/! Geology of Sandia Mountains and Vicinity, New Mexico •:•

— -- J:.

lying east of Albuquerque, is “The great tilted orogenic block composing the Sandia range, regarded as classic in this extraordinary type of mountain modeling.” —Fayette A. Jones, 1904. p. I. President of State School of Mines at Socorro, 1898-1902, 1913-1917. Also, Direc tor of Mineral Resources Survey of New Mexico which he initiated in 1915. Memoir29

New Mexico Bureau of Mines & Mineral Resources

[)IVISION OF NEW MEXICO INSTITITE OF MINING & TECHNOLOGY

Geology of Sandia Mountains and Vicinity, New Mexico

by Vincent C. Kelley and Stuart A. Northrop

SOCORRO I975 iv

NEW MEXICO INSTITUTE OF MINING & TECHNOLOGY Daniel H. Lopez, President

NEW MEXICO BUREAU OF MINES & MINERAL RESOURCES Charles E. Chapin, Director and State Geologist

BOARD OF REGENTS Ex Officio Gary Johnson, Governor of New Mexico Alan Morgan, Superintendent of Public Instruction

Appointed J. Michael Kelly, President, 1992—1997, Roswell Steve Torres, Secretary/Treasurer, 1991—1997, Albuquerque Charles Zimmerly, 1991—1997, Socorro Diane D. Denish, 1992—1997, Albuquerque Delilah A. Vega, Student Member, 1995—1997, Socorro

BUREAU STAFF Engineer Cartography Section FANG LUO, Research Associate/Petroleum ANDERSON, Semor Geologist ICAINRYN G. GLsSENER, Manager, ORes J. WILLIAM MCTNrOSH, Volcanologist/Geochronologist DEBBIE GOERING, Staff Secretary RUBEN ARCHULEFA, Metallurgical Lab. Tech. Facility Manager Metallurgist CHRISTOPHER G. MCKEE, X-ray AUSTIN, Senior Industrial Minerals Geologist IBRAHIM GUNDILER, Senior GEORGE S. MCLEMORE,, Senior Economic Geologist HANEBERG, Assistant Director, VIRGINIA T. ALBERT BACA, Maintenance Carpenter II Wfl,uAM C. NORMA J. MRExS, Director ef Publications Office JAMES M. BARKER, Assistant l)irector, Engineering Geologist Environmental Geologist, LISA PETERS, Lab Technician Senior Industrial Minerals Geologist, JOHN W. HAWLEY, Senior BARBARA R. POPE, Biotechnologist Section Manager Albuquerque Office Superoisoo Cartography RErTER, Senior Geophysicist HEIZLER, Assistant Curator MARSHALL A. PAUL W. BAUER, Field Economic Geologist LYNN JACQUES R. RENAULT, Senior Geologist BRANDVOLD, Senior Chemist MArc HEIzLER, Geochronologist LYNN A. SALISBURY, Cartographic Drafter II HEMFNWAY, Computer Pub/Graphics Spec. CINDIE A. RON BROADHEAD, Assistant Director, LYNNE Associate Editor SANDRA SWARTZ, Chemical Lab. Technician Senior Petroleum Geologist, CAROL A. HJEu,MING, Senior Coal Geologist TERRY TELLFS, Technical Secretary Head, Petroleum Section GRETCHEN K HOFfMAN, Digital Cartography Laboratory REBECCA J. TITUS, Senior Cartographer RITA CASE, Administrative Secretary (Aib. Office) GLEN JONES, Manager JUDY M. VAIZA, Business Son,. Coordinator STEVEN M. CATHER, Field Economic Geologist PHILIP KYLE, Geochemist/Petrologist Secretary MANUEL J. VASQUEZ, Mechanic II RICHARD CHAMaERUN, Field Economic Geologist ANN LANNING, Executive SUSAN WELCH, Manager, Geologic Extension Service Petroleum Section ANNABELLE LOPEZ, Petroleum Records Clerk J. RICHARDS. CHAvEZ, Assist. Head, Hydrogeologist LOPEZ, Receptionist/Staff Secretary MICHAEL WHITWORTH, RUBEN A. CRESPIN, Garage Supervisor THERESA L. MAUREEN WILES, Bibliographer DAVID W. LOVE, Senior Environmental Geologist NEuA DUNBAR, Analytical Geochemist Geologist VERT LOVE, Editor JIRI ZIDEIC, Chief Editor/Senior ROBERT W. EVELETH, Senior Mining Engineer JANE A. CAL Mineralogist/Economic Geologist NANCY S. GILSON, Assistant Editor VIRGIL LUETH,

SAMUEL THOMPSON ill, Emeritus Sr. Petroleum Geologist ROBERT A. BIEBERMAN, Emeritus Sr. Petroleum Geologist ROBERT H. WEBER, Emeritus Senior Geologist FRANK E. KDTTWWSKI, Emeritus Director/State Geologist Research Associates

Unit RUES, UNM GLENN R, OSBURN, Washington WILLIAM L CHENOWETH, Grand Junction, CO BARRY S. ALLAN S. SANIVRD, NMT Alberta, CAN MICHAEL J. RUNE. USGS CHARLES A. FERGUSON, Univ. NV TIMOTHY F. I,AWTON, NMSU JOHN H. SCHILUNG, Reno, JOHN W. GEISSMAN, UNM DAVID V. LEMONE, W’EP WILLIAM S. SEAGER, NMSU LELAND H. GILE, Las Cruces EDWARD W. SMITH, Tesuque Albuquerque SPENCER G. LUCAS, NMMNH&S CAROL A. HILL, USGS GREG H. MACK, NMSU JOHN F. SlITTER, BOB JULYAN, Albuquerque Mus. Nat. Hist. MCMILIAN, NMSU RICHARD H. TEDFORD, Amer. SHARI A. KELLEY, SMU NANCY J. HOWARD B. NICKEISON, Carlshad TOMMY B. THOMPSON, CSU WILLIAM IL KING, NMSU Graduate Students

TINA ORTIZ ROBERT APPELT RICHARD ESSER DAVID Sivus ULVI CETIN JOHN GILLENTINE J. JOE STROUD DAVID ENNIS MIOSIEI, HEYNEKAS,IP

Plus about 30 undergraduate assistants

First edition, 1975 Reprinted 1982, 1995

Published by Authority of State of New Mexico, NMSA 1953 Sec. 63-1—4 Printed by University of New Mexico Printing Services, August 1995

Socorro, NM 87801 Available from New Mexico Bureau of Mines & Mineral Resources, credit requested. Published as public domain, therefore reproducible without permission. Source V Foreword

Several years ago, when the idea for this memoir was but a gleam in Vincent Kelley’s eye, I allowed that, somewhere down the road, we would present the citizens of New Mexico with a worthwhile document on a most significant area. Happily, the finished product has exceeded even those exfrctations. The document is more than worthwhile—it is unusually important. a storehouse of geologic information. Those who seek to understand the geologic framework of their environment will be consulting this memoir for many years. During the initial stages of writing. Vin simply wasn’t satisfied with the scope of the manuscript. Typescripts shuttled back and forth, even laid idle for weeks. Paleontology and stratigraphy were important parts of the story, yet not getting the treatment needed. Then one day, he wondered out loud whether Stuart Northrop might be persuaded to come aboard as coauthor. We thought so. That idea turned out to be inspirational. It ensured the teamwork required for the success of this endeavor: Vin, the indefatigable producer and field geologist—ex perienced in structural geology, regional tectonics, reconnaissance mapping, mineral property evaluation, and resource development; Stu, the meticulous researcher and editor—experienced in paleontology, stratigraphy, geologic history, mineralogy, and seismology. About a year after arriving in New Mexico, I spent a couple of weeks afield with Vin, preparing road logs for an annual field conference of the New Mexico Geological Society. From that occasion and many contacts subsequently, I have come to know him as one of the most dedicated men in our profession. (The sameness of our names is merely coincidental; we are not related.) The coauthors are uniquely qualified to unfold the geologic record of the Sandias terrane. Their combined expertise on New Mexico geology totals 85 years, a considerable portion devoted to the Sandias and vicinity—all in association with the University of New Mexico. Both have chaired the Department of Geology; both have had a long association with the U.S. Geological Survey. No other two professors in the state have directed so many graduate theses. Their influence on the science of geology, and in the education of geologists, has been tremendous. Between them their published contributions to the literature of geology total 223 papers and books; more are in preparation. Their accomplishments, the honors conferred on them, and their professional credentials are far too numerous to list here. The Sandia Mountains dominate the daily scene for more than a third of the population of New Mexico; the upper ridges are only 15 miles east of downtown Albuquerque. But these mountains are much more than a landmark. They contain a variety of valuable resources—geo logical, historical, archeological, recreational. Much of the area is in national forest with trails, campsites, picnic spots, a ski area, a stream, a scenic road to the crest, a tramway to the summit, and magnificent wildlife. As the population of the Albuquerque region expands, so, too, will the use of the Sandia Mountains. Problems involving resources and land use are inevitable. Factual information on the geological resources is a prerequisite in solving those problems. Although this book was prepared mostly for persons interested in the earth sciences, much of the content (including the large maps in the pocket) has value for anyone concerned with either the development or conservation of the area—most particularly those who live, work, or visit there.

Robert W. Kelley Editor and Geologist Socorro New Mexico Bureau of Mines & May 5, 1975 Mineral Resources vi Preface

This report is in many respects a culmination of our studies of the geology of the Sandia Its Mountains and adjoining areas during the past 35 to 45 years. Interest in the area came easily. more nearby location was ideal for teaching University of New Mexico field classes and directing fossils, than a dozen thesis studies in the area. The great variety of rocks, type formations, structures, mineral deposits, and physiographic features makes the area unusually attractive. V. In 1963 at the request of the Water Resources Branch of the U.S. Geological Survey, C. New Kelley prepared a geologic map of the area, and it was published as Geologic Map 18 of the water Mexico Bureau of Mines and Mineral Resources. The immediate need for the map in resources investigations precluded issuing an accompanying report. During the present work Map 18 has been revised with some additions, changes, corrections, map has and deletion of a strip along the bordering Estancia Valley. Furthermore, the geologic been supplemented with a separate topographic map, a structure contour map, and a structure sections plate. The text and map draw freely on the reports of many students who have worked under us. In A. particular we wish to single out Jerome E. Anderson, Bert N. Brown, John J. Bruns, Paul Catacosinos, Thomas A. Fitzgerald, Earl P. Harrison, Phillip T. Hayes, Richard B. Lodewick, Howard Milligan, Charles H. Phillips, Charles B. Reynolds, John W. Shomaker, Arthur H. Stukey, Those Jr., Ernest Szabo, Tommy B. Thompson, Donald F. Toomey, and Gordon H. Wood, Jr. whose works were guided by others are credited in the text where appropriate. In the University Department of Geology J. Paul Fitzsimmons is acknowledged for discussions concerning the Sandia Granite and the orbicular rocks, Wolfgang E. Elston for certain points regarding the mineral deposits, and Douglas G. Brookins for information on radiometric dates obtained on the Sandia Granite. Francis C. Koopman gave us specimens of the orbicular granites line and allowed us to photograph large slabs. During preparation of the maps and numerous drawings William E. Hale of the U.S. Geological Survey made certain facilities and equipment available. Very special appreciation is due our long-time friend, Charles B. Read of the U.S. Geological Survey. Mr. Read did or supervised much of the first modern work on the stratigraphy of the area, and we have benefited from not only his work and publications but also from association and many conversations with him. Up-to-date generic assignments of many fossil species were kindly provided by William A. Cobban, Donald A. Myers, Norman F. Sohl of the U.S. Geological Survey, and Erie G. Kauffman and Leo J. Hickey of the U.S. National Museum. A. K. Armstrong of the U.S. Geological Survey provided information on the Mississippian in advance of publication. Sergius H. Mamay of the U.S. Geological Survey supplied information on both the fauna and flora of the Kinney clay pit, as did Sidney R. Ash of Weber State College. Jiri Zidek of the University of Oklahoma let us see a manuscript on fishes in advance of publication. Frank M. Carpenter of Harvard University sent information on insects; Frederick R. Schram of Eastern illinois University provided data on two shrimps and a myriapod in advance of publication. Robert C. Burton of West Texas State University made a special study of conodonts. Howard J. Dittmer of the University Biology Department assisted with popular names of Upper Cretaceous plants. George A. Agogino of Eastern New Mexico University provided references and comments on the age of Sandia points. U.S. Forest Service officials have been helpful in several ways, and in particular we wish to acknowledge Wallace L. Lloyd, Jack R. Miller, and Tom Smiley. Others who have helped in various ways are Gilbert R. Griswold of Chapman, Wood & Griswold, Inc., Harry J. Javernick and Walter J. Ames of Ideal Cement Company, Edward E. Kinney of Kinney Brick Company, William Vanderslice of Southern Union Production Company, and Edward C. Beaumont. Charles H. Lembke and Clark M. Carr provided some recollections concerning events in the Hagan area. Ruben Cobos of the University Modern Language Department provided some critical help with derivation and spelling of a Spanish name. As in many instances in the past, the University Research Allocations Committee granted funds for typing, supplies, photography, and minor field expenses. Most importantly, however, this report would likely not have been undertaken or completed without considerable encourage ment and financial assistance by the New Mexico Bureau of Mines and Mineral Resources. Bureau draftsmen also prepared the illustrations and made numerous minor revisions on the new geologic map accompanying this memoir. Vincent C. Kelley Stuart A. Northrop Albuquerque Professors Emeriti September 1974 University of New Mexico vii Contents

ABSTRACT II STRUCTURE 77 INTRODUCTION 11 REGIoNAL SETTING 77 LocAlloN AND AREA 11 SANDIA UPLIFT 77 PHYsIOGRAPHY 11 Extent 77 Drainage 11 West Side Faults 77 West Side Canyons 12 East Side Faults SI Tijeras Canyon 12 Terminations 82 San Pedro Creek Area 13 MANzANITA UPLIFT 84 Las Huertas Canyon 15 HAGAN BASIN 85 Sandia Ridge and Dip Slope 15 RIo GRANDE TROUGH 85 Sandia Piedmont 15 TIJERAs RIFT ZONE 87 MARcOU’s 1853 SURvEY 15 Tijeras Fault 87 GEOLOGICAL SOCIETY OF AMEIUCA 1907 19 Gutierrez Fault 88 ROCKS AND FORMATIONS 21 Tijeras Graben and Basin 88 PRECAMBIUAN 21 Monte Largo Horst 90 Tijeras Canyon Metamorphics 21 OTHER STRUCTUREs 90 Monte Largo Metamorphics 23 ORIGIN 90 Rincon Ridge Metamorphics 23 EARTHQUAKEs 93 Sandia Granite 23 GEOLOGIC HISTORY 94 Dikes Related to Sandia Granite 27 MINERAL RESOURCES 97 MISSISSIPPIAN 28 EARLY MINING OPERATIONs 97 Arroyo Peñasco Formation 28 Mining Districts, Subdistricts, and Camps 98 PENNSYLvANIAN 30 METALs 100 Sandia Formation 31 N0NMETALS 105 Madera Formation 33 Barite 105 Fossils 35 Mineral Specimen Occurrences 105 Correlation 44 Cement Materials 107 PERMIAN 49 Building Stone 108 Abo Formation 49 Loose Aggregates 109 Yeso Formation 50 Lime 109 San Andres Formation 51 Shale and Clay 110 TRIAsSIc 52 COAL 110 Santa Rosa Sandstone 52 Hagan Basin Field 110 Chinle Formation 52 Tijeras Basin Field 114 JURASsIC 53 Placitas Field 117 Entrada Sandstone 53 PETRoLEUM POSsIBILITIES 117 Todilto Formation 54 REFERENCES Morrison Formation 56 119 CRETACE0US 57 APPENDIX 1—Stratigraphic Sections 125 Dakota Sandstone 57 Madera Formation 125 Mancos Shale 58 Abo Formation 125 Mesaverde Formation 60 Santa Rosa Sandstone 126 Fossils and Age 61 Chinle Formation 126 TERTIARY 62 Morrison Formation 127 Galisteo Formation 62 Mancos Shale 127 Espinaso Volcanics 67 Mesaverde Formation 127 Santa Fe Formation 67 Galisteo Formation 129 Intrusive Rocks 69 APPENDIX 2—Earthquakes 131 QUATERNARY 70 INDEX 133 Pediments and Pediment Gravel 70 MAPS (in pocket) River Terraces and Gravel 71 1—Areal Geology Alluvial Fans 71 2—Topography Valley Alluvium 72 3—Structural Geology Caves, Artifacts, and Fossils 73 4—Structure Sections Landslides and Rock FaIls 76

(Tables and Figures follow) viii

TABLES 1—Foraminifera in Sandia Formation and Madera Group 42 2—Pennsylvanian Brachiopoda in Sandia Mountains and other New Mexico areas 43 3—Pennsylvanian fossils of Sandia-Manzanita Mountains, excluding Foraminifera and Brachiopoda 45-47 4—Upper Cretaceous fossils in Sandia Mountains and adjoining areas 63-65

FIG URES

I—Location map x 2—Airview south of tilted Sandia uplift 11 3—Topographic profiles of Sandia Mountains 12 4—Drainage areas of Sandia Mountains 13 5—Sandia Granite fresh and weathered outcrops 13 6—The great granite Shield and Thumb surmounted by Pennsylvanian beds 15 7—Central part of Marcou’s geologic profile frontispiece (1858) 14 8—Part of Marcou’s geologic strip map of New Mexico along latitudes 35° to 35° 30’ (1858) 16 9—Geologic sketch map of Manzanita-Sandia Mountains area (1907) 20 lO—Stratigraphic table 21 Il—Precambrian belts along Tijeras Canyon 21 l2—Cibola Gneiss outcrop 22 13—Cibola Gneiss sample 22 14—Tijeras Greenstone belt along Tijeras Canyon 22 IS—North wall of upper part of La Cueva Canyon 23 16—Sandia Granite showing typical weathered surface 24 17—Sandia Granite outcrop with numerous inclusions 24 18—Orbicular structures in Sandia Granite 26 19—Pegmatite dike swarm in Rincon Ridge 28 20—Arroyo Peñasco Formation at Montezuma Mountain 30 21—Basal Sandia Formation resting on spheroidal boulder in Sandia Granite 31 22—Knob of Sandia Granite buried in basal Sandia sandstone 31 23—Marcou’s Camp A, October 8, 1853, at Tijeras 31 24—Airview of northern part of the Sandia ridge 32 25—Pennsylvanian beds near Sandia Crest 32 26—Graphic sections of the Sandia Formation 33 27—Arkosic limestone member of Madera Formation 34 28—Excerpts from Marcou’s plates V and VI (1858) 38 29—Marcou’s plate VII (1858) 40 30—Reddish-brown Abo sandstone beds 50 31—Entrada Sandstone and Todilto Formation 54 32—Todilto gypsum at San Felipe quarry, Tonque Arroyo 55 33—Todilto outcrop along Gonzales Creek 54 34—Disconformable contact of Dakota Sandstone ledges on friable pebbly white sandstone of Morrison Formation 57 35—Massive upper Morrison beds capped by dark ledges of Dakota Sandstone 57 36—Ophiomorpha burrows in Dakota Sandstone 59 37—Airview northeast across Hagan basin near Diamond Tail ranch headquarters 60 38—Airview northeast across Hagan basin near Coyote Arroyo 61 39—Airview east across Hagan basin near Hagan 61 40—Lower Galisteo sandstone north of Hagan 62 41—Santa Fe fanglomerate unconformably overlying soft Galisteo beds 68 42—Fanglomerate of Santa Fe Formation along Tonque Arroyo 69 43—Tuerto Gravel of Ortiz pediment surface 70 44—Large granite boulders and blocks on Albuquerque’s East Mesa 72 45—Steps along Las Huertas Creek near Las 1-luertas picnic area 72 46—Wide alluviated San Antonito Valley, a slightly modified level of Ortiz surface to north 72 47—Cross sections of Sandia Cave 74 48—Mastodon and mammoth teeth (scale is in inches) 75 49—Hornblende andesite dike in Meseta Blanca sandstone 76 50—Lamprophyre dike cutting Sandia Granite 76 51—Monzonite sill in Mancos Shale 76 52—Photomosaic of Sandia Mountains and surrounding area 78 53—Eroded fault scarp along central part of uplift 79 ix

54—Vertical air photo of Juan Tabo area showing triangular fault facets and principal faults 80 55—Triangular fault facets at mouth of La Cueva Canyon 81 56—Faulted Sandia Granite in canyon side near bottom of La Luz trail 81 57—Holocene fault scarp along Rincon fault 81 58—Rincon fault in roadcut on NM-44 81 59—View northwest from head of Las 1-f uertas Canyon 82 60—Cope’s diagrammatic sketch of the Zandia Mountains (1875) 83 6l—Airview southeast of northern end of Sandia Mountains 83 62—Airview east of Placitas area 83 63—Structure section A-A’ from Rio Grande trough to Hagan basin 84 64—Santa Fe fanglomerate (left) downfaulted against Galisteo and older Santa Fe fanglomerate 84 65—Tectonic map of Albuquerque-Belen basin 86 66—Structure section across Hagan basin and northern Sandia Mountains 87 67—Longitudinal structure profiles on top of Precambrian, in and adjoining Tijeras graben and Monte Largo horsi 88 68—Airview northeast of Tijeras anticline and syncline 89 69—Santa Fe fanglomerate unconformably overlying Mesaverde claystone and sandstone 92 70—Mines and prospects: adits, shafts, inclines, trenches, pits, and quarries 99 71—Plan and sections of Blue Sky mine 101 72—La Luz mine workings 102 73—Lower portal of La Luz mine 102 74—Plan of Mary M mine 103 75—Plan of Great Combination mine 103 76—Cerro Pelon mine workings 104 77—Geologic map and section of Las Huertas mine area 106 78—Ideal Cement plant at Tijeras 107 79—Ideal quarry west of cement plant 107 80—Dwelling east of Tijeras built massively ofAbo sandstone 108 8 1—Dwelling in Tijeras Canyon built solidly of Sandia Granite 108 82—Large dwelling built of gneiss in Tijeras Canyon at Atanacio Road 109 83—Highway limestone aggregate quarry along old US-66 109 84—Pina Vjtitos mine portal 111 85—Coal outcrop at left side of Pina Vititos mine portal 111 86—Pina Vititos coal-bearing zone south of main portal 112 87—Upper coal-bearing zone at Sloan mine 112 88—Hagan ruins at center of camp 112 89—Airview of Tijeras basin showing coal-bearing zones, mines, and prospects 116 90—Section I mine in Tijeras basin 117 91—Plan and longitudinal panel of Section 1 mine 117 92—Coal protrusions and flyer thrusts in north wall of Section I mine 118 x

FIGURE I—LOCATIoN MAP II Abstract The Sandia Mountains area is dominated by an flanking the mountains. Thick sequences of early and eastward-tilted fault block that stands imposingly above late Tertiary sediments lie in order above the the deep Rio Grande trough on the west. Structural Cretaceous in the Hagan basin northeast of the uplift. relief from uplift to trough is as much as 6 miles: into The section is 16,000 ft thick exclusive of the late the basins to the east and northeast relief is 2.5 to 5 Tertiary and Quaternary trough-filling Santa Fe For miles. The most unusual structure of the area is the mation. Tijeras rift belt bounding the uplift on the southeast. The long east- to northeast-tilted homocline from the This belt, 2 to 3 miles wide, 16 miles long, and trending Sandia uplift into the Hagan basin contains most of the northeastwards, consists mainly of two longitudinal formations of central New Mexico, and is the most parts: a southwestern folded graben and a northeastern complete sequence in the state. Stratigraphic units horst. Tijeras rift belt is principally a Laramide feature consist of 1) marine Mississippian and Pennsylvanian as are a few other faults along the eastern flank of the shelf beds, 2)continental Permian. Triassic, and Jurassic late Tertiary Sandia uplift. red beds formed under flood-plain, evaporitic, lacus Precambrian rocls, prominent in the bold western trine, and eolian environments, and 3) intertonguing fault scarp, consist of granite, gneiss, schist, quartzite, marine and flood-plain Cretaceous beds of the Rocky and greenstone. Sedimentary rocks range in age from Mountain geosyncline. Mississippian to Cretaceous within and immediately Introduction LOCATION AND AREA the range is from about 6,300 ft near Tijeras to about The Sandia Mountains area covers 400 square miles 6,900 ft near San Antonio and La Madera. For within six 7.5-minute a quadrangles east and northeast of summary of the climate and vegetation see Anderson Albuquerque (fig. I). The Sandia Range is the dom (1961). inant feature, but part of the Manzanita Mountains south of US-66, Tijeras basin, Monte Largo (east of the DRAINAGE Sandias), Hagan basin (northeast of the Sandias), and Drainage of the Sandia Mountains area is semiradial an edge of the Rio Grande depression are all included westward to the Rio Grande. Three major stream in the geologic map (map 1, pocket) and text. Two systems, Las Huertas, San Pedro, and Tijeras, drain the principal highways, Interstate 40 (including US-66) and eastern or backsiope area (fig. 4). Las Huertas NM-14 roughly quarter the area. Additionally, drains the NM-44 backsiope northward from Sandia crosses the northern part of Crest; San Pedro, the the mountains and provides slope between the crest and access to the crest. a point on the ridge divide east of Bear Canyon; and Tijeras, the southern back- The area contains most of the significant Paleozoic to slope including the Manzanita Mountains. Ten prin Cenozoic stratigraphic units and a varied representation cipal stream networks drain the western face and ad of the Precambrian rocks of central New Mexico; joining mesa or bajada. These are from north to south: important stratitectonic relationships are observable Agua Sarca, Del Agua, Juan Tabo, La Cueva, Baca, there that bear on the understanding of the origin of the Pino, Bear, Embudito, Embudo, and Tijeras. Rio Grande depression and of the Sandia Mountains. Tijeras drainage is unique because its tributaries The area is particularly important to Albuquerque, the major city of New Mexico, with respect to environment, recreation, urban development, and esthetics. PHYSIOGRAPHY The Sandia Mountains are an eastward-tilted fault block with large and spectacular outcrops of Precam brian crystalline rocks exposed along the steeper west ern side (fig. 2). The crest and eastern slope of the range are capped by Paleozoic sedimentary rocks. This difference in the nature of the rocks, together with the youthful fault scarp, have given rise to numerous physiographic features for the eastern and western slopes. Furthermore, due to structural differences in the terminations of the range, the northern and southern areas have markedly different physiographic features Phojo Donald A. Mrs (map by 2, in pocket, and fig. 3). Altitudes along the crest FIGURE 2—AIRvIEw OF TILTED SANDIA UPLIFT, LOOKING SOUTH. vary from about 9,200 ft to 10,678 ft. Altitudes along the ESTANCIA VALLEY IN FAR DISTANCE. CREST IS CAPPED BY STRONGLY LEDGED western base vary from about 5,800 ft near Four Hills MADERA FORMATION (PENNSYLVANIAN), BENEATH WIIICH to IS SANDIA FORMATION (ALso about 7,000 ft near Juan Tabo; along PENNSYLVANIAN) FORMING BRUSH- the eastern side COVERED SLOPE ABOVE BOLD PRECAMBRIAN GRANITE CLIFFS. 12

the base of the range. As the piedmont is mostly on the I downthrown subsiding basin west of the fault, the gradient of the stream decreases abruptly and the canyon no longer confines it. As a result the tributary collecting system of canyons turns into a distributary system or alluvial fan on the piedmont. Each of the 9 canyons has an alluvial fan and the coalescence of these has formed the piedmont. This feature is locally re ferred to as East Mesa or the East Heights. Some of the complications of this surface are discussed in connection with the landforms of Tijeras Canyon. A canyon such as Bear or Embudo, when followed mountainward, branches into right and left tributaries, each dividing into successively smaller subtributaries with the result that the whole system is eroded into slopes. Farther into a canyon system the subcanyons become smaller, steeper, and higher in elevation. In the lower reaches of a canyon system the spurs apd ridges tend to be rounded; weathering is deeper; and the granitic rock which predominates weathers into large rounded or spheroidal residual boulders (fig. 5). In the higher and steeper areas more severe weathering by frost action creates a more angular, craggy terrain with fewer rounded residuals. The mouths of the 9 principal canyon systems that dissect the western escarpment are spaced from I to 4 miles apart. The lower part of the escarpment between canyon mouths shows little, and in places no, dissection. These less dissected areas with straight range fronts formed by youthful or actively rising fault blocks, are landforms may be 9782 triangular fault facets (fig. 54). Such Forest Pa rk noted between Embudo and Embudito Canyons (be tween the eastern ends of Candelaria and Menaul Boulevards). The triangular fault facets are best seen doCanyonS0flAflt0fh0 during the winter in morning light. The best or freshest of these remnant fault facets is east of Juan Tabo the La Tijeras Creek Canyon, north of La Cueva Canyon and near Luz trail (fig. 53). The great cliff faces of the high part of the range 4 Miles Crest of range 9 epitomize the grandeur of the Sandias. The greatest • Bose of range Horizontal and Vertical Scale array of faces occurs from Pino Canyon northward; FIGURE 3—SERIEs OF 15 PROFILES OF THE SANDIA M0uNTMNs, outstanding is the great Shield (fig. 6) jutting westward EACH ABOUT I MILE APART. FROM I MILE SOUTH OF PLACITAs TO near the divide between Juan Tabo Canyon (south) and NEAR TuERAS. Del Agua Canyon (north). Of almost equal prominence are the great walls west of the crest, where several knobs drain both the front and back sides of the mountains. Its of granite such as the Needle and the Thumb surmount course was either established before mountain-building the great faces. They are well known to mountain began, or early during uplift along a low, weak struc climbers; excellent photographs and descriptions of tural zone across the axis of the uplift. Not draining the these features as well as approaches to them have been Sandia Mountains is a portion of the Estancia Valley given by Kline (1970). Only a few granitic faces occur in drainage in the southeastern part of the map area. the lower Pino Canyon-Bear Canyon section of the Landforms within these drainage basins have distinctive range. although thick Madera limestone ledges form features based upon structure, rock composition, precip strong cliffs. Around South Sandia Peak the granite itation, vegetation, and altitude. again forms bold cliff faces surmounted by small knobs, locally approaching the magnificence of the northern WEST SIDE CANYONS area. side drainages form contiguous, The 9 other west TIJERAs CANYON steep and short canyon systems. Their sharpness and vigorous erosion is in response to the rising fault Tijeras Canyon bounds the Sandia uplift on the south escarpments, and their erosive power has largely deter and the lower Manzanita Mountains on the north. Like mined the position of the crest of the range. Each most of the other west side canyons, Tijeras enters canyon system (for example, Embudo) consists of eastward into the mountains in granitic terrain. About numerous short tributaries which funnel out of the halfway through the range the canyon passes into and mountain front onto the alluvial piedmont plain along follows, a northeast-trending fault and weak-rock zone 13 A1 rid Hoon I (runs) , — — -.‘

-

— Po -.

ES TAN CIA

- VALLEY

— 1’

-.

C) 2 4 6 8Mes

FIGURE 4—DRAINAGE BASINS OF SANDIA MOUNTAINs AREA.

to the back side where the canyon splits into two ment, applied the Spanish word Tyeras, meaning scis principal forks along fault zones. Where Tijeras Canyon sors. first encounters the weak structural zone an anomalous Erosion of the Tijeras system on the east side of the side fork branches acutely backward to the southwest on Sandias is into formations of diverse composition and line with the main canyon running northeast. This sharp hardness along with faults and folds. As a result the fork, coupled with an on-line fork on the east side of the canyon system is marked by straight and curved mountains forms an acutely crossed or scissor-shaped alternating hogback ridges and valleys with erosion canyon system. Early explorers, noting this arrange- corresponding closely to structure and rock composi tion. North of 1-40, where folds are present, landforms resemble the Ridge and Valley country of middle Pennsylvania; south of 1-40 where beds dip more gently, as in the Cedro Canyon area, landforms resemble parts of the Allegheny Plateau of western Pennsylvania. SAN PEDRO CREEK AREA The northeastern side of the Sandia Mountains is drained by San Pedro Creek. The large system of tributaries of San Pedro Creek includes everything north of a low divide about one mile south of Antonito; all the country along NM-14 north to Golden; the northern side of Monte Largo; the east slope of the Sandias between Armijo and La Madera Canyons; and the Hagan coal basin area. As in the northern part of the Tijeras drainage, landforms are mainly ridges and FIGURE 5—SANDIA GRANrrE, FRESH AND WEATHERED OUTCROPS. valleys adjusted to the composition and structures of the ABovE ROADCUT ALONG 1-40. sc. 25. T. ION.. R. 5 E. stratified bedrock, except in the eastern Hagan basin

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(Johnson, 1932) because often they are the apices of the more extensive alluvial fans. The bare rock surfaces have local patches or narrow strips of alluvium that is being swept across the bedrock to the alluvial plain. The outer margins of the bare rock pediment are gradational into the alluvial fans by thin veneers of sand and gravel that are temporarily resting during their transport down the slope. West of the bedrock border the surface is underlain by a blanket of sand and gravel which thickens away from the uplift. Where the sand and gravel is tens of feet thick erosion only rarely exposes bedrock; this part of the piedmont is largely formed by aggradational deposition. The entire surface outward from the mountain including the aggraclational outer part as well as the near-mountain rock fans and alluvial FIGURE 6—THE GREAT GRANITE Shield AND Thumb SURMOUNTED fans is referred to as a bajada. Commonly, BY CRESTAL PENNSYLVANIAN BEDS. YOUTHFUL Ju TABO CANYON truncated CUT THROUGH RINC0N RIDGE OF MICACWUS QUARTZITES IN faults related to the uplift or the margin of the subsiding FOREGROUND. basin lie beneath the bajada. West of these faults the thickness of gravel may suddenly increase to tens, and in some of the eastern tributaries of the system. In hundreds, or, in some instances, thousands of feet. this area and extending to NM-14 the folded Mesozoic Coalescing alluvial fans along the base of the Sandias beds were covered in early Pleistocene time by the have built a piedmont plain that descends toward the expansive Ortiz pediment gravel. Subsequent erosion of axis of the Rio Grande valley. Normally the drainage this homogeneous blanket resulted in a partially den would consist of a system of partly braided distribu dritic canyon system superposed across the underlying taries, flowing to the Rio Grande, but this system has beds, uninfluenced by structure or rock character. been modified considerably by late Pleistocene cutting of an inner valley by the Rio Grande. As a result the LAS HuERTAS CANYON distributary streams leading to the Rio Grande have been incised, especially near the inner valley. Tijeras Las Huertas Canyon enters the northern end of the Creek which has a larger volume of runoff than the mountains and follows a south-trending fault zone others has been incised all the way to the mountain between the uplifted Montezuma Mountain block (east) front and well into the mountains. and the main Sandia block (west). The canyon is long The incision process results in interlocking of new and narrow and abruptly terminates against Capulin tributaries as they erode headward into the older Peak ridge near Palomas Peak. Tributary canyons east distributary system. During the process there of Las Huertas are steep and short; those are to the west are numerous diversions and long and relatively shallow captures by the younger up the dip slope toward system. Sandia Crest. SANDIA RIDGE AND Di SLOPE MARCOU’S 1853 SURVEY The Sandia crest line is 13 miles long from Tijeras In 1853 the Congress authorized explorations for a Canyon to its plunging northern terminus near Placitas. railroad route to the Pacific coast. Several parties were Two principal eminences stand out on the ridge profile, sent out in the spring of 1853 by the Secretary of War, Sandia Crest (10,678 ft) including the adjoining high Jefferson Davis. According to Northrop (1962, 36), Sandia Peak (10,447 ft) and South Sandia Peak p. (9,782 The ft). The ridge line is broadly convex French-Swiss geologist, Jules Marcou, accompanied eastward in the Lieut. A. W. Whipple on his expedition along the 35th parallel, vicinity of the Pino Canyon-Bear Canyon embayment which left Fort Smith, Arkansas on June 16, 1853, traveled which appears to be due to a frontal fault jogging into across the Texas Panhandle, and reached Tucumcari Sept. 22. the uplift. As a result the same erosional slope up the Here Marcou found an abundance of oysters, noting “I have escarpment intersects lower elevations seen there myself at least two or three thousand,” which he on the uniform took to dip slope of the be a variety of Gryphaea dilatata, a characteristic east side of the Sandias. However, the species of the Upper Jurassic Oxford Clay of England. He later Pino Canyon-Bear Canyon reentrant is not the only named his new variety Gryphaea dilatata tucumcarii and in a contributing factor. The high ridge line at Sandia Crest paper read before the Sociêté Geologique de France claimed have is due partly to the protection from erosion afforded by to discovered the first Jurassic rocks and fossils in all of North America. (Ironically, we now regard the Tucumcari the jutting Rincon Ridge west of Juan Tabo. Addi outcrops as Lower Cretaceous, not Upper Jurassic.) tionally a number of cross faults concentrate in the The expedition continued westward, reached Cerrillos Oct. reentrant area, and fracturing related to them may aid 3, Albuquerque (population of 2,500 in the town and its erosion. environs) Oct. 5, and Tijeras Canyon. Oct. 8. Marcou and Dr. John Bigelow. the botanist of the expedition. started the ascent SANDIA PIEDMONT of the east slope of the Sandia Mountains Oct. 8 and achieved the crest on Oct. 10. Marcou collected Pennsylvanian and This surface consists of two principal parts. Next to Cretaceous fossils from several localities in the Albuquerque the mountain front is an irregular border cut on the Galisteo-Pecos area. In 1854 Marcou became ill and decided to uplifted Precambrian take all his fossils, minerals, and rocks to France and work up bedrock. At the mouths of his report there. He packed up and prepared to sail. ThIs canyons, these rock surfaces are referred to as rock fans proposal displeased Jefferson Davis, who insisted Marcou stay 16

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in this country until he had completed and submitted his William P. Blake (1856) report. But Marcou sailed and was then ordered to turn his prepared a report on the collections over to the U.S. Ambassador in Paris. This he geology of the route, based on Marcou’s field notes and eventually did only in part: some of the fossils and apparently collections. Accompanying that report is a geological most of the rocks were returned to Washington and given to strip map, 36 inches long and lithographed in several (W. P.1 Blake, who studied the rocks and sent the fossils to colors, between latitudes James Hall Albany 34° and 36°N, extending from at for identification. Hall appears to have the received par of the collections from Pecos but not those from Mississippi River near longitude 91°W to Los Tijeras Canyon or the Sandia Mountains. In 1856 the Whipple Angeles and the Pacific Ocean near longitude 1 18°W. Blake-Marcou report was published as a Congressional Docu The map is entitled ment; Marcou’s field notes in French are given in left-hand “Geological map columns and a translation by Blake in right-hand columns. of the route explored by Lieut. A. W. Whipple. Corps of Top.l Marcou published several papers written in French fand Eng)’5 near the parallel of 35° north latitude from the Mississippi German} in various journals during the period 1854-1857 and. River to the Pacific Ocean, 1853-1854; Prepared in the office of Pacific in 1858. a book written in English, modestly entitled Geologvof Rail Road Explora tions and Surveys War Dept.mt. From the North America and containing a chapter. ‘Geology of New notes and collec tions of the geologist of the expedition. M.r Mexico.” The book was printed in Zurich and Jules Marcou. by contains William P. Blake.” hand-colored maps and descriptions and excellent litho graphed illustrations of a number of new species of Pennsylva The scale of the map is 1 inch = 47 miles. Camps shown nian and Upper Cretaceous fossils. in our area include 57, south of Galisteo; 58, San 18

that rest upon the Quart:ose 59. Albuquerque. but curiously this name is quitting the last beds of limestone Antonio: .iletamorphic Rocks, we find Serpentine; then we come upon omitted. masses of Granite. which form the centre of the line of Blake’s report was also accompanied by a geological dislocation of the Rocky Mountains. cross section from the Mississippi River to the Pacific Marcou adds: Ocean, 32 inches long and lithographed in several In a lengthy footnote (p. 20-21), colors, prepared by Marcou: a quaint feature of this Having reached Albuquerque. New Mexico. the 5th October the 10th November. cross section is that tiny U.S. flags are used to designate 1853. the expedition remained there until to recruit the strength of the party and prepare for crossing the campsites. Californian desert. I profited by this interval to explore the Better maps and cross sections were published by country comprised between Albuquerque. San Antonio. Pecos Marcouin 1858. and Santa Fe: and the 8th October I started with my friend Dr. The complete title of Marcou’s (1858) book is John Bigelow. the botanist of the expedition. to ascend the highest peak of the Sierra de Sandia. Geology of North America: with two reports on the prairies of In this exploration. which continued until the 20th October. Arkansas and Texas. the Rocky Mountains of New Mexico I studied with attention the rocks of San Antonio Pass. of and the Sierra Nevada of California, by Jules Marcou. Antonito and of the Summit of the Sierra de Sandia, also those professor of geology in the Federal Polytechnic School of of the environs of the villages of San Pedro. Tuerto, Galisteo Switzerland: formerly United States geologist: and ex and Pecos. The ascent of one of the most elevated Summits of geologist of the “Jardin des Plantes” of Paris. the Rocky Mountains.—which after all is not a very easy matter, considering the wilderness, the ditliculty of the roads The frontispiece of the book is a color-lithographed and the fear of the Apache Indians—was effected by Dr. geologic map of the United States entitled Bigelow and myself the 10th of October 1853. We chose the most elevated poini of the Sierra de Sandia seen from Carte géologique des Etats-Unis et des provinces anglaises de Albuquerque. which attains the height of 12.000 feet above the l’Amerique du Nord, par Jules Marcou. publiée dans le level of the sea. The culminating points of all this Sierra are Bulletin de Ia Sociéié Géologique de France, Tome XII. composed of Carbonçferous Limestone, which here merits most Séance du 21 Mai 1855, et dans les Annales des Mines, Tome its name of Mountain Limestone, for it is the only VII, 1855. truly limestone of any importance met with in the Rocky Mountain region. From the five or six upper beds. I collected the At the top of this map is a 20-inch long, east-west following fossils: Productus Cora, P. scabriculus, P. Flemingii; geologic cross section, entitled Profil geologique dii Fort Zaphrentis cylindrica, Z. Sansburyi and Orthoceras Nova Smith (Arkansas) au Pueblo de los Angelos (Calfornie), Mexicana. to San Antonio, in the middle also lithographed in several colors. The central part of In going from Albuquerque of the Pass or Cañon of San Antonio, 10 minutes from the the cross section, showing New Mexico, is reproduced village of Tigeras. there is a bluff of Mountain Limestone on here as fig. 7. the right of the road, forming a grand perpendicular wall. [This Plate 8 of Marcou’s (1858) book is Geological map of was at Seven Springs.] Fossils abound in the strata of this bluff, New dated 1857, lithographed in several colors and I collected the following species: Productus semi- Mexico, punc tat us, P. pustulosus, brown) was applied by hand. redc ulatus, P. Cora, P. Flemingii; P. except one color (dark P. pyxidformis, Terebratula plano-sulcata, T. subtilita; Spirffer This strip map, 23 inches long and 5 inches high, lineatus, S. striatus, S. Rockymontani; Amplexus coralloides extends along latitude 35°N from longitude l03°W and Zaphrentis Stansburyi. (east of Tucumcari) westward nearly to 109° (near Zuni The mean thickness of the Mountain Limestone of the Rocky Mountains in the region environing Santa Fe and Albuquer Defiance). The scale is 1 inch = nearly 15 and Fort que is 700 feet. miles, which is three times larger than the scale of the map mentioned above that was published by Blake Marcou’s field notes, translated by Blake (1856, p. (1856). A dashed “line shows the trace of Marcou’s 141-143), read: Survey, made during the months of September, Oc Ocober 8—From Albuquerque to Camp A. below Tejera.—On tober, November and December 1853.” The central part going easterly from the Rio Grande, we travel ten miles on the of the map is reproduced here as fig. 8. Small triangles alluviums of the Rocky mountains: then, before entering the indicate campsites, numbered 1 to 38. Note camps 14 cañon of San Antonio, we found outcrops of blackish-grey large crystals of white feldspar, at Tijeras, 17 at Antonito, 18 granite, with hornblende and and 15 at Albuquerque, 16 sometimes yellowish. These exposures of granite are three at Tuerto (Golden), 19 east of Galisteo, and 20 at Pecos. miles wide. Then, after passing the inhabited ranchos, we have At camp 17, note the side trip to Sandia Crest. a rose-colored granite, with but little feldspar, and dykes of Marcou (1858, 20-22) wrote about the expedition rosy-white quartz: finally, a green serpentinoid trap. contain p. Devonian age, and, in heading westward through Tijeras Canyon, ing strata of metamorphic limestone of contact with this green rock, the Mountain limestone or Lower following section: Immediately on leaving the village of Tigeras [sic]. which is carboniferous. At Camp A we have the situated in the middle of the Pass that crosses the Rocky Mountains, called here Sierra de Sandia, also Albuquerque Mountains: black schistose clay is seen, belonging to the Coal-measures, then grayish blue limestone, containing a great quantity of fossils. These last strata of schist and limestone are very much upheaved, dipping to the East at an angle of 30 or 40 degrees: they rest on metamorphic rocks. The principal fossils found in the limestone, which belongs to the Mountain Limestone or Lower Carbonferous, are: Productus semi reticulatus, P. cora, P. Flemingii. P. puncta (us, P. pustulosus and P. pyxidformis, Terebratula plano-sulcata; Spirfer lineatus, S. striarus; A mplexus coralloides. Zaphrenris Stans burn; all fossils very characteristic of the Mountain Limestone of Arkansas, Missouri, Iowa. Illinois. Indiana. Kentucky, Tennessee, Virginia and Pennsylvania, as well as in Europe,

and even in Asia, Australia and South America. . . On 19

The serpentinoid trap is in contact with the limestone of the The height inferior carhoniferous. which dips of the Sandia Mountains is reported to be to the Cast at an angle of 12,000 from thirty-live to forty degrees. the heads of the beds turning ft in one account and 10,000 ft in another; towards the west. The trend is north and south, or from three actually it is 10.678 ft. Apparently elevations o live degrees were E. of N. This limestone is grevish-blue. determined both by aneroid barometer and sometimes black; very compact. with by survey a conchoidal fracture, ing methods, The thickness of the Mountain and sometimes breaks easily when it contains a lumachelle of Limestone fossils. is given as Some strata of very thin and black clay shales are 700 ft in one account and that of the intercalated. This limestone has a thickness of three hundred carbonferous as 2,000 ft in another. In the field feet. notes It is said that a short distance further south ii contains Marcou cited Product us giganreus, but beds of bituminous coal. by 1858 he had The fossils are not vers abundant or decided that this form was not present. well preseved. I gathered principally the Productus giganteus The “Camp A. below and punctatus. a Spirqer. and two Terebraiulae and Pohpi; Tejera,” or Humboldt of the fragments of the stalks of encrinites forming marble—{”]; field notes is camp 16 (triangle) on the map; “Camp B, and many small Producti. the species Cora. From the camp at Douglas, or Antonitto” of the field Tejera notes is camp 17 we have constantly on our right, for the distance of a (triangle) at Antonito mile, this carboniferous on the map. “Tejera” of the field limestone, then in the village we again notes became meet the Trias with all its divisions. Behind “Tigeras” in 1858; modern spelling is San Antonio. near Tije ras. Antonitlo [sic}. we have white gypsum of the Trias; all the beds dip to the east at angles of from twenty to forty-live degrees. Marcou’s fossils are described and illustrated in our October 9.—Frvm Camp A. Humboldt. to Camp B, Douglas, discussion of Pennsylvanian stratigraphy. or Antonitto.—We have the inferior Carboniferous as far as Tejera village, where, as the Trias. the coal has been too much compressed and does not appear. The carboniferous has a GEOLOGICAL SOCIETY OF AMERICA thickness of two thousand feet (2,000,) the Trias four or five thousand (4.000 or 5,000.) Behind San Antonio we find white ANNUAL MEETING 1907 gypsum. and all our route, as far as Camp Douglas. is on the In 1907 the Geological Society Trias. Alluvium from the mountains, and without striated of America, joined by pebbles. We have immense erratic blocks. the Cordilleran section, held its annual meeting in October 10.—We ascended the Albuquerque mountains Albuquerque (Northrop, 1966, 10, 11). W. G. Tight (Sandia p. mountains) 10.000 feet high. They are surmounted by gave a paper on the geology of the Sandia Mountains, the limestones of the inferior carboniferous. The direction is and a field trip was held in the N. and S.. and the rocks dip to the eastward Sandia-Manzanita at an angle of Mountains area between Tijeras from twenty-live to thirty degrees. Gold mountain is less and Hell Canyons. For elevated than Albuquerque mountain. From Camp Douglas the occasion Dr. Tight prepared a “Sketch Map, Sandia we followed for one and a half miles a cañon in the upper Mountains Excursion, G.S.A., 1907” (fig. 9), showing Trias; then we commenced with the greyish-white. blackish the geology, the route, two structure limestone of the sections, and a carboniferous formation; the coal does not brief mileage log. The participants appear—it has been too much compressed. In these went from Albu carbon querque into Tijeras Canyon iferous rocks we found the following fossils: Productus. to about Seven Springs. giganteus They and punctalus; Terebraiulae. Spiri/erae. Orthocera. then returned to near Carnuel where the route Zaphrentis and Crinoids; the Zaphrentis was very abundant. followed the old trail from Santa Fe to Socorro through Coal is found further the to south, in the Manzana mountains. Garcia Canyon to Coyote Canyon, with a side trip up Several beds of black shales, four to six feet in thickness, and Coyote Canyon. They continued southward along very thinly stratified, are found between the beds of compact the limestone. mountain front to about Kidney-shaped masses of black silex are present in Hell Canyon before returning the limestone, and at the summit it is a little marty. with silex, across the mesa to Albuquerque, a trip distance like of 51 the limestone of Fort St. André. There are no visible traces miles. of glaciers in the canons. The section is much like that seen The geologic map reveals a considerable understand yesterday. Some beds of very hard and rose-colored sandstone are ing of the principal geologic interposed in the limestone. One of these beds is of coarse features. Of interest is the rolled grains. The limestone is the predominating rock. fact that the Cibola Gneiss is mapped as “Fine granite,” the Tijeras Greenstone as “Intrusive,” Among discrepancies between and the East the field notes made Mesa alluvial fan and pediment gravel by Marcou in 1853, as translated as “Mesa by Blake (1856), and Marls.” The spelling of “shist” is also curious. Marcou’s (1858) account, the following may be noted. -TI C rTi ‘0

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Rocks within the area range in age from Precambrian T. ION., R. 5 E. a northeast-trending belt of metamor to Holocene, and include an array of igneous. metamor phic rocks appears and occupies the Canyon nearly to phic, and sedimentary lithologies. However, lower and Tijeras where it passes beneath Paleozoic beds. The middle Paleozoic rocks, so well represented 150 miles to Tijeras belt is prominent in Cerro Pelon Ridge and into the south, are completely missing in the Sandia area. Coyote Canyon along the southern edge of the area. Among the igneous rocks are basic to acidic types of The metamorphic sequence south of Tijeras Canyon plutonic and hypabyssal origins. Both thermal and extends southward in a nearly continuous belt along the dynamic metamorphic rocks of all the common types western side of the Manzanita and Manzano Mountains are represented. The sedimentary rocks are rather (Reiche, 1949; Stark, 1956). Gneiss, schist, quartzite, evenly proportioned among shale, sandstone, and lime and greenstone occur in distinctly separate masses stone and are marine and continental in origin. Among except for some of the quartzite that lies within the the continental types are flood-plain, paludal, eolian, gneiss along Tijeras Canyon. Only the petrology of the lacustrine, piedmont, and bolson environments. There is rocks is considered here. Some of the complex structural also considerable intertonguing of continental and ma relations are explained in the chapter on structure. rine types. Lithology and age are summarized in the The northwesternmost unit of the belt is here stratigraphic table (fig. 10). referred to as the Cibola Gneiss. It forms an outcrop strip up to PRECAMBRIAN about 0.75 mile wide by 5 miles long between the Sandia Granite on the northwest and the Tijeras Precambrian fault rocks of the Sandia Mountains and and Tijeras Greenstone on the southeast (fig. 11). The environs are scattered and diverse. The most extensive gneiss is distinctly foliated, dipping 40 to 65 degrees exposed unit is the Sandia Granite which predominates northwestward toward the granite contact. Midway in the uplift. in Metamorphic rocks lie in three principal the northwestern part are narrow strips of quartzite. areas, Tijeras Canyon and vicinity, Monte Largo, and Where present the quartzite holds up a ridge in the Rincon Ridge west and northwest of Sandia Crest. gneiss as seen from 1-40 just west of the big turn in Tijeras Canyon. The quartzite is as much TIJERAs CANYON METAM0RPHIcs as 200 ft thick and trends left diagonally across the belt and is Most of the lower part of Tijeras Canyon is eroded truncated by the Tijeras fault. The gneiss is generally into Sandia Granite, but beginning in the NE ¼ sec. 30, light pinkish and medium grained, and the parts either side of the quartzite are not greatly different — in appear ERA SYSTEM SERIES GROUPS, FORMATIONS, MEMBERS ance. However, the southeastern part is slightly finer grained Holocene Landslides and Lodewick (1960, p. 13-14) noted that it o Quoternory and Valley alluvium contains ö Pleistocene more quartz than the feldspathic part to the “I Terraces and pediments 0 northwest of the quartzite strip. Part z Pliocene of the difference iii Miocene Santa Fe Formation may be due to magmatic (.) replacements from the Sandia Tertiary Oligocene Espinaso Volconics Granite. In Eocene Galisteo Formation order of abundance the gneiss consists of Paleocene quartz, microcline, microperthite, oligoclase, and biotite Mesoverde Formation with accessory magnetite, ilmenite, zircon, and sphene. Cretoceous Upper Moncos Shale The texture is uniformly Dakota Sandstone gneissic and homogeneous but locally layered biotite foliation is present (fig. 12). Morrison 0 Formation As the Sandia Granite is approached the gneiss 0 Todilto Formation: Gypsum ,, j urossic Upper becomes w and limestone members irregularly coarser grained and develops more Entrado Sandstone

Chinle Formation Triassic Upper Santa Rosa Sandstone

Bernal Formation

Guodolupian Fourmile Draw Member Perm ion San Andres Bonney Convon Member Formation Rio Bonito lember Glorieta Sandstone Member o Leonardion San Ysidro Member ‘i’eso uJ0 Formation Meseta Olanca Member -I Wolfcompian Abo Formation

Virgilian 0 Madero torkosic limestone member Missourian Lower gray Pennsylvanian Desmoinesian Formation limestone 2I I member Atokan Sandia Formation Morrowan — —. L — — — — Mississippian Osagean Arroyo Peasco Formation Pho,o by Donald A. Myers PRECAMBRIAN Gneiss, Schist, quor/zile, greens/one, groni/e FIGURE I—PRECAMBiuAN I BELTS ALONG TI.tERAS CANYON. PENNsYLvANIAN BEDS CAP CERR0 PEL0N RIDGE. VILLAGE FIGURE 10—STRATIGRAPHIc TABLE. OF TIJERAs AND IDEAL CEMENT PLANT BEYOND. 22

NEAR US-66 AND SANDIA FIGURE 12—CIB0LA GNEIss OUTCROP. GRANITE TRANSITIONAL CONTACT. Photo b Donald A Myers FIGURE 14—TuERAs GREENST0r’tE BELT ALONG TIJERAS CANYON (fig. 13). Some minor FORMATIONS wavy foliation and feldspar augen (LooKING NORTHEASTWARD). SANDIA AND MADERA RIDGE OF migmatitic structures occur locally nearing the contact; ALONG CERRO PELON RIDGE ON RIGHT. FAULTED WT OF Lodewick (1960, fig. 4) delineated sillimanite gneiss QUARTZITE IN CIB0LA GREIss CROSSES TIJERAS CANYON near the contact. The contact with the granite is TRACE OF TIJERAS FAULT. widths of 100 to 300 ft. generally gradational through occur together. Epidote, quartz, plagioclase, and zircons in the gneiss and monly Lodewick (p. 25-30) compared calcite are also common along with lesser quantities of their differences, together with the granite and based on biotite, sericite, actinolite, and opaque minerals. petrographic relationships, con the field structural and Although the greenstone is mostly schistose there are belt was derived from arkosic cluded that the gneiss large masses distributed along the belt of nonschistose (quartzite), and siltstone. sandstone, pure sandstone mafic metaigneous rocks. Bruns (1959, p. 25) recognized Canyon is here named the The greenstone of Tijeras metapyroxenite. metadiorite, metadiabase, metabasalt, occurs in a belt about I mile wide Tijeras Greenstone. It and metarhyolite interspersed with the hornblende and the Tijeras fault and Cibola and 5.5 miles long between chlorite schists. Some parts of these rocks are nearly and Cerro Pelon ridge on the Gneiss on the northwest unaltered and recognition by composition and texture is (1959) mapped the greenstone southeast (fig. 14). Bruns not difficult. Epidotization, sericitization, and chloritiza and metasedimen and recognized several metaigneous tion in veinlets or in fine granular mosaics are the The greenstone is typically tary types within the belt. common metamorphic effects. Why some masses have from nonfoliated to dark green, its texture ranging escaped conversion to schists is not clear. A few masses generally parallel to the highly schistose. Foliation is resemble residual plugs; others, sills or flows. Original dips 60° to 70° SE, although elongation of the belt and form, texture, or primary structure may have deter from this attitude. there is considerable local variation mined the development or lack of development of either hornblende or Foliated greenstone is generally schistosity. Perhaps the nonschistose bodies were mas but they corn- chlorite schist; either may predominate sive or dense and the schistose rocks were thin bedded, less dense, or tuffaceous. The metasedimentary rocks associated with the greenstone occur mostly next to Tijeras fault in secs. 29, 31, 32, T. 10 N., R. 5 E., but also in small masses elsewhere in the greenstone. They consist of mica schist, quartzite, quartz-mica schist, phyllite, marble, and banded epidote marble resembling ricolite, a variety of verde antique. Quartz-mica schist is concentrated along the border of the metarhyolite and mica schist (mostly muscovite) and is commonly intercalated with nonschis tose metaigneous layers. Quartzite occurs as a band along the boundary between the metasedirnents and the typical greenstone near the bottom of Tijeras Canyon in sec. 29, T. 10 N., R. 5 E. There are marble lenses in the greenstone locally; one particularly good occurrence bears sulfide ore at the York mine in sec. 10, T. ION., R. 5 E. A small area of the Tijeras Greenstone is exposed in Cedro Canyon in sec. 35, T. 9 N., R. 5 E., where faults have combined to produce an inlier sur FIGURE 13—CIB0LA GNEI55 SAMPLE. NEAR GRANITE CONTACT. and erosion ARE BIOTITE: CENTER OF SEC. 20, T. 10 N., R. 5 E. DARK STREAKS rounded by Pennsylvanian rocks. FELDSPAR: WHITE MEDIUM-GRAY BANDS ARE AUGEN OF POTASH Quartzite and schist bound the greenstone belt on the NOT READILY STREAKS ARE PLAGIOCLASE: QUARTZ IS south and southeast. Quartzite holds up Cerro Pelon DISTINGUISHABLE. 23

and extends southward and southwestward to Coyote sillimani te- and garnet-bearing gneisses to andal usite Canyon and into the edge of the Four Hills area west of schist. The sequence at the Rincon is not as white as Tijeras fault in sec. 14, T. 9 N., R. 4 E. In this that at Cerro Pelon, and the rocks tend more to light metamorphic sequence white and grayish-white quartz gray. even to dark brownish gray. The two sequences ite, about 2,000 ft thick, forms the lower part; schist, lying on opposite sides of the Sandia Granite pluton can phyllite. and slate form the upper. The principal part of hardly be correlative. the sequence occurs between Cerro Pelon and Madera A small outlier of the Rincon metamorphics Canyon where a northeast-plunging is set of isoclinal folds exposed at the base of Montezuma Mountain in is overturned and thrust northwestward the over the green- southeastern part of the San Antonio de Las Huertas stone belt. In the Four Hills area the folded sequence is Grant. intruded by the Sandia Granite. SANDIA GRANITE MONTE LARG0 METAM0RPHIcs The escarpment of the Sandia Mountains is dom The Monte Largo Precambrian area is exposed in a inated by the distinctive light-colored porphyritic pluton narrow northeast-trending horst between the Tijeras known as the Sandia Granite. It extends for 20 miles in fault and the Gutierrez fault. Pennsylvanian rocks outcrops along the front of the mountains from the tip nonconformably overlie the Precambrian at both ends of the Four Hills in T. 9 N. to near Placitas. Its principal of the horst, and a low, broad northwest-trending cross outcrop belt is bounded on the west by alluvial outwash anticline has uplifted Precambrian in a rectangular area or locally downfaulted Tertiary Santa Fe sand and of about 7 square miles to form Monte Largo. gravel and on the east in Tijeras Canyon by the Cibola The Precambrian is generally foliated in the direction Gneiss. Along the crest of the range it is bounded by the of the elongate horst. The metamorphic rocks consist overlying Pennsylvanian rocks (fig. 15). Several inliers principally of quartz-feldspar gneisses, hornblende and of the granite are exposed east of the crest in canyons biotite gneisses, some muscovite and hornblende schists, eroded through the Pennsylvanian dip slope. Overall, and quartzite. All these rocks were thought by Huzarski the Sandia pluton appears to trend northeastward (1971) to have formed from sediments and metamor across the range between the Rincon Ridge metamor phosed synkinematically to an amphibolite facies. The phics on the northwest and the Tijeras Canyon meta metamorphics are locally intruded by small bodies of morphics on the southeast; the exposed pluton width is granite and local aplite and pegmatite dikes. Lambert about 9 miles. The length is not known in the subsurface (1961, fig. I) discovered small bodies of carbonatite and but might be several times its projected 20-mile outcrop quartz-tourmaline-calcite rock in the southwestern cor length. It is of interest that its projected extent to the ner of the Monte Largo complex in association with southwest beneath the Rio Grande trough is on line breccia plugs. The carbonatite consists largely of dolo with similar granite in the Ladron Mountains some 50 mite, apatite, phiogopite, and magnetite, with local or miles away. minor quantities of chlorite and possibly nepheline and The Sandia Granite is homogeneous throughout its pyroxene in the form exposures. of melteigite (Lambert, 1961, p. Perhaps its most distinctive aspect is its 68-70). Analysis of the carbonatite by Chapman, Wood, porphyritic texture—microcline phenocrysts in a grani and Griswold (personal communication) showed 0.295 toid groundmass of quartz, feldspars, and micas. In Nb205. weathered outcrop the rock has a distinctive nubby surface owing to more rapid disintegration of the RINc0N RIDGE METAM0RPHIcs granular matrix relative to the microcline (fig. 16). Some microcline phenocrysts are as One of the more prominent features of the Sandia much as three inches across (Fitzsimmons, 1961, 91) but are Mountains is Rincon Ridge (8,201 ft) which stands as a p. most typically about one inch. The fresh granite large jutting corner from the northern part of the range. is most commonly light gray, but colors range through The existence of the ridge is due largely to its makeup of medium gray, resistant quartzite and quartz-mica schist. Hayes (1951, P. 7, 8) referred to the rocks as the Juan Tabo sequence and believed that the thickness could be in excess of 7,000 ft. Within the sequence there is much gradation between quartzite and schist. Pure quartzite such as dominates the terrane at Cerro Pelon is not the rule; Hayes estimated that 75 to 80 percent of the rock is either micaceous quartzite, which is more abundant and contains much detrital feldspar, or micaceous quartz schist. Some feldspar and sillimanite schists occur near the Sandia Granite. Greenstone and chlorite schist occur in patches along the northwestern part of the Rincon in secs. 22, 14, T. 12 N., R. 4 E. Green and Callender (1973, p. 643) described a contact aureole in the regionally metamorphosed sedimentary and volcanic FIGURE rocks formed by the Sandia Granite 15—NORTH WALL OF UPPER PART OF LA CUEvA CANYON. intrusion. The SHOWS aureole, more than DIVERSE JOINTING IN SANDIA GRANITE. MUCH OF WHICH 1,000 m wide, ranges from DIPS AT LOW ANGLES HERE. 24

In general. oligoclase is altered to epidote and quartz and b,ocite to chlorite. Sphene. magnetiie. and apalite remain nearly unaltered, and microcline is not much altered except to sericite. as is usual throughout the granite. The highly altered material is actually slightly more resistant to weathering than fresh granite. and forms low ridges and knobs. On the other hand, these altered rocks seem to be zones of structural weakness, and more often than not are followed by faults. Slickensides on altered material show that at least some of the movement along the faults has occurred since alteration took place. Alteration does not extend into the overlying Pennsylva nian limestone, even though the faults do continue into it. Where aplite dikes are crossed by the fractures along which the altering fluids moved, they are altered in the same way as the granite. Faults are so often associated with the altered rocks that degree of alteration proved to be a mapping guide. The alteration must have occurred after emplacement of aplites and pegmatites. but before the main periods of faulting. for some intensely altered bands show no evidence of shear or FIGURE 16—SANDIA GRANITE SHOWING TYPICAL WEATHERED displacement. In addition, veins and stringers of epidote SURFACE. REsIsTANT MICROCLINE PHENOCRYSTS AND SMALL associated with the alteration phase are displaced by faults, INCLUSIONS. and spessartite dikes cut by faults along altered zones are not faults were active pinkish, and light reddish brown. Fitzsimmons has altered. It is possible, however, that some that slickensides on altered rock were reddish tints are primarily in the before alteration, and noted that the created by later movement. microcline and that color variations appear to be more common near the unconformity with the overlying Magmatic inclusions are common in the Sandia Pennsylvanian rocks, implying a pre-Pennsylvanian Granite (fig. 17). They range in size from tiny blebs to weathering effect. However, this is not a consistent bodies several feet in length. Flattened, elongate, and relationship because the reddish coloration is evident rounded shapes occur usually with no systematic ar for 300 to 400 ft below the unconformity around the rangement. They are not uniformly distributed in the head of La Cueva Canyon. granite and are more abundant in some areas than The most common minerals of the Sandia Granite others. Shomaker (1965, p. 15) found four petrologic are microcline, quartz, oligoclase, and biotite. Accessory types: 1) melanocratic [dark-colored] granitoid, 2) minerals generally consist of sphene, magnetite, and leucocratic [light-colored] granitoid, 3) gneissic, and 4) apatite, with rare occurrences of hornblende, muscovite, quartzitic. Dark-colored granitoid inclusions are most tourmaline, or pyrite. The rock is a porphyritic biotite abundant and, except for being fine or medium grained granite in which the essential minerals commonly and slightly foliated, are of very nearly the same average about: quartz, 35 percent; microcline pheno composition as the granite. The light-colored types crysts, 15 percent; albite and oligoclase, 35 percent; differ only in containing less biotite and more quartz. biotite, 10 percent; microperthite, 5 percent. However, Shomaker noted them to be in spherical, ellipsoidal, or considerable variations from these proportions occur bladed shapes. The gneissic types are smaller, banded locally and Feinberg (1969, p. 10) has noted as much as in variations of biotite, quartz, and feldspar. Quartz 51 percent quartz and 43 percent biotite; Shomaker ite inclusions are the least common, small, and less content suggestion of diges (1965, p. 10) has estimated a range in quartz rounded. All inclusions show some from 18 to 36 percent. He also estimated sphene as high tion by the magma, and reaction halos, especially of as 5 percent, and magnetite 4 percent. Through areas of biotite, are common within the granitic types. Micro several acres, biotite reaches concentrations of 50 per dine porphyroblasts similar to the smaller phenocrysts cent appearing to be primary or early magmatic concen in the granite are common in the inclusions. Nearly all trations; and in some areas the microcline phenocrysts the inclusions probably come from the country rock and amount to 20 to 25 percent of the granite. are considered xenoliths. Late magmatic, deuteric or perhaps hydrothermal alteration has modified considerable volumes of the granite. Such alteration occurs in local patches but is related to primary fracture systems. It is later than the aplite and pegmatite dikes associated with the granite. Shomaker (1965, p. 20-22) has carefully described the alteration product consisting of hematite, chlorite, and epidote as follows: Long bands of granite that has been highly altered by hydrothermal hematite, epidote, and chlorite are very common throughout the area. Apparently the introduction of material follows well-defined fractures, for a definite lateral progression of alteration is visible. The outer zone consists of granite whose phenocrysis are pink, probably due to small amounts of hematite, or to iron in solid solution. This granite appears no different in thin section from unaltered material. Closer to the axis of the band, fine fractures begin to appear. and finally, GRANITE WITH NUMEROUS along the axis, the granite may be altered entirely to a mass of FIGURE 17—OUTCRoP of SANDIA BOULDERS ALONG US-66 IN epidote, chlorite, and hematite. Only some fragments of INCLUSIONS. REstou& SPHEROIDAL hematite-stained potassium feldspar remain. TIJERAs CANYON. 25

Small masses of orbicular rock have been found in the strike direction; the principal stress axis appears to the northern part of the Sandia Granite, and these have have been north-south in the magma during growth. A been described briefly by Fitzsimmons (1966) and considerable number of centers or cores of the orbicules Feinberg (1969), and in more detail by Daugherty and lie loose in the weathered surface float near the cut face. Asqwth (1971), and Thompson and Giles (1974), and The axes of about 40 of these have been measured. Enz (1974). The principal known deposits occur just Prolate and oblate triaxial ellipsoids are about equal in south of the ridge spur along which the lower new La number; a lesser number are more or less eqwdimen Luz trail ascends. The orbicular mass is described in sional. In the group, the long axes ranged from I to 1.8 more detail than the Sandia Granite and some other inch; the intermediate axes, 0.6 to 1.4 inch; and the Precambrian rocks because of its unusual and striking short axes 0.6 to 0.9 inch. Sawed equatorial sections of character. New Mexico is one of II states from which the cores are commonly slightly squarish or obtuse only 19 occurrences are known; 8 of these are from rhombic in outline. California (Leveson, 1966). Cross-sections of the ellipsoids reveal numerous The main mass on which a small cut face has been minor distortions away from bilateral symmetry due dug is 500 ft south of to the Sandoval County line at an irregular growth but also in part to some deformational altitude of about 7,800 ft. It is reached by a short hike warping by plastic flow. Slabbed “urfaces of the rock from the next to the upper north switchback on the show some fracturing of orbicules. In other surfaces lower end of the La Luz trail. The principal outcrop orbicules appear to protrude into adjacent ones, as trends S. 75° E. up the ridge, and is about 40 ft long. A though by force of growth, with development of indi maximum of 7 feet is exposed more or less midway. The vidual orbicules apparently beginning at different times. upper smaller occurrence is about 65 ft higher and 150 In such instances, growth around later nucleation ft in a S. 65° E. direction up the ridge. The two deposits centers seems to have destroyed or thinned may be continuous outer shells with one another, but much hillside of previously formed orbicules nearby. debris prevents complete tracing between. The concentric bands consist predominantly of oligo In the small cut face at the principal exposure, the clase and biotite. These are usually wrapped around a northern contact of the body is exposed against the granitoid core which in many samples resembles the typical pinkish, porphyritic Sandia Granite. The upper, normal Sandia Granite, although not with as large hanging wall contact is sharp and dips N. 5° E. at 60° to phenocrysts as in the typical porphyritic granite. Some 65°; the lower contact is not well exposed, but appears cores are quite light colored consisting of orthoclase, in places to be gradational. In part, the footwall granite oligoclase, and to a lesser extent, quartz. Some slabbed is richer than normal in biotite, and feldspar pheno surfaces of the rock show biotite at the center, but crysts are more abundant and slightly more euhedral. A nearly all equatorial sections would probably show gradation is further suggested by thin wraps of biotite granitoid feldspar. Thompson and Giles (1974, around some phenocrysts. p. 911) found the cores to be biotite monzonite. However, the The northern 5 ft of the mass is almost completely cores are likely a facies of the regular granite. Sections orbicular with no more than 20 to 30 percent granitoid that are not equatorial may be misleading in making matrix. The southern 2 ft consists of 60 to 70 percent the core texture appear either slightly gneissic or light-colored granite with rounded floating orbicules 1 nonconcentric. Nevertheless, the concentric zones ex to 1.5 inches in diameter (fig. 18B). The highly orbicular hibit some regularity and the following consistency of main body contains more coarse crystalline biotite, order: whereas the floating orbicules of the footwall zone have I) Core less biotite and are finer grained. Orbicules in the main zone of weakly concentric-banded or un banded mass are larger than those in the footwall zone and granitoid rock 2) Intermediate commonly attain ‘maximum diameter of 4 to 5 inches. A zone dominated by biotite 3) Outer shell few orbicules adjacent to the hanging wall are nearly I of radiate oligoclase ft in greatest diameter, but most are granite autoliths The intermediate zone typically consists of wrappings with thin wraps of biotite. of biotite alternating with several thin concentric oligo Nearly all the orbicules in the main mass are triaxial clase or oligoclase and biotite bands. The biotite is ellipsoids, with major axes roughly parallel to the usually tangential in growth but may be radial or tabular form of the body. However, some are of oblique random in orientation. Outside the core the predom orientation as by slight swirling or plastic distortion. inant feldspar is oligoclase forming radiate columns and Within the dominant alignment there are also many needles in each concentric layer. In numerous places individual orbicules of aberrant crosswise orientation. radiate oligoclase is transected by tangential biotite. The following are axial dimensions (in inches) of 8 Accessory minerals that are common in the typical orbicules measured in the outcrop. granite also occur in the orbicules; these include apatite, zircon, and opaque minerals such as magnetite, pyrite, (I) (2) (3) (4) (5) (6) (7) (8) chalcopyrite, (inches) and ilmenite. Some malachite staining Near-strike axis 2 4.2 3 3 2.7 3 9 7.5 exists in the cut face. Deuteric epidote and chlorite are Near-dipaxis 1.2 3 2 2.2 2.2 3 6.2 5.7 present locally and sericite is widespread, especially in Near-width axis 1 2.6 1.5 1.5 1.3 1.5 5.5 3 the oligoclase of the orbicules. The upper smaller occurrence of the orbicular rock is In all examples the width axis is the shortest, and in 7 150 ft east of the main body and only 50 to 60 ft down or 8 orbicules the strike dimension is longer than the dip the ridge from a prominent cliff. This smaller body is direction. No. 6 is oblate discoid. Growth was easiest in poorly exposed, roughly on line with the lower body; it 26

f -

Ii ORBICULES OF OF GRANITE. B—MAIN OUTCROP CUT FACE SHOWING FLOATING A—MAIN OUTCROP CUT FACE SHOWING HANGING WALL FOOTWALI. SIDE OF THE TABULAR MASS. ABOUT 6 INCHES INTERVENES ON CUT FACE BETWEEN A AND B.

WALL NOTE D—FINE-GRAINED ORBICULES CHARACTERISTIC OF HANGING C—SAWED SLAB OF TYPICAL ORBICULAR PART OF A. ZONE AND UPPER OUTCROPS. PENCIL LINE ON FACE IS 2 INCHES. DIFFERENT CORES, SOME GRANITE. SOME FELDSPAR. AND SOME BIOTITE; DIFFERENCE MAY MERELY BE APPARENT BECAUSE SLICE FrancisKoopmancspecimen DID NOT GO THROUGH CENTER OF THE ORBICULE. NOTE ALSO GRANITE LIGHT-COLORED MATRIX WHICH IS FINER GRAINED THAN AUTHOLITHIC CORES.

F—CENTER-SAwED, ROUND ORBICULE FROM UPPER EXPOSURES. DIAMETER IS 4 INCHES; CORE DIAMETER IS 1.5 CORES; CENTER-SAWED. NOTE RECTANGULAR SHAPE HORIZONTAL E—ORBICULE BY INCHES. NOTE CONVEX OUTWARD BULGING OF CORE SHOWN AND FIRST BIOTITE WRAP; SECOND WRAP AROUND COARSE FIRST BIOTITE WRAP. FELDSPAR CORE IS SHOWN ON HALVES LYING FACE-DOWN. FIGURE I8—ORBICULARsTRUCrURES IN SANDIA GRANITE

texture is more ragged and less appears to extend for about 35 ft with a maximum the average granite; the the Sandia Granite becomes width of 4.5 ft. The orbicules are more rounded than in porphyritic. Up the ridge to 30-ft zone that extends the main deposit and are largely floating in granite in a quite dark colored in a 20- content becomes as high as 50 similar manner to the footwall zone at the lower cut nearly to the top. Biotite rock is a basic magmatic face. No sharp contact with the adjacent nonorbicular percent, indicating that the granite, it contains sparse pinkish Sandia Granite is observable. The enclosing segregation. Like the normal schist, and quartz. and surrounding granite is slightly more biotitic than small inclusions of gneiss, 27

Maximum diameter of the rounded orbicules ranges analysis of biotite and muscovite from the granite from to 2 5 inches. These orbicules are finer grained (Aldrich, Wetherill, and Davis, 1957, 656) yielded than those with prominent p. biotite intermediate shells of K-Ar and Rb-Sr ratios suggesting ages of 1,340 and the main body. Concentric banding is usually well 1,350 m.y. (million years). Since 1957 some 50 dates developed and visible because of biotite bands across determined using U, Th-Pb, Pb-Pb, K-Ar, Rb-Sr the radial oligoclase. Biotite consists of subhedral grains (whole-rock and mineral), and fission-track data suggest arranged radially and tangentially. As many as 15 a best age of crystallization of the granite of 1,500 ± biotite bands 100 may be counted on equatorial cuts of the m.y. (Douglas G. Brookins, written communication; larger orbicules. Individual bands are less than 0.04 Brookins, 1973). The Sandia Granite has been age- inch thick with average biotite grains running 0.004 to dated most often of any rock in North America; some of 0.01 inch. Magnetite is also concentrated with biotite in the recent papers including data on the possible age of some bands. Feldspar is dominant in all the orbicules. the Sandia Granite are by Wasserburg and Steiger In addition to forming pure or nearly pure bands of (1967), Aldrich and others (1957), Aldrich and others radiate oligoclase up to 0.1 inch in the concentric shells, (1958), and Tilton and Gruenenfelder (1968). the feldspar pervades the biotite bands and occurs in Naesser (1971, 4980) cites French geochemist nonradiate coarse subhedrons p. and anhedrons in the Poupeau (1969) for a Sandia Granite apatite fission- feldspathic cores. The oligoclase is greatly sericitized track date of 50 my., which is thought to indicate a but numerous unaltered crystals are common. Biotite Laramide geothermal perturbance effect during that makes up less than 10 percent of the average orbicule, orogeny. but in some it is less than 1 percent, or essentially absent. DIKES RELATED TO SANDIA GRANITE The nonconcentric cores range from I to 2 inches in Large areas of the Sandia Granite are intruded by diameter and consist of oligoclase, orthoclase, and thousands of aplite and pegmatite dikes. Map I shows quartz, minor biotite, and the usual accessories. Ortho the distribution of most of these. They range in clase and quartz tend to be more abundant in the thickness from an inch or so to as much as central part of the core. 50 ft, and A few cores contain irregular some are nearly I mile long. Most inclusions of of the mapping of the what Thompson and Giles concluded are dikes has been done hornfels. by Hayes (1951), Shomaker (1965) and Feinberg (1969). Numerous thin and short dikes Thompson and Giles recognized three orbicular either go undetected or are hardly mappable at the structures: type I, the principal kind with alternating working scale; most dikes mapped are between 500 and biotite- and plagioclase-rich shells (fig. 18C); type H, 1,500 ft in length. The dikes generally occur in irregular plagioclase with or without a continuous biotite shell single sets, although in places a lesser set crosses the near the periphery (fig. 18E); and type III, plagioclase dominant one. The dominant set trends eastward cores surrounded by thin concentric fol shells of fine lowed by lesser sets of northwestward or northeastward grained biotite (fig. 18D, 18F). Autoliths of biotite trend. Individual dikes tend to be slightly or, granite or monzoflite shown by Thompson in rare and Giles instances, sharply curved. Dikes and well-defined (1974, fig. 2c) and in fig. 18A (near the faults hammer) might rarely coincide and many dikes terminate be another type. at faults. As noted by Shomaker (1965, General paragenesis p. 20) the greatest concentra consists of the following princi tion of dikes is in pal stages: the central area of the granite body. Relatively few dikes occur in the Cibola Gneiss on the 1) Early magmatic crystallization to form autolithic southeast, but numerous dikes and sills occur in the blobs of unba11ed granitoid crystals Rincon metamorphic complex on the northwest. Hayes 2) Orbicule formation involving principally oligo (1951, p. 20) observed that dikes are numerous in the clase and biotite in repetitions of concentric bands Rincon Ridge country rock but are sparse in the border with both radiate and tangential crystal orienta of the granite batholith. tions The small intrusions related to the Sandia batholith 3) Post-orbicule formation, nonorganized, fine- to fall into four principal categories: I) composite aplite medium-grained or normal granitoid matrix pegmatite, 2) aplite, 3) pegmatite, and 4) quartz (silex crystallization (fig. I 8C) ite). Most are dikes or dikelets but in places are pod- or 4) Deuteric or hydrothermal alteration forming epi finger-like bodies. Composite aplite-pegmatite dikes dote, chlorite, and sericite are most abundant, but the proportion of aplitic or pegmatitic texture may range considerably in individual Thompson and Giles believed that the rare presence of dikes. The composition may also range considerably hornfels xenoliths in cores, along with other considera locally or even across the dikes. Microcline tions, indicated that orbicule development was metaso microperthite, quartz, and oligoclase are the predomi matic, seemingly implying late magmatic development. nant constituents with only minor biotite, muscovite, However, it is difficult to imagine that orbicules of the and very minor apatite, pyrite, tourmaline, beryl, mag kind shown in fig. l8D, F are replacements to any great netite, and ilmenite. extent, hence our conclusion that they are of early Aplite is most abundant in the thin, small dikes. It magmatic origin. is typically sugary textured, consisting of quartz and Except for late magmatic aplite, pegmatite, and orthoclase with accessory muscovite. Some aplite dikes lamprophyre dikes the Sandia Granite is the youngest bear garnet in amounts of as much as 5 to 10 percent. It Precambrian rock in the area, and this is generally also occurs in circular bodies which may be bulbous or shown by field relationships. The first radiometric fingerlike beneath the surface. Feinberg (1969, fig. 3) 28

diagnostic fossils—with the exception of a ft in diameter in Prior to 1951. no mapped several such bodies up to 500 foraminifer. Endothvra hai/e’i—had been found in pre the Bear Canyon-Pino Canyon reentrant. Pennsylvanian slrata in New MexIco north of Ladron Peak. Pegmatites occur as short dikes, pods, lenses, or small between Socorro and Belen. More than a century ago Marcou is simple for the (1856; 1858) misidentified Pennsylvanian fossils from Pecos. fingerlike masses. The composition Mississippian garnet, or the Sandia Mountains, and Tljeras Canyon as most part, with sparse development of mica, that the Madera or Magdalena lime the species. He concluded black tourmaline. Only few small masses occur in stone was “calcaire du carbonifere inferieure” or limestone of granite, but they are the dominant rock of the dikes in the Lower Carboniferous. Later he called it the “Mountain 1951, 20) (fig. 19). The Limestone” and stated that the Sandia rim was “composed of Rincon Ridge (Hayes, p. most truly its a swarm across the schist in Carbonferous Limestone. which here merits pegmatite dikes, forming Limestone. for it is the only limestone of ft long and 10 ft name of Mountain the western escarpment, are up to 3,000 any importance met with in the Rocky Mountain region.’ wide. Many show crude zoning consisting of borders, I Within a few years other workers assigned this limestone to the to 3 inches wide, of fine-grained feldspar and quartz Upper Carboniferous or Pennsylvanian. muscovite. The border zones grade Apparently. the first recognition of pre-Pennsylvanian with fine-grained New Mexico north of L..adron Peak was in which is coarser and locally Paleozoic strata in inward to the wall zone, 1940, when the 7.407-foot well in the Rattlesnake field was graphic in texture with small muscovite books up to completed; Needham and Bates (1942) assigned 215 feet of about 1 inch in diameter. In many dikes the central strata in this well to the Mississippian. This same year cores, but these are absent in most dikes Thompson (1942) found 106 feet of pre-Pennsylvanian rocks at parts are quartz near Placitas. Above and composition occupy all the north end of the Sandia Mountains where wall-zone textures he measured 16 feet of conglomerate and (Hayes, 1951, the Precambrian but the fine-grained borders of the dike p. sandstone overlain by 90 feet of unfossiliferous limestone and 23). Pegmatites, like the other dikes, range considerably hazarded the opinion that these rocks might be “of lower in mineral proportions. The approximate mean of 40 Paleozoic age” (Thompson, 1942, p. 19). During the period range from 20 to 60 percent and 1942-1947 it was suggested by several members of the U.S. percent for quartz may scattered remnants of pre from 25 to 75 percent. Geological Survey that such the 50 percent mean for feldspar Pennsylvanian strata might be Mississippian or older (Read Quartz dikes (silexite) occur locally, are generally and Henbest. 1942: Henbest, Read, and others. 1944; Read short and pod-shaped. In places dikes contain black and others 1944: Henbest, 1946a, l946b; Kelley and Wood, are identical in many respects to 1946: Wood and Northrop, 1946; Northrop and others, 1946; tourmaline. The dikes 1-lenbest or aplite-pegmatite Read and Wood, 1947). On the basis of Endorhyra, the quartz cores of the pegmatite this unit in the Sangre de Cristo and crosscuts dikes l946a, 1946b) correlated dikes. Quartz forms late in the dikes and Sandia Mountains with the Leadville of Colorado. in other places. Quartz dikes are not to be confused with It remained for A. K. Armstrong. an undergraduate student which may be banded or crusted and at U.N.M., to discover the first diagnostic megafossils in the quartz veins en barite, calcite, or base metals. pre-Pennsylvanian rocks. Early in 1951 Armstrong was associated with fluorite, under the direction of J. Paul in sedimentary rocks as the gaged in a field problem Silexite dikes never occur Fitzsimmons. He was examining Precambrian rocks at the quartz veins commonly do. south end of the Nacimiento Mountains west ofJemez Pueblo, when he found fossils in small patches of limestone faulted down into the Precambrian basement. The first two slabs of MISSISSIPPIAN this limestone Armstrong submitted to me early in 1951 contained Conularia sp. and Eu,netria sp. Recognizing the that Armstrong ARR0Y0 PEAsco FORMATION latter as a Mississippian form, I suggested make further search for fossils. Fitzsimmotis concurred and Recognition of Mississippian rocks in northern New the emphasis of the problem shifted from Precambrian to Mexico—Mississippian strata are the oldest known Mississippian, Further collections were made by Armstrong age in the Sandia Mountains and some were made by Fitzsimmons and myself. On May 21, Paleozoic rocks of definite memorandum on all the thicknesses of Cambrian 1951. I submitted to Armstrong a area. By contrast, considerable material, tentatively identifying a variety of brachiopods and to Mississippian strata occur in southern New Mexico. representatives of five other classes of invertebrates, I wrote as A detailed summary of investigations on the Missis follows: sippian rocks of northern New Mexico was given by “The age of these fossils is Mississippian. I had antici New Northrop (l96la, 105-106): pated that any Mississippian strata of northern p. Mexico would prove to be older Mississippian, that is, Kinderhook or Osage, because these strata extend farther north in southern New Mexico than do younger Mississip pian strata, such as Meramec and Chester. Again, in southern Colorado the Leadville or Madison limestone is chiefly Kinderhook or Osage in age. “However, the Eumetria in your collections seems close to Eumetria verneujijana, which is found in the Middle Mississippian Meramec of the Mississippi Valley region (Salem limestone and St. Louis limestone) and ranges up into the Upper Mississippian Chester series.” I suggested to Fitzsimmons that, because these were the first pre-Pennsylvanian megafossils ever found in northern New Mexico in a distance of 200 miles between Ladron Peak, New Mexico, and Piedra River Canyon. Colorado the fossils should be submitted to Mackenzie Gordon, Jr., a Mississippian specialist of the U.S. Geological Survey. It was decided to name the formation the Arroyo Penasco formation. Gordon’s report on the fossils, listing 39 species, a Meramec, possibly St. IN RINC0N RIDGE. COUNTRY corroborated my determination of FIGURE 19—PEGMATITE DIKE SWARM and Gordon SCARP AT Louis age. A paper by Fitzsimmons. Armstrong. ROCK IS MICACEOUS QUARTZITE. NOTE H0L0cENE FAULT (1956) was submitted in June 1955 and published in August BASE OF RIDGE. 29

1956. Meanwhile Armstrong (1955) had published iridepen photomicrographs of various dently a repori ihat included rocks (pls. 2. 5, 7); calcis observations on Mississippian pheres. ostracods, rocks in the Sangre de Cristo. Sandia. Manzano, and Ladron and foraminifers are illustrated. Mountains. Chiefly on the basis of microfossils. he concluded In 1972 and 1973 Armstrong re-examined and made that the upper part of the “Arrovo Penasco” of the Sangre de additional collections from Mississippian outcrops in Cristos is Meramec in age but that the lower unfossiliferous northern New Mexico. Armstrong strata might be equivalent and Mamet (1974, p. to the Leadville of Colorado or the 148-149) note that Caloso of Ladron Peak. In this connection i may be noted that Baltz and Read (1960) collected Early Mississippian fossils at “The knowledge of Mississippian microfossils has greatly several localities in the Sangre de Cristos: they named two new increased, and more refined zonation is now possible since the formations, the Tererro of Early Mississippian (Kinderhook publication of Armstrong’s 1967 paper. Taxonomic changes and Osage) age. and the Espiritu Santo of possible Devonian have been rapid. and more than 60 new generic taxa have been age. In view of the fact that the Meramec fossils of the Arroyo proposed in S years.” Penasco at the type locality of that formation occur in the They raise the upper part. it is possible that the unfossiliferous lower part of Arroyo Peñasco Formation to group the Arroyo Penasco may be Lower Mississippian and equiv rank and include in it two formations, the Osagean alent to the Tererro formation. Espiritu Santo and the Meramecian Tererro of Baltz In the Placitas area at the north end of the Sandia and Read(1960). Mountains, Toomey (1953) measured ten sections of pre At the north end of the Sandia Pennsylvanian strata, ranging from 20 to 81 feet in thickness. Mountains near The only determinable fossils he found were poorly preserved Placitas, 33 miles southeast of the type locality of the Euomphalus sp., two high-spired gastropods. and a cephalo Arroyo Peñasco Formation, the Arroyo Peñasco Group pod. Later, in the Placitas area. Armstrong (1955) measured is represented by 73 ft of the Espiritu Santo Formation one section of 102 feet of pre-Pennsylvanian rock and cited (Osagean). At the poorly preserved Straparolus? base, Armstrong and Mamet (1974, [Euompha!us?j sp.. Stegocoelia? 155) recognized p. sp.. Goniatires sp.. and Plectogyra sp. Subsequently Armstrong 6.6 ft of the Del Padre Sandstone (1958) cited Endothyra prodigiosa. Member, followed upward by 33 ft of stromatolitic At the south end of the Sandia Mountains in Tijeras dedolomites, followed by lime mudstones and dolomites Canyon. Szabo (1953) measured ten sections of the pre and minor amounts of wackestones. They report well- Pennsylvanian sequence, ranging from 8 to 48 feet in thickness. preserved However, in his thickest section. microfossils in the nodular dark-gray cherts as much as 32 feet of red in the shale may be Pennsylvanian in age. If the questionable red lower part of the section, as well as microfossils in shale that appears in most of his sections be assigned to the the lime mudstones in the upper parts of the section. Pennsylvanian, the remaining pre-Pennsylvanian strata range They list calcareous algae and foraminifers from from 8 to 27 feet in thickness. Armstrong (1955) measured only three levels: 1) near the one section in Tijeras Canyon. base of the section (12.2 to 15.2 16 feet thick. Some of my ft), 2) middle part of the colleagues hold the opinion that, in the absence of diagnostic section (42.2 ft), and 3) upper fossil evidence, the so-called pre-Pennsylvanian rocks in Tijeras part of the section (69.3 ft). A combined list follows, Canyon should be assigned to the Sandia formation. Certainly. Calcareous Algae along much of the Sandia crest, the pie-Pennsylvanian seems to missing. be On the other hand. Toomey (1953, p. 12) Calcisphaera laevis observed that the basal unit of the Sandia formation in the Foraminifera vicinity of the Sandia crest “contains numerous, large, re worked fragments of pre-Pennsylvanian limestone.” Earlandia c/a vatula At Bosque Peak in the southern Manzano Mountains, east Endospiroplectammina? sp. of Los Lunas and a few miles southwest of Mosca Peak, Endothyra sp. Armstrong (1958) found 22 feet of limestone that may be Inflatoendothyra Mississippian. He observed also a few isolated remnants of sp. limestone, 20-30 feet thick, at several places in the Manzanita Latiendothyra of the group L. parakosvensis * and Manzano Mountains between Tijeras Canyon and osque L. sp. Peak. Palaeocancellus sp. It now seems likely that all of the pre-Pennsylvanian rocks Parathurammina of the of the Sandia-Manzanita-Manzano area should be assigned to group P. cush,nani the Tererro (or Tererro and Espiritu Santo formations). As P. of the group P. suleimanovi Baltz and Read (1960, P. 1768) have well said, “Further P. sp. paleontologic studies and studies of the physical stratigraphy Radiosphaerina must precede correlation, firm assignments of age. and adjust. Septaglomospiranella sp. ments in the terminology of the Espiritu Santo. Tererro, and Arroyo Penasco formations.” Septatournayella sp. Spinoendothyra sp. Tournayella sp. After the above summary was written, Catacosinos Vicinesphaera sp. (1962) examined the Precambrian-Pennsylvanian con tact at 6 places along the Sandia Rim but did not find *lncludes any Mississippian Endorhyra skipae of Armstrong (1967). In 1967 Arm rocks intervening. Armstrong pub strong had also reported Septabrunsiina parakrainica and fragments lished several papers on the Mississippian of south of echinoderms and ostracods. western and west-central New Mexico during the period 1958-1965. Armstrong and Mamet note further that the age is Early Mississippian Osagean, upper Keokuk, and not Late Lithology and Fossils—Armstrong and Holcomb Mississippian Meramecian. The earlier report by Arm (1967) described and illustrated the Placitas section. strong (1967, fig. 40) of Endothyra prodigiosa, E. Armstrong’s (1967) paper, entitled “Biostratigraphy and irregularis, and E. macra must be discarded. carbonate facies of the Mississippian Arroyo Peflasco There are two principal occurrences of these pre Formation, north-central New Mexico,” includes anno Pennsylvanian strata in the northern Sandia Mountains. tated sections of the Placitas section (fig. 40, p. 49) and One section, studied by Armstrong, is in duplicated of the Tijeras Canyon section (fig. 41, p. 50), and faulted strips 1 mile east of Placitas at the base of 30

for exposures at the Montezuma Mountain (fig. 20). The other occurrence is and 1-lerrick and Bendrat (1900) (actually in the about 3 miles west-southwest of Placitas in sec. 12, T. 12 southern end of the Sandia Mountains Madera limestone N.. R. 4 E.; the section there consists of 20 ft of cherty Manzanita Mountains) and the for exposures near gray limestone and 10 ft of white dense marble named by Keyes (1903), presumably Madera on the eastern overlying Precambrian greenstone. The Mississippian the old village or canyon of La point here is that a beds are overlain directly by a thinned section of side of the mountains. An intriguing Canyon in the Madera limestone with the elastic Sandia Formation Madera Canyon is tributary to Coyote been the source missing. The contact with the overlying Madera may be Manzanita Mountains; could this have a low-angle fault which has cut the Sandia or the area of Keyes’ name? of the Sandia Mountains may have stood as a high during Sandia time. In the first modern mapping his associates (Read and At the southern end of the Sandia Mountains Szabo and adjoining areas Read and Madera into the Lower (1953) measured ten sections of what he considered to others, 1944) subdivided the and the upper Arkosic lime be pre-Pennsylvanian beds, ranging from 8 to 48 ft in gray limestone member was based partly upon thickness. About half of the material may belong to the stone member. This mapping between the lower and overlying Sandia Formation. Armstrong (1955) did not distinct lithologic differences and partly upon physio find fossils in the single 16-ft section he measured in upper halves of the Madera of stratigraphic differ Tijeras Canyon. graphic breaks which arose out Northrop and others Read and others (1944) had mapped these Mississip ences between the two members. in the Sangre de Cristo pian beds as a Lower limestone member of the Sandia (1946) used these same members Wood and Northrop Formation, suspecting that they might be Mississippian Mountains near Las Vegas, and Mountains. or in part older. The same procedure was followed in (1946) used them in the Jemez-Nacimiento change the southern Sangre de Cristo Mountains in the Las The fact that lithology and stratigraphy the two is in Vegas area (Northrop and others, 1946) and in the regionally, and that the contact between prevented the two Jemez-Nacimiento Mountains (Wood and Northrop, places transitional or indefinite, has in New Mexico. 1946). members from being extended widely have been Our geologic map shows Mississippian rocks only in Other informal subdivisions of the Madera (Herrick, the Placitas area at the north end of the mountains; made locally, such as the Coyote sandstone Herrick and instead of using Espiritu Santo Formation of the Arroyo 1900a; Herrick and Bendrat, 1900; 40-ft bed Peñasco group we prefer the name Arroyo Peñasco Johnson, 1900, pl. 22 of U.N.M. Bull. 23), a at Formation. The few feet of strata between the Precam within the Lower gray limestone member. Students geology brian and Pennsylvanian Sandia Formation in Tijeras the University of New Mexico mapping in field the top of the Canyon at the south end of the mountains are not courses commonly mapped a thin unit at and marine shown on the map. Madera that consists of mixed continental deposits. In areas to the south and west this unit has been given several formal names, such as Red Tanks PENNSYLVANIAN Member (Kelley and Wood, 1946); Bursum Member (Wilpolt and others, 1946); and Agua Torres Member Pennsylvanian rocks of central New Mexico and The (Stark and Dapples, 1946, 1154). Mountains consist of the Magdalena Group, p. the Sandia Based on mapping and studies in the Manzano proposed by Gordon in 1907 806-8 12) for all a term (P. Mountains since 1962, Myers (1973) elevated the in the Magdalena Mountains between the the beds Madera to group status and defined it to include all the Kelly Limestone and the Permian Abo Mississippian beds between the Sandia Formation below and the Abo The group generally has been divided into Formation. Formation above, which is essentially what Kelley and Sandia Formation, named by Herrick (l900a) the basal Wood (1946) did in the Lucero uplift west of the Rio Grande depression. Myers (Myers, 1969; Myers and McKay, 1970) has been able to map several divisions of the Madera rather widely through the Manzano and Manzanita Mountains in units formally named as follows: Madera Group Bursum Formation (100+ ft) Wild Cow Formation La Casa Member (280+ ft) Pine Shadow Member (240+ ft) Solse Mete Member (210+ ft) Los Moyos Limestone (600+ ft) The Wild Cow Formation is probably roughly equivalent to the informal Arkosic limestone (upper) and the Los Moyos Limestone to the informal Lower FIGURE 20—ARR0Y0 PEIAsco FORMATION AT MONTEZUMA gray limestone of Read and others (1944). In this Motn’uAIN. THICK MADA LIMESTONE LEDGES OVERLIE SANDIA memoir the Madera unit will be referred to as Madera ABOVE LEDGED SANDSTONE, SHALE, AND THIN LIMESTONE IN SLOPE Formation rather than Madera Group or Madera ARR0Y0 PESa.scO (AP). A WHITE QUARTZITE CONGLOMERATE, 3 FT THICK, MARKS BASE ON PRECAMBRIAN SCHIST (pC). Limestone. 31

SANDIA FoRMATIoN Definition—Except in few small areas where thin Mississippian strata are present the Sandia nearly everywhere overlies the Precambrian and is overlain gradationally by the Madera Formation. The Precam brian surface upon which the Sandia deposits were spread was a peneplain and relief appears to have been no more than a few tens of feet. Relief on the surface was principally in the form of monadnocks or low ridges of quartzite. Along Cerro Pelon ridge in the northwest corner of sec. 5, T. 9 N., R. 5 E. a quartzite hill about 50 ft high on the Precambrian surface rises into onlapping Sandia beds nearly to the base of the Madera. A similar small buried ridge occurs high along Tijeras Canyon north of Seven Springs in sec. 16, T. 10 N., R. 5 E. Elsewhere the surface has little or no relief beyond the few feet of buried residual boulders or small pinnacles (figs. 21, 22). For detail of this nature few exposures surpass those in the old roadcut above the present NM-44 in Tejano Canyon about haIfa mile southeast of Tree Springs. FIGURE 23—MARC0U’S CAMP A. OCToBER 8. 1853. AT TIJERA5. CAMPSITE WAS AT TRIANGLE NUMBERED “16.” ENLARGEMENT The top of the Sandia Formation is transitional and OF is PART OF OUR FIGURE 8; SFE ALSO PAGES 18-19 OF THIS MEMOIR FOR typically chosen at the base of the first massive lime MARCOU’s DESCRIPTION OF THE ROCKS AND FOSSILS. stone ledge of the Madera. Because of the difference in the erosional resistance of the thin-bedded sandy or shaly Sandia beds as compared to the Madera limestone ledges, the top is commonly mapped at the top of a slope or the base of the cliffy outcrops. Limestone is also common in the Sandia Formation in thin- to medium- bedded ledges. In many places these ledges increase in number and thickness near the top of the Sandia,just as thin shale and sandstone beds occur near the base of the Madera. Because of these variations at the upper boundary and because the contact zone is commonly not well exposed, the boundary is not chosen or mapped uniformly from place to place. The variability of lithology and surface expression of this boundary is as much (or more) responsible for differences in apparent thicknesses of the Sandia as irregularities on the ,e - Precambrian at the base. a.... The Log Springs Formation—This unit was named by Armstrong (1955, 5, 9) for Log Springs FIGURE 2 I—BASAL SANDIA FORMATION p. in Peñasco RESTING ON SPHEROIDAL Canyon, near the south end of the BOULDER IN SANDIA GRANITE. EXPOSURE IS ir. oi.o NM-I4 ROAD Nacimiento Moun tains. CUT 0.5 MILE SOUTHEAST OF TREE SPRINGS. NOTE DEFORMATION OF There the Log Springs Formation consists of 10 to COARSE-GRAINED CALCAREOUS SANDSTONE AROUND ANCIENT 75 ft of ferruginous shales, sandsones, and conglom SPHEROIDAL RESIDUAL BOULDER. erates.

The immediately underlying part of the Arroyo Peflasco Formation is brecciated and Contains numerous solution cavities that are filled with the basal ferruginous shales from the overlying Log Springs Formation. The basal shale of the Log Springs Formation is highly ferruginous. with numerous oolites of hematite. and is followed by a medium-bedded series of deep-red shales. sandstones, and conglomerates. The sand stones tend to form small prominent ledges. It is interesting to note that the lower beds of this formation contain sporadic rounded pebbles of Mississippian chert; but the higher con glomerate beds contain angular pebbles of Mississippian chert and limestone as well as of Precambrian gneiss and green schist. No fossils have been found in the Log Springs Formation.

At Placitas, according to Armstrong and Mamet (1974, p. 155), The Espiritu Santo Formation is uncomformably overlain by 2 to 3 m of red shale and siltstone of the Log Springs Formation, which are unconformably overlain by the coarse grained cross-bedded sandstones of the Sandia Formation. 32

Canyon in sec. 35, T. ION., R. In Tijeras Canyon. Armstrong (1955. p. 29 and fig. small inlier east of Cedro 19) found 16 ft of Mississippian strata, “overlain by 23 5 E. end of the Sandias feet of ferruginous red shales tentatively assigned to the Thickness—At the northern 6 sections of Sandia Log Springs formation.” We include this Log Springs in Toomey (1953, p. 53-64) measured above the Arroyo our basal Sandia Formation. ranging from 49 to 85 ft in thickness 28-29) measured Originally Armstrong (1955) believed that the Log Peñasco Formation. Szabo (1953, p. beds Springs Formation was of Early Pennsylvanian age. 116 ft above 38 ft of presumed pre-Pennsylvanian the Madera Formation. Later, he (1967, 32) concluded that it might be Late or a total of 154 ft below p. Sandia sections at Mississippian and/or Early Pennsylvanian. At present, Phillips (1964, p. 63-71) measured 6 ranging fror, Armstrong and Mamet (1974, figs. 1,2; p. 150) consider inliers on the east side of the mountains Reynolds (1954, 76-77) it to be Late Mississippian (Chestenan) rather than 113 to 138 ft in thickness. p. his Las Huertas Early Pennsylvanian. measured 159 ft of Sandia above Montezuma Distribue’ion—The Sandia Formation crops out limestone (Arroyo Peñasco Formation) at 172 ft at the mostly on the high western face of the mountains (figs. Mountain. Harrison (1949, p. 21) measured Johnson (1948, 1) 24, 25) and extends in a nearly continuous narrow band same location. At Palomas Peak, p1. (1962, 27-36) from Coyote Canyon at the southern edge of the measured 200 ft of Sandia. Catacosinos p. of the Sandia along geologic map (map 1) to the northern end of the Sandia measured 6 poorly exposed sections between North Sandia and Mountains around Placitas. It also occurs in several the high western escarpment thicknesses range from 175 inliers on the east slope of the mountains from near the South Sandia Peaks and his are in excess of all other head of Las Huertas Canyon south to Sulphur Canyon. to 300 ft. These thicknesses could directly observe the Some of the best exposures are found in these areas. measured sections; as he section, because of the The Sandia also crops out north and south of Monte contacts in only the thinnest cover, his upper con Largo in the eastern part of the area, and there is one extensive talus and heavy plant tacts were probably chosen too high. The thicknesses measured by Harrison, Reynolds, and Phillips agree reasonably well, averaging about 150 ft, but those of Toomey do not agree, averaging only 60 ft. Lirhology—The Sandia is dominantly a siliceous clastic unit consisting of sandstone, shale, limestone, conglomerate, and siltstone (abundances in general in the order given). Considerable variation occurs laterally as shown comparatively in graphic sections of figure 26. In some sections sandstone is dominant; in others shale, limestone, and siltstone are more abundant with thin coal or coaly shale seams present. Conglomerate occurs mostly at the base but is present in higher parts. Sandstone occurs in unusual thicknesses around the head of Las Huertas Canyon, in Osha Canyon, and especially in Capulin Canyon in sec. 34, T. 12 N., R. 5 Photo by Donald A Myers E., where thicknesses of 50 to 60 ft of thick-bedded, FIGURE 24—AIRvIEw OF NORTHERN PART OF SANDIA RIDGE. grayish sandstone are well exposed. In SLOPE ABOVE coarse-grained, SANDIA FORMATION UNDERLIES BRUSH-COVERED more black shale is present in CLIFFS. CREST IS HELD UP BY RESISTANT contrast, considerably PRECIPITOUS GRANITE sections. MADERA LIMESTONE LEDGES. PALOMAS PEAK, UPPER LEFt MARGIN. Barro Canyon and in the Tijeras Canyon TIJERAS SYNCLINE IN VALLEY NEAR TOP IS SHOWN BY ARCUATE In general the Sandia sandstone varies from thin to OUTCROPS OF TREE-COVERED DAKOTA SANDSTONE RIDGE AND thick bedded, white, yellowish, brownish, or light gray, GRASS-COVERED MANCOS SHALE VALLEY. medium to coarse grained, locally conglomeratic, and rather commonly contains shaly or silty partings. Cross and lenticular bedding is not uncommon. Carbonized and silicified wood or other plant remains occur locally. The sandstone is commonly micaceous and locally arkosic. Rock fragments are angular to subrounded and consist mostly of quartzite with lesser quantities of schist, gneiss, greenstone, or granite depending upon the underlying Precambrian rocks. Locally limestone frag ments are present. Conglomerate in the Sandia is mostly pebbly and only locally bouldery or granulitic; conglomerate beds, present primarily in the basal section, are not thick, and are usually lenticular. Limestone is widely distributed throughout the San dia section, even at the base, although most of the limestone occurs in the upper part. Beds range from FIGURE 25—PENNsYLvANIAN BEDS NEAR SANDIA CREST. SANDZA thin to thick with the thicker ledges being hackly, dense, BY FORMATION UNDERLIES BRUSH-COVERED SLOPE AND IS OVERLAIN and gray. Chert occurs in many beds but is not as VIEW NORTH THICK-LEDGED LIMESTONE OF MADERA FORMATION. common as in the Madera Formation. Textures range FROM SANDIA PEAK TRAMWAY. 33

Mount - 200 ft Wash000 n g ton 000 , - 50

00 —

Modera - I 00 Canyon

Tejano — —- Canyon

- 50 Palomas .• Tijeros Peak (No.2)

Ba rio ECr — Canyon . - — -o — - North Montez uma

limestone sandstone

Toomey Toomey Philhps PhillipsI Phillips Phillips Szobo Myers 970 FIGURE 26—GRAPHIc SECTIONS OF THE SANDIA FORMATION.

from micritic to arenitic. Many limestones are sandy crest and forming the eastern dip slope of the Sandia and gradations between sandstone and limestone ap Mountains. Its outcrop area (exclusive of Cenozoic pear to occur laterally as well as vertically. Some deposits) is more than twice that of either the limestone beds are conglomeratic with either remaining or both pre-Cenozoic stratified rocks or the Precambrian quartz and feldspar fragments. The thin expo and medium- sures. The Sandia uplift is surfaced thick beds are commonly dark yellowish by Precambrian or brown or black Pennsylvanian rocks (in approximately and they may be nodular and locally equal western shaly. Limestone and eastern halves). The largest also occurs as lenses or concretions expanse of Madera is in in the shale units. the flat-lying beds of the Shale in the Sandia is black, Manzanita Mountains area olive drab, and gray. It is south of Tijeras Canyon commonly silty or sandy and US-66, where the unit is and commonly calcareous with quite thick and relatively local thin coal seams in resistant. The Lower gray the shale or siltstone units. limestone member forms Shale units are probably the crest of the Sandias and more prevalent in the middle some of the upper eastern part of the Sandia Formation. dip slope of the mountains. It Locally reddish residual also occurs along the western soil-type shale or claystone occurs faces of the northern end in the Sandia and has of the Manzanita Mountains been compared to the red and in the deeper canyons Molas sediments of Colorado of the eastern side or put in a pre-Pennsylvanian of the mountains. Elsewhere the category as Szabo (1953, Madera shown 22) did in on the geologic map (map 1) is surfaced p. Tijeras Canyon. by the Age—Fossils upper Arkosic limestone member. and age of the Sandia Formation are Lirhology—The discussed Madera Formation is dominantly a at the end of the section on the Pennsylva gray nian. marine limestone sequence, but with variable interbeds of black, gray, reddish-brown, or purplish MADERA FORMATION shale, sandstone, and conglomerate. The formation consists of a lower part comprising Definition—The base thick ledges of gray of the Madera Formation is or black cherty limestone transitional and hence and an upper part of lime completely conformable with the stone in which arkosic underlying Sandia Formation. sandstone, conglomerate, and In most places the top of reddish-brown shale or the Madera is also transitional mudstone beds are common. or gradational with the The lower part has overlying continental been termed and mapped by Read Permian Abo Formation. The first and associates as the red-bed Abo-type Lower gray limestone member and strata appear near the top of the the upper part, the Madera, below Arkosic limestone member (Read the uppermost marine limestone that and others, 1944). customarily is used to map the top of the Madera. The name of the upper member was chosen not Distribution—The Madera is the most widespread so much because the limestone beds are outcropping formation in the Sandia area, capping arkosic the (micaceous and feldspathic) but because abundant 34 feldspathic and micaceous sandstones and mixed con glomerates are interbedded with the typical Madera limestone. The Lower gray limestone member constitutes 40 to 45 percent of the thickness of the Madera and is dominated by limestone ledges from 10 to 60 ft thick. In the lower and upper parts of the member black shale, micaceous siltstone, or shaly limestone partings up to 10 ft thick are present. A few thin light-gray to yellowish sandstone beds and very rare conglomerate lenses are present. Many thick limestone ledges are hackly weathering arenite. Many others are cryptocrystalline or are finely crystalline. White, ,..:n lithographic micrite; others .—. --,.—,—. — _5’%_. is abundant in the -— gray, black, and brown chert ,-t ,-,.. ., — or irregular REDDIsH-BRowN limestone as nodules, lenses, thin layers, A—ROADCUT along US-66 WEST OF TUERAS. SANDSTONE. stringers and masses. In parts of the section chert may SHALE BEDS ALTERNATE WITH GRAYISH ARKOSIC constitute 50 percent or more of thick ledges composed GRAY LIMESTONE ON RIGHT. of alternating thin layers of chert and limestone. Occasionally chert forms beds up to 2 or 3 ft thick; chert is commonly found along cross fractures or joints. A section measured across the northern end of Montezuma Ridge, modified from Harrison (1949, p. 31-33), is given in Appendix I. The Arkosic limestone member makes up 55 to 60 percent of the Madera section. The quantity of clastics in the member differs greatly and is in general about twice that in the Lower gray member. The lower member clastics consist of more black shale and silt- stone and cleaner sandstone, whereas the upper mem ber clastics are muddier, arkosic, and more conglomer atic with reddish-brown, greenish, and yellowish colors prevailing over grays or blacks (fig. 27). Upper member than those of ZUZAX. GRAY THICK limestone beds are somewhat less cherty B—RoADcuT ALONG tJS-66 EAST OF MUDSTONE WITH the lower member, and they are more commonly LIMESTONE ON LEFT OVERLIES DEEP MAROON argillaceous, arenaceous, or arkosic. However, there are THIN-BEDDED LIMESTONE AND SHALE ON RIGHT. OF MADEA many nearly pure limestone units, and the limestone FIGURE 27—ARK0sIc LIMESTONE MEMBER (UPPER) quarried by the Ideal Cement Company at Tijeras is in FORMATION. the upper part of the member. clastic and carbonate intervals in Limestone in the Arkosic limestone member is thin to several alternating member over a distance of some 10 thick bedded, light gray to black, and fine to very fine part of the upper effort to place the highly fossiliferous grained. Limestone occurs in intervals up to 30 ft thick miles during an beds at the Kinney clay pit with and these may aggregate in units up to 60 to 70 ft thick shale and limestone of the Madera Formation. His with little or no sandstone or shale, but some intervals reference to the top sections (Stukey, fig. 1) split and alternate or intertongue with thin units of descriptions and stratigraphic the lithologic variability within shale, siltstone, or sandstone. Gray, black, and olive reveal much about drab shale units are as much as 30 to 40 ft thick and are zones of beds. thickness of the Madera generally commonly calcareous, many units containing nodular Thickness—The 1,300 to 1,400 ft. Read and others limestone concretions. Much of the shale contains ranges from about 14, 15) measured two complete admixtures or intercalations of micaceous siltstone or (1944, fig. 1, nos. Sandia area as follows: fine-grained sandstone, or is in places just arenaceous. sections within the Sandstone units arc up to 40 ft thick and are generally Monte Largo Tejano Canyon 855 ft buff, tan, or reddish brown, medium to coarse grained, Arkosic limestone member 780 ft 450 ft and locally conglomeratic. Conglomerate in the mem Lower gray limestone member 495 ft 1,305 ft ber is most variable, occurring in local lenses or Totals 1275 ft channels that may reach several tens of feet in thickness of the area around Cedro Peak, with fragments consisting of limestone, chert, or quartz In the southern part 36) was able to piece together a ite. Brown (1962, p. the Arkosic member and about Variability is a characteristic of the upper member thickness of 875 ft for member for a total Madera especially within individual units. However, groups of 500 ft for the Lower Harrison (1949, 33) and beds may be followed using overall lithologies, fossils, thickness of 1,375 ft. p. 16) measured sections of the Madera and geomorphic expressions. Brown (1962, p. 29-31) Reynolds (1954, p. of 1,261 and 916 ft, but followed zones of beds in the northern Manzanita at Montezuma Mountain Harrison had measured some strata Mountains around Cedro Peak in an effort to obtain a Reynolds believed fold. Read and others (1944, fig. thickness for the Madera. Stukey (1967, fig. 1) mapped twice in crossing a tight 35

I, no. 14) measured 985 ft at Montezuma Mountain, FossiLS allowing for an estimated interval of interruption in the section. Several thousands of years ago the prehistoric Two sections of the Sandia and Madera Formations inhabitants of New Mexico occasionally collected fossil were measured by R. B. Johnson (1948) for a study of shell, bone, and wood. The buttonlike segments or the lithology and insoluble residues, one at Palomas columnals of Pennsylvanian crinoid stems were used in Peak and one at Seven Springs. making bracelets and necklaces. Early Spanish ex plorers and colonists must have seen and collected fossils Palomas Seven of various ages, but we have never seen any Peak Springs mention of fossils in the several chronicles and narra Madera Upper arkosic limestone mem. 140 ft 40+ ft tives of the early expeditions beginning with Coronado Fm. Gray limestone mem. 316 ft 300 ft in 1540 and extending through the Pueblo Revolt in (456) (340+) 1680. This is rather surprising Sandia Formation 203 ft 20+ ft in view of the many references to ores of silver, copper, and lead; to 659 ft 360+ ft minerals, such as turquoise, gold, silver, copper, salt, garnet, peridot, alum, sulfur, Johnson recognized 8 “lentils” in the Gray limestone azunte, malachite, lode stone, selenite, mica, jet, etc.; member and was able to recognize them in the section and to various rocks (Northrop, 1959, 1962). at Monte de Belen, 56 mites southwest of the Seven Lieut. J. W. Abert (1848) was Springs section. In most cases, fossils were identified in the territory between only generically. September, 1846 and January, 1847. He visited both the Old and New Placers A decade later, Perkins (1959) studied the lithogenesis near Golden and submitted his collections of Pennsylvanian of the Madera Formation at Palomas and Upper Cretaceous Peak. He fossils Prof. measured two sections 660 ft apart. to J. W. Bailey. who prepared a 2-page report entitled

I 2 Notes concerning the minerals and fossils, collected by Lieu Upper tenant J. W. Abert, while Madera Formation I I I ft 149 ft engaged in the geographical exam ination of Lower Madera Formation 432 ft 481 ft New Mexico, by 3. W. Bailey, professor of chem istry, mineralogy, and geology (543) (630) at the United States Military Sandia Formation Academy. 32+ ft 40+ ft 575+ ft 670+ ft which was appended to Abert’s 130-page report, pub lished in 1848 as a Congressional Document. The Abert-Bailey report is accompanied by 24 unnumbered Johnson’s thickness of his Upper arkosic limestone lithographed plates; the 24th plate illustrates “fossils member (140 ft) agrees with Perkins’ thickness of his from the lead mine at Tuerto [Golden],” including two Upper Madera (149 ft), but note the discrepancy views of a brachiopod, labeled “Terebratula” (now between Johnson’s thickness of his Gray limestone Composfla), and one of a shark’s tooth. These are the member (316 ft) and Perkins’ thickness of his Lower earliest known illustrations of any New Mexico fossils. Madera (432 ft in one section and 481 ft in the other). The next description and illustration of Major rock types of the Madera fossils from Formation, accord New Mexico was by Lieut. J. H. Simpson ing to Perkins (1959), include (1850), of calcarenite, calcirudite, Upper Cretaceous petrified wood between microcoquina. recrystallized the Rio calcisiltite, sandstone, Puerco and Rio Chaco, with the remark: coquina, and “Do not these shale. Fossils were identified only by petrifactions show that this phylum. country was once better timbered than it now is?” His plates bear the notation: Perkins (1959, fig. 5) noted rhythmic deposition “Printed in colours at P. S. Duval’s Steam evidenced by alternating lith. Press clastic and bioclastic limestone Establ. Phila.” and constitute the second units; he recognized illustration of 6 clastic and 6 bioclastic units in New Mexico fossils and the first in color. the Lower Madera. He also suggested that a high The next important description and illustration of percentage of silica occurring as chert, chalcedony, opal, Pennsylvanian fossils was by James Hall (1856). As and quartz probably had a syngenetic origin. noted previously in Marcou’s 1853 Survey, some of the Good complete sections of the Madera are difficult to fossils collected by Marcou at Pecos village were find in the Sandia Mountains area owing to faults, returned to Washington and given to Blake, who in turn spreading of outcrops across dip slopes, or cover by soil submitted them to James Hall for identification. (How and vegetation. The Montezuma section is difficult ever, it is obvious that Marcou retained some of the because of dip-slope extension of beds and faulting at Pecos specimens, as well as all of the specimens from the top. The Tejano Canyon section is well exposed in the Sandia Mountains and from Tijeras.) Hall (1856) nearly continuous roadcuts along NM-44 but is compli described and illustrated I new species and 6 referred cated by longitudinal faults which may both lengthen species: Productus rogersi Norwood and Pratten, P. and shorten the section. The Monte Largo section is the semireticulaws Martin, Spirfer cameratus Morton least disturbed but is much covered by trees and is (which, according to Hall, includes S. triplicatus somewhat spread out down slopes. Hall), The Manzanita area S. Kentuckensis Shumard, S. lineatus is much covered and complicated Martin, Terebra by a number of faults tula millepunc (ala, n. as well as considerable sp. (= Beecheria millepunctata), spread between the base and and T. subtilita Hall. top. It is interesting that Hall correctly dated these fossils from Pecos as coming from “the coal 36

or LIsT OF MARC0U’s(1858) FOSSILS FROM THE MOUNTAIN LIMEST0NEOR or upper carboniferous limestone” MExico. NOW measures, Lowut (‘ARBONIFEROi.s (MISSISSIPPIAN) OF NEW two years later, Marcou CURRENT Pennsylvanian. In his report, KNOWN TO BE OF PENNSYLVANIAN AGE, WITH SUGGESTED Sandia ARE TO MARCOU (1858) still dated all the fossils from Pecos, the STATUS (PAGE. PLATE. AND FIGURE REFERENCES Mountains, and Tijeras as Mountain Limestone or (1858): FOR ILLUSTRATIONS, SEE OUR FIGS, 28 AND 29; T=TVPE(s) ). Lower Carboniferous or Mississippian. Hall’s forms, Producrus rogersi, deserves 0 One of , special comment. This seems to be what Marcou (1858) identified and figured as Productus scabriculus Mart. According to Dunbar and Condra (1932, p. 269), P. Sow. 53) = status uncertain X x rogersi of Norwood and Pratten “is an ordinary Amplexus coralloides? (p. Juresania nebrascensis (Owen).” However, BeIIt’roplzon sp. (p. 44) (in last chamber of Orthoceras specimen of x Sutherland and Harlow (1973) did not find any Jure Nora.Mexicana) Marcou’s sania at Pecos. Comparing Hall’s (1856) and Mi’alina .4pachesi, n. sp. (p. 44-45, p1. 7, figs. 6, 6a) = T (1858) figures with those of Sutherland and 1-larlow Septims’alina apachesj (Marcou) that Produclus rogersi and P. x (1973), it seems likely Opt!? is crenistria Phill. (p. 49) = Derbyia sp. scabriculus are identical with Buxtonia n. sp. B of Orthis Pecosli, n. sp. (p. 48-49, p1. 6, figs. 14, 14a-b) and 1-larlow, described by them from Pecos T Sutherland Cieiothyridina pecosii (Marcou) and recognized by them at Tijeras. number of Orthoceras Nova-Mexicana, n. sp. (p. 44, p1. 7, fig. 1) Marcou (1858) described and illustrated a T = generic assignment uncertain Pennsylvanian fossils from the Sandia Mountains area Pecos, not far to the northeast. He thought Productus Core d’Orb. (p. 45, p1. 6, figs. 4, 4a, from and from or L. prat of Lower Carboniferous or Mississippian Pecos) Linoproductus platyumbonus that they were tenlanus xxx age and called the Madera Formation the Mountain book, published in Zurich, is Productus Fleiningii Sow. (p. 47, p1. 6, fig. 7, from Limestone. Because his Sutherland available in libraries, we Tijeras) probably = Sandia santafeensis quite rare and not generally and Harlow xxx present his account of these fossils in some detail. Mart. 48, p1. 6, fig. 2, from Weller’s (1898) bibliographic index of Carboniferous Productus punctatus (p. x Tijeras) probably = Echinaria sp. x invertebrates was useful in checking certain of Marcou’s Shrock’s (1944) Productus pustulosus Phil. (p. 48, p1. 6, fig. 1) prob (1858) species. In addition, Shimer and x = sp. Index fossils of North America and various volumes of ably Echinaria the Treatise on invertebrate paleontology, R. C. Moore, Productus pyxidifisrmis de Kon. (p. 48, p1. 6, figs. 3, possibly ..4ntiquatonia sp. x ed. (not included in References) were consulted in 3a) = status uncertain; checking the status of many generic names. Productus scabriculus Mart. (p. 47-48, p1. 5, figs. 6, 6a, and new; 1 was identified only from Pecos) = Buxtonia n. sp. B of Sutherland Of the 22 species, 5 were xx generically, and 16 were referred to previously named 1-larlow forms. Of the 16 referred species, Marcou identified 13 Productus serni-reticulatus Mart. (p. 46, p1. 5, figs. 4, with English and European species with which he was 4a, from Pecos; not p1. 6, fig. 6, from Arizona) = sp. xxx more familiar, and only 3 with American species. In the .4ntiquatonia introduction to his chapter 3, Paleontology, Marcou Spirifer lineatus Mart. (p. 50, p1. 7, figs. 5, 5a-b, from Phricodothyris perplexa (1858, 32) states that “the greater part of these fossils Pecos; Sc, from Tijeras) p. (McChesney) x x have been submitted to Messieurs Agassiz, de Verneuil, de Koninck, d’Archiac, Jules Haime, Pictet and De Spirifer Rocky-Montani, n. sp. (p. 50, p1. 7, figs. 4, Anthracospirifer rocky who were kind enough to aid me in their 4a-e) includes two species: shayes, montanus (Marcou) figs. 4c-e; and .4. curvilateralis T determination.” chavezae Sutherland and Harlow = figs. 4, 4a-b cited 15 species form Tijeras, including Thus Marcou figs. 2, 2a, from from Sandia Crest and Spirifer striatus Mart. (p. 49, p1. 7, I new species; 11 species Pecos) Neospirifer sp. xxx vicinity, including 1 new species; and 15 species from triplicatus Hall (p. 49-50, p1. 7, fig. 3, Pecos, including 3 new species. Some species were rare Spirifer striatus xxx from Pecos) = Neospirifer dunbari King but others occurred in abundance. Phil. 52, p1. 6, figs. 8, Some pertinent comments by Marcou concerning Terebratula plano-sulcata (p. x 8a-b) = Composite cf. ovata Mather rarer species are as follows: at Pecos village Terebratula Rocky-Montana, n. sp. (p. 50-51, p1. 6, Orthis Pecosii—only one specimen rockymontana specimen, “in a figs. 13, 13a-c) Leiorhynchoidea? Orthoceras Nova-Mexicana—a single (Marcou) T deep ravine near the summit of the Sierra de Sandia” Hall 52, 6, figs. 9, 9a-f, all Product us pustulosus—”only one specimen well Terebratula subtilita (p. p1. xxx from Pecos) = Composite subtilita (Hall) preserved at Tigeras” very abundant” Zaphrentis cylindrica Mime-Edwards and Jules Haime P. scabriculus—”not de Sandia) status very common” (p. 53, p1. 7, fig. 8, from Sierra Spirfer linearus—”not uncertain xx

some of the more Zaphrentis Stansburyi Hall (p. 52-53, p1. 7, fig. 7, Marcou’s comments concerning xxx common species are even more interesting, as follows: from Tijeras) = possibly Caninth? Productus Cora—1 found several dozen specimens in In addition to the above, Marcou noted crinoid columnals (“frag the course of four or five hours exploration, at Tigeras ments of the stalks of encrinites”) at Tijeras and “several unpublished canon of San Antonio, at Pecos village, and lastly at the Bryozoa” at Tijeras. Sandia Summit, and Pecos. 37

summit of the Sierra de Sandia, at 12,000 feet above the em Sangre de Cristo Mountains sea-level area are listed in thAs column. Note again that this is not the complete P. Flemingii—”is found in great abundance fauna at Tigeras of that area; many species reported from near the summit of the that area have Sierra de Sandia. . . also at not yet been reported from the Pecos village” Sandia and Manzano Manzanita areas. Chief P. p’xidformis—”quite sources for Column 2 are common ... near the village Needham (1937) and Sutherland of Tigeras” and Harlow (1973, p. 10, identified by D. E. Waddell). P. semi-reticulatus—”very abundant at Tigeras 3. This column is for the Sandia Mountains area, [and] at the very top of the Sierra de Sandia”; at Pecos, principally Tijeras and Cedro Canyons. Sources “in an hour or two several hundred specimens are in good Needham (1937), Werrell (1961), and several theses. preservation might easily be collected.” 4. The remaining 6 columns present the fauna of Spir(fer Rocky-Montani—”l found the this beautiful Manzano-Manzanita Mountains area, based species in the Mountain Limestone on Myers of Tigeras, Canon of (1973) and six U.S.G.S. Geologic Quadrangle San Antonio, New Mexico; Maps where it is not rare.” published 1966-72 (Myers, 1966, 1967, S. srriaus triplicarus—”abundant” 1969; Myers and McKay, 1970, 1971, 1972). A complete chart compiled Terebratula plano-sulcata---”l have met with it at by Northrop was kindly checked by Donald A. Myers. Tigeras, New Mexico, where it is quite common.” For purposes of mapping, Myers and Myers and T subtilita—”! have seen several thousand specimens McKay used units designated Sandia Formation and of this species at Tigeras, at Pecos village, [and] on the Madera Limestone. The summit latter was subdivided into a of the Sierra de Sandia . . Lower part, followed upward by Units B, C, and D. Zaphrentis cylindrica—”This gigantic species of coral, Later, Myers (1973) raised the Madera Limestone so common in the Mountain Limestone to of England, group rank. He concluded that the Sandia Formation Belgium, and France, had not been found is previously in of Atokan age and that the Madera Group America. I saw a great ranges from number of specimens in earliest Desmoinesian through ascending the Sierra Missourian and Virgilian de Sandia from Antonito, and to Early Permian or Wolfcampian several limestone age. He named two beds were full of them. I also found it new formations, the at Tigeras.” Los Moyos Limestone and the Wild Cow Formation; the latter was subdivided into three Z. Stansburyi—”Some specimens of the coral are members: Sol se Mete, Pine Shadow, and La Casa. The quite large and sometimes much curved, having a Los Moyos Limestone is the “lower part of the Madera semi-circular form . . . I saw a great many at Tigeras, Limestone” of the six maps; age is Desmoinesian and on the summit of the Sierra de Sandia, and at Pecos earliest Missourian. It is what had been called village. The limestone in which it is the found is so hard, Lower gray limestone of the Madera by earlier that it is difficult to obtain well-preserved workers. and complete The Wild Cow Formation is the Arkosic specimens.” The figured specimen limestone is a “fragment show member of the Madera and includes units ing the interior of the turbine.” B, C, and D of the upper part of the Madera. The basal part of the It may be noted that Sutherland and Harlow (1973) Wild Cow Formation is the So! se Mete Member; it is make reference to some of the species described from unit B of the upper part of the Madera; age is Pecos and Tijeras by Hall (1856) and Marcou (1858) but Missourian. The middle part of the Wild Cow Forma do not mention all of them. tion is the Pine Shadow Member; it is unit C of Pennsylvanian the fossils of the Sandia Mountains area upper part of the upper Madera; age is early Virgilian. and some nearby areas are listed in tables 1, 2, and The upper sequence of the Wild Cow Formation is the 3: Table 1—Foraminifera, Table 2—Brachiopoda, and La Casa Member; it is unit D of the upper part Table of the 3—Fossils exclusive of Foraminifera and Brach upper Madera; age is middle and late Virgilian. iopoda. The uppermost formation of the Madera Group Table is the I, Foraminfera in the Sandia Formation and Bursum Formation, of Early Permian Wolfcampian Madera Group, Sandia Mountains, Manzano -Manzanita age. The Bursum is present in the southern part Mountains, of the and adjoining areas, presents the complete Manzano Mountains; the top of the Bursum foraminiferal Formation fauna of the Sandia Mountains area is the top of the highest marine limestone that underlies (Column 3) and of the Manzano-Manzanita Mountains the Abo Formation. Myers (1973, p. 11-12) notes that area (group of 6 columns to the right of Column 3). “northward ... the formation either becomes thinner or is replaced by the overlying Abo Formation . . . Prefatory Remarks to Table I (page 42) In the northern half of the Manzano Mountains, the 1. Identical or related species occurring in the Bursum is absent in most places. Field evidence sug Jemez-Nacimiento Mountains area are listed in this gests that north of Pine Shadow Spring many of the red column. Note that this is not the complete fauna of that beds of the Bursum have been replaced by gray shale area; many species reported from that area have not yet and limestone. If such replacement has occurred, then been reported from the Sandia and Manzano the uppermost beds of the La Casa Member include Manzanita areas. Chief sources for Column I include a Bursum equivalents in the northern Manzano Moun list by Northrop (1974), which is based on an earlier list tains.” (Northrop, 1961a), compiled from Wood and Northrop Table 2, Pennsylvanian (1946), which Brachiopoda in the Sandia included identifications by Henbest, Mountains and Read, other New Mexico areas, presents the and others (1944); and Armstrong and Mamet complete brachiopod (1974). fauna of the Sandia Mountains area in 8 columns and partial brachiopod 2. Identical or related species occurring in the south- faunas of nearby areas in 3 additional columns.

IA ]IVld

S,flOD’HVVi HRZ lNf9Ii

vxz 3Uf1fJJ

A ELLV]d

C

IA A

GNV 3)jfl9I SIV1d S,flODIV4 PONI S1dI3JX3— 39

Prefatory Remarks to Table 2 (page 43) of the Manzanita Mountains, although Herrick and I. In Column I, identical or related species occurring Bendrat regarded it as being in the Sandia Mountains; in the Jemez-Nacimiento Mountains area are listed. other workers, not recognizing the Manzanita Moun Note that this is not the complete fauna of that area; a tains, would place Coyote Canyon in the northern end number of species reported from that area have not yet of the Manzano Mountains.* been reported from the Sandia Mountains. Sources for Herrick and Bendrat’s paper is entitled Identification Column 1 are a list by Northrop (1974), which is based of an Ohio Coal Measures horizon in New Mexico. In on an earlier list (Northrop, 196 Ia, p. 109-111) compiled 1887 1-lerrick had published an annotated list of fossils from Wood and Northrop (1946), and Sutherland and from the shale immediately above the cannel coal at Harlow (1967). Flint Ridge, east of Newark, Ohio. Herrick and Bendrat 2. In Column 2, identical or related species occurring (1900) are rather vague as to the precise locality and in the southern Sangre de Cristo Mountains are listed. horizon at which they discovered a number of fossils in Again, note that this is not the complete fauna of that the Sandia Mountains; their list is entitled “List of area; many species reported from that area have not yet fossils from the Sandia Mountains of New Mexico, been reported from the Sandia Mountains. Sources for found in a band of shale supposed to correspond to the Column 2 are Marcou (1858) and Sutherland and Flint Ridge Shales of Ohio.” In the Coyote Canyon Harlow (1973). area, Herrick and Bendrat found 34 species, of which 3. For the Placitas area, at the north end of the “24 are also found at Flint Ridge, Ohio.” The Flint Sandia Mountains, there are two columns, one for the Ridge shale of Ohio is in the lower Mercer limestone Sandia Formation and one for the Madera Formation. (Pottsville or Atokan). However, it appears that the Chief source for this area is Toomey (1953). Flint Ridge of the Manzanita Mountains area must be 4. For the crest or rim of the Sandia Mountains, in the Los Moyos Limestone of Myers (1973), which is there are likewise two columns, one for the Sandia dated by him as Desmoinesian, not Atokan. Formation and one for the Madera Formation. Chief Herrick and Bendrat’s Flint Ridge shale is apparently source is Catacosinos (1962); a few species were cited by about 150 ft above the base of the Madera Formation Marcou (1858). (compare right-hand columnar section given by Herrick 5. For the Tijeras-Cedro Canyons area, at the south ern end of the Sandia Mountains, four columns are *In 1900. Herrick. first given, one professor of geology and second president of for the Sandia Formation and three for the the University of New Mexico, along with colleagues Madera and students, Formation; the Madera is subdivided into generally referred to Coyote Canyon as being in the Sandia Moun Desmoinesian, Missourian, and Virgilian. Sources are tains, probably because it was more accessible from Albuquerque than Tijeras Canyon was. principally Marcou (1858), Szabo (1953), and Stukey A bit of evidence in this connection is that (1967). W. G. Tight—second professor of geology and third president of U.N.M.—led a field excursion into the Manzanita 6. In this Mountains in 1907 last column, for the Coyote Canyon, for the annual meeting of the Geological Society of America, held in Manzanita Mountains area, species cited by Herrick Albuquerque Dec. 30-31. For this excursion he prepared a geologic and Bendrat (1900) are given. Coyote sketch map (fig. 9) with cross sections, entitled Sandia Mountains Canyon lies south Excursion S. of Tijeras G. A. 1907 (Northrop. 1966, p. 10. II; see discussion. p. Canyon and currently is considered to be part 19 of this memoir).

FIGURE 28A—ExCERPTs FROM MARCOU’s (1858) PLATE V. (On page 8 Terebrarula plano-sulcata PHILL. 32 Marcou noted: All the specimens are represented of the natural 8, 8a. 8b) DIFFERENT size exactly as VIEWS OF SPECIMEN FROM TIJERAS. PROB they are; and I have not attempted to restore the ABLY Composita imperfect CF. Orata MATHER. portions, as has been done by many paleontologists, 9 Terebratula subtilita from a fear of making HALL too fantastic additions to nature, which are THREE SPECIMENS very dilcult to avoid FROM PEcos: 9, 9a) SPECIMEN SHOWING in such cases.) THE Figures SINUS ON BOTH vALVES; 9b, 9c) LARGER SPECIMEN, MORE ELONGATED; 9d, 9e, 9f) VERY GIBBOUS AND ELONGATED 4 Productus semi-reticularus MART. SPECIMEN. Composira subtilita (HALL); PROBABLY OTHER 4) FRONT VIEW WITH TUBERCLES, FROM PEcos; 4a) SAME, SIDE SPECIES REPRESENTED. VIEW. PROBABLY Antiquatonia. 13 Terebrarula Rocky-montana, N. SP. 6 Productus scabriculus MART. TWO IMPERFECT SPECIMENS FROM PEc05: 13, I3a) IMPERFECT 6) FRONT VIEW, FROM PEcos; THE 6a) SAME, SIDE VIEW. SPECIMEN 13b, 13c) ANOTHER PROBABLY Buxtonia. SPECIMEN LATERALLY COMPRESSED. Leiorhynchoidea? rockymotitana (MARC0U). SUTHERLAND AND HARL0W FIGURE 28B—ExcERPTS (1973, i’. 60-61, PL. 13, FIG. 19) FROM MARc0U’s(1858) PLATE VI: CHOSE Figures THE SPECIMEN FIGURED BY MARCOU AS HIS FIGS. 13, 13a AS THE LECTOTYPE (R1TIsH MUSEUM OF NATURAL HISTORY I Producruspusrolosus PHILL. B79165), AND CHOSE THE OTHER SPECIMEN FIGURED BY FRONT VIEW, FROM TIJERAS. PROBABLY Echinaria. MARC0U AS HIS FIGS. I3b, l3c AS THE PARATYPE 2 Producruspuncrarus MART. (BMNH B79166). SUTHERLAND AND HARL0W (1973. ‘. 61) STATE THAT FRONT VIEW, FROM TIJERs. PROBABLY Echinaria. THIS “IS THE 3 TYPE SPECIES FOR THE NEW GENUS Corrugatimedio Producruspyxid([ormis DE K0N, rostrum PROPOSED BY SxTENAER (1970, p 23). WE REJECT THE 3) FRONT VIEW, FROM TIJERAs; 3a) SAME. “NOT WELL USE OF THIS GENERIC NAME UNLESS VALID UNCRUSHED DRAWN.” STATUS UNCERTAIN. POSSIBLY Antiquatonia. TOPOTYPES COULD BE COLLECTED TO DETERMINE THE INTERNAL 4 Productus Cora D’ORB. CHARACTER OF THE TYPE SPECIES.” TWO SPECIMENS FROM PEcos: 4) FRONT VIEW, SHOWING 14 Orthis Pecosii, N. SP. TUBERCLES; 4a) DORSAL VALVE, FLATTENED BY VERTICAL MARCOU HAD ONLY THIS ONE SPECIMEN FROM PRESSURE. CERTAINLY PEC0S: 14) Linoproductus, CF. platyumbonus OR VIEW OF prattenianus. DORSAL VALVE 14a) SAME, VIEW OF VENTRAL VALvE; 14b) SAME. VIEW OF BEAK. Cleiothyridina pecosii 7 Productus Flemingii Sow. (MARcOU). THE HOLOTYPE IS BMNH B79168, ACCORDING TO FRONT VIEW, FROM TIJERAS. PROBABLY Sandia sanrafeensis, SUTHERLAND AND HARL0W (1973, p 67-68, PL. 14, FIG. SUTHERLAND AND HARLOW. 24).

C

(

I

N

/ 1” 41

and Johnson, 1900, p1. 22, with Herrick and Bendrat, culina, Juresania, and Schuchertella. All occur in the 1900, p. 3-4). Sandias. Older generic and specific names are given in paren Table 3, Pennsylvanian Fossils of the Sandia theses and quotation marks. Type specimens are indi Manzanita Mountains area (excluding Foraminifera and cated by T. Additional information is noted at the Brachiopoda), presents the complete Pennsylvanian bottom of the table. fauna and flora of the Sandia-Manzanita Mountains Contrasts between the Pennsylvanian brachiopod area (excluding the Foraminifera and Brachiopoda. faunas of the Sandia Mountains area and other areas in which were given above in Tables I and 2) in 9 columns. northern New Mexico are as follows. Note that the Jemez-Nacimiento and southern Sangre Genera reported from the Sandia Mountains but not de Cristo areas are not included. yet reported from the southern Sangre de Cristo Moun tains include Cancrinella, Enteletes, Hystriculina,* Prefatory Remarks to Table 3 (page 45) Juresania, Lissochonetes, and Retaria. Those desig I. For the Placitas-Tejon area, at the north end (*) of nated by asterisks are found in the Jemez the Sandia Mountains, there are two columns, one for Nacimiento Mountains. the Sandia Formation and one for the Madera Forma Genera in the Sandia Mountains not yet reported tion. Chief sources are Toomey (1953) and Lee and from the Jemez-Nacimiento Mountains include Buxto Girty (1909). Under the heading, Sandia Mountains, * nia, Enteletes, Lissochonetes, Mesolobus, * Retaria, Lee and Girty (1909, 19) give a columnar “section * p. of Rericulatia, Rhynchopora, * and Sandia. * Those desig a part of the beds exposed (*) at the north end of the nated by asterisks are found in the Sangre de Sandia Mountains, near Tejon.” This section ranges Cristos. from “Magdalena Limestone” through Abo, Yeso, and Genera in the Sangre de Cristos not yet reported Morrison? to Upper Cretaceous. Above the Madera from the Sandias include Calliprotonia, Crania, Horn limestone there is 40 ft of “sandstone, red, conglomer donia?, Isogramma, Krotovia,* Leiorhynchoidea?, Lepra atic, with limestone pebbles at the base,” overlain * by 2 ft losia, Orthotetes, Plicochonetes? “, Pulchratia? ‘I’, Rhipi of “limestone, granular, earthy.” This is overlain by 700 * domella, Spir(fer Spirferellina, Tesuquea, * and Zia. * ft of Abo red beds, followed by 400 ft of Yeso. Ten One reason that so many of these genera have not been species of mollusks are listed at about the middle of the found in the Sandia Mountains is that 7 of them, Yeso. This is an error; these ten (*), species should have designated by asterisks are found only in the been designated as coming from the 2 ft of limestone Morrowan. So far Morrowan strata have yielded few near the base of the Abo, which fact can be confirmed fossils in the Sandias. by checking Lee and Girty’s fauna! table (p. 48-49) and Genera in the Sangre de Cristos not yet reported the register of three localities (p. 120, U.S.G.S. localities from the Jemez-Nacimientos include Buxtonia, * Calli 3796, 3797, 3798). We suspect that the entire fauna of 20 protonia, Horridonia?, Kroto via, Leio rhynchoidea?, species, including 10 bivalves, 7 gastropods, * 2 Mesolobus, Onthotetes, Plicochonetes?, Reticulatia, * brachiopods, and 1 scaphopod, came from the top of the Rhipidomella, Rhynchopora, * Sandia, * Spirfer Madera Formation, not from the Abo, and certainly not SpirfereIlina, Tesuquea, and Zia. Those designated by from the Yeso. The (*) three localities were given as Ojo de asterisks are found in the Sandia Mountains. San Francisco, road between Ojo de San Francisco and Genera in the Jemez-Nacimientos not yet reported Tejon, and two miles south of Tejon. Unfortunately, a from the Sandias include Crania, Isogramma, Leptalo number of padlocked gates make these localities inac sia, and Pulchratia. All occur in the Sangre de Cristos. cessible today. Genera in the Jemez-Nacimientos not yet reported 2. For the crest or rim of the Sandia Mountains, from the Sangre de Cristos include Cancrinella, Hystri (continued on page 44, right column)

FIGURE 29—MARcou’s(1858) PLATE VII: GIRTY’S LECTOTYPE OF Anthracospirfer rockymontanus Figures is BMNH B79I55; SEE SUTHERLAND AND HARL0W (1973, P. 86, 1 Orthoceras Nova -Mexicana, N. SP. PL. 17, FIG. 7) AND COMPARE WITH THEIR FIG. 8. WHICH IS A A SINGLE SPECIMEN FROM A DEEP RAVINE NEAR THE SUMMIT PLA.STOTYPE OF THE LECTOTYPE. OF SIERRA DE SANDIA. GENERIC ASSIGNMENT UNCERTAIN; 5 Spirfer lineatus MART. PRESUMABLY THE HOLOTYPE IS IN THE BRITISH MUSEUM OF 5, 5a, 5b) DIFFERENT VIEWS OF SPECIMEN FROM PEC0s: Sc) NATURAL HISTORY. SPECIMEN FROM TIJERAS, SHOWING TO THE NAKED EYE THE 2 Spirfer striatus MART. RETICULATION OF ITS SURFACE. THIS IS NOW Phricodothyris 2) SPECIMEN FROM PEc0S, VIEW OF DORSAL VALVE; 2a) SAME, perplexa (MCCHESNEY). VENTRAL VALVE. Neospirfer, PROBABLY. 6 Myalina Apachesi, N. SP. 3 Spirfer siriatus VAR. iriplicatus HALL FROM NEAR THE RANCHOS OF PEC0s VILLAGE. 6) SIDE VIEW OF FRONT VIEW OF SPECIMEN FROM PEcos. PROBABLY Neospir A SPECIMEN WITHOUT THE BEAK OR THE CARDINAL BORDER; ferdunbari KING. 6a) SIDE VIEW OF THE BEAK. PRESUMABLY THE HOLOTYPE IS IN THE 4 Spirfer Rocky-Montani, N. sp. BIUTIsH MUSEUM OF NATURAL HIsTORY. Now Seprimyalina TWO SPECIMENS FROM TIJF.r,.s: 4, 4a, 4b) DIFFERENT VIEWS apachesi (MARC0U), ALTHOUGH NEWELL (1942. P. 67-68) OF A LARGE SPECIMEN (NOW Anrhracospirfer curvilareralis DOUBTFULLY PLACED THIS SPECIES IN THE SYNONYMY OF S. chavezae SUTHERLAND AND HARL0w); 4c, 4 YOUNG 4e) bur,nai NEwL, A PERMIAN FORM; WE THINK MARCOL”S SHELL A LITTLE COMPRESSED (NOW Anthracospirfer rockymon ORIGINAL NAME SHOULD BE REVIVED. tanus (MARCOU)). 7 Zaphrentis Stansburyi HALL ACCORDING TO SUTHERLAND AND HARLOw (1973, P. 82-84, FRAGMENT OF A SPECIMEN FROM TIJERAs, “SHOWING THE PL. 17, FIG. lO), MARC0U’s (I858) SPECIMEN SHOWN AS HIS INTERIOR OF THE TURBINE.’ MAY BE Caninia. FIGS. 4, 4a. 4b IS BMNH B79154. AND Is Anthracospirfer 8 Zaphrenriscylindrica MILNE-EDwARDS AND JULES HAIME curvilateralis chavezae; SUTHERLAND AND HARL0W’s FIG. II IS FRAGMENT OF A LARGE SPECIMEN FROM SIERRA DE SANDIA. A CAST OF THE SAME SPECIMEN. STATUS UNCERTAIN. 42

TABLE I —FORAMINIFERA IN SANDIA FoRMATIoN AND MADERA GROUP, SANDIA MOUNTAINS, MANzAN0-MANzANITA M0UNmIN5, AND ADJOINING AREAs (Superscrtpts at heads of columns refer to prefatory remarks n text: numbers in table refer to notes at bottom of table)

—

— MANZ000MANZ*Nlt* MrS.4 U*01A140-MANZ*NI7A MIS Mod.,. Oo,,p M.d., G,oop WildCowF,.,. Wild Cow Ow. 01 j a I L I s1 El P1 .. i, J : t. i sp. X X Aptereinellids x x M.7 pinosensis X Beedeina aff. arizonensis ( Fusulina) I N ole I) X Schwagerina X B. cf. bow,ens,s X S. sp. Tefrataxis sp. X X B. euryteines x x Textulacia? sp. X 8. aff. cut t!eines x Textutariidae X 11.? aff. insolita X Trificites aff. cameratoides X B. noramexicana x x aff. creekensis x B. ci. notamexgcana X T. cf. cuchilloensis X X B. aff. pattoni x T. fresnalensis X X B. rockymontana XX T. cf.fresnalensis X B. aff.rockymontana x 7: fresnalensis X X B. socorroensis x x T. aff. X X X X B cf. suiphurensis X T. irregularis irregularis X X X B. taosensis X T. aff. x x B. aff. taosensis X T. nebraskensis X B. spp. X X X X T. cf. ,sebraskensis X B.? sp. X T. aff. pinguis x Biseriella of the group B. parva X X T. cf. plummeri X Bradyinaspp. X X X X X T. off. plummeri X X Climacammina sp. X X X T. aff. secalicus X X Dunbarinella? sp. x 7: ventrico sun car. X X X X Endothyra tp. X T. ventricosus, cf. weilsi (Note 2) X E.? sp. X X 7: aff. welisi X Eoschuberrella aff. bluensis X 7: aff. wherstonensis (Note 3) X X Eowaeringella aff. ultimata X T. X X X X X X X Fusulinella devexa X 7: spp. Wedekindellina ellipsoides X F aff. devexa X euthysepta X X X F. famula X W. excentrica X X X F cf.famula X W cf. henbesti X F spp. X X W. x F.? spp. X X X W aff. henbesti x x x x Globivalpulina st. X X w. spp. Millerella sp. X

NOTES a limestone of the Jemez Springs Shale Member of the Madera For beds, just 1. Donald A. Myers (letter, Feb. 21, 1974) writes: “With regard mation 29 ft below the base of the Abo Formation red to my use of Beedeina, I am following lshii, 1957 (Proc. Jap. Acad., west of Battleship Rock 4 miles above Jemez State Monument near and re v. 23, 652-656) and 1958 (Jour. Inst. Polytechnics, Osaka Univ. Jemez Springs (Sutherland and Harlow, 1967, p. 1068), P. was ser. G, v. 4, p. 29-70). In these articles, Ishii restricted Fusulina s.s. garded as late Virgilian in age. Again, T. aff. whetstonensis June 12, 1974) in a collection . . identified by D. A. Myers (letter, to the group of F cylindrica. . As thus defined, most of what has been called Fusulina in this country is now referrable to Galloway’s made by us and J. F. Callender from the Arkosic limestone member the west genus Beedeina.” of the Madera Formation, in abandoned railroad cuts along NNE of San Antonito and 2. The type locality for T. wellsi Needham (1937, p. 12, bc. 8; side of San Pedro Creek, about 6.5 miles 37-3 8) is about 1.5 miles east of the east edge of our map (map 1), about 6.7 miles S of Hagan. Myers reported that the form is close to about a mile east of Barton, along 1-40. Barton is just off the map. material that he has from the upper part of his La Casa Member of 3. Thticites aff. whetstonensis was identified by D. E. Waddell in the Wild Cow Formation of the Madera group (late Virgilian). 43

TABLE 2—PENNSYLVANIAN BRAcHI0PODA IN SANDIA M0uNTMNS AND OTHER NEW MEXICO AREAS (T type(s): superscripts at heads of columns refer to prefatory remarks in text; numbers in table refer to notes at bottom of table)

WOIA MflU#TAIt

. -

M I]!j . .! I I J-!J. ; I; ii I III I I eohrocospirifer t I I I I I I I A curwilaterabs chore:ae Ju,esanw Sutherland and Hanloss nebnrsce,uis (‘Productua.” ‘Ptsstuta’) (“Spirifer Rock v-,kIovta,ts (Note 5) X x x xx tn past) (Note I) T x ko:lowskw sptendens (‘Morgsntjrra”) X x x xx A. mother, (Note 2) x x A.’ np x A occiduiss Spsr,fcr L,ngula occsdsntabs 1 x x x x x x x L. ci, carbonarw A. ci. occiduut x L. t,ghe, A. ncctduut. vat x x L, npp. x x A. opimus x x x x x x Lsnoprodu clot instnuatun (“Produces,,’) A. rock smonranus (Marcou( x I.. (Note 3) x x x x T oklahontac x A. cf. rock v,nontonus x x I.. cf. ok)ahomae x A. spp. x x L, plutyurnbonua x x x Antiquotoaw coloradoe,ssis (Productus. L, ci. or au. p)alj’uen bonus x x x ‘Sic: voclostus 1 x x x L. prateenianus (“Productun coral x x 9 X xx A. crossicv stata x x x L. 7 tp. x A. portlockiana x x x x Lissochonctes sp. x A. spp. x x x x Meekella srriaeocostata x x x Beecheria bovidens (“I.3,e)asma”) x x x x M, ci striatocostata x x Buxtonia scabricula (“Productus. “an English Mesolobus Mississippian sp.) x x decipiens (“Chonetes”) x M, strjotus I’M. mesolobaa”) B. n. sp. B of Sutherland and tIarlow T x x x x x Neocho,tetes granu!ifer (“Chorreses’) Cancrinella boone,tsis (“Productella pertenuis ‘7 x x x x x x x Neospirsjeralotun Chonettnelia crassirodiota (“Chonetes.” (“Spirifer’) (Note 6) x x x x x “Cho,tetista”) x N, cameratus x x x C firntingi x N, du,tbart (“Spirifer striatus triplicatus”) C. ci. flentingi x x x xx X, N gibbosun C. fleeningi ajata x x x x N. spp. C terneujljana x x x x Orbicu)oidea capubjormis C(e,othvridina pecosii (“C orbicularis”) (“Discina convexa”) , 9 (Note 4) x T x x 0. mistouriensis x x Composila argentra ( Terebratula,’ Athvrss”) x x 0. ,,itida (“Discina nitida, “an C elongata x x x x x English sp.) x C ci. elongata x 0, spp. x x x C. ntagna x x Phrrcodoehyrss perp)exa (Note 7) x x x x x x xx xx C ci. snagna x “Productus Flemingii” of Maecou; an English tp., pnobably Sandia tp. x x C. Ovatsl x x x x x “P. punceatus” of Marcou; an English C. ci. osata sp., ptobubty Eclti,taria x x C. subtj(ita x x x x x x x “P. pustulovus” of Marcou; an English vp, now Pustula pastukrsa x C. irsiubato x x x “P. prxsdiforenrn” of Marcou; an C’ sp. English vp, now Ptuntula: possibly Ant,quatonia crurithyris pl.anoconce.va (‘A mbocoelsa “3 x x xxx x Ptunc’tospirifer Serb via crassa (Serbia”) x x x xxx kenruckyensis x x xx P. S. sp. x ci. kentuckyensis x x Relaria lasallensis Desmoines,a missouriensis (“Marginsfero x x (“Marginifera”) x x R.’ S. ci. mlssourtensts x x all. laval)ens,s x Reeissulatia D. muricatina (“Rudinga”) sp. (Productar rensireticukrus,” x x x and “Dictyoc)ootusamericanas”) S. cf. ,nuricat,na x (Note 8) x x x xx S.’ sp. x Rhj nchopora magntcosea x x Echissaria knight, (“Productus.” Sand,,, santafeenais (age probably Atokan) T x ‘Echinoconchus”( Schizophorsa oklahonsee x x E. ci. ksttght, x S. ci oktohonrae x E. seinipunctara x x x xx S. resupinoides x E. ci. sem,puncsata x x Schuchersdlla prateeni x E. spp. See several species listed below S.? under ProduCes sp. x “Sprriferfuieonensis” Enicletes (rcmiphcatus of Hernick and Bendtat x (1900) maybe Anehracospirifer x E. heeniplica rut plarrtburgensis x Weflerella imeesara,a x x x Nussedia mormoni (“li’rebrutula ‘1 x x x x x k 010gensis x x x x Hyntriculina re’abashensis (“Marginifera”) x x x 147? sp. (“Rhynchonella sp.”) x 44

NOTES TO TABLE 2 (continuedfrom page 41) 1. Marcou’s types of Spirifer Rock v-Montani include at least two there are two columns, one for the Sandia Formation species: Anthracospirifer rockymonranus (Marcou) and A. curvi and one for the Madera Formation. Chief source is and Har (ateralis charezae Sutherland and Harlow; see Sutherland (1962), but Marcou (1858) cited a dozen (1858, 50, 7; our fig. Catacosinos low (1973, p. 3-4, 83, 86-87). Marcou p. p1. of the Sierra de Sandia,” 29) collected his specimens from the “grand perpendicular wall” of species from “the summit “Mountain Limestone of Tigeras, Cañon of San Antonio,” which is “near the summit,” “at the very top of the Sierra de near Seven Springs, west of Tijeras. Sutherland and Harlow (1973, Sandia,” etc. The holotype of “Orthoceras Nowa-Mex (Marcou’s figs. 4, p. 83) believe that the larger of the two specimens icana”came from “a deep ravine near the summit of the 4a-b) is a variant of A. cureilateralis chavezae. Also placed by them Gixty (not Swallow), 1903, and Sierra de Sandia.” in synonymy are Spirifer boonensis’? at the Spirifer occidentalis of Dunbar and Condra (not Girty), 1932. 3. For the Tijeras-Cedro Canyons area, Weller’s (1898, p. 589) synonymy of Spirifer rockymontanus for southern end of the Sandia Mountains, 4 columns are the period 1858-79 included 18 citations and included some of S. I for the Sandia Formation and 3 for the Madera had 22 cita given, opimus and S. subventricosa. Girty (1903, p. 383-384) subdivided into Desmoines Mather (1915, 181-183) had 19 Formation; the Madera is tions for the period 1858-99; p. Principal sources are citations for the period 1858-1911. Girty (1903, p. 384) proposed Ian, Missounan, and Virgilian. restricting the name S. rockymontanus to the smaller of Marcou’s Marcou (1858), Szabo (1953), Werrell (1961), and two specimens and thought the larger specimen might be a variety Stukey (1967). A few citations are from Herrick (1900a), speci of S. cameratus. Mather (1915, p. 184) argued that the larger Hernck and Johnson (1900), and Bisbee (1932). Hernck of two to be mentioned in his (Marcou’sj men was “the first the illustrated 10 species of “Upper Carboniferous,” text as well as in the legend to the plate and therefore the type of (1900a) the species.” Dunbar and Condra (1932, p. 319) disagreed, noting “Permo-Carboniferous,” or “Permian” fossils—probably that Girty’s selection had precedence by 12 years, and proposed a all of Pennsylvanian Virgilian age. Four of the fossils new name, S. matheri, for Mather’s species from the Morrowan. came from the Sandia Mountains; one came from the and Harlow 2. In discussing Anthracospirifer matheri, Sutherland east side of the Sandias; and five were “from base of (1973, p. 86-87) state east of Sandia Mountains at “We believe Dunbar and Condra were incorrect in referring section near adobe smelter Marcou’s (1858, p1. 7, figs. 4, 4a-b) larger specimen of Spin the base of the Permian.” A difficulty in connection with fer rocky-montani to this species. That specimen, apparently recognizing the last locality is that there were at least 2 from Desmoinesian strata, is a larger form (with a shallower smelters in the area, 1 near La Madera and I near to Anthracospirifer curvi sulcus) we consider closely related We have credited these fossils to the Virgilian of lateralis chavezae.” Tijeras. See Mather (1915, p. 181), Dunba.r and Condra (1932, p. 322), and the Tijeras-Cedro Canyons area. Sadlick (1960, P. 1212). 4. For the Coyote Canyon, Manzanita Mountains 3. See Marcou (1858, p. 50, p1. 7, figs. 4c-e; our fig. 29). This is area, see Prefatory Note 6 to Table 2 (Brachiopoda) for one the smaller of the two specimens figured by Marcou and is the fuller explanation of Herrick and Bendrat’s (1900) list as the lectotype. It had long been a selected by Girty (1903, p. 384) shale fossils. A few records are from believed that Marcou’s specimens were lost, but Sutherland and Har of “Flint Ridge” and Bisbee (1932). low (1973, p. 86) note that both are preserved in the British Herrick and Johnson(1900) Museum of Natural History. Also worth noting is the foUowing Northrop’s (l961a, p. 109-111) list for the entire abstract, entitled “Spirifer rockymontanus Marcou from the type Sandia-Manzanita Mountains area might also be cited. area,” by James Steele Williams (1946): are given in paren from ‘Tigeras, Older generic and specific names “Marcou described Spirifer rockymontanus are indi Canyon of San Antonio, New Mexico.’ Bed-by-bed collec theses and quotation marks. Type specimens tions made in 1946 from the type locality show that this cated by T. Additional information is noted at the species has a much greater range in variation than is generally bottom of the table. attributed to it and that certain forms now considered sep arate species from S. rockymontanus should be more logic ally considered as mere varieties having little stratigraphic CORRELATION significance.” some years ago, 4. Marcou (1858, p. 48, p1. 6, figs. 14, 14a-b) named this Orthis As Northrop (196 Ia, p. 111) wrote village. Girty (1915) and Dunbar and Condra Pecosii for Pecos The first significant attempt to correlate the Pennsylvanian orbicul.aris (McChesney) 1859. (1932) referred it to Cleiothyridina strata of New Mexico with standard sequences in other regions one year (Sutherland and Harlow, Marcou’s name has priority by was by Needham (1937) in his bulletin on New Mexico 1973, p. 67). fusulinids. In 1940 he published a short paper entitled “Corre Harlow (1973) did not find 5. It is surprising that Sutherland and lation of Pennsylvanian rocks of New Mexico.” Using about although Juresania in the southern Sangre de Cristo Mountains, twenty-five species of fossils, chiefly brachiopods and a few Springs. Similar genera, earlier they (1967) had found it near Jemez fusulinids, he suggested that the oldest Pennsylvanian strata of by several such as Pulchratia? and Buxtonia are each represented central New Mexico are younger than Bend, Morrow, or lower species in the Sangre de Cristos. Pottsville. Two years later, Thompson (1942) proposed the two species, Neospinifer 6. In 1932 Dunbar and Condra described term Derry series for the essentially pre-Desmoinesian and 1-larlow triplicatus alatus and N. torus. According to Sutherland Pennsylvanian rocks of central to south-central New Mexico, and the latter the (1973, p. 75), the former represents the young and correlated the Deny with the Atoka of Oklahoma, adult, respectively, of the same species. Cheney’s Lampasas of Texas, and the basal part of the Des species: Spin 7. Many different names have been applied to this Moines of some areas in the Mid-Continent region. He did not Spirifer fer lineatus Hall (not Martin), 1856, and Marcou, 1858; believe that the New Mexico Pennsylvanian sequence included of Mather, 1915, perplexa McChesney, 1860;Squamularia perplexa, any part of Morrowan time. been referred to and of Dunbar and Condra, 1932. The species has Thompson correlated the Sandia formation of the Sandia Martinia, Reticularia, and Condrathynis. Mountains with his Elephant Butte formation of the Armen 8. According to Blake’s (1856, p. 142) translation of Marcou’s daris group of Desmoinesian age. According to him, a section near Tijeras. (&o field notes, the latter found Productus giganteus at the northern end of the Sandia Mountains includes rocks of J. 1822, is now Gzantoproductus ductus giganteus, of Sowerby, Desmoinesian, Missourian, and Virgilian age, while sections at In his 1858 paper, Marcou (p. giganteus of the British Mississippian.) Jemez Springs include rocks of Derryan age as well. However, Productus giganteus, but does cite Productus 56) does not mention in the same year. Read and Henbest (1942) stated that the forms of the latter species were given a new semi-reticulatus Some Pennsylvanian of northern New Mexico includes rocks of name, Dictyoclostus americanus, by Dunbar and Condra (1932, p. (continued on page 48, bottom) 218); this in turn was changed to Reticulatia by Muir-Wood and Cooper (1960, p. 284). 45

TABLE 3—PENNsYLvr.uAN FossiLs OF SANDIA-MANzANrrA MoUNTAINs AREA, ExcLuDING FoR1INIFERA AND BRAcHIOPODA (T=ype(s): superscripts at heads of columns refer to prefatory remarks in text: numbers in table refer to notes at bottom of table)

SA%DIA MO5$TA)NS — SANDIA T.4r.. MOUNTAINS C.d,., Cany.,.,? 1’... C.d C — M.d. F.., P1.mt..1 C,..52 Cd — M.d.r. F., . . I ii C . . I I -2 .2 • I — I I I I I I ! U I I I I SCYPHOZOA (Extinct jellytish-iike forms) A iculopecten basilicus Conulorw x sp. N .4.7 core canoe (“Deltopecten”) ANTHOZOA (Corals) x “.4mplexas coralloides’’ (an English sp.; A accidentolis x status uncertain) x A. spp. x x Auloporo? anna x Baker cOw pore a x Caninia torquio x x x7 Cepricardinia corbonorw (Macradon ) C.? sp. x x Dunbaretlo knighti x Choetetes milleporaceas x x Ed,nondia ospinwallensis x C. cf. milleporaceus x F. g.bbosa x Dibanophytlum ealerioe x xx £ nebroscensis D. sp. x x F. sp. Laphophyllidium proliferum x xx Fasciculoconcho scalaria (‘A utculopecten”) Mtchelinro sp. (‘Pleurodictyum’) x Myolina (Myalina) wyomingensis x x Neozaphrentis sp. x M. (Orthomyalina) subquadrata x Syringoporn multotrenuata x .14. sp. and .41? sp. (Note 3) x S. cf. multattenuata x “uculana bellistriata x x S. sp. x ‘N.’ bellistriata attenuato x “Zophrentis cytindrica’ (an English sp.) x x .llonopterio marion x “Z. Stonsburyi (may be Caninia) x x Poloeo!ima retifero (Limo”) Tetracorals, undet. xx Polevoldia glabro (‘I-oldin”) x x BRYOZOA (Moss animals) Parallelodon obsoletus Fenestella a!buquerqucano Herrick and x x Bendrat (Note Syntypes 1). T P. tenuistriatus x F. limbata x Permophorus mexiconus? (“Pleurophorus”) x F. norwoodiona x P. subcuneatus x F. spp. (“Fenesirellina”) xxx x xx P. aff. taffi? x Fistalipora incruStone x 7 9 P. tropidophorus x x F. nodulifero x Prom vtilus swalloci (‘Myalino”) Megacanthopora sp. x Pseudomonotis equistriota x x Penn tretepora trilineata (“Pinnotopora”) x P hawni x P. cf. whitei x Pterio? longa (“Gervillia”) 9 P. spp. x x Preronites nebraskensis (“Aricukspinna’) x Polyporn coyotensis Herrick and Bendrat. P. peracu rue I-bIotype x x (Note 2) T Schizodus wheelcri P. elliptica x xx x x Septimyalino apachesi (“3lcalma”) (Notc 4) x P. fostuosa x S. perottenuata P. sp. x x S.? sp. Prismoporo sp. x x x Streblochondrio? tenuilineata (‘Crenipec ten Rhomboporo lepidodendro ides , x foersti”) R. ef. lepidodendroides x Wilkingia terminale (A ilorisma,” R. sp. x “Allerisma”) x x x SCAPHOPODA sp. xx (Tusk-shells) Plagioglypro conna x Septopora (Synoc!odio) biserioks x P. sp. (‘Dentohum”) x S. sp. x GASTROPODA (Snails) Su(corerepora aff. carbonana A maurotoma subsinuato (‘Yannanio ‘) x (“C)’stodictyo ) x A.? sp. x Tobuiipora heteropora xx Anonias ,nanzonicum? (“Phonerotremo) x T. sp. x Anompholus rotulus Bryozoans undet. xx x x Bellerophon crossus x x BIVALVtA (Pelecypods, clams, scallops) B. Acanthopecten corboniferus xx sna/usculus x B.? A nnu!iconcha interlineoga x sp. x x Donaldino? Astartella concentrica x sp. x Eucanospira A. newberryi x n,issoariensis x E, A. enrico x turbiniformis x

continued 46

TABLE 3—PENNSYLVANIAN FOSSILS OF SANDIA-MANZANITA MOUNTAINS AREA, EXCLUDING FORtlNIFLRA AND BRAcHIOPODA (cont’d) (T=type(s); superscripts at heads of columns refer to prefatory remarks in text; numbers in table refer to notes at bottom of table) continuedfrom page 45

SANDIA MOUNTAINS — SANDIA MOUNTAINS — Tq.. C.&o C.nvna? C.OC..uy..,? Cel2 — U.d.,.F,, -— — .d.Fuu I E ! E I EEE1 . I I I I I I I 1 ¶1 S I I .S I I Euphemrrs ca,bona,ius (Euphemus’) xx Ku’kbya aft. conyonensis x nodocarinatus x K. aft. permiana earica x

E. wbpapiilosus? x Papaparchites claytonensis K. ‘ittatus x Silenites up. x Gontasma lasailensis xx MALACOSTRACA (Shrimps, etc.) (Note 9) a. gen., n. up. (order uncertain) x lanthinoptis primogenius (St,obeus’) xx Syncarid, gen. and up. undet. x Knightites (Cymatospi,a) montfortianas xx (Beilerophon “) MYRIAPODA (Centipedes, miliepedes) (Note 9) gen. and up. undet. x Murchisonia? terebra’ x x INSECTA (Insects) (Note to) Naticopsis deformis Madera ,namayi Carpenter (Holotype) T x N. remex Pseudobiellu fasciata Carpenter (Holotype) T x x N. scintilla Blattarian, gm. and sp. undet. x x N. sp. Thysanuran, gen. and sp undet. x Palaeostylus (Pseudo:ygopleura) perversus x CRINOIDEA (Sea-lilies) x ‘Pateilostium aff. nodicostatum’ of Girty x Cibolocrinus puncraroa tumidur x Platyceras (Orthonychia) parvum x x x x x C. verus Straparollus (Euomphalus) plummeri x Delocrinus cf. n. sp. S. (K.) reedsi x D.’ (Jiocrinus sp. x S. (E.) sp bofGirty x calyx, plate, columnals, undet. x x Worthenia speciosa xx Crinoid Columnals, undet. x CEPHALOPODA (Nautioids) Metacoceras cornutum x ECHtNOIDEA (Sea-urchins) sp. plates and spines perelegans x Archaeocidaris M. fEchinocrinus’) x x Mooreoceras sp. x x CON000NTS (Extinct problematical Orthoceros NovoMexicana’ Marcou organisms) (Note 11) (I-biotype) T h’ibbardella cf. acute x TRILOBITA (Crustaceans) Hindeodella delicatulo x A meant ma/or (‘Phillipsia ) H. megodenticulata x A. songamonensir xx Idiognathodus acutus x Ditomopyge olsoni x x xx I. delicatus x a. spp. x x I. humerus x Phillipsia, sp. not Herrick and Johnson x (NoteS) x I. meekerensis x n.’ of 1-lerrick and Johnson Ligonodina up. ‘Phillipsia, sp. x (Note 6) Ozorkodina ct. camaro x ‘sea FIJRYPTERIDA (Extinct asachnoids, 0. delicotula x scorpions”) gen. and sp. undet. (Note 7) x Spathognathodus minutas x OSTRACOtSA (Crustaceans with a bivalved carapace) (Note 8) Streptognarhr,dus cancellorus x Amphissites sp. A of Werrefl xx S. elegantulus x 4. sp. B aft. irregularis xx S. simulator x Bairdia chaseoe x S. tenuis x B. sp. A aft. conilata x Synprioniodina micrr,denta x B. sp. B aft. auricula x FISHES (Note 12) x 8. sp. C aft. geisi x Acanthodea aft. bronni x B. up. D aff. ventricosa x Acrolepis aft. sedgwicki x B. up. E aft. summa x Cladodus sp. x B. up. F aft. beedei and gorrisonenris x Crenoptychius sp. x B. sp.G x Listracanthus sp. x Bairdiacypris cf. acuminata x x x Orodus sp.

Bythocypris procera x Petalodus 5g. x B. aff. tasmidus x x x aft. Plarysomus? a. gen., n. sp. T Cytherella aft. emaciate x x Proceratodus hlau’ini Zidetc (Holotype) x C. aft. footei x Family Coelacanthidae, gen. and sp. indet. Keilettina binoda Vas. A x Shark tooth, undet. x K. binodavai*B x 47

TABLE 3—PENNsYLvIAN FOSSILS OF SANDIA-MANZANITA M0UNmINS AREA, ExCLUDING FORAMINIFERA AND BRAcHIOPODA (cont’d) (T=type(s); superscripts at heads of columns refer to prefatory remarks in text; numbers in table refer to notes at bottom of table)

IANDIA MOUwTA)N1 — SANDIA MOUNTAINS TIj.,. TtI... C.d.a Cnye.3 c.*. Cva3 pI.n,I C,,2 s-—-- Fiw Wad.,. F,,,. — 6 f E f £ j I I I I I I I ¶: J I I I I I I AMPHIBIA (Note 13) Neuroptens cf. du,’tcsoni Lafonnis X lehmani Berman (Nolotype) T N. opera PLANTS (Note 14) X Asterophyllhzex equisetiformis N. X rcheuchzer, X X X Cajamites aft. asctcowi X N. renuifolia X X C Si,. x Pecoptens pseudovesfita X Calliprvris conferta Plgiozansites X n. sp. X C ci. lyratifolia Sigillaria x sp. X Cardiocarpon t. I (seed on Cordaites Waichia gracillima X foliage) X W. piniformis C sp. 2 (seed on Cordaites X Petrified foliage) X wood, logs X X X C. sp. x Poorly preserved pollen of a primitive coniferous type (Bradbury, 1963; cited Cordaitessp. X X by Stukey, 1968, p. 51) X Ginkgophyte n. gen., n. sp. X Calcareous algae are widespread in marine strata Lebachia sp. X Lepidodendron sp. X

NOTES 6. Another “Phillipsia, sp. n.” was illustrated by Herrick 1. Described as a new species and but not illustrated by Herrick and Johnson (1900, p1 21, fig. 11) but not described Bendrat (1900, or named. This P. 7-8). Fragments of 3 specimens were “found in specimen came from the “Sandia the limestone near Coyote Spring” black limestone below ‘Flint Ridge’ [shale] in Carboniferous (our Sandia Formation). exposures ‘in the corners,’ three miles about south of Coyote 7. A eurypterid, found by Sergius H. Mamay Springs, Sandia (letter, Nov. 21, [Manzanita] Mts., N.M.” This horizon would have 1974) at the Kinney clay pit, been was sent to Leif Stormer, of Oslo, in the lower 75 ft of the Madera. The syntypes and all Univer Norway for identification. sity of New Mexico collections of the early days were presumably 8. The ostracods from Tijeras and Cedro Canyons were described lost in the fire May 23, 1910 that destroyed the Hadley Cimatolog and illustrated by W. L. Werrell (1961) in an unpublished thesis. ical Laboratory. Coyote Spring is about quarter a of a mile north of 9. Axthropods collected at the Kinney clay pit by the southern edge of the geologic S. H. Mamay map (map 1). were submitted to F. R. Schram for study. According 2. Described as new to the latter a species by Herrick and llendrat (1900, p. (letter, Feb. 25, 1975), there and are 2 shrimps, 1 a new genus and new 7) illustrated by Herrick and Johnson (1900, figs. 8, 8a). From species, and an undetermined the syncarid. There is also a poorly pre “Flint Ridge shale near Coyote Springs.” The horizon was ap served mysiapod. parently about 150 ft above the base of the Madera, and in Myers’ 10. Apparently the first fossil insect found in the Sandia Moun (1973) Los Moyos Limestone, dated by him as Desmoinesian. tains area was collected by Sidney R. Ash at the Kinney clay pit on 3. Fragments of a large Myalina are abundant in the Sandia For Oct. 6, 1961 but this specimen has been misplaced. While collecting mation (Toomey, 1953). Myalina? was recorded by Herrick (1900a) fossil plants at the same locality in 1967 and again in 1969, Mamay from “Permo-Carboniferous east side of Sandia Mountains.” found a number of insects which he submitted to F. M. Carpenter. 4. ‘Myalina Apachesi” was described as a new species by Marcou Two new genera and species were named by Carpenter (1858, p. 44-45, pL (1970). 7, figs. 6, 6a) from “near the ranchos of Pecos Order Palaeodictyoptera (extinct, dragonfly-like) village.” Girty (Lee and Girty, 1909, p. 8 1-82, p1. 9, figs. 6-7) identi Family Lycocercidae fied this species from about 50 ft above the base of the Abo sand Madera mamayi Carpenter stone at Abo Canyon, south end of the Manzano Mountains; he also Order Caloneurodea (extinct) recorded it from about 40 ft above the base of the Abo at the north Family Permobiellidae end of the Sandia Mountains. Newell (1942, p. 67-68, p1. 12, figs. Pseudobiella fasciata Carpenter 1-6) thought “Girty was not justified in reviving Marcou’s Myalina Order Blattaria (cockroaches) apachesi for this species,” and doubtfully placed Marcou’s species in gen. and sp. undet. the synonymy of Newell’s new species, Sep timyalina burmai, based Order Thysanura (“silverfish”) on a form occurring in the Lower Permian of Kansas. We disagree Suborder Monura with Newell’s assignment and suggest that Marcou’s species be re gen. and sp. undet. vived as Septimyalina apachesi (Marcou), which seems rather differ An interesting and significant aspect is that both the fore wings ent from Newell’s species. Compare Girty’s figures with those of and hind wings of Madera and Pseudobiella show traces of original Marcou and of Newell; note also that in our opinion the specimens color patterns in conspicuous transverse bands of dark pigmenta from Abo Canyon, from the north end of the Sandias, and from tion. Because of the difficulty of making assignments Pecos are all Virgilian in age. taxonomic of Paleozoic cockroaches, 2 specimens were not described formally but 5. “Phillipsia, sp. n.” was illustrated by Herrick and Johnson Carpenter (1970, fig. 7) published an excellent photograph of one (1900, p1. 21, fig. 9) but not described or named. Horizon and of them. Another cockroach wing, found by Kenneth Kietzke in locality were given as “Flint Ridge shales near Coyote Spring.” This 1972, was donated to the Field Museum of Natural would be in the Madera History. The Formation about 150 ft above the base. It is thysanuran will be described by Carpenter worth (letter, Jan. 14, 1975) in noting that Herrick and Bendrat (1900, p. 10) stated: “A a forthcoming paper. small trilobite is represented by pygidia alone and although it is 11. Apparently the first conodonts reported from the Pennsyl undoubtedly new it does not seem to us desirable to name forms in vanian of New Mexico were found in 1964 by Robert C. Burton. In this genus upon pygidial characters only.” an unpublished study of the paleoecology of the Kinney clay pit, he 48

Dipnoi (lungfishes) illustrated several specimens belonging to 7 genera. Recently he Class separated approximately 500 specimens from 2 kilograms of rock Order ‘Ceratodontiformes and now reports 16 species in 8 genera (Burton, letter, Jan. 10, Family ?Ceratodontidae Procerajodus hiavini Zidek 1975). In his opinion the age is Virgilian. Sutherland and Harlow Atokan, and fishes) (1973, p. 11) report a few conodonts from Morrowan, Class Crossopterygii (fringe-finned or lobe-tinned lower Desmoinesian rocks of the southern Sangre de Cristo Moun Order Coelacanthiformes tains; none were reported from Missourian or Vtrgilian strata of that Suborder Coelacanthoidei area. Family Coelacanthidae 12. In 1963, while collecting fossil plants from the upper Madera gen. and sp. indet. Formation at the Kinney clay pit, John P. Bradbury discovered fossil fishes. David H. Dunkle collected a large number of specimens in 1964; additional material was collected in 1967 and 1969 by 13. Described by Berman (1973) as a new genus and species of Sergius H. Mamay. The combined collections have been studied by labyrinthodont amphibian—”the first Pennsylvanian tetiapod to be Jiri Zidek (1975), whose paper includes most of the fish fauna reported from New Mexico.” This specimen, a juvenile, was col except for the Palaeonisciformes, to be described in a later paper. lected at the Kinney clay pit in 1971 by Neal LaFon and Thomas Orodus was recorded by Yale (1964, p. 23) in the Arkosic limestone Lehman. Classification is as follows. Petalodus member near Los Pinos on Sedillo Hill. A large tooth of Class Amphibia early was collected by Northrop from the rim at Sandia Crest in the Subclass Labyrinthodontia 1930’s. All other specimens are from the Kinney clay pit. Order Temnospondyli Romer Taxonomy of the fishes is changing rapidly. For example, Suborder Rhachjtomj (1945) had placed the acanthodians in the class Placodermi; in 1966 Superfamily Trimerorhachoidea he transferred them with a query to the class Osteichthyes; now Family Trimerorhachidae the they constitute a class, Acanthodii. Current classification of Lafonius lehmani Berman fishes from our area is as follows, according to Zidek (letter, Jan. 21, 1975). determined over a period of years Class Chondrichthyes (sharks and rays) 14. Most of these plants were by Toomey (1953, p. 9-10), Subclass Elasmobranchii by Charles B. Read, as acknowledged 8, 51-52). Family Edestidae Northrop (1961a, p. 109, 111), and Stukey (1967, p. pit in 1961 Orodus sp. Well-preserved specimens were found at the Kinney clay according to Ash (letter, Family Petaiodontidae by S. R. Ash, C. J. Felix, and G. D. Glover, in 1963. S. H. Ctenoptychius sp. Oct. 3, 1974). More were collected by J. P. Bradbury extensive collections in Petalodus sp. Mamay, of the U.S. Geological Survey, made ginkgophyte, not yet Incertae sedis 1967 and 1969 which yielded a new genus of reported occurrence Cladodus sp. described. There is some doubt concerning the noted Listracanthus sp. of Callipteris at the Kinney clay pit. Stukey (1967, p. 51) earlier Burton (1964, Class Acanthodii (spiny “sharks”) that Read had identified C. conferta and p. On the other Order Acanthodiformes 10) stated that Read had identified C. cf. tyratifolia. examining Family Acanthodidae hand Mamay (letter, Nov. 21, 1974), after carefully Acanthodes aft. bronni many tons of material, states he has never seen any species of Cal Class Actinoptergyii (ray-finned fishes) lipteris at the clay pit. widely distributed in Subclass Chondrostei Calcareous algae, although undoubtedly by most writers. Yale Order Palaeonisciformes marine strata, have not been mentioned 18B) noted algal Suborder Palaeoniscoidei (1964, p. 27, fig. 15; p. 28, fig. 16; p. 31, fig. of the Madera near Los Family Acrolepididae nodules in the Arkosic limestone member was submitted to J. A crolepis aff. sedgwicki Pinos and Sedlllo Hill. One of his thin sections felt made by the blue-green Suborder Platysomoidei Harlan Johnson, who reported “an algal 29, 49) also noted algal nodules Family Platysomidae algae.” Stukey (1967, p. 13, 26, 38, to the Spongiostromata. aff. Platysomus? n. gen., n. sp. 1-2 inches in diameter, which he referred

(continuedfrom bottom ofpage 44) Morrowan age. In 1944 Henbest and Read recognized the The Schizophoria oklahomae zone of Morrowan age Millerella zone in the Jemez country near Jemez Pueblo and in the Jemez-Nacimiento area has been informally that it is of probable again at the Soda Dam, and concluded named the Osha Canyon formation by DuChene (1973, Morrowan age. (See also Read and Wood, 1947.) Northrop Pennsylvanian Northrop (1946) assigned a 1974). His section of Mississippian and and Wood (1945). and Wood and is as Morrowan age to certain strata in the Jemez country, citing strata at Guadalupe Box north of Jemez Pueblo especially the large and distinctive brachiopod Schizophoria cf. follows: which occurs in the oklahomae (ranging up to 73 mm across), ft Wapanucka and Morrow of Oklahoma. We collected this striking brachiopod near the base of the Sandia formation at Madera Limestone 760 two localities in Guadalupe Canyon, about 7 and 9 miles, Sandia Formation 225 Armstrong (1955) Pennsylvanian respectively, north of Jemez Pueblo. Later, Osha Canyon formation 56 found an abundance of good specimens of this species in I, Penasco Canyon. about 7½ miles west of Jemez Pueblo. Pennsylvanian In 1946 Northrop f in Wood and Northrop] reported for the or Mississippian Log Springs Formation 2-5 Jemez-Nacimiento area a total of about 185 species, based on a collections from 33 strati- preliminary study of nearly 100 Mississippian Arroyo Peñasco Formation 25-26 graphic sections, and proposed five faunal zones—designated A, B, C, D, and E (from oldest to youngest)—”each of which is characterized either by species having short stratigraphic Mountains, Suther of longer-ranging species, by In the southern Sangre de Cristo ranges. by the earliest appearance the Sandia and a notable abundance of certain long-ranging species which land (1963) was unable to delineate range through more than one zone, or by a combination of Madera Formations and therefore proposed two new these.’ Faunal zone A = Morrowan; B = late Morrowan, formations: 1) La Pasada (equivalent to the Sandia = late Desmoinesian Lampasan, and early Desmoinesian; C Formation plus the Lower gray limestone member of and earliest Missourian; D = remainder of Missourian; and E Madera Formation), overlain by 2) the Alamitos = Virgilian. the 49

Formation (equivalent to the upper Arkosic limestone few inches of conglomerate member of the Madera Formation). occur at the base. The only Farther north, in megafossils seen are indistinct the Rio Pueblo valley, outlines of brachiopods Sutherland described the Fle and cnnoid columnals. chado Formation as the northern equivalent of the La Stukey (1967), working chiefly with the Arkosic Pasada Formation. The La Pasada and Flechado For limestone member (upper), attempted to correlate the mations range in age from Morrowan through Atokan Late Pennsylvanian rocks between the Kinney clay to middle Desmoinesian. The overlying pit Alamitos For and the sequence that Yale (1964) had studied mation ranges from middle Desmoinesian along through US-66 at Sedillo Hill. He reviewed the faunal and floral Missourian to Virgilian in the southern part of the evidence and concluded that as much as Sangre de Cristos near Pecos 400 ft of the (Sutherland and Harlow, upper part of the Arkosic limestone 1973, fig. 8). member (upper) might be Permian. The plants and particularly the fishes Toomey (1953, p. 47-49) concluded that the few at the Kinney locality seem to indicate a Permian age, fossils he had collected from the upper part of the even though the fusulinids are regarded as being of Sandia Formation at the north end of the Sandia Late Pennsylvanian age. Some part of these beds Mountains indicated early Desmoinesian is age, and (in undoubtedly equivalent to the Agua Torres Formation his p1. 4 and again in fig. 10) suggested that the lower in the Los Pinos Mountains dated as Permian part of the Sandia by Stark Formation is of Morrowan and and Dapples (1946, 1154) or Atokan age. p. to the Permian Bursum Catacosinos (1962, p. 24) concluded that Formation in the Manzano the Sandia Mountains (Wilpolt and Formation along the western scarp below others, 1946). Sandia Crest ranges from Atokan to Desmoinesian. In the Manzanita Mountains, Szabo (1953) regarded Myers and McKay the Sandia Formation at the (1970) divide the Magdalena into south end of the mountains 1) Middle Pennsylva as ranging from Atokan to nian, including the Sandia Formation Desmoinesian. In the Manzanita-Manzano (Atokan) and a Mountains, “lower part” of the Madera, and Myers (1973) believes 2) an Upper Pennsyl that the Sandia Formation is vanian, including the remaining Atokan in age. exposed Madera. Of the 1,300 to 1,400 ft of Madera in the Manzanitas, 700 ft Morrowan strata are present in the Santa Fe-Pecos may be equivalent to the Arkosic limestone member area to the northeast, as well as in the Jemez (upper), all Upper Pennsylvanian. Myers (personal Nacimiento area to the northwest, and it seems likely communication) has identified Virgilian-type Tnticites that better evidence may eventually be found in the above the fish-bed horizon in the upper part of the northern Sandia Mountains for Morrowan-age strata. Madera. As the situation now stands, the age of about However, Morrowan may be lacking in the central 300 ft of the upper Madera is in doubt. However, Sandia Mountains and in the Tijeras area. it is still likely that an uppermost transitional zone The Madera Formation was divided between by Toomey the Madera and the Wolfcampian Abo may (1953) into three members (ascending): be equiv 1) Clastic alent to the Wolfcampian Bursum Formation. limestone member (Desmoinesian), 2) Chert armor member (Missourian), and 3) Arenaceous limestone PERM member (Virgilian?). Catacosinos (1962) reported that IAN the lower part of the Madera Formation exposed along The Permian beds of central New Mexico are of two the western scarp of the mountains is of Desmoinesian types: I) the continental Abo Formation built across the age. Szabo (1953) concluded that the Madera at the surface left by the regressing Pennsylvanian sea, south end and 2) of the mountains ranges from Desmoinesian the Yeso, San Andres, and Bernal Formations to Virgilian. deposited successively on the Abo flood plain in arid back-reef In 1973 Sutherland and Harlow, in their memoir on seaways or restricted lagoons. The Abo beds are fluvial the brachiopods of the southern Sangre de Cristo subaerial deposits whereas the later formations are Mountains, reported on their brief examination of the evaporitic, marine, and in part littoral and eolian in area near Tijeras that Marcou had visited on October 8, origin. 1853. They did not specifically mention the Sandia Formation, but observed that the lowermost Pennsylva ABO FORMATION nian rocks cropping “out on a steep hillside just west of Definition—The Abo Formation was named by Lee the great clifi” [Marcou’s “grand perpendicular wall” at (Lee and Girty, 1909, p. 12) for exposures at Abo Pass Seven Springs] “are poorly fossiliferous, but we col at the southern end of the Manzano Mountains. The lected specimens of Sandia santafeensis, suggesting an Abo rests either disconformably on or with probable Atokan age. Fossils of definite Morrowan age are conformable lacking.” intertonguing with the underlying Madera Formation. It has been the custom to map the basal On the other hand, a limestone knob rising above the contact just above the last marine fossil-bearing beds, alluvium west of the mountains and only 4.6 miles west and higher limestone beds yielding no marine fossils of Seven Springs (secs. 14, 23, T. ION., are R. 4 E.)contains included in the Abo. Selection of the boundary a sparse microfauna that suggests a possible on this Morrowan basis is workable although not completely satisfactory, age (A. K. Armstrong, letter, May 10, 1974) but the as marine beds are not everywhere fossiliferous. The Madera elsewhere in the area is not older than Des highest fossil-bearing bed in one outcrop may pinch out moinesian. This small mass of limestone, several tens of in another area, requiring that the contact be shifted feet thick, seems to resemble some part of the Lower stratigraphically downward in order to follow the gray limestone member of the Madera Formation highest recognizably marine bed. Of course, the con rather than any limestone of the Sandia Formation. A verse situation is also encountered. In most instances the 50

sequence in the northern part of projected sec. 23, T. 13 stratigraphic interval involved is a few tens of feet or N.,R.5E. less; where beds dip appreciably as in the Sandia area A section modified from Harrison (1949, p. 42-44) few mapping problems result, as the contact line may measured across San Francisco Creek 2 miles north of nearly cover the intertonguing strip at the map scale Montezuma Mountain is given in Appendix I. used. Abo-type red beds as described for the upper part Thickness—Most sections of the Abo in the Sandias of the Madera may be found hundreds of feet below the are faulted, covered in large part, or exposed in ways top of the Madera, but those considered to be in the that make measurement difficult or uncertain. However, transition zone are commonly more purplish red-brown calculations based on width of outcrop, together with in color as compared to the brick-red browns of the average dip, indicate thicknesses of 700 to 900 ft. Abo. Fossils—It is curious that so few fossils have been The top of the Abo is conformable with the overlying found in the Abo of the area. Some wood, in places Yeso and the contact is fairly sharp. In places, however, partly replaced by copper minerals, is found in the Abo the highest sandstone of the Abo and the basal sand east of Tijeras. By contrast, plants, amphibians, and stones of the Yeso are of very nearly the same texture reptiles have been found in the formation near Jemez and color, making selection of the boundary somewhat Springs and again in the Chama country farther north. difficult. Abo sandstone beds are usually deeper reddish Plants and reptiles are also found at the south end of the brown, lenticular, and in places intercalated with Manzano Mountains near Abo Pass. reddish-brown mudstone. The basal Yeso beds by tan and in places include a white contrast are more YEso FoRMATIoN sandstone. The sandstone is even bedded, nonlenticu 1909, 12) named lar, and is not intercalated with mudstone. Definition—Lee (Lee and Girty, p. the Yeso from Mesa del Yeso about 12 miles northeast outcrops are scattered. One belt Distribution—Abo of Socorro, but as measured the unit included the near Tijeras Canyon northward along the extends from Glorieta Sandstone and part of the San Andres Forma of the Sandias in a curving and broken low eastern flank tion. Needham and Bates (1943, 1658) redescribed against the Rio Grande trough p. belt to a termination the type section but in doing so began the section too Ridge. Also at the northern end of north of Montezuma high thus omitting the Meseta Blanca part of the miles west-southwest of Placitas a the Sandias several formation. This part was later recognized and the strip of Abo dips northward from the short, east-west section redefined (Bates and others, 1947, p. 27). Wood best exposures of the formation occurs uplift. One of the and Northrop (1946), mapping in the Nacimiento northeastward in a 6-mile strip at Tijeras and extends Mountains, subdivided the Yeso into the lower Meseta Creek and IJS-66. Lesser outcrop followed by Tijeras Blanca Sandstone Member and an upper San Ysidro around the Monte Largo horst block, areas also occur Member, and these two members are recognized and Mountain, and in the San around the base of South mapped in the Sandia area, despite Baars’ (1961a, p. Pedro Mountains. 196; l96lb, p. 115) contention that the term Meseta Lithology—The Abo Formation consists of an alter Blanca Member should be supplanted by De Chelly nating sequence that is dominated by reddish-brown Sandstone. mudstone and sandstone with minor beds of conglom The Meseta Blanca Sandstone Member appears to be erate and limestone, especially in the basal part. Where conformable on the underlying Abo Formation. It is exposures are reasonably good, as in the north-south distinguished from the Abo principally by its even outcrop band north of Montezuma Ridge, it may be beddedness, tan color, and finer clean sandstone. The observed that the lower part is marked by some upper contact with the San Andres Formation is variegation of lavender, purple, and gray in the prevail conformable to disconformable, and there is no inter- ing red-brown colors, whereas the upper sandstone and tonguing or transition zone. mudstone is more uniformly reddish brown (fig. 30). Distribution—Yeso distribution is similar to that of Sandstone occurs in sequences as much as 100 ft thick consisting of thin to thick beds that are commonly cross-bedded, and in thin-bedded sequences mixed with mudstone ranging from 50 to 200 ft thick. Locally white to light-gray sandstone ledges as much as 60 to 70 ft thick are present. Sandstone beds range from fine to coarse grained and locally are conglomeratic. White or light-gray sandstone tends to be fairly free of clay or mica, whereas the reddish-brown varieties are com monly argillaceous. Both types of sandstone are com monly feldspathic and calcareous. Mudstone is about equal in abundance to sandstone and probably consists of siltstone or silty and arenaceous claystone. Limestone beds are uncommon, mostly in beds less than 5 or 6 ft thick in the lower 100 ft of the formation. It is commonly nodular and dark gray to purplish gray. Thin and are BEDS. ROADCUT conglomerate beds occur locally in the Abo FIGURE 30—REDDIsH-BRowN AB0 SANDSTONE NORTH. usually composed of limestone pebbles. A 3-ft black ALONG US-66 BETWEEN JUNCTIONS NM-14 SOUTH AND shale, possibly marine, is exposed about midway in the WHITE BLEACH SPOTS ARE CHARACTERISTIC. 51

the Abo Formation with the principal outcrops in and 3) Upper member. The Gloneta Sandstone was first interrupted exposures along the lower eastern base of named by Keyes (1915, 257. 262) for exposures on the Sandias. Owing to its friability and p. low resistance to Gloneta Mesa in San Miguel County. Darton (1922, erosion, it forms poor outcrops except for p. the basal 181) subsequently lumped the Yeso, Glorieta, and San Meseta Blanca beds. The best exposures are in the Andres Formation (all the beds between the Abo sparsely vegetated terrain of the Town of Tejon Grant Formation and the Santa Rosa Sandstone) into the northeast of Montezuma Ridge. There are also reason now-abandoned term Chupadera Formation. He did ably good exposures along Gonzales Canyon in secs. this principally on the basis of exposures in the southern 13, 24, T. 12 N., R. 5 E., 3 to 4 miles northeast of part of Chupadera Mesa in Socorro County, which Palomas Peak. There are also reasonably good expo suggested to him that the three formations named by sures in both flanks of the San Pedro syncline east and Lee intertongued or changed lithologies laterally west of NM-14 in to the central part of the San Pedro such an extent as not to be distinct Grant. sequences super posed one above another. In central New Mexico the Lithology—The Yeso typically contains gypsum, three formations are everywhere distinct, and workers tan-brown sandstone, light reddish- or orange-brown before and after Darton have mapped them. An siltstone, and limestone or dolomite. In the Sandia area, important relationship that Darton had seen was inter- however, gypsum is not evident, However, as many tonguing of the San Andres and Glorieta, and this weathered veneers on sandstone or siltstone are gyp relationship has been defined by recent mapping in siferous, it may be that gypsum beds have been southeastern New Mexico (Kelley, 1971, 9-12). dissolved at the surface. In any event gypsum beds, p. if It has developed that Read (Read and others, 1944) present, were probably few and thin. The Meseta was right when he designated the Glorieta of the Sandia Blanca Sandstone Member consists of thick, even- country as part of the San Andres Formation. It is now bedded, tan-brown, light-orange, and white sandstone, known to be a facies of the lower (Rio Bonito Member) which is fine to medium grained and somewhat friable, part of the San Andres Formation in southeastern New with loose calcareous or argillaceous cement. Parallel Mexico (Kelley, 1972b, 73). The San Andres cross-bedding is common. p. Lime stone member of Read is probably the Bonney The upper Canyon San Ysidro Member is thinner bedded Member of southeastern New Mexico. than the Meseta Blanca and is friable, affording poor Not long after Read’s early work in New Mexico he exposures. It consists mostly of alternately fine- and began to suspect that the upper member of the San medium-grained sandstone, although some beds are of Andres, as he and his associates had mapped it, was very fine or even silt-sized grains. All the sandstone is likely a post-San Andres unit, and he was instrumental clean and lacks argillaceous or arkosic debris. In the in its later being formalized as the Bernal Formation middle of the section some sandstone is gypsiferous. (Bachman, 1953). It was not without planning that he Limestone beds from 3 to 8 ft thick are present, labelled the outcrops around the Sandias, and at Bernal, especially in the middle of the section. The limestone is “Pb” on U.S.G.S. Oil and Gas mv. Prelim. Map 21 commonly crinkly and contorted. It is light gray, finely (Read and others, 1944). Read also actively encouraged crystalline, and cavernous owing to ground-water solu the Roswell Geological Society (Tait and others, 1962, tion. Considerable chert is found in some beds. Current p. 504-505) to venture equivalency of the Bernal with and oscillation ripple marks are not uncommon. some part of the Artesia Group. Recent mapping in Thickness—The Meseta Blanca varies in apparent east-central New Mexico has shown this to be true thickness in part depending upon the degree of cemen (Kelley, 1972a, 15,), and that the Bernal tation; cementation results p. Formation in massiveness and resis should be used in the Sandia tance Mountains as a post-San to erosion of the Meseta Blanca sandstones, which Andres sequence. in turn affects the San Ysidro thickness. However, the The Glorieta Sandstone Member of the San Andres evidence of this is inconclusive owing to paucity of good Formation rests conformably, or disconformably with exposures. The thickness of the Meseta Blanca appears out gradation or intertonguing, on the Yeso Forma to range between about 70 and 150 ft and that of the tion in the Sandia area. The top of the San Andres is in San Ysidro between 250 and 400 ft. The total Yeso disconformity with the base of the Bernal. The Bernal is thickness in the area averages about 500 ft. too thin to be shown at the scale of the geologic map Age—No fossils have been found in the Yeso of the (map I) and has been included with the San Sandia area. Based on evidence Andres principally in south Bonney Canyon Member. Also owing eastern New Mexico to map scale the Yeso is probably of Leonar limitations the Gloneta and dian age. Bonney Canyon Members are mapped as one unit where dips are steep and the outcrops narrow, as along the prominent north-south SAN ANDREs FORMATION ridge through the Town of Tejon Grant and also in the east-west hogbacks west of Placitas. Definition—The San Andres was named by Lee Distribution—The San Andres. including the (Lee and Girty, 1909, 12, 29) for occurrences p. in the Glorieta, crops out around the Sandia Mountains in San Andres Mountains, and Needham and Bates (1943, strips closely parallel to those of the Abo and Yeso. The p. 1664) designated a type section at Rhodes Pass in the Glorieta and Bonney Canyon are resistant to erosion, same mountains. Read and associates (Read and others, both supporting prominent ridges. For example, in the 1944) divided what they thought to be the San Andres north-south ridge in the western part of the Town of Formation into three members, in ascending order: 1) Tejon Grant the Bonney Canyon limestone holds up the Glorieta Sandstone Member, 2) Limestone member, crest, with the underlying Glorieta down slope to the 52

the Permian is well represented in west and the Triassic Santa Rosa Sandstone down slope Early Triassic beds; New Mexico and the Early Triassic in to the east. southeastern Rosa or its equivalent Lithology—Two disti net lithologies characterize the Arizona beneath the Santa The top of the Santa Rosa is San Andres Formation in the Sandia area. The first is Shinarump in Arizona. with the Chinle. that of the Gloneta Sandstone, which is a clean, white, gradational and intertongues Rosa crops out in several medium-grained sandstone. The bedding is usually Distribution—The Santa the Sandias. One of these is an massive but with both parallel laminae and cross beds separate areas around around the Tijeras basin area internally, resulting primarily from minor grain size, interrupted elliptical belt in the ridge west of Cañoncito. cementation, and sorting differences. Texture varies with the best outcrops are narrow slices preserved from friable to well cemented; grains are mostly Also in part of this belt bounding the southeast side of u bro unded. along the Gutierrez fault s side of this belt The San Andres Bonney Canyon Member is com the Tijeras graben. On the northeastern in the Sandia Knolls area (2 posed of gray to black, very fine to fine-grained outcrops cross the graben Antonito along Frost Road). The limestone with some intercalated sandstone beds similar to 3 miles east of San of Santa Rosa outcrops is around the to those of the Glorieta. The limestone is thin to other large area of the Hagan basin. Because of the medium bedded and locally cavernous. Chert is not south and west sides these outcrops are particularly well uncommon, and the limestone is locally dolomitic. A sparse vegetation from the southern part of T. 12 N., few undeterminable fossils have been seen in the San exposed, extending and then northward through the Andres. R. 6 E., westward Town of Tejon Grant to the Rio The Bernal Formation consists principally of tan- western half of the near Arroyo de San brown, fine- to medium-grained sandstone with local Grande trough fault boundary outcrop occurs southwest of Placitas thin limestone beds, and is generally similar to the Yeso, Francisco. A small segment or ramp of the northern although gypsum is probably absent in the Sandia area. in the downfaulted Thickness—The Glorieta varies in thickness end of the Sandia Mountains. Santa Rosa typically consists of throughout the area from about 65 to 125 ft. Thickness Liihology—The buff, and reddish-brown sandstone of the San Andres, on the other hand, varies greatly white, light-gray, thick bedded. Slabby and flaggy bedding owing to erosion of its upper surface prior to deposition that is thin to and such sandstones have been quarried, of the Santa Rosa Sandstone, but the maximum is common Cañoncito. Lenticular bedding and thickness where Bernal is still present may be 180 to 200 especially near bedding are common. Grain size ranges ft. The Bernal has been removed in many places by irregular cross coarse with medium-grained sandstone pre-Santa Rosa erosion. Remaining outcrops are up to from fine to is also locally and variably ft thick. dominant. The formation 75 lenses and beds occur Age—On the basis of age determinations for San conglomeratic. Conglomerate lower part, and pebbles consist mostly Andres- and Artesia-equivalent units in southeastern principally in the and chert (Appendix 1). New Mexico the San Andres may range in age from late of limestone, sandstone, produces rusty and yellow- Leonardian to Guadalupian, and the Bernal would Weathering commonly and conglomerate, and both sand most likely be Guadalupian. Inasmuch as the thick colored sandstone beds are purplish or lavender Fourmile Draw Member of other parts of New Mexico stone and conglomerate is absent in the Sandia area the remaining part may be locally. is dominant, reddish-brown only Leonardian. Locally, the limestone of the Bernal Although sandstone and intervals up to several tens of contains small brachiopods. mudstone partings feet thick are interspersed within groups of sandstone ledges or elsewhere intercalated with thin-bedded, TRIASSIC reddish-brown sandstone units; mudstone intervals higher in the formation. The bound The only Triassic beds of central New Mexico and the become prevalent overlying Chinle is not everywhere an Sandia Mountains are of Late Triassic age. The ary with the transition of mudstone and sandstone; in the sequence is thick and divided into a thinner lower part alternating for example, the boundary is fairly abrupt. referred to as the Santa Rosa Sandstone and a thicker Tejon area, contact is more difficult to choose upper part termed the Chinle Formation. The Santa Elsewhere the of the gradational zone and because local Rosa Sandstone was named for the beds at Santa Rosa, because are present in the basal Chinle. east-central New Mexico (Darton, 1922, p. 183). The sandstone units wood, probably coniferous, is present locally Chinle Formation was named for exposures near Chinle Petrified in northeastern Arizona (Gregory, 1915, p. 102). Both in the Santa Rosa. thickness of the Santa Rosa varies formations are continental red-bed sequences of fluvial, Thickness—The partly to intertonguing, partly to flood-plain derivation similar in most respects to the considerably due from sandstone to shale at Abo Formation described above. variations in the gradation the top, and partly to the presence of some broad swales less SANTA ROSA SANDSTONE or channels at the base. Thicknesses range from than 100 ft in some places on the Tejon Grant to more Definition—The Santa Rosa rests unconformably than 400 ft, as near Cañoncito. on Permian San Andres or Bernal beds in the Sandia relief on the pre-Santa Rosa area; local and regional CH1NLE FORMATION surface of deposition is several tens to several hundreds Formation is completely of feet. Missing at this erosional and nondepositional Definition—The Chinle or is gradational with the surface are most Guadalupian and all Ochoan and conformable and intertongues 53

underlying Santa Rosa Sandstone. The top is discon massive-bedded sandstone; the Todilto formable with the overlying Entrada is a lacustrine or Sandstone (Juras lagoonal carbonate and an evapori sic). In Arizona, northwestern tic or possibly partly New Mexico, and in eolian gypsum; and the east-central New Morrison consists of arkosic and Mexico the Chinle is subdivided into tuffaceous variegated several members mudstone and sandstone of mixed but no such divisions are apparent in lacustrine and flood-plain the Sandia area. origins. The term Entrada Sandstone, at one time Distribution—Chinle outcrops for the most more part properly referred to as the Wingate Sandstone (Dutton, parallel those of the Santa Rosa. However, because of 1885, p. 136), was applied mistakenly by Gilluly and its greater thickness and less resistant lithology it forms Reeside (1926) in a press bulletin to Wingate beds poor outcrops and underlies a number of wide valleys. at Entrada Point in the San Rafael Swell, Utah. When Good exposures are seen along NM-14 between Ca the error was finally discovered the U.S. Geological Survey ñoncito and San Antonio, and the broad, much culti (Baker, Dane, vated alluvial and Reeside, 1947) ruled against the valley north and east of San Antonito is prior name underlain Wingate for what is probably New Mexico’s by a wide expanse of flat-lying Chinle in the grandest formation. broad San Pedro syncline (map 1). It also underlies Only shortly prior broad valleys along to the change to Entrada U.S. San Pedro and Gonzales Creeks in Geological Survey geologists the northern part had extended the Wingate of T. 12 N. in R. 5, 6 E. Farther north nomenclature to strata down Gonzales near Tucumcari, New Mexico Creek, the unit is greatly restricted and (Dobrovolny and Summerson, cut out by faulting, but 1946), to beds which still farther north in the Tejon only miles away in Union Grant and San Felipe County had been named Indian Reservation the outcrop Exeter by the Survey widens and (Lee, 1902, p. 45-46). Recently the soft Chinle is well exposed in dissected Mankin (1972, badlands. p. 91) recommended the abandonment of the term Entrada in northeastern New Lirhology—The Chinle consists predominantly Mexico in of favor of the earlier, long-established term Exeter, reddish-brown mudstone with numerous local and thin this move has the concurrence of the New sandstone units within the sequence. Across Mexico the badland Bureau of Mines and Mineral Resources exposures in the Tejon Grant (Kelley, 1972a, there is a slight color 8, 22, p1. 2). The term difference between the p. Exeter could with much mudstone of the lower and justification be applied upper parts also to the old Wingate unit in of the formation. The lower part is charac central New terized Mexico including that in the Sandia by variegations of lavender, blue, light gray or Mountains. greenish gray, and reddish brown. The upper part The Todilto (Gregory, 1916) was named from (about two-thirds) of the sequence is more uniformly expo sures at Todilto Park, McKinley County, New tan brown to reddish brown. However, it is not uncom Mexico. Although first applied to the limestone lower part it has mon to find olive-drab and greenish-gray mudstones in been extended to include the thick overlying gypsum many places. Thin nodular limestone beds are present which is widespread in northwestern New Mexico. locally in the upper part of the formation. In the Tejon As used in much of New Mexico it is equivalent to the Grant area there is also a flaggy sandstone unit, 20 to 30 Wanakah Formation (Baker, Dane, and Reeside, ft thick, at the top of the formation. Although 1947). the The type Morrison is at Morrison, Colorado lithology is somewhat different (Eld the position is ridge, 1896). The unit has been equivalent to the Correo traced widely through Sandstone Member mapped out the Rockies from Montana by Kelley and Wood to New Mexico and (1946) along the base of Mesa from the Colorado Gigante north Plateau to the High Plains. Lee of Correo on the Santa Fe railroad (1902) first (Appendix traced the Morrison into northeastern New I). Mexico. Thickness—The Chinle thickness is difficult to determine because of poor exposures from which atti ENTRADA SANDSTONE tudes must be measured and the broad expanse of Definition—In the Sandia area the Entrada lies outcrops. The fine exposures in the northern part of the disconformably on the Chinle Formation and in places Tejon Grant (map 1) are complicated by faults which with minor erosional irregularity. It is overlain discon both thicken and thin the section. Based on dips and on formably to conformably by the Todilto Formation. In width of outcrop along San Pedro Creek in secs. 9, 16, the central Colorado Plateau it overlies the Carmel T. 12 N., R. 6 E. and across Frost Creek in sec. 28, T. 11 Formation and underlies the Curtis Formation, both of N., R. 6 E., our calculations indicate that the Chinle is which can be dated as Late Jurassic on the basis of about 1,300 to 1,400 ft thick. marine fossils. Elsewhere in Arizona and New Mexico it Apparently no fossils have been reported from the may rest on the Navajo Sandstone, Kayenta Shale, or Chinle Formation in the area. Elsewhere in New Wingate Sandstone as has been suggested for exposures Mexico Upper Triassic strata have yielded numerous at the great Wingate cliffs east of Gallup. In the plants, freshwater bivalves (Unio), amphibians, and northeastern part of the San Juan basin the Entrada is reptiles of several types, including small dinosaurs. overlain by Summerville beds included in the Morrison. JURASSIC In central eastern New Mexico the Entrada rests on a Wingate-like sequence The Jurassic of red beds which is referred to rocks of the Sandia area consist, in as the Redonda ascending Formation (Dobrovolny and Summer order, of the Entrada Sandstone, Todilto son, 1946). Formation, and Morrison Formation. They are well Distribution—The Entrada crops out in three places developed and exposed in several places. The three are in the Sandia area, the largest and best exposure lying of contrasting lithologies and origins. The Entrada is a in a long curving strip around the southwest side of the 54

gypsum unit overlies the limestone and in places either 1-lagan basin. A second exposure is a short east-west intertongues with the limestone or contains similar thin strip in the downfaulted end of the Sandia uplift west of beds of limestone. Current usage of the term includes Placitas. The other exposure is around the northeast end lithologies. The contact of the Todilto with the of Tijeras basin, south and east of San Antonito. The both underlying Entrada is sharp. although some alternation best exposures are those in the Tejon Grant and the of sandstone and limestone laminae through I or 2 ft is San Felipe Indian Reservation (fig. 31) along Tonque common. The Todilto is overlain by the Morrison. in Arroyo at the northern edge of the mapped area. The places disconformably. and in places by intergradation unit is also readily seen in the gully just west of the old with the lowest Morrison sandstones through a few Ideal Cement Plant gypsum quarry and along NM-14 or 2 ft. east of Cañoncito. inches to I one-half mile Todilto outcrops in the Sandia Litho/og—The Entrada is predominantly a buff. Distribution—The area are the same as those of the Entrada described tan, or bleached white sandstone. It is typically mas above. Along the northern side of the Tijeras basin in sively bedded and commonly holds up cliffs. It is fine to sec. 19. T. II N., R. 6 E. a round sinkhole has formed medium grained. consisting almost entirely of fairly well over poorly exposed gypsum outcrop. As the forma sorted subangular to subrounded quartz. In places a tion is thin in most places, especially where the Gypsum “floating” rounded coarse grains are present. Large- member is absent, it nas been included with the Entrada scale eolian cross bedding is common. One or two thin on the geologic map (map I). reddish-brown mudstone units occur locally in the lower Lithology—The Todilto in most places comprises a part of the unit. The white or light yellowish colors are thin lower Limestone member and a thicker upper found in the upper part and appear to be a ground Gypsum member. The Limestone member consists of water bleaching effect, as the white-to-tan color contact fissile, papery thin laminations of gray to dark-gray in places runs across inclined crossbeds. The sandstone limestone, especially in the lower part. Distinctive is slightly to highly cemented, and cement consists features of the limestone are the laminated bedding and mostly of calcite. petroliferous or fetid odor from freshly broken Thickness—The thickness ranges from about 60 to the surfaces. The lower few feet is usually a transitional 120 ft in the Sandia area with the greater thicknesses in mixture of Entrada-like sandstone and Todilto lamina the vicinity of Hagan basin. Thicknesses in wells drilled tions. The upper contact with the gypsum is usually by Southern Union Production Company along the In places the Limestone member consists of 4 southern part of Tijeras anticline ranged from 70 to 90 sharp. distinct parts as shown in a well exposed section in the ft. Differences are partly due to irregularities both on ¼ of projected sec. 6, T. 12 N., R. 6 E. It is the Chinle surface and, in some instances, at the top of NW by massive white Entrada Sandstone and the Entrada. Where the Todilto is absent, thinner underlain by a 50-ft section of the Gypsum member (fig. sections are due to pre-Morrison erosion. overlain Age—The Entrada can be accurately assigned to 33). with the fossil- the Late Jurassic owing to gradation Thickness the marine fossils bearing Todilto in New Mexico and Bed No. Description ft Carmel and overlying Curtis on the of the underlying 4 Limestone: gray. massive breccia of laminae and irregu Colorado Plateau. lar algal forms: porous with fragments up to nearly O.Sinch Ii T0DILTO FORMATION 3 Limestone: gray. crinkly laminations 6 even laminae 1.5 first applied to 2 Limestone: gray to black, very Definition—The term Todilto was limestone: buff to gray, even parallel New 1 Sandstone and the distinctive limestone outcrops at Todilto Park, laminae: sandstone is dominant and fine-grained 2.5 Mexico. However, through northwestern New Mexico, adjoining Colorado, and in the Sandia area a thicker

:

is. FIGURE 33—TODILTO OUTCROP ALONG GONZALES CREEK. 6 E. EXPOSURE IN NW SEC. 6 (PROJECTED), T. 12 N., R. 31—ENTRADA SANDSTONF AND TODIL 10 FORMATION. FIGURE ENTRADA SANDsTONE, LOWER LEFT: PICK IS ARR0Y0. WHITE UNDERLYING WHITE TELEPHOTO VIEW FROM WnT SIDE OF TONQUE BED: PITTED. KNOBBY OUTCROP IS LOCAL SHALE IS REDDISH ON CRINKLY LIMESTONE MIDDI.E ENTRADA. ABOUT 80 FT THICK. CHINLE INTERVAL. ALGAL LIMESTONE MOUND. BROWN. TODILT0 LIMESTONE IS FLAGGY 10-FT 55

A—UNIT No. 2 OVERLAIN BY UNIT No. 3. S0UTHwFST WALL OF PIT B—UNIT No. 2. WEsT WALL NEAR ENTRANCE TO AS EXPOSED OCToBER, 1972. PIT.

C—UNIT No. 2. EAST WALL NEAR ENTRANCE TO PIT. D—UNIT No.4. EksT WALL OF PIT. FIGURE 32—T0DILT0 GYPSUM AT SAN FELIPE QUARRY T0NQUE ARR0Y0.

The lower 3 beds are widely present in the member, but the upper one is local and occurs in low, broad mounds. Thickness Bed No. Description In the above exposure the outcrop length is about 100 ft ft. Morrison Formation Todifto Formation The Gypsum member consists almost entirely (Total thickness) 189 of 6 Gypsum: white and pink: large-scale massive gypsum with limestone beds mottling: intercal I to 4 inches thick, ated with two or three, 2- to 3-inch gray limestone especially in the upper part or locally at the top. The beds; 4- to 6-inch carnelian bed at top. 16 gypsum in good exposures is both thin bedded and 5 Gypsum: white, mottled with spider-web limestone lines lenticular or nodular, producing a “chicken-wire” through large nodules, spindles, and cannon ball-sized gypsum masses; mottled pattern with distorted gray limestone. Small most limestone lines are inclined more steeply eastward than the parallel grains of carnelian chalcedony may beds, also be found in the as though they were foresets. 45 gypsum, particularly near the top. 4 Gypsum: white; parallel-banded gypsum and limestone The following section (fig. 32) was measured across couples: gypsum layers 0.1 to 5 inches; limestone layers 0.01 to 0.6 the gypsum quarry on the San Felipe Indian Reserva inch; 40 to 50 couples per ft (fig. 32D). 57 tion at Tonque Arroyo (SW /4 sec. I, T. 13 N., R. 5 E.). 3 Gypsum: white; nodular with crude banding Anderson and averaging Kirkland (1960, p. 38-40) have shown about 2.0 to 2.5 inches thick, but ranging from I to 6 that the laminations in the gypsum beds form annual inches; “chicken-wire” pattern of reticulated black sets or varves consisting of “repetitions limestone 0.02 to 0.2 inch thick; some diagonal of three lam- limestone mae: light-brown microcrystalline laminae cross the banding (fig. 32A). 44 limestone, thin straw- 2 Gypsum: white; with limestone laminae colored organic material, more regular and a discontinuous layer of than in no.3; limestone laminae 0.01 to 0.1 inch thick: clastic grains. These three laminae constitute a cycle gypsum wavy bands 0.25 to 1.0 inch but averaging about that is repeated an average of 2,200 times per foot of 0.5 inch; 20-25 couples per ft (figs. 32B, C). 22 Limestone: black and gray section.” At the transition into the overlying gypsum a laminated: overlies the Entrada Sandstone. 5 “lamina of gypsum is added to the three-fold varved sequence” and “the four-fold cycle persists for several diminished in the gypsum, but in feet.” Laminae of many places carnelian dark-brown bituminous limestone jasper grains can be found, persist throughout and these are probably a the gypsum unit but are greatly chemical precipitate accompanying distorted evaporitic precipita - by recrystallization. Clastic grains are greatly tion of gypsum. 56

1944, 966) and Dead Mans Peak The Todilto basin was a large lake which may have Mountain (Stokes, p. All these units possess lithologies connections across subaqueous bars with the Upper (Swift. 1956, p. 43). had and in places they may Curtis sea to the northwest. Calcium sulfate for characteristic of the Morrison Jurassic with the Morrison. Also, in the evaporitic gypsum may have come partly from the grade into or intertongue their equivalents have been included in sea but mostly from streams from surrounding uplands places they or (Anderson and Kirkland, 1960. p. 45). the Morrison. years the Morrison of west-central New Fossil fish have been found in the limestone member In recent been divided (in ascending order) into the in peripheral parts of the basin and Anderson and Mexico has Shale Member, Westwater Canyon Sand Kirkland 44) believe that they likely lived in streams Recapture (p. and Brushy Basin Shale Member lying or areas of nearly fresh water near the mouths of stone Member, the Summerville Formation and Bluff Sand streams feeding the lake. between the Dakota above (Hilpert, 1963, 7). Thickness—The Todilto Limestone member ranges stone below and p. area, especially in the Hagan basin, in thickness from 5 to 20 ft. The Gypsum member In the Sandia of all the above, down to the Summer where present ranges up to about 190 ft. The thickest representatives may be present, but they have not been gypsum sequence occurs along Tonque Arroyo in sec. ville beds, separated, thus the Morrison is mapped and 12, T. 13 N., R. 5 E. This thickness is greater than any effectively as a unit between the Todilto at the base and other known outcrop in the surrounding region. The top described at the top. of the Todilto is commonly eroded, and it may be that the Dakota Distribution—The Morrison outcrops closely paral the Tonque exposure is one of the very few original full described above for the Entrada and Todilto. sections. Several miles to the southeast the Gypsum lel those especially good exposures east of Tonque member thins markedly and the outcrops along Gon There are in sec. 12, T. 13 N., R. 5 E., but a number of zales and San Pedro Creeks, although poorly exposed, Arroyo exposures are found throughout the outcrop belt appear to be 50 ft thick or less. Around the Tijeras basin good the west and south sides of Hagan basin. the gypsum is only locally present; soil and vegetation around different and significant exposures may be cover are heavy in the area and the only known surface Somewhat the northwest side of Tijeras basin, occurrence is the short outcrop, 50-75 ft thick, at the found around the ridge east of the abandoned Ideal old Ideal Cement Company gypsum quarry just east of particularly in gypsum quarry in sec. 36, T. 11 N., NM-l4 in NW, SW sec. 36, T. II N., R. 5 E. However, Cement Company questionable outcrop with some Chinle Southern Union Production Company in 1964 drilled at R. 5 E. A small lies west of the Sandias in sec. 10, least one well through the Todilto in which the total shale and sandstone near the Juan Tabo road. This outcrop thickness of both members was 150 ft. Gypsum outcrops T. 11 N., R. 4 E. Chinle beds were thought to be all in the Tijeras basin are near the southern terminus of and the associated and others (1944) and Galisteo by the gypsum as it is known west of the Rio Grande and Chinle by Read Galisteo beds have lithologies in the Colorado Plateau, and they are the southernmost Kelley (1963). Although in various parts we believe designation Todilto gypsum outcrops in eastern New Mexico, there of all these beds fault slices of Morrison and Chinle is being none in the Todilto outcrops of the Tucumcari of this inlier as basin. more likely. lithology in the Sandia area is Although the prevailing concept for the origin of the Lithology—Morrison units of the Hagan basin (Appendix Todilto gypsum is by evaporation in a desiccating lake, variable. Matching in the Tijeras basin is impossible. The Tanner (1972, 58) has made strong points for a more 1) with those p. dominantly of greenish, reddish, complex derivation. He favors a combination origin as a sequence consists light-gray mudstone, claystone, and silt- subaqueous bar and dunes, possibly with alternations of lavender, and with white, buff, and orange sand the two conditions. However, he believes that some of stone interbedded Variable thin beds of limestone and conglom the forms as observed today may have been modified by stone. found in the middle and upper parts. Much of ground-water solution. Certainly units 3 and 5 at the erate are is slightly arenaceous and commonly Tonque quarry differ so markedly from unit 4 as to the claystone The sandstone is friable and consists of require quite different modes of origin. bentonitic. medium to coarse grains of Algae have been the only reported fossils from the subangular to subrounded lesser feldspar. The conglomerate is in Todilto of the area; elsewhere in New Mexico, this quartz and and beds with fragments of quartz, formation has yielded at least two genera of fishes, irregular lenses limestone, and altered fine-grained or vitric ostracods, and aquatic insects. chert, dense rhyolitic volcanic rocks. White kaolin fragments and MORRISON FORMATION kaolin cement are common especially in sandstone of formation. The limestone is light Definition—Between the lacustrine Todilto or the the upper part of the fine grained, and nonfossiliferous. Entrada Sandstone and the Dakota Sandstone in New to medium gray, in the middle mudstone or claystone units Mexico there is a diverse sequence of mudstone, Occasionally silicified beds that may be silicified sandstone, and conglomerate of variegated reds, are thin, dense, of the sandstone beds could be tuff or browns, greens, and grays that is generally referred to as air-fall tuff. Many tuff. the Morrison. However, in some places and especially in reworked water-laid the Morrison is an erosional disconform surrounding regions a number of units both at the The top of that there was some mild broad bottom and the top have been removed from the ity, and it appears accompanying erosion after Morrison Morrison as separate formations. Chief among these at warping and before the laying down of the basal the base have been the Summerville and Bluff; at the deposition and (fig. 34). This accounts for most of the top are such units as the Purgatoire (Stose, 1912), Cedar Dakota sands 57

considerable differences in thickness observed in the 1-lagan area, and in the Gonzales Creek area divergence of a few degrees can be observed between some high Morrison ledges and the Dakota basal beds (fig. 35). Some of this disturbance and erosion appears to have occurred in latest Morrison time, and the uppermost sandstone beds show some internal discordance, as in the prominent exposures on the west side of San Pedro Creek. Thickness—Harrison (1949, p. 100-102) measured 730 ft of Morrison east of Tonque Arroyo in sec. I, T. 13 N., R. 5 E. It is about 500 to 550 ft thick in the Placitas area. In the Tijeras basin exposures are usually poor with either the top or bottom obscured. Furthermore, the upper part consists of sandstone beds that have been confused with those FIGURE 35—MAssivE UPPER of the overlying Dakota. On the MoRRIsoN BEDS CAPPED BY DARK LEDGES OF DAKOTA basis of wells drilled by Southern SANDSTONE. SAN PEDRO CREEK, SEC. 5, T. Union Production N..R.ÔE. 12 Company on Tijeras anticline, and allowing for some thicknesses excluded into the Dakota, we estimate a mation. Their combined thickness is nearly as great thickness for the Morrison of at least 760 to 915 as ft. the combined thickness of all the previous Mesozoic Age—The Morrison of the area has not yielded and Paleozoic formations. They are marine and inter- determinable fossils. Elsewhere in New Mexico, several tongued marine and nonmarine flood-plain beds depos genera of dinosaurs have been found, especially west of ited in the Rocky Mountain geosyncline during Middle Albuquerque near Correo and Mesa Gigante, near and Late Cretaceous time. The sediments consist mostly Acoma, and near Grants; some of the bones are of shale and sandstone, some coal, and minor con impregnated with uranium minerals; both perminer glomerate. The total thickness is about 4,700 ft. alized wood and dinosaur bones have been found in some of the uranium mines (Northrop, 1972, p. 6 1-62). DAKOTA SANDSTONE Although age of the Morrison has generally been Definition—The Dakota type considered to be Late Jurassic, it was earlier thought locality is near Dako to ta, Nebraska (Meek and Hayden, be Early Cretaceous (?) (Darton, 1928). In 1862, p. 419-420). places, at This unit has been mapped least, the Purgatoire seems to have been separated and extended widely from through the High Plains, Rockies, the Morrison on the grounds that it is Early Cretaceous and Colorado Plateau from Montana to New in age rather than on lithology. In Mexico. Winchell (1875, 32) the Tucumcari basin designated it a p. this certainly appears true, group. Later several sandstone units even though the Mesa Rica separated by sandstone beds are similar shales were included. Some of the lower to those in the Morrison, and units had the overlying Pajarito varied lithologies more characteristic of the claystone and sandstone are all Morrison typical of the Morrison. (Lee, 1927, p. 17-23) and were subsequently At least part of the uppermost (Waage, Morrison may be 1955, p. 15-49) separated from the Dakota. Early Cretaceous in the Hagan basin. Nevertheless, there are many places where several Dakota sandstone units separated only by thin intervals CRETACEOUS of gray or black shale justify inclusion in the Dakota. Elsewhere, The Cretaceous rocks of the Sandia area consist of the especially if the intervening shale is thicker, the second Dakota Sandstone, Mancos Shale, and Mesaverde For and successive units may be given separate names or referred to as Tres Hermanos Sandstone (Herrick, 1900c) and included as members of the Mancos Shale or the Graneros Shale. Owing to transgressive spreading over so wide an area, the basal sandstone unit and the age of the formation are not everywhere the same; because of local changes in near-shore sediment from mud to sand, coupled with minor seaward-landward shifts of the shoreline, the Dakota sandstone is not a continuous sheet or layer. In some places the intervening shale units of the Dakota rest on the Morrison and Morrison

— shales then _3T : are included with at least the first succeeding shale unit in the Dakota proper, as in the Galisteo basin not far northeastward of the Hagan basin (Stearns, 1953b, p. 965). The Dakota overlaps - the Morrison on a broad regional FIGURE 34—DIScONFORMABLE scale in the Sandia area, CONTACT OF DAKOTA SANDsToNE but to the south it LEDGES ON FRIABLE, gradually oversteps PEBBLY WHITE SANDSTONE OF MORRISON formations as old as the Abo in FORMATION. MORRISON southern CONTAINS MANY FRAGMENTS OF BLEACHED New Mexico. The upper contact OR is grada KAOLINIZED FELDSPAR. IN SW SEC. (PRoJECTED), tional, 31 T. 13 N., R. the Dakota intertonguing with the Mancos 5 E. NEAR GONzALEs CREEK. Shale. 58

area. Distribution—Dakota Sandstone outcrops follow Hagan basin and also from the Cerrillos-Madrid pls. 62-63) was closely those of the Morrison along the south and west Roland W. Brown (1939, p. 253-254, warty or tuberculate sides of the Hagan basin. The formation is especially the first to suggest that these but burrows of some prominent around the northeast end of the Tijeras basin structures were not seaweeds were droppings of the and in a short, steep, faulted hogback along the organism and that the tubercles the burrow. The tuberculate southwestern border of the Tijeras graben, just east nI animal that inhabited colloquial name “fossil corn San Antonio. In the Placitas area thin units of Dakota appearance gave rise to the the burrows of as small outcrops in three separate fault blocks. cob.” Weimer and Hoyt(1964) described occur major Say. They Lithology—The Dakota consists dominantly of the living ghost shrimp, Callianassa crustacean is about 4 inches sandstone but contains smaller beds of black shale, note that this decapood diameter; it is a permanent especially in the upper part. Sandstone beds are thin to long and 0.5 inch in rarely being seen on the thick or massively bedded with local small cross beds. It inhabitant of its burrow, explain the common name “ghost varies from white to light grayish or buff and is surface, which may are 0.1 to 0.4 inch in diameter commonly stained yellowish to rusty brown on blocky shrimp.” The burrows enlarge downward to as much as weathered outcrops. The sandstone ranges from near the surface and Some burrows extend medium to coarse grained and contains thin beds of 0.6 to 0.9 inch in diameter. are normal to the surface but conglomerate at places in the basal part. Beds are well downward 3 to 6 ft; most horizontal; burrows may cemented, weathering out in angular ledges or hillside some are diagonal, and some scree; surfaces of weathered outcrops are also com branch. burrows are somewhat monly rough and pitted. The angular aspect of its The Dakota Sandstone and Mesaverde For weathered outcrops is in marked contrast with the smaller than those of the Mancos Fossils). It is an interesting rounded, somewhat spheroidal, outcrops and boulders mations (Table 4, Trace name, that Say in of the underlying friable Morrison sandstone beds. coincidence, regarding the specific near Jacksonville, Thickness—The Dakota Sandstone in the Hagan 1818 named the shrimp he collected major and that Lesquereux more basin and at Placitas is unusually thin but variable. It Florida, Callianassa (1872) named the supposed may be as thin as 5 to 10 ft or as thick as 40 to 50 ft in than half a century later major. Currently the trace local areas, but most commonly it is 20 to 25 ft thick. fossil seaweed Halymenites Ophiomorpha major. The top part is difficult to measure owing to stripping in fossil is known as Reeside (1952, p. 1028, note 9) wrote: hogbacks where dips are 25 to 35 degrees. Lee (Lee and Cobban and in this Knowlton, 1917, P. 203) observed variation between 15 The relations of the sandstone designated “Dakota” (1953b, 964) found a range of 6 INew Mexicol and many other areas to the typical Dakota and 50 ft, and Stearns p. Iowa, are not from normal sandstone on the Missouri River near Sioux City, to 25 ft. The variation probably results usage of the name may cover beds of from well understood. Such differences of accumulation on a uniform surface, both Early and Late Cretaceous ages, though it was apparently some filling of swales in the Morrison surface, or from the intent originally to include in the Dakota beds no older any apparent local additions of the basal sand of the than the European Cenomanian. There is much doubt that are Late Cretaceous. overlying Mancos. Around Placitas the Dakota is sim part of the typical exposures ilarly thin. In the Tijeras basin area, on the other hand, However, several years later, in discussing the Dakota the Dakota is considerably thicker, probably because of Sandstone of the eastern side of San Juan basin, Dane appear to sandstone additions at the top. Thicknesses (1960, p. 67) stated that 200 ft. Massive sandstone of the approach 150 to writer, fossils closely diagnostic of underlies the Dakota, In so far as known to the Morrison, which immediately age have not been found in the Dakota of the eastern San Juan in picking of some the Dakota sandstone of Dakota; . of may be mistaken for the Basin . . It seems likely that most well-log tops in the Tijeras anticline the Morrison the eastern San Juan Basin is of Late Cretaceous age and may of to have been picked 150 to 200 ft low, thus be entirely younger than any part of the Dakota sandstone appears southeastern Colorado, much, much as 150 to 200 ft to the Dakota. northeastern New Mexico and adding as . of Early Cretaceous age . . The two feature if not all, of which is Fossils and Age—A peculiar and distinctive areas may well have been separated by an erosional barrier 15 of the Dakota Sandstone is the presence in many places to 25 miles wide trending southward along the 106° meridian of warty or tuberculate cylindrical concretions known as toward central New Mexico. (fig. 36). The cylinders are generally Ophiomorpha Thus, the Sandia Mountains area is critically located; to the bedding and range from 0.25 to 0.5 nearly normal the 106° meridian lies only a few miles east of our map and nearly a foot in length. Ophiomor inch in diameter area, between Cerrillos and Galisteo. pha was originally named Halymenites major by Les a century ago; see Lee and quereux more than MANcos SHALE Knowlton (1917, p. 242) for description and synonymy. Shale was named by Cross “One of the most abundant and widely distributed fossil Definition—The Mancos Mancos in southwestern organisms known in the Rocky Mountain region,” it (1899) for exposures near thick black marine shale was interpreted as a form of algae or seaweed. It was Colorado. It is typically a and Mesaverde (above). early thought to indicate marine conditions, and between the Dakota (below) are conformable, generally to indicate shallow-water and near-shore The lower and upper boundaries intertonguing from place to conditions. It is most abundant in the higher beds of the being both gradational and from the western sources or Upper Cretaceous but is found in the Colorado Group place. Tongues of sandstone sources in places have made it as well as in the Montana Group. Halymenites major limestone from eastern Mancos into members. has been reported in our area from sandstones of both possible to divide the marine and only one or two thin the Mancos Shale and Mesaverde Formation of the Few persistent sandstones 59

., ;II iE ‘1.

A—L0NGITU DINAS. AND TRANSVERSE SECrIONS (sCALE, 6 INCHES). B—TUBERcuLATE MOLD (KNIFE, 3¼ INCHES).

C—MoLDs AND CORE, NUMEROUS LICHEN (HORIZONTAL LINE D—MoLos AND CORES SHOWING BIFURCATION (vERTIcAL LINE SEGMENT NEAR TOP CENTER. 1 INCH). SEGMENT NEAR TOP CENTER, 1 INCH). 36—Ophiomorpha FIGURE BURROWS IN DAKOTA SANDsToNE. OuTcRops LOCATED IN NORTHEAST PART OF TIJERAS COAL BASIN IN SE SEC. 32. T. I I N., R. 6 E. SOME BURROWS ARE PARALLEL OR DIAGONAL TO BEDDING, BUT MOST ARE NORMAL TO BEDDING. NOTE WARTY OR TUBERCUL.ATE APPEARANCE.

limestones are traceable in the Mancos of the Sandia amphitheater valley eroded in the Tijeras anticline area and, therefore, no members or subdivisions are in secs. II, 12, T. 10 N., R. 5 E. Some additional narrow designated. However, equivalents of such units as the outcrops are present along NM-14 near San Antonio. Graneros, Tres Hermanos, Greenhorn, Carlile, Juana Lithology—The Mancos Shale is predominantly Lopez, and Niobrara are present and recognizable, black to gray and, locally, brown. The shale is cal especially in the Hagan basin area (Stearns, 1953b, p. careous to varying degrees and locally carbonaceous 966-969; Lee and Knowlton, 1971, 203). or p. The lower siliceous. It is quite fissile and commonly laminated part of the Mancos, including the Graneros Shale, Ties with siltstone or fine-grained sandstone. Hermanos tongues, Graneros Secondary Shale, and Greenhorn gypsum in the form of selenite Formation, is considered or satin spar is locally transgressive (Coates and present (Appendix 1). Kauffman, 1973, 965-966). p. The highest Greenhorn The Mancos sequence of the and Carlile Shale are considered Hagan basin area differs regressive in origin, from that of Tijeras basin in having but the Juana Lopez, which more thin sand is well developed in the stone beds or sandy zones and Hagan area where exposures in intertonguing more are good, and the upper with the Mesaverde Formation. Mancos shales are transgressive. At Tijeras, Mancos underlies a smooth valley in which there are essentially Distribution—The Mancos occurs in a wide belt no low ridges or knolls to indicate the presence of curving from westward to northward trend through the sandstone tongues. A few thin sandstone units inter- Tejon Grant (fig. 37), but much of it is covered by bedded with shale occur just above the main Dakota terrace gravel and valley alluvium. In the Tijeras basin ledges, but these are easily included in the Dakota the Mancos underlies a nearly circular valley around Sandstone. The upper 50 to 75 ft of the Mancos consists the basin between the Dakota or other resistant beds on of intercalated thin sandstone and shale beds which the outer side and the Mesaverde ridges on the inside. It grade into the thick basal Mesaverde ledges. Exposures is mostly covered by alluvium and the only outcrops of in the Tijeras basin are by no means as good as in the note are on slopes up to the overlying Mesaverde or in a Hagan basin, but gullies do expose parts of the section, few small gullies cut into the Mancos valley near Tijeras especially along the southeast side; no consistent sand Creek. The best partial outcrops occur around the stone units are seen. Locally a thin limestone bed is 60

marine fossils; perhaps the Mancos top exposed in the lower part of the Mancos which may or above contain at the base of the next higher may not be a Greenhorn equivalent. should be chosen ledges that consist of terrestrial coal-bearing In the Hagan basin where exposures are better sandstone and in so doing increase the thickness of the several thin sandstone horizons are observable and two shale beds by about 500 ft (Harrison, 1949, p1. 1). of these have been mapped (Harrison, 1949, pl. 1). One Mancos Thickness—Definite thicknesses for the Mancos are of these, about 135 ft above the base of the Mancos, is to obtain for either the Tijeras or Hagan basins, 25 to 50 ft thick and such sands have been termed Tres difficult poor exposures and to indefinite or inter- Hermanos. Elsewhere, as along Gonzales Creek, Tres owing to boundaries, particularly with the Mesaverde Hermanos-type sandstone beds are thin or absent. Local tongued In the Tijeras basin lack of outcrops and exposures show them to be no more than 5 to 10 ft thick Formation. change of attitude across the formation make measure or only thin-bedded intercalations with siltstone or or calculation uncertain. Along the northern side shale. Another sandstone, 650 to 700 ft above the base, ment the basin, averaging of available dips at the top of the is 18 to 20 ft thick and may be the Juana Lopez of Dakota and base of the Mesaverde ledges yields a Sandstone (Rankin, 1944, p. 19-20). A sandy limestone thickness for the Mancos of 1,400 to 1,500 ft. unit about 8 ft thick crops out about 480 ft above the calculated Tijeras anticline along the southern side of the base. A very fossiliferous concretionary brown silty In the well spudded in the middle of the Mancos gives calcareous zone 1 to 2 ft thick was noted about 480 ft basin, a top of the Dakota of 887 ft. Surface above the base by Harrison. The two thin sandstone a depth to the from the well collar across the east limb Units are tongues which locally divide the Mancos into measurements to the base of the Mesaverde yield the three shale units, especially south and west of Hagan. of the anticline and these two measurements—887 north in the Tejon Grant the sandstone beds remaining thickness, To the a total thickness for the either die out or are covered and not mappable. and 573 ft, respectively—suggest The calcareous bed which Harrison (1949, p1. 1) Mancos of 1,460 ft. Hagan, Harrison (1949, 118-119; p1. 1) noted at about 480 ft above the base of the Mancos may West of p. section across an outcrop width of about 0.5 be the Greenhorn zone which Stearns (1953b, p. 966, measured a totaled 1,304 ft in thickness between the top 967) stated was represented by “no more than one mile which and the base of a sandstone about 512 ft limestone” bed less than 1 ft thick in the Tonque area, of the Dakota the Cano Sandstone of Stearns (1953b, p. 971), but Stearns gave only 200 to 250 ft for the underlying below his Mancos thickness thinner by 512 ft. If Graneros Shale. and this left base of the Cano, Harrison’s measured The upper sandstone horizon at 650 to 700 ft above adjusted to the be 1,816 ft. Based on cursory inspection the base of the Mancos is probably the Juana Lopez, Mancos would of fossils in the Hagan Mancos Reeside thought the and Stearns (1953b, p. 968) has suggested member be thickened by faulting (C. B. Read, status and usage of the term, Juana Lopez Member, section to communication). because of variations in lithology including limestone personal in Mancos Shale are listed in Table 4 and shale as well as sandstone. Rankin (1944, p. 12) Fossils found discussed with other Cretaceous fossils after believed that the Juana Lopez is very near the top of the and are Formation. Carlile. However, as is common in central New Mexico Mesaverde of the Carlile with the overlying Nio the boundary MEsAvERDE FoRMATIoN brara Shale is not readily identified. known as Harrison (1949, 1) chose the top of the Mancos at Definition—The sedimentary sequence p1. Verde the base of the prominent sandstone which Stearns Mesaverde gets its name from exposures at Mesa (Holmes, (l953b, pl. 1) termed Cano member and used as the near Mesa Verde National Park in Colorado into three base of his “Upper Mancos shale” near Hagan. Stearns 1877, p. 245-248). He divided the formation the base did not cite Harrison’s thesis and probably was not parts: 1) a massive sandstone sequence at aware of it, although he did cite his own unpublished termed the Lower Escarpment, 2) a middle coal-bearing at manuscript. The Cano and the thick shale interval shale sequence, and 3) a massive sandstone sequence the top termed the Upper Escarpment. Later Collier used formal (1919, p. 296) proposed the now widely names Point Lookout Sandstone, Menefee Formation, Ridge and Cliff House Sandstone for Holmes’ units. The term Piao Vititos Mesaverde is widely used as either a group or formation

rn - depending upon the ability to recognize or use the Collier formation names, or it is used to bracket within a group other formation names which do not correlate or fit well with the type names. The term Mesaverde has been widely extended in mapping and correlation through the Rocky Mountains from Montana to New Mexico; in places the term may be applied to beds above and below those not present at the type locality. The Mancos grades into and intertongues with the overlying Mesaverde as described above. Southward and westward from the type locality the Mesaverde much thicker by intertonguing downward at ACROSS HAGAN BASIN NEAR becomes FIGURE 37—AIRvIEw NORTHEAST the Mancos. In the northwest, and DIAHOND TAIL RANCH HEADQUARTERS. the expense of 61

northern San Juan basin, the Mesaverde is overlain by the thick marine Lewis Shale. Eastward across the San .. Espinoso Ridge Juan basin the Lewis Shale thins greatly and its presence as far east as in the Hagan basin is doubtful. In the absence of the Lewis marine tongue, younger coal-bearing units would overlie the Mesaverde and would be included in the group. In the Hagan basin the Mesaverde is thick and overlain unconformably by the Galisteo red-beds sequence. It is conceivable that some of the upper part of the Hagan Mesaverde is younger than the type, or pre-Lewis, Mesaverde of the San Juan basin, and that it thus contains Pictured Cliffs, Fruit- land, or younger equivalents. Disrribution—Mesaverde outcrops are found in three separate areas. The most extensive and thickest are in the Hagan basin (Appendix 1) in a northward- FIGURE 38—AIRvIEw NORTHEAST ACROSS HAGAN BASIN NEAR COYOTE trending belt along the Una de Gato Arroyo, from ARR0Y0. MIDDLE LEFT SHOWS FORK OF COYOTE ARR0YO around the abandoned coal town of Hagan northward FROM SAN PEDRO CREEK WHICH RUNS ACROSS THE MIDDLE. IN UPPER across Tonque Arroyo (figs. LEFT CORNER T0NQUE ARR0Y0 CUTS THROUGH ESPINAS0 38, 39). In this belt the beds RIDGE. dip 20 to 30 degrees eastward in the northern part, becoming northward near Hagan. Another large area of The Omera coal mine is 17 miles east of Hagan; Mesaverde occupies the center of the Tijeras syncline Galisteo is 22 miles east-northeast of Hagan; and Lamy and crops out around the rim of the adjoining Tijeras is 27 miles east-northeast of 1-lagan. anticline. The top of the formation is not preserved in Earlier workers extended the terms Mancos and the Tijeras area. There is a small outcrop just northwest Mesaverde from the San Juan basin eastward to the of Placitas, which is overlain by Galisteo beds as in the Tijeras and Hagan basins, and still farther eastward to Hagan basin, but the section is much thinner owing to the Omera coal mine in the Galisteo area. Recently, the much more stripping of the Mesaverde prior to deposi Kansas-Colorado nomenclature of Graneros, Green tion of the Galisteo. horn, Carlile, and Niobrara has been brought into the Lithology—The Mesaverde Formation consists of Lamy-Galisteo-Omera mine area. See Stearns (1953b). alternating units of sandstone and shale which form a For a discussion of differing philosophies, see Dane, series of parallel ridges and valleys along much of the Cobban, and Kauffman (1966) and Coates and outcrop belt. Sandstone units range from about 20 to Kauffman (1973). The last paper, on a coral thicket near 600 ft thick and shale from 20 to 500 ft. Some intervals Lamy, subdivides the Graneros Shale, Greenhorn For consist of thin alternating beds of sandstone, shale, and mation, and Carlile Shale each into several members. shaly sandstone (Appendix 1). Sandstone is light gray through buff, to greenish gray or olive drab. Bedding Prefatory Reniarks to Table 4, page 63 ranges from thin to thick. Texture is fine to coarse 1. For the Tijeras basin, two columns are given, one grained and very locally conglomeratic. Grains are for the Mancos Shale and one for the Mesaverde subangular to subrounded. Composition ranges from Formation. Chief source is Lee and Knowlton (1917); relatively clean quartz sandstone through some feldspa invertebrates were identified by T. H. Stanton, and thic types into abundant subgraywacke types exhibiting plants by Knowlton. Several species of bivalves were distinctive salt-and-pepper qualities which result from a cited by Stevenson (1881) from near San Pedro, which mixture of feldspar and dark fragments resembling Lee and Knowlton (1917, p. 25) interpreted as having propylite. come from the Tijeras basin. Shale units are of twO types, noncarbonaceous and carbonaceous or coal-bearing. Shale colors vary from gray to dark gray or locally black, and from brown to olive drab. Brown colors are more common in the upper part of the section. Sandy seams intercalate with many shale units.

FOSSILS AND AGE Table 4, Upper Cretaceous Fossils in the Sandia Mountains and adjoining areas, presents the complete Upper Cretaceous fauna and flora of the Tijeras and Hagan basins. In addition, the complete faunas and floras of the Cerrillos-Madrid area and of the Omera mine-Galisteo-Lamy area are included, chiefly because many fossils found in these areas may eventually be found in the Sandia Mountains area. The Upper FIGURE Cretaceous outcrops of the Cerrillos are are only 8-10 39—AIRvIEw EAST ACROSS HAGAN BASIN NEAR HAGAN. miles to the northeast and east of the ORnz MOUNTAINS IN BACKGROUND. BUILDINGS OF ABANDONED Hagan-Tongue COAL CAMP OF HAGAN, ALONG outcrops; Madrid is about II miles UNA DE GAT0 ARROY0, JUST RIGHT northeast of Hagan. OF CENTER. NOTE BASALT DIKE CUTTING ACROSS THE FORMATIONS. ______

62

2. For the Hagan-Tonque basin, two columns are GALIsTE0 FORMATION and one for the given, one for the Mancos Shale Definition—The Galisteo was named by Hayden Sources include Lee and Mesaverde Formation. (1869, 40, 67, 90) for exposures along Galisteo Creek and Stearns (1953b). In the latter p. Knowlton (1917) near Cerrillos. Johnson (1903, p. 332-338) reviewed at identified by J. B. Reeside, Jr. paper, invertebrates were length the early literature on the “Galisteo Sand Stearns [1953b, table 2, 970]; in 1942 and 1947 (see p. Group” in the Cerrillos area and concluded that its age fossil localities, see Stearns for a map showing U.S.G.S. was Late Cretaceous or Laramie. He noted that some 195k, p1. lJ). workers had thought the Galisteo was Triassic. In that area, two columns are 3. For the Cernilos-Madrid area the formation unconformably overlies Mesaverde Shale and one for the given, one for the Mancos and is overlain conformably or disconformably by the include Herrick and Mesaverde Formation. Sources Espinaso Volcanics. Locally Galisteo beds appear to (1902-03), Lee and Knowlton Johnson (1900), Johnson parallel the underlying Mesaverde in the Hagan basin, and Kauffman (1966). A (1917), and Dane, Cobban, but the considerable differences in thickness of the reported by Lesquereux (1872) few fossil plants were Mesaverde beneath the Galisteo in such places as is some reason for from “Placer Mountain”; there Placitas, Hagan, and in the Galisteo Creek area strongly Madrid. believing that this was near suggest warping and erosion of the Mesaverde prior to 36-37, 2, fig. 3) described Marcou (1858, p. pl. Galisteo deposition. species from the vicinity of Inoceramus lerouxi as a new Distribution—In the Sandia area the Galisteo crops Cerrillos, out in four separate areas. The largest is a broad belt in at the point where the road from Santa Fe to Algodones the Hagan basin north of the abandoned coal town of crosses the Rio [Galisteo] I have dedicated this fossil to Hagan (fig. 39). Most outcrops are in the drainage area my friend and travelling companion. the celebrated guide and across Tonque Arr the Mexicans Don of Coyote Arroyo and northward mountaineer Antoine Leroux. called by northeastward Joachin. oyo, where formation dips change from to eastward at about 30 degrees. West and northwest of because We have not included this species in the table Placitas 2 short east-west-trending outcrop strips are locality we are not certain of its status, nor of the exact separated by a large fault crossing the downthrown end from which it came. of the mountains. In both outcrops dips are 60 to 70 did not Marcou (1858, p. 42) also identified but degrees northward. illustrate two bivalves, Cyrherea missouriana and Tel/ma Lithology—The Galisteo is a thick sequence of occidentalis, among variegated sandstone and mudstone with lesser beds of a great number of bivalves forming a lumachella in a conglomerate (Appendix 1). Sandstone beds are not yellowish-gray limestone placed between the gray marls that unlike those of the Mesaverde but the presence of the villages of occupy the country between Gold Mount and pebbles and cobbles in the sandstone, lenses and thin and Algodones. Galisteo beds of conglomerate, and petrified wood fragments These species have not been included in the table; and large logs distinguishes the formation. Limonite Marcou may have found them either in the Cerrillos staining is prevalent. In the lower beds iron-stained area or in the vicinity of Tonque and Hagan. sandstone concretions are common (fig. 40). 4. For the Omera-Galisteo-Lamy area, five columns In the Hagan basin the Galisteo consists of 3 are given. Many of the earlier workers cited fossils sandstone units separated by reddish-brown and simply from the Mancos Shale at the Omera mine. variegated mudstone units (Harrison, 1949, p1. 1). Later workers used the Kansas-Colorado nomenclature Bedding is thin to massive with cross-bedding. The of Graneros, Greenhorn, Carlile, and Niobrara. Sources sandstone is generally medium to coarse grained, locally include Reeside (1927), Cobban (1951), Stearns (1953b; conglomeratic, and commonly friable. Quartz predom map in 1953c), and Coates and Kauffman (1973). inates, with minor quantities of feldspar, chert, and Marcou (1858) described a new species of shark various rock fragments. Conglomeratic fragments are tooth, Ptychodus whzpplei, from 3 miles north of Gal (continued on page 66) isteo; see footnote 4 at bottom of table. Type specimens are indicated by T. Older generic I names are given in parentheses and quotation marks. For modern generic assignments of many species of J invertebrate fossils, we are indebted to W. A. Cobban (cephalopods), E. G. Kauffman (bivalves), and N. F. Sohi (gastropods). Additional information is noted at the bottom of the table.

TERTIARY The Tertiary rocks of the Sandia area consist of two types, stratified and intrusive. The stratified rocks include the Galisteo Formation red beds, Espinaso Grande NoTE Volcanics, and Santa Fe Formation of the Rio FIGURE 4O—LowGALISTEO SANDSTONE NORTH OF HAGAN. AND trough. They contrast strongly in origin, sites, and ROUND LIMONITE-IMPREGNATED SANDSTONE CONCRETIONS extent of deposition. PETRIFIED LOG. 63

TABLE 4—UPPER CRETACE0Us FOSSILS IN SANDIA MOUNTAINS AND ADJOINING AREAs (Ttvpe(s); superscripts at heads of columns refer to prefatory remarks in text; numbers in table refer to notes at bottom of table)

S.rrd,. Mt. A’.. Sn.d.. M. Hag4., C.,,dlo. OmnG.I,st.o At.. Ternt To..ma2 M.dttd3 1.,r,y C..ndIo. O...-G.h.n. Tip....t T.n.s.2 M.d,id L.ntr.4

0 S 0 — B f;s 8 8 f f r3z I 0R’SSII\II I N S fter,tal,s,a’ sp “I.. spp x N x It,,r’ard,a (fish, rtrSasp sp N Sodowar,o I.rgun,er, alt. p.’anulotunt x ASTJIOL0A tCasalo 1.. sp. Ira hoSt/to Jar!,,,,, Nell, Note I I..,’ sp. x Sol,vt, ,,or,tI, tilde!. x l,,,ria osa)tentrs BIt AC ‘I IOPOt)A I,. aft utahent,s ,egula I ,,sh,paatulasa N Liopistha” mad,,densrs Johnson (“..lrca’’) BJV ALS I A (I’de pods, cIae,s, ostc to T .4 nat/na sp. x I,ohopl,oga (“L,thophagus”) ttr)Sr,ua sp. l.opha N N hagshnn I ‘‘Otters “1 N N L, all, bags x bets x N .1 51’. x L. sp l”Alt’ctr’uort,o”) x ‘I ‘s’llo Strong) Johnson (ptohabls sr/rio ‘‘all. juicers Inc,cerarnut J,midiut( T “L. “7 n. sp. of Rees,de it, Stearns Callisr,r,a? sp. (Calljsta’? tp.’’ x ‘Macera” all, alto Corn ptrtnectes all. platessa x all. formosa N C, sp x “M. “ all, gracilin x Crdiorn sp. (ma, be Erh,nocardj,a,n) N x N ‘tSP,’’ pulchella [letrick and Johnson T Cladoceratnut aff. undulatopl,calus (“lnoceramttt’) “tSP” spp. N x “M, “7 spp, Corbula sp. (Stevenson c/ted 3 sp.) x x x x x ,Sfod,olus sp. t”,iiod(ola”3 (‘rassa),’/Ia ar,dre,s’s, (“Crassatell,teo”) x x it, tilojdet C. ohs mard, x x lab/also s. I. (‘‘(rroceramus ‘3 x x M. cl, labsatoo ‘4. Crassatella t Landinia? ) Jitch, Johnson ct, ,n,’tiloidev l”Corb,alo nr’mowphcara fitch,’) T M, opalersntt (‘rassootrea glabra M. “prohlematicoo’’ x C? all. glaht’a x .11.’ all. stanton, (‘‘Ir,,,ceromus all C ecu tiplicatus”) alt’. solenit cut N xx Ccmella ,nonranensis (“1. top/nt/to undata ‘1 x x Nucula subplana x Cvprin,eria sp x x x .5? SP. N C’? s,alcata Johnson T Nucularta sp, (“I,eda’’) x x Lndocv,stea (sr,,oko, Johnson T “Ottrea”anomioides x

if.” barabi,,/ “ (“lnoce’rarnuo “I N “0. anomie/des r,anos Johnson T K’? otmpsont “0,” helo/ti x F.’? tt’pi,’a 7 N “0,” nlegantula N Entot,urn n. SF. 01 Kaullnsan “0” and Pooch 5FF. xx N N (Note 2) “Pecten”sp, N x Ethrno,’ard tote paupercolutn x Phelopeeria gastrodes (“Pter,a,” ‘A c/cola ‘3 Fxogcra colurrt hello P. n. sp of Kauffman and Powell // pondo’rosa x (Note 2) if creche/li 7 N Ph,atadornya sp. x (s’r’t’rll,o sp. x Pinr,a petr,na x Idor,earea? sp (“Cucollaea “I x N P. sp. x I,,ocerosnut halchr, Plot, N ceramso? all. proximus (“Inoceramon ‘3 N I. ‘‘frag,lrt N P.” sagentiS x I perple out N P.? all. sagennio x I. ci perple.vot P.? t’anuxem, x I “ rutherjitrdt Phcatsla sp. x x Ir,o,’era,nst (lstoc,’rarrt,t, I di,r,,dus N Protecardia ears 7 x I (I I all. Jta,’ot Pseudoperna cungesta l”Ostrea”) N I, (I. I at’. piston Pycnodonte? bentoner,sis

I (I / an. tosoto,rth,,nat,,n P.? neeaberr,’i (“Gryphsea’) ‘‘l,,oc,’ra teas dcfortrt,t x Solen cuneaeus 7 ‘‘I’’ alt, te’rtuir,,Otrtt x Syncvclonema fl. Sit, x ‘‘I sp. no,. of Johnson “Tellirro” sp. ‘5 x

‘I ‘ sp. “veti large’ “7’:-? SF,

continued 64

AND ADJOINING AREAS (cont’d) 4—UPPER CRETACE0US FOSSILS IN SANDIA MouNT.JNS TAHLE in text; (T=type(s); superscripts at heads of columns refer to prefatory remarks numbers in table refer to notes at bottom of table) caniinuedfrom page 63 U. S.,.d,. MI, A.,. U..,- CrrdIo. O,ne.G.Isns... U.n. C..ni4Io. Orn.,O.Io.... Tn..., To.nsn..2 M.d.d3 Lnor4 lu..,.1 T...in.2 M.d,1d3 l,.rn04

0 0 - I 33I I3t3d

ci. (i,cl tennis Trigonarta ci. obliqoa xx B. ‘5 B nasus lolvice,arrrus? rregisiaris Johnson rounD T (Inocera B. 5I5 abs (rarest ‘5 x SCAPHOPODA (Task-shells) x xx x x B. spp Dentalium sp. 8.’ p GASTROPOLJA (Snails, conchs, drills. Lirnpels) ,Jcmaea cerrillosennis Johnson T finns’ viler corhlcnsr,s

A.? n. 5. at Renside In Stearns (‘aiscoceras taL IL ala, 5i Acleon sp. x C. spp.

A.? sp. Calycocerid7 ammonise, n, 5p. 01 Coates and Kautfman x ‘.4drm’ropsir1 ele.ala’ Johnson (probably Buccinid’t inder.) T Clioscaphits’s ,tos’imexicanas (Reessde) (“Dcnenoscaphises”) T Anchura SP. x L’odopoceras? sp. (“Sphenodiscus A.? up. ?ensicularis” of Hyatt) x Anisonr coniforinis Johnson (“Scurria’”) T von Csllignosriceras ssoollgani (“Prionotropis “) x Aporrhais po’olahiata C. 2 or more spp. (Herrick and Buccinopsis? occrdenealis Dernsoceras (Moremanoceras) troth x Johnson) (“Horpa?”) T n. sp. 01 Coales and Kauffman x Car’otss dalli (‘Rosts’lliten”) Futrephoreran alcs’sense xx x C. oellsi (Johnson) T F dekas’i (“s’osstilns”) xx errrhiopsis n. up. of Caates and Kauffman 1,, up. x Cerithium 5. sp of Reeside in Stearns Glypro.ssceras ,uacinsexicanssm (“Harniles”) x Charonga? kanabense (“Tritoniurn”) x G. sp. x Fasciolaria? sp. x “He?ieoeerao” n. up. of (‘oases and Kauffman x Fustis? sp. x Hoplssssraplsites nodosras (“Scaphilen”) Gvrodeu cf conradi x Karsahiceras sepsensoeriasum x G. depressa x xx K. off. septemseriatuns G. sp. (“Neocardioceras”) x Liops’plarer sp. ttesoicoceras s. hiiei x Lunatia sp. x “Pac/,rd(scus” n. sp. of Ssanton in Lee and x Knoo son ‘5 ‘5 ,atrca 51, T Odonrojusus? sp. x x Peroniceras (Reginaites) (cci Reeside x Placenliccras intercalare x Pterocerella sp. xx x Pyrrfusus? sp. x P. nrceki P. ,nseeki) x Pcropsrn up. ‘5 P. plas’s’nta? (proh. xx x P.? sp. x P. planunr (psob. P. nses’ki) x RoDe?(aria cf arnbigna C’ Volutods’rrna,” P. ss,hilfieldi ‘‘Rosts’llites’’) x p. ,pp. ‘5 xx Tessoro?ax? sp P. sp. “very large” x Turns up. Placenticeros (Stan Ionocs’ras) guadalupe Turritel?a galisieoens(s Johnson T (also as “sadaiupae”and “guadeloupas’”) x x T. aff. 55/I jtej P (S. I off. guadalupv x T. sp. xx P. (S.) ness’herrci ‘5 I OllsIodr’/’rtIa’ Sp mas he Rostcl!onia) xx P. (S.) sancarlurense xx x olnrornorpho ,roconre.sicona Hersick and Johnson x T P. (5.) sancar?ooense pseudonyrtale x Johnson C? ts’.sorsa (‘Roorelloria’ ‘‘) x Placerssiceras? ssrrs’nrnediu,n ( Place,iticeras planuns) T I’.’ sp. ‘5 x P.? rosundatuor Johnson (“P. CEPHALOPODA (Nauttloids. snsmonotd,) (Starr r000ceras) sancanlosessne) T A canthocenas alvanodoessoe x P.? sp x A. anrphibolurn? (“Plesiacarrt/roceros”) Pnionoc ye/us ,nacomhi x

Acanthocerid? alnmonlrn. n. up. at Cones P. u’sontinge?rSrS x and Kanitman P. uvornittgcn 555 elegans x Allocnroeeras annulalum? (‘Helscoeeras x P. n. sp. of Johnson parrense” and “lrsireiocerao x pane,tse”) Psessdoea?ycoceras de,slonersse x xx Bacrilils n aquilaerrsis 8 assceps 1 P. ci. india,sessse P. ci. den tone,rse) ‘5 B. aquilas’srsrn separarus x Puebloises corrssgatus (Helicocenas”) x B. aoper x 65

TABLE 4—UPPER CRETACEOUS FossiLs IN SANDIA MOUNTAINS AND ADJOINING AREAS (cont’d) (Ttype(s): superscripts at heads of columns refer to prefatory remarks in lexI: numbers in table refer to notes at bottom of table)

S.,,d,. Mr. A’.. 15.n Cr,,IIos O,,w,G.Inl.o. fl,1.,..t To.,q.a.Z M.d,d3 Lw,.4

0

Stop/ilk \ C in’g’il, I s/nra/Il I ‘‘C brpt/nhct a I ra/, tn S all on,,,:, \ seed) S hq’p”,’t ptt C. n sp. tI kr,ooIl,,n

S h,gi;”,r, rid ,raltnl C’e/a,ln,n n sp. ,t/ Knots Iron )hltterSSSoe

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NOTES 1. Specimens were collected at Lamy by N. H. Darton in 1914; 2. To be described in a forthcoming Geol. the species was described by J. W. Soc. America Special Wells in 1933. Corals are rare Paper by Kauffman and Powell. throughout the Western Interior Cretaceous. Coates and Kauffman 3. Formerly interpreted (1973 953) as an alga or seaweed; now regarded as p. describe the occurrence at Lamy as “a lenticular, burrows with paucispecific wartlike ornamentation made by a decapod crustacean thicket consposed predominantly of the egarious similar ahermatypic to the shrimp, Callianassa. coral.. . . This is the first coral framework known from 4. A current classification of the shark teeth and the entire Vestern Interior Cretaceous seaway.” fish scales, as suggested by un Zidek (letter, Jan. 21, 1975), follows. (continued on page 66) 66

( (OPI(Ifl uecl/ro,n page 65 at once as a flew species 01 his genus Ptvchodus.” I-arlier. Rorner (‘lass Chondrichthyes (sharks and rays) (1945. 577) had assigned It to the order Batoidea (skates and Subclass Hasmobranchii p. rays) but later (Romer, 1966, p. 349) transferred it to the order Cohort Selachii (= Euselachii) suborder Ilybodontoidea. and (ibid., p. 43) characterized it Order Hybodontiformes Selachii, shark. l.amna. on thc other hand, is one 01 the Family Ptychodontidae (shell-crushine teeth) as a mollusk-eating sharks, ss ith long, slender. liattened teeth, suitable for P(;’chodus ii.’hipplei Marcou mackerel cutting flesh. Scales of Bercx were figured by Johnson (1902, p1. 1, Superorder Galeomorphii Order Lamniforrnes fig. l2a). Leo J. Flickey was unable to cheek the present status of all Family Lamnidae (flesh-cutting teeth) 5. names, but wrote (letter, May 23. 1974): Lainna sp. these plant Most of Knowlton’s assignments of fossil leaf specimens to fishes) Class Actinopterygii (ray-tinned modern living genera are incorrect. Thus the assignments to Subclass Telcostei (‘elasinis, Cinna,nomupn, Dotbergia, I’ji.s’ (especially), (spiny teleosts) Superorder Acanthopterygii Launs, Magnolia, Ms’rica, Quercus, Popidus, Sequoia, and Order Beryciformes Trapa, are all very likely incorrect. Recent work in Russia has Family Berycidae shown that the genus Platanus did, indeed, live during the Beryx sp. (scales) late Cretaceous and early Tertiary, thus this is probably a Ptychodus whipplei was described as a new species from 3 miles good assignment. In addition. Neluinho is probably valid and who north of Galisteo by Marcou (1858, p. 33, p1. 1, figs. 4, 4a), Juglans is probably correct only at the familial level. wrote Hossever, it was thought that a complete listing of the names tjsh to my I dedicate this beautiful species of cretaceous Isici would be worthwhile as a matter of record. Howard .1. Dittmer, of chief of our friend Capt. A. W. Whipple, the able and learned V.N.M., assisted us with names of modern representatives, given in Exploration in the Rocky Mountains. parentheses. He added that Prof. Agassiz saw the holotype “and recognized it

(continuedfrorn page 62) (1848) visited C’erri!!os and noted subangular to well rounded and consist of chert, quartz, 29, 1846, Abert petrified trees.” quartzite, sandstone, and limestone, and minor clay “fragments of immense apparently, was by Knowlton; galls. Fragments of gneiss, coarse angular feldspar, and The first identification, 1903, U.N.M. Bull., 145) rare crystalline rocks indicate that Precambrian terranes Johnson (1902, p. 217; p. 2 miles east of Cerrillos, not had been exposed in Galisteo time. reported ?Quercus sp. from Thickness—The Galisteo thickness ranges consider ing that ably, and Stearns (1943, p. 309) found it to be a In the red sandstones above the coal measures were found wedge which thickens from about numerous fossil tree trunks, many of which were from one to northeast-trending these fossil . one of - . sections from along the eastern margin of the Rio Grande two feet in diameter Thin 1,000 ft by Mr. Knowlton [who wrotel ‘The wood ft along a line from Hagan to trees were examined trough to about 4,000 is a dicotyledon, and while it has been somewhat distorted by Galisteo. He also believed that the section might be still fossilization, 0 appears to be a species ot’Querc’us thicker to the south and southeast, but this is not known that the as there are no exposures in that direction. Source areas Lee and Knowlton (1917, p. 185) reported for the l-lagan-Galisteo area could have been to the Galisteo Formation northwest, north, or northeast, but there is little likeli contains great numbers of petrified logs, which are beautifully hood of a source to the south, such as the Sandia preserved in external form, but the cellular structure of the wood is not well retained and no specific identifications have Mountains. these logs occur of 2,100 ft along Pinove been made. The best-known locality at which Stearns’ calculated thickness of Cerrillos in the so-called petrified forest. section of is a few miles east tito Arroyo agrees well with the hand-levelled where there are many logs 25 to 75 feet or more in length. Logs 2,372 ft measured by Harrison at the same place. The have been found in this formation in many other places in a outcrops at Placitas are incomplete, the upper part much better state of preservation. Fossil leaves have also been preservation is poor and few being overlain unconformably by the Santa Fe Forma found in a few places, but their have been specifically identified. tion. Only 600 to 800 ft of the lower part of the Galisteo crops out south of the overlying Santa Fe. Near Rogers, 2 miles southwest of Cerrillos, Lee and Age—Few fossils other than petrified and Fossils and Knowlton (1917, p. 212) found Sabal? ungeri wood have been found in the Galisteo Formation. Dr,yopteris? sp. in the lowest 10 ft of the Galisteo attention Silicified logs near Cerrillos attracted much Formation. to be from early travelers and explorers. What seems Stearns (1943, 312) notes that collections from 7 of any age in p. the earliest definite reference to fossils localities, “most of them in the upper few hundred feet famous of the New Mexico is by Josiah Gregg, most of the Galisteo,” were studied by W. C. Darrah, who trips to New Santa Fe traders, who made several reported that Commerce of the Mexico during the 1830’s. In his diary, pine The bulk of the specimens belong to the conifers—the Prairies, published in 1844, he described beautiful genera of flowering ... There are several on land that type. Plivosilon specimens of silicified wood near Cernllos plants_an oak [QuercusJ, a Fagus’? (beech). a woody legume later (about 1900) became the Sweet ranch. He wrote related to .4cacia, a diffuse-porous wood allied to poplar, and that one log “lies between Santa Fe and the Placer, two indeterminate. ring.porous hardwoods. broken into blocks since its petrifaction, which shows Forest, 1 tree was about every knot, crack and splinter almost as in its ligneous At the Sweet Ranch Petrified estimated to be 135 ft; state. It is said that there are some of these arboreous 6 ft in diameter and had a length (oral communication to petrifactions in the vicinity of Galisteo, still standing many years ago I. C. Sweet traces of both gold erect.” Northrop) stated that assays showed a tree 4 ft in diameter In the summer of 1846, Wislizenus (1848) saw “large and silver. Woods (1947) reported describing and illustrat masses of petrified wood” near Cerrillos. On September and 185 ft long. Popular articles 67

ing this “forest” include Northrop and Popejoy (1931), large particle sizes suggest mudflows or torrential Harrington (1939), and depo Woods(1947). sition, but the character of the bedding and rounding Vertebrate fossils have been collected at several of many fragments suggest a predominantly alluvial localities. Theodore White made small a collection in origin for the coarse material. Stearns (1953a, 422) 1939 from less than 200 ft below the top p. of the Galisteo describes 2 trachyte flows (10 to 50 ft thick) high in the Formation near the Sweet ranch that yielded Teleodus formation at the northern end of the ridge and a sp. and Uintacyon. The former is a titanothere (extinct hornblende quartz latite flow in the eastern part of the perissodactyl) and the latter a primitive carnivore outcrop belt near Huerfano Butte (sec. 23, T. 13 N., R. (Stearns, 1943, 310). Stearns 6 p. found abundant disartic E.). The following is a description of a section measured ulated bones in the Arroyo Pinovetito (sec. 4, T. 13 N., by Stearns: R. 6 E.), in the zone of transition between the Galisteo Formation and the Espinaso Volcanics. According to Thickness Bed No. White (Stearns, 1943, p. 311), both a large and a small Description ft titanothere are represented in this collection; the age Espinaso (Total thickness) 1,450 was given as 4 “Duchesnean [sicj ... uppermost Eocene Breccia and conglomerate interbedded, gray, fragments [or] lowermost Oligocene.” up to 6 inches in diameter, water-laid Abiquiu above 150 3 Breccia and conglomerate In 1955, Robinson (1957) found an upper molar of interbedded. gray. indurated, Coryphodon minor amounts of water-laid Luff, fragments up to 2 ft (an archaic hoofed mammal known as an in maximum amblypod diameter, some blocks up to 6 and 8 ft or pantodont) about 700 ft above the base of across occur in the upper half ridge-forming the 1,050 Galisteo Formation about 2 miles northeast of 2 Tuff. blue-gray. a few beds of clay, I to 2 ft thick near Cerrillos. Robinson notes the base, pebbly beds in upper halt water-laid 200 I Clay. green. tuffaceous. Lenses of red clay and limonite “Corvphodon is an excellent lower Eocene index fossil and stained sandstone in the lower 25 ft are transitional indicates Wasatchian age for the lower part of the Galisteo with the underlying Galisteo Formation. Abundant formation Both White’s and Stearns’ collections indicated fossil bone occurs in a bed I to 2 ft thick midway of Duchesnian age (latest Eocene) for the upper Galisteo rocks the unit (Stearns, 1943, p. 310 and fig. 7), Galisteo The presence of Corphodon in the lower Galisteo beds below shows 50 that these deposits began to accumulate in the early Eocene.” Age—The Espinaso is relatively younger than the The considerable likeness of the Galisteo to the San Eocene Galisteo and older than the Miocene Abiquiu Jose Formation (formerly Wasatch) of the San Juan Formation. The porphyry intrusions at Cernllos deform basin suggests that the 2 were either once continuous or and probably intrude the Espinaso. These geological deposited at the same time on opposite sides of the relationships suggest at least an Oligocene age and Laramide Nacimiento uplift. probably a late Eocene age as maintained by Stearns (l953a, p.423). EsPINAs0 VOLCANICS SANTA FE FORMATION Definition—The formation was named by Stearns (1943, p. 304), as suggested by Bryan and Upson in an Definition—The name “Santa Fe mans” was given undated unpublished manuscript, as the Espinaso Vol by Hayden (1869, p. 60, 69) to beds exposed north of canics exposed in Espinaso Ridge (fig. 37). Here the Santa Fe. The term was intended for the thick sequence Espinaso is in near conformity in the Tesuque and with the underlying Espanola Valleys. Johnson (1903, p. Galisteo and is overlain by white to pinkish beds that 313) credited Hayden for the name “Santa Fe Marl may be either the Abiquiu Formation or a lower part of Group” and applied it to the late Tertiary gravel beds in the Santa Fe Formation. the Cerrillos Hills area, including the gravel on the Ortiz Distribution—In the Sandia map area the Espinaso surface of planation (p. 472). Johnson(1903, p.3 I3-332) crops out in a north-northwestward-trending belt about reviewed at length the early literature on the Santa Fe 4 miles long in the north-central part of T. 13 N., R. 6 E. Marl Group in the Cerrillos area and concluded that its The relatively resistant Espinaso, compared with the age ranged from Loup Fork (Miocene, Pliocene, and adjacent, less resistant Galisteo on the west and Pleistocene?) to the present. In time the term was Abiquiu on the east, holds up the prominent Espinaso changed to Santa Fe Formation (Darton, 1922, 187). Ridge. p. Dips are regular ranging between about 15 and Bryan(1938a, p. 205) observed that 20 degrees, and the attitude of the lower part of the The main body overlying Santa Fe beds is essentially of sedimentary deposits of the Rio Grande the same. No depression, from the north end of other outcrops of the Espinaso the San Luis Valley to and occur in the area. beyond El Paso, is considered to be of the same general age Lithology—At Espinaso Ridge the formation is Ia and to belong to the Santa Fe Formation. tite and quartz latite porphyry breccia and conglomer The term has been extended widely to deposits along ate with considerable water-laid tuff in the lower 200 to the Rio Grande valley and also out of the valley to 250 ft. For the most part the formation is well bedded similar deposits, especially in southern New Mexico and resembling a fanglomerate. Some tuff-breccia beds, to some deposits in the Puerco, Estancia, and Jornada however, strongly suggest pyroclastic air-fall deposition. del Muerto valleys. Kelley (1952, 102) suggested the The general color of the formation is bluish P. gray, but term, group, again for the Santa Fe including all the brownish, purplish, and reddish grays are common. The trough-filling beds including the pedimental and allu most abundant fragments of the breccia and conglom vial fan beds. Later Spiegel and Baldwin (1963, erate range from pebbles to small p. boulders, but locally 38-39) more formally proposed usage of the term, blocks as large as 10 ft in diameter Santa may be found. These Fe Group, to include Quaternary as well as Tertiary 68

northeast corner of the map area (map 1), east of beds and volcanic flows in the Rio Grande trough and treme Ridge, Santa Fe beds lie conformably on the adjacent areas. They also proposed expanding the unit, Espinaso (Zia?) beds of Stearns (1953c, p1. I). No Santa in its group status, to include the Abiquiu Formation of Abiquiu is exposed west of the main escarpment of the Smith (1938, 301) and Stearns (1953c, p. 477, p1. I). Fe proper p. Mountains except along the sides of Tijeras Galusha (1966, 4-7) defined and delineated the Zia Sandia p. (secs. 26, 35, T. 10 N., R. 4 E.). However, Sand Formation in Sandoval County as separate from Arroyo Santa Fe may lie only a few tens of feet beds previously referred to as the Santa Fe Lower gray considerable the terrace or pediment gravel veneers along member (Bryan and McCann, 1937) and retained the beneath entire front of the mountains. The best exposures of term, Santa Fe Formation, for the overlying beds. Hoge the Santa Fe near the mountains are in the Rio Grande (1970. fig. 6) included the Zia in the Santa Fe Group west and north of Placitas between NM-44 and and used the term Tesuque Formation (Baldwin, 1956, trough Francisco Arroyo (figs. 41, 42). En the southeastern 115-116) for the overlying beds exclusive of the San p. of the San Felipe Pueblo Grant (sec. 4, T. 13 N., R. uaternary insets and terraces related to the present part Q 5 E.) the formation is tilted as much as 45 degrees, river. He recommended the substitution of Zia for revealing a considerable section. Excellent exposures of Abiquiu as extended into the Santo Domingo basin the coarse basal part of the formation lie across steep area by Stearns (1 953c. p1. I). plicated beds of formations from the Morrison to the Galusha and Buck (1971, p. 30) restricted the Spiegel Galisteo. These outcrops as well as other nearby basal and Baldwin term, Santa Fe Group, to the occurrences beds are also tilted as much as 10 to 45 degrees. in the Espanola basin and described it as consisting of 2 Lirhology—The Santa Fe is variable in composition formations, the thick and extensive Tesuque below and and texture depending upon the source of materials; in the lesser Chamita above. They further restricted and general it has had two contrasting sources. The most redefined the Tesuque Formation to include 5 members source has been local—the adjacent uplifts in the Espanola Valley and 2 in the Abiquiu area. The abundant either side of the Rio Grande trough. The basal base of the Tesuque and the Santa Fe Group, as along Fe fanglomerate in the dissected mesas west and restricted, is variously on such trough units as Abiquiu Santa of Placitas consists predominantly of large and Picuris, and possibly Espinaso (p. 37-38). Galusha northwest of reddish Abo and Meseta Blanca sandstone. and Buck 39) point out the inadvisability of extend boulders (p. must have been the nearby mountains ing the type Santa Fe outside the area and specifically The source the Abo was eroded from the crest. The other recommend that a different formation name be applied before most of the existence of the trough has to beds in the Santo Domingo Valley. On the other source during to the basins, regardless of whether these hand, they apply “Tesuque Formation” to the Bryan been axial by a through-flowing river or not. Axial and McCann “Middle Red” unit in the Jemez Creek were joined long ago recognized by Bryan (l938a, p. area while at the same time recommending that none of gravels were and other workers. The local source materials the other Jemez Creek and Rio Puerco units should be 205-206) in coarseness from place to place, depend correlated with formations at the type locality of their differ greatly upon proximity, abruptness of uplift, and the Santa Fe Group (p. 40). In short, they propose that the ing of the rocks being eroded. The axial term, Santa Fe Group, be restricted to beds of the type composition are a mixture of rocks derived locally and area or to “those that can be shown to be traceable from materials far up the drainage system. the type area to contiguous areas” (p. 41). Although from The influence of local sources on composition is there are cogent reasons why this proposal might be seen in the Santa Fe (fig. 42). If the source is followed, in all practicality the term Santa Fe has been frequently in Cretaceous terranes the grays and olive drabs of the so widely used in the less restricted sense that the show up in the Santa Fe. If the source is largely change is hardly feasible or even desirable. in our shales beds of the Permian or the Triassic, the Santa Fe is minds there is little doubt about the equivalency of red some of the thick, strongly tilted Santa Fe beds northwest of the Sandia uplift with the Tesuque beds of the Espanola basin. Regarding recent suggestions that Santa Fe Group be used in either expanded or restricted senses, it is difficult to follow either, and there are undesirable aspects to both recommendations. The ranks of formation, includ ing member, and group are interchangeable to suit the particular needs in different areas, as in the use of “Mesaverde” to refer to either a formation or group. Therefore, in this work the long-established Santa Fe Formation is used for rocks in the Albuquerque and Santo Domingo basin areas. The term Tesuque is not used as it includes too nearly the same strata as the Fe, and because it tends to displace a widely used Santa 4, —,—‘ and well-established name for what is probably the F r - ‘- OVERLY earliest recognized New Mexican formation. FIGURE 41—SANTA FE FANGLOMERATE UNCONFORMABLY lie SIDE SEC. 31. T. 13 N., R. 5 E.. 2 Distribution—Most of the Santa Fe outcrops ING SOFT GALIsTL0 BEDS. WEST CONSISTS LARGELY OF northwest of the Sandia Mountains where they are MILES WEST OF PLAc-ITAS. FANGLOMERATE ABOUT 40°. GALIsTE0 DIPS 55° TO 60°. downthrown into the Rio Grande trough. In the cx- AB0 FRAGMENTS AND DIPS 69

bouldery material near the base of the formation in the mesa west of Placitas where the material consists predominantly of Abo sandstone, but several hundred feet above the base Madera limestone dominates. The bulk of the Santa Fe is a mix primarily of sand, mud, and gravel from many sources. It was derived or deposited under warm and humid to savannah-type climatic conditions; thus, the subaerially weathered debris developed a characteristic pinkish terra cotta or light-gray tone. Reddish-brown shades are found mostly in muds, and their colors may in many instances reflect those of the source beds. No significant thickness of Santa Fe is exposed in the area, but exposures in nearby parts of the trough and penetrations in wells suggest FIGURE 42—FANGL0MERATE thicknesses of several thousand OF SANTA FE FORMATION ALONG feet. T0NQuE ARR0YO. HERE Apparently IT IS DROPPED ON WT SIDE OF SAN no significant fossils have been found FRANCIsCO FAULT AGAINST ENTRADA AND CHINI.E. FRAGMENTS within the map area that have been determined ARE DIVERSE AND INCLUDE to be of QUARTZITE. GNEISS, SANDSTONE, AND Oligocene, Miocene, TERTIARY PORPHYRITIC or Pliocene age. Lambert (1968, ROCKS. table 7, p. 237) found a few vertebrates west of the map reddish; area on the south side of Tijeras Arroyo (Sec. 15, T. 9 if from the Madera limestone, the Santa Fe N., is R. 3 E.). He assigned these to his upper buff formation calcareous with prominent limestone and chert gravels. of the Santa Fe Group, and D. E. Savage identified Bryan and his co-workers (Stearns, 1953c, 472) have p. them as: ef. Camelops (extinct camel) and Equus emphasized the coarse resistant gravels of cf. quartzite, plesippus or E. bauristensis (zebrine horse), gneiss, and foreign volcanic rocks in the with a range recognition of in age from late Pliocene to early Pleistocene. an axial throughgoing drainage. Although these are diagnostic their absence does not rule out the existence INTRUSIVE ROCKS of an ancestral Rio Grande. This is evident from the Tertiary intrusive rocks in the Sandia Mountains present and Holocene river bed in which the are material is few and widely scattered. Complex intrusions largely sand and mud, much of which of lacco obviously has liths, stocks, and sills form a north-south-trending been transported from great distances. belt just east of the Sandia map area; a few of these extend Bryan used the term, axial gravels, and he mapped into the edge of the map area near Monte Largo; and these as a narrow strip roughly parallel to the present there are a few small intrusions elsewhere that seem river between the latitudes of Santa Fe and to Albuquer be petrologically related to porphyritic bodies. que; he believed that the gravels came In Ferry from the San boat Hill northeast of Monte Largo Juan Mountains country via an a monzonitic sill up ancestral Rio Chama to 60 ft thick has been intruded (Bryan, 1938a, 206). His term just above the Sandia p. appears to have been Formation. Little contact metamorphism restricted mostly to the well-rounded cobbly or mineraliza quartzite tion is associated with the intrusion. A gravels obviously transported from afar small sill-like by high-reg exposure of monzonite also occurs imen stream flow. The evidence for near the head of the source and the Coyote Arroyo in sec. 25, T. axial continuity is tenuous; however, 13 N., R. 6 E. The intrusion there is an axial is mostly covered by Tuerto Gravel suite of gravels along the Rio Grande but at the west end depression. This it is in contact with Mancos suite comprises more than the Shale. Another small cobbly beds and includes monzonitic dike sand, silt, and mud of crops out along San Pedro Creek 1.5 a distant source; the term, axial miles downstream facies, would be better. from NM- 14. Considerable alteration The distribution of the axial and metamorphic facies varied in response effects are observable in the sur to shifts in the sag axis, influx rounding volume from tributaries, area in the high beds of the Madera Forma and meandering of the river. tion, as though Tijeras Arroyo has gravel a larger intrusion may lie just below the foreign to the Sandias as far surface. The metamorphic as 6 miles from the present minerals include some epi Rio Grande junction, dote and, locally, garnet. showing that at the time One other intrusion of monzo the foreign gravels were nitic porphyry is deposited there was far from the porphyry belt in the an axial river within only 2 or 3 Sandia uplift in miles of the border NW¼ sec. 35, T. 11 N., R. 5 E. The of the trough at about the position intrusion is of Sandia Laboratories. in the Yeso Formation east of the road up Cañoncito Canyon to the Cole Springs Mixing of source types is inevitable, picnic area. It especially with appears to be either a small plug the longer tributaries that or a short, thick sill extend into a variety of with little associated mineralization formations. Tijeras Creek or metamorphism. is an example; when it In the Hagan basin reaches the axial area there are several long dikes, of the Rio Grande, it carries several sills, and debris from every 2 thick concordant tongues. Some of formation in the area except the these appear Galisteo and to be related petrogenetically to the Espinaso, having mixed it with far-off porphyry axial materials belt rocks, but several of the dikes are basaltic such as from the Jemez Mountains. San and probably Pedro Creek related to the younger Rio Grande trough does likewise but also transports debris eruptions. from The largest dike lies north of Hagan, and is the Galisteo, Espinaso, and the laccolithic porphy ries. nearly 3 miles long and 20 ft wide. It strikes east-north eastward and cuts Mancos to Galisteo beds. Similar but Dominance of local source is evident in the angular much shorter dikes occur about 1 mile to the north and 70

of especial interest are those around the Sandia about I mile south of 1-lagan. Still farther southeast Mexico: Ortiz Mountains, in the plains to the east, and in another basaltic dike, somewhat porphyritic, is intruded and Grande valley. One of the highest and oldest of along a north-northeast fracture that appears to be an the Rio the Ortiz surface or pediment (Bryan. l938a, p. extension of the Perlas del Polvo fault. these is which surrounds the Ortiz Mountains and extends The largest intrusion in the Hagan basin is a sill up to 215) the Sandia Mountains area. Johnson (1903, p. 60 ft thick near the base of the Mancos Shale (fig. 51, p. into with 174-175) was possibly the first to note this surface and 76). It is monzonitic and extends along strike referred to it as “the erosion plains sloping away from interruptions of outcrop for 2.5 miles. Little meta the the Ortiz Mountains” without formally naming the morphism or mineralization is associated with pediments the Ortiz surface. About the same time intrusion. surround in the Mancos, Ogilvie (1905, p. 34) described the pediment Several short tonguelike sills occur as the from faults ing the conical Ortiz porphyry-cored mountains some in positions which could have been fed to and “conoplain of the Ortiz.” However, Bryan appears or other fissures. These intrusions are monzonitic have been the first to name the pediment and to extend petrogenetically related to the porphyry belt. The ft it by mapping and correlation widely away from the largest tongue exposed is about 100 ft thick and 600 and Sandia area. wide with apparent elongations downdip to the Ortiz The Ortiz surface was eroded following deposition east-northeast. subsidence of the Santa Fe Formation into the Rio A single basalt dike occurs northwest of Placitas in and trough. During development of the Ortiz sur Mesaverde beds. It is up to 30 ft wide and dips 55 to 60 Grande the Rio Grande or a stream at the basin axis was at degrees southeastward. Three north-striking hornblende face of level of 400 to 500 ft higher than at present, and long latite or andesite dikes occur east of the Sandias. Two a erosion of the surrounding uplands formed the Ortiz these are in the east limb of the Tijeras anticline (fig. 10, surface across the Santa Fe and older rocks. Since that 49, 76), and the third is in Tejano Canyon (secs. p. time uplift of the region caused canyons and valleys, 15, T. 11 N., R. 5 E.). The dike of figure 49 contains in including the Rio Grande and its tributaries, to dissect numerous hornblende phenocrysts up to about 5 mm and largely remove the old surface. The surface has length. been named for preserved areas around Ortiz Moun A number of lamprophyric dikes occur in the Sandia tains about midway between Albuquerque and Santa Granite (fig. 50, p. 76). Shomaker (1965, p. 23) assigns of Fe (Bryan, 1938a). them a Tertiary age based upon 1) the existence its (see Considerable areas of the Ortiz surface and similar dikes cutting much younger sediments overlying Tuerto Gravel (Stearns, l953c, p. 476-477) are above) and 2) the lack of any diaschistic field relation shown on map I east of Hagan (fig. 43) to NM-14 and with the aplites. The few lamprophyres in the ships southward into the San Pedro Valley around generally longer than the aplites and almost extending granite are Numerous remnants occur west of the trend. Shomaker described the dikes as San Antonito. all of northward of San Pedro Creek between Gonzales and spessartite and vogesite varieties. They are lower part principally Creeks and extending well into Tecolote wide and extend as a swarm some 12 miles Arroyo Seco up to 20 ft Madera. Some fingers of this surface are dark-green, fine- to Canyon near La long and 2 miles wide. They of the mountains and are distinct chilled extend up the eastern slope medium-grained dikes, usually with such as south from the preserved in a few places along low ridges, margins, and they differ in many respects R. 5 E. and and of Cienega picnic area in sec. 23, T. 11 N., aplite dikes. Shomaker (p. 38) also found granite near Cienega and Bill Springs a short distance to the aplite inclusions in the lamprophyres, which cut across north. These remnants range in altitude from about the aplite dikes. 8,000 ft of the 7,200 ft (southwest of Sandia Park) to nearly Woodward (1970) described the petrography Gravel typical (near Bill Springs). The elevation of the Tuerto dikes and presented chemical analyses of the near San Antonito is 6,850 ft. The higher remnants hornblende spessartite and a light-colored hornblende appear to represent canyon extensions of the Tuerto syenite differentiate found locally in dikelets and segre Gravel and the underlying pediment, as seen in San gations. Q UATERNARY PEDIMENTs AND PEDIMENT GRAVEL A pediment is an erosional surface at the base of mountains. It is covered by thin to moderately thick blankets of gravel; where thin, the gravels are in a sense the cutting tools and products of the cutting. Pediments form through prolonged erosion under stable conditions of elevation and erosional base level, to which the pediment surface grades. A widespread old pediment occurs north and east of the Sandia Mountains. The term pediment was first used by McGee (1897, p. 130-131) had although others (Gilbert, 1877, p. ORTIz PEDIMENT SURFACE. 92) FIGURE 43—TUERT0 GRAvEL CAP OF of corrasion” (Johnson, 1903) EAST OF HAGAN. HERE recognized these “planes NW SEC. 34. T. 13 N., R. 6 E., I MILE of these EDGES OF REDDISH GALIsTE0 in many places. Large and small remnants GRAVEL RESTS ACROSS UPTURNED New SANDSTONE. features are widespread at many altitudes in MUETONE AND WHITE 71

Pedro Valley and farther north. Elevations of the cito. However, there are a number eroded edge of the gravel of still higher gravel and pediment are 6100 to remnants along the 6,200 ft. Remnants Sandia slopes between Canoncito of this surface are also preserved and Tijeras. Two north of small patches occur at 6,500 to 6,600 ft Montezuma Mountain, 2 to 2.5 miles on the low east-northeast hills just north of Tijeras. about 200 ft above of Placitas at about 6,200 ft. The high the lower level gravel along the canyon bottom. Several on the gravel west and north of Placitas, mapped ridge-capping strings of gravel occur north and south of by I-loge (1970, pl. 19. Qpt). may also be equivalent to Lorenzo Canyon and south of Cañoncito. Near Cañon the Ortiz. The surface levels are at elevations from 6,000 cito these are about 200 ft above the gullied gravel to 6,300 ft. with the higher levels near the Sandia, along San Antonito Arroyo. The old high gravel Monte Largo, and Cerrillos Mountains; at a broad swale Cañoncito extends up the ridge to about 7,100 probably existed in the Hagan Valley ft from where the present its lower eroded end at 6,930 ft—a rise dissecting drainage concentrates. of about 225 ft per mile. The ridge gravel remnant north of Lorenzo There is a pediment surface with gravel east of Monte Canyon is about 6,000 ft long and it rises from 6,850 Largo that extends into Estancia Valley. ft The head of to 7,450 ft at a rate of 100 ft per mile. These are this surface next to Monte Largo is at 6,900 to 7,200 ft. probably alluvial remnants of higher valleys, leading Across the uplift along the San Pedro to Valley, side an older higher pediment that may have been elevations are about 6,600 ft, showing equiv that the two alent to the Ortiz pediment. The lower surfaces were graded to different end of the bases. Two remnants Cañoncito remnant is about 50 ft lower than of the Estancia surface are preserved any of the on the Abo at the present divides between the Tijeras and southwest end of Monte Largo San Pedro at elevations of 6,850- drainage systems proving that gravels 6,900 ft (map 1). In later Quaternary in the Tijeras time the San Pedro drainage area did not connect with drainage extended itself along the alluvial rem Frost Creek in the weak nants. No remnants of higher gravels Triassic rocks, and it is now eroding are along the the higher Estancia Sandia front. A few obscure local flats on surface a few miles north of Corners. the low part of the Sandia escarpment between Tijeras Canyon and the The other large pediment in the Sandia area lies Juan Tabo area might, however, be remnants of cut along the western base of the mountains. It formed later rock surfaces at the heads of a former higher surface at elevations 200 to 300 ft lower than the Ortiz surface now completely eroded on the valley side. The flats at and has been correlated with Bryan’s (1938a) La Bajada Juan Tabo picnic area are only about 200 ft above surface. The piedmont surface consists the of two parts, one heads of the pediments near La Cueva south of Campus Wash (an old Canyon. A Tijeras arroyo) referred higher pediment of this sort might to as the Airport surface account for the and a younger, lower, more anomalous cutting of Juan Tabo dissected surface extending Canyon across Rincon northward along the moun Ridge. North and west of Placitas tain front to near thick gravel deposits, Bernalillo. The older surface at the with mountainward surface Albuquerque International altitudes from 6,000 to Airport and south of Tijeras 6,300 ft. appear to be above Arroyo is the Sandia (Bajada) surface a pediment remnant. Along the north side of to the west (Hoge, Tijeras 1970, p1. 19, Qop) as described above. Arroyo, just west of Four Hills Road, the gravel-veneered surface can be seen slightly truncating RIVER TERRACES AND GRAVEL Santa Fe beds below. North of Campus Arroyo (Kelley, River terraces have some affinities with pediments in 1969, p. 27), Embudo, Bear, Pino, and other streams that they are commonly surfaces cut on bedrock have completely dissected the at the Airport surface and base of steep slopes along canyon sides. nearly regraded the surface Like pediments to the Rio Grande flood they are usually capped with gravel. plain; the high bluffs The two are closely seen west of the airport are absent related around the northwest here. This is especially side of the Sandia uplift. true near the mouths of Baca Terrace gravels are present and Pino Arroyos. While along the sides of Tijeras this late cutting was going on Canyon but these have alluvial fans continued already been mentioned in to build onto the old surface in connection with the extension places along the of the Sandia piedmont base of the mountains. However, the level into and back larger canyons of the mountains. from the mountains have adjusted River rapidly terraces have long been known along the Rio to the base formed in the Rio Grande flood Grande plain. inner valley and they have been studied by Bryan (1938a) and his associates who gave names The Sandia pediment has been traced to around the these levels. Several terrace surfaces are preserved northern end of the uplift to intermediate in surfaces in the northwest corner of the map the Santo Domingo basin area (J. E. Anderson, and Hagan embayment 1960, 79-82). Anderson described (Hoge, 1970, p1. 19), p. the Sue terrace 25 and into what has generally been ft above the river which thought to be may have been cut only a few the wide La Bajada surface along 1-40 to hundred years Santa Fe. ago. He also identified remnants of the Pefla Blanca terrace, about 150 ft above the river; and a Extensions of the Sandia pediment can be traced well Rio Grande terrace about 95 ft above river. Long into Tijeras Canyon from the levels around the Western northwest-sloping pediment surfaces, extending from Skies Motor Hotel. Shoulders on both sides of the well up the slopes along the Sandias dissect canyon are evident almost to the big and turn in the canyon. intersperse at their lower ends with terrace gravels. The gradient of Tijeras Canyon through the mountains and the shoulders in the lower part of the canyon is 100 ALLUVIAL FANS ft per mile. The Sandia surface gravels appear to be Sand and gravel at the base of a mountain without equivalent to those up the canyon at Seven Springs, lateral confinement by ridges or arroyo banks are Tijeras, San Antonito, and on the flats around Cañon- alluvial fans; if small, alluvial cones; and if coalesced 72 with adjoining fans, alluvial piedmont plains. Around the East Heights or East Mesa near the bases of the Sandias and the Four Hills are a number of fans built from the major canyons debouching onto the alluvial piedmont. The largest of these are Embudo, Embudito, and Baca. Smaller ones have formed along the base of the Four Hills, along Rincon Ridge, north and south of Monte Largo, around the south and east sides of South Mountain, and south of the San Pedro Mountains. The deposits have an arched fan shape. They are thickest and highest along a medial axis and thin in all directions from a mid-point on the axis. The alluvial fans along the Sandia front consist predominantly of granitic debris with minor quantities of limestone and sandstone. Torrential flow and rare mudflows have brought local strings of boulders and some blocks weighing up to 20 tons far out onto the fans (fig. 44). At the mouth of La Cueva Canyon enormous granite boulders have been debouched across a fan-form rock surface eroded into disintegrated weathered granite. The boulders of the thin alluvial fan are not the products of spheroidal weathering in place because some boul ders are of red granite or limestone derived from high on the mountain. Spheroidally weathered granite blocks as much as 5 ft in diameter have been found I to 2 miles away from the mouth of La Cueva Canyon. to 8 1948 The wide area of alluvium in T. 9 to 12 N., R. 6 Photo buiames Bollich, Louis Goldsmith, and Richard Huzarski, valley alluvium CREEK NEAR Lks HUERTAS E. is a piedmont of coalesced fans and FIGURE 45—STEPs ALONG LAS HUERTAS All FORMED BY A SERIES OF CALCAREOUS TUFA that is spreading into the interior Estancia Valley. PICNIC AREA. STEPS ARE WATER. SOME POOLS ARE 5 fans are Holocene in age. DAMS PRECIPITATED FROM THE LIME-RICH to 6 FT DEEP BEHIND THIN DAM WALLS. VALLEY ALLUvIUM alluvium inset within the wider slightly older Alluvial fans and valley alluvium are the youngest of valley valley deposit. The most extensive deposits of valley deposits. Valley alluvium includes the deposits of sand are in the Estancia Valley, shown on the and gravel along the bottoms of valleys, arroyos, and alluvium part of the geological map, where stream flow gullies and even the narrow stringers on top of alluvial eastern the many arroyos and sheet runoff spread sand fans. Only the large strips of such deposits are shown on from gravel in wide expanses. the geological map. Notable for length and width are and alluvium consists of central deposits trans those in the arroyos and canyons of Las Huertas (fig. Valley down the canyon or valley, and marginal 45), Tijeras, Una de Gato, San Pedro (fig. 46), Gonzales, ported contributed from adjacent hillsides and small Juan Tomas, Coyote, and San Jose. Some of these material accumulations of alluvium have been dissected during side canyons. Clay or Placita Marl—There has been some the last 100 years or so by gullies as much as 30 ft deep, Zandia literature involving the Zandia (San- and the bottoms of the gullies have floors of younger confusion in the

SLIGHTLY FIGURE 46—WIDE ALLUVIATED SAN ANT0NIT0 VALLEY, A SURFACE IS LEVEL OF THE ORTIz SURFACE TO THE NORTH. AND BLOCKS ON ALBU MODIFIED FIGURE 44—LARGE GRANITE BOULDERS AXIS OF SAN LARGELY ON SOFT CHINLE SHALE ALONG EMBuDITO ARR0Y0 AT EUBANK ERODED QUERQUE’S EAST MESA. ALONG KNor.i.s TOWARD PEDRo SYNCLINE. PHOTO TAKEN FROM SANDIA AND ABOUT 1.5 MILES WEST OF BASE OF BLvD. (SHOWN ON FIC. 4). OF SANDIA UPLIFT. THE NORTHWEST. SHOWING DISTANT DIP SLOPE MOUNTAINS NEAR GLENwO0D HILLS. 73

dia) Clay and Placita Marl. In his “Report on the geol known of these is Sandia Cave located in a massive ogy of that part of northwestern New Mexico examined limestone ledge at an elevation of about 6.980 ft and during the field-season of 1874.” submitted to the Chief about 80 ft above the bottom of the canyon floor. Ac of Engineers. War Department. Cope (1875. p. 996-997) cording to Hibben (1941, 3-5) all the caves described his visit to Placitas and wrote: p. show some degree of past human habitation, but only 2, In the intervals between the hills there is a deposit of indurated Davis and Guano, in addition to Sandia, are of any clay of 40 feet in thickness of post-Pliocene age. I obtained considerable size. Hibben teeth and other bones (p. 5) also mentions a large of Elephas primigenius subspecies cave “just below the columbi. from this bed, and found bones of old Ellis ranch near the head of Las the same species in Huertas Canyon.” place in the banks of the arroyo. Shells of Planothis. Phvsa, Typically all the caves, when first etc.. indicated the lacustrine character of the deposit. which entered for exploration, were blocked by fallen rock, may be known as the Zandia clay. washed-in debris, and calcareous tufa. The present entrances of several In his text, Cope does not mention the Placita Marl, of the caves may have been eroded back 10 ft or so since but in an accompanying sketch (Cope, 1875, fig. 3, they were originally occupied. p. Sandia Cave, 997), reproduced here as our fig. 60, the “Placita mans” excavated by solution in limestone of the Madera are shown, designated p and noted in the legend. Formation, is located high on the steep eastern wall of Two years later, Cope (1877, p. 25) wrote as follows: Las Huertas Canyon. 3.5 miles south of Placitas (fig. 47). The cave is tunnel-like, In the intervals between more than 450 the hills, there is a deposit of ft long, and 7 to 10 ft indurated clay of 40 feet in thickness, of in diameter. The slope is 72 ft in Postpliocene age. I 453 ft “or approximately obtained teeth and other bones of Elephasprimigenius subspe 9 degrees, somewhat less steep cies columbi than from this bed, and found bones of Elephants in the dip of the limestone beds so that the cave place in the banks of the arroyo. Shells of Planorbis, Physa, begins in one bed and ends in higher etc.. indicate a one” (Bryan, the lacustrine character of the deposit, which I 1941, 48). Boy Scouts have called the Placita marl. p. from Albuquerque had ex plored it in 1927-28. A ground sloth claw found by A footnote cites his 1875 paper. Apparently he Kenneth Davis aroused the interest of Frank C. Hibben changed his mind and decided to use Placita Marl and the U.N.M. Department of Anthropology began rather than Zandia Clay. excavation in 1936; excavations continued through 1940 In her lexicon, (1-libben, Wilmarth (1938, p. 1676) gave the age 1941). Three age levels were delineated. The of the Placita Marl as “Tertiary? (probably Pliocene and oldest or Sandia level, with its Sandia points, thought by Miocene),” and the age of the Zandia ( Sandia) Clay Bryan (1941, p. 58) to be somewhat older than 25,000 as Quaternary (p. 1907). In the past several writers have years B.P., contains mentioned the Placita Marl, generally regarding it as Bison antiquus (bison) equivalent to the Santa Fe Formation and of Miocene Camelops sp. (camel) Pliocene age. It seems clear that Cope meant to Elephas sp. (mammoth) Enow Mammuthus substitute Placita Marl for his Zandia Clay and that he, (Parelephas) sp.J both in 1875 and again in 1877, dated it as Quaternary Equus excelsus (horse) or post-Pliocene. fl’Iastodon americanus (mastodon) In his paper on Sandia Cave, 1-libben (1941, 6, 7) The overlying noted that p. Folsom layer, containing Folsom the lake in which the Placita Marl accumu points, was lated thought by Bryan to be somewhat younger than 25,000 years B.P., but possibly only 8,000 to 10,000 could never have been very large. As a result of the cutting of a years B.P. (discussion by Northrop, large 1959, p. 5-6; and arroyo. extremely deep exposures have been made. Hibben, 1961), contains permitting thorough study of these sediments. In the bottom of Bison this wash or arroyo. residents of Placitas found two ungrooved sp., near but smaller than taylori Folsom-shaped points similar to those from Sandia Cave. They Catnelops sp. (camel) presumably washed out of the Placitas deposits. Fire areas, Canis cf. lupus (wolf) usually accompanied by sporadic chips of flint, are fairly Elep frequent has sp. (mammoth) [now Mammuthus at several levels in the Placitas sediments. Most of these burned (Parelephas) sp.1 areas occur at a depth of some 9 feet below the present surface Equus on what appears to be an old soil level or near occidentalis (horse) stratum darkened by vegetable material. Robert Ariss, of the Nothrotherium sp. (ground sloth) Department of Geology of the University of New Mexico. has recovered The uppermost layer, possibly a few thousand a variety of Pleistocene remains from these deposits to less including horse (probably Equus excelsus) and mastodon. than a thousand years old, contains Cervus sp. (elk) Erethizon CAvEs, ARTIFAcTs, AND FOSSILS sp. (porcupine) Neotoma sp. (wood rat) Several caves of Quaternary age occur in the Madera Nothrotherium sp. (ground sloth) limestone along the east side of the Sandia Mountains. Odocoileus sp. (mule deer) Embudo Cave is high (8,940 ft) in the mountains a short Ovis canadensis (mountain sheep) distance south of the Sandia Peak ski area, along a Tadarida mexicana and other spp. (bat) forest trail to the crest in projected sec. 4, T. II N., R. 5 Ursus sp. (bear) E. (map 2). In recent years the cave has been used by The Hibben (1941) paper, with an appendix the University of New Mexico Physics Department by Bryan, for illustrates points, scrapers, and other artifacts. underground measurements of cosmic radiation. The Charcoal specimens from fire hearths of the best known caves lie along the east wall of Las Huertas Sandia level were dated by Libby in 1948 (Hibben, 1955) Canyon in sec. 22, T. 12 N., R. 5 E. (map 2). The best at 17,000+ and 20,000+ years B.P. In 1952, Hibben sent ______

74

A B

-r ,tEi

SCA&.E T.

‘C ,. z EXPLANATION LI Recent deposit Ochre Clay LI SCM,E Calcium carbonat. crust Sandia deposit Limestone — LI 1/SWETE1t FoIom Charcoal Sandstone AK

ADAPTED FROM HIBBEN, 1941. FIGS. 5, 7). A, FIGURE 47—CROSS 5ECTtONS OF SANDIA CAVE (HIBHEN, 1961; LOCATION OF THE CAVE tN LAS HUERTAS CANYON; B, LONGITUDINAL EAST-WEST CROSS SECTtON SHOWING GENERAL SHOWING STRATIGRAPHY OF CAVE DEPOSITS. TRANSVERSE CROSS SECTION OF THE CAVE, 15 M FROM THE ENTRANCE, 270) commented: two specimens of ivory (one from a mammoth tusk and Witthoft (1962, p. one from a mastodon tusk) to H. R. Crane (Hibben, It is hard to believe that Sandia can be other than a local type. comparable 1955; Crane, 1955) for carbon-14 dating. In 1954, a specialized variant or derivative of the Clovis few very poorly known eccentric forms from other areas. third fragment was submitted. Crane concluded that to a was at least 20,000 years old and one of the Sandia tusks A few years later Wiley (1966, p. 41) wrote: that the others were about 25,000 years old, but noted According to G. A. Agogino, one of the recent investigators, that there is strong suggestive evidence that Sandia points, while The great age of the Sandia tusk naturally raises the question antedating the Folsom points. may originally have lain in the whether it is contemporary with the evidence of habitation same geologic stratum with them and not in the layer below among which it was found, or whether, instead, we have the yellow ochre. Redeposition to the layer in which they were discovered that among the men who inhabited the cave there reported found was probably the result of rodent activity were archeologists who collected and brought home tusks which carried the artifacts through the cracks and fissures into belonging to earlier times. the sub-ochre layer. This reinterpretation would mean that the Sandia culture is approximately the same age as the Llano or On the other hand Hibben (1955) observed that meat Clovis complex. had been “cut from the bones, as is indicated by occasional scars on the bone surfaces. Subsequently the More recently, Agogino (personal communication, bones were cracked and broken lengthwise to extract October 1, 1974) writes: the marrow.” Based on several years research regarding Sandia Cave, I feel Several workers have disputed the 25,000-year dating that the age of the Sandia level is roughly that ofClovis, that is of Sandia points. For example, Mason (1962, p. 229) roughly 11,500 years old. This is based on geologic evidence themselves. The noted that plus typological characteristics of the artifacts earlier age of more than 25,000 was based on the belief that the the dating of Sandia points is uncertain. Radiocarbon Pleistocene period ended roughly 25.000 years ago rather than dates alleged to pertain to the Sandia cultural complex have the currently accepted age of 10.000 years ago. been disputed, and there is little but confusion to be gained by appealing to them. All that can definitely be stated is that In addition to the vertebrate remains found in Sandia of Sandia is earlier than Folsom by an unknown number years, Cave a most spectacular fossil discovery was made in at least at the type site. 1956 by J. Nicoll Durrie, Jr., then aged 9, while hunting In commenting on Mason’s paper, Agogino (1962, p. arrowheads near Tree Spring (on the wooded east slope of 247) stated that of the Sandia Mountains about 3 miles northwest several remarkably well- the late E. H. Sellards informed me Sandia Park). He found Shortly before his death jaw of Mastodon that Sandia points were reported from apparently the same preserved teeth and part of the cultural honzon as Clovis points at the Clovis type site, eastern americanus (fig. 48A). This occurrence at an elevation of New Mexico. The discovery had been made by a student 8,470 ft may constitute an altitude record in New himself associate and since he had not uncovered the material for the species. Jerry Harbour, a University of material “in situ” he hesitated to Mexico and had not seen the excavated the left lower jaw from announce the discovery publicly. New Mexico student, 75

A—SIDE VIEW OF TWO MOLARS (LOWER LEFT, 2n AND 3D MOLARS) OF Mastodon americanus, FROM NEAR TREE SPRINGS. NOTE ABRASION OF CUSPS AT UPPER LEFT. COMBINED WEIGHT IS A LITTLE LESS THAN 8 POUNDS.

B—TWO VIEWS OF A SINGLE MOLAR OF THE MAMMOTH. Mammuthus (Pare!ephas) co!utnbi, FROM ALBUQUERQUE GRAVEL PRODUCTS COMPANY NORTH EDITH PIT. ALBUQUERQUE. AT LEFT IS VIEW OF GRINDING SURFACE AT RIGHT WEIGHT IS 12.5 POUNDS. IS SIDE VIEW.

F(GURE 48—MASTODON AND MAMMOTH TEETH ON EXHIBIT AT UNIvERsITY OF NEW MExICO GEOLOGY MUSEUM (SCALE. INCHES).

only a few inches below the surface. The teeth and jaw Actually, are proboscidean remains, including tusks and not mineralized and appear to be only slightly more molars, decomposed are not uncommon in nearby areas, such as than some bones of modern animals found gravel pits in within the city limits of Albuquerque, in the the same area. This individual may be only a few Estancia thousand Valley, and in the Isleta Caves south of the years old. city. The second and third left lower molars are on exhibit Lambert (1968) found Bison, Equus, turtle, and a in the tJ.N.M. Geology Museum. Mastodons were poorly preserved mammoth or mastodon tusk in about the height of the modern Indian elephant the but Edith Formation (Late Pleistocene) at the Albuquerque much stockier. They were forest-dwelling animals Gravel Products quarry (sec. 3, T. 10 N., R. 3 E.). A whose teeth were adapted for a browsing diet, eating mammoth molar (fig. 48B) found at the same quarry chiefly leaves. Mammoths were larger than mastodons was donated to the Geology Museum by John H. Doyle. and were plains-dwelling animals whose teeth were Mammoth remains have been found at the Chavez adapted for grazing herbs and grasses. quarry (sec. 26, T. ION., R. 2 F.). Extinct forms of bear, 76

DIKE C(JTLING SANDIA GRANUrE. Photo by Gene Polk. Marvin Mathenv. and John Lookingbill FIGURE 50—LAMPR0PHYRE ROADCUT ALONG 1-40. SEC. 25, T. ION., R. 4 E. FIGURE 49—H0RNBLENDE ANDESITE DIKE IN MESETA BLANCA A SHORT SAN1TONE. Cur ALONG ZAMORA RD. (OLD US-66) DISTANCE SOUTH OF GUTIERREz FAULT. moved across NM-44 and into the steep part of the canyon below. There are excellent exposures of crum camels, and horse, as well as proboscid two genera of pled and broken beds in the roadcut just north of the in the Isleta Caves (Harris and eans, were found entrance to the ski run. The steep part of the slalom is and ground sloth are known Findley, 1964). Camel the pull-away face back of the slide. The lodge and the at the south end of the Manzano from Manzano Cave, low beginners’ slope is on a flattened surface of the 35-36). Mountains (Hibben, 1941, P. slide. The slide has probably stabilized, but it is not out of the realm of possibility that with heavy or prolonged LANDSLIDES AND ROCK FALLS precipitation the slide could move again. Other hillside Landslides are masses of rock that have moved along slides occur at Cole Springs, northwest of the Hobbies the ground under the influence of gravity. Rock falls store, and at several points between. involve free fall of rock from cliffs or steep slopes. Many Most of the high bare faces on Sandia escarpment are landslides have occurred on the eastern slope of the kept bare by severe weathering. Large joint blocks and mountains-but none occurs on the western side because slabs continually work loose, and debris of this Sort of more resistant rocks and stronger disposition of occurs in many places at the bases of the cliffs. An internal structures such as joints and bedding. unusual rock fall was observed in 1936 by Mr. E. W. Doubtless numerous rock falls have occurred on the Cottam of the Forest Service (Workman and Kelley, so western side, but they are generally so small and 1940). Lightning struck a prominent point north of the scattered as to go undetected. upper tower along the Sandia Peak tramway and Landslides are common on the eastern slope where knocked ofT a large joint block of granite 40 ft wide and bedding nearly parallels the surface allowing individual 150 ft long, a volume of some 2,000 cubic yards. The beds, a group of beds, or weathered mantle to slide fresh face of the slide is still visible from the tram car Eleven landslides have downhill on bedding planes. (Kelley, 1969, p. 73). been mapped (map I) and many more, either unseen or too small to show, are present. Two of the largest occur I to 2 miles north of Sandia Park. The largest of these, nearly I square mile in area, is near the head of Tecolote Canyon. The other is a long narrow mass on the east dip slope of the ridge east of Doc Long picnic area. both of these slides are chaotic masses that have been broken and jumbled in sliding probably no more than a few hundred feet down steep eastern slopes. Another large slide occurred high on the Madera dip slope 2.5 miles south of Placitas. A thick limestone slid on a shale zone and was broken into chaotic blocks; the downward movement lowered the surface of the upper area of the slide by 30 to 40 ft. A small slide 1 mile southeast of Palomas Peak, near the head of Tecolote - . - haIfa mile. IS Canyon, has moved down the canyon about FIGURE 51—M0Nz0NITE SILL IN MANCOS SHALE. HOGBACK SEC. 4. T. 12 N.. R. A similar canyon slide exists near the head of Madera ALONG SAN PEDRo CREEK AT WESTERN EDGE OF MONZONITE IS Canyon at the bottom of the Sandia Peak ski run. The 6 E. Two SMALL FAULTS HAVE DISLOCATED SILL. THE MEDIUM GRAINED. slide broke loose from the Upper Slalom slope and DENSE AND FINE TO 77 Structure

REGIONAL SETTING uplift of the Sandia Mountains land of the Manzano and more southern rangesj For this great movement I propose the The Sandia area consists of several structural ele name of “Sandia uplift. ments: we will discuss the regional Setting, then the Sandia area and its elements. Selection of structural EXTENT elements of an area is difficult and somewhat subjective. The Sandia uplift is an eastward-tilted fault block 22 However, it is desirable to describe large elements miles long and up to 12 miles wide (map 3); it is within which the details of structure may be organized bounded on the west by faults separating the uplift from bra better analysis of the mechanisms and origins. the Albuquerque basin. The boundary on the east Within a region there are usually is several magnitudes indefinite because in most places the tilted slope merges of deformation; in central New Mexico the north-south with the western limbs of basins or synclines that lie on structural belt of the Rockies is of the greatest magni the east. To the northeast the uplift merges into the west tude. The Rockies belt can then be divided into units of and south flanks of the Hagan basin; on the east the second order; in the report area these are the Rio uplift merges into the San Pedro syncline and the Grande trough and its two flanking belts of tectonically Tijeras basin. On the southeast the uplift is bounded related uplifts. In this classification by the Sandia area lies the Tijeras fault, which sharply separates the Sandia astride two second-order tectonic elements, the Rio uplift from the structurally lower Manzanita uplift (fig. Grande trough and the eastern flanking belt of uplifts. 52). The Tijeras fault is the southeast boundary of a The eastern flanking belt includes several third-order wedge that comes to a point at the southern end of the elements such as the Sandia, Manzanita, and Manzano Four Hills, where the uplift dies out. This termination of uplifts, and others; the Rio Grande trough consists of the uplift is several miles south of Tijeras Canyon, two basins of third order, the Albuquerque and the which topographically separates the Sandia and Santo Domingo. Thus, Manza the structural description of this nita Mountains. However, uplifts and physiographic area involves a number of third-order elements and, mountains are not always the same and the emphasis where necessary for understanding, still lower order here is on the uplift. Where the structural boundary is elements. In an area such as the Sandias any particular absent or poorly defined, as along most of the eastern fault, fold, or set ofjoints, may be of fifth or sixth order side of the uplift the boundary must be chosen arbitrar of magnitude in the overall tectonic development. ily, for the flank of an uplift is also the flank of an This type of analysis may not be simple, as the several adjoining syncline or basin. The Tijeras fault is a good elements of structure are commonly of distinctly dif boundary to near the area where it crosses NM-14 and ferent ages and origins. For example, the ages of the begins to diagonally cross the Tijeras basin with dimin Precambrian structures are greatly different from those ishing throw. Northward from there the boundary is of the third-order structural elements. Futhermore, the arbitrarily chosen paralleling NM-l4 on the west for crustal depth at which the Precambrian deformation about 8 miles to where the road turns east across San took place represents possibly three or four times the Pedro Creek. It is then drawn northwestward along the observed depth of deformation of the Sandia uplift or Madera-Abo contact to the Seco fault which drops a the Tijeras basin. Less obvious are the probable differ southwestern reentrant of the Hagan basin into the ences in age and modes of deformation between the Sandia uplift. North of the Seco fault the boundary Sandia uplift and the Hagan is basin, on the one hand, followed to Tejon Canyon and thence along and the Monte Largo-Tijeras the uplift belt or the South ing Ridge and Frisco Springs faults to Mountain-San Pedro porphyry a termination structures on the other. with the San Francisco fault. The northwestern In view of such differences it is necessary to add to boundary is then chosen successively southwestward magnitude of deformation the sequence and mode of along the San Francisco, Suela, and Placitas deformation in delineation faults to of the structural elements. the big west side Rincon fault. For older elements assignments of magnitude or desig nation of second or third orders are uncertain. As an WEST SIDE FAULTS example the northeast-trending structural belt including the Tijeras fault, Tijeras graben, and Monte Largo horst Uplift of the Sandia block occurred primarily on faults is probably older than the Sandia uplift. Whether it was near the western base of the mountains. In nearly all such a second-, third-, or fourth-order feature at the time of tilted blocks the main fault is either presumed or found its origin is uncertain. The descriptions that follow are to be very near the base (fig. 53). In many tilted of geometric elements; following the descriptions the fault blocks there is a set of parallel faults which elevate mechanics and origin of the whole structure are con the uplift by step faulting. Step faulting is sidered. difficult to detect unless there are stratified rocks that show dislocation of beds. Whether one or several faults SANDIA UPLIFT are present their traces are commonly not exposed owing to Johnson (1903, covering alluvial deposits. The presence of one P. 456-457) was apparently the first to or more use the term Sandia faults near the base of the Sandias is well uplift. In describing the Cerrillos indicated area, he wrote: in one or two places by great stratigraphic displacement between the top and bottom of the uplift The movement which produced this uniform eastward dip (map 4). was probably the same which resulted in the great monoclinal The actual exposure of a fault at the base is seen in 78

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FIGURE 53—ERoDED FAULT SCARP ALONG CENTRAL PART OF SANDIA UPLIFT. only three places. One of these is at the mouth of Tijeras exposed with lowermost Santa Fe beds downthrown Canyon along the east side of Four Hills Road 0.4 mile against Mancos Shale (fig. 58). Although not an actual south of the Western Skies Motor Hotel. The exposed fault surface exposure, the several relatively undissected fault surface dips westward about 55 degrees, with triangular fault-scarp facets along the base of the uplift gravel of the Santa Fe Formation downthrown against north and south of the mouth of La Cueva Canyon are the Sandia Granite. A second exposure is in the form of physiographic evidence of youthful, actively uplifting a Holocene fan scarp (fig. 57) at the base of Rmcon fault blocks so common in the Basin and Ridge. This exposure can be seen at the Range edge of the Province of western Nevada and eastern California. Precambrian outcrop and is traceable for about 1 mile. Along the main crest of the uplift the The other exposure of this fault occurs top of the across NM-44 Precambrian is 9,000 to 10,300 ft above near the northern end of the mountains sea level (not a (sec. 1, T. 12 N., large difference), but along the R. 4 E.). Several closely spaced faults basin margin the are traceable but difference in projected downthrow the best exposure is in a roadcut where between Morrison Santa Fe gravel and Madera beds could amount is downfaulted against Mancos to 5,000 to 6,000 ft. Shale (fig. 58). Therefore, the basin block About 1.3 miles north appears relatively much of 1-40 (sec. 14, T. 10 N., R. 4 more deformed internally E.) is a small inselberg than does the uplift bordering of Sandia Granite and Madera the fault. limestone in alluvium. The apparent vertical displace In addition to the main ment of the limestone from Sandia and Rincon faults equivalent beds capping the which lie very near mountain 3 miles the base of the mountains, it east, is nearly 3,000 ft. The trace of appears possible the Sandia that parallel buried faults may lie west fault is presumed to lie buried beneath the beneath alluvium alluvium and east in granite. It is to be noted between the outlier inselberg and the main that two faults are labeled Sandia on map 1, one near outcrop of the mountain granite (map 4). As illustrated the base of the range and another buried I to 1.5 by Kelley (Kelley and Read, 1961, 18), the miles p. limestone to the west in the stretch along the Pino Canyon-Bear may be projected (without faulting) as the west limb of Canyon reentrant. Perhaps the entire belt of roughly an anticline. However, the general evidence strongly parallel faults, both in the granite and favors a fault just east of the inselberg in the alluvium as shown on the should be referred to as the Sandia geologic map (map 1). fault zone. Because of the homogeneity of the granite, The Sandia fault faults therein are not appears to terminate near the readily evident. Crushing entrance to Juan Tabo and shearing along the faults Canyon (fig. 54) in sec. 2, T. 11 have made the rocks N., R. 4 E. The especially susceptible to weather termination is at a diagonal cross-ramp ing and erosion. fault which These faults, therefore, should show jogs the uplift westward to the Rincon fault up physiographically (fig. 54). In the reentrant as short aligned canyons, spurs, there is another inselberg, springs, or saddles. in this instance, Chinle A number of such probable faults and Morrison beds. The two are shown on the geologic formations are considerably map. especially in Bernalillo disturbed but appear to dip County. Five are mostly toward the shown in T. 10 N. that could have Sandia Granite and strike northward been part into the Rincon of the mechanics of uplifting of the range. metamorphics. A fault separates the Another Chinle (west) set of such faults occurs south and west of from the Morrison (east). Vertical separa Sandia tion along Peak in the Elena Gallegos Grant. Ellis (1922, the bounding faults must be at least 10,000 ft, p. and the 30, p1. 1) believed that a great fault zone followed the structural implications are considerable (fig. 66). bases of the high cliffs in the granite for almost the full The outcrop poses puzzling structural problems not the least length of the uplift, and he pointed to a single fault of which is the disparity in ike age of the outcropping scarp 1,000 to 1,500 ft high between Pino Canyon and rocks just west of the fault at the two inselbergs Sandia Crest. There are a number of prominent shields described above.The third exposure is in the roadcut and faces, orientations of which are controlled by either on NM-44 where the Rincon fault is again faults or closely spaced joints forming weak sheeted 80

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AND PRINCIPAL FAULTS. AREA SHOWING TRIANGULAR FAULT FACETS 54—VERTIcAL AIR PHOTO OF JUAN TAB0 FIGURE IN SEQUENCE OF INCREASING HEIGHT. ARE NUMBERED SOUTH (i) TO NORTH (5) FIvF LITTLE-DISSECTED FAULT SCARP FACETS FACETS 4 AND 5 ARE BEST PRESERVED. 81

FIGURE 55—TRIANGULAR FAULT FACETS AT MOUTH OF LA CUEvA CANYON. GRANITE Shield IN BACKGROUND.

FIGURE 58—RINc0N FAULT IN ROADCUT ON NM-44. SANTA FE FANGLOMERATE DROPPED AGAINST MANCOS SHALE.

FIGURE 56—FAULTED SANDIA GRANITE IN CANYON SIDE NEAR BorroM OF LA Luz TRAIL. THIS FAULT FORMS THE BASE OF THE have much more PROMINENT TRIANGULAR FAULT-FACETED stratified limestone preserved above SPURS NORTH AND SOUTH the OF LA CUEvA CANYON. Precambrian basement along the escarpment and base. These beds are displaced by both longitudinal and transverse faults that are zones, that do not follow a line or even a single zone clearly a part of the Late Tertiary uplifting of the tilted paralleling the crest of the range. Many of the faults fault block. By analogy and many of similarly positioned sheeted zones in the granite are Precambrian but faults in the Precambrian of the Sandias probably some of them may have had renewed displacement played a part in the Late during the uplift of the mountains. Tertiary uplifting even though evidence is not direct, owing to The San Andres Mountains of south-central erosion of the once-present younger sedimen New tary beds. Mexico, a long uplift tilted similarly to the Sandias, EAST SIDE FAULTS Faults along the east side of the uplift are different in arrangement and nature from those on the west side. There is very little extension or connection of faults of one side to the other and instead, a minor group of small cross faults along the crest of the uplift appears different from those on either side. The east side faults appear to be more numerous than elsewhere in the uplift and this is puzzling because the greater dis placements have occurred on the west side. However, the smaller number of faults on the west side may be more apparent than real, as suggested previously, because of cover and difficulties of recognition. The east side faults form a complicated and varied • - pattern. Overall, the system is dominated by faults of FIGURE 57—H0L0cENE FAULT northward SCARP ALONG RINC0N FAULT. to north-northwestward trend which are SHADOwED LINE ALONG THE BASE OF RIDGE ACROSS ALLUVIAL FANS arranged in a right echelon. IS SCARP AS MUCH The echelon is most AS 10 TO IS Fr HIGH CAUSED BY SUDDEN MOVEMENT apparent in the southern part where PROBABLY WITHIN LAST 100 YEARS. Abo red beds are dropped in zigzag outcrops by 4 of the 5 principal faults 82

where it merges into the southern end of the Agua the echelon. These 4 faults are Flatirons, Cañoncito, of Sarca fault. The large landslide and springs in the area Wolf Spring, and San Antonito. The first 3 are about appear to be related in part to this terrace. halfway up the dip slope and are positioned about degrees of the high part where the dips of 10 to 15 TERMINATIONS increase to dips of 15 to 30 degrees or steeper. At the uplift terminates on the north at the right southern end of the echelon set the Flatirons fault The Sandia Rio Grande trough from the Albuquerque impinges on the big Tijeras fault zone and offsets offset of the the the Santo Domingo basin. The termination is several of the splays of the Tijeras fault. Some of basin into exposed in the Placitas area (fig. 60), where most severe and complex local deformation of the uplift excellently of a much broken nose that plunges into the occurs near this junction. Beds become steeply dipping it consists also trough as a ramp between two trough to vertical and commonly overturned; they have Rio Grande the Rincon and San Francisco faults (fig. been severely squeezed and crushed, with some thin boundaries, lower (northern) part of the ramp is covered stratigraphic units having been locally faulted out of the 63). The Wolf by the trough-filling Santa Fe beds and normal sequence. The Flatirons, Cañoncito, unconformably a 3- to 4-mile stretch between the Spring, and San Antonito faults probably dip westward pediment gravel along of the Rincon fault on the west and the and are downthrown on the east, with left offsets northward-dying San Francisco fault to the east Abo-Madera contacts of as much as one mile. There is a southward-terminating The San Francisco fault is the main possibility also of minor components of left slip, and the of the nosing ramp. the Rio Grande trough and the mechanics of deformation has a sense of counterclock boundary between the Rincon fault is a trough wise motion. Hagan basin, whereas uplift. The Barro fault contrasts with the other members of boundary with the Sandia the Precambrian together with sharp the echelon in being upthrown on the east, and in this Erosion into turning of blocks by the Placitas and respect it correlates with the big Ellis fault and lesser breaking and have destroyed or modified what was related faults northward along the eastern side. The Agua Sarca faults curved plunging anticline or Barro and Ellis faults bring up small tilted fault blocks once a more smoothly of structure contours along the crest in piggy back fashion and with the same motion as that nose. Projection depict the uplift plunging north for the entire Sandia tilted block. Throw on the Barro and west of Placitas about 3,000 ft in 3 miles, from Sandia fault is as much as 1,800 ft, and that of the Ellis fault ward at a rate of Placitas fault (fig. 62). North of the fault about 1,000 ft (fig. 59). The Barro fault curves broadly Crest to the ramp is much steeper, amounting to at from a northward trend in its southern part (parallel to plunge of the ft in 3 miles (map 3). the Sandia uplift) to a northeastward trend and possible least 10,000 western half of the Placitas fault (fig. 61) connection with the Seco fault (part of a transverse set South of the east-west hogback held up by northward- of faults descending into the Hagan basin). there is a long beds. At the eastern end of the The Ellis fault is part of an irregular right-echelon set dipping Madera only a short distance across a saddle of about seven faults that have broken and jostled slices hogback it is to a spur of the uplift capped the northern half of the back slope of the Sandias. In eroded into Precambrian of Madera. Up the spur this set most of the throws are up on the east but a few by north-northeastward-dipping dips curve gradually into normal are upthrown on the west. Other principal faults of the and to the east, uplift back slope. echelon are from southwest to northeast: Capulin eastward dips of the uplift northern end of the Sandia Springs, Lagunita, Palo Duroso, Apache, and Perdiz Within the north-dipping north-trending faults which (map 1). uplift are several short Rincon and San Fran High along the northern dip slope of the mountains appear to have acted with the ramped block down to the there is a local structural terrace which extends north cisco faults to step fault the to west the Suela fault (just ward in T. 12 N., R. 5 E. from section 29 into section 20 west. These are from east east of the village of Placitas), Pomecerro or Fish Hatchery fault, the Agua Sarca fault, Caballo fault, and a short split from the Rincon fault in secs. 1, 12, T. 12 N., ft. 4 E. Downthrow to the west is indicated by left offset of several of the north-dipping formations; in the case of the Pomecerro fault the throw is more than 2,000 ft and horizontal separation of the Dakota is nearly 4,000 ft. The large San Francisco fault has a problematical southern termination. Much of the termination is covered by alluvium at Tecolote, and beneath the valley at Tecolote the fault appears to either curve into an offset end of the Placitas fault or to continue up Las l-Iuertas Canyon and splay into the east side echelon faults described above. The latter concept is preferred. The westward branching Placitas fault does not bound OF LAS HUERTAS it contributes to the northward FIGURE 59—VIEw NORTHWEST FROM HEAD the trough so much as LIMESTONE LEDGES CANYON. DiP SLOPE ATTITUDE OF MADA down-ramping of the uplift. MADERA IS SHOWS IN NORTH SIDE OF OSHA CANYON. A special feature of this portion of the Sandia SANDIA GRANITE DOWNTHROWN ON THE WEST SIDE AGAINST southward-wedging Las ALL GRANITE. termination is the narrow ALONG Ems FAULT. INNER CANYON WALlS ARE 83

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FIGURE 60—CopEs (1875) DIAGRAMMATIC SKETCH. SITE OF VILLAGE MARKED BY Diagrammatic HOUSES. ONE TO LEFT OF GULLY, FOUR TO RIGHT. sketch of the Zandia Mountains, looking east by south across the village of Placita: g, granite; c, Carboniferous s red beds, looking like gl, Galisteo sandstone; 4, Cretaceous limestone; Nos. 4 and 3; p, Placita marIa; gr, gravel mesas. Huertas graben floored by Abo beds. The Abo and some Meseta Blanca beds are downthrown against Precambrian and Madera beds on the east side of the graben, and the throw could be 2,000 ft or more at the northern end. On the west side of the graben the Abo is stepped down by two faults, one along NM-44 and another to the west along Oso Creek. The graben is tilted eastward. Just to the west of these faults is the short Cuchilla Lupe horst which is surfaced by up- thrown Madera Formation with Abo on either side. In this section of the northern end of the Sandias there is considerable breaking and jostling of small blocks up and down just south of the Placitas fault. North of the Placitas fault jostling has affected many blocks in the northward and northeastward plunging Photo by Donald A. Myers FIGURE 61—AIRvIEw ramp structure that descends TO THE SOUTHEAST SHOWING NORTHERN END toward the Santo OF SANDIA Domingo MOUNTAINS. UPPER RIGHT SHOWS BRUSH-COVERED basin. Additionally a disrupted monoclinal SLOPE ERODED ON SANDIA FORMATION OVERLYING CLIFFS OF flex results in steepening of dips of 25 to 30 degrees SANDIA GRANITE. STRONGLY LEDGED CREST AND EAST DIP SLOPE IS south of N M-44 MADERA to dips of 45 to 70 degrees north of FORMATION. CENTER AND LOWER RIGHT SHARP. ERODED the HOGBACK road. The steep limb passes HILLS ARE CAPPED BY NORTH-DIPPING MADERA BEDS beneath basal Santa Fe FAULTED beds with DOWN AND ROTATED TO FORM THE NORTH RAMP a surface of unconformity below the Santa TERMINATION OF THE UPLIFT. ON THE UPLIFT BACK SLOPE CAN BE Fe. A tectonically significant feature not heretofore SEEN PALOMAS PEAK AND OTHER SMALL PIGGYBACK FAULT BLOCKS. recognized is that the Santa Fe beds are also consider ably deformed but in a different manner and direction. Although some faulting is involved, the post-Santa Fe deformation takes the form principally of several north- northwestward-trending anticlines and synclines that plunge down the ramp (fig. 63). Three erosional lobate forms in the Santa Fe outcrop pattern result from these folds. The anticlines are stripped into the steep pre Santa Fe formations, and the synclines are occupied by the Santa Fe lobes which stand as mesas. The middle (Lomos Altos) syncline of the mesa, 1.5 miles west of Placitas, and the two flanking anticlines are the main elements of this post-Santa Fe deformation. The west ernmost syncline is obscure and perhaps modified by the Rincon fault. The easternmost syncline northeast of Placitas is likewise obscure, possibly disturbed by the San Francisco fault, and also complicated by a fault and erosion along Las Huertas Arroyo. The southwest ern limb of the Lomos Altos syncline has a dip of as much Photo by Donald A. Myers as 40 degrees, and the west limb of the FIGURE 62—AIRvIEW Las EAST OF PLACITAS AREA. MoEzuMA RIDGE, L-Iuertas syncline dips as much NEAR UPPER LEFT; MoNTE LARG0 as 45 degrees. The ON SKYLINE NORTHERN LOW DIP eastern SLOPES OF SANDIA limbs of these synclines are low dipping MoUrAINS BACK OF THE VILLAGE; LEFT CENTER and not DISSECTED HILLS (SEE easily seen. FIG. 41) ARE TILTED, OLD SANTA F BEDS. TEXAS-NEW MEXICO PIPELINE, The SEEN FROM TOP RIGHT TO LOWER northern, ramp termination of the Sandia uplift RIGHT CORNER, TRANSPORTS PETROLEUM FROM UTAH TO TEXAS. LAS is important in displaying evidence of 3 distinct periods FIUERTAS WASH, LOWER LEFT. of deformation. The first was before early Santa Fe and 84

MONTEZUMA TROUGH TO HAGAN BASIN. SECTION CROSSES FIGURE 63—STRUCTURE SECTION A-A’ FROM Rio GRANDE PLACITAS. (LINE OF SECTION SHOWN ON MAP I.) SALIENT AND STRUCTURAL OOWNRAMP NORTH OF

considerable upthrusting and overriding at the second followed early Santa Fe deposition. In sec. facilitated may the Tejon salient and along the south-trending thrusts. 36, T. 13 N., R. 4 E. a north-trending fault, which the Kelley and Reynolds (1954) suggested that these struc be a splay of the Rincon fault (fig. 61), offsets is tures might be older than the late Tertiary block Galisteo and folded lower Santa Fe conglomerate and faulting and possibly Laramide in age. Renewed move younger than the first two deformations. The steep ments may have readjusted the blocks along these faults Galisteo beds near the fault show left drag. parallel with in late Tertiary. similar drag on the San Francisco fault. The basal Santa The southern termination of the uplift is entirely Fe fanglomerate east of the fault consists predom different from the northern. The boundary is the Tijeras inantly of red Abo sandstone with no Madera or fault which lies mostly in Precambrian terrane. The Precambrian fragments, indicating that only Abo sur most obvious termination is in Tijeras Canyon where faced the uplift (fig. 64). West of the fault the down- the trace of the fault passes from the Precambrian into thrown Santa Fe fanglomerate consists predominantly strata. To the north Pennsylvanian strata of Madera fragments with minor small fragments of Pennsylvanian lie high along the Sandia crest and dip uniformly Abo and no Precambrian. Thus, the nearby uplift had eastward to the canyon bottom and the fault. To the been stripped of most of its Abo. but uplift and erosion of Tijeras fault Pennsylvanian beds are lower and had not yet affected the Precambrian. The Madera-bear south strike northeastward parallel to the fault. Projection of ing Santa Fe may be several hundred feet stratigraphic this Pennsylvanian base upward to the fault shows (map ally above the Abo-bearing Santa Fe. the south side of the fault is 800 to 1,200 ft In describing the extent of the Sandia uplift, the 3) that than the projected trace of the north side base to Frisco Spring fault and its branches southward along higher fault. Stratigraphic projections worked out in struc Tejon Canyon were selected as the boundary between the (map 3) suggest a long southward-plung the uplift and the Hagan basin. These curving, high- ture contouring for the southern point of the uplift, from a angle reverse faults dip from 60 to 90 degrees toward ing anticline Sandia Crest of about 11,000 ft on top of the the west or south. Here the uplift is raised steeply and high near to about 7,000 ft near Four Hills in 11 sharply against and over the edge of the Hagan basin. Precambrian However, in a strict sense there may be no At the salient near Tejon, upthrusted Abo rides onto miles. termination on the south—rather, just a change of Santa Rosa Sandstone with all the Yeso and San of uplift across Tijeras fault into the Manza Andres having been overridden and cut out locally. magnitude of the nita uplift. Reynolds (1954, p. 45) believed the western part Montezuma fault to be a left tear fault (map 1) which MANZANITA UPLIFT The Manzanita Mountains are a broad dissected plateau. which lies between the Sandia Mountains on the north and the Manzano Mountains on the south. Most of the uplift is south of the report area. The length, north to south, is about 15 miles and it extends from the western escarpment some 15 to 20 miles to the east where it merges into the Estancia Valley. The western escarpment into the Rio Grande valley is deeply indented by erosion up to an irregular crest line at altitudes of 7,500 to 8,000 ft. which is some 1,000 to 2,500 ft lower than the crests of the more strongly uplifted and tilted mountains to the north and south. The northern boundary of the uplift is at the Tijeras -a-—— fault to about the town of Tijeras, thence southward and (LEFT) DOWNFAULTED along the FIGURE 64—SANTA FE FANGLOMERATE then northeastward around the Tijeras basin SANTA FE FANGLOMERATE. SEC. 36, AGAINST GALISTEO AND OLDER Chamisoso and Gutierrez faults. The uplift merges T. 13 N., R.4E. 85

gradually with the Estancia basin a short distance east Bajada or Rosario fault (as mapped farther north); of the area. The southern end of the uplift is just north farther southward the east structural edge of the basin of Mosca Peak of the Manzano uplift and about at the may be followed along the San Pedro fault and Bernalillo-Torrance county line. The western boundary eventually along the Barro fault of the Sandia Moun is outside the area of the Sandia geologic map. but like tains. The western side of the basin coincides in part the Sandias the Manzanitas are bounded by the Rio with the northern end of Sandia uplift and with the Grande trough. The structural descent San into the trough is Francisco fault, which bounds the Santo by both faulting and downwarping. Donungo basin of the Rio Grande trough. However, the San Francisco The Manzanita uplift is tilted broadly and rather fault either dies out or is buried in the northern part of gently eastward. Dip across the plateaulike structure the basin, and Santa Fe beds merge with those probably averages no more than in the I to 2 degrees. northeastern part of the Hagan basin. In Santa However, very low, broad open anticlines Fe time and synclines the 1-lagari basin was a reentrant structural interrupt the low eastward inclination. embayment In the north- of the Rio Grande trough (Kelley, 1954). central part of the uplift a north-trending set of faults The Hagan structural basin has an embayment on the centers along the Cedro Canyon area. Throws on these southwest that lies between 2 prongs of the Sandia faults generally do not exceed 400 to 500 ft and are uplift. These are the Montezuma salient on the north commonly much less. The principal feature produced and the Madera salient on the south. The boundary of by these faults is the elongate Cedro Peak horst. The the basin embayment with the Madera salient is along horst is bounded by the Otero fault on the west and the the Seco and Barro faults. On the geologic map the Cedro fault on the east. The Chamisoso fault, which is embayment can be easily visualized by. following the probably related to the overall subsidence of the Tijeras Abo-Madera contact. However, northward along the basin, crosses the Cedro Peak horst. The Chamisoso west side of the embayment, the boundary is along fault uplifts the horst by 100 to 200 ft the to the south and north-trending high-angle faults. The embayment brings to view a small body of is Precambrian rock. structural and is cut by an Two broad northward-plunging array of faults mostly of folds modify the northeastward trend. northern end of the Manzanita uplift. On the west is the Along the north-trending side of the Hagan basin, Apachitos syncline. The Apachitos syncline plunges especially in the Town of Tejon Grant, there are several generally toward the southwestern end of the Tijeras longitudinal faults. One is the Largo fault which may basin to which it may be related. However, the syncline duplicate or thicken the Mancos section to some extent. terminates at the Otero fault. The western limb of the However, the largest of these is the Frisco Spring fault Apachitos syncline projects updip through Cerro Pelon which occurs along the eastern base of the high hogback ridge to a termination at the Tijeras fault. The east limb formed by the San Andres and Santa Rosa of the syncline is long and beds. This broken by faults, but except fault, together with two branches, for local reversals near appears to be related the faults, is coincident with the to the Montezuma upthrust west limb of the Sabino to which it ties at the point anticline. The Sabino anticline of the Montezuma salient. extends beyond the Sandia The greatest throw on the map on the south. It dies out Frisco Spring fault is at the into homoclinal northward salient where the entire dips toward the Tijeras thick Chinle section is missing. basin. The east limb extends through 2- to 3-degree dips for many miles into the Estancia basin. RIO GRANDE In the eastern part of the Manzanita uplift, the TROUGH north-trending arcuate Barton fault breaks the monot The parts of the Rio Grande trough directly related to ony of the long Sabino east limb. The Barton fault, the Sandia area are the Albuquerque and Santo shown more completely by Kelley (1963), is 10 to ii Domingo basins (fig. 65) (Kelley, 1952, 93). The miles long. The east side of p. the fault is uplifted several Albuquerque, or Albuquerque-Belen basin (Bryan, hundred feet, and high beds of the Arkosic limestone 1938a, p.209) adjoins the long line of uplifts including member of the Madera are repeated in outcrop. the Sandia. Manzanita, Manzano, and Los Pinos. The Santo Domingo basin adjoins the northern tip of the HAGAN BASIN Sandia uplift as well as the Hagan basin. Only the eastern margins of these two basins are of The Hagan, or Una de Gato, basin concerfl of Stearns (1953c, relative to the structure of the Sandia area. p. 483), is an arcuate tilted halfgraben. The term Hagan In the Santo Domingo basin the trough-filling Santa basin, as applied here, is preferred because of the better Fe beds are dropped along the San Francisco fault known Hagan coal center, and perhaps the designation against beds ranging from lower Santa Fe, north of as a basin rather than half graben is justified because of Espinaso Ridge, to Madera beds along Montezuma the plunging syncline created by the arcuate outcrops Mountain. San Francisco fault appears to die or which curve from west to north in be trend around the buried by upper Santa Fe beds north of southwest side. The southwest Espinaso side of the basin is Ridge: vertical separation increases to more than against the Sandia uplift, particularly, 10,000 the Madera ft at its southern end (map 3). However, this difference salient, as previously described. The east side, largely is in large part due to rise of the southwestern side of buried by pediment gravel, is downthrown the against a Hagan basin with respect to its northeastern part. variety of Mesozoic and older Tertiary rocks and is The upper Santa Fe beds along the western side of exposed where 1-lolocene erosion has removed or cut the fault are approximately the same age, but lower through the gravel (Stearns, 1953c, p1. I). The fault beds dip northeastward and rise structurally to the system on the east is a southward extension of the La southwest in parallel with the northern end of the 86

part of this early trough southeast of the San Francisco Sandia uplift and the southwestern edge of the Hagan fault, if it already existed, might have been a bench of basin. Upper beds of the Santa Fe may be found to dip the deeper main trough along the present Rio Grande. in some places slightly away from the uplift. The older Such a bench or step, down to the trough axis, is present beds of Santa Fe, as in T. 13 N.. R. 5 E. and near west of the Manzanita and Manzano uplifts between Placitas. dip locally as much as 45 degrees northeast the main fault at the base of the mountains and the ward. Hubble Springs fault 5 or 6 miles out into the trough. In the Flagan embayment, east of Espinaso Ridge. Similar ones appear to be present in places along the lower Santa Fe beds, including the Zia or Abiquiu and western side of the Albuquerque basin. underlying Espinaso volcanic beds, dip in near con The structural edge of the Albuquerque basin west of formance with the Eocene and all older beds toward the the Sandia-Manzano line of uplifts is poorly exposed eastein edge of the embayment. This edge, formed by and difficult to define clearly because of masking by the L Bajada fault, is also the eastern edge of the Santo outwash from mountains. Thus, two geomorphic fea Domingo basin (Kelley, 1954). Thus, it appears that the tures, the attitudes of the high surfaces in the valley and Hagan half-basin and the embayment were tilted after the alluvial fans at the base of the mountains, may be early to middle Santa Fe time. Inasmuch as the used together with subtle structures to define the basin southwestern side of the Hagan basin is also the boundary and suggest something of the nature of basin northeastern flank of the Sandia uplift, one may project subsidence. The high surface west of the Rio Grande at a model (fig. 66) showing rise of the Sandia uplift in the latitude of Albuquerque slopes eastward, and it may early Santa Fe time. In doing this one could also suggest be projected across the inner valley to the high surface that the early Rio Grande basin covered much if not all at the Albuquerque International Airport, which slopes the Sandia uplift. In this instance where would the at the same low rate of about 40 ft per mile. The high southeastern margin of the trough have been; could it Airport surface, north and south of Tijeras Arroyo, is have been the Tijeras fault? The Tijeras trend is parallel quite flat with even low swales south of the arroyo, to the present San Francisco fault edge of the Santo where westward slope is less than 3 ft per mile. Beneath Domingo basin and both are roughly parallel to the these surfaces in the sides of Tijeras Arroyo and in the opposite trough boundary along the Jemez margin. The west-facing erosional scarps of the inner Rio Grande beds of 0.5 to 1.5 I 07° valley, dips in the high Santa Fe degrees eastward may be seen in several places. Santa Fe beds in Tijeras Arroyo south of the Western Skies Motor Hotel dip about 1 degree toward the nearby upfaulted Sandia Granite even though the surface at the top of the arroyo slopes slightly westward. Else where beds are nearly horizontal east of the river. Alluvial fans along the uplifts, especially along the Manzano uplift, are not wide or large; they appear to be young and built upon earlier fans which subsided into the basin. The eastward-tilted surface and beds, and small, only slightly coalesced fans all point toward tilting of the Albuquerque basin toward the east side uplifts. Rota tion downward toward the more strongly uplifted eastern side may have accompanied much of the basin subsidence creating what has been termed a vortex monocline, as described for the Triassic Newark basins beds 35 of the eastern United States. In such troughs, increase in dip and thickness toward actively rising this borders. Keyes (l908a, p. 83) long ago showed thickening of half grabens toward the fault. There is an axis of sagging well out in the trough. Between the northwestern end of the Sandia uplift and A Santa Ana Mesa west of the Rio Grande a sag axis follows the river course. The basalt flows on the mesa i and the San Felipe volcano are tilted toward the sag axis. (1’EXPLANATION the Basin deposits In late Santa Fe time the Rio Grande course in —r Normal fault Albuquerque area was as much as 6 miles east of its / Hgh-ongIe by volcanic debris, reverse fault present position as evidenced along the sides Antchne derived from the Jernez area, in the beds / Uplift with of Tijeras Arroyo. / fIt threcion The evidence for late Santa Fe tilt of the basin toward C’° Igneous Center basin 0 5 IOMles the east along the eastern part of the Albuquerque does not assure that the entire basin is also tilted east or that the beds at depth along the eastern side might not FIGURE 65—TEcToNic MAP OF ALBUQUERQUE-BELEN BASIN. 87

3\O Santa __. I————o I Mj— I j (, \)C i_1_ I EOC - 17000 I MESOZOIC I - 13000 I o

-9000 PRECAMBRIA - 5000 41e s

- 1000 Sea level i;ii. --3000 FIGURE 66—STRuCruRE SECTION ACROSS HAGAN BASIN.1AND NORTHERN SANDIA MOUNTAINS. SHOWING POSSIBLE EXTENSION oF FE GROUP BEDS ACROSS UPLIFT.

be tilted westward as they are in the eastern part of the TIJERAs FAULT Espanola basin. The structure is probably more compli cated than can be observed at the surface. The uplift The Tijeras fault, the dominating structure of the rift structure is not simple; confinement stresses should be zone, is exposed in the southwestern part in Precam greater in the subsiding blocks than in the uplifts where brian rocks, where pronounced contrasts in rock types confining stresses are released as uplifts rise above the on opposite sides of the fault suggest displacement. surrounding terrain. Furthermore, some Laramide Stratigraphic units ranging from Pennsylvanian to late deformation may have occurred along the entire length Cretaceous are cut and greatly displaced along and of the Rio Grande fault belt. through the western side of the Tijeras basin. Along the For the entire late Tertiary belt the trough mech northwest side of the Monte Largo horst, Pennsylvanian anism is dominant; uplifts are the smaller, counterpart and Permian beds are dragged steeply down against reactions to the subsidence. There is some suggestion Precambrian rocks. In places the fault parallels the that the greater the subsidence the greater the uplift. strikes of adjacent beds, but elsewhere it is diagonal The high mesa surfaces are lower paralleling the greater (normal) across adjacent attitudes. rises such as the Sandia and Manzano uplifts. The mesa Vertical separation across the fault differs greatly level is higher paralleling the lower Manzanita uplift (zero to several thousand feet). Direction and magni from the Albuquerque International Airport south to tude of vertical separation differs laterally along either the southern boundary of the Isleta Pueblo Grant. side as shown in the table. Overall displacement between the Sandia uplift and I) Locally east of Four Hills down 700+ft the Rio Grande trough has long been a subject of 2) Near Seven Springs up 200+ ft interest. Just as the uplift altitudes differ along the 3) Cedar Springs and San Antonito down 3,000 +ft margins of the trough so do the altitudes of the bottom 4) Northwest corner sec. 2, T. 11 N., of the trough, and there are reasons for believing that R.6E. 0 ft the trough bottom may be more irregular. On the basis 5) Monte Largo up 3,000+ ft of known stratigraphic thicknesses we have recognized Figure 67 shows the vertical comparisons of the walls that the vertical separation into the trough could be on of the rift zone by a longitudinal profile at Precambrian the order of 25,000 ft. However, Joesting, Case, and levels midway to the Tijeras graben and the Monte Cordell (1961) interpreted gravity and magnetic data to Largo horst. indicate a displacement of 22,000 ft. Strike-slip movement is suggested by drag folds and horizontal separations. Several horizontal separations of TIJERAS RIFT ZONE stratigraphic units and fold axes indicate left slip. In sec. 15, T. ION., R. 5 E. north of Tijeras a steeply dragged One of the more unusual structural trends in New Todilto-Morrison contact shows left-lateral separation Mexico is the Tijeras rift zone. It extends northeastward of 1.5 miles. In sec. 36, T. 11 N., R. 5 E. east of across the Sandia map area (fig 52, map 1). The zone Cañoncito, adjoining anticline and syncline axes have consists of four principal parts: I) Tijeras fault, 2) been separated left 1,300 to 1,800 ft. One mile to the Gutierrez fault, 3) Tijeras graben, and 4) Monte Largo northeast the left separation of the Mancos-Dakota horst. The Tijeras rift zone is continuously exposed for contact is 3,550 ft and the Morrison-Todilto contact, 31 miles fromihe edge of the Rio Grande trough to 2,500 ft. Nearby in the area of Sandia Knolls near Golden in the southern side of a narrow the Ortiz Moun section of San Andres beds is dragged tains. Relative to the surrounding to the left in a structure the faults horst. In the same are mostly area Abo and Yeso beds are similarly obliquely transverse; but both parallel and separated. obtusely transverse relationships occur. The trend is Two examples of possible drag folds also suggest left part of a longer lineament of on-line structures to as far offset, the best of which is the steeply plunging north as the southern Sangre de Cristo small Range and to the anticline in the northwest corner of sec. southwest into the Rio Grande 22, T. 10 N., R. trough, possibly to the 5 E., half a mile west Ladron uplift. of Tijeras and north of US-66. Marker beds of sandstone high in the Madera Forma 88

SW F

TIJERAS GRABEN AND FIGURE 67—LONGITUDINAL STRUCTURE PROFILES ON TOP OF PRECAMBRIAN, IN AND ADJOINING MONTE LARG0 HORST. tion can be traced regionally rather sharply around a I) Section 6, northwest ofZuzax fault down 3,900 ft drag fold plunging about 45 degrees to the northeast. 2) Section 12, near Gutierrez Canyon Individual beds are doubled back by left drag from 200 road down 4,200 ft to 300 ft. where they abut the fault and Triassic beds on 3) NM-l4 down 6,000 ft the opposite side. Another possible example of left drag 4) SWsec.22,T. II N.,R.6E. Oft folding is in the southeast limb of the anticline through 5) Monte Largo up 1,500 ft sec. 20, T. 11 N., R. 5 E., southeast of San Antonito. There is little horizontal offset or drag to indicate Although there is the suggestion that this anticline is a strike-slip movement on the Gutierrez fault. Some continuation of the Tijeras anticline, the pronounced evidence that left slip may have occurred is described. steepening and sharp turning may be to a considerable degree the effect of the drag. If this is so, then the left TIJERAs GRABEN AND BASIN separations given for the Dakota and Todilto outcrops The Tijeras graben is the southwestern half of the might be increased to nearly 1 mile. Additionally the elongate Frost fault block lying between the Tijeras and Sandia uplift appears to be offset I to 1.5 miles west of Gutierrez faults (map 3). The northeastern half of the the Manzanita-Manzano uplift. Bases of the ranges and block is referred to as the Monte Largo horst. The block the projected crestal axes are both offset, and horizontal is about 16 miles long and ranges in width from 0.5 mile separation of the crestal axes is 3 to 3.5 miles across the the southwest end to 3 miles at the northeast end. The Tijeras fault. at Precambrian base of the elongate block is tilted south In summary, there is much evidence that the Tijeras and the basement is as much as 2,200 ft is a left wrench fault and that strike-slip movement in westward, sea level in the Tijeras graben and about 8,200 ft post-Cretaceous time could have been as much as 1.5 below sea level in the Monte Largo end of the block. miles. Differences in separation along the fault are above between the graben and the horst is expected, especially in view of the folding normal to the The boundary the change from downthrow to upthrow across fault; also, plunging into the Tijeras basin, as well as drawn at the block, and this is about midway through the arching over the Monte Largo horst, may have accom outcrop in the southwest end of Monte panied wrenching movement along the Tijeras fault. Pennsylvanian Largo and about midway of the total length of the fault block. The Tijeras graben whose side limits are the Tijeras GuTIERREz FAULT and Gutierrez faults is a central part of a larger the The Gutierrez fault is 15 miles long and bounds the depression known as the Tijeras basin. On the west Sandia Tijeras graben and Monte Largo horst on the southeast. basin margin merges with the eastern side of the Cañon Southwest it splits into 2 short branches, 1 of which uplift. This margin is arbitrarily drawn through northward connects with the Tijeras fault and closes the southwest cito along the Santa Rosa-Chinle contact, Pedro end of the Tijeras graben. The northeast end is beneath around the southward-plunging part of the San end of the alluvial outwash south of the San Pedro Mountains. syncline, to a junction with the northwestern San Pedro Vertical separation differs greatly from strongly upward Tijeras graben. Along the western limb of the fault o strongly downward; there is probably none in the syncline downthrow on the San Antonito of area of southeast quarter of sec. 22, T. 11 N., R. 6 E. several hundred feet enlarges considerably the strip of Figure 67 compares elevations on the top of the the basin in the San Pedro embayment. The is miles Precambrian along the southeast wall of the Gutierrez basin that is beyond the graben on the west 2 southeast. fault with those along a profile across the middle of the wide. A similar strip flanks the graben on the through Tijeras rift belt. Opposite the Tijeras syncline the This limb of the Tijeras basin is taken to extend the Gutie vertical difference is about 3,600 ft. Some vertical steep dips (Bartola monocline) southeast of part of separations of the northwest side are: rrez fault to the Chamisoso fault and the eastern 89

the Los Pinos fault. In the 2-mile strip southeast of the The Tijeras syncline is the dominant fold of the graben are 3 faults that accentuate the basin. These are graben and the basin (fig. 68). The basin is asymmetri the Chamisoso, Los Pinos, and Zuzax faults, which step cal to the southeast. The southeast limb dips 25 to 50 the basin strip downward parallel with the graben degrees and has structural relief from the trough to the boundary at the Gutierrez fault (map 3). The Chami Gutierrez fault of as much as about 2,000 ft at the soso fault is also part of the northern boundary of the Mesaverde level. The northwest limb dips 15 to 30 Manzanita uplift. North of the Chamisoso fault the degrees and has structural relief of only about 700 ft beds steepen markedly and they constitute monocline a from the trough to the northern end of the Tijeras that bounds the Manzanita uplift and the Tijeras basin. anticline. in general, dips are highest from the north rim The southwestern boundary of the Tijeras basin is taken around the eastern end of the axes and along the arbitrarily a little east of Cedro Canyon, from the southeast side; they are lowest along the west side of the Chamisoso fault to the Tijeras fault. The Tijeras and basin. Gutierrez faults cut through the Tijeras basin and The Tijeras anticline plunges very gently divide it into 3 parts, northward the central part being the Tijeras at about 300 ft per mile. Its limbs gra ben. have structural relief at the Mesaverde level of 600 to 700 ft. and the fold is A strong contrast in internal deformation exists nearly upright, with the eastern limb being steeper in between the Tijeras basin and the Monte Largo horst. the southern part and the western limb steeper in the In the Tijeras graben there are pronounced internal northern part. right-oblique folds consisting of the Cedar Crest syn The Cedar Crest syncline lies between the Tijeras dine on the west, the Tijeras anticline in the middle, anticline and the Tijeras fault. The east limb and the Tijeras syncline on the east (west limb (fig. 68). The Cedar of the anticline) dips as much as 20 Crest syncline and degrees, but the fold the Tijeras anticline are nearly level is asymmetrical to the east folds. The Tijeras with the west limb inclined syncline is doubly plunging, partly from 30 to 85 degrees parallel with the steeper dips toward the to the trend of the block, with the trough Tijeras fault. bottom coincident with the deepest part of the Tijeras The presence of folds in the Tijeras graben and their basin. All these folds terminate abruptly on the south at absence in the Monte Largo horst is puzzling. It may be the Gutierrez fault, and no such folds exist immediately due to the higher stratigraphic level at the surface and to the south. Both ends of the Tijeras syncline also weaker beds in the basin; the folds in the basin may be terminate against the Gutierrez fault. To the northwest concentric and flatten or die out at depth; or there the Cedar Crest and Tijeras may folds appear to have offset be a stratigraphic level of change in deformation. extensions beyond the Tijeras fault. Examination of Chinle configuration across the fault block at Frost Canyon supports this possibility. Out crops in this area appear to afford the down-viewing cross section described by Mackin (1950). The Chinle has the thickness and weak physical characteristics that could facilitate a rapid change in relative deformation between two depth zones. There are other possibilities that could be related to the attitudes of the faults, differences in width of the block, and timing and nature of relative movement in the block and adjacent masses. Grabens and horsts are quite commonly associated with large wrench faults, where splits or acute branches occur along the belt (Lensen, 1958). Dips of the Tijeras and Gutierrez faults have been presumed to be steep to vertical in the absence of exposures of the fault surfaces, and the evidence of strike-slip motion favors their steepness also. If, how ever, the generally accepted fault-boundary attitudes of grabens and horst are considered, then the attitude of each fault would change from inward to outward in passing from the graben to the horst. Furthermore, mechanics of deformation would have been extensional as vertical separation increased. The width of the horst would increase and that of the graben decrease with depth or erosion. That this geometry does exist is supported by the graben being narrower than the horst, assuming that the two faults were parallel to begin with. In the parts of normal faults where dips would have to change from northeastward to southeastward the faults would be vertical or quite steep. In this area the outcrop width FIGURE 68—AIRvIEw is less than along the horst as it should NORTHEAST OF TIJERAS ANTICLINE AND be, but it is SYNCLINE. HAGAN also less than that of BASIN: ORTIz MouNTAINs, OF PORPHYRY, IN the graben and this is not what BACKGROUND: AND DIMLY, would THE SANGRE DE CRIsT0 RANGE OF THE be expected. The widening of the graben by ROcKIEs BEYOND. VILLAGE OF TIJERAS, LOWER LEFT. northwest bowing of the Tijeras fault next to the deepest 90

crosses a long structural saddle part of the basin could be due to warped flattening of the San Pedro syncline the southern end of the Hagan basin. the fault which might result from a downward wedging and plunges into forms the structural divide between action by the subsiding graben. Westward flattening San Pedro saddle and Hagan basins. The southeast limb is could take place where it appears owing to the presence the Tijeras the syncline asymmetrical to the of relatively weak Mancos. Morrison. and (‘hinle beds much steeper making away from the Monte Largo horst. west of the Tijeras fault where the bowing exists. northwest and between Paleozoic beds and the The matter of timing between the folding and the In 2 places contacts show some missing section. notably the faulting in the Tijeras basin is important. For the Precambrian low-angle, near-bedding faulting Tijeras fault, it appears that the folds are offset and Sandia Formation: caused omission of some strata. One of these therefore older. In contrast, all the basin fold axes could have lies about 3 miles west-southwest of Placitas terminate at the Gutierrez fault and therefore could not situations 12, T. 12 N., R. 4 E. In this area there is a local be older. Thus the Gutierrez fault may be older than the in sec. Mississippian Arroyo Penasco Formation over- Tijeras fault, or possibly the more recent episodes of patch of Madera limestone with little or no Sandia movement on the Tijeras fault. That the Gutierrez is lain by and even where the pre-Pennsylvanian beds older is also suggested in sec. 12, T. 9 N., R. 5 E., where Formation, Sandia is thin or absent. The relationship the short northwest-trending fault that bounds the are absent the brought about by low-angle gravity Tijeras graben at the southwest end is terminated at the could have been dip of the rising late Tertiary uplift in Tijeras fault. The right obliqueness of the folds across faulting down the scooped out the weak Sandia the basin suggests clockwise rotation or left shift such a way as to have could indicate Laramide between the Sandia and Manzanita blocks which could beds, or the relationship Because direct exposure or other explain the internal deformation of the graben. This low-angle faulting. is lacking. possibly the Sandia would also suggest some right slip on the Gutierrez deformational evidence west by overlap of Madera beds fault. beds wedge out to the ontoa high. at the MONTE LARGO H0RsT The other instance of missing Sandia beds is inselberg along the base of the uplift, in sec. 14, T. 10 The northeastern end of the Frost fault block is the N., R. 4 E., a short distance north of “U” rock. ln this Monte Largo horst. Bounded by the Tijeras and Gutie small hill massive gray Madera limestone rests directly rrez faults, the horst merges into the Tijeras graben on on Sandia Granite. The missing Sandia beds could the southwest (fig. 67) and is terminated on the again be explained as above. Their absence is equally northeast at the San Pedro porphyry complex and likely to be due to either gravity sliding or to deposi where the Gutierrez fault dies out. tional overlap. Kelley has seen evidence of missing Along the central part of the horst Madera limestone basal beds along steep east-flank beds in the San is faulted down on both sides against Precambrian rocks Andres uplift of southern New Mexico that are very the core. Longitudinally the horst is a broad anticline of unlikely to be due to sedimentary overlap. However, we with a narrow southeast limb that dips 25 to 35 degrees have several suggestions for a former positive area in into the Tijeras syncline and a more gentle northeast the site of the Rio Grande trough (Wilpolt and others, limb dipping into the San Pedro porphyry complex. 1946: Read and Wood, 1947, fig. 3). In the recent Shell Oil Santa Fe # 1 well drilled about 14 miles west of OTHER STRUCTURES PLacitas the Pennsylvanian is reported to be only 545 ft An examination of the geologic map (map 1) reveals thick. of horizontal shearing a salient of Madera Formation extending eastward from A quite unusual occurrence terminal of the the main part of the Sandia uplift toward the Monte occurs along the road to the lower N., R. 4 E. At this Largo horst. The limestone hills stand physiographically Sandia Peak tramway in sec. 10, T. ii to thick, as well as structurally above the terrane on all sides locality the Sandia Granite is mylonized consists of except on the west in the direction of the uplift. This flat-lying gneiss. The highly sheared rock normal to feature is the Madera salient. Structurally the salient is broadly undulatory foliation with lineation a part of the tilted fault block elevated on the Barro the mountain front. The occurrence is incompletely rock fault and forms a rough nose even though bed attitudes exposed, and neither top nor bottom of the sheared cannot do not trend smoothly around it. However, northward is revealed in the acre or so of outcrop. The zone alluvial cover. dips do occur north of Madera Canyon and adjacent to be traced along the front because of have been the Seco fault and southward dips occur along the Movement indicated by the shear zone could In either case southern side of the salient. The eastern end of the in either Precambrian or Laramide time. the direc salient is crossed by a prominent fault with 2 parallel, it is interesting that the lineation indicating and to the most narrow, closed folds. Relationships do not reveal clearly tion of movement is normal to the uplift the direction of movement on the fault, but distribution likely Laramide trends. and attitude of the Abo Formation east of the fault suggest that the east side is upthrown. Abo probably ORIGIN wraps completely around the eastern end of the salient. structure in the Sandia San Pedro syncline plunges into the Tijeras basin. Prior to the Cenozoic the only the basement orogenies long This syncline is a long northeast-trending downwarp area had been produced in At the end of Cretaceous time that separates the Monte Largo horst from the Sandia before Paleozoic time. low plain underlain by some uplift and from the Madera salient, in particular. the Sandia area was a Paleozoic and Mesozoic strata Between the eastern end of the salient and Monte Largo 10,000 ft of flat-lying 91

with little or no deformation beyond minor subsidence- Notable among the interruptions in thrusting is the related tilts during accumulation of the sediments. Manzanita uplift. Upthrusts formed a staggered line of Except for the Precambrian terrane all the present uplifts asymmetrical to the east, the highlands of which structure of the area must have been produced during appear to have coincided with the present late Tertiary Cenozoic time. On the basis of direct evidence alone, all uplifts or to have lain along the edge of what is now the the structure above the basement could have been late border of the Rio Grande trough. The uplifts probably Tertiary, accompanying the formation of the Rio resembled the Colorado Plateau monoclinal uplifts and Grande trough. However, based upon indirect evidence may have been part of that province prior to the and by analogies with nearby structures it appears that formation of the Rio Grande trough. This concept is not some of the present structure may have formed prior to unlike the more generalized Laramide uplift proposed the subsidence of the Rio Grande trough and possibly by Eardley (1962, 399-402), and that of Herrick during the Laramide. p. (l898a, p. 27). Some of the thrusts that produced the To directly establish a Laramide age for deformation, uplifts lie rooted in the trough, as in the southern end of Cretaceous or early Tertiary beds must be found in a the Manzano uplift and possibly west of the Caballo folded, tilted, or faulted condition overlain unconform and Fra Cristobal uplifts. In some instances, as near ably by late Tertiary (Miocene or Pliocene) beds in Abo Pass and in the Caballos, it appears that either an undeformed the or less deformed condition. West normal faults of the trough may have the of Placitas, same root as Galisteo (Eocene) rests on a somewhat the upthrusts but with opposite displacement. thinned section of Mesaverde beds, compared to the Inasmuch as we believe that the high-angle thrusts sections in the Tijeras and Hagan basins. Although this and the Tijeras rift zone predate the Rio Grande trough, is indicative of an early uplift and erosion, it is not the question of their relative ages remains to be possible to determine whether Laramide uplift took considered. Displacement on the Tijeras fault in the place in the area of the present Sandia uplift. Some of Precambrian terrane appears much greater than in the the structure may be pre-Rio Grande trough and overlying Paleozoic rocks, especially in Tijeras Canyon. possibly Laramide, for several reasons, chief among It is probable that the fault in the sedimentary rocks is a which is that a number of structures do not fit the form Laramide extension of a preexisting Precambrian fault. or the mechanics of deformation observed in the known The Flatirons high-angle thrust impinges on the Tijeras late Tertiary fault-block uplift. The main structures of fault in a zone of squeezing, shearing, and some the Sandia-Manzano line of uplifts are great high-angle overturning. The upthrusting appears to disturb and normal faults accompanied by gentle to moderate bend the Tijeras fault to the east. Assuming that the eastward tilting. The northeast-trending Tijeras rift zone Tijeras rift zone was already in existence at the time of does not fit the mechanics of the late Tertiary deforma the Flatirons upthrusting, it is possible that the tion. Furthermore, it lacks the same fault scarps that charac force might also have aided in the terize the trough boundary. development of the folds in the Tijeras basin. The strain pattern of the right A number of the east side structures such as the echelon of faults from the Flatirons to the Wolf Springs Barro, Lagunita, Ellis, and Las Huertas uptilted fault is clockwise and the stresses involved would be the same blocks are most likely late Tertiary, forming in coordi as those responsible for the left separations along the nation with the main movement of the uplift. However, Tijeras fault. several high-angle reverse faults such as the Flatirons, In summary, most of the structure along the east side Tejon, and Montezuma, which are upthrown to the of the Sandia uplift is quite different from the structure west, do not fit well with the mechanisms of the responsible for the great relief on the west side. A uplifting Sandia fault or the Barro fault. regional correlation with similar structures for 200 miles Similar faults, with related folds commonly over along the Rockies trend, and direct evidence for Lara turned, occur along the eastern flanks of the Los Pinos mide age in the southern part, suggest that the Sandia and Manzano uplifts and were first recognized as west- structures are also Laramide. Assuming further that dipping thrusts (Wilpolt and others, 1946) formed most much erosion would have accompanied the Laramide likely in Laramide time. They were later described in deformation, then a considerable part of the sedimen more detail by Stark (1956, 30-34) who p. also suggested tary section may have been removed from the Sandia Laramide orogeny. However, all the evidence is indirect Mountains area prior to their late Tertiary uplifting. and based on analogies with the Rocky Mountain Where the products of such erosion are is puzzling, but Laramide style rather than Basin and Range block- perhaps they are in the Galisteo Formation. If so the faulting style. Kelley and Silver (1952, 136-137; p. Galisteo, which rests with minor unconformity on the 162-165) found similar compressive structures in the Mesaverde in the Hagan basin, would probably have Caballo tilted fault block and with the presence of early had to overstep down to the Morrison or the Triassic in and late Tertiary beds were able to more directly order to receive any sediments from the Sandia direc demonstrate Laramide orogeny along the Rio Grande tion, and the distance of 2 or 3 miles would suggest belt. R. L. Koogle working under Kelley found direct sharper and greater uplifting than is apparent. From the age evidence for deformation, long considered Lara nature of the proposed uplifting it would appear that mide, along the eastern flank of the San Juan basin. the erosional product would lie to the east, but none is The belt of upthrusting toward the east extends, with known in that area: there is little gravel to the east interruptions, from the northern that end of the Sandias. is derived from late Tertiary uplift. The only remaining through the Manzano, Los Pinos, Fra Cristobal, and locale is in the Rio Grange trough, notably Caballo Mountains lying in its east of the normal faults western part where great thicknesses of post-Cretaceous bounding the east side of the Rio Grande trough. sediments are known. Importantly, because of earlier 92

subsidence of the uplifting and erosion there, not as much of the 10,000 ft dence. Although this is generally true, matched or of pre-Tertiary sediments had to be removed from the trough margin does not appear to be always crustal control, Sandias during late Tertiary uplifting. equalled by uplifts of the border. The in the trough The most direct evidence of possible pre-Basin and however, appears to have been primarily to the crowding Range deformation is in the Placitas area. In this area belt with uplifting primarily a reaction ft is obvious that the the folded Santa Fe rests with marked angular uncon action of the subsiding wedge. along the border. formity on early Tertiary and older formations (fig. 69). reactive uplifting occurred irregularly with the mechanics of The Santa Fe is a fanglomerate consisting of fragments The principal concern here is of Abo, which does not now occur in the nearby Sandia growth of the Sandia uplift. with the Mountains in places that could have been the source. Many early explorers were impressed Marcou (see These Abo fragments could have come from the Sandia abruptness and grandeur of the Sandias. Sandias in 1853 uplift when it was much lower and before all or most Introduction, this memoir) climbed the nothing concern movement on the Placitas fault. The gravel is not a studying the formation but ventured Herrick (l898a, 27) high, Pleistocene gravel as Hoge (1970, fig. 19) thought ing the origin of the escarpment. p. . .. may have but instead must be well within the Santa Fe sequence, speculated that the “abrupt escarpment even if so the western if not in the lowest part. Considerable pre-fanglomerate been the axis of a monocline” but hundreds of feet uplift and erosion are indicated by steepness of beds as limb must have “been faulted many 457) estimated old as Triassic that underlay the surface on which the below the river level.” Johnson (1903, p. (1903, 136) Santa Fe was deposited. The considerable deformation a throw of over 4,000 ft in places; he also p. the range and erosion of pre-Santa Fe age in the Placitas area cited limestone at the bottom and the top of ft. Fayette suggests pre-Basin and Range uplifling in the Sandia and suggested a fault displacement of 3,000 to have been area. A. Jones, engineer and geologist, appears of Late Pliocene Santa Fe beds are downfaulted against the first to have suggested faulting as the main cause 29). the east-tilted Sandia uplift in many places. The general the scarp and illustrated it as such (Ellis, 1922, p. tilted evidence suggests that the Santa Fe beds are the Jones (1904, p. 1-2) stated that “The great lying east principal trough-filling sediments derived from the orogenic block composing the Sandia range, extraor bordering uplifts. The uplifting appears to have gone on of Albuquerque, is regarded as classic in this likely, concurrently with the subsidence and filling of the dinary type of mountain modeling.” It appears gotten trough; therefore, uplifting dates from the oldest of however, that both Jones and Johnson may have in the area. these sediments, or from the late Miocene. However, as their ideas from Herrick who worked more began to suggested in the discussion of the Rio Grande trough Herrick (1904, p. 393), about the same time, it to the much of the rise of the Sandia block may have come believe in the fault-scarp concept, but related into after early Santa Fe time. The uplifts continued rising limb of a broad anticline whose arch had collapsed 435) through the Pliocene and into the Quaternary. The the Rio Grande valley. In 1908 Keyes (l908b, p. fault and Santa Fe is dropped and tilted along the San Francisco published a cross section showing the frontal showed the fault at the north end of the range and at Tijeras also the back-slope (Barro) fault. He also structure sections Arroyo. There is further evidence in the form of fault (p. 447) on three regional Santa Fe, one to Holocene fault scarps that the uplifting may still be radiating from the Sandias—one to Hills. continuing. Glorieta Mesa, and one to the Pedernal the fault origin but Just as the bordering uplifts may be considered as In 1922 Ellis (p. 29-34) followed along the western rims of the trough the trough margin may be considered emphasized only a fault zone high granite facades. a side of the uplift. In many respects the Rio Grande escarpment near the bases of the great seen in a small uplifts, such as the Sandia, are reactions that are He ventured that the Pennsylvanian, 1), lay complementary and counterpart to the trough subsi patch near the mouth of Embudo Canyon (map all along the base beneath the mesa gravel. He thus appears to have suggested that these beds projected upward to the high fault zone as a downfaulted western limb of an anticline. Darton (1922, p. 219) showed the uplift in cross sections as a faulted anticline with the faults well up in the granite and with none at the base. Later he (1928, p. 95-100) used the same cross sections and referred to the Sandias along with the Manzanos as “an anticline of great prominence” recognizing a north ern “pitch” (plunging) of the uplift that has been described above. He (p. 99) also stated that “The strata on the west side of the Sandia Mountains are crushed and faulted along the higher part of the uplift, but the general structure is that of an anticline with a steep western limb.” In part he appears to have reached this conclusion on the basis of limestone beds at the base near Embudo Canyon, but it appears possible that he FIGURE 69—SANTA FE FANGLOMERATE UNCONFORMABLY OVERLY was more influenced by his mapping and observations ING MESAVERDE CLAYSTONE AND SANDSTONE. FANGLOMERATE in such places as the southern end of the Los Pinos AB0 AND DIPS ABOUT 45°. MESA VERDE DIPS CONSISTS MOSTLY OI Mountains and in the Oscura and San Andres Moun 650 TO 700. 93

tains. The San Andres Mountains, in particular, show indicated by relatively undissected fault facets like those many examples of reversal of dip across the faulted of the bold escarpment between Sandia Peak tramway uplift and basinward-dipping beds at the base of the and Juan Tabo Canyon. clearly block-faulted uplift. It is quite probable that the Sandia uplift would have shown parts of such a limb at an earlier stage of uplift and erosion. Nevertheless, the EARTHQUAKES evidence points to faults as the dominating final struc ture. The early form of the uplift may have been an So far as we know, only two earthquakes have been anticline, but as the trough sank more deeply the reported in the Sandia Mountains, one in 1947 and western limb was dragged more steeply and sheared another in 1956. In view of the high seismicity of the into one or more normal faults. By this hypothesis the Rio Grande depression (Rio Grande rift or rift zone of early rise would have been anticlinal or monoclinal some writers) between Socorro and Belen, and to a uplift which was then later faulted resulting from the lesser extent through Los Lunas and Albuquerque, the trough subsidence. It is quite likely that the more low seismicity of the Sandia Mountains is rather strongly tilted Sandia uplift resembled the gentle Man remarkable. Earthquakes have been recorded in New zanita uplift at an early stage of deformation. Mexico since 1849, and since then hundreds of shocks Another quite different hypothesis follows the Her- have been recorded in the Rio Grande depression, rick suggestion of 1904, recently adopted by Eardley chiefly in the Socorro-Belen segment. (See Northrop, (1962, p. 401), which suggests that there is a broad anti 1942, 1945, 1947, 196lb; Northrop and Sanford, 1972; dine with one limb west of the Rio Grande trough Sanford and others, 1972; and numerous papers by and another forming the present eastern flank of the Sanford and by Sanford and others, not included in Sandia-Manzano uplift. By this hypothesis the broken References, published from 1961 on.) steep-limb dips would result entirely from drag against Earthquakes have been felt in Albuquerque on at the normal trough-bounding faults. It is difficult to least 28 different days in 13 different years from 1893 to accept the idea of an uplift as wide and long as the 1974. Some of these originated near Socorro; some were Albuquerque basin, It is also difficult to believe that near Belen; one severe one (May 18, 1918 of MM. pre-existing anticlines existed independently of the Rio Intensity VIll-IX) occurred at Cerrillos; and at least 15 Grande trough. Instead it appears that trough subsi shocks originated beneath Albuquerque. dence initiated the uplift and that westward dip in such The first recorded earthquake in the Sandia Moun an uplift would have been monoclinal drape or drag. tains occurred in the Tijeras coal basin between Tijeras The resulting form could have been a large doubly and San Antonito at 9:50 a.m., November 6, 1947. plunging anticline, the Sandia anticline as depicted in Detailed information gathered from a questionnaire- maps 3 and 4. The physiography of the escarpment card survey is given in Appendix 2. Greatest intensity indicates that there was one dominant fault although (M.M. VI) was apparently at the C. A. Dooley ranch, lesser ones existed. However, the base of the high Gutierrez Canyon, Zamora; M.M. mt. V was reported granite facade is not a fault line. The individual faces at Cedar Crest, San Antonito, and Sandia Park. This are irregular and due largely to contrasts in the type of shock was not felt at Albuquerque or at Placitas. erosion at high altitude which produces cliffs rather The second earthquake in the Sandia Mountains than the rounded forms of lower altitudes. apparently originated at the north end in the vicinity of Deformation by monoclinal bending may have Placitas at 8:30 p.m., April 25, 1956. Detailed informa ceased with the development of a few persistent faults, tion is given in Appendix 2. Greatest intensity (M.M. V) and in the Holocene, creep and occasional discon was reported at Placitas; MM. mt. IV was reported tinuous slips may be the mode of uplifting. Current or from Tijeras and Ties Pistolas Canyon. It is curious that recent creep has not been determined, but the existence the shock was not felt at the Forest Service Ranger of a small 1-lolocene scarp along the Rincon fault (fig. Station in Cedro Canyon, but shocks originating in 57) indicates that strain is likely accumulating and/or mountainous regions of New Mexico have smaller areas being dissipated in creep. Recent and possible continu of perceptibility than those originating in the Great ing rise of the uplift and/or subsidence of the trough is Plains to the east (Northrop and Sanford, 1972, p. 151). 94 Geologic History

A geologic history should summarize in chronological subside and receive lime mud, sand, and argillaceous order the processes, events, and condition of the area mud, but during late Pennsylvanian time a rejuvenation (and adjacent areas, where necessary). including past in the height or size of the land sources is indicated by environments, sedimentation, crustal warping or orog increased sand and granitic debris in the Pennsylvanian eny. erosion, metamorphism, and igneous activity: it sediments. Finally in latest Pennsylvanian and/or ear should not deal in terms of rocks, batholiths, uplifts, liest Permian time the sea became filled and continental mountains, pediments, plains, or faults. It should not be nonmarine sand and mud spread on a vast river flood a repetition of stratigraphy or structure but rather an plain. Subsidence, however, continued as Early Permian integrated, sequential interpretation of observed geo (Abo) red-bed deposition continued apace with the logic events and processes. growing adjacent mountains. By Middle Permian time The evidence of Precambrian events is fragmentary wearing down of the mountains and the long persistent throughout the region owing to widely scattered out regional subsidence allowed seas to again spread widely crops. Even with extensive continuous exposures inter across all of central New Mexico, this time as a shallow pretation of the history is difficult because of the shelf and under arid conditions (Kelley, 1972a, p. 41). profound metamorphism and deep erosion. However, This was the time of the Yeso and San Andres from the existing exposures in the Sandia area it can be deposition in which normal marine-water influxes alter interpreted that sedimentary and volcanic materials nated with drainage or desiccation, which left large and were deposited in the area at different times as early as small lagoons or pools where evaporation was so high as 2 billion years ago. Judging from the evidence of to precipitate calcium carbonate and calcium sulfate. profound deformation and metamorphism, much However, as before, the epeirogenic action was one of mountain building or orogeny of northeasterly trend continued slow subsidence of most of central New occurred in the area. What remains represents the Mexico, allowing several hundreds of feet of shelf considerably infolded or downfolded roots of the an sediments to accumulate. cient mountains, indicating that the mountains were Beginning in Late Permian time crustal subsidence of high and subsequently deeply and widely eroded to a the central New Mexico area ceased, and widespread low level. It is also evident from the existence of the lack of sediment of that age indicates slight broad rise large Sandia batholith that the roots of the old folded and possible erosional stripping of earlier shelf beds. mountains were invaded from the lower crust by large The fine grain size of all the Middle Permian sediments masses of magma which thermally metamorphosed and indicates either absence or greatly subdued presence of shouldered aside mountain roots. This event took place the old lands as a source area. The positive stable about 1.5 billion years ago prior to the prolonged deep condition of central New Mexico during Late Permian erosion which eventually brought most of the Precam time continued into the Mesozoic Era, and the Sandia brian rocks to view. By the end of Precambrian time the area is without sedimentary record during Early Triassic region had been stable so long as to allow erosion to re time. duce the area to a vast low plain. In Late Tnassic time the physical environment re Paleozoic time began with broad downwarping of the turned to river flood-plain conditions similar to those of ancient peneplain which allowed the spreading of the Early Permian. The climate was probably warm and shallow seas across most of New Mexico. From about wet as the red Santa Rosa and Chinle mud, sand, and 500 my. ago, to about 300 m.y. ago, calcareous mud locally gravel were deposited. Again subsidence by very and sand were slowly deposited in the seas. The absence broad epeirogenic downwarp attracted rivers carrying of these deposits in central New Mexico suggests that the sediments. The nearest source of the sediment the Sandia area was exposed above Paleozoic seas, was appears to have been south-central Colorado. Before undergoing erosion, and was contributing sediment to this period of slow Triassic subsidence ended, the the adjacent seas. However, if the area had been Sandia area had more than a quarter of a mile of new submerged at times, subsequent broad, low upwarping thickness added to its crust. in middle Paleozoic, mostly Mississippian, time allowed Some of the latest Tnassic and Early Jurassic the removal of any previously deposited middle and sedimentary record is missing in the Sandia area, most lower Paleozoic sediment. Scattered remnants of thin likely by nondeposition and/or some slight broad Mississippian beds in the northern Sandias and in stripping arising out of cessation of the subsidence and nearby uplifts indicate a marine shelf inundation of possible slight rise. In any event, the Late Triassic flood short duration. plain fluvial environment came to a halt either by With the beginning of Pennsylvanian time the sea obliteration of the upland sources or by a change to moved widely into central New Mexico as the entire aridity, and a whole new environment characterized area gradually subsided except for a few islands and Middle Jurassic time. The first Jurassic sediment of the long north-south ridges or archipelagos that lay west area is largely eolian Entrada deposit. This clean, and east of the Sandia area. One land area, known as reddish and white sand blanket with its dune structures the ancient Pedernal Mountains, lay some 40 miles to was spread over a vast area by strong and persistent the east. Another, the Peflasco, lay perhaps IS to 40 winds as the Sandia climate again markedly changed. miles to the west (Read and Wood, 1947. fig. 2). During Soon, however, the Saharan conditions vanished as the all of Pennsylvanian time the Sandia area continued to shallow Todilto lake spread into the area from the 95

western seaway. The howling Jurassic winds subsided, within the area cannot be known and the tranquil lake dominated directly and one must most of central New examine the mountain structures Mexico for short for type and compati a time; then arid conditions returned bility with the and evaporation latest deformation in the Sandia uplift. turned the lake to wide white flats of Tijeras rift gypsum. zone faulting and folding took place earlier than the late Tertiary rise of the dominant In Late Jurassic time the uplifts, lacustnne environment of although there is some apparent offsetting Todilto time was superseded of the Sandia by a higher energy envi and Manzanita uplifts. The Tijeras ronment, It was belt is a wrench zone a return to slow persistent subsidence in which probably developed which mud, mostly in early Tertiary time sand, and gravel were spread in the vast and possiblyjust prior lakes to or during the deposition of the and associated flood plains of Morrison time. It Galisteo beds. was not an inhospitable time, as the plants and dino The echelons of high-angle reverse faults along the saurs that had made a beginning in Triassic time east and northeast sides of the Sandia uplift have flourished. Sediment of the Sandia Morrison was borne aspects comparable to similar faults farther south in in by rivers, lake currents, and winds from various central New Mexico that have also been considered to sources, much from the south but some from low hills in be early Tertiary in age. However, there is some south-central Colorado. Volcanic sand, dust, and some possibility that some, if not all, the movement on these lapilli were contributed by streams from probable vents faults occurred during middle or late Tertiary uplift of to the south. As elsewhere in central New Mexico the the Sandia Mountains. rather special Morrison environment probably contin Record of middle Tertiary history in the Sandia ued into earliest Cretaceous time. region is largely missing, as in many other parts of New The southern source area for much of the Morrison Mexico. It appears that this was a time of general rise of sediments appears to have been an east-west-trending the backbone of the continent. The broad north-south upwarp, low and slow-developing at first, but growing rise could have been several thousands of feet and may in late Morrison time to become important through have resulted in elevating the still low-relief Sandia area Early Cretaceous time. Concurrently, the large from close to sea level to nearly its present altitudes, Cretaceous seaway was spreading into southern and with the exception of the large uplifts which were to northeastern New Mexico as a forerunner to the return come later. In the northern ramp of the Sandia uplift in force of the oceans that had not occupied the Sandia west of Placitas, considerably deformed Santa Fe beds scene since Pennsylvanian time. The general evidence rest with marked angular unconformity on from New Mexico indicates the Eocene that marine waters moved Galisteo beds, strongly suggesting not into the Sandia area only Laramide from the east and northeast and but possibly middle Tertiary deformation. progressively encroached or lapped onto the southern The late Tertiary record is good and filled with land area. About midway through Late Cretaceous time sedimentational, deformational, and erosional events. flood-plain deposits from the southwest pushed the Beginning sometime in the Miocene, downbowing and shoreline northeastward out of the Sandia area and for faulting began in what is now the Rio Grande valley. the remainder of the Cretaceous the geosyncline con Accompanying the subsidence, probably from tinued its subsidence under nonmarine the conditions. It beginning, the borders buckled or were fault-tilted was in this wet and swampy environment in that the coal response to the outward stresses induced by the subsid deposits of the Hagan and Tijeras areas accumulated. ing wedge or wedges that were part of the trough. As During Late Cretaceous time central New Mexico the trough subsided, drainage into it from the sides, and must have subsided at a much accelerated rate, as is the transfer of mass by erosion from the rising borders indicated by the relatively great thickness of the de into the trough, probably isostatically aided the move posits. The area subsided into the Rocky Mountain ments. geosyncline at a rate nearly 3 times as fast as all Throughout the development of the trough the ter previous subsidence that may be inferred from the rain was undoubtedly similar to that of the present, thickness of the preceding sedimentary deposits in the although lacking the present magnitude of relief. Broad Sandia area. This rapid rate of subsidence was in a playa valley floors, alluvial fans, pediments, terraces, sense a prelude to the disturbances that were to come in fault scarps, and volcanoes all could have been the Cenozoic Era. a part of the scene 5 to 10 million years ago. In the subsiding The next record of events in the Sandia area is from valley, successive surfaces were buried, locally dissected, the thick Tertiary Galisteo deposits. Their age is not and reburied. Older terraces, pediments, alluvial fans, definitely known as the only fossils are a few verte marginal faults, unconformities, and some volcanoes brates, suggesting an Eocene age. Based on comparative were repeatedly buried. These varied and complex lithology it appears likely that the Galisteo is equivalent features should be expected at depth, especially in to several Paleocene (Raton, Nacimiento, the and McRae trough margins. At the rising borders, such Formations) and Eocene deposits as the (San Jose and Baca Sandia uplift, the sedimentary section was dissected Formations). Even with the Galisteo and being Eocene in stripped from the uppermost Mesaverde and perhaps age there is a possibility that some latest Cretaceous and the Galisteo downward until—near the crest earliest Tertiary, Paleocene, of the uplift record is missing in the and especially on the steep, trough side—Pennsylvanian Sandia area. The Galisteo beds rest with erosional beds were stripped to the Precambrian. At unconformity on the Mesaverde that time, deposits; it may be perhaps as much as 5 million years ago, the western concluded, therefore, that some uplifting and erosion escarpment began developing the rugged, cliffy topog occurred in the Sandia area prior to or during deposi raphy that is present today. Is trough subsidence and tion of the Galisteo beds. Exactly what form or where mountain-building over? Quite likely not. A few young 96

air photos of Rincon Ridge show little sign of the fault scarps are present, and the uplift as well as the vation that Kelley discovered about 1965. If 10- to trough may be imperceptibly movingjust as it did in the fan scarp year geologic processes are continuing, then Pliocene and Quaternary. Some small alluvial cones at 15-million flooding, valley-filling, erosion in the the mouths of canyons are sharply dissected in ways sedimentation, and strain or release of strain by warping that indicate a recent change to a steeper gradient. If mountains, (with earthquakes) at the margin are all in they are under strain, the strain could be released by and faulting sudden faulting as appears to have occurred recently progress. along the base of Rincon Ridge. The 1935 Soil Conser 97 Mineral Resources

Mineral resources in the Sandia Mountains ploughed area are up by a local farmer. The above facts varied and include metalliferous, conclusively prove nonmetalliferous, and that the mines in the district were extensively coal deposits. worked Exploration for oil and gas has been and that rich ores had been taken from them. conducted, but as yet without success. Among the The following excerpts pertaining metals, gold, silver, copper, lead, to early mining and and zinc have been prospecting activities in found, but little or nothing the Sandia Mountains and has been produced. The nearby areas are from Northrop(1959). industrial mineral resources constitute the principal Wislizenus (1848) potential. Among these, limestone, shale, stated that several rich silver mines were gypsum, and a worked in variety of rocks for use in construction, Spanish times “at Cerrillos. and in the Nambe landscaping, mountains, but none at present.” and roads have been mined. In the Cerrillos district, Barite and fluorite deposits the water have been as well as the ore had to be conveyed to the prospected, but little or nothing surface upon has been the backs of peons who climbed from terrace produced. Coal occurs in to terrace the Mesaverde Formation in upon notched logs” (Mining World, Las Vegas, v. the Hagan, 2, no. 9, Tijeras, and Placitas areas. In the period Jan. 16. 1882. p. 154). from about The estimated 1900 to the early 1930’s some mining was Spanish production of the Cerrillos district was more than done, but, except for the Hagan basin $3,000,000 to the church and, in addition to little more than this, they “filled household or smithing the coffers of their king” (Mining World, Las usage was made. Ground-water Vegas. v. 2. no. resources 19. July 15. 1882, p. 260). A single mine, the are not considered in this memoir; Mina del Tero (Tiro), the Bureau paid in tithes “to the Catholic Church of has a report in progress. Spain” more than $300,000 at a depth of 100 feet. Another mine, the Rue Alevia, paid $237,000 to the Church of Spain in three months (Mining EARLY MINING World. Las Vegas, v. 3, no. 6, Dec. 1, OPERATIONS 1882, p. 88). In the Old Placers district, Prehistoric inhabitants of the Sandia Mountains “In 1680 the made use of chert and Ortiz mine ... was a famous gold chalcedony thousands of years producer. Here the Pueblo Indians . . . were made to do ago. Artifacts such as points and almost superhuman scrapers in the Sandia tasks, climbing notched poles. which layer of Sandia answered Cave are composed mostly of chert as ladders, with their burdens of gold-bearing although ores” (Anonymous, fragments of chalcedony occur; much of 1901. p. 56). this The placers material had a local source, chiefly chert here and in the New Placers district were operated nodules in the only with the greatest Madera limestone. difficulty. Water had to be packed in on Artifacts in the Folsom layer include burros for scrapers made many miles during the dry season and, in winter, of Pedernal chalcedony and chert, snow was often melted with believed to heated rocks. Referring to the have come from quarries in the Jemez New Placers district, Howe (1881) stated that Mountains, and Folsom “In former points of white chalcedony, years the dirt was carried to the Rio Grande “brownish on burros agate chalcedony,” and mottled purplish and there washed. The dirt is so rich that even chert this expensive method was (Bryan, 1938b; Church and Hack, 1939; Hibben, profitable.” In his report 1941; Northrop, 1959, 5). on the mines and mining of Bernalillo County, p. Howe(l881) The chronicles and narratives wrote: of Spanish expeditions “Numerous of exploration and ruins of smelters are also found, giving colonization, starting with Coronado indisputable evidence that mines were once worked on a in 1540 through 1700, contain numerous large scale. references to Two hundred years ago the Indians, who had mineral deposits of the been enslaved Cerrillos, Old Placers, and New and forced to work these mines broke out in Placers rebellion districts, but no specific mention of and drove the Spaniards from the country. So the Sandia intense was Mountains area. their hatred toward those places in which they had been forced The earliest record of to labor, that they filled up every old mine mining in the Sandia Moun so that no trace could be found tains area was in 1667. of them. A number of years Toomey (1953, p. 5, 7) states: after the Spaniards were allowed to return Documents More specific citations are now in the archives of Mexico and old Spanish certain news items such as this: documents in “An possession of the Gurule family of Placitas, old mine has been discovered in the Tijeras canyon, bearing the date with a tunnel 1667 AD., refer to five lost mines in this 75 feet in. Tools of the old Spanish pattern region of which the Montezuma were found in the Mine is one. This document tunnel” (Mining World, Las Vegas, v. I, mentions ‘Ia mina no. ll,July, de Bentana. Ia mina de Ia Escalera,” and 1881). states: “a) sur de Piacitas Ia mina Nepumeseno y en ci miseno in a description Canon Ia mina of the mines of Bernalillo County, one de Coloa.” (“the Window Mine. the Ladder author (Anonymous. Mine, and to 1906. p. II) stated that the south of Placitas is the Nepumeseno Mine and the Coloa “About two miles from the Placita of Tijeras, Mine”). The document goes on to say, “lado on the orenta de eastern slope of the Sandias. is the Longfellow Placitas Travegardo Ia mina Montezuma Antonio mine. . Jimenez.” It was discovered in 1840 and was meaning, “that to the east of Placitas, Antonio operated by a Jimenez Frenchman who reduced the ore was working the Montezuma Mine.” and to matte in a small adobe supplements furnace. The metal produced it with the statement that “Jimenez took twelve by this furnace was used in mules loaded casting many of the church with bullion to Old Mexico and never returned.” bells for small towns in this Prior to the portion of New Mexico. The remainder of Indian Uprising of 1680 these so-called “Mines the product was of Montezuma” shipped east by pack train. The owner, were extensively worked by Indian slaves by getting into from the pueblos trouble with the native populace, was forced of Cochiti, San Felipe. Santo Domingo, and to leave the Sandia. all situated country. Some time later the mine was again within a half day’s ride of the mines. worked by a During the Indian party from Chihuahua, Mexico, who shipped insurrection the mines of this district were part of the filled in ore east, but most of it went to and completely covered up and to this day Chihuahua. In 1863 the some defy mine passed into the hands detection. However, during the latter part of a Las Vegas merchant, who. of the last century. after a small amount five old Spanish ovens or ore roasts were of development work, encountered a located and in their large body vicinity two gold bars worth approximately of copper glance. He made no attempt to treat $2,000 apiece were the ore, but sent it by ox-team to Kansas City, whence it 98

that an old sheepherder had visited the mine one year before. Coast. the first shipment being was shipped to the Atlantic orin 1888. later shipments to Newark. to Baltimore, Maryland. and South-Western Mines, a monthly mining newspaper edited of three six-mule team-loads first New Jersey. [us last shipment by F. A. Jones. started publication Oct. 5. 1908. The ore was a high-grade copper in the netted a profit of 58.000. The number carried an article entitled “Mining activity and argentite. The gold glance with yellow and red oxide Sandias” (Anonymous. 908). A review of the Placitas district all cost of production. values in the ore alone paid contains the statement that “the Valley View properties In 1882 a contract was let io are transportation and treatment. belonging to the well known aeronaut, J. A. Blondin, the mitie. A body of clean out the old shaft and retimber showing up quite favorable Col. B. Ruppe and asso taken out, part being treated at the ore blocked out in 1863 was ciates were engaged in developing the La Luz mine, near and the rest was sacked and Carnuel San Pedro. Santa Fe County. crest of the Sandias. Also, there was activity in the of smallpox among the miners and the shipped east. An epidemic —Tijeras Canyon area, the Hell Canyon “district,” mine. Once more, in 1891—2. and resulted in the closing of the Coyote Springs “district,” In all, a dozen different contract.” were de work was commenced under independent operations in the Sandia Mountains places in the Ruins of ancient smelters were reported at many scribed in the article. near Mountains and “much of the slag now found Sandia was these old smelters contains gold in considerable quantities” ! had not a little difficulty determining why Mr. Blondin 20], item in the (Mining World, Las Vegas. v. 2. no, 9 110], Jan 16 IFeb. reputed to be well known. Eventual/i’ 1 found a news that ‘1oseph A. 1882. p. 169). Albuquerque Journal (July 7, 1907). reporting the east . . throughout According to Burke (1896. p. 24), Blondin, of Albuquerque . better known Coyote airship trials, proposes to make “The Longfellow mine, between Tijeras and as an expert in ballooning and great of aeronauts by attempting this canons, is an old Spanish working from which A lbuquerquefamous in the world days of distance ballooning held by Lt. quantities of copper were produced in the early fall to beat the record for long sailing in a balloon from Paris Spanish occupancy. Old copper vessels and implements Lahm, who won it last year by a distance of 402 miles.” from this ore are found occasionally, and the old across the channel to the English coast, made the first in show that much ore has been mined here.” In 1909, Blondin and Roy A. Stamm became workings fret. Accord America to make a balloon ascension above 5,000 except Journal, Aug. 8, No mine is known two miles from Tijeras ing to an obituary of Mr. Stamm (Albuquerque Sixth and Central, sailed ... off from possibly the Shakespeare about 1.5 miles to the south, 1957), “The two took over the Manzano Mountains and reacheda height of 13.000feet very doubtful that it was intended, as produc miles away but it is before landing two and a haf hours later and 90 metals in quantity is not of l(fl —not tion of copper or other base considerably short of their destination—Kansas. Loss short of 5 near Escabosa known. Other possibilities are not present bullets which were fired at them by a woodsman miles to the southwest or 10 miles to the north. Reports —was blamedfor the balloon s abrupt descent.” or of the type quoted above are often inaccurate in the AND exaggerated. However, if the Longfellow mine is MINING DIsTRIcTs, SUBDI5TRIcTs, Great area it is most likely either the Mary M or CAMPS below. Combination which are described For a long time the standard practice has been to district in mining district Gen. and Mrs. U. S. Grant visited the New Placers locate claims, prospects, and mines by of the San Pedro and is July 1880. Grant was elected president and subdistrict. Distribution of mines and prospects Company. It was reported that $800,000 was in Cañon de L’Agua shown in fig. 70. A confusing array of names is found paid for the San Pedro property. the early literature on New Mexico mining operations. “Some large nuggets have been taken out, and Grant, the terms “area” or “locality” were who recently went to New Mexico to take a look at Before 1882, the is the term “dis place, is credited with expressing his belief that there a generally used, Beginning about 1883, way. The good deal of money there if worked the right used increasingly. The first map of New can be trict” was great drawback is a scarcity of water. If this Graton, and and Mexico metals districts was by Lindgren, obtained it is said the placers can be worked profitably. our from the (1910). This recognized only two districts in Gen. Grant has an idea that pipes can be laid Gordon and sufficient water obtained” (Mining area, Tijeras Canyon and Placitas. Sandia mountains in 1911 World, Las Vegas. v. I. no. 1. Sept., 1880, p. 4). A Mining Map of New Mexico was published was In the New Placers district, Golden had 1,000 inhabitants the Clason Map Company of Denver, This map Howe by and a newspaper. the Golden Retort. According to Resources Survey of in also in Bulletin I of the Mineral (1881), pipes were being laid to bring water from reservoirs recognizes only 100 distance of 15 New Mexico (Jones, 1915). The text the Sandia Mountains to the New Placers, a 141. Four Later, excessive pressure caused districts whereas the Clason map shows miles. at a cost of $500,000. Bernalillo, pipes to burst on several occasions. districts are shown in Bernalillo County: these or Coyote Springs, Tijeras Canyon, and Hell Canyon hillside cuts for this old line are still east Remnants of Star (the last district is in the Manzano Mountains Palomas Peak. present south of of Isleta and will not be considered). In Sandoval the beaten According to Howard Bryan. in his column “Off County 3 districts are shown: Nero Placers, Placitas, 7. 1955), an article in the path” (Albuquerque Tribune, Nov. and Sandia. The Nero Placers constitute a westward Democrat of May 18, 1889 stated: Albuquerque extension of the New Placers district of Santa Fe “Considerable excitement prevails among prospectors vein of horn silver County. regarding the whereabouts of a certain is that the be hidden by the Indians in the An interesting feature of the Clason map that is supposed to from northern portion of the Sandias. A. & E. Railway is shown heading southeastward be the “For years the Pueblos have been known to Fe line a few miles northeast of in Elota, on the Santa possessors of a secret mine of silver that surpasses indicates a pro Mexico. Algodones, to Hagan, A dashed line richness anything known to exist in northern New few ornaments from Hagan southward to Frost, a They make rings, bracelets and other barbaric jected railroad the metal is Venus to join the out of pure silver, and when asked where miles north of Barton, and through or a obtained only answer by a shrug of the shoulders New Mexico Central Railway at Moriarty. Another grunt.” railroad is shown extending southwestward ore had been projected The article stated further that pieces of the silver Canyon to Albuquerque. Sandias, and from Frost through Tijeras found in arroyos along the western foot of the ______

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I0630 R4E, R. 5 E 3500 I062230’ cloyN’ R 6E. FIGURE 106 5 70—MINEs AND PROSPECTS (INCLuDEs ADITS, SHAFTS, INCIjNES. TRENCHES, PITS, AND QUARRIES). Pb, LEAD; COPPER: Ag. SILVER: Cu, Au, GOLD; Ba. BARITE; Fl, FLUORSPAR. l00

of the rail the Sandia area typically contain one or more Although extensive cuts were made south of 1-lagan be metals together with barite or fluorite which might was never laid. present in sufficient quantities to constitute an ore. few years earlier Frost and Walter (1906, p. 2) had A Small deposits of this type are present in the northern noted: of the mountains (Placitas district): in the southern part lof end The Santa Fe Railway traverses the southeastern along the eastern flank of the of the branch part (Tijeras district): Sandoval Countyj for about forty miles. and part above districts): to the coal camp mountains (assignable to either of the road of the Santa Fe Central from Moriarty to the New Frost. now under construction, is within the and in the Monte Largo area (assignable of Hagan via are mostly county limits. Placers district around Golden). The deposits rocks. With the used for various in the Pennsylvanian and Precambrian So many district names had been deposits in the decided to exception of some minor red-bed copper prospects in the area that Northrop (1959) deposits in Abo formation and possible small uranium recognize only two large districts, the Tijeras Canyon or that could occur in the Santa Rosa, Morrison, Bernalillo County and the Placitas in Sandoval County are Galisteo Formations, the metalliferous deposits (see also File and Northrop, 1966). and restricted mostly to the Pennsylvanian limestones Tijeras Canyon district embraces the following The those Precambrian rocks in proximity to the limestones. subdistricts, and camps: in “districts,” Thus, no precious or base-metal deposits are likely Manzanito Mountains Carnuel the Sandia Granite distant from the Paleozoic uncon North Manzano and Coyote formity, or in the younger (post-Permian) rocks in Sandia (in part) west of Coyote Basin around the Tijeras basin, Hagan basin, or those Sandia Mountains (in part) Coyote Canyon Placi (as. Soda Springs Coyote Springs Numerous small prospects, a few of which have Star The Hell Canyon produced some ore, occur in the vicinity of Placitas. Star Canyon the Hells Canyon Montezuma mine, best known of these, lies at Tij eras western base of Montezuma Mountain in projected and Star Of these, Hell Canyon, Hells Canyon, Star, NY2NW1/4 sec. 34, T. 13 N., R. 5 E. I mile east of Placitas large Canyon are beyond our area. (map 2). The deposits generally lie on or near the 191), According to Frost and Walter(1906, p. Las Huertas fault which has elevated Precambrian, less rocks of the Monte The Tijeras Canyon district has been prospected more or Mississippian, and Pennsylvanian

. properties during the past fifty years. and . . The principal fault block against red sandstone and mudstone the zuma are the Silver Dollar, the Carnuel. the Long View and Abo Formation. Vertical separation on district, better known for of the Permian . . Coyote Magnolia . Nearby is the ft. The wall rocks are consider mines, although at a very early this fault may be 2,000 its mineral springs than its on the surface and in Spaniards prospected near Chaves Spring and old ably broken and dragged as seen period the dug within prospect holes are scattered over the district. the shafts and small cuts. Three shafts were the 200 ft. The northern shaft collars in limestone of Placitas district embraces the following: The Mississippian Arroyo Peñasco Formation. It descends Las Placitas Algodones vertically and then inclines steeply to the west, evidently Montezuma Bernalillo following a vein on the fault zone. The shaft is covered Nero Placers Capulin Peak with heavy wire mesh and not readily accessible. The Placitas-Montezuma Juan Tabo dump contains much vein matter of fine-grained drusy Sandia (in part) from La Luz quartz and gossan along with green trap rock Sandia Mountains (in part) La Madera either a dike along the fault or from Precambrian No. I Sandia greenstone of the wall rocks. The middle shaft is about the The town of Bernalillo is in Sandoval County but 90 ft deep and lagged the full depth. It would be Clason map shows the Bernalillo district in Bernalillo inaccessible except in a rope sling. Similar vein matter County east of Alameda. and rock fragments constitute the dump. The southern The According to Frost and Walter (1906, p. 303), shaft is untimbered and is about 8 x 8 ft. the same limestone as in the The Placitas district is on the northern slope of the Sandia much-broken walls are of have been located: over and an old Mountains . . . The following claims northern shaft. The opening is wired Balcomb. W. J. Bryan. Nineteen Hundred, Shamrock. Bibo. pipe surmounts the shaft. From of headframe of steel Iron Cap. Montezuma. Yellow Jack and Valley View. East seen that Abo red beds in which are cement outcrops to the south it can be the Placitas district is the Sandia district, feet of drifting while copper. silver and lead ores are lie just west of the shaft. Several hundred beds carrying gold. blebs of found. The leading groups are the Gold Ring and Maceo. and stoping extends from the shafts. Small galena are readily found in vein quartz on the dump, but no sphalerite or any copper minerals are evident. METALS Soft seams of micaceous hematite occur locally along of 21 from the vein zone (Kelley, 1949, p. 230). A shipment Gold, silver, copper, lead, and zinc are extracted lead fillings tons of ore reported in 1920 averaged 12.5 percent small mineral deposits consisting of fissure-vein Other fractured, and Il ounces of silver (Elston, 1967, p. 29). with replacements and impregnations of is shipments were made as late as 1926 but the record permeable, or readily replaceable bedded rocks, espe masked by combined reporting from more than I mine. cially limestone. These deposits are usually formed from Ellis (1922, 41) reported copper and abundant hot juvenile or hypogene solutions ascending from p. fluorite from the mine. depth. Possibly some of these deposits may be attri Numerous small prospects are scattered through the buted to percolating ground water. Deposits found in 101

hills south of (he Placitas fault. These prospects are situated vertical fault striking N. 40° W. with principally south and southwest of Tunnel Madera limestone Springs on the east side dropped against Sandia and the old abandoned fish hatchery. The area Granite and is extensively Sandia Formation on the west. The faulted and fractured. Numerous small vein is 4 ft wide. 90 faults either ft long, and is exposed in mine workings parallel or branch from the principal faults through a (map vertical extent of 40 ftor more (fig. 71). I). Most of the prospects are in Pomecerro and The vein zone is Agua much brecciated and cemented Sarca Canyons. Veins and irregular pods cement by numerous white brecciated quartz stringers, often with coxcomb or shattered rocks. Commonly deposits occur crystal develop along ment. Fluorite is widely distributed faulted contacts between Precambrian crystalline replacing both the rocks and granite footwall and the limestone hanging limestone. Until a few years ago many of the wall. String prospects ers and bunches of galena with were still open to inspection, even though minor chalcopyrite much of constitute the principal ore. Calcite and the prospecting had been done as much as barite are also years 100 hypogene minerals in the vein. or so ago. Much information could be found Drusy and vuggy as to textures are common, and Phillips the nature of the deposits and the faults found malachite, or other chrysocolla. cerussite. and limonite structures that influence the formation of as common secon the deposits. dary minerals in Tecolote Canyon. Unfortunately, within the past few years many of the The main adit enters from the prospects have been bulldozed in some misguided south on an 18-degree effort incline intersecting the vein to restore the surface. Small piles of 75 ft from the portal. An ore and mineral incline upward from the specimens of the vein have been obliterated main adit reaches the vein 12 ft and mixed above the back part of with dump material. In some instances the lower level. soil and rock The La Madera mine from adjacent gravel along with is in sec. II, T: 11 N., R. 5 E. shrubs have been high on the west side dozed and shoved over the old prospects of a ridge 2 miles south of the old thus creating site of La Madera village. more scarred land than existed before. At the base of the ridge in Veins Tecolote Canyon are ruins of an old that have been seen or still may be partly smelter which may observed are have treated ores from a number of sources. generally 2 to 3 ft or less in width and not The La very persistent Madera mine consisted of several tunnels along strike. In most deposits barite, one above fluorite, another. The veins are narrow quartz, and calcite dominate, with usually and contain barite, only fluorite, quartz, and some galena. minor or local metallic minerals such as galena, The La Madera mine pyrite, is probably the same as marcasite, chalcopyrite. or sphalerite. The the Darrel prospect mentioned presence of by Rothrock and others former sulfides containing iron is (1946, p. 37, 39-40). markedly evident North along from the abundance of gossan. the ridge in sec. 2 a large cut 250 ft long, 30 ft wide, and 20 ft deep (Phillips, 1964, Ellis (1922, p. 41) described 2 groups of claims: p. 60) opened San the a north-trending vein along a fault José, 2 miles southwest of Placitas at 6,000 in Precambrian ft and rocks. Granite forms the west wall the Buckeye, 3.5 miles southwest at 7,500 with quartzite and ft. We have gneiss in the east wall. Fluorite, not identified these. According to Ellis barite, galena, and the deposit, chalcopyrite are the original which had been developed by two minerals. Secondary shafts and a tunnel, is fibrous malachite, chrysocolla, a fissure vein striking southwest “paralleling and cerussite are com the main mon. This mine may be the Schmidt line of displacement” (probably the Placitas prospect referred fault). The to by Rothrock. Near the northern ores are copper, lead, and silver. Silver end of the ridge and and gold usually the east quarter corner of sec. occur in such deposits but rarely 2 are several short tunnels in observable quanti and shallow shafts with ties. Their presence is similar but smaller veins. substantiated by the existence of The best known some gold-bearing gravel old mine in the Sandia Mountains is in the Placitas area. probably the La Luz, Wells and Wootton perhaps the highest mine in New (1932, p. 16) reported that “a Mexico. The deposit of altitude of the tunnel is 10,040 ft (fig. gold-bearing gravel conglomerate” had been According 72). worked as to Ellis (1922, p. 40-4 1) the La Luz vein a placer in the Placitas area. This might have was been along Las Huertas Canyon, the gold having come mostly from LONGITUOINAL PROJECTION scattered small Precambrian deposits along the base of Montezuma Mountain and in the head of the canyon. A small fluorite prospect known as the Capulin deposit is located in SE¼ sec. 33, T. 12 N., R. 5 E. Capulin on Peak, It is on the Lagunita fault in Madera limestone striking about N. 20° W. and dipping 60° SW (map 1). The vein cements a fault breccia 3 ft wide and consists of fine-grained purple fluorite. Small pockets of galena are present along with some barite, calcite, and quartz. The deposit is reported to have been opened in 1925 (Talmage and SCALE Wootton, 1937, p. 74) and Rothrock and 0 8 68 others (1946, p. 40) found that in 1927 the workings consisted of inclined shafts 20 ft deep and several small pits. A deposit LOWER LEVEL known as the Blue Sky (Phillips, 1964, 58-60) is located p. in the SW¼ sec. 26, T. 12 N., R. 5 E. I mile northwest FIGURE 71—PLAN AND SECTIONS OF BIuE of La Madera. The vein is along a nearly SKY MINE. SEc. 26. T. II N.. R. 5 E. (MODIFIED FROM C. H. PHILLIPs, 1964). 102

may not shown by Fayette A. Jones (Ellis. 1922) may or Upper Cut be correct. Elev l0,040ft According to Eldred Harrington (personal communi (opprox bc Ruppe cation. 1973) the mine was first known as the after the mine, and the term La Luz was not used until mine was La Luz trail was built. Original access to the all mining by trail similar to the La Luz trail, and road to materials and any ore went over the trail, as a used to Sandia Crest did not exist then. A small cabin Soodo Gronte Luz trail stand near the lower tunnel. The present La Lower Tunnel trail to the differs considerably from both the original Etev 9,750 ft Geological workings and the trail shown on the U.S. The lower Lowe, Survey Sandia Crest quadrangle sheet (1961). vein where portal is only about 100 yards north of the trail near its the trail is still on the north side of the canyon, Cross Section head. of the There are several prospects along the belt FIGURE 72—LA Luz MINE WORKINGS. The Tijeras Greenstone south of Tijeras Canyon. lie just Tijeras quadrangle shows 4. and 3 of these drainage. southwest of Cerro Pelon in the Coyote Creek discovered in 1887 by Juan Nieto. The approximate of the peak at the The other, the York mine, is 0.5 mile north position of the upper, discovery tunnel is shown U.S. Geological in Tijeras Creek drainage. head of La Cueva Canyon on the of 6,680 ft in NW¼ about 50 The York mine is at an elevation Survey Sandia Crest quadrangle. It is actually by traveling 2.5 trail to NE¼ sec. 6, T. 9 N., R. 5 E. It is reached than the present trail on an old original mile up a ft lower miles south up Garcia Canyon and thence 0.8 mine. The tunnel was driven northward into Sandia requiring the steep side road to the mine, the last 100 yards about 15 ft to intersect the vein, which strikes Granite a 4-wheel drive vehicle. The deposit is in a 30-inch-thick W. The cut is considerably caved, but much- N. 23° of marble in a fine-grained, greenish-gray green- seen and partly en band 770 timbered small workings can be is S. E. (47 degrees at fault dipping stone schist. Dip of the beds tered. The vein at the upper tunnel is on a to nearly 80 degrees calcareous the surface, but appears to increase eastward 75 to 80 degrees with Sandia in the sandstone in the hanging wall and reddish granite is 2 footwall. The Sandia is downthrown 50 ft. The vein Mineral to 4 ft wide in a sheeted and brecciated zone. of grains ization consists of fluorite with minor scattering and small irregular patches of galena. The ore consisted and mostly of lead and silver, but quite minor gold Luz copper were reportedly present. Currently the La patented mining claims are owned by Maxie Anderson of Albuquerque. According to Ellis the deposit was lost after first being was located but was rediscovered in 1907. The property 1909 purchased by Col. Bernard Ruppe and others. In the La Luz Mining, Smelting, and Development Com pany was formed. Between 1909 and 1921 a crosscut of was dug from the base of the granite cliffs southwest the upper tunnel and at 9,750 ft. It was driven vein northeastward about 272 ft to intersect the La Luz the and hopefully develop considerable backs of ore to ft surface. A vein in reddish granite walls was cut at 230 from the portal (fig. 73), and a small amount of raising ore. and sinking was done without finding appreciable The vein zone is 3 to 5 ft wide in sheeted and shattered granite. Vein matter consists of thin seams and irregular and small replacements and void fillings. Purple fluorite white to brown calcite are the principal minerals along with considerable supergene limonite. Galena or copper minerals are not readily evident, but minor quantities may be present. the There remains some possibility that the vein in lower tunnel is not the one of the upper tunnel and that of the latter would lie a short distance east of the end of the lower tunnel. We have not surveyed the position as 73—Lown PORTAL OF LA Luz MINE. AT BASE OF SHEER. the lower portal with respect to the vein outcrop, and FIGURE as TOO-FT CLIFF OF GRANITE. a result the projected connection of the two veins 103

in the lower part). An inclined shaft follows the ore to a The Great Combination mine depth of 120 ft (Bruns, 1959, lies in the northwest p. 30). The marble is corner of sec. 7. The workings sugary grained and gray Consist of a 255-ft adit to white. It is irregularly driven 5. 17° E. in greenstone impregnated with grains to the quartzite contact of pyrite. chalocopyrite. exposed up the ridge sphalerite, and from the portal. A narrow, quartz, usually in separate bands. Some apparently mineralized, gold shear zone was crossed at 200 ft probably occurred with the sulfides though concen from the portal (fig. 75). This zone was followed and tration is too low to constitute an ore. Bruns studied the apparently encountered good gold values not far ores in polished sections and found an early pyrite to the west of the adit. All the gold ore was mined replaced and cemented by chalcopyrite and sphalerite from the raise and stopes in this area, which is now and a later pyrite that either replaces chalcopyrite caved. The and raise and stopes were open in the early 1940’s sphalente or is contemporaneous with them. during a Late cursory examination of the mine. At that quartz is also associated with the late time an open pyrite. The ore stope 20 to 30 ft above the adit minerals do not appear to be syngenetic level was entered and in fact through a manway ladder. The mined appear to have been deposited after metamorphism area was not of large and mineralization appeared the country rock. Bruns suggests the possibility lenticular and that the spotty. Nevertheless, considerable free ores were of Precambrian age and introduced gold in pockets either was found, and shipments are reported from ore fluids from the Sandia Granite magma to have been or from made to a smelter in Socorro (Vincent a Precambrian metarhyolite mile Moore, written I south of the mine. If communication). In the early the latter source is considered, days the mine was owned an early stage of by a negro miner named Oxindine pre-metamorphic ore deposition would who was killed by a have been fol benzine explosion in his kerosene lowed by redeposition after metamorphism. cook stove! Along with the spottiness of the gold came The deposit was most likely exploited good specimens, for its gold and this is reported further to content. No record of production have led to considerable is known. It was last trouble with high-grading of samples. worked to some extent in the late 1930’s. The remaining exploited prospect The prospects southwest of in this area is in Cerro Pelon Peak are fluorspar veins in the quartzite. located around the head of In the absence of a a small valley that drains known name for the property southward to Coyote Canyon. it is herein referred to as Four are in the Tijeras the Cerro Pelon mine. The Greenstone and one workings consist of two in the quartzite which lies to the tunnels, a lower crosscut east. The 2 prospects adit at an altitude of 6,730 ft shown at the head of the jeep trail and an upper drift on the adit 130 ft higher on the ridge (fig. topographic map are the Mary M prospects. The 76). The lower tunnel was driven S. 34° E. for most of lower of these (probably on the Mary M no. 2 patented its straight-away claim) length of 475 ft. The upper, probably consists of a tunnel driven S. 48° E. for 220 ft, first, tunnel drifts on a slightly arcuate vein whose several short branches, and a finger raise about 75 ft to the surface (fig. 74). The base of the raise is much caved and very little vein material or mineralized rock is evident in any of the faces. However, 2 small shipments of gold ore are reported to have been made to the A. S. & R. smelter in El Paso (Vincent Moore, written communication). The upper prospect, probably Mary M no. 3 patented claim, is a nearly vertical, consider ably caved shaft sunk on a zone 6 to 8 ft wide, of quartz, calcite, and tourmaline stringers reticulated roughly parallel to the greenstone foliation. At the surface the foliation dips 63° S. 45° E. Gold assays probably motivated the prospect.

//

, (V (V U’ SCALE 0 0 50 100(1 (V

raise to surface 75’ lOOft

FIGURE 74—PLAN OF MARY M MINE. FIGURE 75—PLAN OF GREAT COMBINATION MINE. 104

may be found on tunnel appears mined. Minor malachite and azurite overall direction is S. 16° E. The lower descloizite has upper vein at depth the dumps and rare yellowish-green to have been driven to intersect the fractures in other in raises to the been found in thin coatings along where ore might have been stoped either level was cut in the vein material. Significant production from original development level. A similar vein Its strike, is doubtful. lower tunnel about 350 ft from the portal. Tijeras Canyon degrees The quartzite bed in the gneiss along is N. 4° E. with a dip to the east of 43 for however, dips has been prospected in a few places, presumably the upper vein strikes 10° to 28° W. and whereas gold. It is doubtful that more than traces would have to 80 degrees. The southern end of the eastward 50 been found. Also small pegmatite dikes in the Sandia in the tunnel is about 140 ft northwest of the upper vein Granite and the Tijeras Gneiss have been prospected, exposure of the vein in the lower tunnel. northern weak probably for feldspar or mica but without success. upper vein cannot be traced in Furthermore, the deposits described above include the principal tunnel more than a few feet The outcrop above the upper to us. Doubtless, other numerous smaller face of the tunnel. Likewise ones known south of its exposure at the important—remain to be discovered. in outcrop down the deposits—perhaps the upper vein cannot be traced other minerals like uranium, have 50 to 60 ft. Whether In addition, a few ridge north of the portal more than of formational characteristics fissure connection some potential because the two veins have a single common elsewhere. In 1954 E. C. rakes flatly to the that have yielded discoveries is not certain, unless the fissure that uranium claims had projection of the Anderson (1955, p. 18) noted southeast. Figure 76 shows a possible Tijeras Canyon and lower level to been filed for two localities in the vein in the lower drift in the plane of the T. 10 N., R. 5 E., drift. Had Coyote Springs districts: I) in sec. 23, conform with the vein curvature in the upper beds, vein in Madera limestone and associated carbonaceous adit been driven about S. 55° E. the in the lower and 2) in sec. 2, T. 9 N., R. 5 E., with copper minerals might have been intersected in half the distance. as it to Abo Sandstone. The latter location is erroneous upper vein cuts across quartzite beds dipping The contains no Abo outcrops. at 55 to 60 degrees. The vein occupies a the south The Abo Formation has a small red-bed copper brecciated fracture zone and consists of sheeted and near the center of sec. 23, T. 10 N., R. 5 E. The fluorspar, quartz, and jasper with local deposit pale greenish follows a thin shaly seam in a light-brown blades. Galena crystals occur locally. deposit patches of barite and locally granulitic sandstone. An inclined 12 to 30 inches wide and varies feldspathic The vein ranges from long follows bedding in the sandstone linings in breccia voids to tunnel about 60 ft from stringers and cavity is discontinuous and only 1 to 6 The lower vein is similar. (dips 5° N.). The seam rather coarse massive shoots. and minor azurite are the ore on joints to a 2- to 4-ft inches thick. Malachite It ranges from thin stringers the seam. A local flattened log raise and winze from minerals impregnating shoot where stoped in the short especially mineralized in its bark area. main tunnel. In about 3 ft long is the diagonal drift driven south from the veins occur at scattered localities with fluorite. Small barite-fluorite the raise patches of galena remain along of Monte Largo. Lambert have been in the Precambrian rocks fluorspar and possibly lead ore might small body of carbona Some (1961, p. 68-70) has described a tite associated with intrusive breccia in the southwestern A corner of Monte Largo (sec. 16, T. 11 N., R. 6 E.). gravimetric analysis made of a favorable sample yielded scat 0.295 percent Nb205. The exposure is small and elev. 6730 Lower no commercial ore body is indicated. N Tunnel tered and — Several valley and terrace gravel deposits in the area Aupper Tunnel have been prospected in small placer operations. Most barite of these have been more exploratory than productive. veinlets 1oult 52 These include: I) Las Huertas Creek near Tecolote Creek, mostly in the northern part of \ 2) San Pedro breccia \ T.12N.,R.6E. elev\ x T. 13 N., 6862 3) Coyote Arroyo, especially secs. 25-27, 70 fault Upper R. 6 F. 12 2, 3, II, T. 12 N., Tunnel 20” LowerlA 4 Cuchillo Arroyo, especially secs. 50 ° Tunnel 30° faults 2’ 8 ie. R. 6 F. stringers winze schist 80 sheor In the 1-lagan basin uranium has been prospected zones along the 0 using ground as well as airborne methods and probably Mesaverde and Galisteo out gabbed 75 Morrison 1” crops. Numerous claims are reported to have been 3tol /v is staked. According to Elston (1967, p. 59), “Selenium of reported to be associated with uranium in sandstones 0 20 40 80Ff in the Hagan —k--.. I the Mesaverde and Galisteo Formations B” I Abo, basin.” Doubtless other formations such as the been Santa Rosa, Chinle, and even Santa Fe have or considered as targets. So far significant anomalies shows have not been reported. FIGURE 76—PLAN OF CERR0 PEL0N MINE WORKINGS. 105

NONMETALS across of alternating chert and coarse barite bands with the latter Under this category are mineral and rock resources constituting about 60 percent of the exposure. A which have potential use and worth for their physical similar deposit is located along a fault zone in or NW”4 chemical character without extraction of the contained NW”4 SW’/4 sec. 9. T. 12 N.. R. 5 E. at 7.000 ft. The fault metals. For the Sandia area they could include barite. strikes N. 10° W. and is downthrown on the east. As with tluorspar, limestone, shale. gypsum. and stone. Some of the Landsend deposit the mineralization has spread the barite occurrences described here are similar irregularly away from the fault in several to limestone several described above under Metalliferous Deposits beds. Because the slope of the hill is normal to the strike where they were considered as gangue. The deposits of the fault, and because the vein occurs mostly along included here have greater quantities of barite and the fault, early prospectors probably very thought few metalliferous minerals. the vein trended up the ridge to the west. In an effort to find the ore in that direction a number of BARITE shallow dozer trenches were dug up the hillside for a thousand feet or so. but with nothing uncovered. A small barite mine referred to as the Las Huertas A prospect known as the Shakespeare mine existed deposit (Williams and others, 1964. 21-23) occurs p. atop a small hill in the NWV4 sec. 26, T. 10 N.. R. 5 E. near the projected southern quarter-corner of sec. 34, T. 1,000 ft northeast of the junction of the Chamisoso 13 N., R. 5 E. (fig. 77). The deposit is in overturned Canyon road with NM-l4 South. The deposit was basal Sandia Formation sandstone and limestone at developed by a vertical shaft and a few cuts. The shaft 6,450 ft on the steep western slope of Montezuma was more than 100 ft deep and had water in Mountain. A small diapir of fine-grained the bottom. Precambrian Another shaft had been dug on the vein gneiss is thrust up from the west overturning near the the beds to southern base of the hill (Brown, 1962, a dip of 65 to 80 degrees southwestward. p. 60). A short The deposit tunnel on the vein exposed the Otero fault cannot be traced more than about on which the 50 ft up slope above vein is developed. The dip is 80° to the cut face; it has the form 90° W. and the fault of a steep lens. An adit is downthrown to the west enters on the horizontal, (map I). The principal then inclines into steep slopes mineral in the vein and to a vertical is barite; some fluorite, quartz, and winze which is inaccessible but appears calcite are present. to be nearly 100 ft deep. Two caved tunnels 150 and 250 Unfortunately all these prospects have been ft lower on the hill appear to have been com driven to pletely bulldozed away within the intersect the deposit, and if they past two or three did, some barite may years. It is unfortunate as have been mined in raises. the exposures contained very worthwhile geologic relationships for the area. The deposit is predominantly coarse, tabular white barite, but considerable pale-green fluorite is present MINERAL SPECIMEN OCCURRENCES along with occasional 0.25 to 0.5-inch galena cubes. The Exact localities are not known deposit is as much as 8 to 10 ft wide. A sample taken for many of the by following interesting occurrences. Williams and others (1964, 23) contained BaSO4, In other cases, the old p. 71.1 dumps of prospects and percent; CaF2, 9.8 percent; and Pb, 0.17 percent. mines have been destroyed by owners or others wishing to discourage The Landsend barite is on a high ridge spur at 8,980 trespassers. Beryl In 1972 Jerry Cape found ft in NE¼ NW¼ NE¼ sec. 29, T. 12 N., R. 5 E. not far a specimen of beryl imbedded in quartz of a pegmatite dike. from Osha Springs (Williams and others, 1964, 23). The hexagonal p. crystal is 1.5 inches in diameter The prospects can be reached best by 4-wheel drive and light-greenish white. The locality is on the top of vehicle, traveling a distance of 4.5 to 5 miles over a small ridge spur in a the SW¼ NE’/4 sec. 2, T. ION., rough side road that leads from NM-44 at the R. 5 E. end of the Calcite Several varieties paved section. The deposits are in highly have been reported. Good fractured and crystals occur in concretions brecciated limestone along a small fault striking near Hagan. Anthraconite N. 52° has been mentioned in W. that is downthrown a few feet on the southwest early accounts as occurring side. between Placitas and Golden, The Madera limestone dips a few degrees eastward possibly in the Todilto on a Formation. Dripstone, calcareous low dip-slope bench. Eight bulldozer trenches have tufa, travertine, and Mexican onyx occur in been dug across otherwise rather poorly exposed Las Huertas Canyon and out especially in several caves. crops. Some drilling in the trenches is reported to have Cerargyrire (?) A news story been done, and it appears that the better holes were in the Albuquerque Democrat, May 18, 1889, reported subsequently opened into pits to check the ore. The a vein of horn silver somewhere in the northern Sandia prospected area is about 400 to 500 ft in length along Mountains; prospec the zone. tors had found pieces in washes along the foot of the mountains, and these The distribution of ore is irregular along, specimens would readily melt in and a short the flame of a match. distance away from, the fault zone. A honey-yellow Cuprodescloizite or Descloizite fluorite and a white, very coarse, tabular barite are the A thin yellowish- green stain and crust on dominant minerals. Minor galena crystals are present fluorite and quartzite was found on the dump of the Cerro and in places considerable gossan suggests former Pelon mine. Garnet Crystals as large pyrite. No copper minerals were observed. Large as 2.5 inches across were ro found just north of settelike masses of barite in plates nearly Embudo Canyon by Gordon H. 12 inches Wood, Jr. in 1941. in diameter dominate the deposits. The vein minerals both cement and replace “Graphite” Herrick (l900b, 12) described near coarse limestone and chert or Whitcomb’s p. jasperoid blocks. In one Springs “a considerable band of graphite place there is a mass 5 to 6 ft which has been opened under the supposition that it 106

r Shaft Contact Ant id in e -d- 70 Foult,steep reverse Strike and dip of overturned beds Tunnel &dump Fault, showing dip Strike of vertical beds i te A 650

6100 6H 6000 6000 -_/I /‘ 5900 5900 0 20 40 6Oft -1 I I __I J WEST Cross Section EAST Las Huertas Mine 45’-

FIGURE 77—GEoLoGIc MAP ANO SECTION OF LAS HuERT.s MINE AREA. 107

was coal.” Ellis (1922. p. 40) described it as “a rather impure grade of the amorphous variety.” in a bed I to 3 ft thick. Hematite var. Specularite Narrow seams of soft micaceous material were once mistaken for cinnabar in the Placitas district. Ilmenhle Tyson Ashlock (personal communication, July 10 and Sept. 13, 1954) found radioactive ilmenite in a small pegmatite in Tijeras Canyon: plates 3 inches across and 0.4 inch thick contained 0.005 percent uranium, a trace of vanadium, and possibly a trace of thorium. Ocher Older reports mentioned both red and yellow ocher, one bed several feet thick, in the Tijeras Canyon district. Elston (1967, p. 58) notes that Kelley thought one occurrence was probably a local spring deposit. FIGURE 78—IDEAL CEMENT Co. PLANT AT TUERA5 (LOOKING Hibben (1941, 3) found that yellow SOUTH). p. ocher “pervades TUERAS CREEK AND VILLAGE DWELLINGS IN FOREGROUND. the (Sandiaj cave in RoosEvELT all but the very lowest strata.” A. M0NTOYA PUBLIC SCHOOL ON FLAT SOUTH OF CREEK. P’romorphite Small crystals, less than 0.04 to about CEMENT PLANT AND 2 QUARRY PITS IN BACKGROUND. 0.08 inch long, of greenish amber-yellow color, and highly resinous luster, were found by Parry Reiche Nov. were drilled during exploration and development in the 20, 1943 in a small prospect pit on the north side of 1950’s. The bed that is being mined is 30 ft thick, Coyote Canyon north of Coyote Springs. The but pyromor erosional stripping has limited it to about phite is associated with fluorite and calcite. 20 ft in some faces (fig. 79). The bed is referred to as the Lime Kiln, a Silver In 1909, somewhere in the Placitas district, name given for its occurrence and use at the old lime Emil Kleinwort struck “some very high grade silver ore. kilns northwest of the plant. It is immediately underlain One nugget, as large as an egg of almost pure silver was by a reddish-brown shale which is mined for the clay taken out” (South-Western Mines, v. I, no. 12, Sept. 5, needed in portland cement; this unit is 16 to 1909, p. 5). 20 ft thick and is termed the Red Bed. Beneath the Red Bed there Strontianite Apparently the first reported occur is another limestone unit 65 ft thick referred to as the rence in New Mexico was by Guy V. Martin (oral Knobby, a name apparently given for nodular communication, June 27, 1936) at a locality lime about 2 stone and perhaps some nodular chert. The miles west-southwest of Tijeras. It Knobby occurs as radiating unit also has much intercalated shale, fibrous masses, with fibers and only about 15 2 inches long, of pale ft of the unit would be mineable yellowish brown color. limestone. All these units are in the Sol se Mete Member of the Wild Cow Tourmaline Masses weighing as much as 50 lbs were Formation. found by Gordon H. Wood, Jr. (oral communication, The Lime Kiln bed is variable in overall 1941)just north of Embudo Canyon. mine-run composition. Its better parts run about 94 percent Check lists of minerals, both megascopic and micro CaCO3 and mining cut-off’ is at about 75 percent. scopic, reported through 1960 from Silica the Tijeras Canyon is less than 5 percent and most of the lower and Placitas mining districts grade are given by Northrop between 75 to 95 percent of (196lc, 172, 173). the lower grade is p. attributable to shale laminations and the argillaceous nature of some parts of the limestone beds. CEMENT MATERIALS Analyses (Ideal Cement Company) of average quarry face samples are as follows: By far the largest and most important mineral resource of the Sandia area is limestone for the manufacture of cement. Although limestone is the most widespread sedimentary rock in the area, much of it is in high and inaccessible parts of the Sandia and Manzanita Mountains. The most accessible areas lie near Tijeras, along NM-l4 South, along 1-40 east of Zuzax, and around Placitas. Before Ideal Cement Company built its plant both the Tijeras and Placitas areas were prospected. Ideal’s quarries and plant south of Tijeras (fig. 78) are situated along the bottom of the northern end of the Apachitos syncline in the Wild Cow Formation (Myers, 1973, p. I). The limestone bed currently being quarried occurs at the surface of the following places: dip slopes of the west limb of the syncline west of the cement plant, dip slopes FIGURE 79—QuARRY to the south near the syncline axis, and OF IDEAL CEMENT Co. WEST OF PLANT. LIME the KILN BED WHICH HAS PRINCIPAL LIMESTONE ridge top south of the plant about on the axis. The SOURCE IS IN FACE OF SHALLOW QUARRY. “RED mine geologists early assigned names to the BED” SHALE ALSO QUARRIED IN LOWER units that SHALLOW CUT, IS JUST BELOW THE LIMESTONE. 108

buildings at Hagan usually anaisses of average quarr% face samples at The many abandoned Chemical of Mesaverde (Una de Ideal Cement Company. ‘ weight have foundations or lower walls sandstone surmounted by adobe bricks although Limestone: ( Loss-free oxides) Gato) Red Red ones like the old recreation hall have Composition No. 2 some of the larger No. I of concrete or tired clay bricks and 1348 52.04 parts constructed SiO 2139 some of the brick and tile came from the ALt)1 3.95 2.49 18.64 tile. Possibly 1.49 few remaining walls at Coyote Fe:O 1.06 0.67 Tonque brick plant. The 8.13 from CaO 71.47 45.03 are largely adobe although most foundations are 2.38 MgO 1.20 0.76 nearby Mesaverde sandstone. SO 0.03 0.02 0.06 consist mostly of 0.66 In the old part of Placitas dwellings Na.O 0.21 0.13 blocks from 0,22 0.14 1.81 adobe walls with foundations of sandstone KU At old Cañon Loss 36.99 13.86 either Dakota or Mesaverde sandstone. 99.07 the Total 99.43 99.7! cito, just off NM-l4 North on the east side of mountains, the houses are a mixture of Santa Rosa adobe, but considerable exterior stucco Production from the Ideal plant began in 1959 with a sandstone and prevents easy recognition. At Tijeras the old build capacity of 1,000,000 barrels a year. However, expan ing stone, adobe, and log types. The stone- sion was almost immediately necessary to its present ings include raw buildings are scarce but the few remaining ones annual capacity of 2,500,000 barrels. It has two walled built largely of red-brown sandstone of the Abo grinding mills, two kilns, and two finish grind mills. are (fig. 80). Some are a combination of red Fuel is gas. At present limestone is being mined from Formation in the lower parts surmounted by adobe or the third strip quarry to be opened, located on top of the sandstone Along NM-14 North there are a few dwellings ridge south of the plant. logs. of Mesaverde sandstone whereas on NM-14 In the beginning gypsum needed in the cement was made are some of Madera limestone. In Tijeras Canyon mined from a local lens of steep-dipping Todilto South is one stone house built in the 1940’s entirely of gypsum 4.5 miles north of the plant along NM-14 North there surrounding Sandia granite (fig. 81) and another in SW1/4 sec. 36, T. II N., R. 5 E. This deposit soon the on Cibola Gneiss constructed of assorted gneiss proved inadequate as a source and Duke City Gravel buiLt and associated aplite (fig. 82). Products Company was contracted to develop a much types larger source on the San Felipe Indian Reservation along Tonque Arroyo in SW’/4 sec. 1, T. 13 N., R. 5 E. On the average about 60 tons of gypsum per day is trucked some 50 miles from Tonque to Tijeras. In addition to limestone, shale, and gypsum, a small quantity of iron oxide is necessary in the manufacture of portland cement. For this requirement about 20 tons per day of iron ore is contracted from a mine at Jones Camp (Kelley, 1949, p. 2 13-223) in Socorro County. BUILDING STONE Included here is any hard rock trimmed, broken, or untrimmed that is used in construction. Such rock must be well cemented, crystalline, and durable against wear, solution, or staining by weathering. In the Sandia area a variety of rocks has been used or could be used such as granite, gneiss, quartzite, schist, limestone, sandstone, EAST OF TIJERA5 STURDILY CONSTRUCTED and certain dike rocks. In the past many small build FIGURE 80—Dwu.itNG OF AB0 SANDSTONE. ings, walls, streets, or walks in the Albuquerque region have been built of rocks from the Sandias. More use probably would have been made of these rocks had not adobe been so available and suitable. Further curtail ment of the use of natural stone as well as adobe has come during the past three decades with the develop ment of fabricated blocks, slabs, and walls from crushed stone, gravel, and volcanic cinders. In the past many dwellings in the Sandia area have been constructed of the local stone, most commonly Precambrian granite, gneiss, or quartzite, Madera lime stone or sandstone, and sandstone from the Mesaverde, Dakota, Entrada, Santa Rosa, Yeso, Abo, or Sandia Formations. In the construction of such buildings and associated walls or walks pieces of suitable shapes and colors are found in the nearby area or dug by hand from BUILT OF local outcrops or soil, and usually used with a minimum FIGURE 81—DwELLING IN TuERAS CANYON SOLIDLY of breaking or trimming. SANDIA GRANITE. 109

Flagstone for walks has come most commonly from LOOSE AGGREGATES thin-bedded but well-cemented sandstone of the Santa Sand Rosa or Chinle Formations. Bedding needs to be and gravel are the principal loose aggregates used in parallel with easily split partings at intervals of 2 to 4 construction, especially in concrete. Because of inches. Weak clay laminations within the flagstone slabs abundant supplies in the Rio Grande valley little is produced cause them to peel and flake with weathering and use. in the Sandia area. Sources are, however, plentiful During the past decade with the surge in highway in the lower courses of most canyons and in the widespread construction, park development, and architectural land alluvial aprons bordering the front of the Sandias scaping many boulders and huge blocks have been and spreading widely east of the mountains brought from the mountains to the city. Some of these into Estancia Valley. Much sand and gravel is also present have been quarried from favorable outcrops. but the on the Ortiz pediment surfaces around the San best are the very large. weathered, and natural- Pedro drainage system north and east of the Sandias. Elsewhere, appearing boulders often with lichen coverings that particularly along the Tijeras drainage have been selected individually from readily accessible system, local old river terrace gravels constitute lesser spots along the edges of the mountains. Small local sources. The New Mexico Highway Department has firms are sporadically in the business of finding and used these supplies at times mostly as fill barrow supplying such rocks to lawn and landscaping compa material or on occasions as a subgrade. As the area to nies. In other instances contractors and institutions the east of the mountains is developed these local simply find their own as needed. Thus, the University, supplies continue to be used by individuals as well as the city or the county may on occasions use their own contractors for road surfacing and other construction. equipment such as small lifts or cranes to get the stone. Rock for preparation of crushed aggregate used in Along the numerous road dividers in Albuquerque building subgrades has been mined from two quarry pits. there are examples of large boulders brought from the both in Madera limestone beds, One of these is in Sandias. Perhaps the best of these are the large SE1/4 sec. 5, T. 10 N., R. 6 E. (fig. 83) along the old spheroidally weathered residual boulders of Sandia US-66 route. This pit has not been used for nearly 40 Granite. These fine specimens were weathered in place years. Another pit along NM-14 near the edge of sec. 34, and commonly have a nubby appearance caused by the T. tO N., R. 5 E. on the Molly R mining claim (owned resistant large feldspar phenocrysts standing out on the by W. G. Nickol), has been a source of crushed surface. Elsewhere on road dividers are reddish-brown aggregate for 1-40. sandstone blocks from the Abo Formation, Precam LIME brian quartzite and even some white gypsum from the Todilto Formation. In the past lime has been made in small kilns using Another use of stone is as riprap, which is commonly the local limestone. Lime is calcium oxide, CaO, and is laid to prevent rapid erosion. It is used as a lining in the made by dead burning limestone or dolomite to drive south diversion channel, locally on steep fill slopes off the carbon dioxide. Lime has a variety of uses as in along highway fills, especially near overpasses, and plasters, agricultural soil improvement, smelting of ores, along certain dams, spiliways. culverts, and river em refractory furnaces, and numerous chemical processes. bankments. Angular Talmage rather than rounded rocks are less and Wootton (1937, P. 107) reported that at likely to roll in heavy run-off. Most riprap used in the least nine counties in the state had quarried limestone Albuquerque area has been angular volcanic blocks, for the production of lime. obtained along the Rio Grande, as seen in the south A number of old small kilns are scattered in Madera diversion channel and around the Dukes Baseball outcrops of the mountains. Two of the largest of these Stadium. However, in a few small areas quartzite from kilns are at the base of the limestone ridge on the south the Manzanita Mountains has been used. side of Tijeras Creek about one-third mile west of the

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- - h.,, - w7 f- ‘..,/ , Photo b Gene Polk. Marvin Maiheny. and John Lookingbill FIGURE 82—LARGE DWELLING IN TIJERAs CANYON AT ArANAclo FIGURE 83—HIGHwAY LIMESTONE AGGREGATE RD.. BUILT QUARRY ALONG OLD OF VARIOUS TYPES OF GNE1SS, SOME APLITE, AND MINOR US-66. SMALL ANTICLINE EXPOSED IN WALL IS FORMED AMOUNTS OF GREENSTONE. BY DRAG ON FAULT TO RIGHT OF VIEW. 110

claystone in the east and west walls, but village of Tijeras. The old kilns have been filled recently dark-gray of fine-grained shaly sandstone in the south to prevent people from falling into them. They are consists Another smaller pit lies 200 yards to the south. about 25 ft apart and about 30 ft high. One kiln is lined wall. production from the operation is reported to with a huff-colored sandstone and the other with brick; The last about 1938. The following is an analysis of they are surrounded by a buffer fill of sand held in place have been Tonque pit clay by Hawks(1970. 17). by a rock wall. The limestone used to make the lime the p. came from a quarry immediately south of the kilns. The SAMPLE SD64-3 (Mancos Sb.) ft wide, and 15 ft quarry, which was 150 ft long. 100 yellowish-brown now quarried by the Raw color deep is in the same limestone bed Munsell designation IOYR512 Ideal Cement Company a short distance to the south. Water of plasticity () 17.2 Drying behavior good. slight scumming SHALE AND CLAY Linear drying shrinkage (s-) 6.2 Dry modulus of rupture (psi) 921 and claystone occur principally in the sedimen Shale 2000 Madera Formation and in the Mancos Firing temperature (SF) 1800 1900 tary rocks of the good good good Additionally clay of worth Firing behavior and Mesaverde Formations. Color light-brown light-brown grayish-orange might be found in the Sandia Formation, in red Munsell designation 5YR5/8 5YR6/6 IOYR7/4 claystone of the Abo and Chinle Formations, and in the Firing shrinkage ((IL) —0.5 —0.2 0.2 5.7 6.4 gray claystone of the Morrison Formation (Hawks, Total shrinkage () 6.0 Modulusofrupture(psi) 1918 2206 2302 1970, p. 7-13, 15-22). Some valley-bottom alluvial clays just as brick Water oIahsorption () are of potential use in the mountain areas, (5 hr) 18.4 18.8 16.3 the 2.62 clay has been produced from flood-plain clays of Apparent specific gravity 2.70 2.70 1.80 Grande valley (Talmage and Wootton, 1937, p. 64). Bulk density (g/cm1) 1.80 [79 Rio 11.3 11.4 I l.5 The only clay mining in the Sandia area is from a Ignition loss (%) 40-ft dark-gray claystone bed in the upper part of the made at Tonque are reported to Madera. These beds have recently been included in the Many of the bricks poor quality. middle Pine Shadow Member of the Wild Cow Forma have been of tion by Myers (1973, p. 1). The Kinney Brick Company, successor to the New Mexico Clay Products Company COAL bricks from Rio Grande clays, discovered the that made In areas surrounding the Sandia Mountains coal is claystones of the Pine Shadow in secs. 18 and 19, good almost entirely in the Mesaverde Formation. Very R. 6 E. in the early 1950’s and located the T. 9 N., locally it may be found in seams a few inches thick in under several Hattie claims. The Hattie clay deposits the Sandia Formation. One of these may be seen in the pits have continuously produced brick claystone since roadcut opposite the Doc Long picnic grounds. Sur 1954 and have averaged 18,000 tons per year. The rounding the Sandia uplift Mesaverde occurs in the claystone is trucked to the brick plant in Albuquerque. Hagan basin, Tijeras basin, and 2 patches west and data on the Hattie claystone has been given by Test northwest of Placitas. In general, Mesaverde seams are (1970, 12) as follows: Hawks p. thin, discontinuous, and scattered through the section. SAMPLE B64-l (Madera Fm.) Available analyses indicate the coals to be high-volatile ranging from 31 to 55 medium-gray bituminous with fixed carbon Raw color part, is less than I Munsell designation N 5.5 percent. Sulfur content, for the most Water of plasticity () 18.9 percent, although I analysis from the Holmes mine in Drying behavior good Tijeras basin averaged about 3.5 percent. Keyes (1904, 6.0 Linear drying shrinkage (%) 671) records 4 analyses as follows of Hagan coals but Dry modulus of rupture (psi) 1006 p. from his context it is not clear whether they are from the Firingtemperature(°F) 1800 1900 2000 from any of several other mines in the cracks Hagan mine or Firing behavior good good small red-brown red-brown basin. Color red-brown I II III IV IORSI tO M unsell designation l0R5/ tO l0R5/8 0.89 Moisture 5.10 2.50 7.09 Firing shrinkage (%) 0.0 —0.4 —0.4 Volatile matter 39.60 39.35 41.29 32.36 shrinkage 6.0 5.6 5.6 Total (‘) carbon 48.92 50.60 48.17 54.88 2750 2594 2165 Fixed Modulusofrupture(psi) Ash 6.18 7.18 3.45 11.87 Water absorption (%) (5 hrs) 12.4 12.1 10.8 Sulfur 0.53 0.45 0.67 1.07 Apparent spec. gray. 2.36 2.36 2.44 1.86 1.87 Bulk density (g/cm) 1.86 HAGAN BASIN FIELD Ignition loss (%) 13.2 13.2 13.2 Pyrometric cone equiv. cone 4—dark olive Coals of the Hagan basin were designated the Hagan coal field by Keyes (1904, p. 670) and Una del Gato by Campbell (1907, 427) from the aban In the early 1930’s a claystone pit in Mancos Shale coal field p. Mexican settlement of Una de Gato (cat’s claw) I was opened up along Tonque Arroyo near the aban doned mile south of 1-lagan. However, Campbell further doned settlement of Tonque in the Hagan basin. The referred to the Hagan field for the coals mined near the claystone was used for making brick, and kilns near the now-abandoned mining town of Hagan. the Sloan field pit are reported to have been fired by coal from the for the Sloan mines, and Pina Vititos field for the seam Hagan basin. The principal pit next to the abandoned at the Pina Vititos mine. These small areas would have brick plant foundations is 150 x 150 ft and as much as been better referred to as camps or settlements. Inas 20 ft deep. The deposit consists of moderately dipping 111

much as the coals occur in a downwarp best referred to as the Hagan basin the term Hagan coal field is preferred. The most work to date on the Mesaverde Formation of the Hagan basin was done by Harrison (1949). He measured a section along Pinovetito Arroyo (on modern topographic quadrangles referred to as Tuerto Arroyo) in sec. 6, T. 13 N., R. 6 E. and subdivided it into 1’ informal units as follows: Coal-bearing shale member no. 3 5901t Sandstone member no. 4 656 Coal-bearing shale member no. 2 521 Sandstone member no. 3 248 Shale member 67 Sandstone member no. 2 589 Coal-bearing shale no. I 661 Cano sandstone member 246 Total: 3.578 Of the 3 coal-bearing units, only member 3 contained coal seams in the Pinovetito section, although coal does occur elsewhere in the lower coal-bearing units. In the 590-ft upper shale unit Harrison described 9 seams distributed in the middle 245 ft as given in Appendix 1; dimensions are tabulated below: Interval No. (seeAppendixl) 31 32 43 45 50 Interval thickness. ft 24 7 15 43 II Seam thickness. inches 30 12 12,22 12.16,18 4.36

Ft ,,. above base, No. 3 shale 124 148 241 263 358 ,,., . For the Pina Vititos area in general, however, Harrison (1949, p. 167) gave 11 seams ranging from 4 to 44 ,‘— inches, but only 3 were greater than 24 inches thick. The 36-inch seam of interval no. 50 above is the principal FIGURE 84—PINA VITIT0s MINE PORTAL. coal at the Pina Vititos mine. Pina Vititos Mine—The Pina Vjtitos mine lies in the lateral variation would likely be problems for develop SW¼ sec. 32, T. 14 N., R. 6 E. Pina Vititos (small silver ment and mining. Campbell (1907, p. 429) measured 66 fir tree) is a corruption of Pinabetitos, the diminutive of inches of coal in one exposure with two partings, 11.5 “pino abeto,” according to Ruben Cobos (personal and 15.5 inches, with the middle coal 7.5 inches thick. communication). Various spellings have been used, such Campbell (p. 430) gave an analysis of the Pina Vititos as Pinovetito. The principal workings at the Pina Vititos coal as follows: moisture, 9.03; volatile matter, 42.35; mine is an incline driven N. 85° E. down the seam at 28 fixed carbon, 44.17; ash, 4.45; and sulfur, 0.66 percent. degrees. The incline appears to have been dug with 7-ft Sloan Mine—The Sloan mine is 2.3 miles south of auger as shown by a circular cross section partly the Pina Vititos mine; in spite of soil and alluvium preserved in the roof sandstone 50 ft below the portal. concealing 1.5 miles of this distance, the two mines are At the right side of the portal the seam is 27 inches thick doubtless in the same coal zone. The Sloan mine lies including a 2-inch carbonaceous shale parting 8 inches just east of the adobe ruins of the old settlement of from the top. However, on the left side of the portal the Coyote which is along the Tonque road 0.5 mile east of seam is 40 inches thick with no parting (fig. 85). The the Diamond Tail ranch headquarters. Seams appear to roof of the coal at the portal is 36 inches of gray 1 claystone beneath massive buff sandstone. Followed ..,.,.,.-. down the incline the claystone thins to 6 inches as the PS .,, sandstone channels into the coal. The floor consists of - 4:

grayish-brown shale. - The Pina Vititos coal has been prospected for 1,500 ft to the south in several similar inclines (fig. 86). At one of .- these there is a remnant drum of an old horse whim used in mine haulage. In one of the better preserved openings a double seam consists of a 24-inch lower part and a 22-inch upper part separated by an 11-inch claystone parting. At the left of the portal a small fault confined to the coal zone brings claystone opposite the coal seams. The massive sandstone of the main portal also forms the roof at this opening, but south it pinches out locally. The same brownish shale forms the floor. FIGURE 85—CoAL OUTCROP Irregularities of seam thickness, AT LFFT SIDE OF PINA VITITOS MINE splits, and abrupt PORTAL. BOTTOM OF SEAM AT HAMMER HEAO TOP, AT PENCIL. 112

seams is mostly shale and claystone. but a massive sandstone bed lies 5 to 10 ft above. In a small canyon 100 to 200 ft to the north 5 small coal seams crop out in a weathered slope, but only 2 appear to approach 30 inches in thickness. All the main workings at the north end of the exposed belt are nearly completely caved and exposures are lacking. although there is much evidence of mining in the form of widely spread waste dumps. In 1904 the U.S. Mine Inspector described the Sloan seam ft down the (p. 38) as 7 ft thick just above a fault at 200 slope, but stated that “two shale splits ... reduced the net coal materially.” Harrison (1949. p. 167) measured 6 seams near the :. Sloan mine ranging from 8 to 34 inches in thickness, but , with only 2 above 24 inches. Campbell (1907. p. FIGURE 86—PINA VITrrOS COAL-BEARING ZONE SOUTH OF MAIN 429-430) measured 1 coal section at the mine 44.5 IN DISTANT PORTAL. NOTE 3 SMALL ENTRIES. ORTIZ MOUNTAINS inches thick including an 8.5-inch middle shale split. He B ACKGROU ND. further reported two analyses as follows: be in two zones separated stratigraphically by 90 ft (fig. (a) (b) 87). Several inclines are along each zone, but all are Moisture 9.68 7.28 narrowly open. Keyes (1904, p. Volatile matter 42.32 42.49 either caved or only 41.36 43.60 in 92 ft of shale, claystone, and Fixed carbon 671) observed 4 coals Ash 6.64 6.63 sandstone, the thickest being 30 inches. Sulfur 0.66 0.67 The principal exposures are along a dissected 600-ft (a) Analyst A. A. Somermier exposure north of a left-offset oblique fault (map 1). A (b) Pittsburgh Testing Laboratory unit lies about 100 ft west and massive white sandstone Two other analyses of the coal of this zone were made in the lower coals. This is the Una stratigraphically below 1936 (Fieldner, Cooper, and Osgood. p. 56-57: 93-94) 1904) that forms the hog- de Gato sandstone (Keyes, by the U.S. Bureau of Mines which are as follows: backs above the coal at Hagan. About 800 ft south of DonneIl2 the main portals and dumps, the Una de Gato is offset Sloan’ near the Moisture 9.7 ll.0 about 500 ft northwestward to a ridge position 42.3 38.5 coals. The offset Volatile matter fault termination of the uppermost Fixed carbon 4l.4 44.3 seams should be north of this sandstone ridge but little Ash 6.6 6.2 prospecting appears to have been done in this area. The Sulfur 0.7 0.6 seams dip east at 25 to 35 degrees, the steeper near the 1Seam 36 inches and 20 ft from portal. fault. of Sloan mine in SE’4 NW’4 sec. 17, T. 13 N.. and near the 2Prospect southeast At the southern end of the lower zone R. 6 E. sampled 60 ft downslope from 18-inch seam. fault a portal exposure contains a 20-inch seam with a 4-inch shale parting. In the upper zone also near the Hagan Mines—The Hagan mines lie in the NY2 sec. fault there are several portal exposures. One of these 33, T. 13 N.. R. 6 E., south and east of the abandoned shows 2 seams each, 20 to 24 inches thick, separated by town of Hagan (fig. 88). The seams are in a lower zone 10 ft of shale; however, most of the opening is caved than those around the Sloan mine. lies section and it appears that the main, perhaps thicker seam, Keyes (1904, p. 671) found 8 seams in a 151-ft beneath the caved material. The roof of the principal

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- .-, - .— - - 7.,• ..,.——- . .

FtGURE 88—HAGAN RUINS AT CENTER OF CAMP. INCLINE PORTAL AT RIGHT FOR SEAM NORTH OF DIVIDtNG FAULT IS AT BASE OF RIDGE 87—UPPER COAL-BEARING ZONE AT SLOAN MINE. FIvE COAL FIGURE RtDGE TOP IS FROM CUT MADE FOR TO FT ARE tN EDGE OF PHOTO. DUMP FROM SEAMS RANGING tN THtCKNESS FROM 6 tNCHES 2.5 FOR SEAMS TO SOUTH OF FAULT SMALL TREE. CONCRETE WATER TANK. PORTAlS SHALE AND CARBONACEOUS SHALE SLOPES BEYOND LIE BEYOND RIDGE IN UPPER RIGHT CORNER. DUMP OF SLOAN MtNE tN UPPER LEFT CORNER. 113

of shale and thin sandstone beds beneath the ridge- forming (I) 12) massive sandstone unit above the 1-lagan Moisture site. 7.8 6.1 This unit he designated the “LJna Volatile matter de Gato sandstone.” a 29.1 38.5 name Fixed carbon which has been missed by compilers 51.0 of the Ash 43.3 U.S.G.S. Lexicon of Geologic Names. 13.8 Keyes’ section of Sulfur 6.2 the coal-bearing sequence beneath the Una 0.9 0.6 de Gato Sample no. I. 48 inches sandstone is as follows: thick: sample no. 2. 49 inches: both with an 18-inch claystone split, a roof of sandstone, and a floor of shale. Coal No. 8 I ft Coal Shale reserves of the Hagan basin 36 have been Coal No. 7 measured by Harrison (1949. 2 p. 166-169) and by Read Shale and others (1950, 3 p. 16-17, 20-21) with general agree Coal No.6 ment. Read and his associates Shale discussed with Harrison 33 the methods they had Coal No. 5 employed. Read and others 2 Shale (1950) computed the following 8 indicated original Coal No. 4 Hopewell reserves for the 1-lagan seam 4 field (in tons). Shale 9 Overburden Coal No.3 Thickness Intervals (inches) 3 (ft) Total Shale 14—28 28—42 >42 19 Tons Coal No. 0—1000 3.900.000 3.100,000 2 — 7.000,000 Shale 1000—2000 2.900.000 2.800.000 26 — 5.700.000 Coal No. 2000—3000 2.600.000 I 600.000 — 3 3,200.000 Total: Totals: 151 9.400,000 6.500.000 15.900,000 Harrison, although Harrison using the same general guidelines (1949, p. 166) traced and measured 4 seams with regard to extrapolation with average of reserves to depth on the thickness of 18, 45, 8, and 17 inches in basis of outcrop lengths order upward of measured thicknesses, chose in the zone. According to him the 45-inch to present his data seam by individual seams for which he is relatively uniform in thickness, whereas assigned average others the thicknesses. He did not lump the thicken and thin through short distances reserves into the grade and 18-, 28-, and 42-inch categories, except into carbonaceous shale. In 1904 the U.S. to exclude all seams Inspector Mine of average thicknesses less than 14 (p. 37) gave 4 seams for the zone ranging from inches. His totals, which 3.5 to are within the same certainty 5 ft thick named in ascending order: McCance, degrees, are as follows: Kennedy, 1-lopewell, and Andrews. The Hopewell was Hagan area the principal bed; 54 I 1,504,800 tons inches thick, dipping 15 degrees. Sloan area 2,537.050 An east-trending fault followed Pina Vititos by a canyon separates area 8.524.800 the seam and mining Total: into two parts. It is reported that 22,566,650 the two parts were separately owned mines. A single Almost one-half of Harrison’s portal enters the principal seam north reserves are for one of the fault and 45-inch seam at Hagan. near the center of the old town. In both estimates it is obvious The beds in this that most of the upthrown segment dip 550 reserves include seams impractical to N. E. at about 25 degrees. mine, especially Mining from this incline extended on the 25- to 35-degree slopes prevalent in places to the basalt in most of the Hagan dike 3,000 ft to the north where basin. On the geologic side of the coal was cut off. potential (or inferred) South of the fault there reserves it is interesting to note are 6 inclines, mostly caved, that Read’s along the base of an group (1950, p. 20-2 1) gave no reserve east-trending hogback through an the for outcrop distance field at any depth for seams that might of 3,000 ft. The seams in this down- be greater thrown than 30 inches thick and only a potential block dip 35°N. Three principal coal (above their along seams are total of 16.2 million tons of this stretch. The middle seam is indicated and measured located 50 ft categories) of 800,000 tons stratigraphically above the lower end above 14 inches thick. The and about 100 ft basin certainly has more below the upper one. Only the incline potential, especially if under at the west end is ground gasification were on the upper coal. Likewise only to become feasible. Also, these 1 incline is on the calculations of lower seam and this is reserves do not include the potential of at the next to the easternmost the covered mine location where areas in either direction from the there is also an incline on the camp, Sloan middle seam. in the covered area north of the Only the easternmost incline is open, but Pina Vititos even this exposures, or beneath the Ortiz gravel is caved about 40 ft down. A seam 35 inches cap east of the thick was measured. Hagan camp. Prospecting The coal seams terminate for coal and some production for house against the upthrown hold and local northern block approximately use probably went on in the Sandia area 1,000 ft downdip, with for some years the upthrown seam lying prior to 1900. However, better sources 600 to 1,200 ft higher on the the Gallup, in north side. Some mining is reported Raton, and Cerrillos areas tended to to have reached the concentrate development fault. The situation is such and mining in those fields as to have required 2 where coal mining separate operations. began in earnest with the building of Fieldner, railroads in the period of 1878 to 1882. Cooper, and Osgood (1936, 56, In 1903 the U.S. analyzed p. 57, 93) Mine Inspector (Annual Rept., two samples from the Hopewell seam taken p. 66) reported, under C. C. by “new mines opened,” the Una Mather, Nov. 14, 1923, 1,200 ft del Gato (Hagan) and down the slope of Pina Vititos mines what was referred to as the in Santa Fe County operated by the number I left entry: New Mexico Fuel & Iron Company owned by E. B. ______

114

worked No. men Tons mined Tons sold a railroad Year Days Field. In 1904 the inspector first reported (926 (07 7.557 16.477 & S.F. near Algodones. Although 1927 276 (2 22.215 branch from the A.T. 13,712 continue to be mentioned in (928 234 16 18.440 plans for such a spur line (6.348 (2,080 bed was built, no line (929 (90 (9 many succeeding reports and a no reports mine may have (930 was ever completed. The Pina Vititos 7 15 3,110 1.291 tonnage 1931 been the first to produce coal, but there is little Total: 67.670 evidence of mining. recorded despite the considerable by wagon or truck to the Coyote, appears to The Hagan coal was hauled The Sloan mine, early referred to as of about 15 miles. It and mining railroad near Algodones, a distance have accomplished most of its development in New Mexico, reports it is reported to have been marketed by 1905. According to U.S. Mine Inspector period of produced Arizona, and Texas during its principal was not in operation from 1906 to 1908. It ton. Total in production at prices of about $3.00 per small tonnages to the nearby Tonque brick plant only production from the Hagan mines is not precisely was thereafter idle. The Hagan mine, early 1909 and known owning to lack of reports in some years and the to as the Una del Gato, operated in two periods referred fact that the mine and local consumption is not often 1903 to 1909 with two slopes to depths one from about An estimate is: 712 ft. Production was as follows: reported. of at least 1.020 and Tons Year Days worked Tons produced Value/ton (904-1909 12,100 1904 104 970 $1.50 1910—1925 3.200’ 1905 300 1.500 $1.25 1926—1931 67,700 1906 1.000 (est.) $2.00 Total: 83.000 1907 300 2.6(8 $2.00 small tonnages 1908 320 5.000 $2.00 ‘Estimated on basis of men reported working and 1909 200 1.000 $2.00 partly reported by day or year. Totals: 1.224 12.088 The Hagan mines were open through several down mines either did not From 1910 to 1917 the Hagan slopes with cross entries and back slopes. Mining rooms so small that it was not operate or production was are reported to have been 250 ft long and 30 ft wide. are gross production. reported. The figures given here Pillars between the rooms were 50 ft wide. Two mining less owing to The amount sold was often somewhat machines were introduced in 1926, but more than half mine. For example, in operating use of the coal at the of the coal was still conventionally mined by drilling 200 tons were used in 1904 of the 970 tons mined, and shooting. the other hand, in 1908 with operations by the mine. On Production figures are not known for either the Pina 250 tons were used by the 5,000 tons produced only Vititos or Sloan mines but on the basis of the number of of mining at the Hagan mine mine. In the later period openings and size of dumps, production is estimated coal-generated power used to from about 1919 to 1931, respectively at 2,000 and 8,000 tons most of which was at times extended by line and sold operate the mine was probably consumed either at the mine or at very local at Golden and San Pedro. to metal-mining operations markets. Further production for the Hagan coal basin of the 22,215 tons mined 3,353 For example, in 1927 came from the Tejon mine as reported by the State at Hagan, most of it probably to tons were consumed Mine Inspector without identifying its location. The first power plant that they had. In 1928 run the 750-kilowatt record is for 557 tons in 1926 by 1 miner. Later, from even greater amounting to nearly 21 the local use was 1933 to 1939, 8 to 15 men were reported working at the percent of the gross production. mine with production of 3,711 tons in 1937 and 5,137 period of mining at Hagan the During the second tons in 1939. John Jackson of Albuquerque was been owned by J. J. De Praslin property appears to have manager in 1939. and W. H. Stark. From 1919 to 1925 most of the work was development and construction. The work appears TIJERAS BASIN FIELD to have been desultory and interrupted possibly only as An area of about 5 square miles of Mesaverde beds financing became available. In 1925 mining again got occurs in the Tijeras down-faulted graben. Most of the underway for Hagan’s most productive period which coal occurs in the Tijeras syncline in an area approx extended through 1931. By 1932 the mines appear to imately I square mile (fig. 89). Coal was being mined as have been completely idled, and the settlement was early as 1898, for Herrick (1898b, p. 108) observed that soon abandoned. Yet today 35 to 40 building founda “coal is occasionally mined, as is the case north of the tions and collapsed walls can be found. The railroad cabins of Gutierez Esic].” A minor occurrence exists in a was never completed to Hagan. Work on the road bed narrow nearly vertical strip of Mesaverde in the west is reported to have commenced in 1909 but was sus limb of the Cedar Mesa syncline (map 3) in the pended that year. Additional efforts were probably southwestern corner of the graben. Most of the made during the 1920’s, but although the bed was Mesaverde Formation has been removed by erosion completed to Hagan it is doubtful that track was ever possibly less than half of its original thickness to the settlement. A bed was worked on from the and laid Three major sandstone units with two inter in Estancia Valley down San Pedro Creek, but remains. railroad coal-bearing shale units constitute the preserved the bed and necessary cuts were abandoned about 5 vening section. Coal seams in the shale units have been miles from Hagan. prospected and mined to some extent probably all for Production of coal from the Hagan mines for the smithing or household consumption. The seams are period of mining is (State Mine Inspector second generally thin and moderately to severely deformed. reports): 115

Lee (1912. p. 578) had 2 analyses (dry basis) made of stumpier coal penetrations there is commonly consider the coal: able contortion of the surrounding beds. The coal HoIme Mine Tocco Mine in the otTshoots is laminated parallel to the Moisture 1.6 0.8 walls, and it therefore appears that they are some part Volatile matter 31.3 36.4 of the underlying seam that has been thrust in sledrun FRed carbon 36.3 53.9 ner style over the younger beds. If this is so the thrusts Ash 31.3 8.9 Sulfur would be rooted within or at the base of the seam. The 326 0.88 action Btu 0.000 13.900 would arise from the usual slipping of upper over lower beds in the limbs of synclines. Lee 574-575) measured (p. the Cretaceous section Holmes Mine—The Holmes mine lies in the N½ and got a thickness of 1,309 ft for the preserved NWY4 SW¼ sec. 6, T. 10 N., R. 5 E. The Holmes seams Mesaverde beds. The seams in his section fall into 3 are in the same zone as the Section 1 seam but on the stratigraphic positions: 1) in a 32-ft shale section near opposite or southeast limb of the Tijeras syncline. The the top of the lower sandstone sequence that surfaces portal is only about 200 ft from the canyon bottom and most of the Tijeras anticline (Section 1 and Holmes the syncline axis, and the tunnel is driven N. 40° E. into zone), 2) near the base of the lowest of the 2 principal the hillside horizontally. The hillside slopes above the shale units, and 3) in the upper of the 2 principal shale tunnel are not much less than the dip of the coal; coal Units (Tocco zone). Lee did not indicate in his strati- can be found in the hill, mixed with soil in mantle creep. graphic section giving coal 3 zones which one was the Below the tunnel level the seam must flatten rapidly Holmes seam. Our mapping indicates that the Section 1 toward the creek and the syncline axis. The portal is and Holmes mines are on the same seam (fig. 89). Since completely caved. If the tunnel continues horizontally, a no coal is known below the seams mined in the 2 mines considerable zone would be available on strike. After a it is assumed that his middle zone of 2 coals separated few hundred feet in from the portal, backs of coal would by 15 ft of shale is above his ft 30 of sandstone. This not increase to more than about 100 ft for a distance of appears to fit the field mapping and a 40-ft shaft 1,200 ft nearly 3,000 ft from the entry. Below the tunnel, near up canyon from the Holmes mine may have been dug to the portal, the seam flattens rapidly toward the creek the middle coal zone. However, this zone has not and the syncline axis. Into the tunnel and above it, the produced coal. Furthermore, although all 3 zones can dips probably steepen from 20 to 30 degrees. Still be mapped throughout the basin, some exposures farther east the dip increases to 45 degrees along the indicate that none of the coal seams can be expected to zone. According to Lee (p1. 59) the Holmes seam ranged be continuous throughout their zones. from I to 2.5 ft in thickness. He also suggested that Section 1 Mine—The Section 1 mine lies in the “thicknesses vary greatly within short distances” and NE’/4 SE¼ NE¼ sec. 1, T. 10 N., R. 5 E. The incline that the coal is often “crushed and impure.” Some enters coal the side of a small sandstone-capped cuesta that has been produced from the Holmes mine. is stripped down the east flank of the Tijeras anticline. Tocco Mine—The Tocco mine lies near the center of The beds dip S. 85° E. at 15 degrees and the incline sec. 31, T. 11 N., R. 6 E. in Tijeras basin. The portal is slopes N. 85° E. at 10 degrees. The length is 225 ft (fig. caved but the incline can be seen to descend S. 12° E. at 90). Little or no work appears to have been done on the about 28 degrees. A waste tipple 25 ft high stands on the property since about World War I. The portal is nearly flat just north of the incline, which is reported to have closed from caving of the weak claystone which forms descended on the seam to 260 ft where water made the roof. There are no drifts or stopes; no coal, beyond mining more and more difficult. Of the 2 seams that of the incline, has been mined. The dumps are reported for the Tocco zone, Lee 577) reports the considerably eroded. (p. Some sand and mud have been upper I to have been mined, perhaps because it is more washed into the incline so that the base of the seam is uniform. However, he reported its thickness to range largely covered. Inasmuch as the incline is still 5 to 7 ft from 14 to 20 inches. The area underlain by the Tocco high, the seam apparently is not more than about 2 ft seam is only about 80 acres. thick. Even though I or 2 other seams may lie just below the Unusual exposures of folding and faulting of the coal one mined, the original inferred reserves would hardly and shale make the prospect a valuable geological be 1 million tons, quite small and essentially uneco feature for teaching and for interpreting the mechanics nomic. of deformation of the Tijeras basin. In numerous places, Very little history of development activity or mining well exposed in the tunnel walls, the coal has been exists for the Tijeras basin coal mines, although the thrust or buckled into the overlying claystone beds (figs. State Mine Inspector report (1908, 13) sheds some 91, 92). The protrusions rise from p. as little as 1 ft to well light on the Tocco mine. It was first opened in 1908 and above the tunnel roof and usually taper upward from I that year shipped 350 tons valued at about $4.00 per to 2 ft thick at the base of merging with the undisturbed ton. It was reported to have the rather dubious seam. They typically dip about N, 55° to 65° E. at 45 “distinctions of operating the smallest coal seam devel degrees. This direction is toward the bottom of the oped in New Mexico” and one of the smallest in the Tijeras syncline and oblique to the S. 85° E. dip of the United States and Europe. The seam exposed at that beds at the mine. Although basinward dips are dom time was 12 to 15 inches thick with ito 3 inches of bony inant there also conjugate coal flyers dipping in the coal at the top leaving only lO to 13 inches of clean coal. opposite directions. The coal does not completely The slope had been driven down 255 ft an average of 25 crosscut the claystone, rather the claystone beds above degrees. Cross entries were driven about 30 ft apart and the flyer are parallel to the coal. With the shorter, a right entry at the bottom was 70 ft long and a left 116

MINES. AND PROSPECTS. FIGURE 89—AIRvIEw OF TIJERAS BASIN SHOWING COAL-BEARING ZONES.

appears to have been entry 30 ft. It was very good coal and was hauled to thickness. Some household coal of these prospects. Albuquerque where the principal marketing was for mined sporadically from one basin cannot be given a smithing at $9 to S12 per ton. In 1908 the mine operated Reserves for the Tijeras measured and indicated cate 270 days with an average of 4 miners per day. The mine realistic estimate within poor surface and subsurface control. operated only into 1911 and produced 300 tons in 1909. gories because of would have to be done. Such l60tonsin 1910.and l6Otonsin 1911. Much trenching or drilling because the inferred or Three small coal prospects occur along the steep an effort is hardly warranted relatively small. Nevertheless, Read hogbacks of Mesaverde that form the west limb of the geologic potential is 400,000 tons of what Cedar Mesa syncline (map I) east of San Antonio. The and others (1950, p. 21)calculated reserve and 1,200,000 tons of prospects appear to be in the same zone as the Holmes they termed measured under 28 inches thick and only to and Section 1 mines. Attitudes are steep to near vertical indicated reserve—all of 1,000 ft. This depth would and the seams are not thick. Lee measured seams in 3 a depth of overburden potential coal-bearing zones. portals that range from 1 inch up to nearly 2 ft in take in essentially all the 117

PETROLEUM POSSIBILITIES The Madera Formation and the Cretaceous rocks are the principal rocks of hydrocarbon potential in the area. All the large areas surfaced by Madera are not likely to contain petroleum. owing to the relatively shallow depth to Precambrian crystalline basement. Cretaceous formations of potential are the Dakota, Mancos, and Mesaverde principally found in the Hagan and Tijeras basins. These are also the better places for finding the Madera at favorable depths. The most extensive Cretaceous terrane is the Hagan basin which forms an open broad arcuate syncline plunging to the northeast. Dips throughout the basin are from 20 to 30 degrees. No anticlines are present, but FIGURE 90—SEcTIoN I MINE IN TUERAS BASIN. ERoDED DUMP AND traps of sorts could be fashioned against faults or dikes PARTLY CAVED PORTAL TO INCLINE. in a few places. Perhaps the best possibilities are stratigraphic traps that might exist in some of the lenticular or intertonguing sandstone beds of the PLAcITAs FIELD Mesaverde and Mancos Formations. There is also some Three coal prospects occur in steeply dipping Mesa- possibility of fracture reservoirs in the Mancos Shale. verde beds on the San Antonito Las Huertas Grant The Tijeras anticline of the Tijeras graben has long 1 to 2 miles west of Placitas; all are caved. Judging from been a target for petroleum exploration. The north- the size of dumps, the easternmost prospectjust north of trending anticline is 2.5 to 3 miles long and I mile wide the road appears to have been the largest. The enclosing from the Cedar Crest syncline axis on the west to the beds dip N. 500 E. at 47 degrees. The middle prospect is Tijeras syncline axis on the east, It is a nearly upright near the creek about 200 ft east of a prominent basalt anticline with flank dips of 8 to 15 degrees on the west dike. The seam near the caved portal is I to 2 ft thick and 40 degrees on the east. The anticline is nearly level and dips N. 20° E. at 68 degrees. This prospect and the with possibly a plunge of 1 or 2 degrees northward. The one to the east appear to be on the same seam. The anticline is terminated against the Tijeras fault on the easternmost prospect is down the same arroyo 3,000 ft north and the Gutierrez fault on the south. Height of west of the dike. A drift adit appears to have been the fold is 500 to 700 ft. The anticline has been drilled a driven easterly on the N. 80° E. strike of the beds and number of times without finding oil or gas. The first test coal. The dip is 65 degrees to the north. The seam is was Wright #1 located in the SE¼ NW¼ sec. 12, T. 10 poorly exposed in the arroyo banks and appears to have N., R. 5 E. It was drilled with a rotary rig, possibly to been 1 to 2 ft thick. The State Mine Inspector report for the Dakota. A second well, the Hickerson-Wright #2, 1933 (p. 12) reports the Traddei mine with 4 men was drilled in 1947 a few tens of feet south of the first working the Placitas area, but its precise location is not well using cable tools. The location of the second well is given. immediately east of a north-trending basalt dike. Both

-WALL SECTION

flyer

0 20 40ff 14

FIGURE 91—PLAN AND LONGITUDINAL PANEL Of SEcTIoN 1 MINE. 1l8

A—FLYER UPOIP; SEAM IN PLACE ALONG INCLINE FLOOR, LOWER B—CONJUGATE FLYERS, UPOIP AND DOWNOIP FROM SEAM ALONG LEFT CORNER. FLOOR.

C—SMALL THRUST DOWNDIP. D—PROTRUSI0N WITH CONJUGATE FLARE.

FIGURE 92—CoAL PROTRUSIONS AND FLYER THRUSTS IN NORTH WALL OF SECTION I MINE. locations collar in Mancos Shale and are about 700 ft A small oil seep is reported along the creek just west east of the crest of the anticline. The penetrated Mancos of San Antonio (Katherine M. Wright, personal com probably dips east 5 to 10 degrees. The top of the munication). The location, now much obscured by Dakota was reached at a depth of 1,295 ft and the brambles, was near the base of the steeply overturned Morrison Formation at 1,360 ft. Dakota Sandstone. Despite low porosities reported for the sandstones in Winchester (1933, p. 120) found that some shale of previous tests, in 1964 Southern Union Gas Company the Madera yields oil on distillation, and Foster and drilled 3 wells on the southern end of the structure, others (1966, p. 8, 15) found that shale from the Sandia testing it as a possible gas storage reservoir for meeting Formation in the Manzano, Manzanita, and Ladron peak winter demands of Albuquerque. Southern Union Mountains and from Cretaceous shales such as the tested Dakota, Morrison, and Entrada sandstone with Mancos and Mesaverde Formations contained traces to out finding a suitable reservoir. These wells were a few gallons per ton. For the Sandia Mountains area drilled on a north line in the Mancos shale 900 ft east of the potential would appear to be only slight for the the west boundary of section 12. The southern well is Mancos or Mesaverde in the Hagan basin. Judging only about 600 ft from the Gutierrez fault; the northern from Foster’s results the Sandia shale appears to be well (No. 3) is 3,200 ft north of the southern well (No. more likely as a source. 1). The northern well is about 700 ft west of the anticline crest, and the southern well is 200 ft west. 119 References

Abert. J. W.. 1848. Report of LIeut. 3. W. Abert. of his examination New Mexico. of Mexico: Ans. Assoc. Petroleum Geologists in the years l846-’47: U.S. 30th Cong.. 1st sess.. Bull.. v. 44. p. 1749- Senate 1774. ex. doe. 23. 130 p. See Bailey. J. W.. for appendix. Reprint Bates. R. L.. 1942. The oil and gas ed.. 1962. with foreword by W. A. Keleher: Albuquerque. resources of New Mexico: New Horn Mexico Bureau Mines & Mineral and Wallace. 182 p. Resources Bull. 18 (2d ed). 320 Agogino. 0. A.. p 1962. comments following Mason. R. 3.. 1962: Current Anthropology. Bates. R. L.. and others. 1947. Geology v. 3. no. 3. p. 246-247. of the Gran Quivira Aldrich, quadrangle. New Mexico: New Mexico L. T.. Wetherill. G. W., and Davis. 0. L.. 1957. Occurrence Bureau Mines & Mineral of 1.350 million-year-old Resources Bull. 26. 52 p. granitic rocks in western United States: Berman. Geol. Soc. America Bull.. v. D. S.. 1973. A trimerorhachid amphibian from 68. p. 655-656. 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New & Mineral Resources Bull. 20. 27 Mexico: U.S. P. Geol. Survey Geol. Quad. Map GQ-886. Read, C. B.. and Henbest, L. G.. 1942, Pennsylvanian and Permian 1971, Geologi map of the Bosque Peak quadrangle. Tor stratigraphy of northern New Mexico (abs.): Am. Assoc. Petroleum rance, Valencia, and Bernalillo Counties. New Mexico: U.S. Geol. Geologists Bull., v. 26, 910. Survey Geol. P. Quad. Map GQ-948. Read. C. B., and Wood, G. H., Jr., 1947, Distribution and correlation 1972. Geologic map of the Capilla Peak quadrangle. Torrance of Pennsylvanian rocks in late Paleozoic sedimentary basins of and Valencia Counties. New Mexico: U.S. Geol. Survey Geol. northern New Mexico: Jour. Geology. v. 55, 220-236. Quad. Map GQ-l008. p. Read. C. B., and others. 1944. Geologic map and stratigraphic Naesser. C. W.. 1971. Geochronology of the Navajo-Hopi diatremes, sections of Permian and Pennsylvanian rocks of parts of San Four Corners area: Jour. Geophys. Research, v. 76, p. 4978-4985. Miguel. Santa Fe. Sandoval, Bernalillo, Torrance. and Valencia Needham. C E., 1937. Some New Mexico Fusulinidae: New Mexico Counties, north-central New Mexico: U.S. Geol. Survey Oil and Bureau Mines & Mineral Resources Bull. 14, 88 p. Gas mv. Prelim. Map 21 [l945J. 1940. Correlation of Pennsylvanian rocks of New Mexico: Read. C. B.. and others. 1950. Coal resources of New Mexico: U.S. Am. Assoc. Petroleum Geologists Bull.. v. 24. p. 173-179. Geol. Survey Circ. 89, 24 Needham, C. E., P. and Bates, R. L.. 1942. Pre-Cretaceous, in Bates, R. Reeside. J. B.. Jr.. 1927. The cephalopods of the Eagle Sandstone and L.. The oil and gas resources of New Mexico, 2d ed.: New Mexico related formations in the western interior of the United States: U.S. Bureau Mines & Mineral Resources Bull. 18, 117-121. P. Geol. Survey Prof. Paper 151. 87 p. 1943, Permian type sections in central New Mexico: Geol. Reiche. Parry. 1949, Geology of the Manzanita and North Manzano Soc. America Bull., v. 54, 1653-1667. p. Mountains, New Mexico: Geol. Soc. America Bull., v. 60, p. Newell. N. D., 1942. Late Paleozoic pelecypods, Mytilacea: Kansas 1183-1212. State Geol. Survey. v. 10. Pt. 2. 115 P. Reynolds. C. B.. 1954, Geology of the Hagan-La Madera area, New Mexico State Mine Inspector. Ann. Repts.. 1912-1921. Sandoval County, New Mexico: MS. thesis, Univ. New Mexico. 82 New Mexico State Inspector of Coal Mines. Ann. Repts.. 1922-1932. p. 123

Robinson. Peter. 1957. Age of Galisieo Formation. Santa Fe County. Talmage. S. B.. and Wootton. New Mexico: Am. Assoc. Petroleum T. P.. 1937. The non-metallic mineral Geologists Bull.. v. 41. p. 757. resources of New Mexico Romer. A. S.. 1945. Vertebrate and their economic features (exclusive of paleontology. 2d ed.: Univ. Chicago fuels): New Mexico Press. 687 Bureau Mines & Mineral Resources Bull. 12. p. 159 1966. Vertebrate paleontology. p. 3d ed.: Univ. Chicago Press. Tanner. W. F.. 1972. Large 468 p. gypsum mounds in the Todilto Forma tion. New Mexico: The Mountain Geologist. v. 9. Rothrock. H. E.. and others. 1946. Fluorspar resources p. 55-58. of New (974. Mesozoic lake history of northern New Mexico: New Mexico Bureau Mines & Mineral Resources Mexico: in New Bull. 21. Mexico Geol. Soc. Guidebook 25th Field Coni. 239 p. Ghost Ranch. central-northern New Mexico. 2 19-224. Sadlick. Walter. 1960. New name for Spirfer p. occidenralis (Girty) and Thompson. M. L.. 1942. Pennsylvanian itsgeologic history: Jour. Paleontology. System in New Mexico: New v.34. p. 1210-1214, Mexico Bureau Mines Mineral Sanford. A. R.. and others. & Resources Bull. 17. 92 1972. Seismicity of the Rio Grande rift in Thompson. T. p. New Mexico: B.. and Giles. D. 1.. l974. Orbicular rocks of the New Mexico Bureau Mines & Mineral Resources Sandia Mountains. Circ. New Mexico: Geol. Soc. America Bull., v. 85. 120. l9p. p.911-916. Sartenaer. Paul. 1970. Nouveaux genres rhynchonellides (brachio Tilton. G. R.. and Gruenenfelder. M. H., 1968. Sphene: podes) du paleozoique: Inst. Roy. Sd. Natur. Belgium Uranium- Bull.. v. 46. lead ages: Science. v. 159. p. 1458-1461. no. 32. 32 p. Toomey. D. F.. 1953. Paleontology and stratigraphy of Shimer. H. W.. and Shrock. R. R.. 1944. Index fossils the Carbon of North iferous rocks of the Placitas region. northern America: New York. John Wiley & Sons. 837 Sandia Mountains. p. Sandoval County. New Mexico: MS. thesis. Univ. Shomaker. J. W.. 1965. Geology of the southern portion New Mexico. of the Sandia 192 p. Granite. Sandia Mountains. Bernalillo County. New Mexico: MS. U.S. Coast and Geodetic Survey. thesis. Univ. New Mexico. 80 1948. Abstracts of earthquake p. reports for the Pacific Coast and the Western Simpson. J. H.. 1850. Journal of a military reconnaissance Mountain region: from Santa MSA-56. Oct.. Nov., D. 1947. 56 Fe. New Mexico. to the Navajo country p. made in 1849: U.S. 31st U.S. Coast and Geodetic Survey. Cong.. 1st sess.. Senate ex. doc. 1956. Abstracts of earthquake 64. p. 56-168. Reprint ed.. 1852, reports for the Pacific Philadelphia. Lippincott. Coast and the Western Mountain region: Grambo and Co.. 140 p.: reprint ed.. MSA-90. April. 1964. with annotations May. June l956. 19 p. by Frank McNitt. Univ. Oklahoma Press. U.S. Mine 296 Inspector for the Territory of New Mexico. Ann. Repts., p. 1899-1911. Smith, H. T. U.. 1938. Tertiary geology of the Abiquiu quadrangle. Waagë. K. M.. 1955. Dakota New Mexico: Jour. Geology. v.46. Group in northern Front Range p.301-3’9. foothills. Colorado: U.S. Geol. Survey Prof. Spiegel. Zane. and Baldwin. Brewster. 1963. Geology Paper 274-B. p. 15-51. and water Wasserburg. G. J.. and Steiger. R. resources of the Santa Fe area. New Mexico: H.. 1967, Systematics in the U.S. Geol. Survey Th-U-Pb systems and multiphase Water-Supply Paper 1525. 258 assemblages. in Radioactive p. dating and methods of low-level counting: Stark. J. T.. 1956. Geology of the South Manzano Internat. Atomic Energy Mountains. New Agency. Vienna. 33 1-347. Mexico: New Mexico Bureau Mines & Mineral Resources p. Bull. 34. Weber. R. H.. and Kottlowski, F. 49 p. E.. 1959, Gypsum resources of New Mexico: New Mexico Bureau Mines & Mineral Resources Stark. J. T.. and Dapples. E. C.. 1946. Geology of the Los Pinos Bull. 68. Mountains, 68 p. New Mexico: Geol. Soc. America Bull.. v. 57, Weimer. 1121-1172. p. R. J.. and Hoyt. J. H., 1964. 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Woodward. L. A.. 1970. Differentiation trends of spessarite dikes. Tippin & Streeper. 141 p.: reprint ed.. 1969. Albu Washington. Sandia Mountains. New Mexico: Jour. Geology. v. 78. p. 74 1-745. Calvin Horn. 141 querque. p. Workman. E. J.. and Kelley. V. C., 1940. A rock slide caused by l962. comments following Mason. R. J.. 1962: Witthoft. John. lightning: Am. Meteorol. Soc. Bull.. v. 21. p. 112-113. Anthropology. v. 3. no. 3. 267.270. Current P. Yale. F. R.. 1964. Petrography of a cyclical sequence. upper Madera H.. Jr.. and Norhrop. S. A.. 1946. Geology of the Wood. G. Limestone. Sandia Mountains, New Mexico: M.S. thesis. Univ. Mountains. San Pedro Mountain. and adjacent Nacimiento New Mexico. 81 in parts of Sandoval and Rio Arriba Counties, New p. plateaus Zidek. Jiri. 1975. Some lishes of the Wild Cow Formation (Pennsylva U.S. Geol, Survey Oil and Gas mv. Prelim. Map 57. Mexico: nian) in the Manzanita Mountains. New Mexico: New Mexico Betty. 1947. Trees of stone: New Mexico Mag.. v.25. no.4. p. Woods. Bureau Mines & Mineral Resources Circ. 135 (in press). 13-14. 51-52. 125

App e ndix 1—Stratigraphic Sections

MADERA FORMATION Thickness Unit Montezuma Ridge, Las Fluertas and Tejon grants Description (ft) (Mod(/ledfrom Harrison, 1949) 5 Limestone: gray. medium-grained. crystalline, medium- bedded, nodular; highly fossiliferous zones 3) 4 Sandstone: greenish-gray; medium- to coarse-grained. Thickness slightly Unit conglomeratic. thin- to medium-bedded, rath Description (ft) er friable, angular to subangular grains 9 Abo Formation above 3 Limestone: gray, crystalline, fine- to coarse-grained. medium- Madera Lime3(one (total thickness) 1.267 to thick-bedded, fossiliferous 130 31 Limestone: gray. fossiliferous 2 Limestone: dark-gray, fine-grained. crystalline, with ir 30 Limestone: gray-green, extremely fossiliferous, thin- regular brown cherty deposits on weathered surfaces. bedded, with shaly partings, nodular 15 medium- to thick-bedded, fossiliferous, cliff-forming 215 29 Limestone: gray crystalline, fine-grained. thin-bedded, I Limestone: gray-buff. crystalline, medium- to thick-bed fossiliferous IS ded. very fossiliferous; weathers to very rough, irreg ular surface; 28 Shale: gray 8 slope partly covered 63 27 Sandstone: buff, medium-grained. thin- to medium-bed Sandia Formation ded. hard, quartz and feldspar grains 15 26 Limestone conglomerate: gray 25 Shale: red, slope covered 14 24 Shale: blue-gray, with limestone nodules 4 23 Limestone: gray, dense to fine-grained. crystalline, thin- to massive-bedded, with silty shale partings, fossil ABO FORMATION iferous, weathers to olive-drab, buff-brown surface; Projected S½ sec. 23, T. 13 N., R. 5 forms front E. slope and ridge 122 (Modifiedfrom Harrison, 1949) 22 Sandstone: grayish-pink, medium to coarse, angular to subrounded grains, thin- to thick-bedded, with shale partings locally, cross-bedded locally; grades upward Thickness Unit to maroon-lavender near the top; color and texture Description (ft) vary laterally and vertically; slope-forming 28 Aba Formation (total thickness) 21 Sandstone: grayish-pink, fine-grained, 891 thin, shaly-bed 45 Sandstone: red-lavender, fine- ded, micaceous, slope-forming to coarse-grained, suban 14 gular to subrounded, 20 Sandstone: greenish-maroon, thin- to thick-bedded, with shaly arkosic, medium- to partings; also thin, gray coarse-grained, thin- limestone bands; extreme to medium-bedded, with soft, cross-bedding present silty, conglomeratic 103 partings; angular to subangular 44 Shale: red, sandy grains 4 5 43 Sandstone: white to pink, medium-grained, 19 Limestone conglomerate: red-lavender; angular to with quartz, subrounded; thin-bedded, cross-bedding limestone, feldspar, and present 7 chert fragments; with thin. 42 Shale: red-lavender, sandy red shaly streaks 12 2 41 Sandstone: pinkish-red, 18 Siltstone: gray-green medium- to coarse-grained, micaceous and shaly; grades up angular to subrounded ward into mineral grains; medium- to top 6 ft of gray-maroon, mottled, micaceous thick-bedded, siltstone cross-bedding and shale partings are IS present; grades into gray sandstone at 17 Sandstone: red-gray, silty the top 14 and shaly; 4 inches of red 40 Sandstone: red, shaly, shale at bottom fine-grained, thin-bedded; 4-inch 2 gray to white sandstone 16 Claystone: red, at base, angular to subangu with earthy limestone nodules 29 lar, medium-grained. IS Shale: gray thin-bedded, slightly calcareous I 6 39 Shale: red, silty to sandy 14 Limestone: green, crystalline, 23 fine-grained, brittle, with 38 Sandstone: gray-buff, medium-grained, silty, shaly partings thin-bedded, and some earthy limestone nod with shaly ules bands, and slightly conglomeratic shale 8 partings with a red and gray mottled 13 Shale: gray-green, friable color 12 9 37 Shale: red, silty 12 Limestone: gray. crystalline, fossiliferous 68 6 36 Sandstone: dark-red, very fine grained. micaceous, thin, II Limestone: gray, crystalline, with earthy limestone shaly bedded, thin white calcareous at top nodules, fossiliferous, thin-bedded 13 39 35 Shale: dark red-brown, silty (covered) 10 Limestone: blue-gray, dense, 68 thin- to medium-bedded, 34 Siltstone: light-red. calcareous. cherty along seams, nodular; lateral variation in pods and lenses, slightly in thickness fossiliferous; 2 weathers to a brownish-colored surface; 33 Sandstone: probable red-brown, very fine grained, shaly, mica base of Arkosic member 126 ceous 9 Limestone: gray, crystalline. tine-grained, medium- to 32 Sandstone: gray-lavender, very fine grained to silty. thin. thick-bedded, cherty along seams and in nodules. shaly bedded, extremely cross-bedded with fossiliferous; weathers to lenses of rough, irregular surface; green-gray. oolitic limestone conglomerate; forms crest of ridge lincstone, 131 feldspar, and hematite 8 Sandstone: greenish, grains, very hard, very irregu buff-gray, medium to coarse, larly bedded; subangular. grades laterally into calcareous nodular to subrounded grains, scattered mica siltstone flakes, thin- to medium-bedded, 6 rather friable, orange 31 Sandstone: brick-red, very timonitic specks fine grained to silty, thin to 5 shaly bedded, with bands of red shale; interbedded 7 Limestone: light buff-gray to gray. crystalline, thin- to thin, gray, micaceous sandstone lenses thick-bedded, with highly 46 fossiliferous zones, scat 30 Shale: dark-gray. with 2 ft of black tered chert nodules shale in the middle; and pods; weathers to a rough, locally, highly stained spiny surface by malachite and some azurite 16 194 29 Sandstone: brown, fine-grained, thin- to medium-bed 6 Limestone: gray. conglomeratic, quartz. feldspar, and ded, cross-bedding present; limestone fragments; conglomeratic band near arkosic appearance on top with limestone. quartz, weathered surface and feldspar granules 8 5 28 Shale: red. with sandy streaks 11 ______

126

Thickness Thickness Description (ft) Unit Description (ft) Unit glomerate wiih rounded red shale and siltstone peb 27 Sandstone: brown-huff. fine-grained. medium-bedded. bles and granules. ibm-bedded 4 with shale partingscross-bedding present. grades into I Sandstone: light reddish-purple to brown, medium brown siltstone near top. with I ft bed of green grained. thin- to medium-bedded 25 nodular limestone 12 36 San Andres Formation 26 Shale: red 25 Sandstone: dark red-brown, very fine grained. silty. 19 micaceous: thin-bedded with dark-red shale partings 24 Sandstone: buff to maroon, fine- to medium-grained. subangular to subrounded. medium-bedded, becomes silty at the top 35 61 CHINLE FORMATION 23 Shale: red 22 Sandstone: buff. medium-grained. subangular to sub- Sec. 13, 14,T. 13N.,R.5E. rounded with quartz. feldspar, and a few dark mineral grains: weathers brown 3 Thickness gray, medium- to coarse-grained. medium- (ft) 21 Sandstone: Unit Description bedded, cross-bedding present: conglomeratic. with quartz. feldspar, and abundant angular to rounded Entrada Sandstone above limestone granules: weathers to dark brown with a Chinle Formation (total thickness) 1.861 sandpaper texture 29 Shale: red-brown, with 6-inch gray sandy streak in 20 Shale: red middle 15 to coarse 19 Sandstone: light-buff. medium-grained 28 Sandstone: brown. medium-grained. subangular to grained, subangular to subrounded, medium-bedded; subrounded, thin- to thick-bedded, cross-bedding 13 quartz. feldspathic grains; arkosic locally; hard present, with thin bed of light purple shale; thin 27 18 Shale: light-red conglomeratic lenses of limestone, fine-grained sand 17 Sandstone: light-buff to light-brown, medium-grained. stone with red shale pebbles. angular to well-rounded 54 subangular to subrounded, medium- to thick-bedded; 27 Shale: red, with thin, red sandy streaks 346 quartz. feldspaihic grains 26 Sandstone: red, fine-grained. shaly, cross-bedded 9 16 Shale: red 25 Shale: red 18 fine-grained. 15 Sandstone: maroon-brown, thin-bedded, 24 Sandstone: red, fine-grained. shaly. thin- to thick-bed- 6 micaceous, shaly ded. cross-bedding present 17 61 14 Shale: red, with few sandy streaks 23 Shale: red, with 6- to 12-inch beds of fine-grained gray subangular to 13 Sandstone: buff to pink, medium-grained, sandstone 65 some subrounded, thin- to medium-bedded, with greenish-gray, earthy, nodular, gypsiferous, 31 22 Limestone: feldspar grains conglomeratic with well-rounded claystone pebbles 2 32 12 Shale: red and green. partly covered red, partly covered 55 2 21 Shale: 11 Limestone: light-gray, slightly nodular Sandstone: red. fine-grained, thin- to medium-bedded, 6 20 10 Shale: brown with shale partings and thin, gray sandy streaks: 2 9 Limestone: red-lavender, earthy, nodular cross-bedding present 24 5 8 Shale: red Shale: red, sandy, with I- to 2-inch streaks of con- 2 19 7 Limestone: maroon-brown, nodular glomeratic, nodular limestone 23 6 Shale: light-red Sandstone: red, fine-grained. thin-bedded. shaly; 8 18 5 Shale: gray-maroon 10-inch greenish-gray, earthy, nodular, conglomeratic 10 4 Shale: red limestone near bottom; thin, gray sandy streaks 3 quartz. 3 Limestone: gray. conglomeratic. with limestone, 17 Clay: red 40 may be and feldspar fragments; some fragments 16 Sandstone: red, fine-grained, thin- to medium-bedded, reworked fossils shaly, with thin calcareous seams; small amounts of 2 Shale: red barite deposited along seams and fractures 153 I Shale: green-gray IS Clay: light red with streaks of gray, gypsiferous along Madera Formation seams 59 14 Sandstone: red, fine-grained. shaly, thin-bedded 86 13 Clay: light-red with 2- to 4-inch gray nodular limestone bands 65 12 Sandstone: red, fine-grained, shaly with 4-inch to 6-inch beds of gray. medium-grained. calcareous-cemented SANTA ROSA SANDSTONE sandstone 21 Center projected sec. 36, T. 13 N., R. 5 E. II Clay: light-red, with thin, light-gray nodular limestone streaks 202 Limestone: gray-brown. conglomeratic Thickness 10 9 Clay: variegated 41 (ft) Unit Description 8 Conglomerate: gray-brown. with well-rounded lime stone and red claystone pebbles 2 Chinle Formation above 7 Clay: variegated 106 Santa Rosa Sandstone (total thickness) 333 6 Sandstone: gray. fine-grained. thin-bedded 6 Sandstone: white to gray buff, medium-grained, thin- to 5 Clay: light-gray 6 medium-bedded. micaceous and fine-grained at top; 4 Sandstone: gray, medium-grained, thin-bedded, lime siliceous (partly covered) 284 stone and quartz grains 2 5 Sandstone: buff, pebble conglomeratic. with subangular 3 Clay: light-gray 8 to well-rounded quartz and chalcedony pebbles; 2 Sandstone: gray-brown, medium-grained, subangular to 6-inch beds of medium-grained, well-sorted gray subrounded. thin-bedded. cross-bedding present; sandstone 3 lower part is brown, pebble conglomeratic with gray gray to yellow-buff. medium-grained. thin- 4 Sandstone: limestone, gray siltstone bands 5 to medium-bedded, some cross-bedding 6 I Clay: variegated, highly gypsiferous in seams, with thin. red-brown, fine-grained. shaly- to medium- 3 Sandstone: earthy, brown, nodular limestone bands 432 hard, slightly argillaceous II bedded, Santa Rosa Sandstone 2 Sandstone: reddish-brown, granulitic to pebbly con- 27

MORRISON FORMATION Thickness Sec. 36, T. II N., R. Unit 5 E. Description (ft) 3 Mudstone: purplish-brown and gray with occasional Thickness thin white sandstone Unit Description beds 59 (ft) 2 Sandstone: white, thin to thick, friable. medium-grained Dakota I Mostly covered 27 Sandstone above by caliche: float and small elposures Morrison Formation indicate purplish-brown (total thickness) 392 mudstone and gray claystone I I Sandstone: with a few thin thick-bedded, light-gray to white, medium friable white sandstone layers 81 Todi/to Formation grained. friable, considerable kaolinization of grains 10 68 Sandstone: massive, light-gray to light-green, medium grained. some kaolinization 60 9 Shale: mottled, reddish-brown and green 9 8 Sandstone: medium- to thick-bedded, light-gray, fine- to medium-grained. well-indurated 18 7 Sandstone: MANCOS medium-bedded, light-gray. fine-grained, ar SHALE gillaceous Sec.31,T. 12 N., R.6E. 6 6 Mudstone: mottled gray. green. and purple. slightly (Modtfiedfrom arenaceous, calcareous Harrison, 1949) 28 5 Claystone: gray. calcareous 8 4 Mudstone: reddish-brown and green. calcareous in upper part Thickness 42 Unit Description 3 Mudstone: green and purple (ft) 82 Mesa verde 2 Mudstone: gray-green, calcareous Formation above 12 Mancos Shale I Mudstone: variegated reddish-brown, (total thickness) 1,544 light-gray, and IS Shale: green gray to olive drab with thin silty and sandy layers 309 59 17 Sandstone: buff Todilto gypsum to olive drab. tlne-grained. thin- to medium-bedded with calcareous zones and cone-in- cone concretions: thin shaly partings: fossiliferous zones, local crossbedding 16 203 MORRISON Shale: olive-drab to buff-gray, silty to sandy gradations. FORMATION sand content increases toward top; sandy beds, cal SW cor. sec. 31, T. 13 N., careous R. 6 E. on Gonzales Creek concretionary beds or zones, fossiliferous zones; weathers to buff-cream color and is generally slope-forming 487 Thickness 15 Sandstone: light buff-gray. Unit Description fine-grained, thin- to (ft) medium-bedded, hard, siliceous cement, ledge-form Dakota Sandstone ing above 18 Morrison Formation 14 Shale: (total thickness) 622 buff-gray, silty, weathers to cream-buff color. 27 Sandstone: valley-forming white, medium- to thick-bedded, friable, 172 13 Limestone: medium- and coarse-grained. locally pebbly. locally brown, crystalline, silty to sandy, thin-bed cross-bedded, ded. with white, angular pumiceous and chert thin shale partings, highly fossiliferous 8 fragments 12 Shale: in upper 5 ft. Overlain disconformably by gray-buff, silty, with 1.3 ft gray concretionary 17 ft of yellowish-brown, thin- to medium-bedded calcareous bed near middle, and 1.5 ft yellow-brown Dakota calcareous Sandstone bed with few fossils near bottom 70 26 Claystone: II Shale: gray gray 58 25 Sandstone: 10 Limestone: brown, concretionary, white, medium-bedded, medium-grained 11 sandy, highly fossil 24 Claystone: iferous. many greenish-gray, floating sand grains in some fossils in concretions. ridge-forming 6 beds 9 Shale: gray 27 32 23 Sandstone: 8 Sandstone: gray-buff. white, thin-bedded, medium-grained 10 fine-grained. thin-bedded. suban 22 Claystone: gular to subrounded, like unit 24 63 hard, siliceous cement; ridge- 21 Sandstone: forming white, medium-bedded, weathers rusty yel 3 lowish-brown 7 Sandstone: buff, fine-grained. silty; friable 2 20 Claystone: 6 Shale: buff to greenish-gray. with local thin sandstone beds 15 gray. sandy 2 19 Sandstone: 5 Shale: gray white, thin-bedded, medium-grained II 12 1 Claystone: 4 Sandstone: greenish-gray, with several 6-inch lenses of light gray-buff. fine-grained. thin- to medium-bedded, rusty sandstone subangular to subrounded: hard, 17 Sandstone: 19 siliceous grayish-green, medium-grained. weathered cement, ridge-forming 25 brown 3 Shale: gray. with thin sandy streaks 34 16 Claystone: 2 Limestone: greenish-gray with variable floating sand gray. concretionary. silty. cone-in-cone grains structure, forms 59 pods 2 15 Sandstone: white, I Shale: dark-gray, thin-bedded. medium-grained 18 with thin scattered sandy and cal- 14 Mudstone and careous claystone: greenish-gray streaks 101 13 Sandstone: 27 greenish-white, medium-bedded, medium Dakota(?) Sandstone grained 12 6 Mudstone: purple and greenish-gray, mostly covered II 22 Sandstone: greenish-white. medium to thick-ledged. medium-grained II JO Mudstone: light-gray MESAVERDE FORMATION 9 Sandstone: 12 greenish-gray, medium-ledged. medium N ½ sec. 6, T. grained 13 N., R. 6 F. II (Modtfiedfrom 8 Mudstone: gray Harrison, 1949) and purplish-brown, green in upper 3 ft 24 7 Sandstone: white, medium-ledged, medium-grained 12 6 Mudstone: purplish-brown 9 Thickness 5 Sandstone: white, Unit medium-bedded, medium-grained 10 Description (ft) 4 Sandstone: largely covered, white, friable, medium grained Galisteo Formation above 16 Mesa verde Formation (total thickness) 3,057 128

Thickness Thickness (It) (ft) Unit Description Unit Description Sandstone: gray. fine-grained. thin-bedded with local SHALE MEMBER NO. 3 (sub 25 COAL-BEARING calcareous concretions. top of ridge 4 total): (590) 24 Sandstone: yellow-buff. fine-grained. thin- to medium 64 Sandstone: gray. fine-grained. medium-bedded. limon 19 8 bedded. gypsiferous along seams at bottom ite-stained 2 (sub I COAL-BEARING SHALE MEMBER NO. 63 Shale: gray (521) shale total): 62 Sandstone: gray. fine-grained. with thin brown 3 23 Shale: gray. sandy seams. calcareous concretionary seams in 3 zones: cone-in-cone concretions present. gypsum 61 Shale: brown 103 to sub- seamsat top 60 Sandstone: gray. tlne-grained. subangular 418 white 22 Shale: gray. with sandy seams rounded, thin- to medium-bedded, black and (248) 14 SANDSTONE MEMBER NO. 3 (subtotal): mineral grains abundant 21 Sandstone: gray. line-grained. thin-bedded, with sandy silty to sandy 12 59 Shale: gray, shale bed in middle 7 gray. fine-grained. massive-bedded 30 2 58 Sandstone: 20 Shale: yellow-buff, sandy brown-gray 29 57 Shale: 19 Sandstone: gray. flne-grained. thick-bedded. subangular drab. limonitic concretionary zone, 8 56 Shale: brown-olive to subrounded, cross-bedding present; fossils locally. shale at top 23 inches of carbonaceous ripple-marks, worm-burrows, and fossil casts on ex fine-grained. massive-bedded, argil 55 Sandstone: gray. posed top of sandstone bed 9 limonitic concretions; about 3 ft of thin, laceous, with Sandstone: yellow-buff. fine-grained. thin-bedded, in the middle 27 18 cross-bedded sandstone shaly; fossil zones, slope-forming 79 zones and a thin carbonaceous shale 54 Shale: gray, sandy 17 Sandstone: gray. fine-grained. thin-bedded, very fossil near bottom 25 3 argil iferous 53 Sandstone: gray-buff. fine-grained. thin-bedded, and shaly 80 5 16 Sandstone: gray, fine-grained, thin-bedded, laceous thin-bedded, 8-inch cal some 15 Sandstone: gray. tine-grained. 52 Sandstone: gray. fine-grained. massive-bedded, zone in middle 9 27 careous cone-in-cone concretionary cross-bedding present thin-bedded, shaly con 14 Sandstone: yellow-buff, fine-grained. 51 Sandstone: gray. fine.grained, shaly, with limonitic seams along bedding 4 and slope-forming: selenite cretions planes 29 to brown with 4-inch coal seam near top and 50 Shale: gray 13 Sandstone: gray. gray-buff and brown, fine-grained. near middle II a 3-ft coal seam thin-bedded, with shale partings and shaly zones, also yellow-buff to gray, fine-grained, subangular 49 Sandstone: thin. calcareous concretionary zones, fossiliferous thick- to massive-bedded, some to subrounded, beds present 30 cross-bedding is present; brown limonitic concretion SHALE MEMBER (subtotal): (67) ary beds with evidence of organic material 41 67 3 12 Shale: yellow-buff, sandy 48 Shale: brown, 2 ft coal seam (589) 6 SANDSTONE MEMBER NO. 2 (subtotal): 47 Shale: gray 32 5 II Sandstone: gray-buff, fine-grained, shaly. fossiliferous Sandstone: gray, fine-grained, massive-bedded 46 10 Sandstone: yellow-buff, fine-grained, thin-bedded, to brown, one-ft coal seam near bottom, a 45 Shale: gray shaly, few fossils and worm burrows (7) 270 coal seam just above the middle, and a 1.5-ft 1.3-ft 9 Sandstone: gray-buff, fine-grained. thin-bedded. shaly: at top; carbonaceous shale and sandy shale coal seam bottom I-ft coarse-grained to conglomeratic locally. the seams 43 separate fossiliferous (shark teeth) 262 Sandstone: gray, fine-grained. thin-bedded, limonite shaly 44 7 8 Sandstone: gray-buff. fine-grained. thin-bedded. stained with sandy shale partings 25 I-ft coal seam near 43 Shale: gray to brown, carbonaceous, COAL-BEARING SHALE MEMBER NO. I (sub middle and 1.8-ft seam near the bottom; slope-form (661) 15 total): ing 7 Shale: buff-gray, with sandy seams 108 shaly at top, slope-form 83 42 Sandstone: gray, fine-grained. 6 Shale: buff, sandy 2 168 ing 5 Shale: gray. silty slope-forming 6 41 Shale: gray and brown, thin sandy zone, 4 Shale: gray, brown to black, with carbonaceous shale with thin Sandstone: gray. fine-grained, thin-bedded, coaly shale beds; also sandy seams and cal 40 6 and brown shale and calcareous concretion beds zones 56 6 careous Shale: brown, thin gray sandy streaks SANDSTONE MEMBER (subtotal): (246) 39 4 CANO Sandstone: gray. fine-grained, thin-bedded, argillaceous gray-buff, fine- to medium-grained, thin- to 38 8 3 Sandstone: Shale: brown, 8-inch coal seam near bottom subangular to subrounded; with thin 37 3 massive-bedded, Sandstone: gray. fine-grained. thin-bedded partings and calcareous lenses: cross-bedding is 36 13 shale 35 Shale: brown to gray. carbonaceous present in some beds 246 thin-bedded, with 34 Sandstone: gray-buff, fine-grained, Mancos Shale green, and shaly and calcareous zones: black, orange. 18 in 21 (Units 1 and 2 of Harrison are nos. 17 and white mineral grains are common 14 the Mancos section above.) and Siltstone: gray-buff 33 Shale 7 32 Shale: brown. I-ft coal seam near middle middle, Shale: gray to brown. 2.5 ft coal seam near 31 24 sandy near top VERDE FORMATION sandy 30 MESA 30 Shale: gray to brown, bottom half is more measured with buff-yellow. gray-buff. and gray. A general section in the Tijeras basin 29 Sandstone: gray-white, T. 11 N., R. 6 E. fine-grained. thin- to massive-bedded; shale partings. students in the E½ sec. 31, are limonite stains, black and white mineral grains and rather abundant, with minor amounts of orange Thickness friable to green mineral grains in some horizons; (ft) 72 Description well-mdu rated Unit seams 22 28 Shale: gray with rust-colored sand Mesa verde Formation (135) (387) SANDSTONE MEMBER NO. 4 (subtotal): UPPER SANDSTONE (subtotal): forms small ridge 6 27 Sandstone: buff. fine-grained. 24 Sandstone: buff to gray. medium- to thick-bedded. shale, sandy string 84 26 Shale: gray to brown, carbonaceous medium- to coarse-grained. local cross-bedding is highly ers, and calcareous zones; top 8 inches Siltstone: mostly covered 69 106 23 Shale and fossiliferous 129

‘Thickness Unit Thickness Description (ft) Unit Description (ft) 22 Sandstone: buff, medium- to thick-bedded, medium grained. 59 Sandstone: yellowish-buff, fine- to coarse-grained. welt-cemented 29 21 Shale: medium- to massive-bedded, local conglomeracic monly covered, some intercalated sandstone and siltstone beds, and shale partings 175 82 58 Sandstone: buff, 20 Sandstone: gray to buff, thin- fine- to coarse-grained. 4-ft con to medium-bedded, local glomeratic cross-bedding. friable, local bed near bottom, fragments of petrified carbonaceous layers 12 wood 19 Covered: 141 21 57 Sandstone: gray. 18 Sandstone: gray. thin- to medium-bedded, fine-grained. thick- to massive-bedded. with inter friable, calated shale and siltstone limonitic stains 59 66 56 Sandstone: I? Covered: mostly shale yellowish-buff. medium-grained. local peb 24 bles (Top Eroded) 6 55 Conglomerate: MIDDLE SANDSTONE (subtotal): buff, fine to coarse, angular to subround (224) ed matrix; fragments 16 Sandstone: dark-gray. medium- to thick-bedded, are chert, quartz, limestone, siliceous and feldspar 30 2 IS Sandstone: 54 Sandstone: gray, buff, yellowish, dark-gray, massive-bedded, cross and len and tan, fine- to ticular bedding, coarse-grained, thin- to medium-bedded, firm siliceous cement, cliff-forming 30 subangular 14 Sandstone: to subrounded, grains of quartz. light-gray, medium- to thick-bedded, me chert. feldspar; some dium- intercalated thin, variegated to coarse-grained, feldsparhic and micaceous, shale and local granule local cross-bedding, lenses, friable friable. calcareous 57 316 53 Claystone: brick-red with silty streaks 13 Sandstone: buff to light-brown, thin- to medium-bed 20 52 Sandstone: tan to light-red, fine-grained. ded, fine- to medium-grained, argillaceous with some massive 13 interbedded SHALE UNIT silistone and shale 107 (subtotal): (212) LOWER SI Claystone: SANDSTONE (subtotal): (528) variegated, with sandy streaks 212 12 Covered: mostly shale and siltstone 165 UPPER CLAYSTONE UNIT (subtotal): II Sandstone: buff to (336) tan, thick-bedded with some 50 Sandstone: fine- to medium-grained, massive cross-bedding, medium-grained 34 14 49 Conglomerate: buff, fine to coarse matrix, 10 Sandstone: gray subrounded to buff, thin-bedded, fine- to medium to rounded granules and pebbles, grained limonite-stained, 19 indurated 9 Sandstone: 2 gray to buff, medium-bedded, fine- to 48 Sandstone: gray, massive, fine-grained, medium-grained silty 8 24 47 Claystone: grayish maroon 8 Covered 2 16 46 Claystone: bright-brick-red 7 Sandstone: 10 light-gray, thin- to medium-grained 22 45 Sandstone: gray, fine-grained, 6 Covered shaly 7 6 44 Shale: bright-reddish-brown 5 Sandstone: light-gray, 18 thin- to medium-bedded, 43 Sandstone: cross-bedded, yellowish-gray, medium-grained, fine- to coarse friable 10 grained, angular to subrounded 4 Sandstone: pebble conglomerate buff, massive and laminated 18 at bottom 3 Sandstone: 41 gray, thin-bedded, friable 12 42 Shale: brick-red 2 Sandstone: 9 buff to tan, thick- to massive-bedded 41 Sandstone: light-tannish-red, I 12 thin-bedded. fine-grained. Sandstone and Shale: mostly covered, largely medium- shaly to thick-bedded 9 sandstone in upper two-thirds and 40 Sandstone: gray-buff, cross-bedded, thin-bedded fine- to medium sandstone and intercalated shale in the grained, shaly. friable, locally conglomeratic IS lower one-third; top eroded 39 Shale: light-red 210 6 38 Conglomeratic sandstone: coarse-grained, angular to subrounded, pebbles and cobbles of chert, quartz. limestone, and sandstone, limonite-stained 3 37 Sandstone: yellowish-buff, fine- to medium-grained, medium-bedded, GALISTEO FORMATION conglomeratic toward top 21 36 Conglomeratic sandstone: cross-bedded, Along Pinovetito Arroyo, sec. 4, 5, T. 13 N., brownish or R. 6 E. ange, fine- to coarse-grained, subangular to subround ed, granules to cobbles of chert, quartz, limestone, and pinkish Thickness granite 14 Unit 35 Shale: purplish-red Description (ft) 2 34 Sandstone: gray, massive, fine-grained, Espinaso Volcanics pebble con above glomeratic lenses in bottom ft Galisgeo Formation 6 23 (total thickness) 2.474 33 Shale: tan- and purplish-red, with UPPER SANDSTONE silty and sandy gray UNIT (subtotal): (1,116) streaks 71 Sandstone: light-buff, 112 medium-grained, thin- to MIDDLE medium-bedded, SANDSTONE UNIT (subtotal): (290) argillaceous and thin granule lens 32 Sandstone: near top gray. thin-bedded, fine-grained, silty 7 107 31 Shale: brick-red 70 Limestone: white, 8 dense, with clay streaks 30 Sandstone: 69 Shale: gray gray. thin-bedded, fine-grained, silty II 4 29 Sandstone: 68 Sandstone: gray. buff, medium-bedded, grains angular to fine-grained, shaly 9 subangular, 67 Sandstone: buff, feldspathic, locally conglomeratic 6 fine- to medium-grained 7 28 Sandstone: 66 Shale: gray yellowish-gray, medium-bedded, fine 16 grained, silty 65 Sandstone: gray-butT, 16 fine-grained, thin- to medium- 27 Claystone: bedded brick-red 9 9 26 Sandstone: 64 Sandstone gray-buff, gray, fine-grained, silty, friable 4 fine- to coarse-grained, medium- 25 Sandstone: bedded, conglomerate yellowish-buff, medium- to coarse-grained. lens in upper one-third 67 pebbles 63 Shale: red with yellowish of quartz. limestone, and minor feldspar 6 calcareous concretionary band 24 Claystone: near the top light-brick-red 4 8 23 Sandstone: 62 Sandstone: gray. flne-grained, gray. fine-grained, friable with indurated medium-bedded 23 streaks 61 Shale: variegated, with thin 9 gray. fine-grained sandstone 22 Clay: near bottom reddish I) 41 21 Sandstone: gray, 60 Sandstone: gray, pinkish, buff, medium-bedded, fine-grained. bottom massive, fine- to coarse 1 ft coarse-grained grained. angular to subrounded and granulitic 10 92 20 Shale: light-brick-red, sandy 19 130

Thickness Thickness (it) (it) Unit Description Unit Description gray, orange. thin- to medium-bedded. granulitic 9 Sandstone: 19 Sandstone: gray. thick-bedded. fine-grained. limonite stains, ridge-former 64 13 fine-grained. shaly. at base sandy streaks, thin calcareous 14 8 Claystone: gray. silty and 18 Shale: variegated bed near bottom 37 thick-bedded. 17 Sandstone: yellowish-gray, thin- to buff, thin- to medium-bedded. scat 7 Sandstone: gray, fine-grained. 2-ft claystone in lower one-third, with shaly seams 36 143 Imne-grained. friable tered granule and pebble lenses, friable streaks. gypsiferous 16 (359) 6 Shale: yellowish-gray, sandy LOWER CLAYSTONE UNIT (subtotal): (subtotal): (161) 6 LOWER SANDSTONE UNIT 16 Shale: gray. sandy. friable thin- to thick-bedded, fine granuli 5 Sandstone: variegated, IS Sandstone: gray. medium-bedded. fine-grained. 20 17 grained. limonite stains tic to pebbly. petrified wood, limestone seams fine-grained. 5 4 Sandstone: gray. thin- to medium-bedded. 14 Shale: yellowish-gray, sandy limonite stains 8 fine silty and shaly layers. 13 Sandstone: gray-buff. thin- o thick-bedded, 30 pebble conglom 3 Siltstone: gray grained. subangular to subrounded; red. valley-forming 25 shale 2 Claystone: gray. brown, erate 8 inches thick overlain by 5-ft sandy gray cross-bedded. 110 I Sandstone: thin- to massive-bedded, in lower middle part scattered granule seams, 22 line-grained. argillaceous. 12 Shale: gray, sandy gravel and pebble conglomerate at bottom. shaly to medium-bedded, fine-grained, I I Sandstone: gray, thin- toward top with occasional thin calcareous lenses, argillaceous with thin calcareous nodular concretion 78 33 limonite prevalent ary zone shaly 13 Mesa verde Formation 10 Sandstone: gray, medium-bedded. fine-grained. l3l

Appendix 2—Earthquakes

EARTHQUAKE OF NOVEMBER 6, 1947, 09:50 MST The following summary of responses to a question Placitas. which is 12 miles N-NW of Sandia Park. The shock was naire-card survey of the earthquake of November 6, probably not felt at Edgewood or Madrid. This earthquake occurred 1947, 09:50 MST was published by the U.S. Coast and in the vicinity of the Tijeras Coal Basin. a graben-like block on the Geodetic Survey (1948) eastern dip slope of the Sandia Mountains fault block. San Antonito in Abstracts of earthquake and Sandia Park reports for the Pacfic are on the north side of the major fault bounding the Coast and the Western Mountain Coal Basin on the north. Cedar Crest Region, is just south of this same fault. p. 12-13. The C. A. Dooley ranch is located either directly on, or within 100 feet of. the major (Albuquerque fault bounding the Coal Basin along the southeast Press) Slight tremors believed an earthquake were side.” reported felt Thursday morning at San Antonito, about 24 miles east Intensity VI: of here in the Sandias. Bill Marcum, school teacher there, said the Zamora (C. A. Dooley Ranch). Motion shock shook his classroom, jarred the floors rapid, lasted 10 or 15 and rattled the desks. He seconds. Felt by all in home and gave the time as 9:50 am. and community: frightened all in home. estimated it lasted 15 seconds. A Rattled windows, doors, housewife in the community dishes. Cracked plaster and fireplace. Dam said dishes were jarred from shelves in age slight to fireplace her house. Marcum and south wall of house. related. Marcum, who said he had experienced a Intensity V: “quake” before, said he drove around the neighborhood later and in Cedar Crest. talks with IS persons Motion rapid, lasted I second. Felt by all and representing residents in a 10-mile radius frightened few learned they in home. Rattled windows. Ground: Soil, compact; had felt the shock. Dr. S. A. Northrop. seismologist here, level. said he had no report of a quake but promised to check his Cedar Crest. 4’/, miles instruments today. These, N of (Crane’s Store). (IV) Motion rapid. he said, were at the time running vibration Felt by all in home. tests on truck rumblings Rattled dishes. Ground: Soil, compact: sloping. on East Central. San Antonito. The following Motion rapid. lasted 5 seconds. Felt by many in is quoted from a letter from Professor Stuart A. community: Northrop, frightened few. Rattled windows, doors. Ground: Rock: Collaborator in Seismology. U.S. Coast and Geodetic sloping. Survey. University of New Mexico. Albuquerque: “This is the first Sandia Park. Motion rapid, lasted a record of a shock in the Sandia Mountain fraction of second. Felt by Region. However, it may all in community. Rattled windows, be noted that San Antonito is only doors, dishes. Shifted small 23 miles SW of Cerrillos, where objects. Ground: Rock: level. there was a severe shock (Rossi-Forel VIll-IX) in 1918. San Antonito Sandia Park and vicinity. is I mile east of Sandia Motion rapid, up and down, lasted ‘h Park, and 18 miles N-NE of Albuquerque. second. Felt by Cedar Crest several in home. Rattled windows, doors, dishes. and Zamora are located about 4 miles south of San Everything Antonito moved up and down. Ground: Rock, compact: sloping. and Sandia Park. We have no record of this shock being felt outside Reported notfelt: of this small area. It was not felt here at Albuquerque, nor at Albuquerque, Placitas (12 miles N-NW of Sandia Park).

EARTHQUAKE OF APRIL 25, 1956, 20:30 MST The following summary for the earthquake of April askew. “Some new 25, 1956, cracks in outside plaster may have occurred.” 20:30 MST was published by the U.S. Coast Tijeras Canyon (E of Albuquerque). and Geodetic IV. Awakened many; Survey(1956, p. 15-16). frightened few. Windows, doors, and dishes rattled. Ground: Rocky. sloping, steep. Ranger reported Sandia Mountains, the shock was not felt at the near-by east of Albuquerque. Sandia Ranger Station. Placitas (village at north end of Sandia Mountains, about 17 Tres Pistolas Canyon (branches off north from Tijeras Canyon). miles north of the Tres Pistolas-Tijeras area). V. Felt by 3 families at IV. Motion rapid, lasted 2-3 seconds. Low rumble heard. Felt by least. First a muffled, explosivelike noise followed immediately by a several in home (sitting and active). Doors rattled; roof creaked. distinct jolt. House creaked. Aluminum tumbler, on the sink in the Ground: Rocky soil, compact, sloping and steep. Press reported house next door, rattled enough to be heard in adjoining room. a neighbor of the foregoing reporter heard a noise and Another neighbor across street felt jar. Dogs barked. noticed that Floor and couch windows and walls shook. “Rather pronounced. on which observer was sitting seemed I knew it was an to fall about an inch and then earthquake.” Lasted about 3 seconds. bounce back. Pictures on SE and NW walls of 2 rooms knocked

133 Index A&E Railway. 98 lithology, 53 Abert, J. W., 35 flood-plain conditions, thickness, 53 94 Abiquiu Formation, 67, ancient, 94 68, 86 Chinle Shale. 54 Abo Formation, 49-50, fluorite, 100, 101, 104 125 chloritization, 22 definition, 49 fluorspar, 105 Cibola Gneiss, distribution, 19, 21, 22, 27 Foraminifera, 42 50 clay. 110 fossils, 50 Four Hills, 11,23 analysis of, lithology, 50 110 Frisco Springs fault, coal, 110 77, 84, 85 thickness, 50 Frost fault block, 90 coal protrusions, 118 Agua Sarca fault. 82 coal-bearing shale, 128 Airport surface, 71, 86 galena, Cope, E. D., 73 104 Albuquerque basin, 85, 86 Galisteo Formation, Correo Sandstone Member, 53 62-66, 70, 84, 129 structural edge, 86 definition, Coyote Arroyo, 61, 62 62 Albuquerque-Belen basin, distribution, 85 Coyote Canyon, 21, 23 62 alluvial fan, 12, 15, 71 fossils Coyote Sandstone, 30 and age, 66 altitudes, 11 thickness, Coyote Springs district, 66 ancestral Rio Grande, 104 Galisteo 69 Cretaceous, 61-62 red beds, 61 Antonito, 19 Garcia Canyon, fossils and age, 61-62 102 Apache fault, 82 garnet, geosyncline, 95 105 Apachitos syncline, 85 geologic table of fossils, 61-62 history, 94-96 aplite, 27 graphite, crushed aggregate, 109 105 Arroyo Peñasco Formation, Glorieta 28, 48, 90, 100 Cuchilla Lupe horst, 83 Sandstone, 50,51,52 fossils, 29 gold, cuprodescloizite, 105 66 lithology, 29 gold-bearing gravel, 101 artifacts, 73 Gonzales Canyon, Dakota 51 Atokan, 37, 49 Sandstone, 56-58 Gonzales Creek, definition, 54, 57 axial gravels, 69 57 Graneros Shale, distribution, 57, 59, 60 azurite, 104 58 granite facades, fossils 92 and age, 58 great cliff faces, 12 lithology, bajada, 14 58 Great Combination mine, 98, thickness, 103 barite, 100, 104, 105 58 Greenhorn Formation, 59 Darrel prospect, Barro fault, 82, 85, 90, 91, 92 101 Greenhorn zone, 60 Davis, Bartola monocline, 88 Jefferson, 15 Gregg, Josiah, 66 Dead Mans Barton fault, 85 Peak. 56 ground sloth, 73 decorating Basin and Range blockfaulting, 91 rocks, 109 Gutierrez fault, 52, 84, descloizite, 87, 88, 89, 90, 118 basins, 77 104, 105 dips of, 89 Bernat Formation, 51, 52 Desmoinesian, 37, 49 beryl, 105 deuteric alteration, 24 Hagan basin, 11, 13, 52, Blake, William P., 17, Dockum Group, 21 54, 59, 60, 61, 62, 18, 19 69, 70, 77, 84,85,90 Blue Sky deposit, 101 Donnell prospect, 112 Hagan field, 99, 110 Blanca Sandstone Member, drainage basins, 13 50 coal analysis, 113 Bluff Sandstone, 56 coals of, 113 Bonney Canyon, 52 early mining operations, 97 production from, Brachiopoda, 43 earthquakes, 114 93, 131 reserves of, 113 bricks, 110 East Heights, 12 Hagan half-basin, 86 Brushy Basin Shale Member, East Mesa, 12 56 Flagan mines, 114 building stone, 108 east side faults, 81 Hagan ruins, 112 Bursum Formation, 30, 37, echelon of, 81, 49 82 Hall, James, 35 Ellis fault, 82 Hattie claims, 110 CabaLlo fault, 82 Entrada Sandstone, 53, 54 hematite, 107 calcareous tufa, age, 72 54 Hell Canyon calcite, 105 district, 98 definition, 53 Herrick,C.L.,92 Cano member, 60, 128 distribution, 53 high-angie reverse faults, Cañoncito fault, 82 lithology, 54 95 hogback ridges and valleys, Capulin deposit, 101 thickness, 54 13 Holocene fan scarp, 79 Capulin Peak, 15 Eocene deposition, 95 Holocene fault scalps, 28, Capulin Springs fault, eolian environment, 81,92 82 94 Holmes mine, 115 carbonatite, 104 ancient, 94 hornblende andesite, Carlile Shale, 59, epeirogenic 76 60 subsidence, 94 horn silver, 105 caves, 73 Espinaso Ridge, 67, 68, 85 Hubble Springs fault, 86 Cedar Crest syncline, 89 Espinaso Volcanics, 62, 67, 86 Cedar Mesa syncline, 114 age, 67 Cedar Mountain, 56 definition, 67 Ideal Cement plant, 21, 54, 107 ilmenite, Cedro Canyon, 13, 22 distribution, 67 107 Cedro fault, 85 lithology, 67 inselberg, 79 iron Cedro Peak, 31 Estancia basin, 85 ore, 108 isoclinal Cedro Peak horst, 85 Estancia Valley, 13 folds, 23 cement materials, 107 drainage, 12 cerargyrite, 105 surface, 71 Johnson, D. W., 92 Cerro Pelon mine, 103 Exeter Sandstone, 53 Jones, Fayette A., 92 Cerro Pelon Ridge, 21, 22, 103 Juana Lopez, 59, 60 Chamisoso fault, 84, 85, 88, 89 Fish Hatchery fault, Juan Tabo, 11, 15, 71,80 Chinle Formation, 52, 82 53, 56, 126 flagstone, 109 definition, 52 Flatirons fault, 91 distribution, 53 Kinney Brick Company, 110 Flint Ridge shale, 39, 47 Kinney clay pit, 34, 49 34

Rincon Ridge, 12. 15, 21, 28, 71, 72, 79, Ridge, 50. 51, 83. 125 Bajada fault, 85. 86 Montezuma 80. 96. 99 La salient. 84, 85 La Bajada surface. 71 Montezuma riprap, 109 76 La Casa Member. 30. 37 monzonite. rock fall, 76 Formation, 53, 56, 127 La Cueva Canyon. 24 Morrison rock pediment, 15 age. 57 lacustrine environment. 95 Rosario fault. 85 56 ancient. 95 detinition, ruins of ancient smelters, 98 distribution, 56 Lagunita fault. 91. 101 lithology. 56 La Luz mine, 98. 101. 102 Sabino anticline. 85 thickness. 57 La Luz trail. 102 San Andres, 51 Morrowan, 48.49 La Madera. 30 age, 52 mudtlows, 72 La Madera mine, 101 definition, 51 lamprophyric dikes, 70, 76 distribution, 51 landscaping rocks. 109 Needle, 12 lithology, 52 98 landslides, 76 Nero Placers district, thickness, 52 district, 97, 98 Laramide. 95 New Placers San Antonio, 18 Railway, 98 Laramide deformation, 91 New Mexico Central San Antonito fault, 82, 88 large granite boulders. 109 nonmetals, 105 Sandia anticline. 93 Largo fault, 85 maps, 3,4 Las Huertas, 11 ocher, 107 Sandia batholith, 27,94 Las Huertas fault, 91, 100 oil seep, 118 Sandia Cave, 73, 74 Las Huertas graben, 82-83 oil shale, 118 Sandia Crest, 15,21 Las Fluertas mine, 106 Old Placers district, 97 Sandia dip slope, 15 lime, 109 Omera coal mine, 61 Sandia Formation, 11, 30, 31-33, 42, 48, Lime Kiln bed, 107 orbicular rock, 25 49, 90 analysis of, 108 Ortiz pediment, 70, 71 age, 33 Log Springs Formation, 31,48 Ortiz pediment gravel, 15 coal in, 110 loose aggregate, 109 Ortiz surface, 70, 71, 72 definition, 31 Longfellow mine, 98 Osha Canyon, 82 distribution, 32 Lomos Altos syncline, 83 Osha Canyon formation, 48 graphic sections, 33 Los Moyos Limestone, 30, 37 Otero fault, 85 lithology, 32 Los Pinos fault, 89 Log Springs Formation, 31, 48 Paleozoic seas, 94 thickness, 32 30 13, 21, 23, 24, 83,90 Madera Canyon, 23, Palo Duroso fault, 82 Sandia Granite, 11. 30, 33-35, 48, 49, Madera Formation, Palomas Peak, 15, 35 age, 27 73, 83, 125 Pedernal Mountains, 94 color of, 23 member, 30, 85 Arkosic limestone ancient, 94 composition, 23 in, 90 definition, 33 Pennsylvanian, 30, 43 horizontal shearing distribution, 33 correlation, 37-48 inclusions, 23 26 lithology, 33 fossils, 35-49 orbicular structures, member, 30 12, 19, 20, 28, 30 Lower gray limestone pegmatite, 27, 28 Sandia Mountains, 30 Manzano Mountains, zoning, 28 photomosaic, 78 thickness, 34 Peña Blanca terrace. 71 Sandia Peak, 15 Madera Group, 30,43 Perdiz fault, 82 Sandia pediment, 71 Madera salient, 90 petrified wood, 66 Sandia piedmont, 71 30 Magdalena Group, 21, petroleum possibilities, 117 Sandia Range, 11 malachite, 104 piedmont, 12 Sandia surface, 71 mammoth tusk, 73 plain, 15 Sandia uplift, 77 74, 75 84 Mastodon americanus. Pina Vititos field, 110, 112 ramp, 79, 82, 83, mastodon tusk, 73 Pina Vititos mine, 110, 111, 114 terminations, 82, 84 127 54 Mancos Shale, 57, 5 8-60, Pine Shadow Member, 30, 37 San Felipe Indian Reservation, definition, 58 Pino Canyon-Bear Canyon, embayment, 15 San Felipe volcano, 86 92 distribution, 59 reentrant, 66, 67, 79 San Francisco fault, 82, 84, 85, lithology, 59 Pinovetito Arroyo, 111, 129 San Pedro, 11 thickness, 60 Placita Marl, 72, 73 Santa Fe, 68 11, 21, 30, 33,49,99 92 Manzanita Mountains, Placitas, 58, 61, 83, 131 Santa Fe fanglomerate, 68, 84, 85,93 Manzanita uplift, 77, 84, Placitas district, 98, 100 Santa Fe Formation, 67-69 Manzano Mountains, 21 Placitas fault, 77. 82, 83, 101 definition, 67 19, 28, 35, 36, 92 Marcou, Jules, 15, 18, Placitas field, 99, 117 distribution, 68 Mary M mines, 98, 103 Pomecerro fault, 82 lithology, 69 57-59, 60-62, 92, Mesaverde Formation, Precambrian, 11 Santa Fe Group, 67, 68 127-129 Purgatoire, 56 Santa Fe Railway, 100 definition, 60 pyromorphite, 107 San Pedro Creek, 11,61 distribution, 61 San Pedro fault, 85 lithology, 61 San Pedro porphyry complex, 90 Recapture Shale Member, 56 Meseta Blanca Sandstone Member, 50 San Pedro saddle, 90 ricolite, 22 metals, 100 San Pedro syncline, 90 Ridge fault, 77 metamorphic rocks, 21, 22, 23 Santa Rosa Sandstone, 52, 126 Rincon fault, 82 mineral resources, 97 definition, 52 Rio Grande, 13 mineral specimen occurrences, 105 distribution, 52 ancestral, 69 mining districts, 98 lithology, 52 Rio Grande depression, 11, 93 Mining Map, 98 thickness, 52 high seismicity of, 93 Mississippian, 36 Santo Domingo basin, 83, 85,86 Rio Grande trough. 77, 84, 85, 87, 91, 93 Missourian, 37, 49 San Ysidro Member, 50 displacement along, 87 Monte Largo, 11, 21, 35,77 Seco fault, 85,90 subsidence of, 87. 95 Monte Largo horst, 87, 88, 89, 90 1 mine, 115, 117. 118 tilting of, 87 Section Montezuma fault, 84 Sedillo Hill. 49 Rincon fault, 79,81,82,83,84,93 Montezuma mine, 100 sedimentary rocks, 21 Rincon metamorphics, 79 Montezuma Mountain, 15, 23, 30, 34, 71 135

sericitization. 22 Tijeras basin, 11, 54, Seven 58, 59, 77. 84, 87. 89, Una de Gato Arroyo, 61, 85 Springs, 35 90, 128, 131 Una de Gate sandstone, 112, 113 shale, 107. 110 Tijeras Canyon, 12, 15, 18, 21.22, 28 Una del Gate coal field, 110 analysis of, 110 Tijeras Canyon district. Shield, 100, 104 Una del Gato mine. 114 12. 15,81 Tijeras Creek, 11. 15,69 Sue uplift and erosion. 95 terrace, 7 1 drainage, 11 silexite, 27 uplifts, 77 Tijeras fault, 21. 22, 77. 84, 86. 87. silver. 66, 107 88, 89. upper buff formation, 69 90 uranium, 104 Simpson, J. H., 35 dips of, 89 Sloan coals, 112 left wrenching of. 88 valley alluvium, 72 analysis of. 112 Tijeras field, 99 Sloan verde antique. 22 mine, III, 112, 114 analysis of, 115 Sol Virgilian, 37, 49 se Mete Member, 30, 37 mines of, 115 Southern vogesite, 70 Union Production Company, 54, reserves of, 116 57 seams of, 114 South Sandia western escarpment, 12 Peak, 12, 15 small prospects, 116 specularite, 107 Westwater Canyon Sandstone Member, 56 Tijeras graben, 52, 77, 87, 88, 89, 90 Whipple, spessartite. 70 A. W., 15 Tijeras Greenstone, 19,21,22 Wild Cow spheroidal residual boulders, 12 Formation, 30, 37 Tijeras rift zone, 87, 91 Wislizenus, stratigraphic sections, 125 F. A., 66 displacement along, 87 Wolfcampian, stratigraphic table, 37, 49 21 Tijeras syncline, 61, 88, 89, 114 strontianite, Wolf Spring fault, 82 107 Tijeras wrench zone, 95 Suela fault, 77 Tocco mine, 115 Yeso Formation, Summerville Formation, 56 50-5 1 Todilto, 53 age, 51 swampy environment, 95 Todilto basin, 56 definition, 50 Sweet Ranch Petrified Forest, 66 Todilto Formation, 54-56 distribution, 50 definition, 54 tectonic lithology, 51 elements, 77 distribution, 54 orders thickness, 51 of, 77 lithology, 54 Tejano York mine, 22, 102 Canyon, 35 thickness, 56 Tejon Grant, 54 Tonque Arroyo, 61,62 Tesuque Zandia Clay, 72, 73 Formation, 68 tourmaline, 107 Thumb, Zia Sand Formation, 68, 86 12, 15 Tres Hermanos Sandstone, Tight, W. 57, 59 Zuzax fault, 88 G., 19 triangular fault facets, 12, Tijeras 80, 81 anticline, 57, 58, 70, 88, 89, 117 Tuerto Gravel, 70 136

Pocket Contents

MAP 1 -AREAL GEOLOGY MAP 2-TOPOGRAPHY MAP 3—STRUCTURAL GEOLOGY MAP 4—STRUCTURE SECTIONS

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