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Prepared in cooperation with theU.S. GEOLOGICAL SURVEY

NATIONAL GEOLOGIC MAPPING PROGRAM

DEPARTMENT OF ENVIRONMENTAL PROTECTIONWATER RESOURCE MANAGEMENTNEW JERSEY GEOLOGICAL AND WATER SURVEY

BEDROCK GEOLOGIC MAP OF THE DOVER QUADRANGLE MORRIS AND SUSSEX COUNTIES, NEW JERSEY

OPEN FILE MAP SERIES OFM 91

LOCATION IN NEW JERSEY

by

Richard A. Volkert

2012

BEDROCK GEOLOGIC MAP OF THE DOVER QUADRANGLE MORRIS AND SUSSEX COUNTIES, NEW JERSEY

600050004000300020000 10001000 7000 FEET

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Base map U.S. Geological Survey, 1981 Bedrock geology mapped by R.A. Volkert in 1988, 2001, and 2002

Research supported by the U. S. Geological Survey, National CooperativeGeological Mapping Program, under USGS award number 99HQAG0141

The views and conclusions contained in this document are those of the authorand should not be interpreted as necessarily representing the official

policies, either expressed or implied, of the U. S. Government.

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Paleozoic geology adapted from G.C. Herman and J.P. Mitchell (1991)Digital cartography by M.W. Girard

INTRODUCTION

The Dover quadrangle is located in northern New Jersey in a mixed commercial, industrial and residen-tial setting. Development is fairly extensive south of Route 80, whereas large tracts of land to the north remain undeveloped. The quadrangle is in the Rockaway River watershed which constitutes the primary drainage.

The Dover quadrangle is situated in the central part of the New Jersey Highlands Physiographic Province and it is divided into western and eastern segments by the northeast-trending Green Pond Mountain Region (fig. 1). The topography of the central part of the quadrangle is dominated by a series of broad, linear, northeast-trending ridges (Green Pond and Copperas Mountains) and intervening stream valleys that are underlain by rocks of Paleozoic age. The linearity of the ridges and valleys is due to the uniform trend of the bedrock. The rest of the quadrangle is characterized by variably oriented ridges and stream valleys that reflect the greater structural complexity and nonlinear trend of the under-lying Mesoproterozoic bedrock. The maximum elevation in the map area is about 1,320 feet above sea level on Mase Mountain, east of Beaver Brook.

All of the bedrock in the map area has been affected by the effects of Pleistocene-age glaciation. The terminal moraine, which records the southernmost advance of glacial ice, trends roughly east-west through the southern part of the quadrangle, nearly coincident with Route 80. The distribution, thickness and composition of unconsolidated glacial deposits in the map area is discussed by Stanford (1989).

STRATIGRAPHY

Paleozoic rocksThe youngest bedrock in the map area is in the Green Pond Mountain Region, a northeast-trending block of downfaulted and folded sedimentary rocks of Paleozoic age that extends diagonally through the central part of the map. From oldest to youngest, Paleozoic formations include the Hardyston Quartzite and Leithsville Formation of Cambrian age, Green Pond Conglomerate, Longwood Shale, Poxino Island, and Berkshire Valley Formations of Silurian age, and the Connelly Conglomerate, Esopus Formation, Kanouse Sandstone, Cornwall Shale, Bellvale Sandstone and Skunnemunk Conglomerate of Devonian age. The Hardyston and Leithsville are rarely exposed in the quadrangle but are known from borings and water-well records. These formations also crop out to the immediate southwest of the map area. The origin and stratigraphic relationships of the Paleozoic formations in the Green Pond Mountain Region is discussed in Darton (1894), Kummel and Weller (1902), and Barnett (1970).

Neoproterozoic rocksDiabase dikes of Neoproterozoic age intrude Mesoproterozoic rocks in the northwest part of the map near Woodport, at Hurdtown, and along the southern end of Mase Mountain. The dikes range in width from a few inches to as much as 30 ft., and they strike toward the east, northeast, or northwest. They have coarse-grained interiors and fine-grained to aphanitic chill margins and sharp contacts against enclosing Mesoproterozoic rocks. Locally the dikes display columnar jointing and contain xenoliths of Mesoproterozoic rocks. Diabase dikes are interpreted as having been emplaced in a rift-related, exten-sional tectonic setting in the Highlands at about 600 Ma during breakup of the supercontinent Rodinia (Volkert and Puffer, 1995).

Mesoproterozoic rocks Most of the quadrangle is underlain by rocks of Mesoproterozoic age of the New Jersey Highlands. These include a heterogeneous assemblage of granites and gneisses that were metamorphosed to granulite facies at ca.1050 to 1030 Ma (Volkert et al., 2010). Temperature estimates for this high-grade metamorphism are constrained from regional calcite-graphite thermometry to ~769 C (Peck et al., 2006) and from biotite thermometry to ~754 C (Volkert, 2006).

Among the oldest map units in the quadrangle are calc-alkaline, plagioclase-rich rocks of the Losee Suite (Drake, 1984; Volkert and Drake, 1999) that were formed in a continental-margin magmatic arc (Volkert, 2004). These include rocks mapped as quartz-oligoclase gneiss, biotite-quartz-oligoclase gneiss, hypersthene-quartz-plagioclase gneiss, amphibolite, diorite, and albite-oligoclase alaskite formed from plutonic and volcanic protoliths (Volkert and Drake, 1999; Volkert, 2004). Representative samples of the Losee Suite from elsewhere in the Highlands yield sensitive high-resolution ion micro-probe (SHRIMP) U-Pb zircon ages of 1282 to 1248 Ma (Volkert et al., 2010).

Magmatic arc rocks of the Losee Suite are spatially and temporally associated with a succession of supracrustal rocks formed in a back-arc basin (Volkert, 2004). These include a bimodal suite of rhyolitic gneiss mapped as potassic feldspar gneiss and mafic volcanic rock mapped as amphibolite, as well as metasedimentary rocks mapped as biotite-quartz-feldspar gneiss, hornblende-quartz-feldspar gneiss, clinopyroxene-quartz-feldspar gneiss, and pyroxene gneiss. Supracrustal rocks from elsewhere in the Highlands yield SHRIMP U-Pb zircon ages of 1299 to 1251 Ma (Volkert et al., 2010).

Other Mesoproterozoic rocks in the quadrangle of uncertain age include biotite-plagioclase gneiss and hornblende-plagioclase gneiss. Biotite-plagioclase gneiss forms thin layers on Mase Mountain interpreted as sills formed from an anorthosite protolith (Young, 1969; Young and Icenhower, 1989). Hornblende-plagioclase gneiss crops out in two bodies southwest of Mase Mountain. This unit is also interpreted as formed from a anorthosite protolith (Young, 1969; Gorring and Volkert, 2004).

The quadrangle also contains voluminous granite and related rocks of the Byram and Lake Hopatcong Intrusive Suites that comprise the Vernon Supersuite (Volkert and Drake, 1998). Rocks of these suites include monzonite, quartz monzonite, granite, and alaskite. These suites are well exposed throughout the map area where they have intruded rocks of the Losee Suite and supracrustal rocks. Byram and Lake Hopatcong rocks have a characteristic A-type geochemical composition (Volkert et al., 2000). Granite of both suites yields similar SHRIMP U-Pb ages of 1188 to 1182 Ma (Volkert et al., 2010).

The youngest Mesoproterozoic rocks are small, irregular, bodies of granite pegmatite that are unfoliated and have intruded other Mesoproterozoic rocks. Most of these occur in bodies that are too small to be shown on the map. Pegmatites elsewhere in the Highlands yield U-Pb zircon ages of 1004 to 987 Ma (Volkert et al., 2005).

Other Mesoproterozoic rock in the quadrangle includes amphibolite of several different origins. Most amphibolite associated with the Losee Suite is metavolcanic, whereas amphibolite intercalated with the supracrustal gneisses may be metavolcanic or metasedimentary in origin. All types of amphibolite are undifferentiated on the map, and most occurrences are too small to be shown.

STRUCTURE

Paleozoic beddingBedding in the Paleozoic formations of the Green Pond Mountain Region is fairly uniform and strikes at an average of N.42 E. (fig. 2). Most beds are upright and dip northwest and less commonly southeast. Locally beds are overturned steeply southeast. Beds range in dip from 9 to 90 and average 60 .

Proterozoic foliationCrystallization foliation in the Mesoproterozoic rocks (formed by the parallel alignment of constituent mineral grains) strikes predominantly northeast at an average of N.39 E. (fig. 3). Foliations locally are somewhat varied in strike, especially in the west-central part of the quadrangle, owing to the folds of all scale, from outcrop to major regional extent. Foliations dip mainly southeast and very locally dip north-west, although in the hinge areas of fold structures dips are gentle to moderate toward the north. Dips range from 20 to 90 and average 62 .

FoldsFolds in the Paleozoic rocks are dominated by a major regional synclinorium in the Green Pond Moun-tain Region. Beds on Copperas Mountain form an asymmetric, northeast-plunging upright syncline (Herman and Mitchell, 1991), the axis of which extends just west of the ridge crest. Beds on the west limb dip gently to moderately, whereas beds on the east limb dip steeply to vertically. The pattern of folding on Green Pond Mountain is more complex and consists of both upright and overturned synclines and anticlines.

Characteristic fold styles in the Mesoproterozoic rocks consist of northeast-plunging and northwest-overturned to northeast-plunging and upright antiforms and synforms. The plunge of mineral lineations and fold axes is parallel and averages 18 . The plunge trend ranges from N.23 E. to N.76 E. and averages N.52 E., with nearly 60 percent of all lineations plunging from N.45 E. to N.54 E. No southwest plunging lineations or folds were recognized. The overall sequence of folding is uncertain. It may be a continuum of the same fold phase that resulted from differences in the vector of compressional stress. Regardless, the folds clearly predate the development of folds in the Paleozoic rocks of the quadrangle and thus are of Mesoproterozoic age.

FaultsNortheast-trending faults are the most common in the Dover quadrangle and they deform both Mesopro-terozoic and Paleozoic rocks. Some of the wider fault zones are possibly due to the interaction of several smaller parallel or anastomosing faults, rather than consisting of a single, discrete fault. From the north-west, the major faults are the Reservoir, Ledgewood, Longwood Valley, Berkshire Valley, Picatinny, Tanners Brook-Green Pond, and Gorge fault, that partition the map area into a series of structural blocks (fig. 1). In the Mesoproterozoic rocks, these faults are characterized by brittle deformation fabric that consists of breccia, gouge, retrogression of mafic mineral phases, chlorite or epidote-coated fractures or slickensides, and (or) close-spaced fracture cleavage.

The Reservoir fault has a strike length of about 37 miles, extending from New York State southwest to Schooleys Mountain (Drake et al., 1996). Along its northern end, the fault has Paleozoic rocks on the hanging wall and Mesoproterozoic rocks on the footwall, but in the map area, and along strike to the south, it contains Mesoproterozoic rocks on both the hanging wall and footwall blocks. The Reservoir fault strikes about N.40 E. and ranges in dip from steep northwest or southeast to 90 . The fault records a history of multiple reactivations dating from the Mesoproterozoic involving normal, strike slip, and reverse movement, with latest movement having been normal (east side down). The Reservoir fault is characterized by ductile deformation fabric in the center of the fault zone, overprinted by a pervasive brittle deformation fabric that envelops the mylonite on both sides of the fault zone over a total width of as much as 1,000 ft.

The Ledgewood fault has a strike length of about 10 miles. South of the map area it merges with, or is cut off by, the Longwood Valley fault, and within the area it is cut off by the Reservoir fault north of Lake

EXPLANATION OF MAP SYMBOLS

Contact - Dotted where concealed

Faults - Dotted where concealed. Arrow indicates dip direction and attitude, where known.

Normal fault - U, upthrown side; D, downthrown side Reverse fault - U, upthrown side; D, downthrown side

FOLDS

Folds in Paleozoic rocks showing trace of axial surface, direction of dip of limbs, and direction of plunge

Syncline

Anticline

Folds in Proterozoic rocks showing trace of axial surface, direction of dip of limbs, and direction of plunge

Synform

Antiform Overturned Synform

Overturned Antiform

PLANAR FEATURES

Strike and dip of beds

Inclined

Vertical

Overturned Strike and dip of crystallization foliation

Inclined

Vertical

Strike and dip of mylonitic foliation

LINEAR FEATURES

Bearing and plunge of mineral lineation in Proterozoic rocks

OTHER FEATURES Active rock quarry

Abandoned rock quarry

Abandoned magnetite mine Drill hole – Rock type at bottom: G, granite; D, dolomite; Q, quartzite

Form lines showing foliation in Proterozoic rocks. Shown in cross section only

REFERENCES CITED AND USED IN CONSTRUCTION OF MAP

Barnett, S.G., III, 1970, Upper Cayugan and Helderbergian stratigraphy of southeastern New York and northern New Jersey: Geological Society of America Bulletin, v. 81, p. 2375-2402._______, 1976, Geology of the Paleozoic rocks of the Green Pond outlier: New Jersey Geological Survey, Geologic Report Series No. 11, 9p.Bayley, W.S., 1910, Iron mines and mining in New Jersey: New Jersey Geological Survey, Final Report Series, v. 7, 512p. Boucot, A.J., 1959, Brachiopods of the Lower Devonian rocks at Highland Mills, New York: Journal of Paleontology, v. 33, p. 727-769.Chadwick, H.G., 1908, Revision of “the New York series”: Science, new series, v. 28, p. 346-348.Darton, N.H., 1894, Geologic relations from Green Pond, New Jersey, to Skunnemunk Mountain, New York: Geological Society of America Bulletin, v. 5, p. 367-394.Drake, A.A., Jr., 1984, The Reading Prong of New Jersey and eastern Pennsylvania-An appraisal of rock relations and chemistry of a major Proterozoic terrane in the Appalachians, in Bartholomew, M.J., ed., The Grenville event in the Appalachians and related topics: Geological Society of America Special Paper 194, p. 75-109.Drake, A.A., Jr., and Volkert, R.A., 1991, The Lake Hopatcong Intrusive Suite (Middle Proterozoic) of the New Jersey Highlands, in Drake, A.A., Jr., ed., Contributions to New Jersey Geology: U.S. Geological Survey Bulletin 1952, p. A1-A9.Drake, A.A., Jr., Volkert, R.A., Monteverde, D.H., Herman, G.C., Houghton, H.F., Parker, R.A., and Dalton, R.F., 1996, Bedrock Geologic Map of Northern New Jersey: U.S. Geological Survey Miscellaneous Investigations Series Map I-2540-A, scale 1:100,000.Gorring, M.L., and Volkert, R.A., 2004, Possible AMCG-related megacrystic amphibolites and meta-anorthosite sheets in the New Jersey Highlands: Geological Society of America Abstracts with Programs, v. 36, p. 51.Hartnagel, C.A., 1907, Upper Siluric and Lower Devonic formations of the Skunnemunk Mountain region: New York State Museum Bulletin 107, p. 39-54.Herman, G.C., and Mitchell, J. P., 1991, Bedrock geologic map of the Green Pond Mountain Region from Dover to Greenwood Lake, New Jersey: New Jersey Geological Survey Geologic Map Series 91-2, scale 1:24,000.Klemic, H., Heyl, A.V., Jr., Taylor, A.R., and Stone, J., 1959, Radioactive rare-earth deposit at Scrub Oaks mine, Morris County, New Jersey: U.S. Geological Survey Bulletin 1082-B, p. 29-59.Kummel, H.B., 1908, Paleozoic sedimentary rocks of the Franklin furnace quadrangle, New Jersey, in Spencer, A.C., Kummel, H.B., Salisbury, R.D., Wolff, J.E., and Palache, Charles, Description of the Franklin furnace quadrangle, New Jersey: U.S. Geological Survey Atlas Folio 161, p. 10-12.Kummel, H.B., and Weller, Stuart, 1902, The rocks of the Green Pond Mountain region: New Jersey Geological Survey Annual Report 1901, p. 1-51.Peck, W.H., Volkert, R.A., Meredith, M.T., and Rader, E.L., 2006, Calcite-graphite thermometry of the Franklin Marble, New Jersey Highlands: Journal of Geology, v. 114, p. 485-499.Rogers, H.D., 1836, Report on the geological survey of the State of New Jersey: Philadelphia, Desilver, Thomas, & Co., 174 p.Sims, P.K., 1958, Geology and magnetite deposits of Dover District, Morris County, New Jersey: U.S. Geological Survey Professional Paper 287, 162 p.Stanford, S.D., 1989, Surficial geology of the Dover quadrangle, Sussex and Morris County, New Jersey: New Jersey Geological Survey Map 89-2, scale 1:24,000.Vanuxem, Lardner, 1842, Geology of New York, part III, comprising the survey of the third geological district: Albany, N.Y., 306p.Volkert, R.A., 1996, Geologic and engineering characteristics of Middle Proterozoic rocks of the Highlands, northern New Jersey, in Engineering geology in the metropolitan environment: Field Guide and Proceedings of the 39th annual meeting of the Association of Engineering Geologists, p. A1-A33._______, 2004, Mesoproterozoic rocks of the New Jersey Highlands, north-central Appalachians: petro genesis and tectonic history, in Tollo, R.P., Corriveau, L., McLelland, J., and Bartholomew, J., eds., Proterozoic tectonic evolution of the Grenville orogen in North America: Geological Society of America Memoir 197, p. 697-728. _______, 2006, New discovery of Mesoproterozoic high-magnesium orthoamphibole gneiss in the Grenville of the New Jersey Highlands: Geological Society of America Abstracts with Programs, v. 38, No. 7, p. 385.Volkert, R.A., Aleinikoff, J.N., and Fanning, C.M., 2010, Tectonic, magmatic, and metamorphic history of the New Jersey Highlands: New insights from SHRIMP U-Pb geochro nology, in Tollo, R.P., Bartholomew, M.J., Hibbard, J.P., and Karabinos, P.M., eds., From Rodinia to Pangea: The Lithotectonioc Record of the Appalachian Region, Geological Society of America Memoir 206, p. 307-346.Volkert, R.A., and Drake, A.A., Jr., 1998, The Vernon Supersuite: Mesoproterozoic A-type granitoid rocks in the New Jersey Highlands: Northeastern Geology and Environmental Sciences, v. 20, p. 39-43.________, 1999, Geochemistry and stratigraphic relations of Middle Proterozoic rocks of the New Jersey Highlands, in Drake, A.A., Jr., ed., Geologic Studies in New Jersey and eastern Pennsylvania: U.S. Geological Survey Professional Paper 1565C, 77p.Volkert, R.A., Feigenson, M.D., Patino, L.C., Delaney, J. S., and Drake, A.A., Jr., 2000, Sr and Nd isotopic compositions, age and petrogenesis of A-type granitoids of the Vernon Supersuite, New Jersey Highlands, USA: Lithos, v. 50, p. 325-347.Volkert, R.A., Markewicz, F.J., and Drake, A.A., Jr., 1990, Bedrock geologic map of the Chester quad rangle, Morris County, New Jersey: New Jersey Geological Survey, Geologic Map Series 90-1, scale 1:24,000.Volkert, R.A., and Puffer, J.H., 1995, Late Proterozoic diabase dikes of the New Jersey Highlands- A remnant of Iapetan rifting in the north-central Appalachians, in Drake, A.A., Jr., ed., Geologic studies in New Jersey and eastern Pennsylvania: U.S. Geological Survey Professional Paper 1565-A. 22p.Volkert, R.A., Zartman, R.E., and Moore, P.B., 2005, U-Pb zircon geochronology of Mesoproterozoic postorogenic rocks and implications for post-Ottawan magmatism and metal logenesis, northern New Jersey Highlands and contiguous areas, USA: Precambrian Research, v. 139, p. 1-19 Wherry, E.T., 1909, The early Paleozoic of the Lehigh Valley district, Pennsylvania: Science, new series, v. 30, 416p.White, I.C., 1882, The geology of Pike and Monroe Counties: Pennsylvania Geological Survey, 2nd series, Report G-6, 407p.Willard, Bradford, 1937, Hamilton correlations: American Journal of Science, 5th series, v. 33, p. 264-278.Wolff, J.E., and Brooks, A.H., 1898, The age of the Franklin white limestone of Sussex County, New Jersey: U.S. Geological Survey 18th Annual Report, pt. 2, p. 425-457.Young, D.A., 1969, Petrology and structure of the west-central New Jersey Highlands: Providence, Rhode Island, Brown University, unpublished Ph.D. dissertation, 194p.Young, D.A., and Icenhower, J.P., 1989, A metamorphosed anorthosite sill in the New Jersey Highlands: Northeastern Geology, v. 11, p. 56-64

Shawnee. The Ledgewood fault strikes about N.25 E. and dips steeply southeast at about 70 . It contains Mesoproterozoic rocks on both sides along its entire length. Latest movement on the fault appears to have been dip-slip normal. The Ledgewood fault is characterized by a zone of brittle deformation fabric that is 200 to 300 ft. wide.

The Longwood Valley fault has a strike length of nearly 40 miles, extending from Oak Ridge Reservoir south to the vicinity of High Bridge where it is cut off by a segment of the border fault (Drake et al., 1996). Along much of its length the fault contains Mesoproterozoic rocks on the footwall and Paleozoic rocks on the hanging wall. In the map area, the fault strikes about N.45 E. and dips steeply northwest to vertically. The fault is characterized by brittle deformational fabric along its entire length. Kinematic indicators suggest that latest movement on the Longwood Valley fault was predominantly reverse, although south of the map area the fault dips southeast and dip-slip normal movement is predominant.

The northeast-trending Berkshire Valley fault is not exposed in the map area, and its occurrence was inferred by Herman and Mitchell (1991) on the basis of missing stratigraphic units between the Green Pond Conglomerate and Cornwall Shale in the Berkshire Valley. This fault has a strike length of more than 8 miles, extending along the northwest side of Green Pond Mountain southwestward where it is cut off by the Longwood Valley fault. The Berkshire Valley fault contains Paleozoic rocks on both sides along its entire length. It strikes about N.40 E. and dips southeast at about 45 . The latest movement appears to have been reverse. The fault is characterized by a zone of brittle fabric of indeterminate width. The northeast-trending Picatinny fault has a strike length of more than 11 miles, extending along the south-east side of Green Pond Mountain (Herman and Mitchell, 1991). The fault contains Paleozoic rocks on both sides along most of its length except for a short segment near Picatinny Lake, where Mesoprotero-zoic rocks are on the hangingwall. Leithsville Formation is on the hanging wall and Green Pond Conglom-erate on the footwall along most of the length of the fault. The Picatinny fault strikes N.40 E. and dips southeast at about 50 . Latest movement appears to have been reverse. The fault is characterized by a zone of brittle fabric that has a total width of as much as a few hundred feet.

The Tanners Brook-Green Pond fault is a structure resulting from the merger of the Green Pond fault, that extends along the northwest side of Copperas Mountain from near Newfoundland to Picatinny Lake (Kummel and Weller, 1902; Barnett, 1976; Herman and Mitchell, 1991), and the Tanners Brook fault that extends from Picatinny Lake southwest to Califon where it bounds the south side of Long Valley (Volkert et al., 1990). The combined fault has a length of about 30 miles. It contains mainly Paleozoic rocks on both sides to the north and Mesoproterozoic rocks on both sides from Chester southwest to Califon. The fault strikes N.40 E. and dips northwest at about 75 . Latest movement on the fault in the map area was predominantly reverse. The Tanners Brook-Green Pond fault is characterized by a zone of brittle fabric 300 to 400 ft. wide. The Gorge fault is a newly recognized structure that is named for the prominent gorge at Picatinny Arsenal. The fault has a strike length of about 6 miles, extending along the southeast side of Green Pond Mountain north to Newfoundland. The Gorge fault appears to be cut off on both ends by the Tanners Brook-Green Pond fault. The Gorge fault contains Mesoproterozoic rocks on the hanging wall and Green Pond Conglomerate on the footwall. The fault strikes N.40 E. and dips about 60 southeast. Latest move-ment appears to have been reverse. The fault is characterized by ductile deformation fabric that is overprinted by strong brittle fabric over a total width of about 500 ft.

Mesoproterozoic rocks throughout the map area are also deformed by smaller, more localized faults. These northeast-trending or northwest-trending faults have widths of not more than a few tens of feet. Northwest-trending cross faults dip toward the south at about 50 to nearly vertical. Most of these faults are not exposed and are known from the subsurface offset of the orebodies in magnetite mines (Bayley, 1910; Sims, 1958).

JointsJoints are a common feature in the Paleozoic and Mesoproterozoic rocks of the quadrangle. They are characteristically planar, moderately well formed, and moderately to steeply dipping. Their surfaces are typically unmineralized, except near faults, and are smooth, and less commonly, slightly irregular. Joints are variably spaced from a ft. to tens of ft. Those developed in massive rocks such as Mesoproterozoic granite or Paleozoic conglomerate and quartzite tend to be more widely spaced, irregularly formed and discontinuous than joints developed in the Mesoproterozoic layered gneisses and finer-grained Paleozoic rocks. Joints formed near faults have a spacing of 2 ft. or less. The dominant joint trend in the Mesoproterozoic rocks is nearly perpendicular to the strike of crystallization foliation, and this relationship is a consistent feature in Mesoproterozoic rocks throughout the Highlands (Volkert, 1996). Consequently, joint trends in the map area are somewhat varied because of folding of Mesoproterozoic rocks. The dominant joint set strikes northwest at an average of N.54 W. (fig. 4). Joints of this set dip southwest at an average of 73 . A subordinate joint set strikes about N.42 E. (fig. 4) and dips gently to moderately northwest. Within the Paleozoic rocks, northwest-trending cross joints are the most common. These joints strike at an average of N.40 W. (fig. 5) and dip nearly equally northwest and southeast at about 50 .

ECONOMIC RESOURCESSome Mesoproterozoic rocks in the quadrangle were host to economic deposits of magnetite (iron ore) mined predominantly during the 19th century. Detailed descriptions of the mines are given in Bayley (1910) and Sims (1958). Iron mines are distributed throughout the quadrangle, but the most economically important ones are in the south-central part in the Mount Hope district. The Mount Hope and Scrub Oaks mines were among the largest of these. The latter was especially notable for the presence of rare-earth elements in the deposit (Klemic et al., 1959).

Mesoproterozoic rocks in the map area are currently being quarried for crushed stone at Woodport and Mount Hope, and were formerly quarried for crushed stone on a small scale at Picatinny Arsenal. Green Pond Conglomerate was formerly quarried at Roxbury. Deposits of sand and gravel are being mined at Kenvil, and were formerly worked at various locations (Stanford, 1989).

DESCRIPTION OF MAP UNITS

GREEN POND MOUNTAIN REGION

Bellvale Sandstone (Middle Devonian) (Bellvale Flags of Darton, 1894; Willard, 1937) –Upper beds are grayish-red to grayish-purple sandstone containing quartz pebbles as much as 1 in. in diameter. Lower beds are light-olive-gray to yellowish-gray- and greenish-black-weathering, medium-gray to medium-bluish-gray, very thin to very thick-bedded siltstone and sandstone crossbedded, graded, and interbedded with black to dark-gray shale. More sand-stone occurs in upper beds and becomes finer downward. Lower contact conformable with the Cornwall Shale and placed where beds thicken and volume of shale and siltstone is about equal. Unit is 1,750 to 2,000 ft. thick.

Cornwall Shale (Middle Devonian) (Hartnagel, 1907) – Black to dark-gray, very thin to thick-bedded, fossiliferous, fissile shale, interbedded with medium-gray and light-olive-gray to yellowish-gray, laminated to very thin bedded siltstone that increases in upper part. Lower contact with Kanouse Sandstone probably conformable. Unit is about 950 ft. thick.

Kanouse Sandstone, Esopus Formation and Connelly Conglomerate, undivided (Lower Devonian) Kanouse Sandstone (Kummel, 1908) – Medium-gray, light-brown, and grayish-red, fine- to coarse-grained, thin to thick-bedded sandstone and pebble conglomerate. Basal conglomer-ate is interbedded with siltstone and contains well-sorted, subangular to subrounded, gray and white quartz pebbles less than 0.4 in. long. Lower contact with Esopus Formation grada-tional. Unit is about 46 ft. thick.

Esopus Formation (Vanuxem, 1842; Boucot, 1959) – Light to dark-gray, laminated to thin-bedded siltstone interbedded with dark-gray to black mudstone, dusky-blue sandstone and siltstone, and yellowish-gray, fossiliferous siltstone and sandstone. Lower contact prob-ably conformable with Connelly Conglomerate. Unit is about 180 ft. thick.

Connelly Conglomerate (Chadwick, 1908) – Grayish-orange-weathering, very light gray to yellowish-gray, thin-bedded quartz-pebble conglomerate. Quartz pebbles are subrounded to well rounded, well sorted, and as much as 0.8 in. long. Unit is about 36 ft. thick.

Berkshire Valley and Poxino Island Formations, undivided (Upper Silurian) Berkshire Valley Formation (Barnett, 1970) – Yellowish-gray-weathering, medium-gray to pinkish-gray, very thin to thin-bedded fossiliferous limestone interbedded with gray to greenish-gray calcareous siltstone and silty dolomite, medium-gray to light-gray dolomite conglomerate, and grayish-black thinly laminated shale. Lower contact conformable with Poxino Island Formation. Unit ranges in thickness from 90 to 125 ft.

Poxino Island Formation (White, 1882; Barnett, 1970) – Very thin to medium-bedded sequence of medium-gray, greenish-gray, or yellowish-gray, mud-cracked dolomite; light-green, pitted, medium-grained calcareous sandstone, siltstone, and edgewise conglomerate containing gray dolomite; and quartz-pebble conglomerate containing angular to subangular pebbles as much as 0.8 in. long. Interbedded grayish-green shale at lower contact is transi-tional into underlying Longwood Shale. Unit ranges in thickness from 160 to 275 ft.

Longwood Shale (Upper and Middle Silurian) (Darton, 1894) – Dark reddish-brown, thin to very thick-bedded shale interbedded with cross-bedded, very dark-red, very thin to thin-bedded sandstone and siltstone. Lower contact is conformable with Green Pond Conglomerate. Unit is 330 ft. thick.

Green Pond Conglomerate (Middle and Lower Silurian) (Rogers, 1836) – Medium to coarse-grained quartz-pebble conglomerate, quartzitic arkose and orthoquartzite, and thin to thick-bedded reddish-brown siltstone. Grades downward into less abundant gray, very dark red, or grayish-purple, medium to coarse-grained, thin to very-thick-bedded pebble to cobble conglomerate containing clasts of red shale, siltstone, sandstone, and chert; yellowish-gray sandstone and chert; dark-gray shale and chert; and white-gray and pink milky quartz. Quartz cobbles are as much as 4 in. long. Unconformably overlies the Leithsville Formation or Meso-proterozoic rocks in the map area. Unit is about 1,000 ft. thick.

Leithsville Formation (Middle and Lower Cambrian) (Wherry, 1909) – Light to dark-gray and light-olive-gray, fine to medium-grained, thin to medium-bedded dolomite. Grades down-ward through medium-gray, grayish-yellow, or pinkish-gray dolomite and dolomitic sand-stone, siltstone, and shale to medium-gray, medium-grained, medium-bedded dolomite containing quartz sand grains as stringers and lenses near the base. Lower contact grada-tional with Hardyston Quartzite. Approximately 800 ft thick regionally.

Hardyston Quartzite (Lower Cambrian) (Wolff and Brooks, 1898) – Light to medium-gray and bluish-gray conglomeratic sandstone. Varies from pebble conglomerate, to fine-grained, well-cemented quartzite, to arkosic or dolomitic sandstone. Conglomerate contains subangu-lar to subrounded white quartz pebbles as much as 1 in. long. Lower contact unconformable with Mesoproterozoic rocks. Unit ranges from 0 to 30 ft. thick regionally.

NEW JERSEY HIGHLANDS

Diabase dikes (Neoproterozoic) (Volkert and Puffer, 1995) – Light-gray to brownish-gray-weathering, dark-greenish-gray, aphanitic to fine-grained dikes that intrude Mesoproterozoic rocks but not Paleozoic cover rocks. Composed principally of labradorite to andesine, augite, and ilmenite and (or) magnetite. Pyrite blebs are common. Contacts are chilled and sharp against enclosing Mesoproterozoic rocks. Dikes are as much as 30 ft. wide and a mile or more long.

Vernon Supersuite (Volkert and Drake, 1998)Byram Intrusive Suite (Drake, 1984)

Hornblende granite (Mesoproterozoic) – Pinkish-gray or buff-weathering, pinkish-white or light-pinkish-gray, medium- to coarse-grained, massive, foliated granite and sparse granite gneiss composed of mesoperthite, microcline microperthite, quartz, oligoclase, and hasting-site. Common accessory minerals include zircon, apatite and magnetite. Contains small bodies of pegmatite too small to be shown.

Microperthite alaskite (Mesoproterozoic) – Pale pinkish-white- or buff-weathering, pinkish-white, medium- to coarse-grained, massive, foliated rock composed of microcline microperthite, quartz, oligoclase, and trace amounts of hastingsite, biotite, zircon, apatite, and magnetite.

Lake Hopatcong Intrusive Suite (Drake and Volkert, 1991)

Pyroxene granite (Mesoproterozoic) – Buff or white-weathering, greenish-gray, medium to coarse-grained, foliated granite containing mesoperthite to microantiperthite, quartz, oligoclase, and hedenbergite. Common accessory minerals include titanite, magnetite, apatite, and trace amounts of zircon and pyrite.

Pyroxene monzonite (Mesoproterozoic) – Gray, buff, or tan-weathering, greenish-gray, medium to coarse-grained, massive, moderately to indistinctly foliated syenite to monzonite. Composed of mesoperthite, microantiperthite to microcline microperthite, oligoclase, heden-bergite, titanite, magnetite, and apatite. Locally contains sparse quartz and (or) hornblende.

Pyroxene alaskite (Mesoproterozoic) – Buff or white-weathering, greenish-buff or light pinkish-gray, medium- to coarse-grained, massive, foliated rock composed of mesoperthite to microantiperthite, quartz, oligoclase, and sparse amounts of hedenbergite. Common acces-sory minerals include titanite, magnetite, apatite, and zircon.

Supracrustal Rocks

Potassic feldspar gneiss (Mesoproterozoic) – Buff or pale pinkish-white-weathering, buff, pale pinkish-white or light-pinkish-gray, medium-grained, massive, foliated gneiss composed of quartz, microcline microperthite, oligoclase, biotite, and magnetite. Garnet and sillimanite occur locally.

Biotite-quartz-feldspar gneiss (Mesoproterozoic) – Pale pinkish-white, pinkish-gray, or gray-weathering, locally rusty-weathering, pinkish-gray, tan, or greenish-gray, fine to coarse-grained, moderately layered and foliated gneiss containing microcline microperthite, oligoclase, quartz, biotite, and garnet. Very locally contains kornerupine. Graphite and pyrrhotite are confined to the variant that weather rusty. The rusty variant is commonly associ-ated with thin, layered quartzite containing biotite, feldspar, graphite, and pyrrhotite.

Hornblende-quartz-feldspar gneiss (Mesoproterozoic) – Pinkish-gray or buff-weathering, pinkish-gray or pinkish-white, medium-grained, layered and foliated gneiss composed of microcline, quartz, and hornblende. Locally contains biotite, garnet and magnetite.

Clinopyroxene-quartz-feldspar gneiss (Mesoproterozoic) – Pinkish-gray or pinkish-buff-weathering, white, pale-pinkish-white or light-gray, medium to coarse-grained, foliated gneiss composed of microcline, quartz, oligoclase, diopside, and trace amounts of titanite, magne-tite, biotite, and epidote.

Pyroxene gneiss (Mesoproterozoic) – Light-gray or white-weathering, greenish-gray or light-greenish-gray, medium-grained, layered and foliated gneiss containing oligoclase, diopside, varied amounts of quartz and titanite, and trace amounts of magnetite and epidote. Locally interlayered with clots and layers of dark-green, medium to coarse-grained diopsidite composed almost entirely of diopside. West of Longwood Lake unit is interlayered with light-gray or light greenish-gray, layered and foliated quartz-epidote gneiss.

Magmatic Arc Rocks

Losee Metamorphic Suite (Drake, 1984; Volkert and Drake, 1999)

Quartz-oligoclase gneiss (Mesoproterozoic) – White-weathering, light-greenish-gray, medium to coarse-grained, layered to massive, foliated gneiss composed of oligoclase or andesine, quartz, and varied amounts of hornblende, augite, biotite, and magnetite. Locally contains layers of amphibolite too thin to be shown. Commonly has gradational contacts with biotite-quartz-oligoclase gneiss and hypersthene-quartz-plagioclase gneiss. Locally forms thin, conformable layers within diorite.

Biotite-quartz-oligoclase gneiss (Mesoproterozoic) – Light-gray-weathering, light-greenish-gray, medium to coarse-grained, layered and foliated gneiss composed of oligoclase or andesine, quartz, biotite, and local hornblende. Locally contains conformable layers of amphibolite.

Albite-oligoclase alaskite (Mesoproterozoic) – Pale pink, or white-weathering, light-greenish-gray or light-pinkish-green, medium to coarse-grained, foliated rock composed of albite or oligoclase, quartz, and variable amounts of hornblende, augite and magnetite. Locally contains rutile. Commonly contains conformable layers of amphibolite.

Hypersthene-quartz-plagioclase gneiss (Mesoproterozoic) – Light-gray or tan-weathering, greenish-gray or greenish-brown, medium-grained, moderately layered and foliated, greasy lustered gneiss composed of andesine or oligoclase, quartz, augite, hornblende, hypersthene, and magnetite. Commonly contains conformable layers of amphibolite and quartz-plagioclase gneiss containing hornblende and augite.

Diorite (Mesoproterozoic) – Light-gray or tan-weathering, greenish-gray or greenish-brown, medium-grained, greasy lustered, massive, foliated rock containing andesine or oligoclase, augite, hornblende, hypersthene, and magnetite. Thin mafic layers having the composition of amphibolite and leucocratic to mafic layers of quartz-oligoclase gneiss occur locally.

Other Rocks

Amphibolite (Mesoproterozoic) – Grayish-black-weathering, black or grayish-black, medium-grained gneiss composed of hornblende, andesine, and magnetite. Some variants contain biotite and others contain augite and local hypersthene. Amphibolite associated with the Losee Suite is metavolcanic in origin and that associated with supracrustal rocks may be metavolcanic or metasedimentary. All types are undifferentiated on the map.

Biotite-plagioclase gneiss (Mesoproterozoic) – White or light-gray-weathering, greenish-gray, medium-grained, foliated gneiss composed of biotite, plagioclase, and varied amounts of hornblende, clinopyroxene, and garnet.

Hornblende-plagioclase gneiss (Mesoproterozoic) – White or light-gray-weathering, greenish-gray, medium- to coarse-grained, foliated rock containing hornblende, plagioclase, and local clinopyroxene, apatite, and magnetite.

Mesoproterozoic rocks, undifferentiated – Shown in cross section only.

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Figure 5. Rose diagram of 138 joint orientations in Paleozoic rocks

Figure 4. Rose diagram of 861 joint orientations in Mesoproterozoic rocks

Figure 3. Rose diagram of 760 crystallization foliation orientations in Mesoproterozoic rocks

Figure 2. Rose diagram of 116 bedding orientations in Paleozoic rocks

Mean trend = N.42 E.Sector size = 10n = 116

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Supracrustal Rocks

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Figure 1. Simplified map of the Dover quadrangle showing locations of the principal structural blocks and the faults that bound them.

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