DEPARTMENT OF ENVIRONMENTAL PROTECTION Prepared in cooperation with the BEDROCK GEOLOGIC MAP OF THE STANHOPE QUADRANGLE WATER RESOURCES MANAGEMENT U.S. GEOLOGICAL SURVEY MORRIS AND SUSSEX COUNTIES, NEW JERSEY NEW JERSEY GEOLOGICAL AND WATER SURVEY NATIONAL GEOLOGIC MAPPING PROGRAM OPEN FILE MAP OFM 124

(NEWTON WEST)

(FRANKLIN) 74°45’ 42’30” (NEWTON EAST) 40’ 74°37’30” 41°00’ 41°00’ 75 _l 40 65 M 39 24 71 78 Yp 62 64 72 82 _h 43 U M 41 58 D Ybh Yk Yps 35 44 Ybs 82 72 Ybh 60 _ 60 a 38 56 61 83 T Granite and related rocks of the Byram and Lake Hopatcong Intrusive Suites are widespread and O_bl L CORRELATION OF MAP UNITS REFERENCES CITED 70 70 67 79 U 24 81 61 Ym Ybh 80 abundant in the map area where they intrude rocks of the Losee Suite and supracrustal rocks. The A 49 66 DESCRIPTION OF MAP UNITS Barnett, S.G., III, 1970, Upper Cayugan and Helderbergian stratigraphy of southeastern New York and F Ya 64 82 Stanhope quadrangle is designated as the type section (location in the Highlands where the rocks are Ybh 76 56 70 Yfw Ya Green Pond Mountain Region northern New Jersey: Geological Society of America Bulletin, v. 81, p. 2375-2402. M 61 Ybs GREEN POND MOUNTAIN REGION best exposed) for both suites that together comprise the Vernon Supersuite (Volkert and Drake, 1998). 31 Ym Ybh Ya Baum, J.L., 1967, The Tranquility prospect, Sussex County, New Jersey: New Jersey Zinc Company, 54 78 Byram and Lake Hopatcong rocks form a complete differentiation series that includes monzonite and Dkec Kanouse , Esopus Formation and Connelly Conglomerate, undivided (Lower Devo- 20 30

Yb unpublished inter-office correspondence on file in the office of the New Jersey Geological 22 17 Ybh 57 Ym 70 nian) 84 Ybs Dkec syenite, quartz monzonite and quartz syenite, granite, and alaskite. Granite of both suites yielded sim- 82 54 Ypg and Water Survey, Trenton, New Jersey, 14 p. 19 74 Ybs Ym 51 ilar U-Pb zircon ages of 1188 to 1182 Ma (Volkert and others, 2010). 49 Yk 53 57 74 Bayley, W.S., 1910, Iron mines and mining in New Jersey: New Jersey Geological Survey Bulletin 7, 59 Yp 79 60 72 Kanouse Sandstone (Kümmel, 1908) – Medium-gray, light-brown, and grayish-red, fine- to coarse- 43 80 70 74 Unconformity 39 46 Ylo Zd 512 p. T 26 80 The youngest high-grade crystalline rocks in the quadrangle are granite pegmatites that are un- grained, thin- to thick-bedded sandstone and pebble conglomerate. Basal conglomerate is interbedded S Ybs Ybh _ 70 58 Bayley, W.S., Salisbury, R.D., and Kummel, H.B., 1914, Description of the Raritan quadrangle, New a U 45 Ylo deformed and have discordantly intruded most other Mesoproterozoic rocks as small, irregular bodies. with siltstone and contains well-sorted, subangular to subrounded, gray and white quartz pebbles less 49 Ybs Sbp R Ybs Yp Yfw 59 65 R than 0.4 in. long. Lower contact with Esopus Formation gradational. Unit is about 46 ft. thick. Jersey: U.S. Geological Survey Geologic Atlas Folio 191, 32 p. H 61 None of the pegmatites are large enough to be shown on the map. Elsewhere in the Highlands, un- Ym 67 T 32 Yk Boucot, A.J., 1959, Brachiopods of the Lower Devonian rocks at Highland Mills, New York: Journal of

42 deformed coarse-grained felsic intrusions and pegmatites yielded U-Pb thermal ionization mass spec- 65 46 44 63 Ybh LT Sl 47 Yps 57 Paleontology, v. 33, p. 727-769. U 54 troscopy (TIMS) zircon ages of 1004 to 987 Ma (Volkert and others, 2005), indicating they are latest Esopus Formation (Vanuxem, 1842; Boucot, 1959) – Light- to dark-gray, laminated to thin-bedded 61 Yfw 47 A 69 Chadwick, H.G., 1908, Revision of “the New York series”: Science, new series, v. 28, p. 346-348. 71 U F 59 Mesoproterozoic to earliest Neoproterozoic in age. siltstone interbedded with dark-gray to black mudstone, dusky-blue sandstone and siltstone, and yel- 45 Ya 59 55 Sg D Ybs Chapman, D.F., 1966, Petrology and structure of the Byram Cove synform, Precambrian Highlands, Ym lowish-gray, fossiliferous siltstone and sandstone. Lower contact is probably conformable with Connelly 45 86 Ya 40 35 73 50 42 New Jersey: New Brunswick, N. J., Rutgers University, unpublished M.S. thesis, 116 p. 80 Yfw 86 Conglomerate. Unit is about 180 ft. thick in the map area. Y Ya 69 46 Unconformity STRUCTURE T Clarke, J.M., and Schuchert, C., 1899, The nomenclature of the New York series of geological forma- I Paleozoic bedding L Yb I tions: Science, new series, v. 10, p. 874-878. 75 VALLEY AND RIDGE Connelly Conglomerate (Chadwick, 1908) – Grayish-orange weathering, very light gray to yellow- U 79 Ylo 64 Bedding in the Paleozoic rocks has a mean strike of N53°E ± 29°(fig. 1). Beds dip northwest and, Dalton, R.F., Volkert, R.A., Monteverde, D.H., Herman, G.C., and Canace, R.J., 2014, Bedrock geolog- 68 Ybh 51 60 ish-gray, thin-bedded quartz-pebble conglomerate. Quartz pebbles are subrounded to well rounded, NQ 40 88 less commonly, southeast, although in the tectonic lens along Kennedys-East fault they are overturned ic map of the Hamburg quadrangle, Sussex County, New Jersey: New Jersey Geological and A 67 _bl well sorted, and as much as 0.8 in. long. Unit is about 36 ft. thick. Ym 54 Ya O R 66 75 58 and dip moderately to steeply southeast. The dip of all beds ranges from 21° to 87° and averages Water Survey Geologic Map Series GMS 14-3, scale 1:24,000. T Ylo 68 48°. Dames and Moore, 1981, Preliminary engineering analyses, dam, and dike facilities, proposed Hack- 50 67 Ybh M _a Sbp Berkshire Valley and Poxono Island Formations, undivided (Upper Silurian) 59 73 Ybs Ymr 56 ettstown reservoir, Hackettstown, New Jersey: Unpublished consultants’ report for New Jer- 70 19 48 82 37 57 Yps M _l Proterozoic foliation Berkshire Valley Formation (Barnett, 1970) – Yellowish-gray weathering, medium-gray to pink- sey Department of Environmental Protection Division of Water Resources, unpaginated. On Ybh 64 25 42 Ybs 56 Ypd file in the office of the New Jersey Geological and Water Survey, Trenton, New Jersey. 61 41 ish-gray, very thin to thin-bedded fossiliferous interbedded with gray to greenish-gray calcar- 60 51 Ybs 59 Ypg Crystallization foliation (the parallel alignment of mineral grains) is a penetrative metamorphic 55 44 T 50 _ Darton, N.H., 1894, Geologic relations from Green Pond, New Jersey, to Skunnemunk Mountain, New 51 h fabric formed as a result of directed compressional stresses during high-grade metamorphism that eous siltstone and silty dolomite, medium-gray to light-gray dolomite conglomerate, and grayish-black 45 54 50 UL 59 T 80 Ya A 30 Yb 84 York: Geological Society of America Bulletin, v. 5, p. 367-394. 55 59 60 34 F 49 78 deformed Mesoproterozoic rocks during the Grenvillian Orogeny. The strike of crystallization foliation is thinly laminated . Lower contact is conformable with Poxono Island Formation. Unit ranges in T Ybs AS Ypg M Yp 20 Ybh L 78 E thickness from 90 to 125 ft. Drake, A.A., Jr., 1984, The Reading Prong of New Jersey and eastern - An appraisal U Unconformity fairly uniform throughout most of the map area, but varies somewhat locally because of folding of the 46 32 24 80 of rock relations and chemistry of a major Proterozoic terrane in the Appalachians, in Bar- A 67 30 31 83 51 F Yp 78 rocks. The mean strike of foliation is N32°E ± 4° (fig. 2). Foliation dips southeast and, less commonly, Ym 55 58 Ya Ya 44 76 86 NEW JERSEY HIGHLANDS tholomew, M.J., ed., The Grenville event in the Appalachians and related topics: Geological 52 Ylo Ya northwest between 9° to 90° and averages 56°. Locally, in the hinge areas of major folds, foliations Poxono Island Formation (White, 1882; Barnett, 1970) – Very thin to medium-bedded sequence Ya Yk 55 Society of America Special Paper 194, p. 75-109. Ybh Ya 70 strike northwest and dip gently to moderately northeast. of medium-gray, greenish-gray, or yellowish-gray, mud-cracked dolomite; light-green, pitted, medi- Ybs Ybh _ 14 82 81 Drake, A.A., Jr., Aleinikoff, J.N., and Volkert, R.A., 1991, The Byram Intrusive Suite of the Reading 54 Ybh 60 D l 60 um-grained calcareous sandstone, siltstone, and edgewise conglomerate containing gray dolomite; 73 59 49 55 Prong - Age and tectonic environment, in Drake, A.A., Jr., ed., Contributions to New Jersey 65 75 PON 49 Yb 84 Folds and quartz-pebble conglomerate containing angular to subangular pebbles as much as 0.8 in. long. 59 35 Yfw 55 Zd 50 Geology: U.S. Geological Survey Bulletin 1952, p. D1-D14. Ya 70 87 75 58 Ybs 45 83 INTRUSIVE CONTACTS Interbedded grayish-green at lower contact are transitional into underlying Longwood Shale. 70 66 70 _l Yps Folds in the Paleozoic rocks postdate the development of bedding and they were formed during Drake, A.A., Jr., Kastelic, R.L., Jr., and Lyttle, P.T., 1985, Geologic map of the eastern parts of the 15 Ybh 14 Ya 32 70 Unit ranges in thickness from 160 to 275 ft. 61 70 47 Yp 26 78 Vernon Supersuite 76 45 Ym 64 the Taconian and (or) Alleghanian orogenies at about 450 Ma and 250 Ma, respectively. Paleozoic Belvidere and Portland quadrangles, Warren County, New Jersey: U.S. Geological Survey Ybs 24 26 42 70 Ym _l 25 54 Byram Intrusive Suite Lake Hopatcong Intrusive Suite folds include an east-northeast-striking, east plunging, open and upright anticline and syncline pair in Miscellaneous Investigations Series Map I-1530, scale 1:24,000. 82 75 41 28 71 Sl Longwood Shale (Upper and Middle Silurian) (Darton, 1894) – Dark reddish-brown, thin- to very 75 19 32 30 79 80 64 48 48 the Wright Pond area, and a northeast-striking and plunging, upright to locally overturned, and gently Drake, A.A., Jr., and Volkert, R.A., 1991, The Lake Hopatcong Intrusive Suite (Middle Proterozoic) of 72 40 31 55 Ylo M 79 69 thick-bedded shale interbedded with cross-bedded, very dark-red, very thin- to thin-bedded sandstone Ybh 54 Ym 78 Ybh Ybs Ypg Ypa Yps inclined to recumbent syncline in the Green Pond Mountain Region. the New Jersey Highlands, in Drake, A.A., Jr., ed., Contributions to New Jersey Geology: Ybs Ymr Yk 62 66 and siltstone. Lower contact is conformable with Green Pond Conglomerate. Unit is 330 ft. thick. 70 62 Ym M Ybs Ya Yps Yb 63 U.S. Geological Survey Bulletin 1952, p. A1-A9. Yh 45 17 66 _l 56 Ypg RO 23 33 64 51 42 INTRUSIVE CONTACTS Folds that deform Mesoproterozoic rocks deform earlier formed planar metamorphic fabrics and Sg ______, 1993, Bedrock geologic map of the Newton East quadrangle, Sussex County, New Jersey: 69 36 35 E 21 61 Green Pond Conglomerate (Middle and Lower Silurian) (Rogers, 1836) – Medium- to coarse- 46 Z 24 Ybs Yp 39 Yps 47 Ypg 81 68 therefore postdate the development of crystallization foliation. They formed during the Grenvillian Orog- U.S. Geological Survey Geologic Quadrangle Map GQ-1707, scale 1:24,000. Yp Ym 54 Ylo 43 41 Back Arc Supracrustal Rocks grained quartz-pebble conglomerate, quartzitic arkose and orthoquartzite, and thin- to thick-bedded 61 _h Ybh 55 81 85 eny at ca.1045 to 1030 Ma. The characteristic fold pattern in the map area consists of broad, open, Drake, A.A., Jr., Volkert, R.A., Monteverde, D.H., Herman, G.C., Houghton, H.F., Parker, R.A., and Ybh 50 Ybs Ylo Yp 58 68 reddish-brown siltstone. Grades downward into less abundant gray, very dark red, or grayish-purple, Ybh 45 85 58 northwest-overturned to locally upright, northeast-plunging antiforms and synforms. The dominant Dalton, R.F., 1996, Bedrock Geologic Map of Northern New Jersey: U.S. Geological Survey 66 47 79 Yp Yfw medium- to coarse-grained, thin- to very thick bedded pebble to cobble-conglomerate containing clasts 71 26 44 Ym Yb Yk Ymp Zd 65 T 36 61 Ypd Ymr plunge of mineral lineations is parallel to the axes of these folds; it ranges from 4° to 60° and averages Miscellaneous Investigations Series Map I-2540-A, scale 1:100,000. 44 Ybh 24 54 of red shale, siltstone, sandstone, and chert; yellowish-gray sandstone and chert; dark-gray shale and Ym H 80 44 22° toward N50°E (n = 78), although locally this trend plunges an average of 13° to S53°W (n = 7). In Hague, J.M., Baum, J.L., Herrman, L.A., and Pickering, R.J., 1956, Geology and structure of the Frank- IG Ybs 49 Yps chert; and white-to-gray and pink milky quartz. Quartz cobbles are as much as 4 in. long. Unconform- Ybs R 43 41 Ypg Yu 56 51 ? 44 76 Yps Magmatic Arc Rocks the northern and western part of the map, between the Zero and Kennedys-East faults, folds are char- lin-Sterling area, New Jersey: Geological Society of America Bulletin, v. 67, p. 435-474. 81 W Ybs 60 Ypg ably overlies the Leithsville Formation, Allentown Dolomite or Mesoproterozoic rocks in the map area. M 65 51 49 66 Losee Metamorphic Suite acterized by northwest overturned limbs and southeast-plunging axes defined by lineations that plunge Herman, G.C., and Mitchell, J.P., 1991, Bedrock geologic map of the Green Pond Mountain Region 58 Ypg Ypg Ypg Unit is about 1,000 ft. thick. 71 59 50 Ymr 71 53 81 69 an average of 23° to S61°E (n = 14). These folds were interpreted by Volkert and others (1989) to be from Dover to Greenwood Lake, New Jersey: New Jersey Geological Survey Geologic Map Ybs Ylo 31 79 81 Ybs 50 56 80 Ypg 60 M 82 36 - refolded folds that were subsequently truncated by the bounding faults. However, it is here considered Series 91-2, scale 1:24,000. S 35 42 67 Ylo Ylb Yh Yd 55 29 Y Valley and Ridge Ya 54 37 50 D Yps more likely that they formed as a result of rotational movement along the bounding faults. Howell, B.F., 1945, Revision of Upper Cambrian faunas of New Jersey: Geological Society of America, E 70 42 Kittatinny Valley Sequence Ya M 39 65 N 82 56 Memoir 12, 46 p. 72 36 N 76 74 31 E Ylo 56 80 Other Rocks Ybs Ybs K 79 72 Ymp (Clarke and Schuchert, 1899) Karklins, O.L., and Repetski, J.E., 1989, Distribution of selected Ordovician conodont faunas in north- 57’30” 31 75 79 U Faults Beekmantown Group 60 46 28 Ybh 51 Yps 57’30” 67 60 Yps D ern New Jersey: U.S. Geological Survey Miscellaneous Field Studies Map MF-2066, scale 60 63 YapYa The structural geology of the quadrangle is dominated by northeast-trending faults that deform 64 32 47 71 O_bl (Lower Ordovician to Upper Cambrian) – Consists of an upper, mid- 1:185,000. 82 Ya 52 61 Beekmantown Group, lower part 70 Ybh Ym 64 both Mesoproterozoic and Paleozoic rocks and partition the bedrock formations into a series of struc- 73 Ybh Ybs 50 53 dle, and lower sequence, but only the lower sequence is exposed in the quadrangle. Lower sequence Kümmel, H.B., 1908, Paleozoic sedimentary rocks of the Franklin Furnace quadrangle, New Jersey, in Ybh 42 Ybs 37 58 60 Ypg tural blocks. These structural blocks and associated sub-blocks were assigned names by Volkert and 59 41 consists of medium- to medium-dark-gray, aphanitic to coarse-grained, thinly-laminated to thick-bed- Spencer, A.C., Kummel, H.B., Salisbury, R.D., Wolff, J.E., and Palache, Charles, Description 45 44 52 67 71 61 68 others (1989) based on what they perceived to be lithological and geochronological differences be- 65 36 20 37 49 29 45 68 77 70 ded, slightly fetid dolomite having quartz-sand laminae and sparse, very thin to thin, black chert beds. of the Franklin Furnace quadrangle, New Jersey: U.S. Geological Survey Atlas Folio 161, p. Ybh 23 81 tween the blocks. More recent studies by the author in the New Jersey Highlands show that no differ- 45 31 46 80 70 51 Yap 69 78 27 42 50 Individual bed thickness decreases and floating quartz sand content increases toward lower grada- 10-12. 61 83 Yps 70 ences are present between the structural blocks and that the use of names for them is unnecessary. 49 61 54 Ypg 41 Ymr 35 54 52 tional contact. Contains conodonts of North American Midcontinent province Cordylodus proavus to MacLachlan, D.B., 1979, Geology and mineral resources of the Temple and Fleetwood quadrangles, 81 32 83 From the northwest, the major faults in the map area are the Tranquility thrust fault, Zero fault, Wright Ybh 52 71 74 52 69 Rossodus manitouensis zones (Karklins and Repetski, 1989) as used by Sweet and Bergstrom (1986). Berks County, Pennsylvania: Pennsylvania Geological Survey Atlas 187a, b, scale 1:24,000. Ybs 74 32 44 Pond fault, Kennedys-East fault, Reservoir fault, Turkey Brook fault, Ledgewood fault, Longwood Valley 23 84 52 77 Entire unit is Stonehenge Limestone of Drake and others (1985) and Stonehenge Formation of Volkert Markewicz, F.J., 1968, The Hardyston-Leithsville contact and significance ofHyolithellus micans in the 54 45 79 Yps 72 EXPLANATION OF MAP SYMBOLS fault, Berkshire Valley fault, and Picatinny fault. Most faults display complex movement histories and Ylo Ypg 63 64 and others (1989). Markewicz and Dalton (1977) correlate lower sequence to the Rickenbach Forma- lower Leithsville Formation: [abs.], New Jersey Academy of Science Bulletin, v. 13, p. 96. 40 Ylo Ylo Yps multiple reactivations from the Proterozoic through the Mesozoic. Earliest deformation recorded by the 44 76 72 tion. Unit is about 600 ft. thick. Markewicz, F.J., and Dalton, R.F., 1977, Stratigraphy and applied geology of the lower Paleozoic car- Ybs 21 Ybs 67 81 Contact - Dotted where concealed beneath water. faults formed under higher-temperature ductile conditions and consists mainly of mylonitic fabric. This 33 Yps bonates in northwestern New Jersey, in 42nd Annual Field Conference of Pennsylvania Ge- 34 Ybs 45 51 39 74 79 64 fault fabric typically is overprinted by deformation formed under lower temperature brittle conditions that 69 79 86 67 61 Yps _a Allentown Dolomite (Upper Cambrian) (Wherry, 1909) – Upper sequence is light-gray- to medi- ologists, Guidebook, 117 p. 20 Ylo Fault - Dotted where concealed. Queried where uncertain. consists of brecciation, recrystallization, alteration of mafic mineral phases, chlorite- or epidote-coated 79 Ylo Ymr 70 68 um-gray-weathering, medium-light- to medium-dark-gray, fine- to medium-grained, locally coarse- Metsger, R.W., 2001, Evolution of the Sterling Hill zinc deposit, Ogdensburg, Sussex County, New Ybs 27 56 30 Yps fractures or slickensides, and (or) close-spaced fracture cleavage. Ylo Ym Ybh 42 72 45 68 74 grained, medium- to very thick-bedded dolomite; local shaly dolomite near the bottom. Floating quartz Jersey: Society of Economic Geologists Guidebook Series, v. 35, p. 75-88. Ybh Mr 11 Ypg U 24 Ylb 63 Yb 31 51 51 53 67 71 D Normal fault - U, upthrown side; D, downthrown side sand and two series of medium-light- to very light-gray, medium-grained, thin-bedded quartzite and Nason, F.L., 1891, The Post-Archaen age of the white limestone of Sussex County, New Jersey: New 15 43 65 63 The Tranquility thrust fault strikes about N20°E and dips gently to moderately southeast. The fault 31 73 Ybh 83 73 discontinuous dark-gray chert lenses occur directly below upper contact. Lower sequence is medi- Jersey Geological Survey, Annual Report of the State Geologist for 1890, p. 25-50. 82 23 50 Ya 64 70 D is poorly exposed in the map area, but to the north, in the Newton East quadrangle, the fault contains Yp 41 40 45 um- to very-light-gray-weathering, light- to medium-dark-gray, fine- to medium-grained, thin- to medi- Offield, T.W., 1967, Bedrock geology of the Goshen-Greenwood Lake area, New York: New York State Ylo 59 36 Ypg 86 U Reverse fault - U, upthrown side; D, downthrown side Mesoproterozoic marble and gneiss on the hanging wall thrust westward over Paleozoic dolomite and 43 57 Museum and Science Service Map and Chart Series, no. 9, 78 p. 74 Ylo 54 41 79 um-bedded dolomite and shaly dolomite. Weathered exposures characterized by alternating light- and 52 57 42 46 Mesoproterozoic rocks on the footwall (Drake and Volkert, 1993). There the fault was penetrated at Ybh Ybh 41 Zd 58 Yap dark-gray beds. Ripple marks, oolites, algal stromatolites, cross-beds, edgewise conglomerate, mud Palmer, A.R., and Rozanov, A.Y., 1967, Archaeocyatha from New Jersey: Evidence for an intra-forma- Ya 80 64 Yps Inclined thrust fault - teeth on upper plate a depth of -1,422 ft. in drill hole DR2 and -1,593 ft. in drill hole DR1 at the Limecrest quarry during 74 T 28 R L 53 70 Yb cracks, and paleosol zones occur throughout but are more abundant in lower sequence. Lower contact tional unconformity in the north-central Appalachians: Geology, v. 4, p. 773-774. 46 56 54 Ypg drilling in 2009 (Volkert, 2010). West of the map area, the Tranquility thrust fault was encountered by 51 70 U 59 Peck, W.H., Volkert, R.A., Meredith, M.T., and Rader, E.L., 2006, Calcite-graphite thermometry of the Ybh 35 34 A 47 73 36 45 70 82 80 gradational into Leithsville Formation. Unit contains a fauna of Dresbachian (early Late Cam- 49 F Ylo 50 New Jersey Zinc Company geologists in drill core in the Tranquility quadrangle (Baum, 1967). In the 80 78 Franklin Marble, New Jersey Highlands: Journal of Geology, v. 114, p. 485-499. 71 41 brian) age (Weller, 1903; Howell, 1945). Approximately 1,800 ft. thick regionally. Ypd 24 Ybs 56 38 61 52 47 66 Hamburg quadrangle, the Tranquility thrust fault appears to merge with the Pochuck fault (Dalton and 47 56 38 Ybs FOLDS Rogers, H.D., 1836, Report on the geological survey of the State of New Jersey: Philadelphia, Desilver, Ylb M 53 41 41 59 others, 2014). The Tranquility thrust fault is characterized by an older ductile deformation fabric strongly Ybs 78 _h _l Leithsville Formation (Middle to Lower Cambrian) (Wherry, 1909) – Upper sequence, rarely exposed, Thomas, & Co., 174 p. 54 17 60 overprinted by younger brittle deformation. 73 _l 65 Folds in Proterozoic rocks showing trace of axial surface, direction and dip of limbs, and direction 38 55 54 is mottled, medium-light- to medium-dark-gray-weathering, medium- to medium-dark-gray, fine- to me- Stanford, S.D., Stone, B.D., and Witte, R.W., 1996, Surficial geology of the Stanhope quadrangle, Ymr Ch 51 Ymp 43 63 T 64 of plunge. Dotted where concealed beneath water. Morris and Sussex Counties, New Jersey: New Jersey Geological Survey Open-File Map M S 50 46 dium-grained, medium- to thick-bedded, locally pitted and friable dolomite. Middle sequence is gray- Yk 40 64 Yps M Ypg The Zero fault strikes about N35°E and dips steeply southeast an average of 80°. Latest move- 34 65 A 54 48 ish-orange or light- to dark-gray, grayish-red, light-greenish-gray- or dark-greenish-gray-weathering, OFM 22, scale 1:24,000. E Yps ment appears to have been normal. Here, the fault contains Mesoproterozoic rocks on both sides, but 56 51 54 43 Sweet, W.C., and Bergstrom, S.M., 1986, Conodonts and biostratigraphic correlation: Annual Review Yp 68 56 aphanitic to fine-grained, thin- to medium-bedded dolomite, argillaceous dolomite, dolomitic shale, 71 Upright synform 31 northeast in the Franklin quadrangle the fault borders the west side of the Wallkill River Valley where it 51 Yps 73

Yps 59 52 (DOVER) quartz sandstone, siltstone, and shale. Lower sequence is medium-light- to medium-gray-weathering, of Earth and Planetary Science, v. 14, p. 85-112. Zd 36 Yb 40 62 78 64 Yb places Mesoproterozoic rocks on the footwall against Paleozoic rocks on the hanging wall (Hague and

(TRANQUILITY) Ybs

46 47 Ypg medium-gray, fine- to medium-grained, thin- to medium-bedded dolomite. Quartz-sand lenses occur Vanuxem, Lardner, 1842, Geology of New York, part III, comprising the survey of the third geological T Ymp 64 40 56 Ypg Overturned antiform others, 1956). In the map area, the fault merges with, or is cut off by the Wright Pond fault, and at its 43 42 56 80 78 district: Albany, N.Y., 306 p. 67 UL near lower gradational contact with Hardyston Quartzite. Archaeocyathids of Early Cambrian age are 49 northern end in the Franklin quadrangle, the Zero fault loses displacement and terminates in a series 30 41 45 FA 70 Ylo present in formation at Franklin, New Jersey, suggesting an intraformational disconformity between Volkert, R.A., 1996, Geologic and engineering characteristics of Middle Proterozoic rocks of the High- 41 57 Ypg of horsetails that are cut off by the Kennedys-East fault (Volkert and Monteverde, 2013). The Zero fault 39 84 Overturned synform Middle and Early Cambrian time (Palmer and Rozanov, 1967). Unit also contains Hyolithellus micans lands, northern New Jersey, in Engineering geology in the metropolitan environment: Field Ypd 50 43 75 Ya 43 60 65 U is characterized by an older ductile deformation fabric that is overprinted by younger brittle deformation Yk Ylo Ybh D (Offield, 1967; Markewicz, 1968). Approximately 800 ft. thick regionally. Guide and Proceedings of the 39th Annual Meeting of the Association of Engineering Geol- Ybh Yps fabric of probable Paleozoic age (Metsger, 2001). 56 Folds in Paleozoic rocks showing trace of axial surface, direction and dip of limbs, and direction of ogists, p. A1-A33. M - M 80 65 S Ylo 34 _h ______, 2004, Mesoproterozoic rocks of the New Jersey Highlands, north-central Appalachians: 59 64 Y Ypg Yb plunge. Folds in bedding and/or cleavage. Dotted where concealed beneath water. Hardyston Quartzite (Lower Cambrian) (Wolff and Brooks, 1898) – Medium- to light-gray, fine-to 34 41 D 34 The Wright Pond fault strikes about N50°E and dips steeply southeast an average of 75°. Latest 50 E coarse-grained, medium- to thick-bedded quartzite, arkosic sandstone and dolomitic sandstone. Con- petrogenesis and tectonic history, in Tollo, R.P., Corriveau, L., McLelland, J., and Bar- 51 Yb movement was normal, but the fault also preserves a component of left-lateral strike slip movement. In N 47 26 66 75 55 N U tains Scolithus linearis (?) and fragments of the trilobite Olenellus thompsoni of Early Cambrian age tholomew, J., eds., Proterozoic tectonic evolution of the Grenville orogen in North America: 54 45 E 56 Anticline the map area, the Wright Pond fault contains a lens of Hardyston Quartzite and Leithsville Formation 64 D 61 36 K 60 (Nason, 1891; Weller, 1903). Thickness regionally is less than 20 ft. Geological Society of America Memoir 197, p. 697-728. Yp 63 on the hanging wall, but otherwise throughout its length the fault has Mesoproterozoic rocks on both the Ylo 74 Yb ______, 2010, Deep drilling at Limecrest quarry, Sparta, New Jersey: A geologic perspective: The 40 Yps hanging wall and footwall. The fault is characterized by brittle deformation fabric. 56 54 39 Yps Syncline Yp Yps Yps Picking Table, v. 51, p. 10-13. Yp 60 60 New Jersey Highlands

52 69 59 44 64 Yb ______, 2012, Bedrock geologic map of the Dover quadrangle, Morris County, New Jersey: New 53 52 The Kennedys-East fault strikes about N45°E and dips steeply southeast an average of 75°. The Yps Zd Diabase dikes (Late Neoproterozoic) (Volkert and Puffer, 1995) – Light gray- or brownish-gray-weath- 54 44 49 PLANAR FEATURES Jersey Geological Survey Open-File Map 91, scale 1:24,000. 46 63 56 32 fault borders the west side of Lubbers Run Valley in the map area and the east side of the Wallkill River ering, dark-greenish-gray, aphanitic to fine-grained dikes. Composed principally of plagioclase (labra- Volkert, R.A., Aleinikoff, J.N., and Fanning, C.M., 2010, Tectonic, magmatic, and metamorphic history Ybh 55 68 Yp 60 Ypg Valley to the north. It has been mapped as Kennedys fault in the southwest Highlands and the East 60 dorite to andesine), augite, and ilmenite and (or) magnetite. Locally occurring pyrite blebs are common. of the New Jersey Highlands: New insights from SHRIMP U-Pb geochronology, in Tollo, R.P., 52 Yp 47 Strike and dip of beds 79 54 fault in the northern Highlands (Drake and others, 1996), but more recent detailed quadrangle-scale Contacts are typically chilled and sharp against enclosing Mesoproterozoic country rock. Dikes are 57 Bartholomew, M.J., Hibbard, J.P., and Karabinos, P.M., eds., From Rodinia to Pangea: The Ylb 46 35 mapping shows that it is the same fault. In the Hamburg quadrangle, the fault is cut off by the Hamburg tholeiitic to alkalic in composition and hypersthene normative. Ybs Ypg 26 45 40 Lithotectonic Record of the Appalachian Region, Geological Society of America Memoir 206, 47 Yp 30 Ypg Inclined fault (Dalton and others, 2014). Latest movement appears to have been reverse. The Kennedys-East Ymp Ya 52 65 Ypg 67 p. 307-346. 60 54 71 51 46 45 17 51 74 fault contains Mesoproterozoic rocks on both sides along most of its length, but north of the map area 78 46 36 63 Yps LT Vernon Supersuite (Volkert and Drake, 1998) 25 U 65 Volkert, R.A., and Drake, A.A., Jr., 1998, The Vernon Supersuite: Mesoproterozoic A-type granitoid 82 LT 34 Ylb Yk 72 it contains Paleozoic rocks on the footwall and Mesoproterozoic rocks on the hanging wall. The fault is

66 65 U ? 54 26 46 A 65 75 Overturned Byram Intrusive Suite (Drake and others, 1991) rocks in the New Jersey Highlands: Northeastern Geology and Environmental Sciences, v. A 59 68 Ybh F 51 59 F 39 Ylb 66 23 Ypg 68 characterized by brittle deformation fabric. 74 26 Ypg Yb Ymp 20, p. 39-43. _l 52 Yp 45 Strike and dip of crystallization foliation Ybh Hornblende granite (Mesoproterozoic) – Pinkish-gray- to buff-weathering, pinkish-white or light-pink- ______, 1999, Geochemistry and stratigraphic relations of Middle Proterozoic rocks of the New 45 84 49 The Musconetcong thrust fault is a major regional structure that extends from the Delaware River D 41 44 Ya ish-gray, medium- to coarse-grained, foliated granite composed principally of microcline microperthite, Jersey Highlands, in Drake, A.A., Jr., ed., Geologic Studies in New Jersey and eastern Penn- Ya 20 north to the map area (Drake and others, 1996) where it is cut off by the Kennedys-East fault. The T 45 IR 62 quartz, oligoclase, and hornblende. Some variants are quartz monzonite or quartz syenite. Includes _l D S 50 39 63 Ypg sylvania: U.S. Geological Survey Professional Paper 1565C, 77 p. RU 40 71 O 53 63 Inclined Musconetcong thrust fault borders the western side of Schooleys Mountain and the east side of Mus- TH Ylo 31 38 V bodies of pegmatite too small to be shown on the map. Volkert, R.A., and Monteverde, D.H., 2013, Bedrock geologic map of the Franklin quadrangle, Sussex G 52 44 R conetcong Valley. The fault strikes generally northeast and dips moderately southeast an average of ON 40 35 E Yps 55’ CONETC Yp S 45 and Morris Counties, New Jersey: New Jersey Geological and Water Survey Geologic Map MUS 44 59 M E 55’ Vertical 30°. It contains Mesoproterozoic rocks on the hanging wall that have been thrust onto Paleozoic and G 46 R Yb Yb Ybs Hornblende monzonite (Mesoproterozoic) – Pinkish-gray- to buff-weathering, pinkish-gray or green- Series GMS 13-3, scale 1:24,000. 35 Yp Mesoproterozoic rocks of the footwall. The fault does not crop out in the map area but is known from a G Ylo 58 Yps ish-gray, medium- to coarse-grained, foliated monzonite or syenite, and less abundant quartz mon- Volkert, R.A., Monteverde, D.H., and Drake, A.A., Jr., 1989, Bedrock geologic map of the Stanhope 38 58 T 6 Ylb Ya Ylo Ypg series of borings drilled in the Musconetcong Valley to the southwest (Dames and Moore, 1981). zonite or quartz syenite, composed of microcline microperthite, oligoclase, hornblende, and quartz. 49 36 UL quadrangle, Sussex and Morris Counties, New Jersey: U.S. Geological Survey Geologic 85 38 Yb A Contains sparse amounts of pyroxene where in contact with rocks of the Lake Hopatcong Intrusive F LINEAR FEATURES Quadrangle Map GQ-1671, scale 1:24,000. 36 20 48 Ya Ya Yb The newly recognized and named Mount Olive fault extends from the southeastern part of the Suite in the southeastern part of the map. Volkert, R.A., and Puffer, J.H., 1995, Late Proterozoic diabase dikes of the New Jersey Highlands – A

Yps 18 Tranquility quadrangle, through Mount Olive, to the town of Stanhope where it is cut off by an unnamed,

remnant of Iapetan rifting in the north-central Appalachians: U.S. Geological Survey Profes- Bearing and plunge of mineral lineation in Proterozoic rocks Ypg northwest-striking fault. The Mount Olive fault does not crop out and is known from a series of water

Lake Hopatcong Intrusive Suite (Drake and Volkert, 1991) 53 Ypg Ybh 30 sional Paper 1565-A, 22 p.

wells and borings that penetrated Paleozoic Hardyston Quartzite and Leithsville Dolomite (F.J. Marke- 43 39 M Volkert, R.A., Zartman, R.E., and Moore, P.B., 2005, U-Pb zircon geochronology of Mesoproterozoic 23 Ypg Pyroxene granite (Mesoproterozoic) – Buff- or white-weathering, greenish-gray, medium- to coarse- 25 OTHER FEATURES wicz, unpublished data). The fault strikes east-northeast and probably dips southeast at an undeter- 49 Ybs postorogenic rocks and implications for post-Ottawan magmatism and metallogenesis, New 50 grained, gneissic to indistinctly foliated granite containing mesoperthite to microantiperthite, quartz, Ymp mined angle. It is inferred to have Paleozoic and Mesoproterozoic rocks on the hanging wall and Meso- 42 M Jersey Highlands and contiguous areas, USA: Precambrian Research, v. 139, p. 1-19. oligoclase, and clinopyroxene. Common accessory minerals include titanite, magnetite, apatite, and proterozoic rocks on the footwall based on this same structural relationship of fault-bounded Paleozoic 27 Abandoned magnetite mine Weller, Stuart, 1903, The Paleozoic faunas: New Jersey Geological Survey, Report on Paleontology, Ya Ymp trace amounts of zircon and pyrite. K lenses throughout the quadrangle. Latest movement is here interpreted to have been normal. Yps O v. 3, 462 p. 32 Ylo 84 O R Active rock quarry in granite or gneiss R Wherry, E.T., 1909, The early Paleozoic of the Lehigh Valley district, Pennsylvania: Science, new se- Yp G Ypg Ypa Pyroxene alaskite (Mesoproterozoic) – Buff- or white-weathering, greenish-buff to light pinkish-gray, G B Ylo The Reservoir fault here strikes about N45°E and dips steeply southeast an average of 85°. Else- Yb R ries, v. 30, 416 p. 80 Mr where it dips vertically or steeply northwest. In the map area it contains Mesoproterozoic rocks on both medium- to coarse-grained, massive, moderately foliated granite composed of mesoperthite to micro- 78 34 35 36 Yh White, I.C., 1882, The geology of Pike and Monroe Counties: Pennsylvania Geological Survey, 2nd 40 Abandoned rock quarry in granite or gneiss, R; marble, Mr antiperthite, quartz, oligoclase, and sparse amounts of clinopyroxene. Common accessory minerals 36 sides of the fault, whereas northeast of the quadrangle the fault places Paleozoic rocks on the hanging

include titanite, magnetite, apatite, and trace amounts of zircon. series, Report G-6, 407 p.

wall against Mesoproterozoic rocks on the footwall. The fault records a history of movement involving Ypg Ybs Yps 55 Dkec Wolff, J.E., and Brooks, A.H., 1898, The age of the Franklin white limestone of Sussex County, New Ylo Mr D Bedrock float used to draw lithologic contact reverse, dextral strike slip, and normal, with latest movement having been normal. The Reservoir fault Ymp R Ylo O Jersey: U.S. Geological Survey 18th Annual Report, pt. 2, p. 425-457. is characterized by ductile deformation fabric in the center of the fault, overprinted by a pervasive brittle Yps Pyroxene monzonite (Mesoproterozoic) – Gray-to buff- or tan-weathering, greenish-gray, medium- to Yps O Ylo Ypg T Zd Yps R Young, D. A., 1969, Petrology and structure of the west-central New Jersey Highlands: Providence, L W Spb coarse-grained, massive, moderately foliated monzonite or syenite and less abundant quartz monzon- U Bore hole or water well in granite or gneiss, R; marble, Mr; dolomite, D deformation fabric that envelops the mylonite on both sides of the fault over a total width of as much A E R.I., Brown University, unpublished Ph.D. dissertation, 194 p. 41 F G ite or quartz syenite. Composed of mesoperthite, microantiperthite to microcline microperthite, oligo- G as 1,000 ft. Yps Ypg D 35 83 clase, clinopyroxene, titanite, magnetite, and sparse apatite and local quartz. Locally contains sparse E Yps Sl Zd 65 L Form line showing foliation in Proterozoic rocks. Shown in cross section only. 78 amounts of hornblende. Ypg The Turkey Brook fault strikes about N40°E and dips steeply southeast an average of 75°. The 64 79

fault contains Mesoproterozoic rocks on both sides along its entire length. The latest movement is

Yps 41 inferred to have been normal. The fault is characterized by brittle deformation fabric as much as a few Back-arc basin supracrustal rocks (Volkert, 2004) D 79 Yp M 75 Sg hundred feet wide. M Yh Ypg D 50 84 65 Yd Ym Microcline gneiss (Mesoproterozoic) – Pale pinkish-white weathering, tan to pinkish-white, fine- to G 82 U M D Ylo G D 81 The Ledgewood fault strikes about N20°E and dips steeply toward the southeast at about 70°. The medium-grained, layered and foliated rock composed of quartz, microcline microperthite, and oligo- 76 Ypg 41 clase. Common accessory minerals include biotite, garnet, magnetite, and sillimanite. Locally inter- fault contains Mesoproterozoic rocks on both sides along its entire length. Latest movement on the fault Ymp INTRODUCTION Ypg appears to have been normal. The Ledgewood fault is characterized by brittle deformation fabric. layered with quartz-rich metasedimentary rock. Contains conformable clots and lenses of partial melt. Yps 77 N 40 Yh 66 The Stanhope 7.5-minute quadrangle, located in the New Jersey Highlands Physiographic Prov- E Yps Y 71 V 69 66 I E 36 Yps ince, is characterized by parallel, northeast-trending ridges with elevations that locally exceed 1,100 ft. Yb Biotite-quartz-feldspar gneiss (Mesoproterozoic) – Gray-weathering, locally rusty, gray, tan, or Ybs L D K The Longwood Valley fault strikes about N40°E and dips steeply southeast an average of 80°. G O greenish-gray, medium- to coarse-grained, moderately layered and foliated gneiss containing micro- D G UR Ylo Yp above sea level. This topographic expression is disrupted in the southern part of the map area by the In the map area and to the northeast, the fault contains Mesoproterozoic rocks on the footwall and D T Zd Yd 69 61 generally east-west-trending Wisconsinan-age terminal moraine that includes more than 200 ft. of gla- cline microperthite, oligoclase, quartz, and biotite. Locally contains garnet, tourmaline, sillimanite, and Paleozoic rocks of the Green Pond Mountain Region on the hanging wall (Herman and Mitchell, 1991; magnetite; graphite and pyrrhotite occur in rusty gneiss. Ypg _ LT cial sediment deposited on the bedrock surface (Stanford and others, 1996). The Stanhope quadrangle Drake and others, 1996). The latest movement on the Longwood Valley fault was normal. The fault is G l U A 41 F is situated in the Musconetcong River watershed, and along with Lubbers Run these two streams characterized by brittle deformation fabric along its entire length. 65 U G 82 Yk Potassic feldspar gneiss (Mesoproterozoic) – Light-gray- or pinkish-buff-weathering, pinkish-white 83 D constitute the dominant regional drainages.

Ypg or light-pinkish-gray, fine- to medium-grained and locally coarse-grained, moderately foliated gneiss Ybs Ylo The Berkshire Valley fault is not exposed in the map area, or to the northeast in the Dover quad- U Yp MOUNT 83 The bedrock geology of the Stanhope quadrangle has been the subject of study for more than a composed of quartz, microcline microperthite, oligoclase, and variable amounts of biotite, garnet, tour- D _h 82 45 rangle. Its occurrence was inferred by Herman and Mitchell (1991) based on missing stratigraphic units

T century (Bayley and others, 1914; Hague and others, 1956; Chapman, 1966; Young, 1969; Volkert and maline, sillimanite, and magnetite. U L between the Green Pond Conglomerate and Cornwall Shale in the Berkshire Valley. The fault strikes 69 D 44 Yps U others, 1989). However, most previous bedrock studies lack continuity with the more recent detailed 5101520 24 Ylo A about N40°E and dips southeast an average of 45°. It contains Paleozoic rocks on both sides along its Yk F % Sg geologic mapping of adjacent quadrangles and conformity with the present geologic framework pro- Ymp Clinopyroxene-quartz-feldspar gneiss (Mesoproterozoic) – Pinkish-gray- or pinkish-buff- weather- G Y entire length. The latest movement appears to have been reverse. The fault is characterized by a zone E Ylo Yps L posed for Mesoproterozoic rocks in the Highlands. Moreover, new interpretations of bedrock geologic ing, white, pinkish-white, or light-gray, medium-grained and locally coarse-grained, moderately well fo- Ypg L 39 of brittle fabric of unknown width. Ybs Yk 5 47 A _ relationships, based in part on detailed major and trace element geochemistry, stable isotope analysis, liated gneiss composed of quartz, microcline, oligoclase, clinopyroxene, and trace amounts of epidote, 64 72 V l G 74 M 75 Y 66 and uranium-lead (U-Pb) geochronology, has considerably improved much of the previous work in the biotite, titanite, and magnetite. Ylb 45 E The Picatinny fault strikes N30°E and dips southeast an average of 50°. The fault contains Paleo- G 76 L 71 10 U L quadrangle. Therefore, interpretations presented here supersede those shown on the more recent zoic rocks on both sides along most of its length, except for a short segment in the Dover quadrangle, 78 75 G D 79 62 81 A Yp Ypg Yp V T bedrock geologic maps of Volkert and others (1989), and Drake and others (1996). This report provides Pyroxene gneiss (Mesoproterozoic) – White- or tan-weathering, greenish-gray, fine- to medi- Ypg Ypg 78 84 L near Picatinny Lake, where Mesoproterozoic rocks are present on the hanging wall (Volkert, 2012). Ypd Ypg 84 64 U updated, detailed geologic information on the stratigraphy, structure, ages and descriptions of geologic um-grained, well layered and foliated gneiss containing oligoclase, clinopyroxene, variable amounts 15 Ypg A Latest movement appears to have been reverse. The fault is characterized by brittle deformation fab- Ypg M Sg F of quartz, and sparse amounts of epidote, titanite, scapolite, or calcite (Yp). Unit is spatially associat- 61 55 units in the map area. Cross-section A-A’ shows a vertical profile of the geologic units and their struc- ric. 72 ed with thin, generally conformable layers of medium-grained, green, nearly monomineralic diopsidite Ylo 82 E ture, and rose diagrams in figures 1-3 provide a directional analysis of selected structural features. 20 D R Yd 64 78 O I (Ypd) composed of diopside. 70 79 H Mesoproterozoic rocks throughout the map area are also deformed by smaller, less regionally per- O S 35 Ylo W K Y vasive, northeast- or northwest-striking faults, some of which appear to be confined to outcrop scale. G 66 Yh 61 R N STRATIGRAPHY Yfw E N Marble (Mesoproterozoic) – White- to light-gray-weathering, white or grayish-white, fine- to coarse-crys- Ylo 42 Ypa NG B I _l Paleozoic rocks Fault widths are typically a few inches to a few feet. These faults are characterized mainly by brittle 70 Yk O T Ymr Sector angle = 10° L A deformation features. talline, calcitic to locally dolomitic marble with accessory graphite, phlogopite, chondrodite, and clin- 23 Ypg C n = 21 63 I 47 Lower Paleozoic formations of Cambrian and Ordovician age of the Kittatinny Valley Sequence opyroxene. Contains pods and lenses of clinopyroxene-hornblende rock, clinopyroxene-garnet rock, Yk P Sg crop out throughout the quadrangle where they unconformably overlie, or are in fault contact with Me- Yd Yh Joints scapolite-phlogopite rock, and clinopyroxene-rich rock. Marble was separated by New Jersey Zinc 36 Ybh 79 34 Figure 1. Rose diagram showing the orientation of bed- Ypg 36 26 Ymp soproterozoic rocks in tectonic lenses on some of the major faults. Lower Paleozoic rocks that do not Company geologists (Hague and others, 1956) into a structurally lower Franklin Marble layer (not ex- 69 Yh 80 76 Joints are a common feature in Mesoproterozoic and Paleozoic formations in the map area. Those ding in Paleozoic rocks. 40°52’30” 40°52’30” crop out were also recently discovered under part of the Wisconsinan terminal moraine north of Budd posed in map area) and an upper Wildcat Marble layer (Yfw). Marble outcrops exposed near Cranberry 74°45’ 42’30” (CHESTER) 40’ 74°37’30”(MENDHAM) Lake (F.J. Markewicz, unpublished data on file in the office of the New Jersey Geological and Water developed in Paleozoic rocks are common in limestone, dolomite, and sandstone. The dominant joint Lake, Stag Pond, and Wright Pond cannot be definitively correlated to the Wildcat Marble and are Survey) and are shown on this new iteration of the bedrock map. The Kittatinny Valley Sequence was set in Paleozoic rocks strikes northwest an average of N66°W and, less commonly, N23°W. Joints dip mapped as undifferentiated marble (Ymr). Base map by the Army Map Service and United States Geological Survey. Geology mapped by R.A. Volkert in 2009 previously considered to be part of the Lehigh Valley Sequence of MacLachlan (1979) but was reas- with near equal abundance northeast and southwest an average of 67°. A subordinate joint set strikes Edited and published by the United States Geological Survey. signed by Drake and others (1996). In the map area it includes the Kittatinny Supergroup (Hardyston N66°E and dips with near equal abundance southeast and northwest an average of 74°. Magmatic arc rocks (Volkert, 2004) Digital cartography by R.S. Pristas (HACKETTSTOWN) Quartzite, Leithsville Formation, Allentown Dolomite, and lower part of the Beekmantown Group). East Losee Suite (Drake, 1984; Volkert and Drake, 1999) Control by USGS, USC&GS, and New Jersey Geodetic Survey. of the Longwood Valley fault, in the southeastern part of the quadrangle, Lower and Middle Paleozoic Joints developed in Mesoproterozoic rocks are characteristically planar, moderately well formed, This geologic map was funded in part by the U. S. Geological Survey, rocks of Cambrian through Devonian age of the Green Pond Mountain Region unconformably overlie, moderately to widely spaced, and moderately to steeply dipping. Surfaces of joints are typically unmin- SCALE 1:24 , 000 National Cooperative Geologic Mapping Program, eralized, except where proximal to faults, and are smooth and less commonly slightly irregular. Joints Ylo Quartz-oligoclase gneiss (Mesoproterozoic) – White-weathering, light-greenish-gray, medium- to Topography from aerial photographs by photogrammetric methods. Aerial or are in fault contact with, Mesoproterozoic rocks. N 1 .5 2 0 1 MILE under STATEMAP award number G09AC00185. The coarse-grained, moderately layered and foliated gneiss to indistinctly foliated gneiss and less abundant photographs taken 1942. Field check 1943. Culture revised by the United States are variably spaced from a foot to tens of feet. Those developed in massive rocks such as granite tend views and conclusions contained in this document to be more widely spaced, irregularly formed and discontinuous than joints developed in the layered granofels composed of oligoclase or andesine, quartz, and variable amounts of hornblende, biotite, and Geological Survey 1954. 1000 0 1000 2000 3000 4000 5000 6000 7000 FEET Neoproterozoic rocks are those of the author and should not be interpreted gneisses and finer-grained crystalline rocks. Joints formed proximal to faults are typically closer and clinopyroxene. Locally contains thin layers of amphibolite (Ya). as necessarily representing the official policies, Northeast-striking (~N54°E, n = 9), dark greenish-gray, medium- to coarse-grained diabase dikes Hydrography Dataset Streams and Waterbodies, 2002. 1 .5 0 1 KILOMETE R spaced 2 ft. or less. either expressed or implied, of the U. S. Government. of Late Neoproterozoic age intrude Mesoproterozoic rocks throughout the quadrangle but not Cambri- Ylb Biotite-quartz-oligoclase gneiss (Mesoproterozoic) – White- or light-gray-weathering, medium-gray CONTOUR INTERVAL 20 FEET an or younger rocks. The dikes are as much as 15 ft. thick and have coarse-grained interiors and fine- The dominant strike of joints within the Mesoproterozoic rocks is nearly at a right angle to the trend or greenish-gray, medium- to coarse-grained, moderately well layered and foliated gneiss composed Polyconic projection. 1927 North American datum 10,000-foot grid based on New 1 Retired, New Jersey Geological and Water Survey grained to aphanitic chilled margins against Mesoproterozoic rocks. Very locally they display columnar of the crystallization foliation, a relationship that has been observed in Mesoproterozoic rocks through- of oligoclase or andesine, quartz, biotite, and trace amounts of garnet. Some outcrops contain horn- Jersey coordinate system, 1000-meter Universal Transverse Mercator grid ticks, cooling joints and contain xenoliths of Mesoproterozoic rocks. Diabase dikes were emplaced into a blende. Locally interlayered with amphibolite (Ya). zone 18. out the Highlands (Volkert, 1996). Consequently, the strike of joints in the map area displays some rift-related extensional tectonic setting in the Highlands at about 600 Ma (million years ago) during variability because of folding of the rocks. The mean strike of the dominant joint set is N56°W ± 8° (fig. breakup of the supercontinent Rodinia (Volkert and Puffer, 1995). 3) and dips mainly southwest and, less commonly, northeast. A subordinate joint set strikes northeast Yh Hypersthene-quartz-plagioclase gneiss (Mesoproterozoic) – Gray- or tan-weathering, greenish-gray about N45°E and dips with near equal abundance northwest and southeast. The dip of all joints ranges or greenish-brown, medium-grained, moderately well layered and foliated, greasy lustered gneiss com- 15 10 5 Mesoproterozoic rocks from 36° to 90° and averages 73°. posed of andesine or oligoclase, quartz, clinopyroxene, hornblende, and hypersthene. Commonly con- % Bedrock Geologic Map of the Stanhope Quadrangle The Stanhope quadrangle is predominantly underlain by Mesoproterozoic rocks that include a tains thin, conformable layers of amphibolite and mafic-rich quartz-plagioclase gneiss. heterogeneous assemblage of granite, gneisses of sedimentary and volcanic origin, and marble. Me- ECONOMIC RESOURCES 5 soproterozoic rocks were metamorphosed to granulite-facies conditions during the Grenvillian Orogeny Yd Diorite (Mesoproterozoic) – Light-gray- to tan-weathering, greenish-gray or greenish-brown, medium- to medium-coarse-grained, greasy lustered, massive, moderately foliated rock containing andesine or between 1045 and 1030 Ma (Volkert and others, 2010). The peak temperature calculated for this high- Mesoproterozoic rocks in the Stanhope quadrangle are host to numerous economic deposits of Morris and Sussex Counties, New Jersey oligoclase, augite, hornblende, hypersthene, and magnetite. Thin mafic layers or schlieren having the 10 grade metamorphism is 769°C from regional calcite-graphite thermometry (Peck and others, 2006). iron ore (low-Ti magnetite) mined mainly during the 18th and 19th centuries. Detailed descriptions of composition of amphibolite and leucocratic to mafic layers of quartz-oligoclase gneiss occur locally. these mines are given in Bayley (1910). In addition, several unnamed magnetite mines previously unre- 1 13 / 2° Among the oldest map units in the quadrangle are magmatic arc rocks of the Losee Suite that ported were discovered during the course of this mapping. The locations of all known mines in the map 15 include plutonic variants mapped as quartz-oligoclase gneiss and diorite gneiss, and volcanic rocks area are provided in a database available online through the New Jersey Geological and Water Survey. Other rocks MAGNETIC NORTH by TRUE NORT H mapped as biotite-quartz-oligoclase gneiss and hypersthene-quartz-plagioclase gneiss. Rocks of the Mesoproterozoic granite and marble were quarried at locations throughout the quadrangle, and granite Ya Amphibolite (Mesoproterozoic) – Grayish-black, fine- to medium-grained, moderately layered and fo- Yap 1 Losee Suite yielded sensitive high-resolution ion microprobe (SHRIMP) U-Pb zircon ages of 1282 to is currently quarried for crushed stone in the southern and northeastern parts of the map area. liated rock composed of hornblende and andesine (Ya). Most of the unit is associated with the supra- Richard A. Volkert 1248 Ma (Volkert and others, 2010). The Losee Suite is spatially and temporally associated with a suc- crustal succession and the Losee Suite and interpreted to be metavolcanic, although some amphibolite Sector angle = 10° cession of supracrustal rocks formed in a back-arc basin adjacent to the Losee magmatic arc. These that is intimately layered with pyroxene gneiss contains abundant clinopyroxene and titanite (Yap) and n = 993 2018 include felsic volcanic rocks of rhyolitic composition mapped as microcline gneiss and mafic volcanic may be metasedimentary in origin. Metavolcanic amphibolites are undifferentiated on the map. LOCATION IN APPROXIMATE MEAN rocks mapped as amphibolite, as well as metamorphosed sedimentary rocks mapped as potassic NEW JERSEY DECLINATION, 2006 Figure 2. Rose diagram showing the orientation of crys- feldspar gneiss, biotite-quartz-feldspar gneiss, pyroxene-quartz-feldspar gneiss, pyroxene gneiss, and Yu Mesoproterozoic rocks, undifferentiated – Shown in cross section only. tallization foliation in Mesoproterozic rocks. marble. Felsic volcanic rock from varied stratigraphic positions within the succession of supracrustal rocks yielded U-Pb zircon ages of 1299 to 1240 Ma (Volkert and others, 2010) that closely overlap the age of the Losee Suite.

N Tranquility Thrust Fault Tranquility Zero Fault Fault Wright Kennedys-East Fault Reservoir Fault Lake Hopatcong Brook Fault Turkey Ledgewood Fault Fault Longwood Valley Interstate 80 FEET FEET 10 8 6 % 2,000 2,000

Yk 1,000 _l Yh Sl 1,000 Ybh Ybh Yb 6 Ybh Ybs _h Ym Yfw Ya Ybs Yps 8 Ya Yb Ymp SEA LEVEL Ym Ylo Sg SEA LEVEL 10 O_bl Ybh Ybh Ya Ypg Ya Ybh Ybs Ypg Ypg Yps Ypg Yps Ypg Ylo Ym Ym Ya Ylo Yps a Ybs Ybs _l l Ybs Ypg Yps -1,000 -1,000 Sector angle = 10° h Ybs Ylo n = 1356 Yu _h Yps Yd Yk Ya Ybs Yu Yh Figure 3. Rose diagram showing the orientation of joints in -2,000 -2,000 Mesoproterozoic rocks.