits sampled, tite and marble are exposed in the workings. Hornfels because it contains few silicate minerals representing is in contact with granite at several places in the mine. lower grades of metamorphism. The change from tac­ Sampling data are given in table 24. tite to marble commonly is abrupt, there being no clearly defined light-colored silicated marble zone. Table 22 TABLE 24. Beryllia in samples from the Yankee Girl mine gives beryllia contents. BeO Sample Description (percent) 329-1229 Chip sample of hornfels 6 in. to 12 in. TABLE 22. Beryllia in samples from the Nevada Scheelite mine from contact with granite, near end of BeO northeast drift______<0. 0001 Sample Description (percent) 1230 Chip sample of granite 6 in. to 12 in. froir 329-1189 Chip sample across 15-ft thickness of contact with hornfels of sample 329- marble beds adjoining granite, north 1229____ - <. 0001 end of drift on 300-ft level, about 540 1231 Chip sample across 5-ft thickness of horn­ ft north of shaft. (No tactite zone fels at end of northeast drift ______

^^ Z'-^&Ki . rs :-^- __ \

... "'..... - --4^ ,__lX'^&^.V:T:r^""'v?'r~""~"^.^-

329-1237 329-1236-V.;:

SHAFTB

EXPLANATION

FiuR Approximately located or inferred

Strike and dip of b«ds

B Vertical shaft

Contact Inclined shaft Dashed where approximately 329-1236 located or inferred, dotted Locality sampled and number where concealed

Geology by E. N. Cameron ard 100 200 Feet J. H. Macleod, August 1919

FIGURE 6. Geologic map of part of the Desert Scheelite mine, Mineral County, Nev.

The tactite is fine- to coarse-grained, massive to main working consists of two adits that lead to stopes layered rock consisting of garnet with some quartz, on three levels. The tactite is prevailingly garnet-rich carbonates, and epidote. The color of the garnet but contains also quartz, calcite, epidote, and sch^elite. ranges from red to greenish brown or yellowish brown. A chip sample (329-1242) was taken across the lowest The mineral proportions vary locally and in places the tactite layer exposed in an old foundation excavation tactite is rich in epidote. The silicated marble is main­ north of the adits leading to the main workings. This ly a thin-bedded fine-grained rock of indeterminate layer is exposed for 60 feet along the strike and aver­ composition. The marbles are gray to white, and fine ages 3 feet in thickness. A second sample (329-1243) grained to medium grained. The white marble evi­ was taken across the main tactite bed exposed in a wall dently formed along bedding and cross fractures by between the mouths of two adits in the first stcr>e of recrystallization of gray marble. The gray marble was the main workings. The samples showed no BeO, the derived from blue-black fine-grained limestone similar limit of sensitivity being 0.0001 percent. to that exposed outside the tactite zone. Samples were taken as listed in table 25 and shown on figure 6. MANGANESE-TUUGSTEN DEPOSIT AT SODAVILIE The Sodaville manganese-tungsten deposit, also TABLE 25. Beryllia in samples from the Desert Scheelite mine known as the Black Jack claim, is on a pediment about BeO Sample Description (percent) half a mile west of U. S. Highway 95 opposite the 329-1236 Chip sample across full width of tactite__ <0. 0001 former railroad station at Sodaville. The deposits are 1237 Chip sample, bed by bed, across 15-ft thickness of marble and silicated marble mostly on the crests and flanks of two small knot s that directly underlying tactite, south wall rise above the pediment. They have been described of opencut______-______<. 0001 1238 Chip sample across full width of tactite by Kerr (1946a,p. ITS). (includes 4 ft of interbedded tactite The deposits are veins in two steeply dipping north- and light silicate rock)______<. 0001 1239 Chip sample across full width of tactite__ <. 0001 to northeast-trending fracture zones cutting cherty 1240 Chip sample across lower 10 ft of tactite- <. 0014 rock that forms the knobs and underlies the pediment. 1241 Chip sample across 5-ft thickness of dense thin-bedded green hornfels immedi­ The richest veins are on the eastern knob and the ad­ ately overlying tactite______<. 0001 jacent part of the pediment. They range from less than 1 inch to 2 feet in width and are as much as 20 GTINMETAL MINE feet in length. The veins consist largely of tungsten- The Gunmetal mine is in gently dipping tactite layers bearing psilomelane, with varying amounts of pyro- interbedded with marble and silicated marble along the lusite, wad, iron oxides, calcite, gypsum, quarts, and contact of the beds with quartz-monzonite. The tactite chalcedony. The tungsten content of the psilomelane beds extend as much as 100 feet from the contact. The is reported to be 4.88 percent (Kerr, 1946a). Ke?epves 70 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES are small, and operations at the deposits have never the brown granular mineral. Irregular bodies of simi­ gone beyond the prospecting stage. lar pyrophyllitic rocks are scattered over t^e crest of For comparison with the larger deposit at Golconda, the hill between the northeast opencut anc1 the main a chip sample (329-1235) of high-grade manganese- working. The largest of these bodies appears to be tungsten ore was taken from blocks on various small about 50 feet long and 20 feet wide. ore piles. It contained 0.0075 percent of BeO. Samples taken at the Green Talc mine are described in table 26. ANDALUSITE DEPOSITS HEAR THORHE TABLE 26. Beryllia in samples from the Green Talc mine The andalusite deposits that are exposed on both BeO edges of the Soda Spring Valley a few miles east of Sample Description (percent) 329-1197 Chip sample across 10-ft thickness of Thorne, Mineral County, occur in a belt about 7 miles pyrophyllite-carbonate(?) rock, nortl - long that traverses the lower foothills of the Gillis east wall of lower part of northeast opencut, above layer of dark, altered Range (Hawthorne quadrangle). Another andalusite volcanic rock______<0. 0001 deposit is exposed at the Deep mine, a prospect on the 1198 Chip sample across 10-ft layer of dark altered volcanic rock, underlying rock southeast side of a prominent knoll immediately south of sample 329-1197______. <. 0001 of Highway 95, about 8 miles east-southeast along the 1199 Chip sample across full width (8-10 ft) of andalusite-bearing core rock. Small highway from the center of Hawthorne. opencut north of main working. ______<. 0001 1200 Chip sample across full width (15 ft) of Two deposits on the south edge of the Gillis Range, andalusite-bearing core rock, north ws.ll the Green Talc mine and a mine of unknown name of main working______<. 0001 about 0.4 mile west-northwest of the Green Talc mine, were visited and sampled. MINE NEAB GBEEN TALC MINE An unnamed mine 0.4 mile west-northwest of the GBEEN TALC MINE Green Talc mine consists of a glory hole about 60 feet in The Green Talc mine is on the lower southeast end diameter and about 60 feet in maximum depth. On the of a spur of the Gillis Range. The mine consists of southeast side of the pit there is a vertical shaft re­ three opencuts and a series of prospect pits scattered ported to be about 75 feet deep. over an area about 500 feet long and 125 feet wide, The mine is in a lens of andalusite-pyrophyllite rock trending northeast across the spur. The main working, that strikes N. 65° E. and is nearly vertical. The lens rear the southwest end of the area, is an opencut 100 feet is about 40 feet in maximum width and its strike length long, 90 feet wide, and about 40 feet in maximum depth. is probably not much more than 60 feet. On its north­ At the northeast end of the area is a second opencut west side the lens appears to grade irregularly into about 45 feet long, 45 feet wide, and 25 feet in maximum altered volcanic rock, and on its southwest side it is cut depth. A third, small opencut is immediately north of off by a steeply southeast-dipping, gouge-filled fault the main opencut. zone. The principal body of andalusite-bearing rock appears Chip sample 329-1224 was taken across an andalusite- to be the one exposed in the main working. The core bearing lens exposed in the southwest wall near the of this body strikes N. 5° W. across the opencut and is bottom of the glory hole. It showed no BeO, the limit more than 125 feet in exposed length and 10 to 15 feet of sensitivity being 0.0001 percent. thick. It is exposed to a maximum depth of about 12 NTE COUNTY feet and appears to dip steeply east. The core consists principally of 10 to 50 percent andalusite in blue to GABBS AREA lavender crystals and clusters of crystals % inch to 1 We spent one day near Gabbs, Nov., sampling de­ inch in diameter and 14 inch to 4 inches long, set in a posits of scheelite, magnesite, and brucite. The main green to brownish-green matrix of pyrophyllite. The purpose of the visit was to sample the scheelite-leuch- andalusite crystals are stout, rounded prisms apparently tenbergite vein in the Paradise Range described by Kerr showing marginal alteration to pyrophyllite. In places and Callaghan (1935). Examination revealed, how­ a brownish granular material, possibly a carbonate, is ever, that the vein is poorly exposed and probably of present in the greenish matrix, and locally this is the small tonnage; consequently no samples T^ere taken. dominant constituent. Enveloping the andalusite-bear­ The newly developed Victory tungsten deposits were ing rock is a variety of altered volcanic rocks. examined and sampled. A few samples we-re taken at The northeast cut exposes dark volcanic rocks irregu­ the mine of the Sierra Magnesite Co. and from the larly altered to pyrophyllite, with varying amounts of brucite deposits at Gabbs. LOCALITIES IN NEVADA 71

VICTOBY TUNGSTEN DEPOSITS being worked by the Basic Refractories Co. The work­ The Victory tungsten deposits are in the northwest­ ings consist of two series of large irregular opencuts, ern part of the Tonopah quadrangle and on the south­ one in an upper deposit, the other in a lower one. The west slope of the Mammoth Range about 3 miles west- workings visited are in the upper deposit. They have southwest of Marble. They are in the north part of a maximum depth of more than 350 feet and extend sec. 22, T. 13 N., R. 36 E., and are accessible by a dirt along the strike of the deposit for about 800 feef.. road that turns northeast off State Highway 23 at a The deposits are in a thick series of magnesite and point about 1 mile northwest of the Gabbs airport en­ dolomite beds along the contacts of a northwari-pro- trance road. The deposits are on the crest and north­ jecting prong of a granodiorite stock. The brucite east side of a spur and are at the west border of a north­ formed by hydrothermal alteration of the carbonate ward-trending body of granodiorite. The granodiorite rocks. Irregular masses of dolomite and magnesfite in mass is probably more than a mile long and is at least various stages of alteration are contained in the brucite. a quarter-mile wide. The deposits are of two types: The deposits are capped by blankets of supergene hy- disseminated scheelite in granodiorite, and scheelite- dromagnesite that are as much as 50 feet thick. The bearing contact-metamorphosed calcareous rocks. whole assemblage of dolomite, magnesite, and tmcite Deposits of the first type are exposed in a series of 5 is cut by an intricate network of granodiorite dikes, trenches 30 to 75 feet in length. The surface slopes 22° each bordered by serpentine. The high-grade tmcite E. and the trenches extend for about 250 feet along a is compact and appears soapy. It grades into rock line that trends northwest. The trenches are excavated locally called "limy brucite" that contains much dolo­ in a medium- to coarse-grained biotite granodiorite lo­ mite and calcite. cally containing streaks and patches of quartz. Exam­ Two grab samples of the brucite were obtained from ination by ultraviolet light shows that scheelite is dis­ the lower level workings of the east (upper) ore body. seminated through the rock, but the content varies Sample 329-1245, high-grade brucite, containei less markedly from place to place. A chip composite sam­ than 0.0001 percent BeO; sample 329-1246, limy bru­ ple (329-1248) was taken along 57 feet of the second cite, contained 0.0014 percent BeO. trench (counting from north to south along the line of The extensive deposits of magnesite in this area have trenches) and 37 feet of the third trench. Spectro- been described by Rubey and Callaghan (Hewett and graphic analysis showed 0.0034 percent BeO in the others, 1936, p. 142-143). A sample (329-1244) of raw sample. magnesite obtained from the crusher at the mine of the The second type of deposit is exposed west of the first, Sierra Magnesite Co. contained less than 0.0001 percent in a series of trenches at and near the crest of the same BeO. spur. The trenches are 15 to 30 feet in length and are PERSHING COUNTY spaced at intervals along a line trending northeast for at least 200 feet. They expose an undulating contact ROCKS IN THE WEST HUMBOIDT RANGE of granite with limestone and quartzite. At the crest The West Humboldt Range is noteworthy for the of the spur the contact is nearly horizontal, but it ap­ association of scheelite and beryl in two deposits on the pears to dip west where exposed on the west side of the west slope of the range the Humboldt Canyon beryl- spur. Along parts of the contact where limestone abuts scheelite prospect and the Oreana tungsten mine. With against granite, a zone of silicated marble 6 inches to the idea that these deposits might indicate the presence 2 feet thick is present. The minerals present include of an unusual amount of beryllium in one or more of biotite, chlorite, and possibly amphibole and pyroxene. the several types of granitic intruded rocks exposed in In the two southernmost trenches a well-exposed con­ the range or in the contact-metamorphic rocks border­ tact zone, according to local report, contains the best ing them, a fairly extensive program of sampling was showing of tungsten along the west contact of the gran­ undertaken. odiorite. A chip sample (329-1249) of the contact- LIMERICK CANYON AKEA metamorphosed material was taken along the 25-foot Large masses of aplite have been described by Fnopf length of the southernmost trench and was found to (1924, p. 33) and Jenney (1935, p. 34, 35) from the contain 0.014 percent BeO. In view of the relatively Rochester mining district and the area immediately high beryllium content of this sample, further study of north of it. The aplite is a fine-grained massive rock the deposit seems advisable. that, according to Jenney, consists mainly of quartz, BBUCITE AND MAGNESITE DEPOSITS orthoclase, and albite, with traces of magnetite, sphene, The brucite deposits at Gabbs are on the west slope tourmaline, zircon, and biotite. of the Paradise Range, east of town. They are No exhaustive study of the aplite was attempted, but 72 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES two samples were taken from exposures in Limerick quartz monzonite underlies an area of 20 acres, and Canyon (see fig. 7), as follows: contact-metamorphosed rocks associated with it under­ 329-1126. Chip sample from various exposures on the aorth side lie large parts of an area 2,400 feet by 3,200 feet, extend­ of Limerick Canyon (0.0007 percent BeO). ing from the south side of Rye Patch Agrss Canyon 1127. Chip sample from various exposures on the south across Panther Canyon (see fig. 8). Because Vitali- side of Limerick Canyon (0.0011 percent BeO). ano's report includes detailed maps of both tH intrusive body and the associated contact aureole, tl ?, area ap­ peared to offer excellent ground for sampling. The quartz monzonite is a light-gray medium-grained massive rock reported by Vitaliano to consis4: mainly of quartz, feldspar, and mica, with accessory sphene, apatite, magnetite, and pyrite, and traces of epidote, calcite, hematite, chlorite, and zircon. It is finer grained than the granite in Rocky Canyon (fig. 11) and con­ tains more plagioclase. The quartz monzcnite shows little variation. At a few places it grades into aplite. Outcrops of the quartz monzonite along Rye Patch Agnes Canyon were carefully examined, for beryl and for indications of uncommon minerals. A chip sample of granite (329-1124) was taken from outcrops at 15- foot intervals along the bottom of Rye Patch Agnes Canyon, from the east contact nearly to th°, midpoint of the granite body. The sample contained 0.0016 per­ cent BeO. After Jenney, 1935, pi. 1 Two principal groups of rocks have been affected by 2000 4000 Feet contact metamorphism in the Panther Canyon area: Contour interval 200 feet calcareous argillite, now represented by hc^nfels lay­ Datum is mean sea level ers; and limestones, ranging from pure to argillaceous EXPLANATION and including thin layers of argillite. Contact The hornfels is mainly represented by thr?e layers of a brownish (limonitic) sugary textured rock from 6 to Fault 50 feet in width. The easternmost layer was sampled 329-112^ (329-1123) on the north side of Rye Patch Agnes Can­ yon just above the canyon bottom. At this point it is Locality sampled about 45 feet thick. The rock consists largely of quartz and number and orthoclase, with subordinate amounts cf diopside, epidote, and other minerals. The sample contained 0.0008 percent ^eO. Keratophyre The limestone layers are an extremely varied assem­ FIGURE 7. Geologic map of part of Limerick Canyon, West Humboldt blage, ranging from blue-black, fine-grained marble Range, Pershing County, Nev. that apparently has undergone recrystallization but lit­ tle silicification, through blue-black marble containing Dikes of granite porphyry cut aplite on the south side streaks and patches that range from white marble and of Limerick Canyon (fig. 7). Sample 329-1128 con­ silicated marble to tactite. Metamorphosed limestone sisted of chips from various exposures of five dikes. occurs mainly in two zones: an inner zone immediately The BeO content proved to be less than 0.0001 percent. contiguous to the quartz monzonite in Rye Patch Agnes This same rock forms large bodies in the area extending Canyon, and an outer zone east of this body and, ex­ north from the Rochester mining district toward tending roughly north from the south side of Rye Patch Unionville Canyon. Agnes Canyon across the south fork of Panther Canyon (see fig. 8). PANTHER CANYON ABEA In the inner zone, silicification of the limestone series The Panther Canyon area has been described by is only locally complete and the rocks consist largely of Vitaliano (1944). In Rye Patch Agnes Canyon blue-black marble with streaks, patches, lenses, and lay- LOCALITIES IN NEVADA 73

R.33E. EXPLANATION SEDIMENTARY ROCKS

Metadiorite

Contact Dashed where approximately located or inferred

U D Fault Dashed where approximately located or inferred; U, up- thrown side; D, downthrown side

5,5

Strike and dip of bedr

After Vitahano, 1944, fig. 2 2000 Feet i i Contour interval 100 feet Datum is mean sea level FIGDKE 8. Geologic map of a part of Panther Canyon area, Rye Patch, Nev.

ers of white marble and silicated marble. Samples structure of the outer zone is complicated by a steeply taken and analyzed for BeO are described in table 27. dipping fault that marks the eastern margin of the zone, at least between the North and South Forks of Pan­ TABLE 27. Beryllia in samples from inner contact zone, Panther Canyon area ther Canyon (fig. 10), and there may also be on<* or « , BeO Sample Description (percent) more faults along the bottom of the south fork of the 329-1111 Chip sample taken at intervals across a series of thin layers of silicated marble intercalated with marble. Zone is 40 ft across strike and 200 ft long...____ < 0. 0001 w. 1112 Chip samples across zone of interbedded gray, white, and blue-black marble Streaked gray and white silicated containing layers of silicated marble. marble 15 feet thic Total thickness of zone is 54 ft; 18 ft is silicated marble (329-1112) and 36 ft is marble (329-1113)______. 0078 1113 __.__do______.0013 1122 Grab sample of tremolite marble from limestone area north of quartz monzo- nite______.______. 0013 1125 Chip sample from various outcrops of blue-black marble containing patches of white marble and veins of silicates.- . 0016 The outer contact-metamorphic zone includes rocks that are thoroughly silicated. These rocks range from hornfels and silicated marble to tactite and can best White marble zone Contact Sample number 140 feet thick Dashed where approximately be seen in the ridges separating the North and South located or inferred forks of Panther Canyon. The section exposed on the FIGDEB 9. Sketch of part of north wall, South Fork Panther Canyon, north wall of the south fork is typical (fig. 9). The Pershing County, Nev. 74 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES canyon. Sampling was restricted largely to the north wall of South Fork Panther Canyon, west of the fault; sampling data are given in table 28.

TABLE 28. Beryllia in samples l from outer contact zone, Panther Canyon area BeO Sample Description (percent) 329-1115 Chip sample across belt of silicated marble, north side Rye Patch Agnes Canyon______0. 0007 1116 Chip sample across beds approximately 15 ft thick in lower part of section of silicated marble______0009 1117 Chip sample across tactite zone, taken along crest of ridge______0037 1118 Chip sample across beds of hornfels_____ 0026 1119 Chip sample across 15-ft thick zone of silicated marble______0029 1121 Chip sample across 140-ft thickness of beds, mostly marble______0036 i Samples 329-1116 to 329-1121 are from the section on north side of South Fork of Panther Canyon. See figure 9 for locations. 2000 4000 Feet Contour int«rval 200 feet Datum is mean sea level BOCKY CANYON-WEIGHTS CANYON AREA EXPLANATION SEDIMENTARY AND The area extending from Rocky Canyon to Wrights METAMORPHIC ROCKS Canyon includes the Oreana tungsten mine, described Contact Dashed wher* approximate// by Kerr (1938; 1946a, p. 189-192), where scheelite and located beryl occur in pegmatite. The general geology of the area is shown in figure 10, and detailed geology in the Fault Dashed where approximately vicinity of the Oreana mine is shown in figure 11. The located; dott<*i where concealed; U, upthrowr side; D, downthrown rocks sampled include limestone in various stages of side recrystallization and silicification, hornfels, granite and aplite. Locations of samples are shown on figures Strike and dip of beds 10 and 11, and sampling data are given in table 29. Shaft TABLE 29. Beryllia in samples from the Rocky Canyon-Wrights 329-1133 329-1135 Canyon area I Locality sem-?led and number Sample Description (percent) ROCKY CANYON AEEA 18°3(V 329-1130 Chip sample across pegmatite-aplite dike, north side of canyon______0. 0001 1131 Chip sample of aplite from composite dike on south side of canyon______. 0011 1132 Chip sample of granite; chips taken at 150-ft intervals for 4,000 ft up canyon from mouth______,______. 0011 1133 Composite sample of six pegmatite-aplite dikes, north side of canyon______. 0007 1135 Chip sample of granite; chips taken at FIGURE 10. Geologic map of part of Kocky Canyon ani vicinity, West intervals along ridge south of canyon._ . 001 Humboldt Range, Pershing County, Nev.

WBIGHTS CANYON (OBEANA) AREA 329-1137 Chip sample across aplite dike______0011 The granite was examined for beryl, but none was 1138 Chip sample across hornfels layer_ _ _ 0008 found. 1139 Chip sample across aplite dike or sill____ 0015 1140 Chip sample across lens of silicated marble Aplite-pegmatite dikes are found in great profusion. and tactite between aplite dikes._____ 0031 Proportions of aplite and pegmatite material in the 1141 Chip sample across silicated marble.____ 0015 1142 Chip sample across aplite dike, north side dikes vary markedly, even from place to place within Wrights Canyon______. 001 the same dike, but the aplite fraction predominates. In general the dikes strike N. 30° to 45° W. and dip The granite is exposed in the gorge forming the lower 35° to 50° NE.; some strike northeast and are vertical. part of Rocky Canyon. It is a medium- to course- They range from a few inches to many fe<>t in width, grained massive biotite granite. Apart from patches and some are exposed for hundreds of feet along strike of biotite-rich material present locally, particularly or dip. Apparently, they are of several generations near the mouth of the gorge, it appears homogeneous. and some of the older are sill-like bodies in rhyolite LOCALITIES IN NEVADA 75

>>; i "or,; i ' *Vo~' ' \ / ^ ^>'0

Adapted from map by Kerr, 1946a, pi. 7

500 1000 Feet

EXPLANATION

Marble Limestone and Hornfels Aplite Older aplite Metadiorite Granite marble and rhyolite

LOCALITY AND SAMPLE NUMBER 1. 329-1137 4. 329-1140 2. 329-1138 5. 329-1141 Contact Fault Localities sampled 3. 329-1139 6. 329-1142 Dashed where approximately Dashed where approximately located or inferred located FIGURE 11. Geologic map of vicinity of Oreana tungsten mine, Pershing County, Nev. 76 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES (Kerr, 1946a, p. 189-190, pi. 7). Beryl was not found to tactite and impregnated with scheelite. Scheelite- in the dikes examined. bearing tactite has been found in some of the beds for In the area east of the Oreana mine, contact-meta­ distances as great as 2,000 feet from the nearest in­ morphosed rocks consisting of blue-black limestone and trusive body, and the deepest workings have reached marble, silicated marble, tactite, and hornf els were sam­ 1,700 feet without sign of bottoming of the beds against pled. These rocks are in contact with metadiorite on granite. the west and granite on the east (see fig. 11). No one of the calcareous beds is uniformly mineral­ ized. In general, a bed traced along dip or strike will RESULTS OF SAMPLING be found to show four facies, as follows: In view of the occurrence of beryl in scheelite de­ 1. Tactite, consisting chiefly of garnet, epidote, diopside, and posits in the West Humboldt Range, analytical results quartz in various proportions. of the rock samples collected in this region are disap­ 2. Silicated marble, with pale-green silicates and pale garnet. pointing. Of the 27 samples of all rock types that were 3. White marble, commonly with some light-colored silicates analyzed spectrographically, only 1 (329-1112) con­ and grading in places into silicated marble. tained more than 0.005 percent BeO, and only 3 others 4. Blue-black fine-grained marble grading into limestone. Cer­ contained more than 0.003 percent. The average BeO tain beds contain partings or lenses of hornfels. content of the other 23 samples is less than 0.002 percent. The number of calcareous beds is large and the work­ Sample 329-1112, containing 0.0078 percent BeO, rep­ ings are extensive; no attempt at overall sampling resents material which might some day be of commer­ could be made. Two groups of beds, known locally as cial interest, though the tonnage probably is small. The the Sutton beds and the George beds, were selected sample is from a zone of silicated marble adjacent to for the major part of the sampling, because each was the intrusive quartz monzonite in Rye Patch Agnes easily accessible in several opencuts. A few samples Canyon. The zone is more than 50 feet wide and per­ were also taken from beds on Humboldt Hill and Stank sists for at least 200 feet along the strike. It is esti­ Hill. The various ore-bearing beds and surface work­ mated to contain about 3,500 tons for each 10 feet of ings are shown on figure 12. depth. The beryllium-bearing mineral is not known, None of the samples from this area contains sufficient and there is no assurance that the beryllium is recover­ beryllium to be of commercial interest at present. In able. view of the large number of samples taken and the va­ In evaluating results of the sampling, it should be riety of rock types represented, the prospect that sub­ emphasized that the metasedimentary rocks at each of stantial quantities of higher grade materiel is present the localities sampled in the Humboldt Range are of seems unlikely. extremely diverse composition. Hundreds of samples, each taken from a single bed, would be needed to de­ SUTTON BEDS OF LOCAL USAGE termine the exact distribution of beryllium. Consider­ The rocks known locally as the Sutton beds consist able contamination is inherent in the present sampling; of two calcareous layers separated by about 40 feet thus further investigation might reveal material of of hornfels. Samples were taken from these beds in the much higher beryllium content than that indicated by Baker workings, the workings immediately north of the analyses given above. However, the present work the Springer stock, and the south opencut of the Sutton gives no indication of large individual deposits of rela­ mine. The samples are described in table 30. tively high-grade beryllium-bearing material. TABLE 30. Beryllia in samples from the Sutton beds of local usage BeO TUNGSTEN AREA, MILL CITY DISTRICT Sample Description (percent) EAST SUTTON OPENCUT; EXPOSURES IN LOWER PART OF HEADWALL The tungsten deposits at Tungsten, near Mill City, (NORTH WALL) Nev., are among the most important of the tactite type 329-1143 Chip sample, layer by layer, across erst in the United States. The deposits, which are worked ore bed, thickness 9 to 9.5 ft. Inter- banded tactite, white marble, silicated by the Nevada-Massachusetts Co., are on the southeast marble, quartz, and hornfels. Tact;*,e slopes of the Eugene Range, in Pershing County. They includes both garnet-rich and epidote- rich material..______.____ <0. 0001 have been described by Kerr (1946a, p. 182-188). 1144 Chip sample of west ore bed, 8.5 ft thick. At Tungsten three steep-sided stocks of granodiorite Garnet-epidote-quartz-calcite tact;t.e with minor hornfels layers ______.0017 cut a series of calcareous strata interbedded with horn- 1145 Chip sample of blue-black and gray horn­ fels. In general the beds strike nearly north and dip fels from 40-ft thickness of beds sepa­ rating the two ore beds______. 0016 steeply east or west. The beds are offset by both pre- 1146 Chip sample from same beds as 329-1145 and post-mineralization faults. The deposits are in but consisting of hornfels altered alo^g layering and cross fractures to a gre^n parts of the calcareous beds that have been converted fine-grained rock______. 0012 LOCALITIES IN NEVADA 77

TABLE 30. Beryllia in samples from the Button beds of local GEOBGE BEDS OF LOCAL USAGE usage Continued BeO Sample Description (percent) The rocks known locally as the George beds are a EAST BUTTON OPENCUT; EXPOSURES IN LOWER PART OF varied assemblage of layers of marble, calc-silicate HEADWALL (NORTH WALL) continued rocks, and tactite composed of diopside, garnet, and 329-1147 Chip sample across 6 ft of hornfels im­ epidote in various proportions. In part the diopside- mediately overlying the west ore bed__ 0. 0018 1148 Chip sample of 4 ft of hornfels immedi­ garnet rocks appear to have been formed by alteration ately underlying the east ore bed. ____

EXPLANATION

Tailings

Contrct Dashed where approximate/)' located or inferred

Fault Dashed where approximately located or inferred

Strike and

^-» BUTTON Sutton beds of VM M/N£- local usage. _f?'SOUTH SUTTON\ SUTTON OPENCUT\ GULCH

Contour interval 250 feet Datum is mean saa laval FIGDBB 12. Geologic map of part of Tungsten area near Mill City, Pershing County, Nev. cated marble, white marble, and blue-black marble. The TABLE 32. Beryllia in samples from Humboldt Hill and Stank Hill Continued beds on the west side of Stank Hill were sampled in the BeO hope of getting representative material from the outer Sample Description (percent) fringes of the mineralized area. Samples from these BEDS WEST OF STANK HILL localities are described in table 32. 329-1176 Chip sample of 6-ft thickness of argillite immediately east of (overlying) the ore beds__.______0. 0023 TABLE 32. Beryllia in samples from Humboldt Hill and Stank 1177 Chip sample across 32 in. of silicated Hill marble and 30 in. of interbanded diop- Sample Description (percent) side and garnet tactite. These beds form the top (east) part of the main HUMBOLDT BEDS OF LOCAL U8AGEJ OPENCUT ON HTTMBOLDT HILL zone of calcareous strata.______.0016 329-1168 Chip sample across the full width of the 1178 Chip sample across 6-ft thickness of blu> beds______.____ o. 0033 black and white marble and silicated 1169 Chip sample of 5-ft thickness of hornfels marble forming the middle part of tl * immediately beneath (east of) the ore main zone of calcareous strata______. 0005 beds..______._____ . 0014 1180 Chip sample across 4^-ft thickness of 1170 Chip sample from various layers of garnet hornfels overlying (east of) the main tactite ______. 0036 zone of calcareous strata and separat­ 1171 Chip sample of white marble having ing them from 2.5 ft of blue-black ard abundant pale garnet.______. 0022 white marble..._-__---__.______.___ . 0014 LOCALITIES IN NEVADA 79 A composite (329-1181) of granodiorite from vari­ 370 feet northeast of, and 117 feet lower than, the ous outcrops in the southwestern part of the Springer portal of the upper adit to intersect the winze (fig. 13). stock had a BeO content less than 0.0001 percent. This adit was flooded at the time of the present in­

ROSE CREEK MINE vestigation. A sublevel consisting of a few short drifts was excavated after Roberts' survey. It joins the The Rose Creek tungsten mine is in the northeastern winze about 35 feet vertically below the upper adi4:. part of the East Range, 11 miles south-southwest of The deposit is a bed of scheelite-bearing tactite en­ Winnemucca. A detailed study of the deposit was closed in interbedded quartzite and hornfels. The bed made by R. J. Roberts (1943). Rocks of the area in­ is 2 to 4 feet thick, averaging about Zy^ feet. The a ver- clude dolomite, limestone, argillite, and quartzite which age thickness of the parts of the bed remaining in the have been cut by a small granite body (see fig. 13). underground workings is probably H/^ to 2 feet. The Argillite next to the granite has been altered to horn- bed strikes northeasterly and dips northwesterly at a fels, and tactite has formed in the limestone. moderate angle. It is offset by a number of postmin- The main, or upper, workings consist of an adit that eralization faults, mostly of small displacement, and extends westerly for about 400 feet and connects with is cut by preore lamprophyre dikes and postore diabase a series of drifts, raises, and stopes (see fig. 14). An dikes. Mining has been confined to the richer and thick­ inclined winze extends down the ore bed to the north­ er parts of the bed. west. A lower adit was driven westerly from a point The tactite is fine grained and is composed chiefly of

EXPLANATION

Fault Dashed where approximately /ocrfect or inferred; doffed where conceded

oc Thrust fault o> T, upper p/afe 2< -2° Strike and dip of beds oc 90 -t- !P Strike of vertical beds -*?° Strike and dip of joints H Mine shaft Q C= Pit or trench 329-1105 Locality sampled and number

18°3(H

Tactite bed

Contact Approximately located or inferred

After R. J. Roberts, A. E. Granger, and M. W. Cox (Roberts, 1943, pi. 2)

250 1000 Feet I Contour interval. 100 feet Datum is mean sea level FIGURE 13. Geologic map of the Rose Creek mine and vicinity, Persblng Cotwty, Nev. 80 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES

103 , , ,,. »",-^lr"'^^ -lllll(,;^^ UPPER ADIT ^%2. ' . ''$; El. 4994 ft || g. ''''''?""'',',""" llm| IIU' WW^^^ i "%; ';;»Niimmn»u^\ .^ ^ l "Hlllll.llmimlV\\\V' .^Cv

Strike of vertical beds

Inclined working Chevrons point downward K Mine shaft

Shaft going above and below levels 0 Head of winze H Foot of raise or winze

Approximate outline of stope Contact, showing dip Stopes are filled in part Dashed where approximately located or inferred Dump Fault or shear zone, showing dip , 329-1099 Dashed where approximately located or inferred Locality sampled and nunber

Opencut

Strike and dip of beds 100 Feet After Roberts (194 3, pi 3) Later workings (dashed lines) Datum is mean sea level by E N Camenn, August 1949 FIGURE 14. Geologic map of the Rose Creek mine workings, Pershing County, Nev. diopside, actinolite, feldspar, quartz, calcite, epidote, Sampling was done mainly in the underground work­ and zoisite in varying proportions. Minor amounts of ings, because surface exposures are poor. One sample other minerals, including sulfides, are present in quartz each of silicated marble and granite was obtained from veins or disseminated through the tactite. Pyrite and surface outcrops. Sampling data are given in table 33; chalcopyrite are the common sulfides. The absence of locations of samples are shown on figures 13 and 14. garnet and prominence of pyroxene and amphibole dis­ Analytical results of the sampling show that parts tinguish this deposit from the ordinary tungsten-bear­ of the tactite bed contain beryllium in abnormal ing tactite of the region. amounts, but that its distribution in the tacflte is quite LOCALITIES IN NEVADA 81 irregular. For the six tactite samples analyzed the Smith of the U. S. Geological Survey. It is near the range in BeO content is from 0.0032 percent to 0.024 southeast edge of an area of granodiorite containing percent, the average being about 0.007 percent. The inclusions or pendants of limestone. The limestone average BeO content of the rocks may, of course, differ patches are contact-metamorphosed, along their mar­ markedly from this in view of the small number of gins where in places tactite containing scheelite is samples taken. The beryllium-bearing mineral is not formed. Most of the tactite bodies are small but one known. about 1,000 feet northwest of the mine has a strike length of more than 1,000 feet (fig. 15). TABLE 33. Beryllia in samples from the Rose Creek mine Since Smith's map was made, a series of shallow BeO Sample Description (percent) cuts and trenches has been excavated along the length 329-1095 Chip sample across full width of tactite of the tactite body. These excavations indicate that (21-32 in.), northeast wall of winze, 80-85 ft above bottom____..____. 0.0033 the body is more complex than was supposed. In 1097 Chip sample across full width of tactite trench A (fig. 15) it consists of two principal southeast­ (16-29 in.), intersection of sublevel and winze______. 024 ward-dipping layers of garnet and garnet-diopside 1098 Chip sample of 3-ft thickness of quartzite tactite separated by a limestone parting. The lower overlying tactite at locality of 329- 1097--_------_-_.______. 0015 layer of tactite is probably about 15 feet thick, anc1 the 1099 Chip sample across full width of tactite limestone parting probably has roughly the same thick­ (15 in.) at east end of sublevel_____ . 0074 1100 Chip sample across full width of tactite ness. The upper layer may be as much as 35 feet tl ick, (13 in.), junction of upper adit and raise but this figure includes a few feet of limestone. The No. 1__._____.______.______.0042 1101 Chip sample across full width of tactite lower layer is exposed in trench B, but its thickness of (13 in.), underhand stope, upper adit southeastward-dipping beds abutting against gr-mo- level, 25 ft southwest of raise No. 2___ . 0047 1102 Chip sample across full width of tactite diorite includes about 4 to 5 feet of tactite in two (2.5 ft), east end of stope extending layers separated by 5 to 6 feet of limestone. The bot­ down from upper adit level, 45 ft inside portal_-_-_---______. 0032 tom of the lower layer is not exposed, but it prob?,bly 1103 Chip sample of 5-ft thickness of gray is not more than a few feet thick. Trench C exposes a hornfels, footwall of tactite, portal of upper adit.----_----_____-_--__-___ . 0013 single zone of tactite, 18 to 25 feet wide, containing 1104 Chip sample of black hornfels overlying blocks of silicated marble. In cut E a width of 62 tactite, opencut at portal of upper adit_---_-----_ .______<. 0001 feet of tactite is exposed, but the mass appears to be 1105 Chip sample of silicated marble from ridge dipping gently to the southeast and may bottom on southeast of tungsten mine______. 0012 1106 Chip sample from granite outcrops south­ granodiorite at shallow depth. At the head of the cut east of tungsten mine______. 0015 it contains a mass of blue limestone and silicated marble. North of this cut the width of tactite decreases Roberts (1943, p. 13) estimated the amount of ore in and it finally pinches out, though small pods of tactite the mine to be about 6,000 tons but a large part of are present here and there along the granodio^ite- the ore between the sublevel and the surface appears marble contact for some distance. Samples taken from to have been subsequently removed. It is doubtful that the tactite body are described in table 34. more than a few thousand tons of tactite remains in the mine. That much larger reserves might be dis­ TABLE 34. Beryllia in samples from the Ragged Top area closed by further development seems unlikely. BeO Sample Description (percent) 329-1182 Chip sample along 110 ft from upper tac­ RAGGED TOP AREA tite layer (which includes limestone parting) to east edge of trench A_____ <0. 0001 The Ragged Top tungsten mine is on the west side 1183 Chip sample covering 8 ft along western of the Trinity Range, in sec. 11, T. 25 N., R. 28 E., end of trench A, from upper part of lower tactite layer.______. 0016 Lovelock quadrangle. It is accessible from U. S. high­ 1184 Chip sample, full width of lower tactite way 40 by about 8 miles of gravel road leading west layer, trench B-_____-______-______. 0014 1185 Chip sample of silicated marble forming from Toulon. The mine consists of a series of small parting 4.5 ft thick between tactite shafts, opencuts, adits, and test pits excavated to ex­ layers trench D______,______. 0005 1186 Chip sample across full width of tactite plore scheelite-bearing tactite deposits along the con­ layer, cut E______. 0016 1187 Grab sample of granodiorite from chunks tacts of limestone and granodiorite. of rock on dump of Ragged Top mine- . 0013 The mine is described briefly by Kerr (1946a, p. 192) 1188 Chip sample of tactite from low knoll east of mine road 2,300 ft N. 10° E. of north and was mapped during World War II by Ward C. end of tactite body shown on figure 15_ . 0019 82 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES

EXPLANATION

* ".» t TRENCH_C\^._^^P TRENCH D -^ x--""""'I5-- ^-*^--",&4«<-: . / cK-3i Granodiorite /« . -A>1 ^t*^ Contact Dashed where approximately located or inferred

Strike and dip of beds

Trench or opencut

, __,__ Geology by E. N. Cameron and 300 Feet J H Macleod. August 1949

FIGURE 15. Geologic map of tactite body near Bagged Top mine, Pershing County, Nev.

CHAMPION DTJMOHTIERITE MINE age dip of about 40° W. The rocks of tie two zones The dumortierite mine of Champion Sillimanite, have been described as schists, but they are mostly Inc., is near the head of Humboldt Queen Canyon, on gneisses with subordinate mica. the west side of the Humboldt Eange, about 5 miles According to Kerr and Jenney (1935), tre andalusite east of Oreana, Nev. A gravel road branching north­ was formed by replacement of tuffaceous schist and the eastward from the Oreana-Limerick Canyon road gives dumortierite by replacement of andalusite. Dumortie­ access to the mine. Geology at the mine has been de­ rite in the western zone is largely in veinlets, some of scribed by Kerr and Jenny (1935). which contain quartz. A small amount of prospecting Dumortierite occurs in two zones of andalusite- in this zone has failed to discover sizable bodies of quartz-albite-sericite rock. These rocks are most dumortierite. abundant on the north side of Humboldt Queen Can- The mine workings are in the eastern zcne, which'is yoii. The zones are about 225 feet apart, stratigraphi- roughly 60 feet thick. They extend from the canyon cally; they strike N. 10° to 20° E. and have an aver­ bottom up the north side of the canyon for about 1,000 LOCALITIES EST NEVADA 83 feet, through a vertical distance of about 600 feet. The The deposits on the Happy claims are in a shattered lower part of the workings, extending from the canyon zone in westward-dipping blue-black limestone; the floor upward through a vertical distance of about 270 zone trends roughly north and is traceable for at l°>ast feet, appear to have furnished all the production. The 400 feet along the axis of the ridge in which the mine workings, which consist of opencuts and, at various workings lie. The limestones are irregularly mineral­ levels adits leading to inclined stopes, extend as much ized with quartz, calcite, and minor amounts of as 600 feet into the canyon wall. Most of the stopes are scheelite. The ore bodies apparently consist of more inaccessible. heavily mineralized parts of the zone that contain Owing to the poor condition of the workings and the scheelite in minable amounts and are large enough to lack of satisfactory cross-sectional exposures, system­ warrant exploration. atic sampling was not attempted. The samples col­ There are two ore bodies, both near the south end of lected and analyzed are described in table 35. the crest of the ridge. The west ore body, reportedly worked during World War I, was mined by an irregu­ TABLE 35. Beryllia in samples from the Champion mine lar opencut 30 feet long. The ore consisted of ex­ BeO Sample Description (percent) tremely coarse calcite with quartz and scheelite. Little 329-1108 Chips from various blocks of lavender du- ore remains, and the deposit was not sampled. mortierite-bearing rock on the dumps, main workings______0. 0011 The ore body being mined in 1949 is northeast of the 1109 Chips from various blocks of andalusite- bearing rocks on the dumps, main work- west ore body and appears to be connected with it by ings__l______. 0006 small irregular stringers of calcite and quartz. Mining 1110 Chips from various blocks of pink dumor- tierite-bearing rock on the dumps, is chiefly from an opencut 60 feet long. At its north main workings.______. 0013 end the cut leads to an inclined stope trending noHh- 1129 Chip sample across full width of the east zone, from exposures above the upper­ west. The ore body dips steeply eastward and appears most stope and its connected opencut- <. 0001 to have been highly irregular in outline. In the in­ WHITE PINE COUNTY clined stope it is a more regular veinlike body striking CHERRY CREEK DISTRICT N. 5° W. and dipping 42° E. It consists of quartz, calcite, and accessory scheelite. The average grad^ of The tungsten deposits of the Cherry Creek district ore in the stope is reported to be about 1.5 percent WO3. are in the Egan Range, west and northwest of the town Sampling data for the Happy claims are showr in of Cherry Creek. They are in a northeastward-trend­ table 36. ing belt extending more than 2*/2 miles southwestward from a point northeast of the Ticup mine. The main TABLE 36. Beryllia in samples from the Happy claims part of the belt, which is in the vicinity of the Ticup BeO mine, has been mapped and described briefly by M. R. Sample Description (jvrcenf) 329-1024 Chip sample of ore from walls of inclined Klepper (1943, fig. 3). stope ______0. 0009 The belt is underlain by northwestward-dipping in- 1025 Fines scooped up from floor of stope_ _ _ _

oissv.anr

« >» e s si

Q. » c M LOCALITIES IN CALIFORNIA 89 below the level, which is at altitude 4,997. The lower in figure 19. The rocks are prevailingly thin-bedded adit connects with these workings at a point southwest and show marked changes in mineral composition of the incline. The beds are much faulted and are dif­ across strike. ficult to trace in some parts of the mine. The middle The beds overlying the upper tactite layer, in order adit level (glory hole level) and the level developed of stratigraphic sequence from top to bottom, are rib­ from the inclined shaft, which are the most important bon tactite, consisting of alternating thin layerr of of the western workings, are shown on figure 17. garnet-rich and diopside-rich rock, gray to white mar­ The eastern workings consist of three adits and ap­ ble veined by silicates, calc-silicate rock interlayored pended underground workings that expose a third tac- with tactite, and idocrase-bearing marble. The pnn- tite bed. This bed dips westward and is stratigraph- cipal beds of the upper tactite layer are garnet-rich ically below the tactite beds in the western workings. tactite and garnet-diopside ribbon tactite. A spotted The two upper adits are short; the lower and main adit tactite bed of undetermined mineral composition is is about 175 feet long and leads to drifts, a winze, and present in the glory hole. The rock underlying the several raises (see fig. 18). upper tactite layer and separating it from the lower The rocks explored by the workings are a varied as­ tactite is thin-bedded calcareous shale, largely altered semblage of blue limestone, white to gray marble and to calc-hornfels. The lower tactite layer is similar in silicated marble, calc-silicate rock, calc-hornfels, and composition to the upper tactite. These rocks corsti- tactite. The general geology of the mine area is shown tute a more varied assemblage than those of most tactite

EXPLANATION

Shale and hornfels

Contact, showing dip Dashed where approximately located; dotted where concealed

Fault, showing dip Dashed where approximately located or inferred

70 Strike and dip of beds

0 2-foot gouge and breccia zone along fault Head of winze .0

6-inch gouge zone along fault Hard greenish garnet rock After Lemmon, 1941, pi. 77

50 100 Feet I I Datum is approximate sea level FIGURE 18. Geologic map of the lower eastern adit, Bound Valley mine, Tungsten Hills, Inyo County, Calif. 467945 59 7 90 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES

150 Feet Contour interval 10 feet Datum is mean sea level

EXPLANATION

Contact Dashed where approximately Dump located or inferred 329-1278

Fault, showing dip Locality sampled and number Dashed where approximately located or inferred

Building Vertical fault

Strike and dip of beds

Tactile and light-colored calc-hornfels Rim of glory hole or opencut

B Mine shaft Tactile with scheelite After unpublished map by P. C. Bateman and M P. Erickson

FIGUEB 19. Geologic map of the Bound Valley mine, Inyo County, Calif. LOCALITIES IN CALIFORNIA 91 deposits and were, therefore, sampled in detail, The in tactite than in other rocks. In general however, the samples are described in table 41. beryllium content of tactite deposits in the Tungsten Hills is low and compares to that of tactite deports TABLE 41. Beryttia in samples from the Round Valley mine in the Mill City district, Nevada. The productior of BeO Description (percent) tungsten in both districts has been large and, inasmuch as tungsten and beryllium tend to be associated in WESTEBN WOBKINGS Beds overlying main tactile: tactite deposits, the scarcity of beryllium is puzzling. 329-1271 Chip sample across lower 14 ft of inter- At the Round Valley mine the presence of idocrase and layered calc-silicate rock and tactite, glory-hole level__-______<0. 0001 the occurrence of ribbon tactite that is structurally, 1275 Chip sample along three lines at 5-ft in­ though not mineralogically, similar to that at Iron tervals across idocrase-bearing marble immediately above tactite, inclined- Mountain, N. Mex., might be taken as indicators of shaft level..______. 0024 helvite, but none was found. Only two samples from 1278 Chip sample across outcrop of ribbon tac­ tite, 300 ft southwest of glory hole__ <. 0001 the Tungsten Hills 329-1255 from the Little Sister 1279 Chip sample across marble outcrop, 50 ft mine and 329-1269 from the Round Valley mine con­ south of glory hole______<. 0001 Beds of mam tactite zone: tained more than 0.0025 percent BeO. These samples 329-1269 Chip sample at intervals across spotted contained 0.0036 and 0.0045 percent BeO, respectively, tactite layer, southwest wall of glory hole___--_-______.______. 0045 and reserves of these grades probably are small. Be­ 1270 Chip sample across garnet-diopside tac­ cause of the large number of samples taken at the two tite, southwest wall of glory hole___ <. 0001 1272 Chip sample across garnet diopside ribbon mines, there seems small hope that larger deposits of tactite, north side of glory hole_-_-___ <. 0001 better grade would be revealed by further sampling. 1276 Chip sample across garnet tactite, inclined shaft level.______-_--__-_____ .0019 Though sampling at the Aeroplane mine was less exten­ Beds underlying main tactite: sive, the fact that beryllium was not detected in any of 329-1267 Chip sample of 7% ft of calc-hornfels, east side of glory hole at adit level. ______. 0006 the samples collected is discouraging. 1268 Chip sample of 7}_ ft of calc-hornfels im­ mediately below beds of sample 329- PINE GREEK DISTRICT 1267___-______. 0003 1280 Chip sample of 10-ft thickness of calc- PINE CEEEK TUNGSTEN MINE hornfels from shallow cut at northeast edge of glory hole______. 0017 Lower tactite zone: The Pine Creek tungsten mine is in the northern part 329-1273 Chip sample across 7-ft thickness of of the Mount Goddard quadrangle, 1 mile southeast of banded garnet-diopside tactite, glory- hole level __ .-__-_-_-__--___ <. 0001 Mount Morgan, in the Sierra Nevada. The mine is 1274 Chip sample of 15-ffc thickness of calc- reached from Bishop, Calif., by way of U. S. Highway silicate rock containing coarse patches of light-pink garnet, glory-hole level_ . 0018 395 to Round Valley and thence by paved and grr.vel 1281 Grab sample of garnet-tactite from dump roads. The history of the mine and discussions of the of small glory hole east of main glory hole______-______. 0017 tungsten-molybdenum-copper ore bodies have t°^n given by Lemnion (1941b, p. 89-91) and by Baterian LOWEB EASTERN ADIT (1945). The deposits have been worked intermittently 329-1282 Chip sample across 55 in. of fine-grained garnet tactite containing a few thin since 1916. Operations since 1938 have been conducted layers of calc-silicate rock______<. 0001 by U. S. Vanadium Corporation. A visit to the mine 1283 Chip sample of thinly laminated light calc-silicate rock, 25 in. thick______<. 0001 was made with Bateman on August 26,1949. 1284 Chip sample across 37 in. of thinly lami­ The ore bodies are in a contact zone between marble nated limestone, poorly silicated-_ _ _ _ _ <. 0001 1285 Chip sample across 41 in. of thin, alter­ and intrusive quartz diorite. The contact zone consists nating tactite and calc-silicate rock. __ <. 0001 1286 Chip sample across entire thickness of shale mainly of garnet-diopside tactite but includes quartz- and hornfels.______<. 0001 epidote tactite, quartz, and quartz-feldspar ro^ks. 1287 Chip sample across 5-ft thickness of bio- tite schist (feldspathized hornfels).-_____ <. 0002 Thicker parts of the contact zone constitute the ore 1288 Chip sample of granite, 1 to 5 ft from fault bodies. The ore minerals are scheelite and molybderite, contact with limestone.-- ______. 0001 1289 Chip sample of granite showing full tex- with minor amounts of chalcopyrite and borrite. tural range from aplite to fine-grained Gangue minerals are quartz, garnet, diopside, epidote, pegmatite.. ______. 0007 1290 Chip sample of vaguely defined dike of and feldspar. Five ore bodies crop out in the area of aplite, 2 ft wide.______. 0011 the Pine Creek mine. All contain tungsten in com­ mercial amounts but only the North and South ore EESTOTS OP SAMPUNG bodies contain molybdenum in important quantities. As in adjacent districts, the results of the sampling The geology in the vicinity of these two ore bodieq is show that beryllium occurs somewhat more abundantly shown in figure 20. 92 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES the tailing dumps remain. Two samples were taken. Sample 329-1265, consisting of handfulls of material taken at intervals along the edge of the main and older pile of tailings, contained 0.0058 percent BeO. A simi­ lar sample (329-1266) from the newer pib of tailings contained 0.0021 percent BeO.

YANEY TUNGSTEN PROSPECT, BISHOP DISTRICT The Yaney prospect is at the base of the Sierra Ne­ vada, about 5 miles southwest of Bishop, C^lif. Work­ ings consist of an opencut leading to irregular stopes in the upper part of the deposit, and an adit, at a level about 50 feet lower, leading to drifts. A brief inspec­ tion of the deposit was made with Paul C. Bateman, on August 29, 1949. Bateman furnished the information on which the following description is based. 329-1260 Locality sampled and numbe The workings are in an altered tactite deposit along the contact of metasedimentary rocks and granite. Ap­ parently the deposit originally was an assemblage of tactite and silicated limestone beds similar to those exposed in the deposits of the Tungsten Hills to the west. Subsequently, parts of the deposit were altered to a mixture of friable opaline silica, ocher, and jaro- site, in various proportions. Alteration has been in­ FIGDEB 20. Geologic map of part of Pine Creek mine area, Inyo tense in places, and large masses of the alteration prod­ County, Calif. ucts are present. Some of the altered material contains crystals of f erberite ^2 to % inch in diameter which are The South ore body is in a prong of altered marble apparently pseudomorphs after scheelite. The average that extends into the quartz diorite. In the opencut the grade of the ore is about 1 percent WO3. Unaltered ore body is 300 feet long and 150 feet wide; its width tactite is exposed in the lower workings, but it is barren diminishes with depth. The ore dips steeply east and of scheelite. In places the tactite is altered to a clayey rakes 60° S. Near the center of the body are two horses material. Samples taken at the prospect are described of calc-silicate rock and silicated marble. The North in table 43. ore body is largely covered. Sampling data for the Pine Creek mine are given in TABLE 43. Beryllia in samples from the Yaney prospect BeO table 42; locations of samples are shown on figure 20. Sample Description (percent) 329-1295 White opaline material, entrance cut, TABLE 42. Beryllia in samples from the Pine Creek mine upper working______---_---__----- <0. 0001 BeO 1296 Jarositie material with f erberite, entrance Sample Description (percent) cut, upper working ______<. 0001 329-1258 Chip sample across silicated marble, 35 ft 1297 Ocherous material, entrance cut, up">er thick______0. 0016 working______-- < 0001 1259 Chip sample across tactite beds, 12 ft 1298 Ferberite-rich material, entrance cut, thick______. 0018 upper working______-______---_- <. 0001 1260 Chip sample across 10 ft of silicated mar­ 1299 Clayey material, lower workings __ <. 0001 ble adjoining the tactite-______

TAILINGS FBOM MILL OF TITNGSTAB MINE ATOLIA DISTRICT The Tungstar mine is on the west shoulder of Mount The Atolia mining district in southeastern California Tom, at an altitude of 12,000 feet, in the northern part straddles the boundary between San Ber^ardino and of the Mount Goddard quadrangle. The mine was Kern Counties. Paved roads connect the district with worked for tungsten in the early 1940's, and the tactite Bandsburg and Johannesburg, 4 miles to the north, and ore was milled in Pine Creek Canyon below the mine. with Kramer, 23 miles to the south. Tungsten was dis­ The mine is closed and the mill has been destroyed, but covered in the area in 1904, and placer and lode mining LOCALITIES IN ARIZONA 93 have been carried on intermittently. In late August FLATIEON-SPANISH VEIN SYSTEM 1949 a few of the mines were being operated on a small The Matiron-Spanish vein system is an easterly- scale by men working under leasing arrangements with trending Y-shaped system of steep northeast-dipping the Surcease Mining Co. The district has been de­ linked veins. The stem of the Y is to the west. The scribed by Hulin (1925) and Lemmon and Dorr (1940). Flatiron vein system forms the stem and south brr.nch Tungsten is found both in lode deposits and placer of the Y; the Spanish vein forms the north branch. deposits. The lode deposits are veins that strike N. 75° The deposits are in general similar to those of the E. to N. 75° W. and dip 45° N. to 85° S. Faulting Union mine. during and after deposition of the minerals has compli­ Two samples were taken in the vicinity of the inter­ cated the structure of the deposits. The veins consist of section of the two vein systems. Sample 329-1314 is a scheelite in a gangue of quartz and carbonates, with grab sample of ore from a stringer two to four inches pyrite, stibnite, and cinnabar. The scheelite ore bodies thick in a small stope. Sample 329-1315 is a grab occur as steeply raking shoots as much as 1,260 feet in sample of pieces of high-grade ore from the ore piles. strike length and 1,080 feet in known pitch length. In The samples did not contain as much as 0.0001 per­ places the ore is as much as 17 feet thick. The wallrock cent BeO. is quartz monzonite. The placer deposits are concen­ ARIZONA trations in Quaternary alluvium that blankets the area By WILLIAM T. HOLSER of the tungsten vein. Field investigations for beryllium in nonpegmatite UNION MINE rocks in Arizona were undertaken in August 1949 by The Union mine, largest producer of the district, has W. T. Holser, assisted by W. I. Finch. The districts been worked to a depth of more than 1,000 feet. It con­ from which samples were taken are shown on figure 21. sists of a series of inclined shafts leading to 14 levels; Traces of beryllium had been found previously in the main shaft was the only one open at the time of samples from the pyrometasomatic deposits at the inspection. The workings are drifts, raises, winzes, Christmas, Clifton-Morenci, and Old Hat districts; no and inclined stopes in two veins, the North vein and additional work was done in these areas. the South vein. The veins strike east-northeast and The most promising resources of nonpegmatite dip 40°-63° N. In the western part of the mine the beryllium in Arizona are in beryl-bearing tungpten veins are as much as 180 feet apart; eastward and veins at Boulder Creek, Yavapai County; the Tungsten downward the veins converge, intersecting at a low King mine, Little Dragoon Mountains, Cochise angle in the eastern part of the mine. Each vein con­ County; and the Boriana mine, Mohave County. Pre­ tains one principal shoot. In the most productive parts vious sampling in the San Francisco district, Mol ave of the veins, the strike lengths of the shoots range from County, in connection with the Mine, Mill, and SmcUer 600 feet to about 1,000 feet. Samples taken at the mine Survey, indicated the presence of beryllium in epi- are described in table 44. thermal gold-silver veins. The only pyrometasomatic deposits in which beryllium was found are in the Dra­ TABLE 44. Beryllia in samples from the Union mine goon Mountains, Cochise County. BeO Sample Description (percent) 329-1307 Chip sample across full width of north COCHISE COUNTY vein; 9th level, 200 ft west of main shaft, small stope upward from level.__ <0. 0001 DRAGOON MOUNTAINS 1308 Chip sample across 18 in. of wallrock on either side of vein. Same locality as The Dragoon Mountains rise steeply from the desert sample 1307.______<. 0001 1309 Chip sample across full width of branch 12 miles northeast of Tombstone, to an altitude of more vein extending from south vein into than 7,500 feet (fig. 22). They have a northwesterly hanging wall; 9th level, crosscut about 80 ft east of main shaft.______<. 0001 trend from the old mining camps of Courtland and 1310 Chip sample across full width of south Gleason for about 22 miles to Dragoon, a station on the vein zone (8 ft wide) consisting of shattered quartz monzonite cemented Southern Pacific Railroad. A graded dirt road f^om by quartz, carbonates, and scheelite; Tombstone provides access to the southwestern sid-> of sublevel between 9th and 10th levels, 200 ft east of shaft.______<. 0001 the range, from where the mines are reached by steep 1311 Chip sample across full width of mineral­ mountain roads. ized zone, south vein; stope 100 ft east of main shaft, 40 ft below 9th level._ <. 0001 The geology of the Dragoon Mountains has been de­ 1312 Chip sample across horse of quartz mon­ scribed by Darton (1925, p. 292-296) and by Gilluly zonite separating two parts of south vein. Same locality as sample 1311.-- <. 0001 (1941). Precambrian Pinal schist is overlain by Bolsa 94 OCCURRENCE OP NONPEGMATTTE BERYLLIUM IN THE UNITED STATES

114

EXPLANATION 4 Locality sampled for this report

36'

Cochise County Mohave County Santa Cruz County 5. Boriana 1. Courtland-Gleeson 6. San Francisco 10. Patagonia 2. Gordon and Abril mines Pima County 3. Little Dragoon Mountains 7. Empire Yavapai County 4. Tombstone 8. Helvetia 9. Pima 11. Boulder Creek FIGURE 21. Index map of localities sampled in Arizona. LOCALITIES IN ARIZONA 95

329-549; 0.004 Sample number; percent beryllia

N RULE MINE

/ 329-547:0.007 329-543: 6.04 MIDDLEMARCH MINE

Courtland HUMBOT MINES HIGHLAND MINE

Contour interval 500feet Datum is mean sea level

Base from U. S. Geological Survey Dragoon, Cochise, Benson, and Pearce quadrangles FIGURE 22. 'Index map of beryllium occurrences in Dragoon Mountains, Cochiae County, Ariz. 96 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES

quartzite and Abrigo limestone of Cambrian age. Con­ COUBTI-AND-GLEESCHSr DISTBICT formable on the Abrigo limestone are 350 feet of mixed The Courtland-Gleeson district (Turquoire district) shales and limestones of the Martin limestone of De­ is in the southeastern part of the Dragoon "fountains, vonian age which are succeeded by at least 700 feet of 15 miles east of Tombstone. The geology of the dis­ massive Escabrosa limestone of Mississippian age. A trict was described by Eansome (1913) and by Wilson thick section of limestone of the Naco group of Penn- (1927). Limestones of Paleozoic age and shales and sylvanian and Permian age overlies the Escabrosa lime­ sandstones of Cretaceous age have been intruded by a stone. The rocks of Paleozoic age have been de­ variety of igneous rocks of which quartz monzonite formed and invaded by intrusive rocks of Cenozoic age, porphyry is the most widespread. Contact metamor­ chiefly the Stronghold granite. After erosion the re­ phism of the sedimentary rocks near the intrusive por­ gion was covered by sandstones of the Upper Creta­ phyry has been slight. Locally minor quantities of ceous and Tertiary volcanic rocks. The geology has been garnet, epidote, quartz, and pyrite have forced in the complicated further by thrust faulting. Abrigo limestone of Cambrian age. At least three Metamorphism of the sedimentary rocks of Paleozoic periods of normal faulting and one of thnrt faulting age has been particularly intense near their contact with have been recognized. the Stronghold granite. The Escabrosa limestone and Deposits containing disseminated chalcopyrite and part of the Naco group are changed to white marble minor quantities of galena occur in the metamorphosed with some tremolite. The more argillaceous parts of Abrigo limestone. Oxidized copper minerals are com­ the Martin and Abrigo formations and the Naco group mon in the upper parts of the deposits. According to contain large quantities of andradite, hedenbergite, Kansome (1913, p. 533), the copper mineralization was and epidote. Garnet also occurs in the sedimentary simultaneous with the silication. The Humbot mine rocks along a fracture zone several thousand feet from (Wilson, 1927, p. 55-56) is typical of these deposits. A the granite, and some metamorphism is found as much 22-foot channel sample (329-551) was cut through as 5 miles from the granite outcrop. garnet-epidote tactite from an outcrop 30 feet west of There has been little mining activity other than in the Humbot shaft. A composite grab sample (329- the Courtland-Gleason district at the south end of the 552) of chalcopyrite-pyrite-specularite ore with garnet- range. A small production has been credited to the epidote gangue was taken from the dumps of the Dragoon and Johnson (Cochise) districts. The Golden Humbot and Highland mines. These samples did not Eule mine, producing principally lead, at the north contain as much as 0.0001 percent BeO. end of the range and the Middlemarch mine, producing

principally copper, on the eastern side, were the only GOBDON MINE producers before World War II. The Gordon mine, on the southwest crest of the range, reportedly pro­ The Gordon mine is near the southwestern crest of duced lead-zinc ore during World War II. The Abril the range at an altitude of 7,000 feet, abont 14 miles mine, on the western slope, has been the source of con­ by graded dirt road from Tombstone. The mine work­ siderable zinc since 1945. All of these mines are in sedi­ ings include three adits. mentary rocks close to the border of the Stronghold The principal ore mineral is galena. It occurs along granite. The dominant ore minerals at the Golden a west-trending fracture zone in the Abrigo limestone, Eule, Gordon, and Abril mines are chalcopyrite, galena, a few hundred yards east of a mass of Stronghold and sphalerite; the gangue minerals are garnet, epidote granite. On the surface the fracture zone is 50 to 100 and specularite. feet wide and can be traced for half a mih along the Samples from the Dragoon Mountains contain as strike. In and adjoining the zone of fracturing are much as 0.04 percent BeO (fig. 22). Although the interlayered thin-beddedcherty limestones end epidote- beryllium-bearing mineral has not been identified, the garnet-specularite tactite. A 7-foot chaimel sample analogy to other beryllium deposits suggests that hel- (329-547) taken across the tactite at the portal of the vite may be the source of the beryllium. The similarity between the ratios of beryllium and base metals in ore northern upper adit contained 0.007 percent BeO. and gangue indicate that the beryllium is associated According to Mr. J. H. Macia, the mill at Tombstone mainly with the ore. The amount of beryllium in the was built during World War II to treat tih°< ore from tactite at the Gordon and Abril mines is at least 10 this mine. A grab sample (329-543) of o:"e from the times that found in 85 percent of the tactite deposits receiving bin at this mill contained 0.04 percent BeO sampled in the Western United States. and O.OX percent each of bismuth and cachnium. LOCALITIES IN ARIZONA 97

ABRIL MINE of the Eepublic mine, generously furnished mill samples and analytical data. Mr. Edwin Over of Colo­ The Abril mine is at an altitude of 7,000 feet on the rado Springs, Colo., supplied details concerning the steep western slope of the Dragoon Mountains. The occurrence of beryl at the Bluebird mine. mine is accessible by a dirt road that leads from the southwestern side of the range. The mine was de­ TABLE 45. Beryllia and tungsten in sample from the Little Dragoon Mountains veloped by Bargain Mines, Inc., in 1945. From 1945 Percent to 1948 it was operated by the Shattuck-Denn Mining Sample » Locality and description BeO» W» Corp., and about 20,000 tons of lead-zinc-copper ore was TUNGSTEN KING MINE processed in their flotation mill at Bisbee, Ariz. The 329-435 Channel sample across 2.5-ft quartz vein______0. 0008 0. 0860 ore was carried on an inclined tramway to the bottom 436 __ _ do ______. __ . 052 . 1340 of Stronghold Canyon, whence it was trucked out. 437 Channel sample across 3 ft of chlorite schist between quartz The mine workings consist of several adits driven vein and quartz monzonite _ . 010 . 0700 in a large block of Escabrosa(?) limestone, that is 441 Channel sample across 2 ft of chlorite schist with some nearly surrounded by Stronghold granite. The lime­ quartz______. 016 . 1340 stone and interbedded shales have been metamorphosed 442 Channel sample across 3 ft of altered quartz monzonite rock to hornfels, marble, and tactite. Sphalerite and chal- near sample 441______. 0013 . 0028 copyrite fill small fractures and partly replace the epi- 444 Chip sample of fresh quartz mon­ dote-specularite tactite. Some ore is found in garnet- zonite rock ______. 0014 . 0016 epidote tactite. Samples of tactite (329-549) and of BLUEBIRD MINE ore (329-550) from the dumps at the mine contained 329-446 Chip sample of 4-in. tungsten- bearing quartz-fluorite vein in 0.004 and 0.02 percent BeO, respectively. Specimens quartz monzonite______. 0005 . 0014 of ore from this mine contained O.OX percent tungsten. 447 Channel sample across 3.5 ft of quartz veins (1/3) and grei- senized quartz monzonite LITTLE DRAGOON MOUNTAINS (2/3). ______. 0019 . 0034 JRC-1 Specimen of fresh quartz mon­ The Little Dragoon Mountains are in northwestern zonite- ______. 0016 (*) 2 Specimen of greisen next to Cochise County. The principal settlement is at the quartz vein______. 0028 (*) old mining camp of Johnson, on the eastern side of 3 Specimen of quartz monzonite with argillic alteration, 15 ft the mountains. Copper and zinc ore are produced from from vein at sample 2______<. 001 (*) the Eepublic and other mines. 4 Specimen of quartz vein contain­ ing huebnerite ______< 001 (*) The Final schist of Precambrian age underlies much of the western part of the Little Dragoon Mountains. JOHNSON CAMP AREA 329-449 Two-week composite of mill The schist is overlain by the Apache group of Precam­ heads at Republic mine, June brian age, which includes conglomerate, shale, and 1949. From 1200, 1500, and 1600 levels west. Garnet-di- sandstone. .Sedimentary rocks of Paleozoic age, pre­ opside tactite, with some chal- dominantly limestone, are nearly conformable with the copy rite and sphalerite ______5 .0007 «.OX 450 Same as sample 449, but taken Apache group and are at least 2,500 feet thick. They in May 1948, from higher constitute the Abrigo (Cambrian), Martin (Devonian), 5 .0007 «.OX 451 Same as sample 450, but tailings. 5 .0007 «.OX and Escabrosa (Mississippian) formations, and the 453 Channel sample across 18-in vein Naco group (Pennsylvanian). Blocks of sandstones of quartz, with fluorite and sulfides, cutting across Abrigo from the Bisbee group of Cretaceous age are faulted limestone, Mammoth mine _ 5.0007 «.OX against the sedimentary rocks of Paleozoic age. Fol­ 454A Idocrase separated from marble of the Naco group, Black lowing regional folding and faulting a body of quartz Prince mine______. 005 (*) monzonite was intruded, cutting rocks as young as the 455 Grab sample of idocrase-wollas- tonite tactite, with copper sul­ Bisbee group. Dikes of aplite and lamprophyre cut fides, from dump of Black the quartz monzonite and the country rocks. Prince mine______. 001 (*) JRC-5 Specimen of garnet tactite, with Sampling data for the little Dragoon Mountains are chalcopyrite, sphalerite, and chlorite, from main ore zone given in table 45 and the localities sampled are shown in Mammoth mine ______<. 001 (<) on figures 23 and 24. J. E. Cooper of the U. S. Geo­ 6 ___ do______<. 001 (*) 7 Specimen of epidote-tactite con­ logical Survey, who had previously sampled some of taining sulfide ore minerals, the localities, conducted the party over the area and diopside, chlorite, garnet, and potash feldspar, from main ore assisted in the sampling. Mr. Oscar Jarrell of the zone, Republic mine______<. 001 («) Coronado Copper and Zinc Co., owner and operator See footnotes at end of table. 467945 59 8 98 OCCURRENCE OP NONPEGMATITE BERYLLIUM IN THE UNITED STATES TABLE 45. Beryllia and tungsten in samples from the Little where the quartz occurs as a discontinuous bns and as Dragoon Mountains Continued irregular veins that cut the schist. Percent Sample > Locality and description BeO * W» As shown in figure 24, the vein is offset in three places JOHNSON CAMP ABBA Continued by steep cross faults. Near the top of the peaks east Specimen of diopside-tremolite of the Tungsten King mine one of these faults cuts the tactite, with quartz and cal- small outlier of sedimentary rocks of Paleozoic age cite, from Abrigo limestone above ore zone, Mammoth that overlie the schist. The displacements of the sedi­ mine______<0. 001 (*) mentary rocks and of the vein indicate that the south Specimen of wollastonite-garnet- idocrase tactite from Abrigo side of the fault was moved downward about 2,000 feet. limestone below main ore zone, Beryl occurs in the vein as prisms 2 or 3 centimeters Standard prospect.______<. 001 (4) 10 Specimen of idocrase-garnet- long and 2 millimeters in diameter, terminated by the wollastonite tactite, with ore minerals in limestone of the pinacoid. It is readily distinguished from the sur­ Naco group, dump of Black rounding milky quartz by a characteristic pale-blue Prince mine______.0023 (4) (5B7/4) color (Goddard and others, 1948). Most of 1 Samples bearing 329-numbers collected by W. T. Holser and W. I. Finch; those bearing JRC-numbers, collected by J. R. Cooper. it is reticulated through the quartz, in radiating or par­ 2 Quantitative spectrographic determination by Saratoga Laboratories, unless otherwise noted. allel groups. The beryl appears to be more common » Determination by Frederick Ward, U. S. Geological Survey, unless otherwise noted. near the schist wall or near schist inclusions. Some Not determined. Spectrographic analyses by J. D. Fletcher. BeO figures determined on plates was found in feldspar-rich selvage along tfo hanging- exposed for general scanning but not for precise determination of BeO alone. Semiquantitatlve spectrographic analysis by J. D. Fletcher. These samples also wall side of the vein. In the schist the beryl apparently contained O.OOX percent Mo. but no extraordinary amounts of 24 other elements (See table 15.) is most abundant in small blebs and stringer? of quartz or aplitic material that are common near tH hanging TUNGSTEN KING MINE wall. The beryl is very irregularly distributed and the quantity that may be readily seen is small. The Tungsten King group of 12 unpatented claims is Scheelite occurs in small shapeless patches sparsely at an altitude of 5,200 feet near the head of Clark Can­ and irregularly distributed through the qur.rtz and to yon on the western slope of the Little Dragoon Moun­ an even lesser extent through the schist near the vein. tains. The mouth of this canyon may be reached by It fluoresces white, indicating the presence of some about 16 miles of unimproved road leading up Tres Ala­ molybdenum. In a pit north of the adit (n^ar sample mos Wash from Benson, Ariz. According to Wilson 329-341 in fig. 24) wulfenite was found on fracture sur­ (1941, p. 43), scheelite was discovered here in 1916, and faces and in small vugs. According to Wilson (1941, during World War I the mine was developed by open- p. 43), chalcopyrite and galena are also fonnd in the cuts and short adits. Mining was renewed during World vein. We saw small cubes of limonite, pseudomorphous War II but the production was small. after pyrite, in the vein outcrop. The Tungsten King claims are along the northerly Along the f ootwall of the vein the quartz monzonite trending fault contact between quartz monzonite on the is intensely altered and silicified. It has a JpUty struc­ west and Final schist on the east (fig. 24). A quartz ture with some slicken-sides, as if it had been strongly vein mined for scheelite follows the fault contact for sheared. The feldspar is altered to a clay mineral. most of its exposed length. The principal opening is a Where the rock is apparently unaltered, as at the portal 2T5-foot adit which crosscuts the vein about 100 feet of the adit, it is similar to the quartz monzonfo of Texas below the outcrop. The adit was partly flooded at the Canyon in the southeastern part of the mountains. time of our visit, and we did not enter it. Drifts fol­ Channel samples were taken from several exposures low the vein for about 200 feet south and north of the of the vein (fig. 24). Results of spectrograpl ic analyses adit. Many pits have been dug along the vein, partic­ (table 45) indicate that locally the vein contains more ularly north of the adit. Near the adit, the vein is as than 0.05 percent BeO. In general, however, the grade much as 6 feet thick and dips about 60° E., but north­ of beryl ore as determined by visual inspection in the ward the dip becomes less. vein is lower than indicated by analyses. Apparently, The vein is composed mainly of fine- to coarse-grained some beryl occurs in ihe chlorite schist adjacent to the quartz and contains also minor quantities of scheelite, vein. The continuity of the vein indicates a large re­ beryl, feldspar (some altered to clay minerals), chlorite, serve of low-grade material, but the small size of the and muscovite. The wallrocks at many places along beryl crystals prohibit recovery except by milling. The the vein have been silicified. The structure of the vein beryl might be a valuable byproduct of a sch^lite mill­ is complex, particularly along the hanging-wall side, ing operation. LOCALITIES IN ARIZONA 99

MAMMOTH JRC-5, 6, 8; 329-453; 0.0007

NGSTEN KING JRC-2 to 4; < 0.001 0.0019 -T* to 0.0028 STANDARD 329-446; 6.0005 / JRC-9;<0.001

Mine mentioned in text JRC-9;<0.001 329-447; 0.0019 Sample number; percent beryllia

Contour interval 500 feet Base from U. S. Geological Survey Datum is mean sea level Dragoon quadrangle, 1943 FIGURE 23. Map showing localities sampled in the Little Dragoon Mountains, Cochise County, Ariz.

BLUEBIRD MINE best-defined one of this group. The space between v^alls The principal workings at the Bluebird mine are in a is about 5 feet, but the ore is only 6 inches thick* Most group of 21 patented claims that are in the hills at the veins in the area are only a few inches thick, and are head of Texas Canyon. Several unimproved roads pro­ bordered by a foot or more of greisen on either side, vide limited access to the area (fig. 23). Tungsten was A small quantity of beryl was collected from on-\ of mined in this area as early as 1899 (Eichards, 1904), the narrow veins by Mr. Edwin Over of Colorado and Wilson (1941, p. 42) reports that about 2 tons of Springs, Colo. The colorless beryl crystals were fcund huebernite per day were produced in 1940. with quartz and fluorite in a small opening at the local­ The tungsten-bearing quartz veins of the Bluebird ity marked "Beryl" in figure 23 (Boericke property). group are part of a vein system that trends northeast­ We saw no beryl during our sampling of this property. ward from the head of Texas Canyon nearly to John­ Analyses of samples from the Bluebird mine (see son. The wall rock is quartz monzonite, which has been table 45 and fig. 23) indicate that the quartz veins are intruded by aplitic and lamprophyric dikes. The main probably low in beryllium content. The greisen ap­ group of veins is in a zone about 600 feet wide. Eich­ pears to have only slightly more beryllium than the ards (1904, p. 264) describes the Bluebird vein as the quartz monozonite. 100 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES

R.21E R.22E.

Pmal schist

Quartz vein, showing dip Strike and dip of foliation

'-'<>* *?****'*?//?) h)

* = n - ". ^ "/,/> ' M :*.* V.^'. .-;MiV/OT'I I i

329-436; 0.052 Strike and dip of beds Sample number; percent beryllia * L i ' U <, ~ f / , /

Geology after G A Fair, 1931

FIGURE 24. Geology of the Tungsten King claims, Cochise County, Ariz. LOCALITIES IN ARIZONA 101

JOHNSON CAMP AEEA age. After extensive folding and faulting, these rocks The Johnson Camp area is on the east side of the were intruded in the western part of the district 17 the Little Dragoon Mountains, about 2 miles northeast of Uncle Sam porphyry (quartz latite) and in the south­ the Bluebird mine (fig. 23). It is an old camp with ex­ west by the Schiefflin granodiorite. Deposits of silver, tensive workings from which has come a large produc­ lead, gold, copper, and manganese are associated with tion of copper and zinc ore. The Republic mine was northeast-trending fissures and related structures. The active in 1949. The geology of the area has been de­ principal ore minerals are galena, gold, chalcopyrite, scribed by Cooper (1950). and argentiferous tetrahedrite, or their oxidation prod­ The principal ore bodies in the Republic and Mam­ ucts. The wallrock at many of the mines is a sedimen­ moth mines are associated with fractures in a bed of tary rock of the Bisbee group, but at some in the south­ contact-metamorphosed Abrigo limestone. The ore ern part of the district it is the more calcareous rocks consists of varying proportions of chalcopyrite, sphale­ of the Naco group. The limestone which is partially rite, bornite, and pyrite, with a little molybdenite and metamorphosed to garnet, epidote, and idocrase, crops scheelite, in a gangue of potash feldspar, garnet, epi- out on Comstock Hill northwest of the town. Silicifi- dote, diopside, quartz, and calcite. Analyses of speci­ cation of the limestone was irregular and apparently mens of typical ore and gangue that were collected by is related to dikes of the Schiefflin granodiorite. J. R. Cooper and of composite samples of mill heads Three samples were taken in the Tombstone district. and tails, that were furnished by the Coronado Copper Sample 329-539 was of manganese ore from the dump and Zinc Co. indicate that beryllium is not abundant at of the Oregon mine, 1-5 miles south-southwent of these mines (table 45). Tombstone. Sample 329-540 was chipped from a 60- The Black Prince and Peabody mines were developed foot-wide outcrop of garnet-calcite marble just west of on an outlying hill in the northern part of the area. the Luck Sure mine, 1.2 miles south-southwest of Tomb­ The ore is partly in thin shaly layers of the Naco group stone. Beryllium could not be found in either sample. and partly in lamprophyre. In addition to the usual A chip sample (329-546) taken along a 50-foofr line garnet and quartz gangue, the ore is found also in ido- across an outcrop of garnet tactite and tremolite-c^leite crase-wollastonite rock formed by metasomatism of marble near the top of Comstock Hill contained C .0007 limestone of the Naco group. Samples 329-455 and percent BeO. JCR-10 of the idocrase-wollastonite rock from the MOHAVE COUNTY dump of the Black Prince adit contained 0.001 and BORIANA DISTRICT 0.0023 percent BeO, respectively. Along the outcrop above the adit, green idocrase occurs in crystals as long Beryl-bearing quartz-tungsten veins occur at the as 3 centimeters in white, wollastonite-rich tactite. Boriana mine in the Hualpai Mountains about 18 miles The idocrase crystals separated from this material con­ east of Yucca, a town on the Atchison, Topek^, and tained 0.005 percent BeO. The small amount of beryl­ Santa Fe Railroad. The mine has been an important lium in the metamorphosed limestones of this part of producer of tungsten ore. The veins were not sarrpled, the district apparently is contained in idocrase. but descriptions by Hobbs (1944, p. 247-258) and Kerr Several quartz veins in the Johnson Camp area trend (1946a, p. 102-104) indicate that they may be potential northwest. Sample 329-453 from a quartz vein in the sources of beryl. Abrigo limestone above the Mammoth shaft contained According to Darton (1925, p. 180), the Hualpai 0.0007 percent BeO. Mountains "consist of Precambrian granite and gneiss cut by dikes of porphyry and other intrusive rocks." TOMBSTONE DISTRICT The country rock of the veins is a roof pendant of The Tombstone district, in western Cochise County phyllite in a large mass of biotite granite. The phyllite on U. S. Highway 80, was visited on August 1 and 2, crops out over a belt half a mile wide that trends north­ 1949. Mr. J. H. Macia of Tombstone kindly served as easterly. Its foliation is roughly parallel to the ver­ a guide to the mines and provided much information tical instrusive contact. The phyllite near the contact on their operations. is recrystallized to a fine-grained schist composed of The geology of the district was described by Butler, chlorite and muscovite. Wilson, and Rasor (1938). Sedimentary rocks of The veins are parallel to the foliation of the schist, Paleozoic age nearly a mile in thickness, principally but are discontinuous, frayed, and have an echelon limestone of the Naco group of Pennsylvanian age, are pattern. The principal gangue mineral is quartz yhich overlain unconformably by more than 3,000 feet of is accompanied by small quantities of fluorite, crlciter sedimentary rocks of the Bisbee group of Cretaceous muscovite, and potash feldspar. Wolframite, scheelite, 102 OCCURRENCE OP NONPEGMATTTE BERYLLIUM IN THE UNITED STATES chalcopyrite, and minor amounts of pyrite, arseno- highly altered by both ascending and descending solu­ pyrite, and molybdenite are the metallic minerals. Ac­ tions, they have not in general been replaced by metals. cording to Hobbs (1944, p. 254), "Some beryl was Lausen (1931, p. 63-72), considers the veins to be epi- found in the veins on the TOO-level and also in the veins thermal and recognizes five stages in the deposition of which cut the granite at the surface." Veinlets of the vein material. Most of the gold, with some silver fluorite and muscovite cut the quartz in some places, in solid solution, was deposited with calcite, quartz, and Kerr (1946a, p. 103) states that muscovite is most adularia, and fluorite during the fifth stage. abundant near tungsten minerals. Scheelite replaces Routine sampling in connection with the Mine, Mill, wolframite, and most of the sulfides were deposited and Smelter Survey in 1943 revealed significant quanti­ with the scheelites. Some sulfides, with quartz and ties of beryllium in tailings of the Gold Read mill at potash feldspar, are younger. Near the north end of Oatman and the Katherine mill at Katherine. Data the Boriana property, a sodic granite cuts across the for these and other samples taken from the district are phyllite. The veins decrease in width and increase in listed in table 46. Locations of the mines listed in the beryl content as they pass from the phyllite into the table are shown in figure 25. The sample containing granite. The sodic granite is thought to be related to the source of the mineralizing solutions. Reserves of tungsten ore were estimated at 2,400 measured tons, 9,900 indicated tons, and 44,000 inferred tons (Hobbs, 1944, p. 258). There were about 150,000 tons of unmined vein material between the under­ ground workings and the surface. The beryllium con­ tent of this material is not known. The mine closed down in February 1943, and no additional production has been reported to date (1951).

SAN FRANCISCO DISTRICT The San Francisco district is in the Black Mountains in southwestern Mohave County, near Oatman, a town on U. S. Highway 66. The southern part of the district is referred to as the Oatman district; the northern part as the Katherine or Union Pass district. Sampling by members of the Mine, Mill, and Smelter Survey during World War II indicated the presence of beryllium in the gold ores from this district. Although the district was not revisited during the present investigation, the results of the earlier sampling are of sufficient interest and importance to be included in this report. The geology of the district has been described by Ransome (1923), Lausen (1931), and Wilson, Cunning- ham, and Butler (1934, p. 80-115). Precambrian rocks are extensive in the northern part of the district, where TOPOCK 28 MILES a coarse gneissic granite intrudes schists and gneisses. FIGURE 25. Mines of the San Francisco district, Mohave County, Ariz. The granite forms the wall rock of the veins at the Katherine mine. The most abundant rocks of the Black 0.03 percent BeO, taken at the Katherine mill, is from Mountains are a thick series of Tertiary lava flows. a large deposit of tailings (about 150,000 tor-f), and no They range in composition from rhyolite to olivine samples of the various ores treated in the nuT are avail­ basalt; andesite and latite are the most important wall able. The source of the beryllium in the sample was not rocks of the veins near Oatman. Quartz monzonite and determined. granite porphyries intrude the flows. The lavas dip Tailings samples from the Chloride and other dis­ gently eastward, presumably as a result of movement of tricts in the Cerbat Range did not contain PS much as several hundred feet along steep normal faults. The 0.001 percent beryllium. The deposits in the^e districts principal mineral deposits are fissure fillings in parts of are gold-silver veins of more complex nineralogy the fault zones. Although the volcanic wallrocks are (Schrader, 1917, p. 199-206; Thomas, 1949). LOCALITIES IN ARIZONA 103

TABLE 46- -Beryllia in mill tailings from the San Francisco district Cretaceous or post-Cretaceous age which has highly [Analyst, John 0. Rabbltt] altered the country rock near its contact. The western BeO Sample Mill and location Contributing mines (percent) part of the area is intruded by granite of proHble 85-MC-3 Katherine; Roadside, 0.03 Katherine. Arabian, Mesozoic age. The contact of the granite with overly­ Katherine, ing limestones in the western part of the area is rlong Frisco, Tyro. Gold Road; Gold Gold Road___._. .006 a thrust plane; the limestones contain bodies of tactite. Road. The tactite, composed of garnet, quartz, diopside, Tom Reed; Tom Reed, . 001 Oatman. Black Eagle, actinolite, and wollastonite, forms the gangue for much Ben Harnson. of the ore. Creasey and Quick believe the metallic 10 Louzon-Oatman _ _ Mossback. _ _ _ _ <. 001 7 United Eastern United Eastern, <. 001 minerals, including fcyrite, chalcopyrite, and minor Mines Corp.; Big Jim. amounts of scheelite, sphalerite, and molybdenite, to be Oatman. Vivian Mining Co.; Leland, Vivian <. 001 later than the silicate minerals. Oatman. Mitchell. Channel samples were taken of tactite, mainly in or

PIMA COUNTY near areas containing copper or molybdenum minerals. The general locations of the samples with respect to the EMPIRE DISTRICT geology is indicated in figure 26; descriptions and The Empire district is in the Empire Mountains in analytical results are given in table 47. eastern Pima County, south of U. S. Highway 80 and east of State Highway 83. A pyrometasomatic tung­ TABLE 47. Beryllia in samples from the Helvetia district sten deposit in the southern part of the district was [Spectrographic analyses by J. D. Fletcher. BeO content determined or plates sampled on July 31, 1949. The deposit is just east of exposed for general scanning but not for precise determination of BeO alone] B«O the Hilton ranch house, on the road to State High­ Sample Description (pe*wnt) way 83. 329-510 Grab sample of hornfels and tactite, with chalcopyrite, from glory holes of Mo­ The deposit was mapped and described by Marvin.6 hawk mine in Helvetia Wash, half a Southeasterly-dipping limestone of the Naco group mile east of Helvetia______<0 0004 512 Channel sample across 6 ft of garnet (Pennsylvanian) is intruded by quartz monzonite. tactite, with pyrite, chalcopyrite, and molybdenite, from 40-ft sublevel of Within 50 feet of the contact, masses of the limestone Leader mine______-_-____-____-_ . 0004 have been changed to tactite that contain garnet, diop- 514 Channel sample across 6 ft of diopside- garnet tactite, with chalcopyrite (in­ side, wollastonite, quartz, epidote, specularite, and cluding 1 ft of fault gouge with secondary some scheelite and copper minerals. copper minerals') from main level of the Leader mine 420 ft from portal______. 002 Four samples (329-524 to 329-527 inclusive) were 515 Channel sample across 20 ft of garnet chipped from tactite outcrops between the road and the tactite and marble overlying the granite, at portal of upper adit Heavyweight next canyon, which is about 900 feet northeasterly along mine, 1 mile east of Helvetia.______. 0004 the contact. Beryllium could not be detected spectro- 516 Chip sample from 25-ft outcrop of garnet tactite above King adit (Rosemont graphically in any of the samples. lease)_._____-_____-______.______<. 0004 517 Channel sample across 10 ft of garnet HELVETIA DISTRICT tactite, with quartz and copper car­ bonates, from portal of adit on Rose­ The Helvetia district is near the summit of the north­ mont lease, 150 ft north of sample 516- _ <. 0004 ern end of the Santa Rita Mountains about 30 miles 520 Grab sample of garnet-quartz-chalcppy- , rite-pyrite ore from bin at King adit_ <. 0004 southeast of Tucson. The western part of the district 521 Grab sample of garnet tactite from dump around the old camp of Helvetia is reached by 14 miles of Narragansett mine______<. 0004 523 Grab sample of garnet tactite, with chal­ of graded road leading east from U. S. Highway 89 at copyrite and pyrite, from dump of Sahuarita. The eastern part of the district is accessible Daylight adit_____ - ______. 0004 by several unimproved roads leading west from State Highway 83. PIMA DISTRICT The geology of the district (fig. 26) was described by The Pima district is on the eastern slope of the Schrader (1915, p. 91-140), Creasey and Quick (1943), Sierritas, about 25 miles southwest of Tucson. The and Johnson (1949). The principal sedimentary rocks district was visited on July 28 and 29, 1949. THnks are limestones of Carboniferous age and clastic rocks of are due to Mr. G. J. Duff, Arizona manager of the Cretaceous age, both of which have been severely de­ Eagle-Picher Mining and Smelting Co., for samples formed and cut by thrust faults. The eastern part of from the San Xavier mine. the district is intruded by quartz monzonite of Late The geology and ore deposits of the district were de­ scribed by Eansome (1922, p. 407-428) and by Wilson « Marvin, T. C., 1942, Geology of the Hilton Kanch area: Arizona Univ. M. Sc. thesis. (1950). Strata of Paleozoic age, mostly limestones, EXPLANATION

SEDIMENTARY ROCKS

Contact Dashed where approximately located

Fault, showing dip Dashed where approximately looted; dotted where concealed

Strike and dip of beds

90 Strrke of vertical beds,

70 Upper Manzano equivalent, Pmu ; tf- including quartzite, Pmq Strike and dip of overturned beds

B Shaft

329-523; 0.0004 Sample number; percent beryllia

Aplite or recrystallized quartzite(?)

Topography from Unn of Arizona, 1943 Geology by S. C Creasey and G, L. Quick, 1943 3000 Feet Contour interval 100 feet Datum assumed FIGURE 26. Geologic map of part of the Helvetia district, Pima County, Ariz. LOCALITIES IN ARIZONA 105 are intruded by coarse-grained rocks that range in com­ position from quartz monzonite to granodiorite. Their structure has been complicated by extensive folding, thrusting, and block faulting. The ore deposits are pyrometasomatic in origin. The ore nearest to the con­ tact of the intrusive rocks is in tactite that is predom­ inantly andradite, with some quartz, epiodote, wollas- tonite, and hedenbergite. The metallic minerals, in­ cluding pyrite, chalcopyrite, magnetite, and rarely scheelite and molybdenite, are erratically distributed along fissures. The San Xavier mine is in ore farther from the intrusive rocks, and the gangue contains less garnet and more hedenbergite; calcite-sphalerite-ga- lena-chalcopyrite ore replaces the gangue minerals along a fault zone. The localities sampled for beryllium are shown on figure 27, and the sampling data are given in table 48.

TABLE 48. Beryllia in samples from the Pima district [Spectrographic analyses by J. D. Fletcher. BeO figures determined on plates exposed for general scanning but not for precise determination of BeO alone] Sample Description (percent) 329-490 Channel sample across 8 ft of yellow gar­ net tactite, with copper carbonates, at abandoned mine shaft.______<0. 0004 491 5.5-ft channel sample across quartz-limo- FIGURE 27. Index map to locations of samples from the Pima district, nite vein and garnet tactite, from pros­ Pima County, Ariz. pect pit _ __ <. 0004 494 Channel sample across 15 ft of garnet tac­ tite, with copper carbonates, from SANTA CRUZ COUNTY workings east of abandoned shaft_____ <. 0004 496 Channel sample across 8 ft of garnet- PATAGONIA DISTRICT hedenbergite tactite (?) from pit south of Minnie shaft______. 001 The Patagonia district is in southeastern Santa Cruz 497 Grab sample of garnet tactite and copper ore from Copper Queen dump.______. 001 County, just north of the Mexican border. It is about 498 Channel sample across 15 ft of garnet tac­ 25 miles by graded road south of the town of Patagonia, tite, with quartz veins, from outcrop 70 ft south of Copper Queen shaft___ <. 0004 Ariz., which is on State Highway 86. The district was 499 Chip sample across 150-ft outcrop of gar­ visited on July 31,1949. net tactite- ______<. 0004 501 Channel sample across 2.5 ft of garnet The geology of the district has been described by tactite in pit 60 ft southwest of Morgan Schrader (1915, p. 292-348). The Washington-Du- mine______<. 0004 502 3-ft channel sample across quartz-scheel- quesne area, in which all the pyrometasomatic deposits ite vein, next to sample 501______<. 0004 are found, was mapped by Arthur Richards and A. L. 503 7-ft channel sample across quartz-scheel- ite vein in pit 250 ft southwest of Mor­ Brokaw of the Geological Survey during World War gan mine______<. Q004 II, and their unpublished report was used as a guide in 506 Chip sample across 45-ft outcrop of garnet tactite at shaft 600 ft north of Morgan the sampling. In this area a block of limestone of mine_.______. Q004 Paleozoic age is surrounded by intrusive bodies of 507 Chip sample across 50-ft outcrop of garnet tactite 300 ft west of Morgan mine__ <. 0004 quartz monzonite and granite porphyry. Masses of the 508 Tailings, from concentrator at Sahuarita, limestone have been metamorphosed to garnet-quartz Ariz. (garnet-calcite-galena sphalerite ore from San Xavier mine), April-July tactite, with minor amounts of hornblende, diop^ide, 1949______<. 0004 and wollastonite near the southern end of the b*ock. 509 Heads from concentrator at Sahuarita, Ariz. average for July 1949 (ore from The principal ore bodies consist of pyrite, chalcopyrite, San Xavier mine)______<. 0004 bornite, and sphalerite along fractures in the tactite. ^*7-'--*'-*'-$ffi~'-*\', ' 's?S ? : '"'-"/-x ^ 7-c °- ^V ^ x /v x ^^r^S J. N - - \ x, '- v-:-0"-o '^l :Aj^Xh-_3 ^^'JS:^

^ T) 0 S? ? . . o 5 OS m o>% ^NN\ \\\\ alticflows XPLANAT Si rphyriticbf 10 & >nglomera Contact \\\\ granite "*? J^f ng \\\S 0 % trg \\\> I CT N N N\\\.' g_ - v >. 3 II X ^ So. b*-?;iS- O °. S S * *

PRECAMBRIAN CRETACEOUS TERTIARY AND OR TERTIARY QUATERNARY LOCALITIES IN NEW MEXICO 107 Precambrian rocks are schists, quartzites, and amphib- According to Anderson (1950b, p. 618), the unaltered olites of the Yavapai schist that have been intruded quartz monzonite contains less than 0.0004 percent P°X). by granite, gabbro, and a little quartz diorite. A stock A biotite-albite-quartz-orthoclase facies of altered (fig. 28) of Precambrian porphyritic biotite granite at quartz monzonite associated with the Bagdad ore de­ Lawler Peak is about 3 miles in diameter. The rock posits contains 0.0004 percent BeO. Beryllium wa? not is characterized by orthoclase phenocrysts as much as detected in samples taken at the Bagdad mine and other 2 inches in length. Small stocks of quartz monzonite mines in Yavapai County for the Mine, Mill, and intruded along a northeast-trending belt during Late Smelter Survey during World War II. Cretaceous or early Tertiary time. Pyrite, chalcopy- rite, and molybdenite occur in the quartz monzonite as NEW MEXICO disseminations and small fracture fillings which consti- ByW.T. HOLSER ture the ore of the Bagdad and other mines. Tertiary conglomerates and basalt flows cover the earlier rocks The localities at which pyrometasomatic deposit? and in parts of the area. alkalic igneous rocks were sampled in New Mexico are The tungsten-beryllium deposit is on the south side shown in figure 29. Tactite deposits are known in many of Boulder Creek about 4 miles airline northeast of of the mining districts of New Mexico (Lindgren, Bagdad (fig. 24), in sec. 24, T. 15 N., E. 9 W. In the Graton, and Gordon, 1910, p. 51-53) and nearly all of vicinity of the prospect the porphyritic biotite granite these were sampled. Samples of tactite from the cen­ is highly altered, with destruction of the biotite and tral New Mexico iron districts were obtained through formation of muscovite and minor amounts of garnet the courtesy of V. C. Kelley of the University of New and fluorite. Some beryl occurs as poiMlitic inter- Mexico. The deposits in the Juarilla district, Otero growths with the other rock minerals and seems to be County, had been sampled previously by the American related to the alteration. The wolframite-bearing veins Smelting and Refining Co. According to L. K. Wilson are also in muscovite-rich granite. The wolframite oc­ of Tucson, district geologist for the company, the sam­ curs in closely spaced nearly vertical parallel quartz ples contained little or no beryllium. veins as wide as 1 or 2 inches. South of Boulder Creek The largest known reserves of nonpegmatite beryl­ the veins form a northeast zone nearly 12 feet wide and lium in New Mexico are in the tactite deposits at Iron 200 to 300 feet long. On the north side of the creek, an Mountain (Jahns, 1944a; 1944b). Vein and tactite de­ eastward-trending zone of veinlets 10 to 50 feet wide can posits in the Victorio Mountains are also of potential be traced for more than 2,000 feet. Beryl is an impor­ importance. Small quantities of beryllium might H re­ tant accessory in the veins and locally is abundant. covered from deposits in the Carpenter and Af ache Some scheelite occurs in thin films and crusts on the districts. Phonolitic lavas of large areal extent in the surface exposures. The veins are thought to be related Eaton volcanic region contain as much as 0.007 percent genetically to the granite stock. BeO, but the beryllium may not be recoverable. Alkalic igneous rocks were sampled in the Eator vol­ The vein zones were sampled by Anderson and his canic region, Coifax County, and in the Conmdas associates. A channel sample taken across the northern Mountains, Otero County. The rocks of the Cornudas zone contained 0.16 percent WO3 and 0.05 percent BeO, Mountains are related to those of western Texas ani are and a similar sample from the southern zone contained described in the section dealing with the Trans-Pecos 0.13 percent W03 and 0.2 percent BeO. Region. Beryl is reported as a minor constituent of pegmatite CATRON COTJNTT dikes that are common in the porphyritic biotite gran­ ite. It also occurs in the granite about 2,000 feet south­ BLACK RANGE DISTRICT west of the wolframite-beryl prospect. Specimens from Tin deposits of the Black Range are in Catron and this locality consist of a granular mass of quartz and Sierra Counties, on the western slope of the range east cloudy feldspar that contains about 30 percent beryl. of State Highway 61, about 50 miles north of Silver The beryl is in euhedral prisms about 3 millimeters in City, N. Mex. They were visited on August 22 acd 23, diameter and 2 centimeters long, reticulated in all di­ 1949. rections through the mass of quartz and feldspar. The The tin deposits, which have been described by Fries beryl-bearing rock occurs in at least two tabular bodies, (1940), and Fries and Butler (1943), occur in a rhyo- or "veins," 6 to 10 inches wide and 30 feet long, and litic volcanic series that contains some interlayered tuffs averages 4.5 percent BeO. and breccias. Small veins that contain specularite and The minerals associated with intrusions of Tertiary cassiterite and minor quantities of cristobalite, tridy- age at the Bagdad mine seem to have no beryllium. mite, fluorite, chalcedony, opal, and quartz occur in a 108 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES

108° 106° 104°

..Z 19 [I20 ^v. 4 I/ x (

J- - _ 1_.. _J 1

34

32* 32

106° 104°

40 120 Miles

DISTRICTS Catron County Hidalgo County Sandoval County 1. Black Range 10. Apache No. 2 21. Cochiti 11. Hachita Colfax County 12. Lordsburg Santa Fe County 2. Cimarroncito 13. San Simon 22. New Placers 3. Elizabethtown Lincoln County 23. Old Placers 4. Baton volcanic region 14. Capitan 15. Gallinas Sierra County Dona Ana County Luna County 24. Apache No. 1 5. Organ 16. Tres Hermanas 25. Cuchillo Negro 17. Victorio 26. Iron Mountain Grant County Otero County 6. Burro Mountains Socorro County 7. Carpenter 18. Juarilla 27. Jones Camp 8. Central (includes Hanover, Fierro San Miguel County and Santa Rita districts) 19. Rociada Taos County 9. Pinos Altos 20. Willow Creek 28. Bed River FIGUBB 29. Index map showing localities sampled in New Mexico. LOCALITIES IN NEW MEXICO 109 porphyritic rhyolite of the lower part of the series. It seems to best fit Gordon's description of the Thunder Alluvial deposits near the veins are rich in placer cas- mine (Ldndgren, Graton, and Gordon, 1910, p. 107- siterite. 108). The mine area on the north slope of the Middle A grab sample (329-711) from a pit above the U. S. Fork, from which samples 329-376 to 378 were taken, is Bureau of Mines adit 1 N in the Taylor Creek area probably the one known locally as the Lambert mine, (Fries, 1940, pi. 55), contained 0.002 percent BeO. The but does not correspond to any mine describc-d by beryllium-bearing mineral was not identified. Gordon. As the mines were not accessible, samples were obtained from dumps and outcrops as follows: COUFAX COUNTY 329-376 Chip sample from 15 ft of outcrop of garnet tactite CIMARRONCITO DISTRICT at portal of upper adit. The Cimarroncito district is in the Cimarron Eange 377 Grab sample of garnet-diopside tactite with pyrite, chalcopyrite, and specularite, from dump of lower in western Colfax County on land of the Philmont adit. Scout Eanch. Eight miles of private road lead from 378 Grab sample of specularite-hornblende tactite with the ranch headquarters on State Highway 21 to Cimar­ pyrite, chalcopyrite, calcite, and epidote; same local­ roncito Camp (fig. 30). From there trails go up both ity as sample 377. the Middle and North Forks of Cimarroncito Creek to 382 Grab sample of garnet tactite from dump of upper the mining area. The district was visited on July 19, adit. (No tactite in dump of lower adit.) 1949. Spectrographic analyses of the samples showed no more than 0.0004 percent BeO.

ELIZABETHTOWN DISTRICT The Elizabethtown district in western Colfax County ^--^j^ 329-376 is northeast of Eagle Nest, a small town on U. S. High­ ££_ ^^^-^'329-377,-378 way 64. The geology of the district was described } 329-382 ~~ by Graton (Lindgren, Graton, and Gordon, 1910, p. /ir

TABLE 50. Correlation of volcanic rocks and related units in the Raton region

[Equivalent or correlative rocks are connected by dashed lines] Collins (1949) and Stobbe (1949) Smith and Bay, 1943 Mertie (in Lee, 1922. p. l-12)(Raton- Griggs, Northrup,and Wood (Colfax and Union Counties) (Cimarron Range) BriUiant-Koehler-quadrangles) (in Griggs, 1948, pi. 1} Quaternary rock names are those (Colfax County) given by Collins (1949, p. 1022-1023) "Youngest lavas" (east of quadrangl.es)- j*>-Late basalt flows Capulin basalts (flows). Basait lava flows and stocks - 1. Intermediate mafic flows - - Clay ton basalts (flows, rrinor dikes) g (with mafic dikes,in part). Andesite flows and stocks ^ Intermediate felsic flows x -Chico phonolites (flows, minor dikes, and Bills). / Slagle trachytes (sills, minor £» a Basalt, rhyolite, and dacite (Urraca Basalt lava flow ' dikes). % » Mesa). Red Mountain dacites (flews, minor W CU / dikes). _ frjEarly basalt flows (with / / g Gravels (including Eagle Nest High-level gravels ' Raton basalts (flows, minor dikes) g formation) mafic dikes, in part) o £ Basalt (in part - La Gruilla Mtn.) Basalt lava flows """ u>OgaUala formation Ogallala formation High-level gravels (in part)

8 Quartz monzonite porphyry § Q^^tz monzonite porphyry sills suu ^ dikes Basic dikes 5 ^ J g and dikes (southwest of quad- 2 ,S rangles). LOCALITIES IN NEW MEXICO 111

105° 104° 103°

LAS ANIMAS

37° - 37 C

36° 36 «

105° 104° 103° Modified polyconic projection After Collins (1949), Griggs (1948), Smith and Ray (1943), Ray and Smith (1941), and Darton (1928) FIGURE 31. Map of post-Cretaceoua volcanic rocks of the Baton region, New Mexico. to the rocks are those suggested by Collins (1949, p. rocks other than basalt. These include the Red Moun­ 1022-1023). tain dacites, Chico phonolite, and Slagle trachyte^ all Three ages of basalt flows have been recognized. The of Collins (1949), which are mainly around volcanic oldest flows, the Raton basalts of Collins (1949), cap centers in southeastern Colfax County. Coitus' the high mesas near Raton. They are gray, fine­ Red Mountain dacites are apparently equivalent to the grained, vesicular rocks with olivine phenocrysts. The "intermediate felsic flows" of Griggs, Northrop, and basalts of intermediate age, the Clayton basalts of Col­ Wood, which they correlate with Collins' Claytor ba­ lins (1949), occur at lower altitude. They contain salts. According to Collins (1949, p. 1032), the boun­ olivine phenocrysts, and a few of the flows are felds- dary relations between his Red Mountain dacites and pathoidal. The youngest basalts, the Capulin basalts his Clayton basalts indicate that the latter is younger. of Collins (1949), generally are in the valleys. They He assumes from physiographic and petrologic data are black, dense to vesicular rocks with large feldspar that his Chico phonolites and his Slagle trachytes are phenocrysts and some olivine. closely related rocks that fall into the same age brr^ket The major differences of opinion concern the volcanic (post-Raton and pre-Clayton) as the Red Mourtain 112 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES dacites. Apparently, the phonolite and trachyte cor­ eastern Coifax County. Most of the samples were respond to rocks referred to by Griggs, Nbrthrop, and chipped at intervals across fresh outcrop^; in a few Wood as "sills and dikes" of early (?) Tertiary age. places carefully selected hand specimens were taken. Although there is general agreement that the trachytes The localities sampled are shown on figure 32, and ana­ are largely sills, Collins (1949, p. 1034) states that the lytical data are given in table 51. phonolites are mainly flows, with few sills and dikes. The Chico phonolites of Collins (1943) and related The phonolite is a green to gray, fine-grained rock dikes are the only rocks in which berylliun? was found. containing phenocrysts of aegirite and feldspar. The These rocks are confined to an area of about 25 square groundmass is composed of nepheline, analcite, ortho- miles in southeastern Coif ax County (fig. 32). Most clase, and aegirite, with accessory sodalite, magnetite, of the phonolite is associated with volcanic centers at and sphene. The trachyte is light brown, fine grained, Turkey Mountain and Temples Peak. Sills and dikes and contains sparse feldspar phenocrysts. The ground- in the Slagle Canyon area, a few miles sout^ of Turkey mass is mostly orthoclase, with some acmite-diopside Mountain, are similar to the phonolite ard probably and barkevikite. related to it. The distribution of BeO in the rocks appears to cor­ OCCURRENCE OF BEBYLLIUM relate roughly with the zirconium content, and an in­ All of the major volcanic rock types were sampled, verse relation to the chromium content if suggested. mainly in the vicinity of the volcanic centers in south­ There is also an apparent correlation between BeO con-

R. 25 E. R.26E. R.27'E.

EXPLANATION

SEDIMENTARY ROCKS

£

Undifferentiated units

IGNEOUS ROC'

Capulin basalts

Clayton basal1

-!0cs';fv

Chico phonolites and Slagle trachytes

Red Mountain da-.ites

Raton basalts Names are those used by Collins, 1949

Contact

329-373; < 0.001 Locality sampled; percent beryllia

4 Miles After Gr'gBs . 1948 ' and Collins. 1949

FIGURE 32. Map of volcanic rocks of southeastern Colfax County, N. Hex. LOCALITIES IN NEW MEXICO 113 TABLE 51. Beryllium and other elements in volcanic rocks of the Raton region Percent

Rock type Sample No. Sample type Description BeO» Or 2 Zr* eU* U*

Capulin basalts. . 329-372 Hand specimen from Highly vesicular black <0. 001 0. OOX 0. OOX <0. 001 _____ flow surface. basalt. Clay ton basalts.. 367 ....do...... ______Gray fine-grained <. 001 .OX .OOX <. 001 .._ basalt. Chico phonolites. 369 Chip sample across Gray-green, fine- . 007 . OOOX .X ,010 0.004 150-ft section, north­ grained, porphyritic. west side Pecks Mesa. 361 Chip sample across Gray, slightly porphy- . 002 . OOOX . OX . 007 .003 125-ft section, east ritic. side Slagle Canyon. Tinguaite dikes similar 360 8-ft channel sample Dark, green, porphy- . 002 . OOOX . OX . 005 .003 to Chico phonolites. across vertical dike, ritic, vertical flow east side Slagle structure. Canyon. 364 Chip sample of 30-ft Green, porphyritic____ .002 .OOX .OX .007 .002 section of sill, east side Slagle Canyon.5 Slagle trachytes (?) 6. _ - 365 Chip sample of 15-ft Gray, slightly porphy- . 002 . OOOX . OX . 006 .002 section of flow, same ritic. locality as 364. Red Mountain 373 Grab sample from east Gray to reddish brown. <. 001 .OOOX .OOX <. 001 _____ dacites (?). base of Timber Buttes.7 1 Rock names are those of Colllns (1949, p, 1022-1023). 2 Spectrographic analyses by J. D. Fletcher. BeO figures were obtained on plates exposed for general scanning, and not for precise determination of BeO alone. * Radiometric analyses by J. N. Rosholt. Equivalent uranium is based on measurement of radioactivity wherein it Is assumed that all of the radioactivity of a sample arises from uranium and its disintegration products, and that none of the radioactivity arises from the thorium series or from potassium; it is assumed, furthermore, t'rat the uranium is in radioactive equilibrium with all of its disintegration products wherein each radioactive product in the series is disintegrating at exactly the same rate at, which it is being formed. * Analyses by L. F. Rader. 5 Outcrop pictured by Collins, 1949, pi. 4, fig. 1. His thickness figures are apparently reversed. 6 Designated trachyte by Collins (1949, pi. 4, p. 1034), although his map does not distinguish Slagle trachytes and Chico phonolites. i Timber Buttes rock is said by Collins and Stobbe to be Chico phonolites. This sample, however, proved to be hornblende dacite. tent and radioactivity in the samples, but the uranium atively soluble in these minerals, they probably ac­ content is fairly uniform. Most of the radioactivity count for most of the BeO in the rock. It is doul^ful probably is due to thorium. It is known that thorium that minerals containing beryllium as an essential con­ may be hard to identify in zirconium minerals (Ran- stituent are present. kama and Sahama, 1950, p. 571). The mineralogical compositions of the rocks are com­ DONA ANA COTTNTY pared in table 52. The Chico phonolites of Collins ORGAN DISTRICT (1949) are characterized by high nepheline content and its pyroxene is chiefly aegirite. As beryllium is rel- The Organ district is in the Organ Mountains near U. S. Highway 70, about 15 miles east of Las Graces. TABLE 52. Average mineralogical composition of volcanic rocks of the Raton region The district was visited on August 28, 1949. [Rock names are those of Collins (1949, p. 1022-1023)] The geology of the district has been described in 1 8 3 4 5 6 detail by Dunham (1935, p. 194-242), A belt of l;me- 84 46 stone of Paleozoic age is upturned along the wertern 46 28 3 54 44 slope of the range; a large body of Precambrian grr.nite 39 11 2 forms the core and the eastern slope of the range. 29 3 15 26 32 Tertiary intrusive bodies of quartz monzonite and 17 6 5 8 4 8 14 in other rocks occur along the range; in the northern part Glass.. _ _ . _ . 57 of the district these are in contact with limestone. 1. Raton basalts. Average of nine modal analyses by Mertie Near the contact, much of the limestone has beer re­ (Lee, 1922, p. 9), "first period of eruption." 2. Red Mountain dacites. Average of four modal analyses by placed by andradite, diopside, wollastonite, tremolite, Stobbe (1949, p. 1068), including one from Red Mountain. epidote, specularite, phlogopite, and idocrase. S'nall 3. Slagle trachytes. Mode of specimen from Red Hill by Stobbe (1949, p. 1072). areas of tactite are rich in magnetite. Quartz, sulf des, 4. Chico phonolites. Average of eight modal analyses by and tellurides were deposited in fractures in the tactite. Stobbe (1949, p. 1074). 5. Clayton basalts. Average of six modal analyses by Stobbe Simple fissure veins in intrusive rocks and replacement (1949, p. 1052). veins in unmetamorphosed limestone were formed in 6. Capulin basalts. Average of four modal analyses by Stobbe (1949, p. 1052), including three from Mount Capulin. other parts of the district at this same time. 114 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES Samples were taken of the tactite and related min­ truded by a stock of Cretaceous or Tertiary quartz mon­ eral deposits. Descriptions of samples and analytical zonite porphyry. The principal ore deposits are dis­ data are given in table 53. None of the samples con­ seminated copper in the quartz monzonite and gold- tained more than 0.0004 percent BeO. quartz fissure veins in the Precambrian granite. A grab sample (329-318) of fluorite fro*n the Long TABLE 53. Beryllia in samples from the Organ district Lost Brother claim, on the western slope of the Burro [Spectrographic analyses by J. D. Fleteher. BeO figures determined on plates ex­ Mountains (see Eothrock, Johnson, and Hrhn, 1946, p. posed for general scanning and not for piecise determination of BeO alone] 73-74, and Gillerman, 1952, p. 278-279) contains 0.002 BeO Sample Description (percent) percent BeO. The other sample (329-319), from an 329-790 Chip sample across 90 ft of outcrop of gar- net-wollastonite-diopside tactite, with unnamed prospect in T. 22 S., E. 15 W., OT* the south­ later quartz veins, in Magdalena lime­ eastern slope of the Big Burro Mountain, consisted stone next to quartz monzonite contact southeast of Roos shaft, Memphis of scheelite-bearing tactite. It contained 0.001 per­ mine___.______<0. 0004 cent BeO. 791 Channel sample across 1.5 ft of garnet tactite, with copper and iron stains, CARPENTER DISTRICT along footwall of fault next to Magda­ lena limestone at collar of shaft 400 ft The Carpenter district is high on the west slope of southwest of Roos shaft ______. 0004 793 Chip sample across 25 ft of outcrop of gar- the Black Eange in northeastern Grant Cmnty. The net-quartz-specularite tactite in Lake principal mines are reached by about 15 miles of rough Valley limestone next to quartz mon­ zonite contact at Big Three mine_____ <. 0004 graded road that leads northeastward from State 794 Grab sample of garnet-quartz-specularite Highway 61 just south of Sherman post office. The tactite from dump of Excelsior mine. Idocrase reported from this area (Dun- district was visited on July 27 and on August 23,1949. ham, 1935, p. 230)______-._----- <. 0004 Mr. H. A. Teel of San Lorenzo, N. Mex., owner of the 796 Channel sample across 18 ft of fine­ grained garnet tactite from outcrop at Grandview mine, guided the writers over the area and portal of Merrimac mine______--___ <. 0004 supplied samples and information. Previous work for 797 Grab sample of garnet-sphalerite-specu- larite ore from bin of Merrimac mine__ <. 0004 the U. S. Geological Survey has resulted ir the discov­ 797a Channel sample across 7 ft of magnetite- ery of helvite in the Grandview mine (Y'eissenborn, chlorite-serpentine tactite in Fusselman or Montoya limestone at quartz mon­ 1948), and therefore the sampling was concentrated zonite contact, on Iron Mask claim in that area. (southeast of the Merrimac mine). (See Dunham, 1935, p. 234) ______<. 0004 A short sketch of the geology of the district was 799 Channel sample across 2 ft of garnet given by Gordon (Lindgren, Graton, and Gordon, 1910, tactite from El Paso limestone at top of San Augustine ridge.______<. 0004 p. 272). During World War II the geology was 802 Specimens of galena-altaite ore from Hill­ studied in detail by E. L. Griggs, S. P. Ellison, D. M. top mine______.___ <. 0004 Kinney, and A. E. Weissenborn of the U. £\ Geological GRANT COUNTY Survey, and exploratory work was carried on by the U. S. Bureau of Mines (Hill, 1946, p. 6-7). The geol-. BURRO MOUNTAINS DISTRICT ogy of a part of the district is shown on figure 33. Although the Burro Mountains district was not Sedimentary rocks of Paleozoic age, mainly lime­ visited during the present investigation, two samples stone, dip westward along the flank of the innge. They were furnished by Elliot Gillerman, who has described include the El Paso (Ordovician), Montoya (Ordo- mineral deposits of the district (Gillerman, 1952, p. vician), Fusselman (Silurian), Percha (Devonian), 261-289). Lake Valley (Mississippian), and Magdalena (Penn- Most of the Burro Mountains is composed of rocks sylvanian) formations. Along the crest of the range, of Precambrian age, which according to Paige (1916, these rocks are covered by Tertiary volcf.nic breccias P. 3) and flows. Normal faulting in places has brought the volcanic rocks into contact with rocks of early Paleo­ * * * comprise many granitoid varieties, some of which are zoic age. Small bodies of quartz monzonite, mainly in gneissic, and minor ill-defined schistose and quartzitic masses, which are metamorphosed ancient sediments * * *. The the forms of sills, intruded the volcanic rocks. Some granite of the Big Burro Mountains is a medium- to fine-grained of the limestone, particularly in the worMngs of the gray biotite granite composed of dominant orthoclase with some Grandview mine, has been altered to tactite composed albite, abundant quartz, and brown biotite, with accessory apa­ of garnet, epidote, magnetite, and chlorite. The tac­ tite, titanite, and iron oxide. Coarse-grained and porphyritic tite is not found at igneous contacts, and if.s occurrence varieties are also found. may be controlled by fractures. Eephcement ore In the vicinity of Tyrone on the northeastern edge of bodies of galena, sphalerite, and fluorite occur irregu­ the Burro Mountains, the Precambrian rocks are in­ larly along fracture zones in the Montoya limestone. LOCALITIES IN NEW MEXICO 115

^ ,"=\$'X EXPLANATION ->> £ \ * // \\ 11 4. */,*'s\-\\ll^\ TV * _.vv * « * "/y^""''?" ;x uartz monzonite TERTIARYSIP- *.**.*>. Q

TV

^^^t.^'^^n^^fj^^-^ ^ Vo\can c breccias anc1 flows -^/^''^o *> ^ . x >* ..v" 'i^-^s.^- VI **.£* **ii. ANDPIA

Lake Valley limestone

13°l 5i MISSISDEVONIANORDQVICIANORDOVICIAN

Percha shale §*^ SILURIAN

Montoya and Fusse man limestone, undifferentiated>

. ' . Qep ; .

E Paso formation

Contact Dashed where inferred

82 t Fault, showing dip Dashed where inferred

Portal of adit D Glory hole ^ Other mine workings

Geology by R. L. Griggs and S. P. Ellison, U. S. Geological Survey unpublished map, 1943 1000 0 3000 Feet I i i i i I _I FIOUBB 33. Geologic map of part of the Carpenter district, Grant County, N. Hex. 116 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES

GBANDVIEW MINE TABLE 54. Beryllia in samples from the Carpenter district [Spectrographic analyses by J. D. Fletcher. BeO figures determined on plates The Grandview mine is in sees. 29 and 32, T. 16 S., exposed for general scanning but not for precise determination OT BeO alone] BeO R. 9 W., 15 miles by road northeast of State Highway Sample Description (percent) 61. The claims had been prospected for about 50 years 329-315 Specimen of white fluorite from dump cf lower adit, Grandview mine..______0. 001 before the first shipment of lead-zinc ore was made in 712 Channel sample of rhodochrosite-galena 1937. From 1938 to 1945 the mine was developed by vein, same adit______-_-_- . 001 717 Grab sample of garnet-galena ore fron the Black Range Development Co., and about 19,000 southern adit, Grandview mine______<. 001 tons of ore, including 1,600 tons of zinc, 900 tons of 718 Grab sample of vuggy quartz vein ma­ terial, with galena, sphalerite, and lead, 46 tons of copper, and 14,000 ounces of silver were fluorite, from upper adit of Grandview produced. The mine was idle from 1945 until 1948, mine. No helvite seen______.02 720 Channel sample of highly oxidized ma­ when small shipments of ore were made to the Black- terial, with chlorite, galena, and hema­ hawk custom mill at Hanover, N. Mex. In August tite, from short abandoned adit jus* north of main upper adit, Grandview 1949, the mine was not operating. mine______----__------. 02 Development of the mine has been mainly through 721 Channel sample of limestone highly al­ tered to chlorite, with iron and manga­ two adits at altitudes of 7,516 and 7,570 feet; several nese oxides: same location as samph stopes connect with a glory hole at about 7,625 feet 720-- < 001 722 Channel sample of cherty limestone with altitude. A winze goes a short distance below the 7,516- vugs containing quartz, galena, and foot level. A short adit was driven about 250 feet helvite, along north-trending vein in glory hole of Grandview mine.______. 01 south of the portal of the lower adit. 726 Grab sample of andradite-diopside banded tactite, with epidote, from dump o* Helvite from the Grandview mine was first discov­ Columbia mine_____-----_--_------. 001 ered by J. W. Adams on a specimen of fluorite collected 727 Specimen of sphalerite-galena-fluorite ore from dump of Columbia mine.______<. 001 by A. E. Weissenborn, both of the Geological Survey. 735c Composite sample of mill heads for 2 day? During the present investigation several specimens of in May and June 1949, from Grandviev helvite were collected, both from the dumps and from mine (Blackhawk mill, Hanover) ______.01 small veins exposed in the glory hole. The refractive OTHEE MINES index of the helvite is variable but is near 1.730 (Weis­ The Columbia mine is about 4,000 feet sonth of the senborn, 1948, p. 649); this indicates that it is essen­ Grandview mine (fig. 33). About 600 feet of drifts tially the manganian member of the series (Glass, explore small veins in the Montoya limestone. Samples Jahns, and Stevens, 1944, p. 183). The helvite occurs of tactite and of sphalerite-galena-fluorite ore taken mainly in vugs lined with small prisms of quartz, from the dumps contain less than 0.001 percent BeO mostly in cherty limestone. Many of the quartz crys­ tals are coated with a thin layer of chalcedony. Crys­ (table 54). tals of fluorite and sphalerite are later than the quartz. CENTRAL DISTRICT (INCLUDING FIERRO, HANOVER, AND Tetrahedra of helvite as much as 3 mm on an edge SANTA RITA DISTRICTS) grow in or on the chalcedony but not on the quartz The Central mining district, about 15 miles east of crystals. Some of the helvite is associated with fluorite, Silver City, covers a large area between Bayard and but a sample of the fluorite contained no beryllium. Fierro, N. Mex. The principal mines are large pro­ Samples were taken from the dumps and under­ ducers of copper, zinc, lead, and iron. During the pres­ ground workings at the Grandview mine, as described ent investigation, the area was visited in July and in table 54. No beryllium-bearing minerals other than August 1949. Several geologists with experience in the helvite were found in the samples, and it is assumed region furnished information and samples. Thanks are that almost all of the beryllium is contained in helvite. due especially to S. G. Lasky and R. M. Hernon of the The possibility of byproduct recovery of beryllium U. S. Geological Survey, Harrison Schmitt, consulting therefore appears to be good if the mine returns to geologist, of Silver City, and geologists and engineers operation as a lead-zinc producer. of the American Smelting and Refining Co., Empire Beryllium was not found in a garnet-rich sample Zinc Co., Kennecott Copper Co., and Peru Mining Co. (329-717) from the southern adit. This may indicate The complex geology of the district has been the sub­ that the occurrence of beryllium at the Grandview mine ject of much study; the numerous published reports in­ is not related to pyrometasomatism. The association of clude those by Lindgren, Graton, and Gordon (1910, p. helvite with chlorite and chalcedony in vugs suggests 305-317), Paige (1916),Landon (1931), Schmitt (1935, deposition at relatively low temperature. 1939), Spencer and Paige (1935), Lasky (19f3), Lasky LOCALITIES IN NEW MEXICO 117 andHoagland (1948), Hernon (1949), Kelley (1949, p. Upper Cretaceous shale and limestone. Although both 83-124), Graf and Kerr (1950), and Kerr, Kulp, Pat- the dikes and the shale were extensively replaced by terson, and Wrighfc (1950). The district is on the Fort quartz, sericite, and pyrite, silicates such as pyroxene Bayard arch, which modifies the eastern limb of a and garnet are much less common. This type of deposit broad syncline of sedimentary rocks of Paleozoic and is represented by the Ground Hog mine, where samples Mesozoic ages. At various times the sediments were in­ were taken mostly from the rare garnet-pyroxene rones. truded by stocks, sills, and dikes of a variety of igneous The large copper deposit at Sana Eita is a replacement rocks. Early quartz diorite sills are conspicuous; one of the granodiorite stock, and was not sampled. known as the Marker sill is found in the Magdalena The samples taken are described in table 55. Ap­ formation of Pennsylvania!! age throughout most of parently the large tactite bodies at the southern end the district. The principal intrusive body is the Han­ of the Hanover stock, both on the western side (Puck- over granodiorite stock, about 21/& miles long; the horn Gulch and Hill 6650) and on the eastern side smaller intrusives at Santa Bita and Copper Flat are of similar age and composition. Related granodiorite TABLE 55. Beryllia in samples from the Central district [Spectrographie analyses by J. D. Fleteher. BeO figures determined or plates dikes of at least two ages were intruded along steep exposed for general scanning but not for precise determination of BeO a1one] northeast-trending faults. BeO Sample Description (percent) Thermal metamorphism has been widespread and in 329-276 4-ft channel sample of hedenbergite-gar- most places was accompanied by large additions of ma­ net-calcite marble from top of Lake Valley limestone in Uncle Sam quarry, terial. Andradite, hedenbergite, magnetite, and ilvaite Buckhorn Gulch, Hanover______<0. 0004 are the principal minerals in tactite bodies formed 277 8-ft channel sample of epidotized shale (so-called Parting shale of local usage) around the southern end of the Hanover stock and at from base of Oswaldo formation, Mag­ Copper Flat, where they replace the Lake Valley (Mis- dalena group, from same locality as sample276______. 0008 sissippian), and the Magdalena (Pennsylvanian) lime­ 280 Chip sample from 50-ft exposure of garnet stones. The occurrence of tactite is controlled by dike- tactite, lower part of Oswaldo forma­ tion at south end of "150 quarry," fault zones and favorable stratigraphic horizons, as Buckhorn Gulch______<. 0004 well as by nearness to the intrusive body. Epidote is 281 8-ft channel sample of magnetite-garnet tactite from Oswaldo formation in iron common in shaly members. The lower limestones of mine at top of Hill 6650, % mile west of early Paleozoic age, particularly the El Paso (Ordovi- Hanover______<. 0004 282 Chip sample from exposure of garnet- cian) limestone at Fierro, are principally replaced hedenbergite tactite in Oswaldo forma­ by magnetite, serpentine, and wollastonite. Small tion above white marble and below epidotized shale, "350 quarry," Buck­ amounts of magnetite and garnet occur along the horn Gulch______....______<. 0004 northern border of the Santa Eita stock. Garnet and 284 Chip sample from 125-ft exposure of gar­ net tactite in Oswaldo formation be­ pyroxene are found in a few places along the dike com­ tween Hanover stock and Hanover sill, plex that extends southwestward toward Vanadium. in road cut 800 ft south of Hanover___ . 0004 286 Chip sample from 20-ft exposure of mag­ Many of the ore deposits are associated with the netite-garnet tactite in upper part of tactite bodies. In the Hanover area large masses of Lake Valley formation, open pit of Snowflake iron mine______<. 0004 sphalerite replace the tactite along its contact with the 287 Chip sample from 6-ft exposure of mag­ unsilicated marble, particularly in the upper member netite-serpentine in so-called parting shale of local usage of Oswaldo forma­ of the Lake Valley limestone. These deposits are repre­ tion, from same locality as sample 329- sented by samples from the Empire Zinc Company 286__-_-__-__-_--_-__-_--___-_____ <. 0004 288 Chip sample from 2-ft bed of garnet-py­ quarries and from the Pewabic mine. At Copper Flat roxene hornfels in upper part of Abo similar deposits occur within the tactite. Between the sandstone, near Mountain Home mine on Humboldt Mountain. Idocrase re­ Hanover and Santa Eita stocks, sphalerite bodies lie ported from this locality (Schmitt, along north-trending fissures. The gangue contains 1939, p. 812) but none was noted in the sampling______<. 0004 hedenbergite and a little garnet, ilvaite, rhodonite, and 289 Specimen of rhodonite- and hedenbergite- epidote, as well as calcite. Although the deposits are bearing limestone from 445 N stope of Oswaldo mine______. OOOX not close to intrusive rocks, they are probably similar 291 Core split of garnet-diopside tactite, with pyrite, magnetite, chalcopyrite, and in origin to those of the Pewabic and Empire zinc sphalerite, in Oswaldo formation, from mines. This type of deposit is represented by samples 41 to 302 ft in diamond-drill hole 1101, Santa Rita area______<. 0004 from the Oswaldo mine. 292 Core split of garnet-pyroxene-epidpte In the southeastern part of the district, near Vana­ tactite and some hornfels, with pyrite, magnetite, and chalcopyrite, in upper dium and Bayard, sphalerite-galena-chalcopyrite ore part of Lake Valley limestone, from 320 to 590 ft in diamond-drill hole 1101, occurs along the contacts of the granodiorite dikes with Santa Rita area______<. 0004 118 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES TABLE 55. Beryllia in samples from the Central district Con. ores of the Ground Hog and Oswaldo mines. The BeO highest value 0.002 percent BeO was found in garnet Sample Description (percent) 293 Core split of epidote-chlorite-pyrite-ser- tactite from the Ground Hog mine, but such material is pentine rock, with some massive biotite quite rare in this part of the district. hornfels, in lower part of Lake Valley limestone, from 590 to 685 ft in dia­ mond-drill hole 1101, Santa Rita area. <0. 0004 PINOS ALTOS DISTRICT 294 Core split of 6 in. out of 15.5 ft of highly altered granodiorite dike in Lake Valley The Pinos Altos district is in the Pinos Altos limestone, from horizontal drill hole east of 436 drift in Oswaldo mine. __ .0004 Mountains about 8 miles north of Silver City. The dis­ 295 Core split of 7 in. out of 12.5 ft of epidote- trict was visited on August 24,1949. James Neumann, garnet-pyrite tactite from same forma­ tion and drill hole as sample 294___ _ <. 0004 chief geologist for the United States Smeltiro; and Ke- 296 Core split of 5 in. out of 1.5 ft of sphalerite fining Co. at Vanadium, N". Mex., supplied specimens and tactite from same formation and drill hole as sample 294______.001 of the ores and information concerning t>e mining 297 Core split of 5 in. out of 10 ft of unmeta- operations. morphosed limestone, same formation and drill hole as sample 294______<. 0004 The geology of the Pinos Altos district was described 301 Chip sample from 50-ft exposure of garnet by Graton (Lindgren, Graton, and Gordon, 1910, p. and sphalerite in lower part of Lake Valley limestone on 160 level Pewabic 297-301) and by Paige (1910; 1916, p. 14). On the mine______<. 0004 west side of the Pinos Altos Mountains is a north- 302 6-ft channel sample of garnet-diopside tactite in upper part of Lake Valley trending mass of limestones of Paleozoic age about limestone on 160 level of Pewabic li/2 miles long and less than a mile wide. Early mafic mine. <. 0004 303 6-ft channel sample of garnet tactite in intrusive rocks, principally diorite porphyry are cut upper part of Oswaldo formation, on by a mass of granodiorite about 2 miles in diameter. 160 level of Pewabic mine______<. 0004 305 Grab sample from 500-sq-ft exposure of Both the main intrusive and diorite porphyry dikes cut granodiorite of Hanover stock, 1,000 ft the limestones and are accompanied by some pyrometa- east of Hanover. Aplite dikes excluded from sample.______<.0004 somatic alteration. Tactites composed of garnet, pyrox­ 306 30-ft channel sample of magnetite-ser­ ene, and epidote are of limited and irregular extent. pentine tactite highly altered to clay, from upper part of El Paso limestone The ore is composed of sphalerite, pyrite, chalcopyrite, at northwest end of open pit at Jim Fair bismuthinite, and quartz; at places it occurs in the mine, Fierro______<.0004 308 Grab sample from 2,000-sq-ft exposure of tactite. Both thrust and normal faults are common garnet tactite in Oswaldo formation, and some faults are mineralized. west side Yellowdog Gulch, near west edge of Copper Flat stock. Idocrase The largest mine in the western part of the district reported from this locality (personal is the Cleveland tunnel, described in detail by Paige communication from R. M. Hernon) but none was found during sampling __ <. 0004 (1910, p. 122-125). A grab sample (329-738) of spha- 730 4.5-ft channel sample of hedenbergite lerite-pyrite ore collected from the dump contained less tactite altered to chlorite, with sphal­ erite, in upper part of Lake Valley lime­ than 0.0004 percent BeO. Although Graton (Lind­ stone near quartz granodiorite porphyry gren, Graton, and Gordon, 1910, p. 300) describes much dike on 1,800 level of Groundhog mine_ .001 732 Specimen of hedenbergite and sphalerite- garnet and specularite from this tunnel, none was ob­ pyrite ore, in upper part of Lake Valley served on the dump. At the Houston-Thomas mine, limestone near hornblende granodiorite porphyry dike 25 ft above 1,800 level of which adjoins the Cleveland tunnel on the northwest, Groundhog mine.______.0008 some garnet-pyroxene-epidote tactite was *ound. A 733 4-ft channel sample of hematite-pyrite- sphalerite-hedenbergite tactite at con­ grab sample (329-740) of sphalerite-pyrite-chalcopy- tact of quartz granodiorite porphyry dike and limestone, 1,800 level of rite ore from the dump of the new shaft of this mine Groundhog mine______.0008 contained less than 0.0004 percent BeO. TH geology 734 Grab sample from 4-in. vein of rhodonite- sphalerite-hedenbergite in limestone of the mine is described in a report by Soule (1948). near quartz granodiorite porphyry dike The gold-quartz fissure veins in the granodicnte of the on 1,800 level of Groundhog mine_____ <. 0004 807 Grab sample 1 of garnet (GrogAnggAlo*)- eastern part of the district were not sampled. hedenbergite tactite with sphalerite, at dike contact on 1,800 level of Ground­ HIDALGO COUNTY hog mine.______.002 APACHE NO. 2 DISTRICT 1 Sample collected by Mr. B.C. Hardie of American Smelting & Refining Co. The Apache No. 2 district is in the Apache Hills, 6 (Pewabic mine), contain little or no beryllium. The miles southeast of Hachita, N". Mex., which is on the same is true of the magnetite deposits farther north Southern Pacific Eailroad and State Highways 9 and (Snowflake and Jim Fair mines). Small amounts of 81. The district is reached by an unimproved road from beryllium were detected in the limestone replacement Hachita. It was visited on August 26 and 27,1949. Al- LOCALITIES IN NEW MEXICO 119 bert Fitch of Hachita, owner of the Apache mine, fur­ R. 14 W. nished much information on the deposits of this and neighboring districts. Little work seems to have been done in the district since 1938 when the United States Smelting and Kefining Co. ceased operations at their new shaft on the Apache claim. The geology of the district was described briefly by Lindgren (Lindgren, Graton, and Gordon, 1910, p. 343-344). Gently-dipping Cretaceous and possibly Pennsylvanian limestones are exposed in the northern part of the Apache Hills (Barton, 1928, p. 348). A sill- like intrusive body of granodiorite porphyry crops out along the southern slope of the hills. Ore deposits are found only at the southern contact of this body with limestone and consist of large masses of marble and tactite that are partly replaced by iron, copper, bismuth, and silver minerals. The ore minerals have been oxi­ dized to a depth of at least 500 feet. Scheelite and wolframite are reported to occur in large quantities in Locality sampled and number. part of the Apache mine. All samples less than 0.0004 Four samples were taken at localities shown in figure percent beryllla 34 and are described below: Sample Description Contour interval 25 feet Datuiji is mean sea level 329-752 Chip sample from 15 ft of exposure of garnetized mar­ FIGURE 34. Index map showing localities sampled in the Apache No. 2 ble, with copper and iron stains, in face of glory district, Hidalgo County, N. Mex. hole 125 ft N. 20° W. of Apache shaft. Scheelite reported at this locality. tions of the metamorphism and mineral deposits in the 755 Grab sample of garnet-epidote-calcite-pyrite marble area. The sedimentary rocks of the Little Hatchet from dump of new Apache shaft. 781 Grab sample of garnet tactite from two lenses ex­ Mountains are of Early Cretaceous age (Bisbee group), posed in limestone and conglomerate. and include possibly 5,000 feet of the Broken Jug lime­ 783 6-ft channel sample of garnet tactite, with copper and stone overlain by about 15,000 feet of clastic sediments iron stains, in limestone (sample 781 from same and volcanic rocks. The several intrusive bodies are layer). mostly of Late Cretaceous or early Tertiary age. Out­ Spectrographic analysis by Janet D. Fletcher did not crops of monzonite and quartz monzonite near Eureka detect beryllium in these samples, the limit of detection and Sylvanite are interpreted as being segments of a being about 0.0004 percent BeO. large continuous sill-like body in the sedimentary rocks. The rocks are displaced by the Copper Dick fault which HACHITA DISTKICT (INCLUDING EUREKA AND SYLVANITE down drops the northern half of the range by 3 miles. DISTRICTS) A stock of granitic rocks forms the southern tip of the The Hachita district is in the Little Hatchet Moun­ range where dikes are common. tains about 12 miles southwest of Hachita. The mines Near their contact with the stock, the sedimentary in the northeastern part of the range, near Old Hachita, rocks are metamorphosed to tactite and hornfels con­ commonly known as the Eureka district, are reached by taining garnet, pyroxene, scapolite, and feldspar. A a graded road from Hachita. This part of the district zone of actinolite marble occurs at greater but variable is in Grant County. The mines in the southern part distances from the contact. of the range, including the old camp of Sylvanite, are The few short veins are mostly within or near the best reached over a road leading southwestward from monzonite at Eureka and Sylvanite. At Sylvanite na­ Hachita across a pass in the Little Hatchet Mountains. tive gold occurs with chalcopyrite, hessite, tetradymite, The road along the southwestern part of the range arsenopyrite, and pyrite in a gangue of tourmaline, ac­ south of Sylvanite was barely passable when the district tinolite, quartz, and calcite. At Eureka galena and was visited on August 25 and 20,1949. sphalerite are in a gangue composed chiefly of man- An account of the geology of the Little Hatchet ganosiderite. Scheelite and molybdenite are un­ Mountains by Lasky (1947) contains excellent descrip- common. 120 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES The following samples from the Hachita district were larite. Fluorspar was deposited with calcite and quartz analyzed for beryllium: in open fissures during a late stage of mineralization. Sample Description Samples were taken hi the Lordsburg district as de­ 329-740a Sample from several 8-in. channels across vein of scribed below: scheelite-hematite-tetradymite ore at contact of Sample Description monzonite and marble, from 25-ft shaft 200 ft 329-421 3-ft channel sample across quartz-gossan at outcrop south of the southeast corner of the Virginia claim of "85" vein. (Lasky, 1947, p. 67). 422 Grab sample of quartz-sericite-tourmaliie vein ma­ 741 4-ft core of mill tailings at American mill. terial with minor chalcopyrite, in granodiorite, from 742 Grab sample of arsenopyrite-pyrite-sphalerite- dump of "85" mine. manganosiderite-calcite ore, from dump of Ameri­ 423 Grab sample of quartz-specularite-chalcopyrite ore in can mine. basalt, from dump of "85" mine. 743 Grab sample of manganese carbonate and oxides 424 Channel sample across 2.5-ft vein of fl xorite, 30 ft from dump of American mine. northeast of Fluorite (Kneyer) No. 1 shaft. (See 744 Chip sample from 100 sq ft of garnet-pyroxene Rothrock, Johnson, and Hahn, 1946, p. 105-106.) tactite exposed northeast of Fitzgerald shaft, 425 Grab sample fluorite-calcite ore from outcrops and American mine. dumps of Fluorite No. 8 claim. 745 Chip sample across 30 ft of garnet-quartz tactite 426 Same, from Fluorite No. 9 claim. exposed north of Fitzgerald shaft, American mine, 746 Grab sample of chalcopyrite-garnet ore from dump of Spectrographic analyses by J. D. Fletcher showed no Copper Dick mine. beryllium in any of the samples. The samples from 747 20-ft channel sample of garnet tactite, with copper the "85" mine were analyzed qualitatively with a limit carbonates, from northeast face of opencuts at of detection of about 0.0004 percent BeO, ard the sam­ Copper Dick mine. 749 Sample of oxidized ore from Santa Maria tunnel, ples from the Fluorite claims were analyzed quantita­ originally consisting chiefly of quartz, calcite, tively with a limit of detection of about 0.0001 percent barite, chalcopyrite, pyrite, molybdenite, and BeO. Samples collected in 1943 from the Bonner mill epidote. in Lordsburg, which was treating ores from the Bonney 750 Grabjsample of garnet-chalcopyrite-molybdenite ore and Anita No. 1 mines, for the Mine, Mill, and Smelter from metamorphosed Broken Jug limestone at contact of monzonite stock, on Wyoming claim Survey of the U. S. Geological Survey also showed no northwest of Hachita Peak. beryllium, the limit of detection being 0.001 percent 751 Chip sample from outcrop of coarse amphibole tac­ BeO. Analysis of samples collected in 1£43 showed tite, from Howells Ridge formation near monzonite 0.003 percent BeO in the fluorite of the Kneyer No. 1 contact, south side of Sylvanite Gulch. mine, but the analysis obtained for sample 329-424 is Spectrographic analyses by J. D. Fletcher did not probably more reliable. detect beryllium in any of these samples, the limit of de­ tection being about 0.0004 percent BeO. The gold- SAN SIMON DISTRICT quartz veins of the Sylvanite area were not sampled. The San Simon district is in western Hidalgo County, next to the Arizona boundary. It is in tH southern LORDSBURG DISTRICT part of the Peloncillo Mountains between Pteins Pass The Lordsburg mining district, also known as the on the north and Antelope Pass on the south. U. S. Virginia district, is in the northern Pyramid Moun­ Highway 80 crosses Granite Gap about 2 miles north tains, a few miles southwest of Lordsburg, which is on of Antelope Pass. An unimproved road leading south the Southern Pacific Railroad and U. S. Highway 80. from the highway at the west end of Steins Pass pro­ The district was visited on July 25,1949. vides limited access to the district. Part of the district The geology of the district was described in detail was visited on July 25,1949. by Lasky (1938) and that of the fluorspar mines by The geology of the district was describee1, briefly by Eothrock, Johnson, and Halm (1946, p. 104-108). The Liiidgren and Graton (Lindgren, Graton, and Gor- oldest rocks are basalts of Early Cretaceous age, in­ dor, 1910, p. 329-332). The principal operation in 1949 truded by plugs of basalt and rhyolite. An irregular was the Silver Hill mine. It is at the head of a canyon stock of granodiorite forms the northeastern part of the on the western slope of the mountains, 4 mT^s directly mountains. Faults in the granodiorite which trend east of New Mexico-Arizona boundary morument No. from east to northeast are the loci of the ore deposits. 334 and 5 miles south of Steins Pass. This part of the The most important veins contain chalcopyrite, galena, mountains is composed of a thick section of gray thick- pyrite, and specularite in a gangue of quartz, calcite, bedded limestone that dips 25° to the north; according and tourmaline. The earliest stage of vein formation to Graton (Lindgren, Graton, and Gordon, 1910, p. 331) included intensive replacement of the granodiorite wall it is probably Carboniferous in age. A monzonite rock by sericite, chlorite, calcite, tourmaline, and specu­ porphyry dike 150-feet thick trends southwest for sev- LOCALITIES EST NEW'MEXICO 121 eral miles. Garnet, galena, and sphalerite replace lime­ GAX.LXHA8 DISTRICT . ; stone in the contact zone near the dike. About 500 feet The Gallinas district occupies about 10 square railed north of the Silver Hill shaft, an aplitic branch of the at the eastern end of the Gallinas Mountains in north­ dike strikes S. 50° W. Several hundred feet from the ern Lincoln County. The area is served by U. S. High­ main dike the contact zone along the aplite branch has way 54 and by the Southern Pacific Railroad at Gal­ been explored by a 30-foot adit on the S and W claim. linas siding, 8 miles east of the district. Although The ore here is similar to that at the Silver Hill mine. time did not permit a visit to the district, samples v^ere Two unidentified silicates, one of which resembles wol- furnished by V. C. Kelley of the University of Few lastonite, form part of the gangue at this locality. Mexico, and R. G. Knickerbocker of the U. S. Bureau About half a mile south of the Silver Hill mine the of Mines. workings of the Johnny Bull mine explore a similar The geology of the district is described by Kelley, dike contact zone. Garnet, quartz, and possible wol- Rothrock, and Smalley (1947). Precambrian granite lastonite and pyroxene are accompanied by pyrite, chal- and gneiss are overlain by sandstone and siltstonc of copyrite, bornite, and oxidized copper and iron Permian age. In early Tertiary time these rocks v^re minerals. intruded by laccoliths and sills of syenite porphyry, A 4-foot channel sample (329-427) was taken across with some monzonite and monzonite breccia. The rocks the ore near the collar of the Silver Hill shaft and a 5- were cut by faults and breccia zones. Ore deposits of foot channel sample (329-429) was cut across the ore magnetite and of fluorite-barite-calcite-bastnaesite vith at the portal of the adit on the S and W claim. A minor amounts of sulfides, occur in the fractures and sample of tactite (329-433) was chipped from a 10-foot breccia zones. Locally, as at the American iron mine, exposure in an open pit below the north shaft of the epidote and tremolite are associated with the ore. Johnny Bull mine. Spectrographic analyses by J. D. Sample 329-808 is a specimen of magnetite-actinclite Fletcher showed no beryllium in any of the samples, rock from the southeastern edge of the main bencl of the limit of detection being 0.0004 percent BeO. the American mine (Kelley, 1949, fig. 34). Quantita­ tive Spectrographic analysis of this sample by Janet D. JLZNCOJLN COUNTY Fletcher showed 0.008 percent BeO. Sample 329-We CAPITAN DISTRICT is a composite of fluorite ore (bastnaesite-bearing) from The Capitan iron-mining district is at the western the Red Cloud mine. Quantitative Spectrographic anal­ end of the Capitan Mountains, just east of State High­ ysis by J. K. Murata showed 0.0002 percent BeO. I "ir- way 48, 6 miles north of Capitan. Although time did ing a previous mineralogical study of the bastnae^te not permit a visit to the district, a sample of contact (Glass and Smalley, 1945), Spectrographic analysis had metamorphic rock was furnished by V. C. Kelley, who not detected any beryllium in this mineral (J. J. Ghss, had been studying the iron deposits for the U. S. Geo­ oral communication). The relatively high beryllium logical Survey and the New Mexico Bureau of Mines content of the sample from the American mine indi­ and Resources. According to his report (Kelley, 1949, cates that further sampling for beryllium in the district is warranted. p. 144-153), a large stock of granite aplite intrudes the LUNA COUNTY San Andres formation of Permian age. The main iron deposit is a ring-shaped body in the limestone mem­ TRES HERMANAS DISTRICT ber of the San Andres formation about 2,000 feet west The Tres Hermanas district is in the Tres Hermanas of the contact with the granite. Structural relations Mountains, just north of Columbus, in .southern Lnna suggest that the ore was localized in a pre-intrusion County. Two localities in this district were visited on sink hole or collapse structure. An inner zone of epi- August 26,1949. dote, phlogopite, and tremolite is surrounded by a The geology of the Tres Hermanas Mountains was phlogopite-tremolite zone, with magnetite concentrated described briefly by Darton (1916, p. 79-82) and the toward the outside. mines by Lindgren, Graton, and Gordon (1910, p. 2r>2- The sample (329-810) collected by Kelley was from 295). The central mass of the mountains is compcsed the outer part of the phlogopite-tremolite zone, between of granite porphyry, flanked in part by andesite, rhyo- magnetite ore and limestone. The locality is shown in lite, and agglomerate, all of Tertiary age. In the north­ the lower center of his figure 25 (Kelley, 1949) as the ern part of the mountains some of the porphyry has northernmost of a pair of trenches just west of the intruded Gym limestone (Permian), which is up­ Capitan road. Spectrographic analysis by J. D. Fletch­ turned and metamorphosed to garnet-wollastonite tac­ er indicated 0.005 percent BeO. Further sampling for tite. Spurrite has also been identified in the tactite beryllium in this area seems warranted. (Lasky and Wooton, 1933, p. 83). 467945 59 9 122 OCCURRENCE OP NONPEGMATITE BERYLLIUM IN THE UNITED STATES The principal mineral deposits are those at the north­ of andesite and rhyolite of Tertiary age form the top western tip of the range which were mined for zinc. of the section. Most of the beds in the southern part of Limestone beds 1,000 to 2,000 feet north of the porphyry the range dip southward, but in the northern part they and limestone contact have been replaced by zinc and are flat or dip northward. Two or more thrust faults lead minerals. Most of the zinc is oxidized, principally may be present in the region. to willemite; smithsonite, hydrozincite, and calamine In the area containing the tungsten and beryllium are also present. A chip sample (329-756) of garnet- deposits, the Fusselman limestone does no* crop out amphibole-calcite tactite from near the contact contains and may be absent as a result of faulting or of uncon- less than 0.0004 percent BeO. formable overlap. The Montoya and Gym limestones The Tres Hermanas mine is at the contact of the por­ are cut by small masses of light-colored granitic rock. phyry and the limestone on the east slope of South The mineral deposits occur mainly in veirs and tac- Peak. In this area the sediments have been metamor­ tites in Montoya limestone. phosed to interbedded garnet-tactite and calcite-marble for a distance of 150 feet from the contact. According TUNGSTEN AND BERYLLIUM DEPOSITS to Barton (1916, p. 82), idocrase occurs at this locality. Tungsten was first reported in 1908 fronr a vein on In a channel sample (329-760) taken of a 1-foot bed what are now the Eloi and Morlock claims (Hess, 1908, of the tactite, the BeO content is less than 0.0004 per­ p. 726); the vein was described briefly by Lindgren cent. (Lindgren, Graton, and Gordon, 1910, p. 2£9). Beryl VICTORIO DISTRICT was discovered in this vein in 1948 by W. P. Johnston of The Victorio district comprises a group of mines and the New Jersey Zinc Exploration Co., Hanover, N. Mex. prospects at the southeast end of the Victorio Moun­ Helvite was found in the scheelite-bearing tactite de­ tains 3 miles south of Gage, a station on the Southern posits east of the vein by W. I. Finch during the pres­ Pacific Railroad. The Victorio Mountains are a range ent investigation. The tungsten deposits am explored of hills that rise about 800 feet above the neighboring by several shafts and many prospect pits. The occur­ bolson. The area was visited in September 1949 in the rence of beryllium in the deposits has been discussed company of Mr. D. S. Tedford of Columbus, N. Mex., byHolser (1953). who generously supplied maps and information. Two Samples obtain from the deposits are described in days were spent in sampling and mapping an area con­ table 56 and the localities sampled are shown on figure taining beryllium-bearing veins and tactite deposits. TABLE 56. Beryllia and tungsten in samples from the Victorio Most of the production has been from the eastern part district of the district, where mines in the vicinity of Mine Hill [Spectrographlc analyses by Janet D. Fletcher. BeO and W figures determined on plates exposed for general scanning but not for precise determination of BeO and W have produced more than a million dollars in gold, sil­ alone] ver, copper, lead, and zinc since 1880. In 1949, mining BeO W Sample Deicription (percent) (percent) operations had ceased except for development work. 329-390 6-ft channel sample of altered The area containing tungsten and beryllium deposits is limestone from south end of pit on Bogle claim. Another about a mile northwest of Mine Hill in sees. 29 and 30, sample reportedly from same T. 24 S., E. 12 W., New Mexico principal meridian. locality contained 1.06 percent BeO.- _ - -.- 0. C3 0.02 The deposits are mainly on claims of the Bogle group, 392 4-ft channel sample of altered including the Eloi, Morlock, Ogre, Bogle, and Yahoo limestone from pit on Bogle claim.______. C13 <. 01 claims, owned by D. S. Tedford, and the Tungsten Hill 393 2-ft channel sample of altered group, owned by H. E. Eaton of Silver City, N. Mex. limestone from pit on Bogle claim..______.014 <. 01 Prospecting has been in progress for many years, and 394 Grab sample of serpentinized a little tungsten ore was produced in 1943. limestone with clay, from bottom of Bogle shaft_____ .005 <. 01 397 Grab sample of garnet marble GEOLOGY from dump of Morlock shaft. _ <. 011 . 06 399 5-ft channel sample of silicated Brief descriptions of the geology of the region are limestone from collar of Yahoo shaft..______.___ .1 .OX in reports by Lindgren, Graton, and Gordon (1910, p. 399a Grossularite separated from 290-292), and Barton (1916, p. 83-85). The rocks of sample 399______.007 ______400 2-ft channel sample from lime­ Paleozoic age are mainly limestone and include the stone on hanging wall of quartz Montoya (Ordovician), Fusselman (Silurian), and vein near its north end, in prospect pit on Eloi claim__ . 02 <. 01 Gym (Permian) formations. These are overlain by 401 2-ft channel sample across quartz- Tertiary rocks consisting mainly of shales and sand­ muscovite-beryl-wolframite vein, same locality as sample stones, with some coarse conglomerate beds. Thin flows 400..-.-___.______. T .08 LOCALITIES NEW MEXICO 123 TABLE 56. Beryllia and tungsten in samples from the Victoria Prismatic beryl crystals oriented perpendicular to district Continued the vein wall occur mostly as part of a selvage on the BeO W Sample Description (percent) (percent) hanging-wall side. The beryl crystals, as much as 5 402 2-ft channel sample of limestone from footwall of quartz vein, centimeters long and 1 centimeter in diameter, are same locality as sample 400_ _ 0. 005 <0. 01 bounded by simple prisms and pinacoid. The beryl is 403 Chip sample from outcrop of 3-ft rhyolite dike, on Morloek very pale green (5G 9/2) to colorless (Goddard and claim______. 003 <. 01 others, 1948). The refractive index (N0) is 1.5T4± 404 Two 1-ft channel samples from quartz vein near its south end 0.001 corresponding to a composition of about 13.5 per­ on Morloek claim______.02 .08 cent BeO. Milky quartz and some fine-grained muwo- 405 1-ft channel sample from quartz vein at bottom of inclined shaft vite make up most of the vein. The tungsten mineral on Morloek claim______.01 .1 is a member of the wolframite series. Accessory min­ 408 6-ft channel sample of tactite from pit on Tungsten Hill No. erals are fluorite, galena, pyrite, wulfenite, lead car­ 3 claim______.03 .OX bonates, and scheelite. The beryl-bearing selvago is 4lOa Idocrase separate from idocrase- f luorite -tremolite-grossularite most evident in the pits near the northern end of the banded tactite, from pit on the vein. Beryl could not be seen in samples taken from Tungsten Hill No. 2 claim._ . 02 _..... 411 Grab sample of garnet marble and the southern end of the vein and from the undergroTrad tactite, average of dump at workings, but the analyses suggest that it is present. shaft 2 on Tungsten Hill No. 3 claim______. 006 . 04 On the hill near the middle of the Eloi claim just 414 4-ft channel sample of quartz vein below a conglomerate bed that presumably marks the from north end of 35-ft level, Eloi claim..______,01 . 1 base of the Gym limestone, several small veins h«ve 415 4-ft channel sample of garnet been prospected by shafts or pits (fig. 35). In the tactite from western edge Eloi claim______.06 .06 westernmost shaft, a 3-inch quartz vein contains caMte 416 Chip sample of 3-in. quartz- and wolframite, and a similar vein that crops out a few calcite-wolframite vein from shaft near middle of Eloi feet east is rich in fluorite. Samples 329-416 and 3^9- claim______%______.02 .X 417 of these veins contained 0.02 percent and 0.005 per­ 417 Chip sample of fluorite-quartz vein, a few feet east of sample cent BeO, respectively. 416---....______-. .005 .2 The walls of the main quartz vein are not gref.tiy 418 Chip sample of green clay-size material in altered limestone, altered, the limestone retaining its gray color and fine from pit on Tungsten Hill No. grain; locally it contains small crystals of grossulaiite. 2 claim. ______.008 <. 01 420 Grab sample of garnet tactite Near the northern end of the vein, a sample (329-401) from dump of shaft on Tung­ across the total width of the vein contained 0.2 percent sten Hill No. 2 claim. _____ .002 <. 01 BeO. A sample (329-400) across 2 feet of the hanging 85. Samples of the vein material contain as much as wall contained 0.02 percent BeO and a similar sample 0.2 percent BeO and average about 0.04 percent; the (329-402) of the footwall contained 0.005 percent BO. maximum BeO content of the tactite and marble sam­ The small veins on the Eloi claim are bordered partly ples is 0.1 percent, with the average about 0.02 percent. by tactite. These amounts are higher than those obtained in any Pyrometasomatio deposits other district sampled during the present investigation. Marble and tactite are most common on the Tungsten Recovery of beryllium in connection with tungsten min­ Hill No. 3 claim (fig. 35) where they occur as irregrlar ing appears feasible, although the tonnage of tungsten lenses and bands several feet in length surrounded by ore probably is not large. Much of the beryllium in unaltered Montoya limestone. The marble and tac*ite the tactite may not be recoverable and their tungsten are not near an exposed intrusive body, although a small content is low; the quartz veins are more promising. mass of granitic rock crops out on the hill to the north. Quartz veins Most of the altered limestone dip steeply. The main quartz vein strikes north for a distance of The most common type of tactite is a coarse aggre­ about 600 feet on the Eloi and Morloek claims, and gate of grossularite and calcite, although in some plrces dips 60° E. It is a uniform fissure filling from 1 to the grossularite has entirely replaced the calcite. A 2 feet thick, making sharp contact with the limestone. pyroxene with optical properties near augite is a com­ A shaft on the Morloek claim follows the vein down 35 mon associate of the garnet. These minerals are re­ feet to short drifts, above which small stopes extend placed by fine-grained tremolite and talc. A mineral upward. Several other shafts and pits have been dug resembling psilomelane coats some of the garnet. along the vein outcrop. Scheelite is rare. Specimens of grossularite marble 124 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES

EXPLANATION

Montoya liriestone

Beryllia-b^ering tactile and marble

Approximate contact t £5 Strike and dip of beds _L£° Strike of vertical beds

329-394; 0.005 Locality sampled end number; percent fa?ryllia

Base from claim map Geology by W. T. Holser and by D S. Tedford W. I. Finch, September 1949 FIGURE 35. Tungsten and beryllium deposits In the Vletorio district, Luna County, N. Mex. from the dump of the main shaft on the Tungsten Hill ters about 3 millimeters in diameter. It is anoma­ No. 3 claim, contained about 10 percent helvite. The lously biaxial negative, with a very small ontic angle, helvite is medium yellow (5Y 7/6) (Goddard and and very low birefringence. The index of refraction others, 1948) very similar in color to several other min­ (Nx or Ny) is 1.701:1=0.002. Spectrographic analysis of erals in this district, such as grossularite, vanadinite- hand-picked grains (329-410A) showed 0,2 percent mimetite, and serpentine. However, the helvite is eas­ BeO. ily recognized, for it occurs in distinctive sharp tetra- In the southern part of the area, on the Ogre, Bogle, hedra scattered through the calcite. The crystals are Morlock, and Yahoo claims, exposures are poor. Pits about 5 millimeters across. Some are twinned on (111). expose several feet of loose bouldery material partly The helvite has a refractive index of 1.735±0.005, and cemented by caliche. The lower part of the loose mate­ a specific gravity of 3.25, corresponding to a composi­ rial is nearly in place, apparently a product cf weather­ tion of about 85 percent helvite, 15 percent danalite ing from the underlying pediment. The rocV is highly (Glass, Jahns, and Stevens, 1944, p. 183). In thin sec­ oxidized and appears to have been originally marble tion the helvite is pale yellow, isotropic, and shows containing garnet and pyroxene. Specimens from some dark peripheral zones of very fine inclusions, sim­ shafts on the Ogre and Bogle claims were particularly ilar to the helvite from Casa La Plata, Cordova rich in serpentine. A sample taken from one of these Province, Argentina, and Schwartzenberg, Germany prospects by the U. S. Bureau of Mines was reported to (Fischer, 1925, p. 146). Crystals of grossularite are contain 1.06 percent BeO (J. H. SouM, 1949, personal euhedral to subhedral against the helvite. communication). The highest value obtained in sam­ A green tactite from the Tungsten Hill No. 2 claim ples of altered limestone and marble taken during the is composed of bands of idocrase and fluorite alternat­ present examination was 0.1 percent BeO (sc^ table 56, ing with bands of tremolite, largely altered to talc, samples 329-390 to 329-399). and garnet. The idocrase occurs as radiating clus­ Helvite was seen only in the specimens from the shaft LOCALITIES IN NEW MEXICO 125 on the Tungsten No. 3 claim. To trace the occurrence has been one of New Mexico's principal metal produc­ of beryllium in the other tactite, several samples whose ers, was visited on July 21,1949. analyses showed beryllium were separated in heavy The geology of the mine is discussed in many papers, liquid. The heavy separate (mostly grossularite) was which are summarized and supplemented by Hsrley tested for helvite by staining (Gruner, 1944), and the (1940, p. 69-89). The mineral deposits are in Precam­ light separate (mostly carbonates) was examined opti­ brian schist and diabase intruded by Precambrian cally for beryl. In several thousand grains examined, granite. These rocks are exposed in a window in l:Tne- no grain of either mineral was found. Idocrase was stone of the Magdalena group (Pennsylvanian and found in only one sample (329-4:10). Grossularite was Permian). The ore deposits occur along a shear zone separated from a sample containing 0.1 percent BeO that trends northeasterly through the schist anc1 di­ (329-399), but was found to contain only 0.007 percent abase. The ore contains pyrite, sphalerite, chalcopyrite, BeO. The mode of occurrence of beryllium in the galena, pyrrhotite, bornite, and gold. Chlorite, actino- tactite may be similar to that in the tactite at Iron lite, sericite, quartz, tourmaline, and roscoelite have Mountain, N. Mex., where beryllium occurs in several formed in the wallrock. silicates and an unidentified alteration product (Jahns, A grab sample (329-386) of ore and wall rock from 1944b, p. 58). the main dumps at the Pecos mine contains less than OTEKO COUNTY 0.0004 percent BeO. The occurrence of beryllium in the feldspathoidal SANDOVAL COUNTY igneous rocks of the Cornudas Mountains, southern Otero County, is discussed in the section on the Trans- COCHITI DISTRICT Pecos Region, Texas and New Mexico. The Cochiti, or Bland, district is in the Valles Moun­ The mines of the Juarilla district, northwest of Oro- tains about 30 miles west of Santa Fe. The gee logy grande, expose extensive tactite zones (Lindgren, Gra- of the district was described in detail by Graton (Lind­ ton, and Gordon, 1910, p. 184-187). Earlier sampling gren, Graton, and Gordon, 1910, p. 150-162). Intru­ of some of this tactite by the American Smelting and sive monzonitic rocks that are exposed in the lower Refining Co. did not detect any beryllium. The district parts of the canyons are covered by extensive floras of was not visited during the present investigation. rhyolite. Quartz, sphalerite, pyrite, and chalcopyrite SAN MIGUEL, COUNTY with minor amounts of argentite and gold, were de­ posited along fracture and breccia zones in the mon­ KOCIADA DISTRICT zonitic rocks. The Rociada district is in the eastern foothills of the According to Mr. C. W. Arnold of Pena Blanca, N. Sangre de Cristo Range. It is reached by improved Mex. (personal communication), a vein at the Big roads leading westward from State Highway 3. The Sambo mine, near Bland, was reported to contain as district was visited on July 20,194:9. much as 1.0 percent BeO. The mine workings, consist The geology of the district was described briefly by of a short adit in monzonite and a crosscut that inter­ Harley (1940, p. 52-56). The mineral deposits are in sects a fracture zone containing quartz and calcite. Precambrian gneisses and mica schists that have been The monzonite is highly altered. Two samples were intruded by sills of diabase and masses of granite. taken at the mine by J. W. Adams of the U. S. Geo­ Quartz veins in the metamorphic rocks contain pyrite, logical Survey. A 6-foot channel sample (JA-49-4) chalcopyrite, bornite, chalcocite, sphalerite, and galena, across the fracture zone contained 0.0005 percent BeO, with minor amounts of gold and molybdenite. and a grab sample (JA-49-5) of the altered monzonite At the Azure-Rising Sun mine, 4 miles southwest of contained 0.0007 percent BeO. Rociada, tactite minerals are associated with the veins in quartz-biotite schist. Epidote, garnet, amphibole, SANTA FE COUNTY specularite, and tourmaline occur in the ore and in ad­ NEW PLACERS DISTRICT jacent wall rock. A grab sample (329-384) from the dumps containing both ore and wall rock contains less The New Placers, or San Pedro, district is in south­ than 0.0004 percent BeO. western Santa Fe County, just east of the village of Golden on State Highway 10. It was visited on July WILLOW CREEK DISTRICT 12 and 13,1949, when, except for the New Placers mine The Willow Creek district is on State Highway 83, on the northern slope of the mountains, the district was about 14 miles north of Pecos. The Pecos mine, which inactive. 126 OCCURRENCE OP NONPEGMATITE BERYLLIUM IN THE UNITED STATES

EXPLANATION

Limestone and sandstone < o Mostly limestone of Pennsylvania!) age in the San Pedro Mountains; mostly sandstone of Cretaceous age in the Ortiz Mountains. Locally metamorphosed to tactife or Aorn/e/s

Intrusive igneous rocks Mostly syenite; some diorite, some rhyolite porphyry sills

Base from U. S. Soil Conservation 106° icy Geology compiled by W. T. Holser from Service planimetric map unpublished maps by J. F. Smith, Jr., and A. H. Wadsworth, Jr., U. S. Geological Survey IMite (San Pedro Mountains) and by C. T. Griswold, Ortiz Land Grant Co. (Ortiz Mountains) FIOUBB 36. Geologic map of the New Placers and part of the Old Placers districts, Santa Fe County, N. Mei, LOCALITIES IN NEW MEXICO 127 The geology of the district was described by Yung TABLE 57. Beryllia in samples from the New Placers district and McCaffery (1903) and by Lindgren (Lindgren, Continued Graton, and Gordon, 1910, p. 170-174). The major Sample Description (pe~*jenf) 336 Grab sample of gamet-epidote tactite at geologic features are shown in figure 36. The sedi­ face of New Placers adit______<0 0004 mentary rocks in the San Pedro Mountains consist of 340 Grab sample of 1-ft quartz vein and asso­ ciated quartz-garnet tactite of the "50 about 1,500 feet of flat-lying limestones, shales, and beds"(?;, near Montezuma shaft-___ <. 0004 sandstones of the Madera formation (Pennsylvanian) 341 15-ft channel sample of garnet tactite with copper stains, from the "50 beds" at Vir­ In the western part of the mountains is a laccolithic ginia adit______.____ <. 0004 mass of porphyritic rock that appears to be mainly 342 6-ft channel sample of garnet tactite with chalcopyrite, from "24 beds" at Virginia syenite and monzonite. Two 60-foot sills that are strati- adit______<. 0004 graphically above and below the laccolith are of 345 Chip sample from outcrop of syenite near its upper contact with Madera forma­ younger rhyolite porphyry. The small intrusive tion, west of the Montezuma shaft.__. . 0004 bodies in the eastern part of the mountains are diorite. Near the laccolith and beneath the upper rhyolite OLD PLACERS DISTRICT sill, shale is altered to hornf els and limestone to tactite. The Old Placers district, also known as the Dc^ores Garnet is the most common mineral in the tactite, but or Ortiz district, is in the Ortiz Mountains just north diopside, feldspar, quartz, specularite, epidote, ido- of the New Placers district. It is east of State High­ crase, and wollastonite are also present. Some of the way 10 and is accessible by several unimproved roads limestone has been changed to coarse white marble. (fig. 36). The district was visited on July 13, 1949. The ore deposits are in the metamorphosed rocks be­ The geology of the region has been briefly described tween the laccolith and the upper rhyolite sill. The by Yung and McCaffery (1903) and by Lindgren (Lind­ chief ore mineral is chalcopyrite. It is disseminated, gren, Graton, and Gordon, 1910, p. 167-170). Mr. C. T. along with some scheelite and molybdenite, in the tac­ Griswold of Albuquerque, N. Mex., who has worked in tite and marble. the district for several years, furnished further I** for­ Samples were taken at most of the mines in the dis­ mation on the geology of the Ortiz Mountains. trict, as shown in figure 36. The samples are described Sedimentary rocks, mainly the Mancos shale of Cre­ in table 57. taceous age, are invaded by intrusive igneous bodies which, according to Griswold, are thick sills. Mc-^t of TABLE 57. Beryllia in samples from the New Placers district the igneous rocks are granular and composed of l^rn- [Spectrographic analyses by Janet D. Fletcher. BeO figures determined on plates exposed for general scanning but not for precise determination of BeO alone] blende and andesine, but the composition varies con­ BeO siderably ; some are porphyritic. These rocks were called Sample Description (percent) 329-323 6-ft channel sample of very coarse marble syenite porphyry by Yung and McCaffery (190S, p. from "lower 50 bed" in Home tunnel . <0. 0004 324 6-ft channel sample of garnet tactite, with 351), essexite, diorite, dacite, and andesite by Ogilvie chalcopyrite, from Swan tunnel at west (1908, p. 230), and quartz monzonite, monzonite, and side Richman shaft_____.-_-______<. 0004 325 6-ft channel sample in garnet-calcite tac­ diorite by Lindgren, Graton, and Gordon (1910, p. 40). tite, with chalcopyrite, from Swan tunnel Near the Black Prince (Old Keliable) and Pat Col- workings______<. 0004 326 6-ft channel sample of garnet tactite from lins claims (fig. 36) along Alpine Gulch, most of the Swan tunnel workings____-___--______<. 0004 328 5-ft channel sample of garnet-calcite from Mancos shale has been metamorphosed to hornfels, and Swan tunnel workings-____--_-______- <. 0004 locally it is completely altered to a coarse garnet tactite 333 4-ft channel sample of garnet tactite re­ placed by copper, iron, and manganese containing chalcopyrite, pyrite, and gold. Tactile oc­ minerals, in "24 beds" (?), upper part of Spanish opencut______<. 0004 curs also in the next canyon north and on the Buckeye 334 Chip sample of 1.5 ft of garnet tactite re­ claim to the northeast. No tactite is present at the Can­ placed by copper, iron, and manganese minerals, lower part of Spanish opencut. <. 0004 delaria mine, the largest in the area.

FIGURE 36 Continued MINUS AND LOCALITIES SAMPLED 1. Buckeye 7. New Placers adit 329-836 12. Home tunnel 329-323 2. 329-350 8. 329-345 13. Richman shaft 3. 329-349 9. Virginia adit 329-341 and -342 14. Swan tunnel 4. Black Prince 10. Montezuma shaft 329-340 829-324 to -320, -328 (Old Reliable) 329-353 11. Spanish opencut 15. Carnahan 5. PatCollins 329-338 and -334 16. Lazarus 6. Candelaria 128 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES Samples of the igneous rocks and tactite that were don (Lindgren, Graton, and Gordon, 1910, p. 260-266). analyzed are described below; localities sampled are The sedimentary rocks are limestone of the Magdalena shown on figure 36. group (Pennsylvanian) and Abo sandstone (Permian), Sample Description which dip eastward on the lower slopes of the range. 329-349 Specimen of leucocratic pyroxene syenite (?) from They are overlain on the upper slopes by Tertiary vol­ locality 8. canic rocks, including andesite, rhyolite tuff, and brec­ 350 Specimen, of syenite (?) from main intrusive body cia. No intrusive rocks are exposed in the district, the at locality 2. nearest being a large monzonite sill in tin Cuchillo 353 6-ft channel sample of garnet tactite from opencuts Negro Eange several miles east of Winston. North- on Black Prince claim. 359 Specimen of porphyritic intrusive rock from road cut trending normal faults slice the eastern part of the where State Highway 10 turns northeast across range into long narrow blocks that are dowrthrown on Ortiz Mountains (not shown on fig. 36). the east; cross faulting is common. These samples do not contain as much as 0.0004 per­ Most of the veins are fissure fillings in ardesite, but cent BeO. some are traceable into underlying limestone. The SIERRA COUNTY principal metallic minerals are pyrite and chalcopyrite, with associated gold and silver. The gangr^ minerals APACHE NO. 1 DISTRICT are quartz and calcite, with some barite. The veins The Apache No. 1 (Chloride) district is on the east show delicate banding and crustification. Harley slope of the Black Eange, a few miles southwest of (1934, p. 76) classified the deposits as epithe^mal. the old mining camp of Chloride (fig. 37). Production Samples were taken only at the Midnight mine, amounting to less than a million dollars has been where small amounts of garnet and epidote had been reported (Harley, 1934, p. 85). The vein is principally quartz with some calcite and fine-grained epidote. Limestone on the footwall is marmorized and silicified; greenish sandstone forms the hanging wall. Ore on the dump contains bornite and copper carbonates. A sample (329-705) cut across the vein at tin collar of 33°20' the south shaft contains less than 0.0004 percent BeO, but a grab sample (329-706) of copper-rich ore from the dump contained 0.01 percent BeO. Further sam­ pling is needed to determine the nature and extent of the beryllium-bearing material.

CUCHILLO NEGRO DISTRICT The Cuchillo Negro district, which is south of State Highway 52 -in the Cuchillo Negro Mourtains, was visited on August 21,1949. The geology, a' described by Harley (1934, p. 113-125), is similar to that in the Apache district a short distance west in th*,t an east- wardly dipping section of about 1,500 feet of limestone of the Magdalena group (Pennsylvanian) is overlain by Tertiary volcanic rocks. A thick sill of monzonite porphyry about 8 miles long intrudes the limestone, which has been replaced along fractures by garnet, 33°15' epidote, and quartz, accompanied by galena, sphalerite, chalcopyrite, and oxidation products. FIGURE 37. Index map of the Apache mining district, Sierra County, N. Mex. Samples were taken in the vicinity of iH Sentinel (Dictator) mine, which is reached by a ro^d turning mainly in gold, silver, and copper. The district was south from State Highway 52, about 2 mf^s west of visited on August 21 and 22,1949, and there was little the HOK ranch. The mine is described in detail by mining activity at that time. Harley (1934, p. 120-123). A grab sample (329-700) The geology and mineral deposits of the area have of galena-sphalerite-calcite ore from the dump of the been described by Harley (1934, p. 73-77) and by Gor­ Sentinel adit contained 0.001 percent BeC. Sample LOCALITIES IN NEW MEXICO 129 329-701 from the same dump was composed of garnet, 1944a, p. 76). Recovery of the beryllium invo1ves epidote, quartz, and calcite, and contained 0.0007 per­ rather complex mining and metallurgical problems, and cent BeO. there has been no production. Results of flotation ex­ A sample (329-702) of highly altered rock from the periments conducted by the U. S. Bureau of Miner on monzonite next to its contact with the marble at the similar ores (Kennedy and O'Meara, 1948) suggest Sentinel shaft contained 0.0005 percent BeO. The area that ultimately the problems may be surmounted. to the north and west of the Sentinel mine, including the Silver Bell mine, was also inspected, but no other SOCORRO COUNTY tactite bodies of any. consequence were found. JONES CAMP DISTRICT Although the geology of this district is somewhat Jones Camp is on Chupadera Mesa in eastern Socorro similar to that at Iron Mountain immediately to the County, north of U. S. Highway 380. The area was north, the ore bodies are small and the beryllium con­ not visited, but a specimen of tactite from one of the tent of the tactite is apparently low. deposits was obtained from V. C. Kelley. IRON MOUNTAIN DISTRICT The geology of the district has been described in de­ Pyrometasomatic deposits containing beryllium and tail by Kelley (1949, p. 213-222). Chupadera Mes*. is tungsten occur in an area of about 15 square miles, capped by sandstone, limestone, and gypsum bedr of largely in northern Sierra County but extending into the San Andres and Yeso formations of Permian age. southern Socorro County. The deposits were studied An anticline in these rocks is intruded by a dike that and sampled in detail by the U. S. Geological Survey trends northwest along the fold axis for about 10 and the U. S. Bureau of Mines during 1942-43 (Jahns, miles. The dike is complex, consisting mainly of mon­ 1944a, 19Mb; Glass, Jahns, and Stevens, 1944; Storms, zonite and syenite, with some later but closely asso­ 1947). The district was visited briefly on August 22, ciated diabase. A narrow and irregular metamorphic 1949, in connection with the present investigation. zone composed of actinolite, tremolite, and magnetite Little development work had been done since 1943, and occurs in the sedimentary rock along the dike. The further sampling was regarded as unnecessary. magnetite ore bodies replace actinolite rock, diabase, Iron Mountain is a narrow north-trending fault block and limestone. composed mainly of eastward-dipping rocks of late A specimen (sample 329-809) of actinolite tae*ite Paleozoic age of the Magdalena group and Abo sand­ from the contact of the diabase dike in trench 9 (Kel>y, stone. To the east, these rocks are overlain by Cretace­ 1949, fig. 44) contains less than 0.0004 percent BeO. ous sedimentary rocks which are in turn overlain by TAGS COUNTY several thousand feet of Tertiary volcanic rocks. Sills, dikes, and pluglike bodies of monzonite, rhyolite, gran­ RED RIVER DISTRICT ite, and aplite cut the sedimentary rocks and part of The Red River district is on the western slope of the the volcanic series. The sedimentary rocks in 4;he Iron Sangre de Cristo Mountains and is crossed by State Mountain block were contact-metamorphosed next to Highway 38. The district was visited on August 30- the intrusive bodies, and some of the more calcareous September 1,1948. E. C. Anderson and P. F. MeEin- rocks were altered to tactite, particularly at the north­ lay of the New Mexico Bureau of Mines, who accom­ ern end of the block. panied the party, suggested areas for sampling. Two main types of tactite are recognized: a massive, The geology of the district was described briefly by garnet-rich tactite and a banded tactite, or "ribbon Graton (Lindgren, Graton, and Gordon, 1910, p. 84- rock." The massive tactite is locally rich in magnetite 88) and the Questa mine was described by Larsen and or fluorite, and parts of it contain sufficient scheelite Ross (1920) and by Vanderwilt (1938). More recent and powellite to be valuable as tungsten ore. The "rib­ work by the New Mexico Bureau of Mines and the bon rock" consists mainly of magnetite, hematite, and U. S. Geological Survey (Park and McKinlay, 1948a, fluorite, with some garnet, diopside, idocrase, and other 1948b) deals only with the part of the district south­ silicates. It contains virtually all of the beryllium, east of the area sampled. mainly in helvite but some in grossularite, idocrase, The Precambrian rocks of the district include horn­ chlorite, and other minerals. blende gneiss, schists, and quartzite that are intruded Beryllium reserves of the district amount to 3,500 and locally replaced by granite. Conglomerates, shales, tons of indicated ore and 1,000 tons of inferred ore, both limestone, and sandstones belong at least in part to the containing an average of 0.7 percent BeO, and 84,000 Magdalena group of Pennsylvanian and Permian f £e. tons of indicated ore and 100,000 tons of inferred ore These rocks are intruded by stocks and sills that range thought to average about 0.2 percent BeO (Jahns, in composition from granodiorite and monzonite to 467945 59 10 130 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES granite. Later intrusions and flows of andesite and plateau is at an altitude of 3,500 to 5,000 fret and is rhyolite cover much of the area. The structure is com­ bounded on the west and south by Rio Granie valley, plex. on the east by Salt Basin, and on the north by the Sac­ In general, hydrothermal alteration has been intense ramento Mountains. The edges of the platear are char­ in the district, particularly in the granodiorite west of acterized by a rough scarp topography resulting from Bed River. At this locality quartz-gold veins occur headward erosion of tributary streams into flat-lying both in the granodiorite and in overlying volcanic sedimentary rocks. Laccoliths, plugs, dikes, and sills rocks. In places along the granodiorite contact, as at of more resistant igneous rock form erosion remnants the Hornet mine on Cabresto Creek, some galena and that are prominent features of the landscape. sphalerite occur with garnet and other tactite minerals. Early reconnaissance surveys by Baker- (1927), The Questa mine is near the edge of a small granite Beede (1918), and Richardson (1904,1909,1914), and stock and explores quartz veins containing molybdenite, recent work by King and others (King, 1948, 1949); fluorite, pyrite, and rhodochrosite. The granite and King, Branson and others (1949); King, Fing, and sedimentary rocks nearby are almost entirely altered to Knight (1945); King and Knight (1944); A dams and chlorite and clay in the vicinity of the mine. others (1949); and Smith and Albritton (1949) em­ Most of the sampling was confined to the molyb­ phasized the sedimentary rocks and their structure. denum-rich area between Red River and Questa; the Huffington (1943) described in detail the igneous rocks samples are described in table 58. The analytical re­ of the Quitman Mountains and Clabaugh 7, Timm 8, sults indicate that the molybdenum-bearing veins and and Zapp 9 made detailed studies of the igneous rocks altered granitic rocks contain small quantities of beryl­ of the Cornudas Mountains, lium, though probably not enough to be recoverable by Most of the Diablo Plateau is underlain by flat-lying present methods. limestone of Permian age that unconformaWy overlies older Paleozoic and Precambrian rocks. T?*ese rocks TABLETS. Beryllia in samples from the Red River district are exposed only along the eastern margin of the [Quantitative spectrographic analyses by A. A. Ohodos] BeO plateau where they have been upthrown by faulting and Sample Description (percent) folding. Cretaceous and Jurassic sedimentary rocks 329-214 Grab sample along 6 ft of outcrop of 6-in. fluorite vein in rhyolite, Chokecherry crop out in the southwestern part of the plateau and Canyon, 3 miles east of Questa ______0. 0007 are complexly folded and faulted. The sedimentary 221 Grab sample of highly altered monzonite on the north side of Red River Canyon, rocks were intruded by laccoliths, plugs, sills, and dikes 3 miles west of Red River______<. 0003 of alkalic igneous rocks, probably of early Tertiary age. 222 Grab sample of yellow clay from same alteration zone as sample 22!_____-___ <. 0003 In most places, contact metamorphism ani metaso­ 223 Sample of heads from molybdenum ore run August 31, 1948, Questa mill..._ . 002 matism have been slight, although rather extensive 226 Specimen of rich molybdenum ore from zones of marble, hornfels, or tactite were formed Questa mine_____.______. 001 227 4-ft core of tailings pile at Questa mill__ . 004 around a few of the intrusive bodies. 233 Specimen of alaskite, with molybdenite Samples of igneous and contact-metamorphosed veinlets, from dump of Questa mine__ . 001 234 Specimen of coarse granitic rock, with rocks collected during an earlier trace elemerts investi­ molybdenite veinlets, from dump of gation by the U. S. Geological Survey from Cave Peak, Questa mine.______. 0005 236 4-ft channel sample of molybdenite vein, Culberson County, Tex., and Wind Mountain, Otero 200 ft inside north tunnel of BJB mine, County, IST. Mex., were reported to contain as much as 3^ miles east of Questa______. 0005 237 Grab sample of garnet-rich galena-sphal­ 0.3 percent BeO. The igneous rocks of the Trans-Pecos erite ore from dump of Hornet mine, Region were known to include feldspatho;dal types north side of Cabresto Creek 7 miles east of Questa______._ . 0008 that, on theoretical grounds, are likely to contain beryl­ 238 Channel sample across 10-ft vein of quartz, lium-bearing minerals. The region was, therefore, calcite, pyrite, and galena, between granodiorite and quartzite, at upper marked for special study during the present investiga­ tunnel of Hornet mine______. 0003 tion. TRANS-PECOS REGION, TEXAS AND NEW MEXICO During August 1948, the Cave Peak and Wind Moun­ tain areas were studied and resampled by Holser and By W. T. HOLSER Wilmarth. Detailed geologic maps were m^de of the INTRODUCTION beryllium-bearing localities in these areas by Polser and The study of beryllium-bearing rocks in the Trans- 7 Clabaugh, 8. B., 1941, Geology of the northwestern Co-nudas Moun­ tains, N. Mex.: Univ. Texas M. Sc. thesis. Pecos Region was restricted to the relatively flat and 8 Timm, B. C., 1941, Geology of the southern Cornudrs Mountains, barren Diablo Plateau in Hudspeth, Culberson, and El Texas and New Mexico: Univ. Texas M. Sc. thesis. 8 Zapp, A. D., 1941, Geology of the northeastern Cornudas Mountains, Paso Counties, Tex., and Otero County, N. Mex. This N. Mex.: Univ. Texas M. Sc. thesis. LOCALITIES IN TRANS-PECOS REGION 131 W. I. Finch in July 1949. A general reconnaissance Phenocrysts of perthitic feldspar, as much as 1 inch was made of the other intrusive igneous rocks in the long, constitute most of the rock. Smaller crystals of region. P. B. King, Earl Ingerson, Charles Milton, perthitic feldspar, nepheline, analcite, aegirite, and and J. F. Smith of the U. S. Geological Survey supplied minor amounts of biotite form the groundmass. Both the field party with information about several of the the large and small perthitic feldspar crystals sh^w a areas visited. pronounced orientation caused by flow. The border phase of this rock is darker, finer grained, and norpor- INTBUSIVB IGNEOUS BODIES AND CONTACT ZONES phyritic. Similar porphyritic syenites form the intru­ Most of the intrusive igneous bodies of the Diablo sive bodies at Cornuda Mountain, (jfranite Mountain, Plateau are small, ranging from laccolithic masses as and Hueco Tanks. The norm of these rocks contains no much as 3 miles in diameter, and sills as much as 1,500 nepheline, and none was seen in thin section. feet thick, to dikes less than a foot thick. The majority The coarse-grained syenite of Marble Canyon in the of the rocks are alkalic; most are silica-rich, but many Sierra Diablo, according to Charles Milton (1941, are feldspathoidal. With few exceptions they are suf­ written communication), contains more than 50 percent ficiently similar in composition to suggest that they sodic plagioclase that is intergrown perthitically with represent a petrographic province. The highly de­ some potassium feldspar. Highly altered hornblende formed Quitman Mountains are included in the Trans- and biotite are the only mafic minerals. ' About 6 per­ Pecos Kegion for convenience although their struc­ cent quartz is graphically intergrown with the feldspar. tural setting and granitic rocks are more nearly com­ The boarder phase of this syenite is a finer grained parable with the mountains of the Arizona and New mela-syenite. Mexico region. They contain some syenitic rocks which Subsidiary intrusive bodies are remarkably lacking are common in the Trans-Pecos but unknown in the around and in most of the large syenite masses. Most Arizona and New Mexico region. of the intrusive bodies are single masses of rock that The areal extent of the intrusive igneous rocks in the have sharp boundaries with the surrounding sedim^ts. Trans-Pecos Kegion is shown in plate 1. The general The intrusive mass at Marble Canyon, however, 1 *s a distribution is peripheral to the Diablo Plateau. Most number of associated aplite dikes and one neph^Iine of the intrusive bodies were examined, and many sam­ syenite dike. The main intrusive mass at Wind Moun­ ples of the igneous and associated metamorphic rocks tain is surrounded by numerous small dikes and sills, most of which are medium-grained, dark aegfrite- were taken. Brief descriptions of the bodies, the con­ tact zones, and the samples collected are given, together nepheline rocks (malignite); some are feldspar-rich and are coarse grained or pegmatitic in texture. The with analytical data, in table 59. Little beryllium is only other dike rocks seen along the many mile^ of indicated in these rocks, except at Wind Mountain and igneous contact examined were a few thin phonolite Cave Peak. dikes at the southern contact of the intrusive boc'y at SYENITIC ROCKS Sierra Prieta. It may be significant that the dike rocks Syenites are common in the region, particularly in apparently are associated only with the coarse-gra ined the northern part (table 62). The most characteristic porphyritic syenite intrusive rocks. rock is a fine-grained, dark gray-green syenite contain­ ing small phenocrysts of feldspar. Its principal min­ GRANITIC ROCKS erals are sodic plagioclase and sodic pyroxene; the Granitic rocks are found in the intrusive mass^ in pyroxene ranges in composition from aegirite to the Quitman Mountains, Wylie Mountains, Sierra augite. Potassic feldspar, sodic amphibole, and biotite Blanca, Cave Peak, and Sierra Diablo. Mos1; of are less abundant. Many of the syenites contain small the Quitman Mountains mass is a medium-grained subhedral crystals of analcite or nepheline in the quartz monzonite that contains orthoclase, oUgo- groundmass. Several of these intrusive rocks, such as clase, biotite, and small grains of quartz. G~an- those at Alamo Mountain, Sierra Tinaja Pinta, and ite occurs in the southwestern part of the irtru- Sierra Prieta, have a finer grained, dark schistose bor­ sive mass (Huffington, 1943, p. 1035) and locally rocks der phase just above the basal contact. The structure are syenitic. Small diorite xenoliths are present ir the parallels the contact in most places and is the result of quartz monzonite. In the Wylie Mountains ani at orientation of the dark minerals by flow. Sierra Diablo the granitic rocks occur next to intrrsive A less common coarse-grained and porphyritic sye­ syenitic rocks. The central part of the intrusive mass nite forms the main intrusive masses of the Wind Moun­ at Cave Peak is composed of granite, associated with tain, Little Wind Mountain, and Black Mountains. rhyolite porphyries and breccias. 132 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES s § i I M o o o o o o o V V V

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i 5 i 1o S o , i»> *£ 1 15 1 " CQ § 1 1 I> '.* '§ a f o3 o iO O ^ !.1£ 3 S >0 pj MOUNTAIN AREA Wind Mountain, thin-bedded light-colored shales are exposed in the Hueco limestone. Wind Mountain, in Otero County, N. Mex., is one of The most prominent structure of the sedimentary the largest intrusive masses of the group that form the rocks is their doming near the laccolith where the beds Cornudas Mountains of Texas and New Mexico (pi. 1). dip at angles of 50° to 80° and generally are parallel The area is most easily accessible by a graded road that to the contact/ The effect of the doming may be de­ turns north from U. S. Highway 62-180 at the Hueco tected as far as 2,000 feet from the laccolith. Inn, 50 miles east of El Paso, Tex. Wind Mountain is Metamorphism of the sedimentary rocks next to the reached by a graded road that leads south from Cornu­ intrusive body at Wind Mountain is variable ir both das Ranch to Wind Tank. extent and intensity. Bleaching and recrystallization The geology of the area was studied by Zapp 10, who of the limestone beds has been developed on the eastern discovered eudialite-bearing syenite dikes on the west­ side through a thickness of more than 100 feet (pi. 4), ern side of Wind Mountain; the eudialite was later de­ but elsewhere the limestone is unmetamorphosed. The scribed by Clabaugh (1950). In 1944 members of the U. S. Geological Survey sampled some of the eudialite- shale beds of the Hueco limestone, where observed near the intrusive mass, are altered to a fine-grained 1 ~own bearing dikes and associated rocks for trace elements. One of the samples was reported to contain 0.2 percent to purple hornfels, but probably very little material BeO (Fleischer and Cameron, 1946). The area was ex­ was added from the intrusive body. At some localities, amined briefly in August 1948 and was studied more however, the metamorphism was accompanied by addi­ thoroughly in July 1949. The earlier geologic map " tion of soda and other substances. Narrow bards of aegirite, riebeckite, analcite, and zirconium silicates 10 See footnote 9, page 130. border many of the dikes. At one area on the south 11 See footnote 8, page 130. side of Wind Mountain (pi. 3) metasomatism was CO R. 14 E.

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Datum is mean sea level FIGUEB 38. Geologic map of Wind Mountain, Otero County, N. Mez. LOCALITIES IN TRANS-PECOS REGION 137 intense, and the sedimentary rocks are altered to a malignite, pegmatitic nepheline syenite, and fine­ coarse tactite of epidote, calcite, and garnet. grained nepheline syenite. Commonly there are only a few such layers, but at one locality (sample 329-145, IGNEOUS BOCKS pi. 3) 25 major layers and many minor ones occur in a The main mass of Wind Mountain is porphjritic zone about 12 feet thick. Although some of the layers nepheline syenite, containing euhedral to subhedral are continuous for 20 feet or more, the pegmatitic phenocrysts of nepheline, perthite, and pyroxene in a nepheline syenite layers are commonly short and len­ fine-grained groundmass of 80 to 90 percent feldspar ticular. In other places masses of pegmatitic nepl eline and 10 to 20 percent aegirite. Nepheline phenocrysts syenite are cut by malignite, and locally the rock re­ constitute as much as 15 percent of the rock and com­ sembles a breccia of pegmatitic material "cemented" by monly shows large crystal faces. The perthite pheno­ malignite. In thin section the malignite layers show crysts show a marked flow structure in which their a pronounced orientation of aegirite prisms parallel to tabular (010) form is parallel to the contact. Adjoin­ the layering. The orientation is apparently the result ing and within a few hundred feet of the contact, the of flow, and the lines of crystals crowd and bend nepheline syenite has a granular texture. Phenocrysts sharply around feldspar phenocrysts. Most of the peg­ are small or absent, and no alinement of crystals is ap­ matitic nepheline syenite dikes lack this structure but parent. Pyroxene, dominantly aegirine-augite, is pres­ the long axes of feldspar crystals near the dike margins ent in minor quantities and is interstitial to the feld­ commonly are perpendicular to the walls. Some c f the pegmatitic nepheline syenite dikes are zoned. The zon­ spar crystals. Porpliyritic rock having flow structure ing is mainly textural, although the inner unit com­ crop out high on the mountain and within 100 feet monly is somewhat richer in aegirite. Planar flow seem to grade into the granular syenite of the border structure is well developed in a dark-gray, gnei^soid f acies. No crosscutting relations or sharp contacts be­ nepheline syenite that crops out on the south side of tween these rock types were seen. Wind Mountain (pi. 3). Perthite phenocrysts and The dikes that border the laccolith are highly variable albite crystals in the groundmass show orientatior. in composition, but two types predominate. The more abundant is dark-green malignite that consists mostly The junction of a vertical dike and a flat-lying dike of aegirite, with some nepheline and feldspar. This is exposed on the Wind Mountain claim (pi. 2). Flow rock is generally fine grained, although in places the lines show that the dikes were formed at the same time. aegirite crystals are as much as half an inch long, and Malignite and similar rocks are found near contact of elsewhere, rectangular phenocrysts of nepheline as much both the porphyritic and granular nepheline syenite as a quarter inch across are scattered throughout the bodies with the laccolith. Their shape ranges from groundmass. The other main type of dike rock is large­ vague schlieren to sharply bounded dikes, but always ly pegmatitic nepheline syenite; it is rich in feldspar and in the same orientations. On the southern side of the contains some nepheline and aegirite. The rock is coarse mountain (pi. 3) near sample 329-622, the granular grained and in places shows tabular feldspar and pris­ syenite of the laccolith grades imperceptibly into fine­ matic aegirite crystals 1 to 2 inches in length. All grained syenite of a dike, and the malignite layers are gradations between malignite and pegmatitic nepheline similarly alined through both rocks. These observa­ syenite may be seen in a single hand specimen. Other tions suggest that all the rock types are closely related dike rocks, similar in composition to the pegmatitic in age and origin. nepheline syenite but finer and more uniformly grained, The most abundant minerals of the dike rocks are are designated as fine-grained nepheline syenite. These feldspar, aegirite, and nepheline. The feldspars include may be as light-colored as the pegmatitic type, or con­ perthitic orthoclase, albite, and minor quantities of siderably darker; however, the content of mafic min­ microcline. The aegirite ranges toward augite in com­ erals is less than that of malignite. The best exposures position; the outer zones of the crystals are richer in of fine-grained nepheline syenite dikes are along the soda. eastern border of the laccolith (pi. 4). Deep red-purple zirconium silicates are important A few dikes with easterly trend occur largely within constituents in some dikes and occur both in single the laccolith. They are dark green and porphyritic, crystals 0.5 to 3 mm in diameter and in aggregates1 In with fine-grained groundmass, and contain inclusions of places they constitute as much as 20 percent of the peg­ limestone and nepheline syenite. The rock is best de­ matitic nepheline syenite. The crystals are grouped in scribed as a phonolite porphyry. irregular stringers and tend to be most abundant near Some of the dikes show a pronounced planar struc­ the edges of pegmatitic layers; a few masses occnr in ture parallel to the walls, owing to interlayering of adjacent malignite. 138 OCCURRENCE OP NONPEGMATITE BERYLLIUM IN THE UNITED STATES The zirconium silicates are highly variable in optical of analcite and other zeolite minerals; these minerals properties and in chemical composition. Purple-red also replace some of the primary minerals. crystals from the western part of Wind Mountain com­ OCCURRENCE OF BERYLLIUM monly are color zoned about a light-brown core. Other The distribution of beryllium in the rockp of Wind crystals are entirely light to dark brown, some occur­ Mountain is shown on the detailed geologic maps (pis. ring in the same rock with the purple-red material. 2-4); a few other analyses are shown on tH general Some of the brown material and much of the red mate­ map of the Wind Mountain area (fig. 38). The sam­ rial is isotropic and has a refractive index of about 1.59; ples are described in table 61. other brown grains show a small negative optic angle The malignite and pegmatitic nepheline syenite dike and indices near 1.62. Spectrographic analyses of three rocks of Wind Mountain are richer in beryllium than is specimens from Wind Mountain are compared in table the porphyritic nepheline syenite that formr the main 60 with a chemical analysis of similar material from part of the laccolith. A channel sample acres s a typical Kola,U.S.S.B. dike, including both malignite and pegmatitic neph­ eline syenite layers, probably would contain about TABLE 60. Analyses of zirconium silicates, in percent 0.007 percent BeO. In some samples no BeO could be i 4 BeO ------0. 0051 0. OOX Present detected, and the maximum BeO content obtained was SiO2 ...... -_._ 51.6 52. 12 0.2 percent. This value was reported for a sample .X .40 FeaOa - - - X.O .73 (S-150-456) collected for the Mine, Mill, ari Smelter Nb ... ----- .53 .X Survey in 1944 from the Wind Mountain claim (pi. 2). TiOa-.- ....-___ .20 .X ..... 2.7 .OX .ox .76 Reanalysis of the same powder, showed only 0.074 per­ Mo. ------.oox cent BeO. Even this value could not be confirmed in Sn_...... ox FeO _ ...... __-_ 2.2 (2) several other samples from the same outcroi (S-150- HfOi . 1 457 and -458; and 329-195 to -205), which gr»ve a max­ 2.0 X. 0 ^>1 3.46 ZrOi...... 11.8 >x.o VO 16.54 imum of 0.026 percent BeO and a minimum of <0.001 .X .X percent (pi. 2 and table 61). CU ------.ooox .oox Na2O. 142 .X 3.74 Although part of the discrepancy may be due to UO2 ------.2 analytical errors, these analyses indicate that the beryl­ CaO--._ -..--- 141 X. 0 V.J.J 3.34 .X .X lium content of the dikes and the altered rocks that Ce...... 56 border them is probably quite erratic. This is further SrO ______. .ox .06 .ox .oox indicated in comparing the analyses of samples from KiO ...... given rock types. The BeO content in 5 samples of Ba------.oox H20+._ ... a 62 fine-grained nepheline syenite ranges from 0.001 to H2O-- ... 6.41 0.022 percent, and in 7 samples of rock that is domi- Cl..- ..... None i Included In MgO. nantly malignite the range is from <0.001 to 0.03 per­ » Included in FeaOj. cent. Of the 10 samples of metamorphic rocks that 1. Purple-red eudialite, west side Wind Mountain. Spectrcgraphic analysis by Saratoga Laboratories, courtesy 8. £. Clabaugh; Univ. of Texas, Austin. were analyzed, those containing detectable amounts of 2. Same mineral, same locality as No. 1 (sample 329-129). Speetrographto analysis by K. J. Murata. Looked for but not found: Ag, As, B, Bi, Cd, Co, Cr, Oa, BeO were all taken within a foot of a dike. However, Oe, In, Ni, P, Sb, Ta, Tl, V, W, Zn. 3. Brown zirconium silicate, south side Wind Mountain (sample 329-145B). Spec- beryllia could not be detected in some sanples thus tographic analysis by K. J. Murata. 4. Lovozerite, Lovozero, Kola, U. 8. S. B. (Gerasimovsky, 1939, p. 754; see also Win- located. chell, 1951,p. 464). Chemical analysis by T. A. Burova, spectrographic analyses fcr U and Hf by I. B. Borovsky, fcr Be oy 8. A. Borovick. Analytical data for the various minerals indicate that the beryllium in the dike rocks is not contained X-ray diffraction patterns of the zirconium silicates in any particular mineral but is distributed among the at Wind Mountain are similar to those of eudialite and feldspar, nepheline, aegirite, and eudialite. Red-pur-i eucolite from southern Norway and Greenland. Min­ pie eudialite from the west side of Wind Mountain erals previously identified as eudialite and eucolite have was found to contain 0.0051 percent BeO (table 60, a wide range of chemical composition (Winchell, 1951, column 2). A sample (329-145) of layered dike rock p. 453-454:). The Wind Mountain specimens differ was separated into mineral components by heavy from these minerals mainly in containing more cal­ liquids, and a spectrographic analysis was made for cium and less zirconium, but are probably members of each of the separates. The aegirite separate contained a eudialite-eucolite series. O.OOOX BeO, the zirconium silicate O.OOX percent, and Other accessory minerals of the dike rocks include the combined nepheline and feldspar 0.003 percent. sodalite, riebeekite, biotite, apatite, and magnetite. Two separate quantitative analyses of pa*ts of the Some of the dikes are intersected by microscopic veins sample showed 0.0074 and 0.001 percent BeO, neither LOCALITIES IN TRANS-PECOS REGION 139

TABLE 61. Beryllia in samples from Wind Mountain [Key to analysts: KJM, K. J. Murata; JDF, Janet D. Fletcher; JTR, J. T. Rczsa, National Speetrographic Laboratories, Inc.; LWS, L. W. Strock, Saratoga Labora*iries, Inc.; MMS: samples collected and analyzed by Mine, Mill, and Smelter Survey. MMSC: gravimetric analysis by Mine, Mill, and Smelter Survey; all other analyses Spectrographic] Plate thow- Sample ing locality BeO (percent) Analyst 329-128 2 Specimen of malignite dike with large nepheline phenocrysts.______0. 014 JTR 129 2 Separate of eudialite from pegmatitic nepheline syenite, near 329-128..______.0051 FJM 132 2 4-f t channel sample across hornfels altered to clay ______<. 004 LWS 135 4 3-ft channel sample across eudialite-bearing fine-grained nepheline syenite dike__ .0065 LWS 136 4 1-ft channel sample across thin eudialite-rich pegmatitic nepheline syenite dike and bordering marble.______._____ .003 JDF 145 3-ft channel sample across lower part of 20-ft dike of banded nepheline syenite pegmatite, fine-grained nepheline syenite, and malignite, containing zirconium silicates _ __j______-___ .0074 145A 3 Separate of aegerite from 329-145______.OOOX 145B 3 Separate of brown zirconium silicate from 329-145.______.OOX 145C 3 Nepheline and feldspar from 329-145______.003 149 3 Specimen of malignite dikes in porphyritic nepheline syenite.______.018 150 3 Grab sample from thin serpentine vein in hornfels______<. 004 151 3 4-ft channel sample across magnetite-bearing hornfels, some altered to clay_____ <. 004 153 (Fig. 38) Grab sample of alteration zone in limestone near northwest corner of figure 38, containing quartz, chalcedony, siderite, and iron and manganese oxides._ ___ <. 001 JTR 156 (Fig. 38) Specimen of 3-in. coarse malignite dike in granular syenite.______.030 JTR 157 (Fig. 38) Grab sample of 6-ft banded dike, predominantly malignite with brown zirconium silicate.______.015 JTR 195 2 Channel sample across 15-in. altered shaly limestone.______<. 001 JTR 196 2 Sample from two 1-ft channels across thin, gray, fine-grained nepheline syenite dike, immediately below 329-195.______<. 001 JTR 197 Sample from three 14-in. channels across black hornfels immediately below 329-196, ______. 026 JTR 198 Broad 1-ft channel sample across limestone, from same locality as 329-197------<. 001 JTR 199 Channel sample across 6 in. of porcelainic limestone, near hanging wall of flat- lying banded dike (329-202) ______<. 001 JTR 200 Chip sample of dark-green aegirite hornfels along hanging wall of same dike as 329-202, ______.______<. 001 JTR 201 2 Same on footwall.______.022 JTR 202 2 Chip sample across flat-lying banded dike, same locality as 329-199 to 201__ . .012 JTR 203 2 Chip sample of vertical banded dike with some very coarse feldspar. Some horn­ fels inclusions.______.001 JTR 204 2 Specimen of granular syenite______-______,______. <. 001 JTR 205 2 Specimen of anthophyllite asbestos lying between dike rock and aegirite hornfels. _ .001 JTR 605 2 5-ft channel sample across banded eudialite-bearing dike______.0068 JDF 607 2 _do______.008 JDF 611 (Fig. 38) Composite of four specimens of porphyritic nepheline syenite from borders of main part of laccolith______.005 FJM 615 3 6-ft channel sample across banded malignite and syenite______._ .0063 JDF 619 3 2.5-ft channel sample across fine-grained nepheline syenite dike______._ .022 JDF 620 3 2-ft channel sample across 'limestone and hornfels at footwall of dike sampled in 329-619. ______.0013 JDF 622 Channel sample across metamorphic rocks at contact porphyritie nepheline sye­ nite, including 10 ft of epidote tactite and 5 ft of calcite marble.___ .001 JDF 631 4 15-ft channel sample across unaltered limestone______.OOOX JDF 632 4 15-ft channel sample across leucocratic fine-grained nepheline syenite _ _ .0072 JDF 633 4 10-ft channel sample across fine-grained nepheline syenite at contact with por­ phyritie nepheline syenite______- .0063 JDF 3 Chip sample across 25-ft outcrop of gneissoid nepheline syenite.______.004 JDF 652 (Fig. 38) Specimen of phonolite porphyry with limestone and syenite inclusions __ .004 JDF S-150-456 2 Chip sample across 0.8 ft of hard altered limestone, with two small eudialite- bearing malignite dikes, same locality as 329-195 to 205______.074 FJM . 14 MMSC .2 MMS 457 Chip sample across 2 ft of eudialite-bearing malignite dike, same locality. <. 001 MMS 458 Chip sample across 6 ft of same type of rock, same locality.---_-- <. 001 MMS

of which can be reconciled with the values obtained for The dikes range in thickness from less than ar inch the mineral separates. Although the accuracy of the to as much as 20 feet and in length from 5 feet to at results may be challenged, some of the discrepancy least 300 feet. Though largely covered by talus they may have resulted from erratic distribution of beryl­ probably are present throughout a zone a few hundred lium in the minerals. An unsuccessful search was feet wide extending around the 5-mile circumference made for the beryllium minerals, such as helvite, eudi- of the Wind Mountain laccolith. Thus, they would dymite, meliphenite, and leucophanite, that occur in represent a substantial reserve if their beryllium could pegmatitic nepheline syenites in southern Norway. be recovered. 140 OCCURRENCE OF NONPEGMATTTE BERYLLIUM IN THE UNITED STATES CAVE PEAK AREA tact, as indicated by a breccia zone several feet thick The intrusive complex at Cave Peak is in the Sierra and slickensides. Diablo, about 35 miles north of Van Horn, Tex., and IGNEOUS BOCKS 2 miles west of State Highway 54 (pi. 1). Though The most abundant rocks are breccias, composed Cave Peak is about 1,300 feet above the alluvial floor mainly of fragments of rhyolite porphyry. Nonbrec- of Salt Basin, it is overshadowed by the cliffs on the ciated felsite, mainly rhyolite porphyry, are less exten­ eastern scarp of the Diablo Plateau. sive in outcrop. The branches are subdivided on the The intrusive rocks of the Sierra Diablo region were basis of color into light rhyolite breccia and c'ark rhyo­ first mapped by Richardson (1914). Later King and lite breccia. The porphyries are similarly subdivided others of the Geological Survey mapped the sedimen­ into light and dark rhyolite porphyry. Field relations tary formations and structures of the region (King suggest that the light rhyolite porphyry is probably the and Knight, 1944; King, 1949). The uncommon igne­ oldest intrusive rock and light rhyolite breccia the ous rocks of the Cave Peak area collected by King were youngest, except for a few late porphyry dikes. The studied by Charles Milton, Earl Ingerson, and others. dark rhyolite porphyry and breccia are of intermediate In 1944 the Cave Peak area was sampled by A. L. age, the breccia being somewhat the younger of the two. Slaughter for the Mine, Mill, and Smelter Survey. The central core of granite appears to be younger than Two samples from one of the prospect pits contained the dark rhyolite. 0.3 to 0.02 percent BeO. Because of the unusual Light rhyolite porphyry occurs as dikes and irregu­ quantity of beryllium reported in these samples, the lar masses mainly in a zone about 400 feet wide around geology in the vicinity of Cave Peak was mapped in the southern end of the intrusive mass (pi. 5). The detail during the present investigation (pi. 5). rock is largely greenish gray and is aphanitic except

GEOLOGY for scattered phenocrysts of feldspar and quartz as much as 3 mm in diameter. It weathers light gray. In The igneous rocks of Cave Peak form an intrusive places other varieties of felsite are associated with the complex that is nearly circular in outline and about half light rhyolite porphyry and were undifferentiated from a mile in diameter. The rocks are mainly light and it in the mapping. In several outcrops on the south­ dark rhyolite porphyries and breccias. The central eastern slope of Cave Peak and in the large outcrop on core of the complex is a plug of porphyritic granite the western ridge, the rhyolite contains no pHnocrysts, about 300 feet in diameter. The complex resembles a but it is otherwise similar to the porphyry ard appears volcanic neck but no lavas are found in the region. The to grade into it. Locally the rock contains no quartz ringlike structure of the various rock types around a and is probably trachyte or andesite porphyry. core of granite (pi. 5) suggests that the pluton intruded The dark rhyolite breccia and porphyry are best ex­ almost to the surface. posed in a circular area on the northern slope of Cave Porphyritic syenite that is more like the igneous Peak. The dark-gray to black, fine-grainei rhyolite rocks found elsewhere in the Trans-Pecos Region forms porphyry contains abundant feldspar and a few quartz the intrusive mass at Marble Canyon, a mile southwest phenocrysts about 2 mm in diameter. Microscopic ex­ of Cave Peak. The relation of this mass to the complex amination by Charles Milton indicates that tH feldspar at Cave Peak is not known. is a slightly albitized orthoclase, and that tlci ground- Most of the sedimentary rocks intruded at Cave Peak mass is orthoclase, quartz, biotite, and a little sphene are dark-gray, thick-bedded limestones of the Hueco (P. B. King, 1948, written communication). The dark- limestone (Permian). Near the southwestern side of gray rhyolite breccia is composed largely of randomly the intrusive body, the Hueco limestone grades upward oriented angular fragments as much as 2 cm in diam­ into the black limestone of the Bone Spring limestone eter. Some of the fragments are similar to the dark (Permian). The formations are similar in appearance rhyolite porphyry. The inclusion of porphyry frag­ and were not differentiated in mapping. The limestone ments in the breccia indicates that the breccia is near its contact with the intrusive mass is largely calcite, younger. but some beds are dolomitic. The rocks dip 2° or 3° Near the contact of the dark rhyolite porphyry with to the south over much of the area, but are highly de­ the porpyhritic granite, the porphyry is brecciated, formed within a few feet of the intrusive mass. Where silicified, highly altered, and crisscrossed by innumer­ observed, the strike of these deformed beds is approxi­ able tiny quartz veins. The resulting rock ir hard and mately parallel to the contact, and dips range from medium- to fine-grained; the colors are light shades of nearly vertical to 35° toward the mass. On the south­ pink, gray, and green. Where replacement ir complete, west side of Cave Peak there is faulting along the con­ parts of the rock closely resemble aplite, but in other LOCALITIES IN TEANS-PECOS BEGION 141 places remnants of the rhyolite porphyry texture are merwinite (Ca3MgSi3O8 ) with a little periclase (MgO). preserved. The altered zone forms an aureole around Another type is a greenish-brown hornfels that is at the granite plug, suggesting that the alteration is re­ least in part grossularite, idocrase, and wollastonite. lated to emplacement of the granite. The presence of spurrite and merwinite indicates meta­ The porphyritic granite is a dense medium-grained morphism at very high temperature (Bowen, 19*0, p. rock of quartz and orthoclase crystals in a fine grained 255-264) and comparatively low pressure (Korzhmsky, groundmass of similar composition. It contains rare 1937) . The association of wollastonite-garnet-spurrite green skeletal crystals, possibly epidotized remnants is also in this same temperature range ( Yoder, 1950, p. of biotite; otherwise mafic minerals are lacking. 249) . The principal constituents of the white and gray Orthoclase is opaque white from slight alteration, and hornfels are silica, lime, and magnesia, according to the rock is partly replaced by manganese and iron chemical analyses (table 62) . oxides. Light rhyolite breccia underlies most of the main TABLE 62. Analyses of hornfels from Cave Peak ridge and is the most abundant rock in the area. It [K. J. Murata, analystl crops out in a ringlike zone about 600 feet wide. The ---,----. __._. .. 5.56 6.28 (SiOj) -___.__-__ ._ . _. (3.60) (1.00) rock is pale orange and consists mainly of angular frag­ - __ __ 25.38 24.56 ments of rhyolite in a felsitic groundmass of quartz and RaOs-- - -- 1.62 2.80 MgO_ . ------5.93 3.06 feldspar. Many of the fragments are like the ground- CaO-.-_. ------55.00 54.04 C02 ------5.95 7.00 mass, others are rhyolite porphyry with conspicuous H20 + ------2.03 2.09 flow structure, and a few are metamorphosed limestone. H2O------_---_------_-__ .29 .09 F-----_------__----_------_-----__ .21 .05 The areas of dark breccia that occur near the top of the SOg- _ .14 None(?) peak may be large blocks of dark rhyolite breccia like 100. 11 99.97 that of the north slope, or a darker phase of the sur­ .06 .02 rounding light rhyolite breccia. Fragment size varies widely from place to place. On the eastern side of the 100. 05 99.95 peak near the outer contact the light rhyolite breccia is i Corrected for oxygen equivalent of fluorine. 1. White hornfels from east side Cave Peak, containing spurrite, merwinite, garnet, composed of fragments as much as 2 meters in diameter, wollastonite, idocrase, calcite, etc. P. B. King's specimen 797A. 0. Gray hornfels, principally spurrite, from same locality. P. B. King's specimen but near the inner contact the average diameter of frag­ 797B. ments is less than a centimeter. The zones of contact, Both the hornfels and the marble are crisscrossed by as well as the character of the inclusions, suggest that thin veins of fine-grained, hard material, ranging from the light rhyolite porphyry is the last of the larger in­ white to light green. Similar material was determined trusive bodies. by Charles Milton as thaumasite METAMOBPHIC BOCKS (CaSiOa CaCO3 CaSO4 14.5H2O) The limestone on the eastern and southern sides of Cave Peak has been metamorphosed to marble or horn- and calcite. Also, he noted the alteration of much spur­ fels in a zone as much as 150 feet wide that has been cut rite and merwinite to a hydrous silicate that is prob­ by dikes and irregular masses of light rhyolite ably the rare mineral radiophyllite, (CaO-SiOa'l^O). porphyry. Nearly all the exposures of rhyolite por­ These hydrous minerals undoubtedly represent a retro­ phyry are surrounded by an inner zone of hornfels gression from the intense initial metamorphism. not more than 50 feet wide and by an outer zone of On a weathered surface the metamorphic rock' and marble. These zones indicate that the metamorphism their veins are altered further to claylike material. was related to the intrusion of porphyry. OCCURRENCE OF BERYLLIUM The mineralogy and petrography of the metamorphic rocks are complex. The limestone is mostly meta­ The samples analyzed for beryllium are described in morphosed to a white to buff, fine-grained marble that table 63 and their localities are shown on plate 5. locally contains some fine white needles of tremo- On the eastern slope of the peak a 4-f oot-thick shear lite(?). Chert nodules in the marble are altered to a zone at the face of an adit has brought a block of altered green silicate rock that probably contains diopside. light rhyolite porphyry into contact with the light rhyo­ The areas mapped (pi. 5) as hornfels include a va­ lite breccia. The rock in the shear zone is completely riety of rocks. A common type is a light-gray or white, altered to clay, iron oxides, and gypsum. At the portal very fine grained hornfels that according to Charles of the adit a 1-foot shear zone separates the blo% of Milton is principally spurrite (CaCO3 *2Ca2SiO4) and porphyry from hornfels. 142 OCCURRENCE OP NONPEGMATTTB BERYLLIUM IN THE UNITED STATES TABLE 63. Beryttia in samples from Cave Peak, in percent [All analyses speetrographic except as noted. Analysts: ZJM, Z. J. Murata; JDF, Janet D. Metoher; JTR, J. T. Rozsa, National Bpectrograhphic Laboratories; LWB, L. W. Strock, Saratoga Laboratories, Inc.; MM8, Samples collected and analyzed by Mine, Mill, and Smelter Survey] Sample Description BeO Mo Nb Sn Zn Analyst 329-017a Sample from two 1.5-ft channels across limonite vein with steep westward dip in dark rhyolite por­ phyry and breccia, at portal. 0.004 LWS 020 Channel sample across 7 ft of highly altered, banded rhyolite porphyry dike, some quartz, limonite, and manganese oxide replacement. <.004 LWS 021 Chip sample of 3-ft lignt rhyolite dike altered to clay and hematite. <. 004 LWS 054 Channel sample across 2 ft of hema­ tite-bearing fracture zone in dark rhyolite porphyry, at portal of adit______<. 004 LWS 055 Channel sample across 6 ft of hema­ tite-bearing fracture zone in dark rhyolite breccia.______<.004 LWS 056 Chip sample across 6 ft of hema­ tite-bearing fracture zones in light rhyolite breccia._____.___-_-__._ <. 004 LWS 057 Channel sample across 6 ft of hema­ tite and limonite vein, 20 ft inside adit in light rhyolite breccia__ <. 004 LWS 062 Channel sample along small fracture zone bearing iron oxides, in pros­ pect shaft in dark rhyolite breccia- <. 004 LWS 064 Chip sample across 6-ft wall of adit (35 ft in) veined with iron oxides copper carbonates, fluorite, and minor wolframite in light rhyolite breccia.______<. 004 LWS 065 Chip sample of 0.3-ft vein similar to 329-064, at portal of adit. ______<. 004 LWS 074 Grab sample of various types of horn- fels, near 329-206.______<. 001 JTR 077 Channel sample across 4 ft of shear zone altered to limonite, clay, and gypsum, at contact of light rhyolite breccia and altered light rhyolite porphyry, near face of adit. _ .01 0. OOX 0. OX 0. X 0. OOOX 0. OX JDF (. 0096) LWS 078 Channel sample across 6 ft of altered light rhyolite porphyry, between 329-077 and portal____. ___ .004 .OOX .ox .ox .ooox .ox JDF (. 0063) LWS 079 1-ft channel sample across 1-ft shear zone altered to limonite, clay, and gypsum, at portal.______.01 .OOX . OOX . X .OOOX JDF (, 017) i LWS 080 Channel sample across 3.5 ft of gray hornfels containing grossularite, spurrite, etc., next to portal._ _ <. 004 LWS 081 Channel sample across 15 ft of black hornfels containing spurrite, etc., with many greenish-white veins, outward of 329-080.______<. 004 LWS 084 Specimen of pink hornfels ______<. 001 JTE 206 Chip sample across hornfels area__ _ .001 JTE 208 Chip sample across feldspar-bearing hornfels.______.001 JTE 209 Chip sample across small hornfels in­ clusion. ______<.001 JTE 680 Chip sample across 25 ft.of grossu- larite-idocrase-spurrite (?) hornfels_ .0005 <. OOX ______<. OOOX <. OOX <. OX JDF 682 Channel sample across 3 ft of rhyolite breccia near 329-680______.0076 JDF 684 Chip sample of hornfels ______<. 0001 JDF 685 Chip sample of light rhyolite breccia, near 329-684. ______.0049 JDF 686 Chip sample of light rhyolite por­ phyry, near 329-685 and 685. _____ <. 0001 JDF See footnotes at end of table. LOCALITIES IN UTAH 143

TABLE 63 Beryllia in samples from Cave Peak, in percent- Continued Sample Description BeO Mo Nb Pb Sn Zn Analytt S-150-448 Channel sample across 1.5 ft of brec- ciated contact rock, gypsum-rich and iron-stained (same as 329- 077?)______0.3 0. 02 mor- Information on the BeO content of nonpegmatite phic deposits at the Black Jack and Dragon Iron mines rocks in Utah was obtained at 6 localities (see fig. 39). and near the Carisa stock, all in the central part of the In September 1949 we investigated and sampled the Tintic district and about 1 mile east of Silver City. beryl-bearing granite in the Sheeprock Range and the The Black Jack mine, half a mile southeast of Mam­ ore deposits associated with contact zones in the Tintic, moth, is in metamorphosed limestone near the contact West Tintic, and Ophir mining districts. Samples with an altered monzonite dike. In an opencut a black 144 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES urian and Devonian) dolomite has been cl *,nged to a spinel-garnet-pyroxene rock. A grab sample (328- 925) of this rock from the southwest side of the stock contained less than 0.0001 percent BeO.

WEST TIKTIC DISTRICT The West Tintic district covers an area of several square miles in eastern Juab County about 25 miles airline southwest of Eureka. The geology and ore de­ posits were studied by Loughlin (Butler, and others, 1920, p. 432-444) and Stringham (1942). Precambrian shale, conglomerate, and quartzite are in fault contact with, and unconformably underlie dolo­ mite, limestone, quartzite, and shale of Paleozoic age. These are intruded by granodiorite and monzonite stocks and dikes of Tertiary age. Tertiary rhyolite flows cover the sedimentary rocks east of th°* district. Contact metamorphic and fissure-vein deports in the limestone of Paleozoic age are related genetically to the intrusive granodiorite and monzonite. Gold, silver, lead, copper, and tungsten are the principal metals pro­ duced. A brief examination was made of the Iron King and Desert Tungsten mines. The Iron King mine, in the western part of the dis­ trict, is in a narrow tactite zone in limestone. Mag­ netite and specularite are the principal ore minerals. Garnet, epidote, diopside, tremolite, and quartz replace DISTRICTS the marmorized limestone adjacent to the iron ore. A Juab and Utah Counties 1. Tintic district grab sample (328-930) of monzonite was obtained from 2. West Tintic district 3. Topaz Mountain an exposure 300 feet west of the mine, and a grab Salt Lake County Tooele County sample (328-931) composed of garnet, epidote, quartz, 4. Little Cotton-wood district 5. Ophir district 6. Sneeprock Mountains diopside and magnetite was taken from the mine dump. FIGURE 39. Index map of Utah, showing localities sampled. These samples did not as much as contain 0.0001 per­ manganese-stained siliceous rock is next to a zone of cent BeO. altered monzonite that is composed of clay and quartz. The Desert Tungsten mine, about 1,000 fret east of A grab sample (328-929) of the altered monzonite con­ the Iron King mine, was operated during WorM War II tained less than 0.0001 percent BeO. for tungsten. Scheelite occurs with garnet, magnetite, The Dragon Iron mine is on the north side of Dragon epidote, and some tremolite, in a fissure vein in lime­ Canyon about a mile southeast of the Black Jack mine. stone. A grab sample (328-932) from the dump did The mine is in metamorphosed Ajax and Opohonga not contain as much as 0.0001 percent BeO. limestones of Ordovician age near their contact with a monzonite stock. A northwestward-trending zone of TOPAZ MOUNTAIN, THOMAS RANGE altered rock that is rich in limonite extends for about a By J. C. OLSON thousand feet along the contact of the stock and is ex­ posed in a large opencut. The margins of the zone are Pink beryl occurs in the topaz-bearing rhyolite of largely kaolin. Grab samples were taken of iron ore Topaz Mountain in the Thomas Kange, Juab County, from the dump (328-926) of altered limestone from the Utah. The best known locality for topaz ard beryl is north edge of the opencut (328-927) and of kaolin from nearly 2 miles south-southeast of the summit of Topaz the south edge of the opencut (328-928). All contained Mountain, at an altitude of about 5,700 feet, and is about less than 0.0001 percent BeO. 40 miles northwest of Delta, Utah, by good dirt road. The Carisa stock, a small monzonite body 2,000 feet The pink beryl on Topaz Mountain was first men­ in diameter, is about half a mile northeast of the tioned by Hillebrand (1905). Patton (1908) described Dragon Iron mine. Near the contact, the Bluebell (Sil­ the topaz and bixbyite in the rhyolite, but did not men- LOCALITIES IN UTAH 145 tion the beryl. He states that topaz is scattered through central part of the Wasatch Mountains, just southwest the rhyolite for several miles, but is most abundant of Park City. The geology and ore deposits of the on Topaz Mountain. Palache (1934, p. 14) described region have been described by Butler and Lou^hlin the beryl as follows: (1916). Rocks of the area include Precambrian quartz- Beryl: This mineral, so unfamiliar in such surroundings, has ite and slate that are overlain by formations consisting been reported recently from this locality under the name of of limestone, shale, and sandstone of Paleozoic and apatite. A considerable amount of blasting yielded only a small Triassic ages. These rocks were intruded by stocks number of specimens. It is in the form of small crystals of a and dikes of granodioritic quartz diorite. Tactite de­ rose-red color attached to the cavity wall or to topaz. The crystals are tabular, simple combinations of prism and base, and posits formed locally in the limestone beds. The prin­ rarely reach a diameter of 5 mm and a height of 3 mm. The cipal ore deposits are lead-silver veins and replacement color is a delicate pink and somewhat variable. Under the bodies. microscope the crystals show a zonal structure, the zones hav­ Two grab samples of tactite, containing idoorase, ing slightly varying optical properties. They enclose tiny quartz, and garnet, from an unidentified locality in the quartz crystals. Little Cottonwood district were furnished by T. S. I am indebted to Mr. Harry Berman for the following optical data. The crushed crystals show a variation in refractive index Levering. They contained less than 0.0001 percent BeO. w=1.580± to w=1.570±. This variation* is due apparently to The district was not visited by the writers. zoning. The average values are w=1.576, e=1.570. These values indicate a beryl low in alkalies. The specific gravity 2.67±.01 TOOELE COUNTY likewise indicates a low alkali content. OFHIR DISTRICT The topaz is comparatively abundant as clear color­ The Ophir district is on the west side of the Oquirrh less crystals in cavities in rhyolite that occupies an area Eange, about 30 miles southeast of Tooele. Lousjhlin at least a mile wide and several miles long. At the (1917), Butler (Butler and others, 1920, p. 374-382), principal workings for topaz, about half a mile north­ Wichman (1920), and Gilluly (1932, p. 139-156) have west of the camp maintained by the Utah Geological described the geology and ore deposits of the district. and Mineralogical Society, the rhyolite has been blasted The rocks are largely sedimentary and consist of quartz- at about four places over a distance of 1,000 feet. Topaz ites, shales, and limestones ranging in age from Cam­ is common both in the rock quarried and throughout brian to Carboniferous. The igneous rocks are highly much of the other rhyolite in the area, but beryl is diffi­ altered and occur as small dikes and sills in the sedi­ cult to find. mentary formations. Lead and silver, with minor Beryl occurs as very rare, quarter-inch or less, tabu­ amounts of copper, zinc, and gold are the principal lar pink crystals. The richest locality'found in a day's metals recovered, mainly from replacement bodies in reconnaissance is a small pit dug for specimen material. limestone. In some places the limestone has been al­ A half-hour search at the pit yielded only 3 tiny crys­ tered and replaced by epidote, quartz, sericite, and tals. Because the visible beryl is such a minute per­ orthoclase. centage of the rock, spectrographic analyses were made A grab sample (328-924) consisting of marble, epi­ of 7 samples of rhyolite in which no beryl was visible. dote, and silicified limestone collected from the dump A sample of massive rhyolite containing no large cav­ of the U. S. mine did not contain as much as 0 0001 ities, from about 600 feet north-northwest of the camp, percent BeO. contained 0.0011 percent BeO. Samples from three of SHEEPROCK MOUNTAINS the localities where rock was blasted for topaz con­ tained 0.0020, 0.0012, and 0.0020 percent BeO. Two The Sheeprock Mountains are in southeastern Tooele samples of rhyolite from the pit dug for specimen beryl County and northeastern Juab County about 25 miles contained 0.0039 and 0.0020 percent BeO, and a sample west of Eureka, Utah. Beryl-bearing granite occurs of rhyolite 100 feet northeast of the pit contained 0.0021 in the northern part of the range north of the IfVker percent BeO. The 7 samples range from 0.0011 per­ Ranch. The area is accessible by gravel and dirt road cent to 0.0039 percent BeO, averaging 0.0020 percent, extending northwest from Jericho on U. S. Higl way which appears to be a representative figure for this large 6, 20 miles south of Eureka. Two days were f^ent mass of rhyolite. studying the occurrences of beryl and exploring the granite boundary for tactite deposits. SALT LuA-KE COUNTY Little detailed work has been done in the Sheeprock Range and the general geology is known. Butler and LITTLE COTTONWOOD DISTRICT others (1920, p. 423-426) made a reconnaissance survey The Little Cottonwood mining district is between the of the region, and the Precambrian rocks were de­ Big Cottonwood and American Fork districts in the scribed by Eardley and Hatch (1940, p. 823-P97). 146 OCCURRENCE OP NONPEGMATITE BERYLLIUM IN THE UNITED STATES

These rocks appear to constitute the bulk of the range rock is the beryl-bearing granite stock which extends and consist largely of quartzite with some phyllite and nearly across the northern part of the ran£% cutting a few conglomeratic layers which may be of glacial both Precambrian arid Paleozoic rocks. TH general origin. Limestones and quartzites of Paleozoic age geology of the region and locations of the area we in­ crop out in the West Tintic district at the southern end vestigated are shown in figure 40. of the range and in parts of the Columbia and Erickson Beryl is sparsely distributed through granite and districts at the northern end. The principal intrusive aplite near the central part of the stock about 1 mile north of the Ekker Eanch house (see fig. 41). The major occurrences are in an irregular zone extending for nearly 2,000 feet along the east side of Hard-to- Beat Canyon. The beryl is a bright blue vith index (No) of 1.58, indicating about 13 percent BeO. It occurs as rosettes and single crystals along poorly de­ 40° 00' fined fractures, veinlets, and schlieren which appear to be related to the flow structure in the granite Rosettes are fairly common and some are as much as C inches in diameter, with beryl crystals radiating from the center. One piece of beryl float showed comb structure, with TOOELE_CO,, beryl crystals perpendicular to the walls of a fracture JUAB CO i^>v filling. Other occurrences consist of small irregular aggregates of beryl with quartz and feldspar which form isolated pods and lenses in the granite. Tex- turally these aggregates resemble pegmatite, though pegmatite dikes were not noted in the area examined. WEST TINTiC Much of the beryl, particularly in the aplite, occurs as DISTRICT single crystals or small groups of crystals less than a centimeter in diameter. In most places the beryl ag­ gregates are separated from their nearest neighbors by several feet to several tens of feet of apparently barren granite, and large parts of the zone appear rot to con­ Geology after Butler and others, 1920, fig. 46 tain beryl. EXPLANATION Thin sections of the granite reveal that i*s mineral

SEDIMENTARY ROCKS composition is approximately 35 percent pcrthite, 30 percent albite, 25 percent quartz, 5 percent b;otite, and 5 percent orthoclase and miscellaneous constituents. The composition of the albite is about Ab95, crrespond- ing to that of the blebs in the perthite. A few grains of albite-antiperthite, containing blebs of mierocline, were noted. Perthite was the latest mineral to form, filling interstices between the other minerals. The bio- tite is pale, highly pleochroic, and strongly birefrin- gent. It contains inclusions of zircon which r*iow well- developed pleochroic halos. Mineral composition of the aplite is similar to that of the granite except that orthoclase is abundant and perthite is absent. A thin section cut from a specimen of beryl-rich Granite granite, showed beryl interstitial to corroded grains of quartz and albite; perthite and orthoclase ^ere lack­ Contact ing. A section cut from adjoining beryl-fr^e granite- Approximately located showed abundant perthite interstitial to uncorroded 10 Miles grains of quartz and albite. It seems clear that the FIOCEB 40. Geologic index map showing locations of areas investigated beryl replaced perthite and orthoclase. Thif evidence, in Sheeprock Mountains, Utah. together with the field relations, suggests that the beryl LOCALITIES IN UTAH 147

EXPLANATION

Coarse-grained granite

Contact

75 Strike and dip of foliation 65 Strike and dip of joints

Beryl-bearing area

328-940

Locality sampled and number

Contour lines Approximate interval 50 feet

Geology and topography by L. A. Warner and Y- R- Witmarth, September 1949 500 1000 Feet I______I FIQUBH 41. Geologic sketch map showing occurrence of beryl in Hard-to-Beat Canyon, Sheeprock Mountains, Utah. is of secondary origin, having been introduced by solu­ TABLE 64.- -Beryllia in samples of granite and aplite from Hard- to-Beat Canyon tions that permeated the rocks after their emplacement. B-0 Samples of granite and aplite were taken, as de­ Sample Description 328-933 Chip sample across aplite dike; little~or no scribed in table 64; locations of the samples are shown beryl visible___-_-. ------0, 0049 on figure 41. In sampling, care was taken not to in­ 934 Chip sample across beryl-bearing granite. _ _ . 0052 935 Chip sample of beryl-bearing granite._____ 0050 clude any of the beryl aggregates, for it was desired 936 Chip sample across beryl-bearing aplite 0033 to learn whether the rocks might contain disseminated 937 Chip sample across aplite next to beryl- bearing granite at north end of zone_-__ 0033 beryl not visible in hand specimen. The relatively low 940 Chip sample across beryl-bearing granite, beryllia content of the samples indicates that fine­ south end of zone.-.------0024 grained beryl, if present at all, is probably not abun­ Along its northwestern margin, the granite stocV in­ dant. Without more detailed mapping and sampling vades limestones of Paleozoic (?) age. The contact in the tonnage of beryl-bearing granite cannot be esti­ this area was investigated for about a mile (see fig. mated. Parts of the granite may be rich enough in 42) in a search for tactite deposits that might certain beryl to constitute an ore of milling grade. beryllium. The limestone has been silicified and mar- 148 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES (fig. 43). A variety of samples of igneous rocks and &:£&" '&&£ \ ./" ore deposits was obtained. Principal attention was devoted to the Butte district, where helvitr had been -1 M > --^Y t;:£V :':, ' ^o£^s/ reported in rhodonite veins. The veins apparently do ^^^^r«^o^jx ^^-:^*v:>. - not contain enough helvite to make them a lil'ely source A->N/_/^l-^_IX ¥^?; ^ -". sOv/^XivX\ ":' '' of beryllium. A sample of tactite from the Mill Creek x i i; \ area, southwest of Anaconda, and a sample of mill -944 tailings taken at the Drumlummon mine in the Marys- ville district contained 0.022 percent and O.C11 percent EXPLANATION of BeO, respectively. There is no assurance that the samples are representative and further investigations Quartz and silicified limestone at these localities are needed to determine the nature and quantity of the beryllium-bearing material.

CASCADE AND JUDITH BASIN COUNTIES

LITTLE BELT MOUNTAINS Contact Approximately located In the central part of the Little Belt Mourf,ains, near Neihart, alkalic igneous rocks intrude limestones of y Gossan Paleozoic age, and locally contact metasomatism has taken place. Metamorphosed limestone is exposed in Vein, showing dip 16° 301 Dashed where inferred a road cut on U. S. Highway 89, about 10 miles south

Geology by L. A. Warner Strike and dip of beds of Neihart (fig. 44). The sedimentary rod's are part and V. R. Wilmarth, ^75 of the Barker formation of Weed (1899a) (Cambrian) Strike and dip of foliation September 1949 and consist of altered limestone, quartzsite, and shale. Adit B The igneous rocks are part of the group mapped by Shaft X Weed as diabase, basalt, minette, vogesite, and kersan- Pit tite. The igneous rocks exposed in the road cut include 1000 I 328-942 Locality sampled and a lamprophyre dike and a light-colored aphanitic rock number which may have been separately intruded cr is an ex­ FIGUEB 42. Geologic sketch map of northwest contact of granite stock, Sheeprock Mountains, Utah. tremely altered part of the lamprophyre. The lime­ stone adjacent to the lamprophyre has been marmorized morized, but no tactite was found. A few fissure de­ and partially replaced by silicate minerals. Taylor posits containing quartz, pyrite, chalcopyrite, limonite, (1935) identified 27 minerals in the contact zone. A and in places magnetite, were formed in the granite and grab sample (328-919) was taken from the contact zone adjoining rocks. A veinlike deposit along the west on the east side of the road cut and a chip sample (328- margin of the granite has been oxidized to a gossan 920) was taken across the altered limestone and shale that was traced for more than 1,000 feet. A sample of exposed on the west side of the cut. Beryllium was not this material (328-942) showed no detectable beryl­ found in these samples; the lower limit of detection be­ lium. No beryl was observed in the granite in this ing 0.0001 percent BeO. area, and a chip sample of the granite (328-944) con­ Yogo Peak is a prominent topographic feature in the tained only 0.0008 percent BeO. Along its northern Little Belt Range about 6 miles east of Neihart. It is and eastern boundaries the granite stock is in contact formed by a Tertiary stock of shonkinite that cuts lime­ with Precambrian quartzite, and the southern boundary stones, shales, and sandstones of Paleozoic age. Talus is largely covered by alluvium. The probability that covers most of the contact on the west slope of Yogo further search might reveal beryllium-bearing deposits Peak, and little or no metamorphism was found where along the granite boundary seems small. the contact was exposed. On the east and northeast sides of the peak, massive limestone beds have been MONTANA marmorized and locally replaced by garnet, actinolite, By L. A. WARNER and V. B. WILMARTH and diopside. A grab sample (328-921) of these con­ tact minerals from a tactite zone, 3 miles by road north­ Beryllium investigations in Montana were carried east of the top of Yogo Peak, did not contain as much on during September 1949, in 18 districts and localities as 0.0001 percent BeO. LOCALITIES IN MONTANA 149

112° 108°

200 Mites

LOCALITIES Cascade and Judith Basin Counties Jefferson County Powell County 1. Little Belt Mountains 7. Basin district 13. Ophir district 8. Blkhorn district 14. Priest Pass Deer Lodge County Lewis and Clark County Silver Bow County 2. Georgetown district 9. Marysville district 3. Mill Creek area 10. Spring Hill mine 15. Butte district 16. Highland district Madison County 17. Toll Mountain area Granite County 11. Silver Star district 4. Garnet district 5. Philipsburg district Meagher County Sweet Grass County 6. Red Lion district 12. Gordon Butte 18. Haystack stock FIGURE 43. Index map of Montana, showing localities sampled.

DEER LODGE COUNTY far as 1,200 feet from the contact, and dolomite is re- GEORGETOWN DISTRICT crystallized and irregularly replaced by massive mag­ By W. T. HOLSER netite near the stock. Later deposited pyrite, chalco- pyrite, pyrrhotite, arsenopyrite, and gold are wide­ The Georgetown district is in the vicinity of George­ spread in the contact zone. town Lake, where U. S. Highway 10A crosses the sum­ The recrystallized and replaced limestones were sam­ mit of the Flint Creek Range. It was sampled in June pled at several places along the northern edge of the 1948 in connection with other geological work in the stock as follows: area. The geology of the district was described by Emmons 329-003 22-ft channel sample of magnetite-dolomite-oUvine and Calkins (1913, p. 221-242) and Holser (1950, p. rock, from open pits of Pomeroy mine, 1063-106T). A stock of granodiorite 2 miles in diam­ 329-004 25-ft channel sample of dolomite marble partly altered to limonite, from opencuts on the Uncle Billy claim. eter intrudes a faulted anticline of sedimentary rocks of 329-005 10-ft channel sample of dolomite marble at contact of Paleozoic age. Shaly limestones are metamorphosed to granodiorite, from northeast crosscut of tunnel level, garnet-diopside and hornblende-magnetite tactites as Cable mine. 150 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES 329-006 10-ft channel sample of brecciated dolomite marble, On the north side of Mill Creek, near its headwaters, from main tunnel near third crosscut, Gable mine. shaly limestone in the Silver Hill formation of Cam­ 329-007 15-ft channel sample of dolomite marble breccia and brian age has been contact metasomatized next to a magnetite from tunnel level just north of Nowlan raise, Gable mine. granodiorite stock. A geologic sketch map of the con­ tact zone exposed near the head of a northearVtrending gulch on the southeast side of Mount Haggin is shown in figure 45.

Lake Clear ...Q___*...- Eost side of rood cut A MT. HAGGIN x-

Area of sketch 338-920

West side of rood cut 2 Miles

R. 12 W. 113° Geology by L A. Warner and V. R. Wilmarth, INDEX MAP EXPLANATION September 1949

Quartzite

Lamprophyre Sandy shale

_ Granodiorite 328-920 Locality sampled and Altered limestone and shale number FIGUEB 44. Sketches showing geology in road cut on U. 8. Highway 89, Mainly schist witt some marble, in T. 12 N., K. 8 E., about 10 miles south of Neihart, Mont. pegmatite sills,-and granodiorite di* es

Magnetite deposits near the contact of a granite stock Marble, shale, end biotite schist at Olson Gulch (Holser, 1950, p. 1067, Emmons and Marble Calkins, 1913, p. 244) were sampled as follows: Pegmatite sill Marble, shale, and biotite schist 329-008 40-ft channel sample of magnetite-actinolite tactite in Pegmatite sill limestone, from northern open pits of the Bung- Marble Your-Bye claim. Hornfels 329-009 15-ft channel sample across a hematite-clay shear Talus zone, same locality as sample 329-008. 200 400 Feet Beryllium was not detected in these samples, the LL lower limit of sensitivity being 0.001 percent BeO. FIGURE 45. Index and sketch maps of contact zone near Koant Haggin, Anaconda Range, Dear Lodge County, Mont. HHI CREEK AREA Mill Creek rises in a valley that heads a short dis­ The rocks exposed in the contact zone are biotite tance west of Mount Haggin, a prominent peak about schist, hornfels, marble, pegmatite sills, and narrow 30 miles southwest of Anaconda. The area is in the dikes of granodiorite. In places the marble and horn­ southeast part of the Philipsburg quadrangle, the geol­ fels have been replaced by idocrase and garret. ogy of which was described by Emmons and Calkins A composite sample (328-905) of idocrr ^e-bearing (1913) and Calkins and Emmons (1915). The western rock from this locality contained 0.022 per?«nt beryl­ part of the quadrangle is underlain by rocks of the Belt lium oxide. A mineralogical study of rock specimens series which in most places have "been thrust over com­ from the contact zone was made by J. J. G?ass, of the plexly folded and faulted formations of Paleozoic and U. S. Geological Survey, in an effort to isolate and Mesozoic age that lie to the east. The latter have been identify the berylHum-bearing mineral. The specimens intruded by stocks, dikes, and sills ranging in composi­ were composed chiefly of idocrase, fluorite, cMcite, bio­ tion from granite to diabase. tite, spessartite, diopside-hedenbergite, hyirobiotite, LOCALITIES IN MONTANA 151 quartz, and albite. The results of spectrographic replaced by diopside, garnet, epidote, and magnetite. analyses of these minerals for beryllium are shown in An eastward-trending fracture zone in the metamor- table 65. phic rocks contains local concentrations of quartz, barite, pyrite, tetrahedrite, chalcopyrite, galena, gold, TABLE 65. Beryllia in minerals from contact zone, Mill Creek area, Montana telluride minerals, and molybdenite. [Qualitative spectrographic analyse, by A. A. Cbodos] A 4-foot channel sample (329-014) was cut from a BeO Description (percent) surface exposure of garnet-diopside tactite at the Sh^ra.- Idocrase from idocrase-fluorite-marble rock__ __ O.OX rock mine in the town of Garnet. At the Boston mine, Fluorite from idocrase-fluorite-marble rock______.OOX Calcite from idocrase-fluorite-marble rock______Not found. a 15-foot channel sample (329-015) was taken across Biotite from idocrase-fluorite-marble rock______Not found. garnet and garnet-magnetite tactite in limestone. S^c- Garnet from quartz-feldspar-garnet rock______Not found. Diopside-hedenbergite from hornfels______.OOX trographic analyses of these samples showed no beryl­ Hydrobiotite from marble______.OOOX lium, the limit of detection being 0.001 percent FsO. Quartz and albite from veinlets______.OX Idocrase occurs chiefly in the relatively thin shaly PHILIPSBUBO DISTBICT limestone layers, in which it is an abundant constitu­ The Philipsburg district, which is on U. S. Highway ent. J. J. Glass of the U. S. Geological Survey made 10A midway between Butte and Missoula, was visited the following optical determinations on the idocrase: in July 1948. The geology was studied by Emmons and uniaxial negative; Ne = l.TOO; N0 (variable) 1.707 to Calkins (1913) and by Holser (1950). A northward- 1.717; birefringence (variable) 0.007 to 0.015; dis­ plunging anticline of sedimentary rocks of Paleozoic age tinctly pleochroic in thick grains, colorless to yellowish is intruded by granodiorite of the Philipsburg batho­ green. A quartz-feldspar-garnet rock was found in lith. Limestones are partly recrystallized, and shal^ or float but was not observed in place. The garnet is spes- sandy limestones are replaced by garnet-diopside tac­ sartite (N=1.80 to 1.81) and is associated with micro- tite. Much of the tactite is replaced by magnetite, horn­ cline, albite, and quartz. Bands rich in diopside-hed- blende, and scapolite. East-trending veins contain enbergite occur in hornfels near the pegmatite sills. quartz, rhodochrosite, pyrite, galena, sphalerite, and Veinlets and stringers of quartz and albite presumably argentiferous tetrahedrite; the pxide zones are rich in are related to the pegmatite. manganese. The contact zone in this area is extremely complex, Samples were taken from the contact zone as follows and detailed sampling would be needed as a basis for (for localities see Holser, 1950, pi. 1): estimating tonnage. There is no assurance that the 329-010 Channel sample across 15 ft of phlogopite-bearing material collected at the locality visited is at all typical marble, 235-ft level of Marie mine, 400 ft from of the zone. Calkins' map (Emmons and Calkins, 1913, shaft. pi. 1) shows the Silver Hill formation extending for 329-011 Channel sample across 20 ft of marble containing more than 2 miles along the southern margin of the pyrolusite and quartz at headframe of True Fissure granodiorite stock in the vicinity of Mount Haggin. shaft. 329-012 Channel sample across 15 ft of dolomite marble con­ The mineral assemblage in the contact zone is one taining serpentine and magnetite, from end of south which commonly includes helvite, though none was drift, main level, Climax mine. found. Beryllium was not detected in the samples, the lower GRANITE COUNTY limit of sensitivity being 0.001 percent BeO.

By W. T. HOLSER RED LION DISTRICT GARNET DISTRICT In the Ked Lion district, about 10 miles southeast of The Garnet district, including the Top O'Deep dis­ Philipsburg, sedimentary rocks of Paleozoic age, mr.inly trict, is along the crest of the Garnet Range, about 50 limestones, have been metamorphosed adjacent to the miles east of Missoula, and about 10 miles north of Philipsburg batholith. The metamorphism is les^ in­ U. S. Highway 10. The area was visited in July tense than in the Philipsburg and Georgetown districts 1948. The geology of the district has been described nearby. Fracture fillings and replacement bodies in the by Pardee (1917) and Holser (1950, p. 1067). A limestone contain quartz, calcite, pyrite, hematite, mag­ northwestward-trending anticline of limestones and netite, and gold. shales of Paleozoic age is intruded by granodiorite of A prospect on the Modoc claim (Emmons and Cal­ the Garnet batholith. Although recrystallization is kins, 1913, p. 239) is on the contact between granodiorite widespread, contact metasomatism is confined to a nar­ and marble. Two channel samples were taken at this row zone near the granodiorite where shaly beds are prospect, one (329-001) across 5 feet of granodiorite 152 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES and the other (329-002) across 12 feet of marble. The limestone and shale. A composite grab sample (328- samples contain no beryllium, the lower limit of sensi­ 909) of dump material contained no beryllium, the tivity being 0.001 percent BeO. lower limit of sensitivity being 0.0001 percent BeO. The Sourdough mine, a mile northwest of Elkhorn, JEFFERSON COUNTY is developed on a small pyrrhotite deposit in limestone BASIN DISTRICT near a quartz monzonite intrusive. Minor quantities of The Basin mining district, centering around the town scapolite and epidote were noted on the dump. A grab of Basin, is about 8 miles west of Boulder and 20 miles sample (328-910) of dump material composed of tpi- south of Helena in the northern part of Jefferson dote, scapolite, pyrrhotite, and limestone contained no County. The geology and ore deposits were described beryllium, the lower limit of sensitivity being 0.0001 by Knopf (1913, p. 120-128) and Pardee and Schrader percent BeO. (1933, p. 285-299). The rocks exposed in the Basin dis­ A grab sample (328-911) of garnet frcm a small trict are quartz monzonite, dacite, and andesite of Late prospect pit on the Quartz Lode mining claim, one- Cretaceous and Tertiary age. The ore deposits include fourth mile below the Sourdough mine, contained no gold placers, and lodes that are valuable for silver, lead, beryllium, the lower limit of sensitivity being 0.0001 zinc, and copper. Some composite lodes were worked percent BeO. chiefly for gold and silver. Samples were obtained LEWIS AND CLARK COUNTY at the Eva Mae and Hattie Ferguson mines. The Eva Mae mine and mill are 8 miles north of MARYSVILLE DISTRICT Basin. The country rock is quartz monzonite that has The Marysville mining district is in Lewis and Clark been cut by tourmaline-bearing quartz veins containing County, about 17 miles northwest of Helena. The scheelite, galena, chalcopyrite, sphalerite, and pyrite. geology and ore deposits of the district wer-> discussed Grab samples of mill tailings (328-906) and ore from by Barrell (1907), Knopf (1913, p. 61-76; 1950), and the mine dump (328-907) contained no beryllium, the Pardee and Schrader (1933, p. 63-76). TH rocks of lower limit of sensitivity being 0.0001 percent BeO. the Marysville district include a small quartz diorite The Hattie Ferguson mine is on Cataract Creek, about stock that intrudes limestones and shales of the Belt 6 miles north of Basin. The now abandoned mine was series. Younger intrusive rocks are aplite, pegmatite, on a quartz vein in aplite. Galena, sphalerite, and and diorite porphyry. The ore deposits are steeply dip­ auriferous pyrite are the principal ore minerals. A ping veins in the metamorphosed sedimertary rocks composite sample (328-908) of vein material from the and the quartz diorite. Gold and silver ar^ the prin­ dump contained no beryllium, the lower limit of sensi­ cipal metals produced. tivity being 0.0001 percent BeO. Only the Drumlummon mine (Clayton, 1888; Good- ale, 1915), on the north side of Marysville, ^ras visited. ELKHORN DISTRICT The dump material consisted chiefly of indurated The Elkhorn mining district, centering around the shales, marble, and hornfels, with very little garnet and town of Elkhorn, is about 12 miles northeast of Boulder, epidote; the mine workings were inaccessible. A grab in the eastern part of Jefferson County. The geology sample (328-913) of mill tailings from th*, Rainbow and ore deposits were described by Weed (1901), Stone mill at the Drumlummon mine contained 0.011 percent (1911), Knopf (1913, p. 128-139), and Pardee and BeO. A mineralogical study of this sample by J. J. Schrader (1933, p. 299-303). The sedimentary rocks Glass of the U. S. Geological Survey was undertaken are limestones, shales, and quartzites of Paleozoic age to identify the beryllium-bearing mineral. The ma­ unconformably overlain by sandstones, shales, and im­ terial was too fine for separation of individual mineral pure limestones of Mesozoic age; all have been much species; a magnetic fraction and three heavy mineral altered by contact metamorphism. Tertiary andesite fractions were separated. The minerals recognized in breccia, tuff, and lava overlie the sedimentary rocks of the fraction with specific gravity greater than 3.3 are Mesozoic age. Intrusive igneous rocks of Cretaceous hematite, limonite, biotite, garnet, zoisite, er>idote, and or Tertiary age range in composition from gabbro to pyroxene. In the fraction with specific gravity between granite. Samples were obtained from the Elkhorn and 2.8 and 3.3 chlorite, diopside, and carbonate were iden­ Sourdough mines and the Quartz Lode claim. tified. The fraction with specific gravity less than 2.8 The Elkhorn mine at the town of Elkhorn explores contains chiefly quartz and feldspar. Magretite is the a lead-zinc-silver replacement deposit in indurated chief constituent in the magnetic separation. The re- LOCALITIES IN MONTANA 153 suits of spectrographic analysis for beryllium of the (328-896) of tactite from the workings and a grab sam­ separate fractions are as follows: ple (328-897) of tailings from the mill containec1 no BeO beryllium, the lower limit of sensitivity being 0.0001 Fraction (percent) percent BeO. Specific gravity >3.3______0. OOX A grab sample (328-899) of garnet rock was collected Specific gravity >2.8<3.3______. OOX from the dump of the Reconstruction Lode No. 3 nrine, Specific gravity <2.8______. OOX Magnetic ______. OOX which is about 1 mile northwest of the Broadway nrine. A quartz vein was mined for gold at this locality. The These analyses, though qualitative, cast some doubt garnet contained no beryllium, the lower limit of sensi­ upon the higher quantitative BeO value obtained for tivity being 0.0001 percent BeO. the bulk sample. No beryllium minerals were recog­ nized in any of the fractions and the analyses suggest MEAGHER COUNTY that the beryllium probably is dispersed in the various GORDON BUTTE silicates. Gordon Butte, in the eastern part of Meagher County, SPRING HILL HIKE is an eroded laccolith at the north end of the Cmzy The Spring Hill mine is 4 miles southwest of Helena Mountains, geology of which was described by Wolff on the east side of Grizzly Gulch. The geology of the (1938). The rock composing the butte is theralite, an mine has been described by Knopf (1913, p. 101) and alkalic basalt containing augite, olivine, biotite, nephe- by Pardee and Schrader (1933, p. 207-209). The ore line, sodalite, and feldspar. A grab sample (328-£?2) deposit is at the contact of a small body of diorite that of theralite from the north side of the butte contained intrudes Madison limestone (Mississippian). A dense no beryllium, the lower limit of sensitivity being 0.0001 gray-green rock composed of diopside and tremolite percent BeO. contains gold and some pyrite, pyrrhotite, and chlorite. POWELJL COUNTY In places, garnet, olivine, scapolite, sphene, and epidote OFHIR DISTRICT replace the limestone. A grab sample (328-918) of ore and tactite minerals from the dump contained no beryl­ The Ophir mining district, centering around the aHn- lium, the lower limit of detection being 0.0001 percent doned town of Ophir, is about 24 miles airline north­ BeO. west of Helena in the eastern part of Powell County. MADISON COUNTY The geology and ore deposits of the district were de­ scribed by Pardee and Schrader (1933, p. 29-34). Lime­ SILVER STAR DISTRICT stones, shales, and quartzites of early Paleozoic age oc­ The Silver Star mining district is northwest of the cupy most of the area. East and west of Ophir are town of Silver Star, about 25 miles airline southeast of small masses of intrusive quartz monzonite of Tertiary Butte, in the northern part of Madison County. The age. The ore deposits are mainly gold and silver v?ins geology and ore deposits of the district have been de­ that are genetically related to the quartz monzonite. scribed by Winchell (1914, p. 139-144). The rocks ex­ The sedimentary rocks have been partly altered to mar­ posed in this district are Tertiary granite, Cambrian (?) ble, garnet tactite, and hornfels. The limestones ad­ limestone, and Precambrian schist, slate, and quartzite. jacent to the intrusive bodies have been replaced by The limestone is metamorphosed and replaced by gar­ garnet, specularite, epidote, hornblende, diopside, cal- net, epidote, magnetite, and pyrrhotite at its contact cite, tourmaline, sericite, and hematite. A composite with granite. Gold, silver, copper, and lead occur in sample (328-914) of tactite from the dump of the May­ tactite deposits and a quartz vein. be mine near Ophir contained no beryllium, the lower The Broadway mine, about 2 miles northwest of Silver limit of sensitivity being 0.0001 percent BeO. Star, is on a tactite zone in the Cambrian limestone near the granite contact. A small glory hole exposes a U-­ PRIEST PASS AREA shaped sulfide ore body composed mainly of gold-bear­ The road over Priest Pass, a short route across the ing pyrrhotite surrounded by tactite and hornf els con­ Continental Divide from Helena to Blossburg, turns off taining magnetite, garnet, and epidote. The tactite zone U. S. Highway 10-N about 1 mile west of Spring Creek extends northeast from the glory hole for about 700 feet, on the east side of MacDonald Pass. Near the top of through two smaller opencuts, and southwest for about Priest Pass, a prospect pit explores the contact of Ter­ 500 feet. Ore deposition appears to have been controlled tiary quartz monzonite with the Quadrant quartaite by a northeast-trending fault that approximately paral­ (Pennsylvanian). A limestone layer in the quarteite lels the limestone-granite contact. A composite sample has been partly replaced by brown garnet. A g~ab 467046 59 11 154 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES sample (328-917) of garnet from the pit contained no In the course of sampling the mines of the Anaconda beryllium, the lower limit of sensitivity being 0.0001 Copper Mining Co. at Butte a visit was made to the percent BeO. company's smelter at Anaconda. Company officials

SILVER BOW COUNTY kindly provided samples of the mill and smelter prod­ ucts of ores from several localities. Twelve of the BTJTTE DISTRICT samples were selected for spectrographic analysis and A brief visit was made to the Butte district to inves­ are described in table 67. In connection with the Mine, tigate the occurrence of helvite reported by Hewett Mill, and Smelter Survey, 12 samples of mill and (1937) at the Lexington mine. According to Hewett, smelter products were obtained in 1945 from the the helvite occurs as sparse lemon-yellow grains as much Washoe Keduction Works at Anaconda. The ores as 2 millimeters in diameter and as veinlets about 1 mil­ treated were from various mines in the Bu*te district. limeter wide in rhodonite and rhodochrosite with minor Analytical data for these samples are giv^n in table amounts of galena, sphalerite, and pyrite. 67. Kesults of analyses indicate that very little beryl­ lium is contained in the ore minerals at Butte. Pre­ Through M. H. Gidel, chief geologist for the Ana­ sumably most of it occurs in helvite associated with the conda Copper Mining Co., permission was obtained to gangue and is lost in beneficiating the ore. sample the Lexington mine. Helvite was noted in a mass of rhodonite as much as 3 feet wide and 30 feet TABLE 67. Beryllia in samples from Washoe Reduction Works, long on the 200-foot level of the mine, 300 feet west of Anaconda, Mont. the shaft. A chip sample (328-902) taken across the [nd not detected; lower limit of sensitivity is 0.0001 percent BeO. Samples 310- ACM-1 to -20 collected in 1945 by Mine, MIU, and Smelter Surrey and analyzed rhodonite mass contained 0.00057 percent BeO. Similar by K. J. Murata and E. W. Clafley] BeO rhodonite bodies have been found on the lower levels Sample Detcription (percent) '328-952 Third shift, Sept. 1, 1949, Agitair tails, of the mine. They appear to be lenticular and to occur Butte Copper ore___--_--_._-_ nd generally on the hanging wall of the vein. 963 Final tails bulk float, zinc ores, Butte, Mont______0. 0004 Analyses of composite grab samples from mine 966 Third shift, Aug. 15, 1949, manganese dumps in the Butte district are shown in table 66. concentrate. ______nd 973 Lot No. B-64, copper concentrate, C "oke Helvite was found in rhodonite on the dumps at the City, Mont______nd Moulton, Niagara, Alice, Magna Charta, and Lexing­ 974 Lot No. 981, waste slag ferroman- ganese______- . 0001 ton mines. Khodonite was virtually lacking in dump 975 Second shift, Aug. 28, 1949, man­ material at the Emma mine, rhodochrosite being the ganese tails___--_--____-_-_--.--_ . 0001 975A Conda phosphate footwall rock______. 0004 dominant gangue mineral, and no helvite was found. 975B Conda phosphate hanging-wall rock-,. nd At all other dumps where samples were taken rhodonite 977 Lot No. FM-7, ferromanganese metal, nd 981 Black sand, Rock Creek dist.nct, was present and rhodochrosite rare or absent. The Mont______nd sample containing the most BeO (0.007 percent) was 988 Third shift, Sept. 1, 1949, Agftair concentrate, Butte Copper ores___. nd obtained at the Niagara mine where fluorite occurs in 989 Zinc concentrates, Butte ores _ _ _ nd the gangue. Although analytical data on the BeO con­ 310-ACM-1 Sulflde concentrate, Emma mine (Pb- Zn-Ag ore, rhodochrosite gangue)__ _ . 0002 tent of the Butte ores are too meager for speculation, ACM-2 Sulfide tailings, Emma mine______. 0002 further sampling of rhodonite veins in which fluorite is ACM-3 Copper flotation tailings, Butte mines. .0002 ACM-4 Copper concentrate, Butte mines. _ nd a constituent may reveal local concentrations of helvite. ACM-5 Arsenic roaster residue, Butte mines-_ . 0002 It is doubtful that such occurrences would be large or of ACM-6 Granulated reverberatory slag (copper), Butte mines______- _ - . 0002 high grade, but in view of recent advances in flotation ACM-8 Iron table concentrates, Butte mines.. nd of nonmetallic minerals, recovery of helvite from rela­ ACM-9 Flue dust (copper), Butte mines. nd ACM-17 Zinc concentrates, Butte mines nd tively low-grade material may be possible in a large ACM 18 Lead concentrates, Butte mines___ nd mining operation. ACM-19 Zinc-lead tailings, Butte mines. __ .0008 AC Mr-20 Zinc concentrates, Butte mines_____ nd HIGHLAND DISTRICT TABLE 66. Beryllia in samples from mine dumps at Butte, Mont. BeO The Highland district is in the southern part of Sample Mine (percent) Silver Bow County, about 25 miles south of Butte. Ac­ 328-890 Lexington. ______0.0016 891 Moulton__...______.__ .0023 cording to Winchell (1914, p. 87-90), the rocks of this 891A ...do.. ___-____-_.______.0015 district consist of a series of slates and qrartzites of 892 Alice______.0042 893 Magna Charta______.0030 Belti age underlying a thick limestone bec\ probably 894 Emma__,______n. d.' Paleozoic in age, all of which are intruded by quartz 903 Alice (vein outcrop, east of shaft)._____ . 0005 904 Niagara..______.0070 monzonite, diorite, granite, and aplite, presumably of 1 Not detected, lower limit of sensitivity being 0.0001 percent. Tertiary age. Garnet, epidote, magnetite, diopside, and LOCALITIES IN WYOMING 155 actinolite replace the limestone at its contacts with WYOMING igneous rocks. By L. A. WARNER and V. R. WILMARTH The Highland mine, at the head of the main fork of Fish Creek, is on the north side of a large limestone Beryllium investigations at 15 localities in Wyoming inclusion or roof pendant in granite. The ore body (fig. 46) were made during October 1948 and August has been described by Newcomb (1941). The ore is 1949. The BeO content of 31 samples selected for chiefly pyrrhotite, pyrite, and chalcopyrite, in a gangue spectrographic analysis ranged from less than 0.0001 of coarsely crystalline tremolite, epidote, and diopside. percent to 0.003 percent. The samples represent many A composite grab sample (328-901) from the dump types of nonpegmatite rocks and mineral deports. contained less than 0.0001 percent BeO. Present information does not appear to warrant further Approximately 2 miles west of the Highland mine is sampling at any of the localities. a tactite zone 50 feet wide and several hundred feet long in the limestone. A composite grab sample (328- ALBANY COUNTY 900) of garnet, diopside, magnetite, and epidote from CENTENNIAL DISTRICT the tactite zone did not contain as much as 0.0001 per­ The Centennial district centers around the town of cent BeO. Centennial in the eastern part of the Medicine Pow TOLL MOUNTAIN AREA quadrangle. The geology of the area was described Toll Mountain is 19 miles southeast of Butte near the briefly by Darton and Siebenthal (1909, p. 49-50). The boundary between Silver Bow and Jefferson Counties. ore deposits consist of gold-bearing quartz veins in Pre- At this locality, sedimentary rocks of Paleozoic age cambrian schist, gneiss, and granite. Samples -rere consisting of slate, marble, and quartzite appear to form collected from two mines, the Utopia and the Inde­ a roof pendant in a Tertiary intrusive granite body. pendence. The sedimentary rocks strike N". 45° E. and dip steeply The Utopia mine is 1 mile northwest of Centennial northwest. A garnet tactite zone can be traced north­ on the east side of Centennial Ridge. Gold is fornH in east for several hundred feet along the contact between a 3-foot wide, west-trending quartz vein in hornblende granite and marble, beginning at an outcrop about 800 schist. Additional vein materials are calcite, pyrite, feet north of the Toll Mountain Banger Station. The sericite, limonite, and garnet. A composite sample garnet zone locally contains thin lenses of diopside. (328-877) of dump material showed no beryllium, the The granite adjacent to the sedimentary rocks has been limit of sensitivity being 0.0001 percent BeO. endomorphosed. A composite grab sample (328-895) The Independence mine is 2 miles west of the Utopia of the garnet rock did not contain as much as 0.0001 mine on the west side of Centennial Ridge. The mine percent BeO. is developed on eight narrow pegmatite stringers in hornblende schist. A 6-foot channel sample (328-878) SWEET GRASS COUNTY across the back of the adit, 10 feet from the portal, HAYSTACK STOCK did not contain as much as 0.0001 percent BeO. Haystack stock, about 55 miles south of Big Timber, is 1 mile south of the old mining camp of Independence IRON MOUNTAIN in Sweet Grass County. The geology has been de­ Iron Mountain is on the eastern flank of the Laramie scribed in detail by Emmons (1908). We made a brief Mountains in sees. 22, 23, and 27, T. 19 N"., R. 71 W., visit to the area to sample the contact zone on the west about 40 miles northeast of Laramie. Geology of the side of the stock. The intrusive body, according to area has been described by Diemer (1941, p. 6-11), and Emmons, ranges in composition from quartz monzonite is shown on figure 47. A north-trending dikelike Hdy to olivine gabbro and extends from Haystack Peak to of titaniferous magnetite 50 to 350 feet wide can be Baboon Mountain, a distance of 3 miles. Limestones, traced for nearly a mile. The adjacent rock is Pre- shales, and sandstones of Cambrian age have been meta­ cambrian anorthosite with some gabbro. Near the morphosed and replaced by tactite at the contact with center of the ore body, a small plug of granite cuts the the intrusive rock. Garnet, epidote, quartz, and actino­ magnetite and anorthosite. The anorthosite and gab­ lite are the principal tactite minerals. A composite bro are fractured and hydrothermally altered on either grab sample (328-923) of tactite from the contact zone side of the ore body at its southern end, where the con­ did not contain as much as 0.0001 percent BeO. tacts are exposed on Chugwater Creek. 156 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES

110° . 108°

<- r_

104°

ALBANY COUNTY PBBMONT COUNTY PLATTE COUNTY 1. Centennial district 8. Fort Washakie area 12. Halleck Creek area 2. Iron Mountain 13. Welcome mine 3. Rambler mine LAEAMIE COUNTY 4. Strong mine SWEETWATEB COUNT? 9. Silver Crown district CARBON COUNTY 14. Leucite Hills NATRONA COUNTY 15. Superior district 5. Encampment district 6. Hanna district 10. Casper Mountain 7. Bawling area 11. Garfield Peak FIGURE 46. Index map of Wyoming, showing localities sampled.

Samples were taken as follows (see fig. 4Y for lo­ 210 Chip sample across magnetite body at top of Iron cations) : Mountain. 328-206 Chip sample across 25 ft of gabbroic anorthosite with 212 Grab sample from outcrop of granite plr

CARBON COUNTY ENCAMPMENT DISTRICT The Encampment mining district is in the Sierra Madre range near the southern boundary of Wyoming. The town of Encampment, from which most of the mines can be reached by road, is in the northeast corner of the district. The geology and ore deposits of the area have been described by Spencer (1903 and 1904) and Platt (1947). Copper deposits related to Prec^m- brian diorite and gabbro intrusive masses occur as sr^all lenses and fracture fillings in Precambrian schist, sis tes, and quartzites. The Doane-Rambler and the Hidden Anorthosite Treasure mines were sampled. Includes some gabbro The Doane-Rambler mine is at the abandoned min­ ing town of Rambler about 18 miles southwest of En­ Contact campment. The ore minerals, chalcocite, chalcopyrite,

V328-209 covellite, bornite, malachite, and azurite, occur as frac­ Locality sampled and ture fillings in quartzite. A composite sample (228- number 882) of dump material contained 0.002 percent E«,O. 328-206, 207 Heavy liquid separations were made and the fractions were analyzed for beryllia. The heavy fraction (spe­ 1000 1000 Feet cific gravity greater than 2.60), composed of chalccT>y- rite, chalcocite, pyrite, bornite, and covellite, contained 0.001 percent BeO. The fraction with specific gravity Geology after Diemer, 1941 less than 2.60 was mainly quartz and malachite and con­ FIGURE 47. Geologic map of Iron Mountain magnetite deposit, Albany tained 0.003 percent BeO. No beryllium minerals v^ere County, Wyo. identified. The Hidden Treasure mine is about 2 miles eas* of RAMBLER MINE the Doane-Rambler mine on the main road to Encamp­ ment. The mine explores a narrow, northeast-trenching The Rambler mine is half a mile west of the aban­ vein at the contact of Precambrian quartzite and diorite. doned mining camp of Holmes, about 12 airline miles Chalcopyrite, chalcocite, calcite, specularite, and side- southwest of Centennial. The geology and ore deposits rite are the principal vein minerals. A grab sample have been discussed by Knight (1902), Emmons (1903), Read (1903), Hess (1926), Coulton (1936) and Oster- (328-885) of dump material showed no beryllium, the limit of detection being 0.0001 percent BeO. wald and Osterwald (1952, p. 28). The mine is developed in an altered zone in Precam- HANNA DISTRICT brian pyroxenite. A sample from the dump containing A grab sample (328-248) of coal was collected f~om covellite, azurite, malachite, quartz, and altered py­ the dump of an open pit mine half a mile east of Hanna roxenite and a grab sample (328-879) of the mill tail­ on U. S. Highway 30. The coal is in the Hanna forma­ ings were obtained. These showed no beryllium, the tion of Tertiary age. The ash was found to contain limit of detection being 0.001 percent BeO. 0.002 percent gallium, 0.0003 percent beryllium and 0.01 percent vanadium. STRONG MINE The Strong mine is 12 airline miles northeast of RAWIJHS AREA Laramie in sec. 4, T. 16 N., R. 71 W. (Osterwald and Two chip samples (328-246, -247), mainly limestone Osterwald, 1952, p. 29). Chalcopyrite, tetrahedrite, taken across the Phosphoria formation (Permian) at molybdenite, azurite, and malachite the principal ore exposures on IT. S. Highway 287 near Rawlins v^ere minerals are associated with pegmatite in Precam- found to contain no beryllium, the limit of detection brian anorthosite. A sample (328-200) of ore from the being 0.001 percent BeO. 158 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES FBEMONTCOUNTY pegmatite dike is exposed in altered serpentine ap­ FOHT WASHAKIE ABEA proximately 3,000 feet east of Eadsville. A chip sam­ ple across 50 feet of altered serpentine and a grab sam­ Samples of a Tertiary lamprophyre dike and altered ple of pegmatite and altered serpentine were taken east sandstone of the Wind Eiver formation adjoining the of the dike. None of the samples contained as much dike were collected at an outcrop on U. S. Highway as 0.001 percent BeO. 287 about 10 miles north of Fort Washakie, "\fVyo. The dike is vertical and strikes N. 45° E.; the average width QARFIELD PEAK is about 20 feet. The sandstone is baked and altered Garfield Peak, the highest mountain in the Battle- for about 2 feet on either side of the dike. A chip snake Bange, is about 6 miles southeast of Er^ay. Car­ sample (328-235) across the dike and a grab sample boniferous limestone has been silicified at the contact (328-237) of baked sandstone contained no beryllium, of a Tertiary monzonite stock. A grab sample (328- the limit of detection being 0.001 percent BeO. 234) of silicified limestone from the contact zone on the northeast side of the peak contained no beryllium, liARAMIE COUNTY the limit of detection being 0.001 percent BeO. SILVEH CHOWN DISTRICT PIiATTE COUNTY The Silver Crown district (Osterwald and Oster- HALLECK CREEK AREA wald, 1952, p. 41-42) is near Hecla, about 20 miles west of Cheyenne on the east slope of the Laramie Moun­ Bock specimens from a prospect on Halleck Creek, a tains. Gold and silver-bearing veins and shear zones in tributary to North Sybille Creek, about 30 miles air­ Precambrian schist and granite gneiss contain chal- line southwest of Wheatland, were rumored to contain copyrite, bornite, azurite, malachite, quartz, pyrite, and more than 1.0 percent BeO. Information obtained limonitej from Mr. A. B. Bartlett of Wheatland, former State The Copper King mine, 1 mile southwest of the Hecla Geologist of Wyoming, enabled the writers to locate the post office in sec. 36, T. 14 N., B. 70 W., was the only prospect, which is on McGill ranch in the northeast mine visited. Chalcopyrite, pyrite, quartz, and limo- corner of T. 21 N., B. 72 W. A ranch ro^.d leading nite are disseminated in a nearly vertical northwest- westward to the area joins State Highway 26 just south­ trending zone of shattered Precambrian granite gneiss west of the bridge across Blue Grass CreeV; the dis­ 20 to 75 feet wide and 600 feet long. A 20-foot chip tance from thejhighway to the prospect is about 6 miles. sample (328-202) taken across the mineralized zone in The regional geology has been described by Fowler a small opencut contained no beryllium, the limit of (1930). A sketch map of part of the prospect area is detection being 0.001 percent BeO. shown in figure 48. A quartz pegmatite and four

NATRONA COUNTY

CASPER MOUNTAIN Granrt. pegmatite

Casper Mountain, in the westernmost part of the Quart! pegmatite Laramie Range, forms a prominent ridge 9 miles south of Casper in the east-central part of Natrona County. Amphibolte

Beeler (1911), Diller (1911a, p. 512-516, and 1911b), Btot to schist Beckwith (1939, p. 822-832), and Stephenson (1941) have described the geology and ore deposits of the area. El Casper Mountain is a westward-trending asymmetrical Qrortztte anticline with steeply dipping sedimentary rocks of ~Contart~ Dfshtd where approximately heittd Paleozoic age on the north side. Large masses of Pre­ .10 Strike end dtp of deevege cambrian serpentine, granite-gneiss, hornblende schist, or sclistosity .60 and metadiabase are cut by later metadiabase and Strike w» dip of joM* X granite pegmatite dikes. Small areas of quartzite of Small prospect pit unknown age occur in the northeast part of the moun­ tain. Asbestos-bearing serpentine and chromite-bear- Locality samrHed end number ing schist have been prospected. A grab sample (328-226) of a metadiabase dike was Geology by I A. Warner and soo 500 Feet V R Wlmartb, October 1949 obtained from an outcrop at the abandoned town of 48. Geologic sketch map of part of Halleck Creek area, Platte Eadsville on the north slope of the mountain. A large County, Wyo. LOCALITIES IN WYOMING 159 granite pegmatite bodies have intruded quartzite, sedimentary rocks, being in part flows and in part in­ marble, biotite schist, and amphibolite; all the rocks trusive sheets and plugs. They are composed cl iefly are Precambrian. The intruded rocks show pro­ of the rare alkali-rich rocks madupite, orendite, and nounced schistosity that strikes N. 25°-30° E. and dips wyomingite. steeply southeast. A pronounced plane of cleavage in The rock at Pilot Butte, 7 miles northwest of Bock the quartz pegmatite is parallel to the schistosity and Springs, is madupite and consists of phlogopite and the cleavage surfaces are coated with a greenish mica. diopside in a potash-rich glass base. A grab sample The granite pegmatites show no cleavage and in places (328-240) from the north side of Pilot Butte showed cut across the schistosity of the intruded rocks. The no beryllium, the limit of the detection being 0.001 marble adjoining the pegmatites contains diopside, ac- percent BeO. tinolite, and yellow garnet. Several prospect pits have Orenda Mesa, a remnant of one of the larger lava been excavated in the quartz pegmatite and altered flows, is 26 miles airline northeast of Eock Springs. marble. Orendite, namecl for the mesa, is a vesicular roek com­ Six samples from the area were analyzed spectro- posed of sanidine, leucite, diopside, and mica. A grab graphically and are described in table 68. Locations of sample (328-244) from the northeast side of the mesa showed no beryllium, the limit of detection being 0.001 TABLE 68. Beryllia in samples from Halleck Creek area percent BeO. BeO Sample Description (percent) Wyomingite, a porphyritic rock composed of leucite, 328-218 Chip sample across 100 ft of quartz pegma­ tite body, near center.______0. 001 diopside, and brown mica forms much of Zirkel Mesa, 221 Chip sample across 50 ft of marble contain­ which is 3 miles south of Orenda Mesa. A sample ing thin layers of schist, quartzite, and amphibolite______. 001 (328-242) collected from the north wall of the mesa 222 Chip sample across quartz pegmatite body_ . 001 showed no beryllium, the limit of detection being 0.001 873 Channel sample across 10 ft of marble and schist containing actinolite, serpentine, percent BeO. mica, and idocrase______. 0011 SUPERIOR DISTRICT 875 Channel sample across 10 ft of marble con­ taining diopside and garnet ______.0010 876 Channel sample across 8 ft of marble con­ Coal is mined from Cretaceous rocks in the vicinity taining actinolite and garnet.______._ . 0013 of Superior, about 15 miles northeast of Bock Springs. The geology of the district has been described by three samples are shown on figure 48; the others were Schultz (1909). A grab sample (328-245) of coal was obtained at prospect pits a short distance north of the obtained from the bunker at the Copenhagen mine in mapped area. Petrographic studies did not reveal any Superior. The ash contained 0.004 percent gallium, beryllium minerals in the rocks. 0.0004 percent beryllium, and 0.008 percent vanadium. WELCOME MIKE COLORADO The Welcome mine, half a mile east of Guernsey, ex­ plores a small replacement body of hematite in a lime­ By L. A. WARNER and V. B. WELMARTH stone bed of the Guernsey formation of Devonian and Mississippian age. A 6-foot channel sample (328-872) Field investigations of the occurrence of beryllium of hematite taken across the face of the lower adit at in nonpegmatite rocks and mineral deposits in Colo­ the mine contained no beryllium, the limit of detection rado were carried on during the fall of 1948 and the being 0.001 percent BeO. summer of 1949. Forty-five localities were examined, (see fig. 49) and about 550 samples of rocks and min­ SWEETWATEB COUNTY erals were collected for laboratory studies. Mo^t of the localities are in mining districts in central and LETTCITE HILLS southwestern Colorado, and the samples are primarily The Leucite Hills, in southwestern Wyoming, are a from ore deposits; some samples of sedimentary, igne­ series of buttes and mesas formed from Tertiary vol­ ous, and metamorphic rocks also were obtained. Par­ canic rocks of extraordinary composition. They ex­ ticular attention was paid to manganiferous vein de­ tend from Pilot Butte, near Rock Springs, northeast­ posits in the San Juan region, because helvite had been ward for 30 miles to Steamboat Mountain. The geolo­ reported in such veins at the Sunnyside mine near gy of the region nas been described by Cross (1897), Eureka. The alkalic rocks of Iron Hill in Gunnison Kemp and Knight (1903), and Schultz and Cross County, from which beryllium had been reported, also (1912). The fine-grained volcanic rocks of the Leucite were studied in detail. The occurrence of beryl in Hills rest on or cut through Cretaceous and Eocene quartz veins at Mount Antero, Chaffee County, had 160 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES

108° 106° 104° 102°

| EXPLANATION ""* ' ' Locality sampled for this report

40'

,0d£^^ >^4 -i )-^^~- ty'^ Glenwood 7^- r j5 (*4* 4-«/ !iii? A Ii

xr oc°|orad< >>^ "j Springs - 1

38< 38° ----a/V?&*^

120 Miles

Boulder County Gunnison County Ouray County 1. Lafayette area 17. Crested Butte district 32. Ouray district. 18. Gold Brick district 33. Red Mountain district Chaffee County 19. Iron Hill 34. Upper Uncompaghre district Calumet mine 20. Italian Mountain Geneva claim 21. Snowmass Mountain Park County Monarch district 22. Tincup district Mount Antero 23. Tomichi district 36. Tarryall district Ouray Peak Sedalia mine Winfleld district Hinsdale County Pitkin County 24. Lake City district 36. Redstone area Clear Creek County Georgetown district Huerfano County Saguache County Conejos County 25. Wakenburg area 37. Bonanza district 10. Platoro-Summitville district Lake County San Juan County 26. Climax mine Costilla County 38. Eureka-Animas Forks district 39. Mineral Point district Grayback district LaPlata County La Veta area 40. Silverton district 27. Durango area Custer County San Miguel County Las Animas County Querida district 41. Ophir district 28. Morleyarca Dolores County Summit County Rico district Mineral County 42. Breckenridge district Fremont County 29. Creede district 43. Montezuma district 30. Wagon Wheel Gap 44. Upper Blue River district Florence-Canon City area Garfleld County Montezuma County Teller County Rifle-Silt area 31. Bush Basin 45. Cripple Creek district FIGURK 49. Index map of Colorado, showing localities sampled. LOCALITIES IN COLORADO 161 been previously investigated by J. W. Adams of the 004 Chip sample across garnetized inclusion of Weber for­ Geological Survey. A brief summary of his findings mation in sill. 007 Chip sample across 25 ft of banded epidote-magn^tite is included in this report. None of the deposits sampled tactite. in Colorado are of present commercial interest for their 008 Chip sample across 25 ft of magnetite ore and diop- beryllium content. side-epidote tactite. 009 Chip sample across 15 ft of banded actinolite-mag­ BOTJIJXER COUNTY netite tactite. COAL DEPOSITS Spectrographic analyses showed no beryllium in any Coal is mined in southeastern Boulder County, prin­ of the samples, the limit of detection being 0.001 per­ cipally in the vicinities of Louisville and Lafayette, cent BeO. from the lower part of the Laramie formation of Late Cretaceous age. The regional geology of the coal de­ A-0 v// \ <, ,| posits has been discussed by Martin (1910). Fault -A \ ~ I, * n^ Samples of coal from the Black Diamond and Wash­ ington mines were collected and the ashes were analyzed for beryllium. Ash of coal from the Black Diamond mine at Lafayette (sample 328-357) contained 0.004 percent gallium, 0.01 percent vanadium, and no beryl­ lium, the limit of detection being 0.0001 percent beryl­ lium. Ash from a grab sample of coal (328-358) col­ lected at the Washington mine, 7 miles northeast of Lafayette, contained 0.0003 percent beryllium, 0.003 percent gallium, and 0.01 percent vanadium.

CHAFFEB COUNTY

CALUMET MINE The Calumet iron mine (Behre, Osborn, and Rain­ water, 1936) is about 8 miles airline northeast of Sal- ida. A geologic map of the immediate vicinity of the mine is shown in figure 50. Mississippian limestone has been marmorized, and partially replaced by magnetite, epidote, actinolite, tre- molite, garnet, pyrite, and chalcopyrite at or near its ±328-004E-~ Geology by L. A. Warner and contact with a Tertiary granodiorite sill. Much of the Garnet V. R. Wilmarth, September 1948 rock in the contact zone is banded magnetite-bearing tactite. In the northern opencut, a zone 25 feet wide EXPLANATION composed of alternating layers, as much as 6 inches SEDIMENTARY ROCKS . Contact thick, of actinolite and magnetite, occurs in the lime­ ZJasAerf where approximately stone below the granodiorite. The actinolite-magnetite located zone is bounded on the west by a fault zone 5 feet wide that contains abundant kaolinite. In the southern open- Strike and dip of beds cut adjoining the granodiorite sill is an epidote-rich rock containing stringers and bands of magnetite, sev­ E eral of which are more than 1 foot thick. A small body Vertical shaft of low-grade massive magnetite ore is exposed between the two cuts. Opencut Six samples were collected at the mine (see fig. 50) as follows: \329-009 Magnetite Locality sampled and number 328-001 Chip sample across 20 ft of banded epidote-actinolite rock in the Weber formation above granodiorite sill. 50 100 Fe«t 002 Chip sample across 4 ft of magnetite ore containing epidote. FIGURE 50. Geologic map of Calumet mine, Chaffee County, Cdo. 467945 58 -12 162 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES GENEVA CLAIM from 2 to 4 feet in width and can be traced along the The Geneva claim is about 18 miles airline southwest strike for about 1,500 feet. It contains mainly limonite, of Buena Vista on the north side of South Cottonwood pyrite, galena, and sphalerite in a gangue of quartz. Canyon. According to Worcester (1919, p. 46), a block A composite grab sample (328-012) of the vein ma­ of dolomitic limestone about one-eighth mile wide and terial showed no beryllium, the limit of detection more than a mile long has been tilted into a vertical being 0.001 percent BeO. position between granite walls along a large fault. The Figure 51 is a generalized geologic sketch map of limestone has been extensively brecciated and altered the area near the head of Taylor Gulch. Th> Tomichi adjacent to the granite. It grades from coarsely crys­ talline marble into tactite containing serpentine, gros- EXPLANATION sularite, diopside, phlogopite, and minor quantities of chalcopyrite, pyrite, and molybdenite. The tactite SEDIMENTARY ROCKS grades into a zone 15 feet wide of black hornfels that formed next to the granite contact. Narrow veins of Tomichi limestone, secondary calcite fill fractures in the marble. Adja­ of former us age cent to the contact the granite shows well-developed IGNEOUS ROCKS foliation which parallels the limestone bedding. Three samples collected at the main workings are as Quartz monzinite follows: (328-711) a chip channel across the black quartzitic rock, (329-709) a channel sample across the r/: tactite zone, and (328-712) a grab sample of metallic Granite minerals from the dump. None of the samples con­ Contact tained as much as 0.0001 percent BeO. Dashed where approximately located

MONARCH DISTRICT Vein

The Monarch district is in the southwestern part of _50 Chaffee County, on the east slope of the Sawatch Range, Strike and dip of beds and joins the Tomichi district on the west. Mines and prospects in the Taylor Gulch, Cree Camp, and Hoff- Vertical srnft man Park areas were investigated briefly. Crawford / X " O'»/ Prospect pit (1913, p. 195-283) has described the geology of the 328-01J/ T>[ \'x0'0" »/ region in detail. The Tomichi limestone (Ordovician) I -,\ »^ix 328-015 B ~ ''v IN Locality samoled of former usage, Our ay limestone (Devonian), and and number Garfield formation of Crawford (1913) (Pennsyl- vanian) are folded into a north-trending syncline. Precambrian granite crops out east of Taylor Gulch Geology by L. A. Warner and and intrusive Tertiary quartz mbnzonite cuts off the V. R. Wilmarth, October 1948 sedimentary rocks to the north and west. The New York mine, on the west side of Taylor 400 800 Feet I Gulch, is at an altitude of 12,000 feet. An adit was L_ driven on an oxidized zone in the Garfield formation FIGURE 51. Geologic sketch map of area near head of Taylor Gulch, Chaffee County, Colo. of Crawford (1913) near its contact with the Ouray limestone. The dump rock consists of indurated sand­ stone and some limestone containing actinolite, garnet, limestone of former usage has been marmorized and and epidote. A small pile of ore, mainly sphalerite, partially replaced by garnet, actinolite, and epidote galena, and chalcopyrite, was noted on the dump. A near a Tertiary quartz monzonite dike and along the composite grab sample (328-011) from the dump contact of the limestone with Precambrian granite. showed no beryllium, the limit of detection being 0.001 Two veins containing magnetite, quartz, and tactite percent BeO. minerals cut the limestone in the area between the dike About 500 feet east of the New York mine, several and the granite. The contacts of the veins, dike, and prospect pits and shallow shafts expose a northeast- granite all trend north, parallel to the strike of the trending vein in the Ouray limestone. The vein ranges limestone. LOCALITIES IN COLORADO 163 None of the four samples described below contain phenakite, and bertrandite, but they do not appear to be as much as 0.001 percent BeO. of sufficient size to be of interest as a commercial source 328-013 Grab sample of tactite from pit near base of Tomichi of beryllium. limestone. At the California mine, 2 miles southwest of Mount 014 Grab sample of tactite from pits near contact with Antero, a quartz vein containing molybdenite and b<>,ryl granite. 015 Grab sample of tactite and vein material from dump occurs in a quartz monzonite stock. Mineralogical of shaft. study shows that some of the beryl was deposited ^ith 016 Chip sample of magnetite and tactite from vein out­ molybdenite. Molybdite is closely associated ^ith crop. molybdenite. Brannerite, an oxide of titanium and In the Cree Camp area, the Garfield formation of uranium, was identified in the material collected. The Crawford (1913) has been metamorphosed to quartzite, mine was operated on a small scale during World ^Tar hornfels, marble, and tactite. A composite chip sample I, but the surface cuts were caved and the mine work­ (328-020) collected from Crawford's Garfield forma­ ings were inaccessible in June 1948. Where exposed, tion on the cliff west of Cree Camp represents tactite the vein at the California mine is 1^ to 3 feet thicv, is zones 1 to 10 feet wide which are separated by wider nearly vertical, and strikes N. 72°-75° E. Early re­ zones of marble and hornfels. A grab sample (328-021) ports of the mining and the material seen on the dump was taken of dark-brown garnet, graphite, epidote, ido- indicate that rich molybdenite ore was accompanied by crase( ?), and quartz from near the base of Crawford's considerable beryl, but no accurate appraisal of the Garfield formation just west of Cree Camp. None of beryl reserves can be made without reopening the nine the samples contain as much as 0.001 percent BeO. workings and trenching the surface. The Royal Purple and Nest Egg claims in Huffman A channel sample taken across the vein at the Cali­ Park, a large glaciated valley about 4 miles northwest fornia mine contained 0.016 percent BeO. A composite of Garfield, were also visited. The rock in this area sample of granite from the north slope of White Moun­ is quartz monzonite, of the large Princeton batholith tain and one of greisen from an outlying granite r^ass of Tertiary age. Worcester (1919, p. 38-39) briefly contained 0.018 and 0.015 percent BeO, respectively. described the ore deposits. The abandoned workings The results obtained for these samples were not verified on the Royal Purple claims are at an altitude of 11,850 by analyses of 14 additional samples of granite and feet, about 2,000 feet northeast of a cabin at the end greisen from the main stock and outlying bodies. The of the road. Two vertical quartz veins strike N. 50° E. 14 samples had BeO contents ranging from less than The southern vein, where exposed in a shaft, is 8 feet 0.0003 percent to a maximum of 0.0006 percent, indict­ wide and contains molybdenite in small pockets, flakes, ing that the average BeO content of the granite is p^ob- and stringers along the walls. Pyrite is locally abun­ ably very low. dant. A channel sample (328-699) across the vein OTTRAY PEAK in the shaft contained 0.0005 percent BeO. The other vein was not sampled. A large granite pegmatite dike, about a mile long and The Nest Egg claims are 2,000 feet northwest of the 500 to 1,500 feet wide, intrudes Precambrian quartz- Royal Purple claims. The main opencut is at the junc­ muscovite-biotite schist at Ouray Peak, 15 miles airline tion of two faults; one strikes N. 25° E. and dips 27° southwest of Salida. Grab samples of the schist ("98- NW., the other strikes N. 35° E. and dips 85° NW. 707) and the pegmatite (328-704 and -706) taken near Molybdenite occurs as small clots and stringers in the the contact showed no beryllium, the limit of detection hanging walls of the two faults. It impregnates the being 0.0001 percent BeO. quartz monzonite for as much as 2 feet beyond the faults. A grab sample (328-700) of molybdenite-bear­ SEDALIA MINE ing material from the dump showed no beryllium, The Sedalia mine is 8 miles northwest of Salidr, on the limit of detection being 0.0001 percent BeO. the east side of the Arkansas Valley at an altitude of MOUNT ANTEKO AREA 7,500 feet. Lindgren (1908, p. 161-166) described the ore deposit as a thick bed of actinolite schist, 800 feet By J. W. ADAMS long and 150 feet thick, richly impregnated by copper Pegmatites commonly containing beryllium minerals minerals. The most productive part of the depos:t is occur in a granite stock in the vicinity of Mount Antero above a pegmatite dike that cuts the schist. A grab and White Mountain, Chaffee County, Colo. (Adams, sample (328-600) of dump material containing alman- 1953). These pegmatites have been known for many dite, actinolite, chlorite, idocrase, epidote, and copper years as a source of fine specimens of aquamarine, minerals contained 0.0004 percent BeO. 164 OCCURRENCE OF NONPEGMATITB BERYLLIUM IN THE UNITED STATES

WINFIELD DISTRICT CONEJOS COUNTY The Winfield district is on Clear Creek, 14 miles PLATORO-STJMMITVILLE DISTRICT west of Granite. The largest mines are west and south­ The Platoro-Summitville district is in r.n eastern west of Winfield. The geology and ore deposits of the extension of the San Juan Mountains in the northern district have been described by Worcester (1919, p. 40- part of Conejos County and the southern p^rt of Rio 43) and Vanderwilt (1947, p. 48). Small veins in the Grande County. Del Norte, the nearest railhead, is 30 Twin Lakes quartz monzonite porphyry of Howell miles to the northeast. The geology and or?, deposits (1919) which is of Tertiary age, have been mined for were described by Patton (1917), and Vanderwilt (1947, gold, silver, lead, and copper. Quartz veins containing p. 63,184-186). Only igneous rocks are exposed in the molybdenite and bismuthinite are also present. A brief district. The extrusive rocks, part of the Hinsdale examination was made of the Swiss Boy mine and the formation and Potosi series of Tertiary age, include Banker Tunnel, which represent the two types of min­ rhyolite, latite, andesite, basalt, and biotite latite. Near eralization in the district. the center of the district, monzonite and monzonite por­ The Banker Tunnel is 2 miles south of Winfield on phyry stocks are exposed, and in the northern part is a the South Fork of Clear Creek. The mine was operated small stock of biotite-augite diorite. Large r.reas of in­ in 1948 and a small quantity of silver ore was produced. tensely altered volcanic rocks occur near Stunner in the Molybdenite and bismuthinite, with minor amounts of central part of the district. The principal alteration pyrite, clay, and sericite, occur as streaks and pockets processes are kaolinization, sericitization, and aluniti- along the walls of quartz veins. A grab sample of silver zation. Gold-bearing veins that also yield sm all quanti­ ore (328-715) was found to contain 0.0008 percent BeO. ties of lead-zinc-silver ores have been mined near a A sample (328-716) of molybdenite and bismuthinite monzonite intrusive body. ore contained 0.0011 percent BeO. The Miser mine is about half a mile west of Jasper The Swiss Boy mine is 3 miles east of Winfield 011 the in the northeast part of the district. The caved mine north side of Clear Creek valley. The upper adit is on workings were reported to have been developed on gold- a narrow quartz vein which strikes north and dips 70° and silver-bearing quartz veins in altered biotite latite. E. The ore minerals are galena and sphalerite. The The ore consists of galena, chalcopyrite, sphrlerite, and lower adit is on a brecciated fault zone that parallels minor amounts of pyrite. A grab sample (328-594) of the quartz vein. Galena, sphalerite, pyrite, and tetra- ore was taken from the dump. hedrite fill small fractures in the fault breccia. A grab The Red Mountain No. 1 mine is about 1 mile north­ sample (328-719) of ore from the bin showed no beryl­ east of Stunner on the north side of the Alamosa River. lium, the limit of detection being 0.0001 percent BeO. The mine is altered in quartz monzonite porphyry. A A sample (328-720) of pale-green crystalline fluorite 2-foot wide quartz vein containing pyrite, chalcopyrite, from a small vein southeast of the Swiss Boy mine did and a minor amount of galena is exposed at the face not contain as much as 0.0001 percent BeO. of the adit. A channel sample (328-595) was taken across the vein. CI*EAR CREEK COUNTY At Summitville the Reynolds mine and mill were GEORGETOWN DISTRICT sampled. The mine was inaccessible, and only a grab sample (328-597) of ore from the ore bunkers was ob­ The geology of the Georgetown quadrangle has been tained. Galena, chalcopyrite, pyrite, covellite, and described by Spurr, Garrey, and Ball (1908) and by sphalerite in a quartz gangue make up tH ore. A Lovering and Goddard (1950, p. 138-153). Except for sample of mill tailings (328-598) was taken from the small stocks and dikes of Laramide age, the rocks of Reynolds mill. the district are Precambrian and consist of schists and gneisses of the Idaho Springs formation that have been None of the 3 samples obtained from this area contain intruded by granitic batholiths. At many places cal­ as much as 0.0001 percent BeO. careous lenses in the Idaho Springs formation have COSTIIdLA COUNTY been altered to tactite, containing garnet, diopside, epi- dote, hornblende, and locally pyrite and magnetite. A GRAYBACK DISTRICT grab sample (328-111) of tactite from talus slopes east The Grayback mining district is in the northern part of Clear Lake, 6 miles south of Georgetown, showed no of Costilla County, about 5 miles north of the village beryllium, the limit of detection being 0.0001 percent of Russell. The geology of the area was described by BeO. Patton, Smith, Butler, and Hoskin (1910). Lime- LOCALITIES IN COLORADO 165 stones, sandstones, and shales of Carboniferous age zonite porphyry body. A chip sample (328-169) across overlie Precambrian gneiss and schist that crop out in the tactite zone showed no beryllium, the limit of detec­ the southwestern part of the district. Tertiary intru­ tion being 0.001 percent BeO. sive rocks ranging in composition from diorite to felsite cut the sedimentary rocks. The principal ore deposits LA VETA AREA of the district are narrow low-grade gold veins in the A grab sample of coal was obtained at a mine 5 miles Carboniferous sedimentary rocks. Small bodies of west of La Veta on U. S. Highway 160. The ash of magnetite occur in tactite adjoining a monzonite por­ the sample contained 0.0004 percent beryllium, C.004 phyry intrusive body at the Star of the West claims in percent gallium, and 0.01 percent vanadium. The coal the southwest slope of Grayback Mountain (fig. 52). is from the Vermejo formation of Late Cretaceous age.

OUSTER COUNTY

QUERIDA DISTRICT

:">=-328-l66 The Querida (Bosita) district is in the Bosita Pills Stor °f the West, upper adit about 14 miles east of Silver Cliff and 25 miles sonth- west of Canon City. The Bosita Hills are a series of ,.., -- ~ *i*?.: 328-167 A:-l^^^' AS»or of the West, adit eroded andesite and rhyolite flows and agglomerates / Star 'of the' West, lower edits resting on Precambrian granite and schist. The f ows EXPLANATION are presumed to be from a local source and pipe^ of

Strike and dip of beds agglomerate in the area may be the necks of volcaroes. Monzonite porphyry Veins containing silver, with some lead, copper, and Portal of adit x gold, occur chiefly in the volcanic rocks. Galena, pyrite, Undifferentiated rocks Prospect pit Stippled where altered and barite are the principal minerals. 328-167 Contact Locality sampled and number A grab sample (328-173) of mill tailings was col­ Dashed where approxi­ lected from an abandoned mill on State Highway 96 mately located near Querida. The BeO content of the sample was 1000 2000 Feet 0.0005 percent. FIG DEB 52. Geologic sketch map of vicinity of Star of the West workings, Grayback district, Costilla County, Colo. DOLORES COUNTY

RICO DISTRICT The Upper Star of the West adit is near the top of Grayback Mountain, about 1,000 feet vertically above The Rico district centers around the town of Bico in Grayback Gulch. Magnetite has replaced a limestone the eastern part of Dolores County. The principal arti­ bed near the monzonite porphyry body. Overlying the cles relating to the geology and ore deposits of the dis­ ore body is a 10-foot thick zone of silicified limestone trict are those by Cross, Howe, and Bansome (If05), and shale which have been partially replaced by epidote, Cross and Spencer (1900), McKnight (1932), Ran- andradite, chlorite, and actinolite. A channel sample some (1901a), and Varnes (1944). Sedimentary rocks (328-166) across the altered sedimentary rocks showed ranging in age from Proterozoic to Jurassic arc in­ no beryllium, the limit of detection being 0.001 percent truded by sills of hornblende monzonite porphyry and BeO. a stock of quartz monzonite. The sedimentary forma­ The Star of the West adit, 150 feet vertically below tions, especially the Ouray limestone (Devonian), have the Upper Star of the West, is developed on a 6- to 10- been metamorphosed adjacent to the stock. Silver, lead, foot-thick magnetite body that strikes F. 75° E., and zinc, and gold ores have been produced from firsure dips 35° to the south. A 15-foot-thick zone of tactite veins and blanket-type deposits. is exposed above the ore in the adit. Fo beryllium was Considerable tactite is exposed in the Smuggler mine found, limit of detection being 0.001 percent BeO, in on the west side of the Dolores Biver at Bico. The a channel sample (328-167) across the tactite zone. Ouray limestone has been replaced in part by chlorite, About 1,000 feet west of the Star of the West adit, specularite, epidote, and garnet. Galena, sphalerite, a group of workings on the Lower Star of the West and chalcopyrite are the ore minerals. A grab sam­ claim explores the contact zone. Magnetite ore, aver­ ple (328-157) of tactite from the dump showed no aging 5 feet in thickness, and a tactite zone 12 feet beryllium, the limit of detection being 0.001 percent thick are exposed along the northwest side of the mon­ BeO. 166 OCCURRENCE OP NONPEGMATITE BERYLLIUM IN THE UNITED STATES FREMONT COUNTY and ore deposits of the district were discussed by Hill FLORENCE-CANON CITY AREA (1909, p. 32-34), and Crawford and Worcester (1916). Two mines the Carbonate Camp and the GoM Links ­ Samples of coal were obtained at two mines, the were visited. Brookside and the Double Dick, in the Florence-Canon The Carbonate Camp mine is near the head of Alder City area. The coal is in the Vermejo formation of Late Creek, about 5 miles airline northwest of Ohio City. Cretaceous age. The geology of the area and the occur­ The abandoned mine is in Leadville limestor-} (Missis- rence of the coal were described by Washburne (1910). Ash of the coal sample (328-171) from the Brookside sippian) that has been replaced in part by magnetite, garnet, and diopside. Small quantities of calamine mine contained 0.0006 percent beryllium, 0.004 percent gallium, and 0.007 percent vanadium. Ash of the sam­ were noted on the dump. A grab sample (328-664) ple (328-172) from the Double Dick mine contained of dump rock showed no beryllium, the limit of detec­ 0.0002 percent beryllium, 0.004 percent gallium and tion being 0.0001 percent BeO. 0.01 percent vanadium. Lead, zinc, and gold were the principal metals pro­ duced from vein deposits at the Gold Links mine, about GABFIELD COUNTY 5 miles north of Ohio City. A grab sample (328-666)

RIFLE AND SILT AREA of mill tailings from the Gold Links mill showed no beryllium, the limit of detection being O.OO')! percent Three coal mines in the Grand Hogback coal field BeO. (Gale, 1910, p. 109-136) north of Eifle and Silt were IRON HILL AREA sampled. The coal is in the Mesaverde formation of Late Cretaceous age. Ash from a grab sample (328- A small composite stock of alkalic rocks occurs at 093) of coal obtained at an abandoned mine 10 miles Iron Hill in the southern part of Gunnison County, north of Silt contained 0.0009 percent beryllium, 0.004 near Powderhorn post office. A 3-mile grave1 road con­ percent gallium, and 0.02 percent vanadium. Ash of nects this area with County Highway 149, a gravel a coal sample (328-095) from a mine 7 miles northeast road that leads to lola, a distance of 20 miles. Gunni­ of Eifle contained 0.0009 percent beryllium, 0.005 per­ son, the nearest city, is 22 miles airline to the northeast cent gallium, and 0.01 percent vanadium. A channel and can be reached from lola by way of paved U. S. sample (328-096) was obtained from a 3-fcot-thick coal Highway 50. ' bed exposed in the lower adit of a coal mine near the The Iron Hill area has been described ir detail by reservoir, 8 miles north of Silt. The ash contained Larsen (1942), who mapped the geology and made ex­ 0.0004 percent beryllium, 0.005 percent gallium, and tensive laboratory studies of the rocks. In connection 0.008 percent vanadium. with this work spectrogaphic analyses of many rock and .mineral specimens were made by George Stei

f Oa

Granite, gneiss, and amphibolite

12 Locality number

Percent bcryllia e <0-001 > 0-001 <0-005 A .Q-005

R. 2 W. Map after E. & Lanen. Jr., 1842. pL 1

FIQUBB 53. Geologic map of Iron Hill area, Gunnison County, Golo. 168 OCCURRENCE OF NONPEGMATITB BERYLLIUM IN THE UNITED STATES direction) and 4 miles wide at its widest part. Iron calcite, and zeolites are common and owe their origin Hill, in the central part of the stock, is a mass of dolo- to alteration of the nepheline. mitic marble that rises about 1,000 feet above the Ce- Soda syenite makes up about 2^ percent of the in­ bolla Creek valley. In an irregular and discontinuous trusive rocks and is later than the ijolite. It occurs aureole along the contact with intrusive rocks, the mar­ as dikes and irregular masses, generally near the ble contains aegirite, phlogopite, and soda amphibole. periphery of the stock. The syenite is a light-gray The marble closely resembles later carbonate veins which medium- to coarse-grained rock consisting chiefly of cut it and the surrounding intrusive rocks. Larsen microperthite, with small amounts of aegirite or soda favors a hydrothermal origin for the marble, and pre­ amphibole and some apatite, fluorite, and sphene. sumes that it may have been deposited in the open Much of the syenite is banded or streaked from granu­ throat of an old volcano. lation during or immediately after intrusion. The oldest intrusive rock of the stock is uncompagh- Nepheline syenite underlies an area of 0.3 square rite, a coarse-grained rock which occurs in irregular mile along the northeastern border of the stock. It bodies and dikelike masses that have been cut by later occurs as dikes and irregular bodies intruded into py­ intrusive rocks. It underlies an area of about 0.6 roxenite, soda syenite, and Precambrian ro".ks. The square mile in the southern part of the basin of Beaver rock consists predominantly of albite and microcline. Creek. The average specimen contains about 70 per­ Other minerals recognizable in hand specimen are cent melilite, 15 percent diopside-hedenbergite, and 10 nepheline, apatite, sphene, biotite, magnetite and aegi­ percent magnetite, the remainder being chiefly apatite, rite. Locally the nepheline syenite has be^n altered perovskite, phlogopite, and calcite. The composition and contains cancrinite and zeolites. varies considerably from place to place, and the color The latest intrusive rocks consist of dikes of in hand specimen ranges from light gray for the meli- nepheline gabbro and quartz gabbro which are most lite-rich variety to dark greenish for specimens rich in abundant in the valley of Deldorado Creel" north of pyroxene. In places the uncompaghrite has been Iron Hill. The nepheline gabbro is a dark coarse­ altered by a series of complex hydrothermal reactions grained rock containing tabular crystals of labradorite, to a rock containing diopside, colorless garnet, ido- interstitial pyroxene, and smaller amounts of nepheline crase, and calcite. and olivine. The quartz gabbro is finer grained and Pyroxenite is the most abundant rock of the complex consists of labradorite and pink titaniferous augite and and is later than the marble and uncompahgrite. It small amounts of intergrown quartz and orthoclase. underlies about 9.4 square miles, the largest exposure Hydrothermal activity accompanied and followed in­ being east of Iron Hill in the drainage basins of Del- trusion, and alteration products are widespread in the dorado and Beaver Creeks. The rock is quite variable, various rock types. The more common hydrothermal both in texture and in mineral composition. The domi­ minerals include aegirite, sodic amphibole, phlogopite, nant variety contains about 60 percent pyroxene, 15 apatite, garnet, idocrase, diopside, zeolites, aFHe, ortho­ percent biotite, and 10 percent each of magnetite, and clase, carbonates, quartz, fluorite, and sulfic'Qs. Veins perovskite, with lesser amounts of apatite and ilmenite. are common in the intrusive rocks of the stocV and some Other varieties contain nepheline, orthoclase, or albite occur in the central mass of marble and in tho surround­ and locally as much as 30 percent sphene. In places ing Precambrian rocks. The major veins arc a few feet difeelike bodies consisting of magnetite and perovskite, wide and can be traced for nearly a mile, but many are with apatite, biotite, and pyroxene, cut the other rocks; smaller. Many of the veins are similar in composi­ some small dikes contain as much as 90 percent apatite. tion to the central carbonate mass and con^st largely Magnetite and perovskite in lenslike bodies are com­ of dolomite, with some calcite and ankerite. Locally monly associated with the apatite- and biotite-rich they contain sulfides, limonite, apatite, and silicate rocks. Masses of biotite pyroxenite containing as much minerals; in places they have been prospected for silver. as 98 percent biotite were mined during World War In some veins lime-silicate minerals are dominant and II for mica. the vein filling closely resembles the material in the Ijolite occurs as dikelike and irregular masses that contact-metasomatic aureole of the Iron Hill marble. cut the uncompahgrite and pyroxenite. It makes up Other veins consist largely of martite and apatite, with about 3 percent of the intrusive rocks. The largest area small amounts of limonite and carbonates. These grade of outcrop, about 0.1 square mile, is west and south of into veins and irregular bodies rich in iron oxides and the main forks of Beaver Creek. The chief mineral chalcedony or opal. Manganese oxides are present constituents are nepheline, titanif erous garnet, and dark locally, and rarely piedmontite. The mar^ite-apatite diopside, but the proportions vary greatly. Cancrinite, veins and siliceous iron-oxide veins are best developed LOCALITIES IN COLORADO 169 in the marble mass of Iron Hill, where they have been most samples the lower limit of detection was 0.001 prospected for iron. percent, and fewer than half the samples contained as

OCCTTBBENCE OF BERYLLIUM much as 0.001 percent. For a few samples the lower limit of determination was 0.0001 percent and for still Fifty-four samples of various rock types in the Iron fewer it was 0.004 percent. Distribution of beryllium Hill area were analyzed spectrographically for BeO. in the various rock types is shown in table 70. Descriptions of the samples and analytical results are given in table 69. The locality numbers refer to sample TABLE 70. Distribution of beryllia in rock types at Iron Hill, locations shown on figure 59. The BeO content ranges Colo. from 0.0098 percent to less than 0.0001 percent. For Number samples BeO (percent) TABLE 69. Beryllia in samples from Iron Hill, Colo. Pock type analyzed High Low Avercoe Marble and carbonate [Analyses by National Spectrographic Laboratories, Cleveland, Ohio, and Saratoga Laboratories, Saratoga Springs, N. Y.] veins: BeO Calcite-dolomite Locality Sample Description (percent) type______8 0.001 -0.001 -0.001 No. Lime-silicate type _ 9 . 0033 -.001 ±.001 nfig. 63 Siliceous iron-oxide 1 328-34 Ijolite__---______-___.__-___-_ <0. 001 type____------4 .0097 .002 .0048 2 35 ____do_- --._ - <. 001 Uncompahgrite : 3 36 -_-_do______<. 001 Unaltered_._._____. 5 .0098 .001 .0035 4 36 A Vein (mainly calcite-dolomite) _ <. 001 Altered______5 .002 -.001 ±.001 5 38 Altered uncompahgrite______<. 001 Pyroxenite: 6 39 Uncompahgrite ______- .003 Normal pyroxenite: 7 40 Uncompahgrite (pyroxene-rich) __ . 0098 Unaltered ___ _ 4 -.001 -.001 -.001 8 41 Vein (siliceous iron oxide) __ __ .002 AH-f»T>»rl 9 _ ftftl flfll _ fM11 9 42 Vein (lime-silicate type) ______<. 001 Biotite pyroxenite: 10 43 Uncompahgrite______. OOOX Unaltered. ______1 ______-.001 11 44 Pyroxenite-_-___-______--__--- .OOOX Altered... ______1 ______... .0075 12 45 Biotite pyroxenite______- -__-- <. 001 Ijolite: 13 46 Altered biotite pyroxenite __ __ .0075 Unaltered ______5 -.001 -.0001 -.001 14 49 Pyroxenite ______<. 001 Altered.______1 ______.001 15 50 Vein (mainly quartz) __ -___ <. 001 Soda syenite ______2 . OOOX . 0005 ± . 0005 16 51 Nepheline syenite ______<. 004 Nepheline syenite. _ _ 2 - . 004 - . 00 1 - . 00 1 17 52 -__-do------_----_------<. 001 18 53 Soda syenite. ______.OOOX Nepheline gabbro. ___ 1 ______<. 0001 19 54 Altered pyroxenite______<. 001 Quartz gabbro _ _ _ 1 ______<. 0001 20 55 Vein (mainly calcite-dolomite) ___ <. 001 Apatite-rich dikes ___ 2 <. 0001 <. 0001 <. 0001 22 57 Altered uncompahgrite. ____ .__ <. 001 23 60 Ijolite__--_-______._--- .OOOX The analytical data indicate that beryllium is concen­ 24 61 Marble (mainly calcite-dolomite) _ <. 001 trated mainly in the siliceous iron oxide veins. The 25 62 Uncompahgrite (melilite-rich) _._ <. 001 26 63 Vein (mainly calcite-dolomite) _ <. 001 BeO content of 4 samples of these veins ranges from 27 64 Vein (lime-silicate type) --___-_ . 0009 0.002 percent to 0.0097 percent, the average being 0.0048 28 65 Marble (lime-silicate rock)__- __ <. 001 29 68 Vein (lime-silicate type) -_-_-- _ <. 001 percent, which is higher than the content of any other 30 69 Altered marble (siliceous iron rock type for which a comparable number of samples oxide)______-__ ___-_.__ . .0035 31 70 Marble (calcite-dolomite rock) _ <. 001 was obtained. The average BeO content for other r?in 32 71 Altered marble (lime-silicate rock types is 0.001 percent or less. The nature of the beryl­ 33 72 Vein (lime-silicate type) _ __ _ _ <. 001 lium-bearing material in the veins has not been de­ 34 73 Vein (siliceous iron oxide) _ __ _ .004 termined. The siliceous iron oxide veins appear to re­ 35 74 Marble (lime-silicate rock) _ _ _ _ . 0006 36 75 _-_-do___-______<. 001 semble somewhat the ocherous beryllium-bearing ma­ 37 76 Marble (calcite-dolomite with terial in the manganese-tungsten deposits of Golcorda, bands of lime-silicate rock) _ _ <. 001 38 77 Altered marble (siliceous iron Nev., in which beryllium and tungsten are presumed to oxide)-- -____.__-_---__ - .0097 be adsorbed in colloidal masses of silica and mangan^se- 39 500 Pvroxenite______----______<. 0001 40 504 Apatite-rich dike in pyroxenite-- <. 0001 iron oxides or hydroxides. The deposits at Golcorda, 41 505 ---_do__----_-__-_--_____-.-- <. 0001 jNTev., are thought to be underlain at depth by high-tem­ 42 506 Granite gneiss (Precambrian coun­ try rock)______.0005 perature veins or tactite bodies containing tungsten and 43 508 Soda syenite. ______- __ _ .0005 beryllium from which these metals may have been 44 510 Nepheline gabbro._- -______<. 0001 45 512 Pyroxenite ______<. 0001 leached by ascending thermal solutions and deposited at 46 513 Quartz gabbro ______<. 0001 or near the surface. Ocherous veins, similar to thos^ at 47 516 Carbonate vein. ______.001 48 518 -_--do.__---_ __ -.___-_.__-_ .001 Iron Hill, occur in the Golconda area. 49 520 Altered ijolite_ ____.-_-______.001 In the igneous rocks beryllium is found chiefly in un­ 50 529 Ijolite- ______<. 0001 51 535 Altered uncompahgrite- ______.001 compahgrite. The BeO content in 5 samples of fresh 52 539 _-__do_- ______.002 uncompahgrite ranged from 0.0098 percent to less than 53 545 _do_-_ ---_ ___ .002 54 564 Uncomcaherite ______.002 0.001 percent, the average being about 0.0035 percent. 170 OCCURRENCE OP NONPEGMATTTE BERYLLIUM IN THE UNITED STATES

In the samples analyzed the BeO content appears to be of beryllium-bearing material at this locality. At least in direct proportion to the percentage of diopside-hed- several million tons of uncompahgrite averaging 0.003 enbergite present, and it is concluded that most of the percent or more of BeO and a smaller amo^mt of ocher- beryllium in the uncompahgrite is contained in the ous vein material averaging about 0.005 percent BeO pyroxene. On this basis it might be assumed that beryl­ are present. Even if accurate figures could be given, it lium would be more abundant in the pyroxenite and is doubtful, however, that these materials should be re­ ijolite, as those rocks, in general, contain more pyroxene garded as beryllium resources, because of the extremely than the uncompahgrite, and according to Larsen (1942, low grade and apparent mode of occurrence. Analyti­ tables 18 and 19), the pyroxenes of the three rock types cal data seem to indicate that most of the beryllium is are very similar. Analytical data indicate, however, contained as an accessory constituent in tin rock-form­ that the average BeO contents of the igneous rocks ing minerals rather than in true beryllirm minerals, younger than uncompahgrite are less than 0.001 per­ such as helvite or beryl. Detailed laboratory study of cent. In general the altered igneous rocks appear to many samples revealed no beryllium minerals. If such contain less BeO than their unaltered counterparts. minerals are lacking, recovery of the beryllium would This applies especially to uncompahgrite, of which the be difficult or impractical. largest number of samples were analyzed, and suggests Some interest has been shown in the rocks at Iron that beryllium was leached from uncompahgrite during Hill for the relatively high content of iron, titanium, hydrothermal alteration. Possibly the beryllium in the gallium, indium, and other metals. In the event mining veins may be accounted for in this way. An exception of these metals is undertaken, further studies on the to the generalization is noted in 1 sample of altered occurrence of beryllium at Iron Hill might be war­ biotite pyroxenite (328-046) that contained 0.0075 ranted in the hope of finding at least small deposits of percent BeO. material from which beryllium might be recovered as COMMERCIAL POSSIBILITIES a byproduct. Because of the extremely variable character of the ITALIAN MOUNTAIN AREA Iron Hill rocks, much more detailed sampling and Italian Mountain, comprised of North Italian, Ital­ hundreds of analyses would be needed to obtain a rea­ ian, and South Italian Peaks, is along the eastern edge sonably accurate knowledge of the grades and tonnages of the Crested Butte quadrangle in the northern part

''- ;U%"f A*NORTH ITALIAN PEAK 328-078r-079 . ;. ' I 328-682 a28-683\ .. b s 328-080 .-081 ^328-082 ,-083

'., -A ITALIAN PEAK

EXPLANATION Weber formation EXPLANATION

Granite Limestone, sandstone, Silicated limestone Tactfte Quartzlte Graphite Marble Garnet tactile Silicated marble end shale end nornfels

, p-328-689 _ 328-683 Contact Strike and dip of beds Locality sampled Contact - Locality sampled and number Dashed where approximately and number Dashed where approximately heated loaned Geology by L. A. Warner and V. R. Wilmarth September 1948 500 500 Feet 40 I FIGCEB 54. Geologic sketch maps of parts of Italian Mountain area, Gunnison County, Colo. LOCALITIES IN COLORADO 171 of Gunnison County. The geology of the Italian Moun­ tactite bodies as much as 25 feet thick occur near the top tain area was described by Emmons, Cross, and Eld- of the Leadville limestone (Mississippian). Thin bands ridge (1894, p. 5) and by Cross and Shannon (1927). of epidote, garnet, diopside, and quartz replace lime­ North and South Italian peaks are formed by masses of stone layers in the Hermosa group (Pennsylvaniar). intrusive rock that range in composition from diorite to granite. Sedimentary rocks of the Weber formation (Pennsylvanian) crop out on the flanks of North and South Italian Peaks, and form Italian Peak. Near their contacts with intrusive bodies the sedimentary rocks have been metamorphosed and replaced locally by tactite (fig. 54). Shannon (in Cross and Shannon, 1927, p. 9) described 28 minerals from the tactite zones. A wedge-shaped body of limestone, shale, and sand­ stone in the Weber is exposed on the west flank of Ital­ ian Peak between the northern and southern intrusive masses. A limestone bed has been replaced by a tactite layer 15 feet thick containing brown and yellow grossu- larite-andradite garnet, actinolite, sphene, idocrase, magnetite, and epidote. Southwest of North Italian Peak is a smaller wedge-shaped mass of intensely al­ Geology by L. A. Warner and tered Weber formation consisting of interlayered V. R. Wilmarth, September 1948 quartzite, hornfels, marble, tactite, and some graphite. V \iooo 0 1000 Feet Ten samples were taken as follows (see also fig. 54): \ 328-078 Grab sample of marble containing epidote, garnet, and EXPLANATION diopside, North Italian Peak. 079 Do. £2 Contact, showing dip 080 Grab sample of tactite containing garnet, diopside, Dakota sandstone 00 Dashed where approximately located and actinolite, Italian Peak. J? 081 Grab sample of tactite containing garnet, diopside, and Hermosa group Strike and dip of beds epidote, Italian Peak. 082 Grab sample of garnet tactite float, Italian Peak. 328-088 083 Grab sample of epidote tactite float, Italian Peak. Leadville limestone Sample number 682 Chip sample across 6 ft of silicated marble contain­ ing magnetite, phlogopite, garnet, and actinolite, Tactite North Italian Peak. FIGURE 55. Geologic sketch map of tactite zone near head of Yule 683 Chip sample across 12 ft of garnet tactite, North Ital­ Creek, Snowmass Mountain area, Gunnison County, Colo. ian Peak. 684 Chip sample across 25 ft of quartzite with thin layers of hornfels, North Italian Peak. Five samples from the tactite layers in this area vere 689 Chip sample across 100 ft of silicated limestone and taken, as shown on figure 55, and are described belor^. hornfels containing tremolite and garnet, Italian Peak. 328-084 Grab sample of garnet-bearing rock from north side of tactite zone. No sample contained as much as 0.001 percent BeO. 085 Same, from south side of tactite zone. 086 Chip sample across 25 ft of garnet tactite. SNOWMASS MOUNTAIN AREA 08T Chip sample along oujtcrop of tactite layer for 2C<* ft. The Snowmass Mountain area is in the Elk Moun­ 088 Grab sample from outcrop of garnet tactite laye". tains in the extreme northern part of Gunnison County. None of the samples contained as much as 0.001 per­ The geology and mineral deposits were described by cent BeO. Vanderwilt (1937). Sedimentary rocks ranging in age In the Rock Creek area, near Schofield Pass 12 nnles from Cambrian to Cretaceous have been metamor­ northwest of Gothic, quartz veins containing pyrite. phosed for several thousand feet outward from their epidote, specularite, tourmaline, galena, and sphalerite contact with a Tertiary albite granite mass that forms occur along north-trending faults. A chip sample Treasury Mountain. Zinc, lead, and silver are the (328-692) across a 10-foot-wide quartz vein contained major metals produced from quartz veins in faulted less than 0.0001 percent BeO, if any. The Niob^ara sedimentary rocks. limestone (Cretaceous) has been replaced by garnet, In the area at the head of Yule Creek (fig. 55) garnet epidote, calcite, diopside, and actinolite at the contact 172 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES of a Tertiary lamprophyre dike. Two channel sam­ with Precambrian granite and are bounded on the west ples (328-693 and -695) across altered limestone ad­ by Princeton quartz monzonite of Crawford (1913) of jacent to the dike showed no BeO. Tertiary age. The ore deposits are replacement bodies in limestone and dolomite, contact deposits, and fissure TINCUP DISTRICT veins. The principal metals produced are lead, zinc, The Tincup district is in the Sawatch Range, a few and silver. Contact deposits and veins nep,r the Iron miles south and southeast of the village of Tincup. King mine, northeast of Whitepine, were sampled (fig. The formations include Precambrian granite gneiss and 56). sedimentary rocks of Paleozoic age, chiefly limestone, ranging in age from Cambrian to Pennsylvanian. Ter­ EXPlANAT1ON SEDIMB'*ARY ROCKS tiary quartz monzonite sills, dikes, and small stocks cut BeliV-n shale the sedimentary rocks. The sedimentary formations Stippled when attend trend northwesterly and dip 10°-35° NE. "IRON KING MINE IGNECOS ROCKS

The ore deposits of the district are of four types Princeton quartz monzonite | E (Goddard, 1936, p. 565) ; silver-lead-gold blanket de­ of Cravford (1913) J " posits, silver-lead-gold veins, molybdenum-tungsten

veins, and pyrometasomatic iron deposits. The silver- Contact Dashed w/ia'e approximately lead-gold deposits account for most of the production. heated The blanket deposits and pyrometasomatic deposits are Strike ar Sample Descripti on (percent) 328-669 Grab sample from 2-ft quartz vein con­ FIGURE 56. Geologic sketch map of part of northern Tomichi district, taining huebnerite, molybdenite, pyrite, Gunnison County, Colo. chalcopyrite, sphalerite, and galena, Ida May mine, 5 miles south of Tincup at The samples collected in the Tomichi d^trict (see Cumberland Pass ______<0. 0001 670 Channel sample across 3-ft quartz vein fig. 56 for some localities) are listed below. None containing molybdenite and pyrite, Emma H mine, 1 mile west of Cumber­ showed as much as 0.0001 percent BeO. land Pass___-______.0013 328-022 8 ft channel sample across tactite on hanging wall 671 Grab sample from 6-ft quartz vein contain­ ing molybdenite at Mammoth mine, of magnetite body. % mile west of Ida May mine,______<.0001 023 Chip sample across silicifled limestone between mag­ 673 Grab sample containing galena, pyrite, netite zones. chalcopyrite, limonite, and quartz from 024 Grab sample of magnetite. dump of Jimmy Mack mine, 5 miles south of Tincup______<.0001 025 Grab sample of epidote, garnet, and s'licifled lime­ 675 Channel sample across 6-ft zone of garnet stone. tactite. Cumberland mine opencut on 026 Grab sample of silicifled limestone. Gold Hill, 4 miles south of Tincup_____ <.0001 027 Grab sample of silicifled limestone with garnet, epi­ 676 Channel sample across 10-ft layer of mag­ netite containing some garnet, Cumber­ dote, and magnetite. land opencut-______<. 0001 028 Grab sample of limonite-stained silicifihd limestone. 677 Channel sample across altered quartz mon­ 029 Grab sample of sulflde ore from vein. zonite sill, Cumberland opencut ______<. 0001 030 Grab sample of altered shale and limestone contain­ 681 Grab sample containing molybdenite, pyrite, and quartz from dump of Bon ing magnetite. Ton mine, 3 miles south of Cumberland 031 Grab sample of epidote-garnet rock from dump of .0005 Erie mine. 033 Grab sample of tailings from Callahrn Zinc-Lead TOMICHI DISTRICT Co. mill at Whitepine. The Tomichi, or Whitepine, mining district is in the 033A Grab sample of mill heads from Callahrn Zinc-Lead eastern part of Gunnison County on the west slope of Co. mill at Whitepine. the Sawatch Kange. Most of the mines are east and 033B Garnet-epidote rock from level 4, Erie mine. 0330 Garnet-epidote, galena, and sphalerite, main drift, north of the mining camp of Whitepine. The geology Erie mine. and ore deposite of the district were described by 033D Galena and sphalerite from main drif4-, Erie mine. Harder (1909, p. 194-198), and Crawford (1913, p. 284- 033E Ore from main drift, Erie mine. 310). Sedimentary rocks ranging in age from Ordo- The Iron King mine is about 2 miles by road north­ vician to Pennsylvanian are in fault contact on the east west of Whitepine near the Morning Glim fault. Mag- LOCALITIES IN COLORADO 173 netite ore in a zone 65 feet wide extends along the fault TABLE 69. Beryllia in samples from the Lake City district Con, for several hundred feet. Masses of serpentine and BeO Sample Description (percent) quartzite interlayed with magnetite are exposed at the 581 Grab sample of lead-zinc ore from dump of Iron King opencut. Adjacent to a quartz monzonite Capitol mine, one-quarter mile southwest of Yellow Medicine mine.- ______<0. 0003 dike the limestone and shaly layers of the Belden shale 586 Grab sample of ore from dump of Golden have been heavily impregnated with epidote, chlorite, Fleece mine, 1,200 ft west of north end of Lake San Cristobal (galena, pyrite, and actinolite, garnet, pyrite, and magnetite. Tactite min­ gold telluride, with rhodoehrosite and erals partly replace the shaly layers of the Belden shale quartz)...______<. 0003- 588 Grab sample containing galena, pyrite, near the Parole tunnel. sphalerite, and quartz from dump of Samples of tactite from the underground workings of General Sherman mine, in Slumgulliqn the Erie mine at Whitepine were obtained through the Gulch 1 mile north of Lake San Cristobal- <. 0001 courtesy of C. S. Robinson of the U. S. Geological Sur­ HUERFANO COUNTY vey. Samples of mill products were obtained from the WALSENBURG AREA Cailahan Zinc-Lead Co. mill at Whitepine. By W. T. HOLSEE

HINSDALE COUNTY Near Walsenburg, flat-lying Cretaceous and Tertiary sedimentary rocks are cut by small intrusive be dies LAKE CITY DISTRICT that are probably related to the Tertiary igneous com­ The mining district near Lake City, in the western plex of the Spanish Peaks to the southwest. The p Hn- part of Hinsdale County, includes two major mining cipal bodies are northeasterly trending vertical dikes camps: Galena (Henson Creek) camp west of Lake several miles long and as much as 50 feet thick; they City along Henson Creek and the Lake Fork camp at range in composition from basalt to granite. There are the north end of Lake San Cristobal about 5 miles south a few sills and plugs. Details of the geology were de­ of Lake City. The geology and ore deposits of the Lake scribed by Hills (1900). City district have been described by Irving and Ban­ One of the plugs forms Huerfano Butte, on the east croft (1911), Brown (1926), and Burbank (in Vander- side of U. S. Highway 85-87 and south of Huerfano wilt,1947,p. 439-443). Creek (Knopf, 1936, p. 1776). The rock is an alkali The rocks of the district are mainly of the Silverton gabbro composed mainly of labradorite, augite, biotite, volcanic series of Tertiary age. Intrusive bodies of olivine, and potassium feldspar. A sample (329-251) rhyolite, latite, and quartz monzonite in places cut the from the top of the butte on the north side contained volcanic rocks. The ore deposits are chiefly fissure veins 0.002 percent BeO. containing lead-zinc ores and a little gold, silver, and An olivine basalt dike containing titanaugite crosses copper. The principal gangue minerals are rhodo- the highway about 3 miles south of Huerfano Butte. chrosite, quartz, and barite. A 12-foot channel sample across the dike contained The veins in the Lake City district are similar to hel- 0.0008 percent BeO. vite-bearing veins in the Eureka area nearby, except Seventeen samples of various rocks collected by Knopf that the latter contain rhodonite. Samples obtained at were analyzed chemically and also were tested spectro- seven mines in the district are described in table 72. No graphically for beryllium with negative results, the limit helvite was noted in any of the veins. of sensitivity being O.OX percent (Knopf, 1936, p. 1779). Although the beryllium contents of the samples f~om TABLE 72. Beryllia in samples from the Lake City district the Walsenburg area are much too low to be of com­ BeO Sample Description (percent) mercial interest, the 0.002 percent BeO in gabbr^ at 328-573 Grab sample containing rhodoehrosite, Huerfano Butte is considerably above the average for quartz, galena, sphalerite, and altered rhyolite from dump of Ulay tunnel, on mafic rocks. Theoretically, some of the silicic anc1 al- Henson Creek 3.5 miles west of Lake kalic rocks in the Spanish Peaks region might be ex­ City-___----_-______,_.__-_-_-.____ 0. 0002 576 Grab sample of ore from dump of Hidden pected to contain appreciably more beryllium. Treasure mine, 2,000 ft northwest of Ulay tunnel (tetrahedrite, galena, sphal­ LAKE COUNTY erite, quartz, rhodoehrosite, and jasper)__ <. 0001 579 Grab sample containing tetrahedrite, galena, CLIMAX MINE sphalerite, pyrite, ehalcopyrite, and quartz from dump of Wave of the Ocean mine, on Ten samples of mill products furnished to the Geo­ Henson Creek 7 miles west of Lake City._ . 0002 580 Grab sample of ore from bunker at Yellow logical Survey by the Climax Molybdenum Co. in 1950 Medicine mine, 2 miles northeast of Capi­ were analyzed for BeO. Descriptions of the samples tol City in Yellowstone Gulch (galena, sphalerite, ehalcopyrite, and quartz)..___ <. 0001 and analytical results are given in table 73. Details 174 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES of the geology of the Climax mine are given by Butler County. The principal mines are a few miles north­ and Vanderwilt (1933). east of the town of Creede. The geology and ore de­ posits of the district were were discussed t y Emmons TABLE 73. Beryllia in samples of mill products from Climax, Colo. and Larsen (1923). The ore deposits are silver-lead BeO Sample Description (percent) veins in Tertiary rhyolite and in quartz latite flows. CMC 1 Molybdenite concentrate______<0. 0001 The principal ore minerals are galena, pyrite, chal- 1A Quartz tailings______.0005 3 Huebnerite concentrate______. 0004 copyrite, and sphalerite in a gangue of amethyst, 4 Quartz tailings. ______.0005 quartz, chlorite, and fluorite. Samples of the mill 6 I*yrite concentrate..-__--_-_-______<. 0001 7 Huebnerite concentrate______< 0001 products were obtained at the Emperius Mill in Creede. 8 Topaz concentrate___-_____--______<. 0003 Analyses of both mill heads and mill tails (samples t 12 Monazite concentrate.______<. 0003 14 Cassiterite concentrate ______. 0005 328-591, -592) showed 0.002 percent BeO. 762 Molybdenite mill heads______. 0006 WAGON WHEEL GAP L.A PLATA COUNTY Fluorspar veins occur in Miocene rhyolite tuffs and DURANGO AKEA breccias about 1 mile south of Wagon Wheel Gap sta­ Coals of Late Cretaceous age occur in the Durango tion on the Denver and Rio Grande Western Railroad. area, principally in the Mesaverde and Fruitland The geology and ore deposits of the are,", were de­ formations. The deposits have been described by scribed by Aurand (1920, p. 61-67) and E^unons and Gardner (1909). Samples were obtained from the Larsen (1913). The main deposit is on tH east side Castle, O. K., and Yellow Jacket coal mines and from of Goose Creek, across the valley from Mineral Hot coal outcrops east of Durango. Springs. It is owned and operated by tl:^ Colorado Ash from a grab sample (328-158) of coal from the Fuel and Iron Corp. at Pueblo. A grab sample (328- Castle mine, 5 miles northwest of Durango, contained 593) of white fluorite from the ore bin contained no 0.0003 percent beryllium, 0.006 percent germanium, beryllium. 0.004 percent gallium, and 0.02 percent vanadium. Ash MONTEZUMA COUNTY of coal (328-163) from the Yellow Jacket mine, east RUSH BASIN of Bayfield on U. S. Highway 160, contained 0.0003 percent beryllium, 0.005 percent gallium, and 0.008 Rush Basin is a large erosional valley at the head of percent vanadium. the East Mancos River in the La Plata mining district. A description of the geology of the area is given in a LAS ANIMA8 COUNTY comprehensive report on the La Plata district by Eckel, MORLEY AREA Williams, and Galbraith (1949, p. 110-115). Many By W. T. HOLSEB dikes, sills, and small stocks of diorite monzonite, and syenite porphyry cut metamorphosed sedimentary rocks Two mafic dikes are exposed in a road cut on the east of Jurassic and Cretaceous age. Several mines in the side of U. S. Highway 85-87 at Morley station, a few area exploit gold-bearing breccia deposits, blanket or miles north of the New Mexico State line. The rock replacement deposits, and fissure veins. A 1-foot-wide is greenish black, fine grained, and rich in augite. A tactite zone composed of brown garnet, epidote, actino- 6-foot channel sample (329-254) across the northern lite, calcite, quartz, and a minor amount of pyrite is dike showed no BeO; the limit of sensitivity for the exposed about 700 feet N. 80° E. of a cabin at the en­ spectrographic analysis was 0.0004 percent. trance to Rush Basin. The tactite zone is in a limestone An intrusive body of basalt about half a mile in di­ member of the Wanakah formation of Jura ssic age. A ameter crops out 2 miles east of Morley. The rock con­ grab sample (328-155) of the tactite showed no beryl­ sists of augite and olivine phenocrysts in a groundmass lium, the limit of sensitivity being 0.0001 percent BeO. of plagioclase, augite, and magnetite (Hills, 1899, p. 3). At the southwestern margin of the intrusive, the rock OUBAY COUNTY is light gray and probably more silicic than basaltic. A sample (329-257) of this rock showed no beryllium, OTTRAY DISTRICT the limit of sensitivity being 0.0004 percent BeO. The Ouray district centers around the torn of Ouray in the San Juan Mountains of southwestern Colorado. MINERAL. COUNTY The geology and ore deposits of the Ouray district have CREEDE DISTRICT been described by Irving (1905); Cross, Howe, and The Creede district is near the eastern edge of the Irving (1907) ; and Burbank (1930; 1940). The rocks San Juan Mountains in the northern part of Mineral exposed in the Ouray district include 8,000 feet of Pre- LOCALITIES IN COLORADO 175 Cambrian quartzites and slates and about 5,000 feet of Silverton volcanic series of Tertiary age several tl ou- limestones, shales, and sandstones of Paleozoic and sand feet thick, constitutes the major part of the ex­ Mesozoic ages. Unconformably overlying the strata of posed bed rock. These rocks are intruded by porj hy- Mesozoic age is a thick series of Tertiary volcanic rocks, ritic latite and rhyolite plugs that range from a few consisting chiefly of andesite flows and latite tuff and feet to more than 2,000 feet in diameter. Much frac­ breccia. The principal ore deposits occur in strata of turing accompanied intrusion, and the volcanic rocks Paleozoic and Mesozoic age near Tertiary granodiorite were altered to clay minerals, alunite, diaspore, and and quartz monzonite porphyry intrusive bodies. Py- quartz along vertical pipelike zones. Ore deposits con­ rometasomatic deposits, fissure veins, and flat-lying re­ taining sulfides of copper, silver, lead, and zinc are placement deposits are represented. Beryllium was not associated with the siliceous pipes. Samples collected detected spectrographically in any of the samples, the in the district are described in table 74; none contained limit of detection being 0.001 percent BeO. as much as 0.001 percent BeO. These are samples collected in the district: UPPER TTNCOMPAHGRE DISTRICT 328-119 Grab sample containing chalcopyrite, pyrite, diopside, epidote, and quartz from dump of Bright Diamond The Upper Uncompahgre district includes the mines mine, 1 mile north of Ouray. along Uncompahgre Canyon, and along Bed Mountain 120 Channel sample across 8-ft tactile zone at portal of Creek between Ironton Park and the junction with Un­ Bright Diamond adit, 500 ft southeast of Bright Diamond mine. (Tactite is chiefly garnet, epidote, compahgre River. The geology and mineral deposits actinolite, and chlorite; ore minerals are pyrite, were described by Burbank (in Vanderwilt, 1947, p. chalcopyrite, galena, sphalerite, and magnetite.) 437-439), and Kelley (1946, p. 355-385). The rocks 123 Grab sample from dump of Portland mine, 1.5 miles in Uncompahgre Canyon are Precambrian quartzites east of Ouray (calcite, siderite, rhodochrosite, and and slates that are uncomformably overlain by sand­ quartz, with minor amounts of galena and sphale­ stones, shales, conglomerates, and limestones of Devo­ rite). 861 Mill heads, American Zinc, Lead, and Smelting Co. nian to Jurassic age. Tertiary volcanic tuff, breccia, mill at Ouray. andesite, and latite, of the Silverton volcanic series and 862 Mill tails from same place. the San Juan tuff, overlie the older rocks. Prevolcrnic intrusive rocks consist of quartz monzonite and dial ^se RED MOUNTAIN DISTRICT dikes. The ore deposits in this area are vein and chim­ The Eed Mountain district is along Eed Mountain ney deposits in the altered volcanics. Two type? of Creek in the southern part of Ouray County, between vein deposits are found: pyrite-gold-quartz, and tung­ Ironton Park on the north and Eed Mountain on the sten-quartz. Chimney deposits are characterized by south. The geology and mineral deposits have been de­ lead, zinc, and copper-silver minerals. We took sam­ scribed by Eansome (1901b, p. 214-250) , Collins (1931) , ples from the seven mines we visited in this area, and and Burbank (in Vanderwilt, 1947, p. 428-431). The one from another mine was supplied us. None of the samples contained as much as 0.0001 percent BeO. They TABLE 74. Beryllia in samples from the Red Mountain district are described below. BeO 328-800 Channel sample across 6-ft vein at portal of lower Sample Description (percent) adit at Gertrude mine, 2 miles south of Orray 328-127 Grab sample of altered volcanic rock con­ (quartz, fluorlte, pyrite, galena, and sphalerite). taining galena and sphalerite from dump of Mountain King mine, 2 miles north­ 802 Chip sample across iron-copper deposit at Dunnore east of Red Mou ntain Pass ______0. 0004 mine on Silver Creek 1 mile south of Ouray (cir­ 128 Chip sample across 125 ft of silicified vol­ cular chimney deposit 200 ft in diameter containing canic material near ore bin at Guston hematite, chalcopyrite, quartz, barite, chlorite, and mine, 1.5 miles north of Red Mountain <. 001 rhodochrosite). 130 Composite grab sample of silicified vol­ 804 Chip sample across tungsten deposit at Dunmore nine canic material from dump of Guston (chimney 20 by 50 ft containing huebnerite, galena, mine. -__--- ______<. 001 sphalerite, and milky quartz). 132 Chip sample across southwest end of silic­ ified pipe at National Belle mine at Red 806 5-ft channel sample across vein at North Star irine, Mountain Pass__-_-_-_-______<. 001 1,000 ft southeast of Dunmore mine (quartz, pyrite, 134 Grab sample of sericitized volcanic rock at rhodochrosite, rhodonite, galena, and sphalerite). southwest end of shaft house, National Belle mine___-______<. 001 807 Grab sample from dump of Chrysolite mine, 1,5C*> ft 137 Chip sample across northeast end of silic­ east of Dunmore mine (galena, sphalerite, qurrtz, ified pipe, National Belle mine ______<. 001 rhodonite, rhodochrosite, and calcite). 859 Mill heads from Idorado mill at Treasury 810 Grab sample of galena and sphalerite in quartz garen MINERAL POINT AND POUGHKEEPSIE GULCH DISTRICTS described by Burbank (1933b), Cross, Howe, and Ran­ The Mineral Point and Poughkeepsie Gulch districts some (1905), and Ransome (1901b). The Tertiary (Ransome, 190lb, p. 185-189; Kelley, 1946; Hazen, 1949) Silverton volcanic series, consisting of andesite, latite, adjoin one another in the northern part of San Juan and rhyolite flows and breccias, cover much of the area. County at the headwaters of the Animas and Uncom- In the deep valley south of Silverton, Precambiran pahgre Rivers. The predominant rocks exposed in the schist is exposed below the volcanic rocks. Several area are latite and rhyolitic flows, tuffs, and breccias of quartz monzonite bodies intrude the Tertiary volcanic the Silverton volcanic series of Tertiary age. In Pough­ rocks. Samples collected from the contact zones on Sultan Mountain, and from 4 mills and 3 mines in the keepsie * Gulch the Silverton_ series is underlain by*/ the San Juan tuff, also of Tertiary age. Kelley (1946, p. Silverton district are described in the following Fst. 289) describes the ore deposits as fissure and cavity fill­ Beryllium was not detected in spectrographic analyses ings, breccia-chimney and breccia-dike deposits, and re­ of the samples, the limit of detection being 0.0001 per­ placement deposits. Most of the productive veins in the cent BeO. area are in the Silverton series. Gold, silver, lead, zinc, 328-151 Grab sample of silicified porphyry containing zunyite and copper are the principal metals produced. Samples from dump of Zuni mine, west side of Anvil Moun­ from the dumps of 10 mines in the area are described tain. 154 Grab sample of garnet-epidote tactite in Hermosa in the following list: formation, northeast side of Sultan Mountain. 328-815 Grab sample contain! ug rhodonite, quartz, galena, and 835 Mill heads from Lead Carbonate mill at Gladstone, 7 sphalerite from dump of Bill Young mine, 200 ft miles north of Silverton. south of Miners Creek at Mineral Point. 844 Mill heads from custom mill at Howardsville. 817 Grab sample of sulfide ore In quartz gangue, with 847 4-ft channel sample across vein in upper adit of minor quantity of rhodochrosite from dump of Un- Adams mine, 1 mile southwest of Gladstone (hreb- compahgre Chief mine, about 1,000 ft southeast of nerite, pyrite, arsenopyrite, calcite, fluorite, and Bill Young mine. milky quartz). 178 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES 851 MiU heads from Shenandoah-Dives mill, 2 miles east p. 122-134). Precambrian granites, gneisses, and of Silverton. schists are exposed over most of the Montezuma quad­ 854 Mill heads from Highland Mary mill, 4 miles south of rangle, but sedimentary rocks of Mesozoic age are ex­ Howardsville. 857 Grab sample from dump of Mighty Monarch mine, posed in the southwestern corner. Tertiary stocks, south side of Kendall Mountain at Silverton (galena, dikes, and sills intrude the older rocks an 0.0001 percent BeO. French Gulch, 1 mile east of Breckenridge. Lenses and bands of magnetite are interlayered with garnet-epidote UPPER BLUE RIVER DISTRICT tactite. The layers range from less than an inch to The Upper Blue River district, about 5 miles south several feet in thickness. Two samples of tactite (328- of Breckenridge, is bounded on the east and south by 099 and -101) were taken from a cliff exposure at the the Park Range, on the west by the Tenmile Range, and eastern end of the zone, near a bend in the road about on the north by the Breckenridge mining district. 1,500 feet southwest of the Wellington mill. A third The geology of this district has been described briefly sample (328-109) was taken near the western end of the by Singewald (in Vanderwilt, 1947, p. 343-f46 and 1951, zone, a few hundred feet west of where it crosses Gibson p. 1-73). The sedimentary rocks include dolomite, Gulch. None of the samples contained as much as shale, quartzite, and limestone of Cambrif.n to Missis- 0.0001 percent BeO. sippian age, which crop out on the east flank of the Tenmile Range. The core of the range corsists of Pre­ MONTEZUMA DISTRICT cambrian granite, gneiss, and schist. Tertiary por­ The Montezuma district is at the headwaters of the phyries occur as dikes and sills in the older rocks. The Snake River, about 40 miles west of Denver. The geol­ ore bodies generally are localized along faults; they are ogy and ore deposits were described by Patton (1909), veins and replacement deposits containing gold, silver, Levering (1935), and Levering and Goddard (1950, lead, zinc, copper, tungsten, and molybdenum. A con- LOCALITIES IN CENTRAL UNITED STATES ]79 tact-metamorphic deposit at the Vanderbilt mine and veins at the Governor mine were sampled. The Vanderbilt mine is 10 miles south of Brecken- ILLINOIS ridge on State Highway 9. The mine is principally a gold producer, although ore from the dump contains small quantities of galena and sphalerite in a gangue (MISSOURI of silicified limestone, diopside, pyrite, specularite, and some quartz. Analysis of a grab sample (328-724) from the dump did not show as much as 0.0001 per­ cent BeO. TRI-STATE The Governor mine is 6 miles south of Breckenridge DISTRICT near State Highway 9. Silver has been produced from a quartz vein in Pennsylvanian and Permian strata. A grab sample (328-727) from a dump, consisting of galena, sphalerite, pyrite, molybdenite, and quartz, did K A N s A not contain as much as 0.0001 percent BeO. LITTLE OCK MAGNET COVE 7 TELLER COUNTY

CRIPPLE CREEK DISTRICT Six samples of mill products were obtained from the BffYANT-BAUXITE JM , S SISSIPPI Golden Cycle mill at Colorado Springs in 1942 for the c i Mine, Mill, and Smelter Survey. Virtually all of the I - ore represented by these samples was from mines in the 100 200 Miles Cripple Creek district, a detailed description of which was given by Loughlin and Koschmann (1935). The FIGURE; 57. Index map showing localities sampled in the Central sampling data are shown in table 77. No samples from United States. the Cripple Creek district were analyzed for this ARKANSAS

investigation. MAGNET COVE TABLE 77. Beryllia in samples from the Golden Cycle mill The igneous complex at Magnet Cove (fig. 58) i« a BeO composite intrusive body about 3 miles in diameter. In Sample Description (percent) 5-GC-l Gold concentrates______0. 005 cross section it is saucer-shaped, with the more resistant 2 Mill heads, gold ore______. 005 rocks forming a rim that surrounds the less resistant 3 Roaster dust, gold refinery.______Not found 4 Flue dust, gold refinery______.01 central part. The geology has been described by Hal- 5 Refinery byproduct (easily removed gold ton (1929), Landes (1931), Spencer (1946), Washing­ has been extracted)______. 001 Refinery slag (from roaster)______. 002 ton (1900), and Williams (1891, p. 163-343). Sedimen­ tary rocks of Devonian and Mississippian age surround the complex and form irregular inclusions within it. CENTRAL UNITED STATES Landes (1931, p. 322) has divided the igneous ro?.ks By L. A. WARNER and V. E. WILMARTH into three types: (1) the cove intrusives consisting of ijolite and biotite-ijolite, (2) the ridge intrusives con­ Several areas in the central United States were ex­ sisting of foyaite, shonkinite, and leucite porphyry, f ,nd amined during November 1948 (fig. 57). Samples of (3) the dike rocks which include pegmatites, jin- feldspathoidal igneous rocks were taken at several guaites, rnonchiquites, and fine-grained porphyr^a places in central Arkansas. Spectrographic analyses Jacupirangite is considered as part of the cove in­ indicate that beryllium is present in relatively high con­ trusive. centrations in some of the rocks at Magnet Cove, Ark., A detailed study was made of the area near C^ve but the volume of these rocks is probably not large and Creek bridge (fig. 59). Marble containing coarse cal- the beryllium may not be recoverable. Many of the cite, monticellite, magnetite, wollastonite, rutile, sphrrie, ore deposits in the Tri-State lead-zinc district were idocrase, and pyrite is exposed in a quarry northwest sampled, but no beryllium was found in any of them. of the bridge. The limestone has been intruded b^ a 180 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES

EXPLANATION

After H. S. Washington, 1900, plate 24 IMile Contact i i i i i i .5 Locafity number see table 78 FIGURE 58. Geologic map of Magnet Cove, Arfe., showing localities sampled. leucite-syenite dike and a nepheline-eudialyte pegma­ TABLE 78. Beryttia in samples from, Magnet Cove, Ark. tite. The leucite-syenite dike averages 10 feet in width Locality No. BeO and extends from Cove Creek northwest to the north on fig. 58 Sample 1 Bock type (percent) side of the quarry where it is covered by dump material. 1 328-305 Leucite porphyry ______0. 0002 2 307 Leucite tinguaite dike ______.0005 The 14-foot-wide nepheline-eudialyte pegamatite is best 3 309 Nepheline syenite porphyry dike___- . 002 exposed in the road cut just west of the bridge. Small 4 318 Shonkinite______. 002 5 312 Biotite ijolite______. 0003 crystals of eudialyte were noted in the pegmatite. Tufa 6 313 Altered biotite ijolite.______. 007 Hill, a large deposit of siliceous sinter, is about 200 7 315 Leueite porphyry______- . 0001 8 317 Shonkinite______._._ . 001 feet north of the road. A small body of ijolite is ex­ 9 319 Foyaite______-___--._----__- . 001 posed on the east side of the hill. Contacts in this 10 320 Monchiquite___-_-__-_____---_--._ . 001 328-293 Silicated marble.______... . 028 area are covered. 294 Nepheline eudialyte pegmatite - - _ _ . 002 Five samples were collected near Cove Creek bridge. 299 Marmorized limestone____-___.__ . 002 300 Silicated marble-______. 001 Elsewhere in the Magnet Cove area, samples of nearly 303 Siliceous sinter______. 003 all igneous rock types were obtained. The samples are i Localities of samples 328-293 to -303 are shown on figure 59. described in table 78; sampling localities are shown on figures 58 and 59. altered biotite ijolite from the stream bed in front The only samples that contain appreciable quantities of the Baptist church, east of Cove Creek bridge. The of beryllium are 329-293, of altered marble from the nature of the beryllium-bearing material in the samples road cut west of Cove Creek bridge and 328-313, of has not been determined. Thus far no beryllium min- LOCALITIES IN EASTERN UNITED STATES 181

TEI-STATE LEAD-ZINC DISTftlCT EXPLANATION In 1942, the U. S. Geological Survey sampled 42 ... ' '. ^ -./sas-aoa X mines and mills in the Tri-State lead-zinc district. The £i8l analytical results of this sampling appeared to indicate that beryllium is concentrated in the lead-zinc ore? of this district. The BeO content of the samples was as high as 0.3 percent by weight. In 1948 Warner and Wilmarth spent 2 weeks in the Tri-State district samp­ ling mines and mills, in an effort to determine the mode of the beryllium occurrence and its distribution in the lead-zinc ores. Many of the localities previously sampled were revisited and duplicate materials ob­ Contact tained. Spectrographic analyses of 23 representative Dished where approximately located samples from the district showed no beryllium, the Limit of outcrop 328-299 lower limit of detection being 0.001 percent BeO; and Locality sampled and number several reanalyses proved the accuracy of these results.

Geology by L. A. Warner and The samples that were analyzed are listed below. V. R. Wilmarth, November 1949 2001 328-257 Grab sample mill heads, Rialto mill, Treece, Kars. 261 Grab sample of stope fill, Peck and Gregory ir"'ue, FIGURE 59. Geologic sketch map of area in vicinity of Cove Creek Commerce, Okla. bridge, Magnet Cove, Ark. 264 Dump rock from Bonnet mine, Hockersville, OkTa. 267 Dump rock from Roanoke mine, Baxter Springs, Kans. erals have been reported from Magnet Cove, and it 268 Dump rock from E. L. Bullard mine, Galena, Mo. seems probable that the beryllium occurs as an acces­ 281 Ore from Little Ben mine, Waco, Mo. sory constituent in other minerals. 283 Ore from Richie mine, Waco, Mo. 285 Ore from Crutchfleld property, Carl Junction, Mo. LITTLE ROCK AREA 324 Ore from Trilby mine, Granby, Mo. 325 Mill tailings from Federal mill, Granby, Mo. An intrusive mass composed chiefly of pulaskite, 326 Ore from Dungy mine, Stark City, Mo. shonkinite, and foyaite is exposed about 3 miles south 327 Do. of Little Rock on U. S. Highway 167. A grab sample 328 Ore from Pioneer mine, Stark City, Mo. (328-323) of pulaskite from the Big Rock quarry did 330 Ore from Bluebird mine, Spurgeon, Mo. not contain as much as 0.001 percent BeO. 334 Ore from Olsen mine, Spring City, Mo. 339 Ore from Mutual mine, Oronogo, Mo. BRYANT AND BAUXITE AREAS 340 Ore from Wingfield mine, Oronogo, Mo. 343 Ore from Federal-Duenweg mill, Duenweg, Mo. By W. T. HOLSER 345 Ore and gangue from Katy C mine, Carterville, Mo. 347 Ore from Buckingham mine, Carterville, Mo. In eastern Saline County, near Bryant and Bauxite, 351 Ore from mine 750 ft south of Capital mill, Stotts several masses of nepheline syenite intrude folded sedi­ City, Mo. mentary rocks of Paleozoic age. The syenite is the 354 Ore from Craig-Owens No. 1 mine, Wentworth, Mo. source of large bauxite deposits. 355 Mill tailings from Sciota mill, Webb City, Mo. Tinguaite dikes cut the nepheline syenite in NE34 sec. 2, T. 2 S., R. 14 W., southwest of Bryant (Hilde- EASTERN UNITED STATES brand, 1949). The dikes are in four zones that are By W. T. HOLSER traceable for 2,000 feet in a northeasterly direction. They contain aegirite, nephelite, sodalite, and alkali Information on nonpegmatite beryllium was ob­ feldspars; some show orbicular structures. tained for six localities in Maine, New Hampshire, Few Three samples (329-842, -843, -844) collected by Jersey, and Virginia (fig. 60). These are mainly lo­ F. A. Hildebrand of the U. S. Geological Survey were calities from which beryllium-bearing minerals had analyzed spectrographically for beryllium. Sample been reported previously. Deposits relatively rich in 329-842, from the centers of the orbicles, and sample beryllium occur at Iron Mountain, N. H., and along 329-843, from the matrix of the orbicles, contained Irish Creek, Va., but the reserves may be sir all. 0.002 percent BeO. Sample 329-844, a composite of 12 Further sampling is needed in these areas to apprise samples of the dike rock, contained O.OOOX percent the commercial possibilities. Beryllium occurs in BeO. willemite and other minerals at Franklin, N. J. The 182 OCCURRENCE OP NONPEGMATITE BERYLLIUM IN THE UNITED STATES one sample and none in another. Probably the BeO EXPLANATION content of the idocrase is irregular but the quantity in Localities sampled in present investigation the Cornell specimen is considerably above the average X Other sampling for analyzed specimens of this mineral. Although it is o doubtful that the idocrase is of commercial value, other Localities having samples containing more than 0.005 beryllium-bearing minerals eoirimonly occur with beryl- beryllia lian idocrase and further investigation of the deposit may thus be warranted.

CARROUL, COUNTY, NEW HAMPSHITVB IBON MOUNTAIN Helvite-group minerals were reported by Wadsworth (1880) from an iron ore prospect near Bartlett, N. H. The locality is on the south slope of Iron Mountain at an altitude of about 2,000 feet. A road lea ding to the mountain turns west from State Highway 16 at Jack­

LIST OF LOCALITIES son. The deposit was not visited during the present 1 Sanford. Maina study, but samples and geological data wer°s furnished 2 Iron Mountain. N. H. 3 Red Hill. N. H. by D. M. Henderson of the University of Illinois. The 4 Beemerville. N. J. 5 Franklin. N. J. following description was taken largely from his notes. 6 Irish Creek. Va. The Iron Mountain deposit is in the Convay granite, of Mississippian( ?) age, near its contact with gneisses 300 Miles of the Littleton formation of Early Devonian age. The FIGURE 60. Index map showing nonpegmatite beryllium occurrences mine workings consist of a 45-foot adit r,nd a small investigated in the Eastern United States. opencut. The ore body is very irregular bu+ its elonga­ tonnage is large but the grade is low, and much of the tion is approximately parallel to a northwest-trending beryllium may not be recoverable. joint set that may have partly controlled the deposi­ tion. In the opencut, the body is about 20 feet wide SANFORD, YORK COUNTY, MAINE and 50 feet long. Beryllian idocrase occurs at Sanford, Maine, as dark Magnetite and hematite are the chief ore minerals greenish-brown prismatic crystals as much as 2 cm and appear to have formed by replacement of granite. thick and 6 cm long, with pinacoidal terminations. Quartz is abundant in small irregular aggregates and The prisms are deeply striated and the crystals have veinlets and in vuggy lenses as much as 3 feet across. a parting parallel to the faces, seeming to follow Irregular streaks and veinlets containing galena, chal- growth zones. The crystals grew at random or in radial copyrite, fluorite, and quartz are common in the iron clusters in openings that were later filled with quartz ore. and calcite. The idocrase-bearing rock overlies an epi- Danalite occurs in irregular aggregates in the ore, dote-rich tactite. The geology of the deposit has hot much of it as apparent reaction rims aronnd quartz. been described. According to the geologic map of Katz Well-formed octahedral crystals occur in a few places. (1917, pi. 61), the locality is near the contact of the Most of the crystals are 2 or 3 mm across ani are zoned, Rindgemere formation of Pennsylvanian(?) age and consisting of a yellow core and a red-brown rim. Re­ the Biddeford granite, which is thought to be related fractive indices (Glass, Jahns, and Stevens, 1944, p. to the White Mountain magma series of Billings 183-185) indicate that the yellow material is probably (1934). helvite and the red material danalite. The locality was not visited during the present in­ Descriptions and analyses of Henderson's samples vestigation but a specimen from the Cornell University are given in table 79. The analyses indicate that the mineralogical collection (CUM 393-26) was spectro- beryllium content of the deposit is probab'y high and graphed by A. A. Chodos and found to contain 0.009 that the granite is relatively rich in niobium. Because percent BeO. Earlier spectrographic determinations of its small size, the deposit is not likely to be of com­ on idocrase from Sanford by George Steiger (1931, mercial interest unless further prospecting in the re­ written communication) indicated a trace of BeO in gion adds to the reserves. LOCALITIES IN EASTERN UNITED STATES 183 TABLE 79. Beryllia and niobium in samples from Iron Mountain, cial uses of these rocks were appraised by Parker (19*8, p. 52-57) and Wilkerson and Comeforo (1946). The [Quantitative spectrographic analyses by K. J, Murata] BeO Nb main intrusive body extends 2 miles along the eastern Sample Description (percent) (percent) face of Kittatinny Mountain, where it apparently iras 329-850c Composite of 2 samples from inside intruded as a thick sill-like mass between the MartHs- of adit, and 1 from 30 ft south of the portal, all in fresh biotite burg shale of Ordovician age and the Shawangunk con­ granite..____.______0.0017 0.02 glomerate of Silurian age. Most of this body ir a 852c Composite of 2 samples from the contacts of the zone of iron min- granular syenite composed of nepheline, orthoclase, and eralization______1.0 .02 aegerite-augite, with minor amounts of biotite, sphene, 853c Composite of chips taken at inter­ vals of 1 to 2 ft across the zone of magnetite, sodalite, garnet, apatite, and fluorite. At iron mineralization______1. 6 <. 01 least 25 sills and dikes intrude the Martinsburg sh^le

BED HILL and the Precambrian formations within a few miles of Beemerville. They have been classified as nepheFne Red Hill is an alkalic ring complex 3 miles in diam­ syenite (tinguaite and bostonite), lamprophyre (min- eter, just west of State Highway 25 at the north end ette or camptonite), and diabase. of Lake Winnipesaukee. As described by Quinn (1937, Samples were obtained from the main mass and s^v- 1944) the rocks are all syenites, of coarser grain to­ eral of the smaller bodies on June 13, 1950. Through ward the outside. Principal minerals are microperthite the courtesy of J. H. C. Martens of the New Jerwy and hastingsite, with some biotite. An inner ring about Bureau of Mineral Research, samples from the bureau's half a mile wide contains as much as 30 percent nephe­ collections also were made available for analysis. The line and sodalite; some of the rocks in the center of analyzed samples are described in table 80. the complex contain quartz. The rocks of Red Hill in­ trude the Winnipesaukee quartz diorite of Precam- TABLE 80. Beryllium, in samples from the Beemerville etrec, brian( ?) to Carboniferous age, but the contacts are no­ New Jersey where exposed. [Spectrographic analyses by A. A. Chodos except No. -828] BeO Specimens of the Red Hill rocks were collected in Sample Location ' Description (percent) May 1950, in the course of other geologic work. Sam­ 329-826 2084.8 N., 845.7 E.; Specimen of boston­ 0. OOX ple 329-812 from a pit known as the "Home quarry," Parker 102; ite dike or sill. Wilkerson 12. in the inner ring contained only O.OOOX percent Be 827 2083.2 N., 841.5 E.; Specimen of porphy- .oox (spectrographic analysis by A. A. Chodos). The rock Parker 103; ritic nepheline Wilkerson 15. syenite from dike. is coarse-grained syenite composed of abundant early 828 2090.3 N., 844.5 E.; Sample of nepheline 3.00" nepheline, albitized microperthite, and hastingsite, Parker 99; syenite from main Davidson 38. mass.2 with streaks and veinlets of later sodalite (Quinn, 1937, 829 2090.6 N., 844.9 E.; Sample of biotite- 001X p. 384-387). Wohlerite (NaCa_(Zr,Nb)FSi2O8 ) is Parker 99; rich nepheline Davidson 46. syenite from main sparingly present (Pirsson and Washington, 1907, p. mass. 270-271). Sample 329-813 was of coarser grained 830 2089 N., 849.7 E.; Composite of three (KTX Parker 100; specimens of hornblende syenite without nepheline and is probably Wilkerson 1; nepheline syenite equivalent to Quinn's "outer coarse syenite" (Quinn, Milton and from sill.4 1937, p. 383-385; chemical analysis on p. 380). Spec­ Davidson. i Location according to U. S. 1,000-yd grid system, as shown on Brand ville trographic analysis did not detect any beryllium in the quadrangle, 1:31,680, IT. S. Army Corps of Engineers, 1943. Localities alf> as numbered by Parker (1948, pl.l); Wilkerson (1952, fig. 1); Davidson (Davidson, K. S., sample, the limit of sensitivity being O.OOOX Be. 1948, The geological relationships and petrography of a nepheline syenite near Beemerville, Sussex County, N. J.: Rutgers Univ. M. Sc. thesis); and Milton and Davidson (1950). SUSSEX COUNTY, NEW JERSEY » Mode is given by Davidson (idem.), in percent: nepheline 43, potasslum-felc'spar 37, aegirite-augite 11, biotite 2, sphene 3, magnetite and pyrite 3. Analyzed by J. K. Murata for BeO, in percent. BEEMEEVILLE AREA 4 Average of 3 modes by Wilkerson, in percent (personal communication from J. K. C. Martens, 1950): nepheline 45, potassium-feldspar 34, aegirite-augite 18, sphene Feldspathoidal rocks are common around the village 2, and magnetite 1. of Beemerville, south of State Highway 23 and west of FRANKLIN DISTRICT Sussex, N. J. The geology of the area was described by Aurousseau and Washington (1922), Milton 12, Wil- The Franklin district, one of the largest producers of kerson (1946), and Davidson.13 Recently the commer- zinc ore in the United States, is between Franklin r,nd Ogdensburg on the western edge of the Precambr^n 53 Milton, Charles, 1929, Nepheline syenite and related rocks of the Franklin Furnace quadrangle, New Jersey: Johns Hopkins Univ. Ph. D. New Jersey Highlands. In June 1950, the district Tas thesis. visited and samples were obtained through the courtesy 13 Davidson, B. S., 1948, The Geological relationships and petrography of a nepheline syenite near Beemerville, Sussex County, N. J.: Rutgers of the New Jersey Zinc Co. and with the cooperation Univ. M. Sc. thesis. of D. W. Jenkins and L. H. Bauer of the chemical de- 184 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES partment, and A. W. Finger and E. N. Newcomb of TABLE 81. Beryllia in mill products from the Franklin district l the geological department. Analytical geological data Franklin mine Ste-ling Hill mine on the occurrence of beryllium in the district were also BeO BeO made available by the company. Material Sample (percent) Sample (percent) The geology, mineralogy, and ore deposits of the Crude ore ______329-832 0. 003 329-837 0. 001 Franklin district have been described in roughly 300 Franklinite concen- ^ reports; among the more recent are those by Kerr ------^ ______(.005) 839 .002 (1933), Palache (1935), and Finger (1948). The dis­ Willemite-franklin- , trict is almost entirely within the Franklin limestone iteproduct.....-/ 836 .001 \ ______(.0008) of Precambrian age, which was metamorphosed to a Willemite concen- 834 . 003 840 . 0005 white, coarse, calcitic marble and squeezed into sharp (.025-0. 03) ______(.0075) northward-plunging folds. At the north end of the ----- .0006 841 .0004 district the Precambrian formations are unconform- 83g (001-0.0015) ______(.0006) 1 Numbered analyses made by A. A. Chodos of composite samr'es for the period ably overlain by limestone and quartzite of Paleozoic 1940-44, submitted by the New Jersey Zinc Co. Unnumbered analyses (In paren­ theses) made by New Jersey Zinc Co. In 1944 (Laboratory Report 160) of composites of similar products from a single month in 1941. The two producing mines of the district are the Franklin mine at Franklin and the Sterling Hill mine have been as a probable source of beryllium. The other at Ogdensburg. At both mines zinc ore occurs in tab­ beryllium-bearing minerals at Franklin are present only ular masses that are conformable to synclines in the in small quantities. Franklin limestone. The composition of the ore is ap­ Barylite, a rare beryllium barium silicate, that con­ proximately 40 percent franklinite, 25 percent gangue tains as much as 15.77 percent BeO is known only on carbonates, 23 percent willemite, 11 percent gangue sili­ the 400-foot level of the Franklin mine (Palache and cates, and 1 percent zincite. The distribution of the ore Bauer, 1930, p. 32) . Small white plates of barylite em­ minerals is remarkably uniform throughout the ore bedded in hedyphane (a calcium-lead-chloro-arsenate) bodies; the distribution of gangue silicates is less uni­ occur in a layered vein. The succession of layers from form. Pyroxene is fairly common at both mines; gar­ vein wall inward are : brown calcite and native copper ; net and rhodonite are common at Franklin and rare at gray calcite; a thin zone of willemite and serpentine; Sterling where tephroite is more widespread. white calcite ; and barylite, hedyphane, and willemite. Granite pegmatite occurs at Franklin but has not There are two types of beryllium-bearing1 idocrase at been identified at Sterling Hill. Some of the pegmatite the Franklin mine. That containing the mor>t beryllium apparently is earlier than the ore and some later. The "occurs in the form of slender brown prisms embedded pegmatite is pink to gray and composed of quartz, or- in a coarsely crystalline mixture of green willemite, thoclase, microcline, albite, and micoperthite, with some brown garnet, leucophoenicite, and barite with subordi­ hornblende, pyroxene, epidote and sphene. Complex nate amounts of svabite, native copper, and gageite" tactite deposits containing rhodonite, hardystonite, (Palache and Bauer, 1930, p. 30). Analyr^s by F. A. manganoan-zincian pyroxenes, garnet, mica, and rare Gonyer of two specimens of brown idocrase from the silicates appear to be localized at places where ore is mine showed 1.56 and 3.95 percent BeO (Tr.ble 85) . A associated with pegmatite. blue to blue-green idocrase, known as "cy^rine," con­ Palache and Bauer (1930) described barylite and tains from 1 to 2 percent copper and as much as 0.11 beryllian idocrase from Franklin, and chemists of the percent BeO. As described by Palache (1935, p. 95), New Jersey Zinc Co. have found traces of beryllium in it occurs for the most part as fibrous crystals associated other minerals. In the present investigation, an attempt with garnet, calcite, willemite, biotite, bus tamite, and was made to determine the distribution of beryllium in native copper in granular tactite. A larg^ pocket of the ore. Analytical data for the mill products are shown this variety of idocrase was found in 1920 on the 850- in table 81. A magnet and heavy liquids were used to foot level of the Franklin mine, but on the whole it is prepare mineral separates from the ore and mill prod­ rare. Both idocrase and calcite replace coarse calcite ucts. The BeO contents of these samples, together with (Hies and Bowen, 1922, p. 561) . In discussing the ido­ results of other workers, are given in table 82. The crase at the Franklin mine, Palache (1935, p. 95) states, analyses indicate that the ore from Franklin is higher "It now appears certain that the beryllium is not geneti­ in beryllium content than that of Sterling Hill. Most cally associated with the primary willemite ore, but is a of the beryllium is in the willemite concentrate and postore element introduced into the deposit from in­ probably is contained in willemite. The average grade trusive pegmatites." While it is probably true that the of the concentrate appears to be much too low for it to beryllium-bearing idocrase is a postore mineral, whose LOCALITIES IN EASTERN UNITED STATES 185

TABLE 82. Beryllia in minerals from the Franklin district Species Location ' Sample * BeO ^percent) Analyst and reference Remarks Franklmite. F 329-833A <0. 0004 A. A. Chodos______No visible impurities. SH 838A <. 0004 ___do______Do. Willemite__. F 834A . 004 _____do______One percent garnet and dark inclusions. SH 840A . 005 _ __do______One percent impurities, including cloudy altered products. Zincite__ F 834B

presence depends on the proximity of pegmatite and periods of fracturing are recognized. Quartz was de­ ore, the source of the beryllium is not known. No beryl posited during the first stage; cassiterite, muscovite, has been noted in the pegmatites at Franklin. beryl, and wolframite during the second stage; musco­ A specimen of pyroxene from the 1,050-foot level of vite, siderite, ankerite, fluorite, biotite, phenakite, f.nd the Franklin mine was found to contain 0.01 percent chlorite during the third stage; and nontronite, vermic- BeO. The pyroxene, tentatively identified as zincian- ulito, hematite, montmorillonite, clinozosite, and cal- manganoan diopside, occurs in a coarse-grained aggre­ cite during the fourth stage (Koschmann, Glass, r.nd gate of willemite, svabite, and leucophoenicite. Minor Vhay, 1942, p. 271). quantities of beryllium are contained in rhodonite and Pale-green to yellow beryl crystals as much as 2 cm svabite. long are most abundant at the edges of the quartz veins, although minor quantities of small beryl crystals are IRISH CREEK DISTRICT, ROCKBRIDGE COUNTY, VA. disseminated in the greisen. According to Glass (oral The tin-beryllium-bearing quartz veins of the Irish communication, 1950), the green beryl forms a.borier Creek district, Virginia, were described by Koschmann, along the quartz-greisen contact and is a replacement Glass, and Vhay (1942). The locality was not visited of quartz. A chemical analysis of the green beryl by during the present investigation. The country rock of E. E. Stevens showed 12.33 percent BeO. Phenacite the district is Precambrian and consists of gneiss and occurs as irregular grains and as pseudomorphs after granodiorite with small dikes of aplite and basic rock. beryl; it is generally associated with chlorite (Korch- The known quartz veins are restricted to the granodio­ mann, Glass, and Vhay, 1942, p. 282). rite and are as much as 9 feet wide, though commonly The reserves of beryl in the Irish Creek district were less than a foot wide. Bordering the veins on one or not determined. However, the beryl is sufficiently both sides are greisen layers as much as 5 feet thick. coarse grained to make it recoverable if the vein ma­ Four periods of mineral deposition with intervening terial is milled for tin.

467945 58 -13 186 OCCURRENCE OF NONPEGMATITE BERYLLIUM IN THE UNITED STATES

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INDEX A Page Page Acknowledgments..., . .-...-...... -.....-...... 4 Hot Springs, deposits, analysis 39 Adams, J. W., section by. -_.. ..._. _. 163 Localities investigated, Arkansas... 180,181 Analysts...... ______...... 3,4 Nevada...... 64,65,69,70 Analytical methods, colorimetric______. ____ 6,7 fluorimetric-.. __.______.______6,7 gravimetric. .______6 Idocrase, analysis______.____ 7,14,17,97,123,185 mineralogic ______.______.______.__ 7-8 occurrence . 25,30,87,123,124,129,151,182,185 radiometric -______.______._,_ 8 Igneous rocks, average beryllium content. 23 spectrographic . . __._.____.....___._...__ & distribution of beryllium__...... 22,23,24 volumetric ...... ___._.___...___...... __ 6 foreign localities, analysis . . . - 20-22 Arizona, localities sampleu and analyses______-.-______93-107 mode of beryllium occurrence -- - 24,25 Arkansas, localities sampled and analyses_____.-______.____ 179-181 localities investigated, analysis..... 20-22 Associated elements in deposits______40-57 Arkansas, Bryant- Bauxite area . 181 Little Rock area.. 181 B Magnet Cove - - 179 Barylite ..-_.- ....______...... __.__...... 184-185 Colorado, Iron Hffl.... 166-170 Bertrandite . ...._____..______.____ 11 Morleyarea . . . - 174 Beryl, alteration.. ______25 OurayPeak...... 163 BeO content.... ______12 Walsenberg area.. 173 concentration in sedimentary rocks______25 Montana, Gordon Butte - 153 mineralogy...... ____.....______._ 7,10,12,25 YogoPeak...... - 148 occurrence, vein_...... 34,35,36,39,71,74,97-99,101,106-107,122-125,163,185 New Jersey, Beemerville area_ - 183 granite...... ______.__...... 145-147 New Hampshire, Red Hffl.... 183 rhyolite.-...... _.___..___....__._ 144-145 New Mexico, Eaton volcanic region .... . 110-113 production______2-3 Wind Mountain area...... - 135-139 Beryllium, genesis of deposits ...... __..._.______...... 58-59 Texas, Cave Peak_.._ ...... ~ 140-143 mineralogy... ______8-20 Trans-Pecos Region_.__ . - 130-135 production...... ______2 Utah, Sheeprock Mountains_ . 145-148 properties and uses ,...... 2 Topaz Mountain, Thomas Range__ 144,145 Wyoming, Casper Mountain... 158 Fort Washakie area.._ - 158 Halleck Creek area_ _. 158 California, localities sampled and analyses______85-95 Iron Mountain_.____ .. - 155-157 Chemistry of beryllium, minerals..... ___.___.______..... 8-10 Leucite Hills... 159 sea water ______.... 26 Investigations, purpose 1-2 spring water.. . ______26 ______.___._._..__ - . 4-5 weathering processes______26 Cbrysoberyl...... __.______....._____.____... 10,11 Goal, deposits, beryllium in______. ____.______28,29 analysis ...... ___...... _____.__ ... 28 Kaolinite analysis. localities investigated, Colorado__ _...... 161,165,166,174,176 Wyoming...... _. _. 157,159 Colorado, localities sampled and analyses______159-179 Lateritic iron ore, analysis 28 Oolorimetric analysis______6,7 Limestone, analysis. . 21*, 27,139 Rawlins area, Wyoming- 157 D DanaHte. alteration__._ ..______25 M mineralogy..... _ ...... 25 Maine, localities sampled and analysis 182 occurrence . __ ..______... . 30,182 Manganese oxide ores, analysis , 27,28 localities investigated, Golconda deposit, Nevada 64,65 P Sodaville area, Nevada... 69,70 Feldspars, analysis... . ______.______14,19 Metamorphic rocks, analysis 29 Fluorimetric analysis..______6,7 Mill products, analysis_..... 92,97,103,105,116,120,130,172,175,179,184 Fluorite associated with helvite. See table 13__ .._____... 30-35,40 concentrate analysis, cassiterite 174 copper . - - -- 154 G frankUnite- - - - 184 Garnet, analysis.. _._ .._..__ 14,17,122,161,185 gold.. 179 occurrence. _. .. ..______...... ___ 14,122,129,151,185 huebernite - 174 Genesis of beryllium deposits. ...______58-59 iron table. - - - 154 Gravimetric analysis-...... __.___.....______...... 6 lead ore. 154 Guide to nonpegmatite deposits, mineralogic.__-_...______. 59-61 manganese 154 elements . . ...__._.______._.. 40-57 molybdenite 174 monazite_ - - 174 H pyrite-... - - . 174 Helvite, analysis.. _____.______.____ 11 scheelite___ ...... 66,83 mineralogy.. . .. ______10,11,12 sulflde - - 154 occurrence, pyrometasomatic deposits____ 29,30,34,122-125,129,176,177,182 topaz - 174 vein deposits . 36,38,39,154 willemite. 184 other deposits ..._ ...... __ 114-116 zinc ore_-. 154 197 198 INDEX Page Page Mineralogy of beryllium.. . ______8-20 Ore minerals...._ _.... . 7 . 2,3,10,59,60 Minerals: See also Beryl, Ohrysoberyl, Helvite, Phenakite. Beryllium as an accessory constituent (table). ______13-15 Ore production...... __... . 2-4 in carbonates, calcite______-______26,151,185 magnesite . - -- 71 rhodochrosite_._ _-______-______16 Phenakite, mineralogy.__ ..... 11,12,17 inhalides, fluorite...... 116,120,130,151,174 occurrence._.. _....___ 35,185 in oxides including complex metal oxides, bauxite ...___. 16,28 Phosphate rocks, analysis______.... _.. 27,154 brucite_._ . ... ______71 Properties of beryllium. __ 2 franklinite - - . .-_...._ _ 186 Pyrometasomatic deposits, analysis 29,30,31,32 ferberite___ . - _-. . ______92 characteristics of beryllium-bearing deposits 33,34 huebnerite .. . 97,99,106,107 foreign localities, analysis...... 29 iron . 28 helvite-danalite bearing deposits, New Hampshire 182,183 scheelite. 66,83,85,93,98,101,102 New Mexico, Carpenter district, Grant County . , 114-116 zincite...... - _ .... 185 Iron Mountain, Sierra County . . 129 in phosphates, arsenates, and sulfates, apatite.. ______185 Vietoriodistrict, Luna County... ___ _...... 122-123 barite. . _ .___...... _...._____.._... 65,66 other deposits, Franklin district, New Jersey. ____ -_ _ 183-185 svabite______...______185 Magnet Cove, Ark...... 179-181 in silicates- ...... 16-20 amphiboles. . .___. ... 18 E andalusite - . ____.... 70,83 Eadiometrlc analysis. anthophyllite_ ...... _.....__...... ______139 dumortierite___ ..______83 8 epidote group 17,18 Sampling methods . 5 eudialyte ...... _...... __...... 138,139 Sandstone deposits, analysis of beryllium 25-27 feldspar, fee Feldspars. Fort Washakle area, Wyoming... . 158 garnet. See Garnet. Shale deposits, analysis of beryllium ...... 25,26,27 idocrase. See Idocrase. Smelter products analysis of beryllium ...__ _ 154,179 lepidomelane...... -..-.. _ 25 Spectrographic analysis . 5 mica minerals______- ______18,19,151 nepheline... - 19,25 Suggestions for prospecting 69-60 pyrophyllite- - - ... 70 T pyroxenes__ . 18,25,139,151,185 tephroite... __...... __...... ___....._ 185 Texas, localities sampled and analysis. See Trans-Pecos Region. tourmaline___._....______... ______18 Trans-Pecos Eegion, Texas and New Mexico, localities sampled and aralysis. 130-143 willemite. . 17,185 Tri-State lead-zinc district, localities sampled .. _ . 181 bisulfides...... 16 sphalerite .. . ___.._. 185 Beryllium essential constituent __ ....____ 10-12 Uses of beryllium - 2 See also Barylite, Beryl, Bertrandite, Chrysoberyl, Helvite, Phenakite. Utah, localities sampled and analysis 143-148 Montana, localities sampled and analysis...______.._..______148-155

N Vein deposits, Beryl-bearing. See Beryl. Nevada, localities sampled and analysis.______...... ______63-85 Beryllium-bearing quartz-gold ...... New Hampshire, localities sampled and analysis______182-183 San Francisco district, Arizona.... _ _ 102, 103 New Jersey, localities sampled and analysis______...______183-185 Helvite-bearing. See Helvite. New Mexico, localities sampled and analysis______..______107-130 types of 35, 36 Also see Trans-Pecos Eegion. Virginia, localities sampled and analysis 185

Olson, J. O., section by.______.______144-145 Wyoming, localities sampled and analysis.. 155-159

O