41 o 07'30'' 74 o 30' 10' 74 o 30' 41 o 15' 27' 30'' 41 o 15' 74 o 22'30'' Prepared in cooperation with the U.S. GEOLOGICAL SURVEY NATIONAL GEOLOGIC MAPPING PROGRAM DEPARTMENT OF ENVIRONMENTAL PROTECTION WATER RESOURCES MANAGEMENT NEW JERSEY GEOLOGICAL AND WATER SURVEY 6000 5000 4000 3000 2000 0 1000 1000 7000 FEET 0 1 1 KILOMETER .5 1 MILE 0 1 SCALE 1:24 000 (NEWFOUNDLAND) (WARWICK) (GREENWOOD LAKE) (WANAQUE) (FRANKLIN) (HAMBURG) (UNIONVILLE) (PINE ISLAND) Wawayanda, N.J. - N.Y. base map from U.S. Geological Survey, 1954. Pine Island, N.Y. - N.J. base map from U.S. Geolgical Survey, 1969 Research supported by the U. S. Geological Survey, National Cooperative Geological Mapping Program, under USGS award number 99HQAG0141 The views and conclusions contained in this document are those of the authors and should not be interpreted as necessarily representing the official policies, either expressed or implied, of the U. S. Government. 12'30'' 27' 30'' 41 o 07'30'' 74 o 22'30'' Digital cartography by M.W. Girard 25' 25' 10' 12'30'' BEDROCK GEOLOGIC MAP OF THE WAWAYANDA QUADRANGLE AND NEW JERSEY PART OF THE PINE ISLAND QUADRANGLE OPEN FILE MAP SERIES OFM 104 SUSSEX AND PASSAIC COUNTIES, NEW JERSEY AND ORANGE COUNTY, NEW YORK LOCATION IN NEW JERSEY Mesoproterozoic geology mapped by R.A. Volkert Lower Paleozoic geology mapped by D.H. Monteverde and R.A. Volkert Middle Paleozoic geology adopted from Herman and Mitchell (1991) and Barnett (1976) Geology mapped in 1988, 1995, and 2010 MAGNETIC NORTH APPROXIMATE MEAN DECLINATION, 1999 TRUE NORTH 11 / 1 2 MAGNETIC NORTH APPROXIMATE MEAN DECLINATION, 1999 TRUE NORTH 11 / 1 2 MAGNETIC NORTH APPROXIMATE MEAN DECLINATION, 1999 TRUE NORTH 11 MAGNETIC NORTH APPROXIMATE MEAN DECLINATION, 1999 TRUE NORTH 11 WAWAYANDA QUADRANGLE PINE ISLAND QUADRANGLE Yp ? U D ? U D Yp C h C a C l Yu Ym Yfw Ya Ya Ya Ym Ym Ym Ya Ym Ya Ya Yfw Ym Yff Ygm Ygm Yff Yu Yp Yb Ymh Ypg Ypg Yp Yp Ymp Yp Ymp Ypa Ypa Ymh Ymp Yp Yp Yap Yb Yp Ymp Yp Yp Yb Yb Yp Ylb Ymp Yp Ymp Ymp Ypa Yp Ymh Ymp Ylb Yp Yp Ya Ymp Dsk Dbv Dcw Sbp Dkec Dcw Yp Yk Ylo Ypg Ymh Ybs Ylb Ylo Yps Ymh Ypg Ymh Ylb Yps Ymh Yk Ylo Ylh Ymh Ybs Ymh Ylb Ymh 1,000 2,000 -1,000 3,000 SEA LEVEL 1,000 2,000 1,000 3,000 SEA LEVEL 2,000 2,000 A' A Pochuck Mountain Glenwood Fault East Fault Vernon Valley Bend in Section Dekay Fault Wawayanda Lake Fault Laurel Pond Fault Passaic County Sussex County 1,000 2,000 1,000 3,000 SEA LEVEL 2,000 B' 1,000 -2,000 -1,000 -3,000 SEA LEVEL 2,000 B Wawayanda Lake Fault Highland Lake Fault Vernon Fault Bearfort Mountain Passaic County Sussex County Reservoir Fault Ymp Ylo Ymh FEET FEET FEET FEET Ybs INTRODUCTION The Wawayanda and Pine Island quadrangles are located in northeastern Sussex and northwestern Passaic Counties, New Jersey, and southern Orange County, New York. They are situated mainly in the New Jersey Highlands Province. The map area is characterized by rugged uplands with ridge top elevations of as much as 1,480 feet above sea level on Wawayanda and Bearfort Mountains, the highest elevations in the Highlands, and 914 feet above sea level on Pochuck Mountain. Upland areas in the northern part of the area are separated by generally broad, northeast-striking stream valleys, such as Vernon Valley. Pochuck Creek and Wawayanda Creek are the principal streams in these valleys. Elsewhere in the area, uplands are drained by tributary streams that have incised narrow, steep-sided valleys that strike mainly north or northeast. STRATIGRAPHY Paleozoic rocks Paleozoic rocks in the map area range in age from Cambrian through Devonian and are subdivided into Middle Paleozoic rocks of the Green Pond Mountain Region that crop out in the area of Bearfort Mountain, and Lower Paleozoic rocks of the Kittatinny Valley sequence that occur in Vernon Valley to the west and north of Wawayanda Mountain. Middle Paleozoic rocks include the 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 origin and stratigraphic relationship of these rocks were discussed by Darton (1894), Kümmel and Weller (1902), and Barnett (1970). Along their western margin, Middle Paleozoic rocks are in fault contact with Mesoproterozoic rocks. Formations of Cambrian and Ordovician age of the Kittatinny Valley sequence include the Kittatinny Supergroup, of which the Leithsville Formation, Allentown Dolomite, Richenbach, and Epler Formations are exposed in the quadrangle. Lower Paleozoic rocks are in unconformable contact with Mesoproterozoic rocks north and west of Wawayanda Mountain, and are in fault contact east of Pochuck Mountain. Based on the final acceptance of the Global Stratotype Section and Point base (GSSP) for the Ordovician at Green Point, Newfoundland (Cooper and others, 2001), the Cambrian-Ordovician boundary in New Jersey is currently accepted as occurring within the lower third of the Epler Formation, at the top of the Cordylodus lindstromi zone, within conodont fauna B as used in Karklins and Repetski (1989). Therefore, the Allentown and Rickenbach Dolomite are currently regarded as Cambrian in age and not Ordovician and Cambrian as shown on previous bedrock geologic maps. Mesoproterozoic rocks Mesoproterozoic rocks consist of an assemblage of granites, gneisses, and marble. Most Mesoproterozoic rocks were metamorphosed to granulite facies during the Ottawan phase of the Grenville orogeny at 1045 to 1024 Ma (Volkert and others, 2010). The temperature for this high-grade metamorphism is constrained from regional calcite-graphite geothermometry to 769 o C (Peck and others, 2006). The oldest Mesoproterozoic rocks in the area consist of the Losee Suite and a thick assemblage of supracrustal metavolcanic and metasedimentary rocks. Rocks of the Losee Suite are calc-alkalic in composition and include various quartz-plagioclase gneisses and amphibolite formed from plutonic and volcanic protoliths in a magmatic arc tectonic setting (Volkert, 2004). Rocks of the Losee Suite yield sensi- tive high-resolution ion microprobe (SHRIMP) U-Pb zircon ages of 1282 to 1248 Ma (Volkert and others, 2010). Spatially and temporally associated with the Losee Suite are supracrustal rocks that include micro- cline gneiss and amphibolite formed from felsic and mafic volcanic protoliths, respectively, and quartzofeld- spathic gneisses, calc-silicate rocks, and marble formed from sedimentary protoliths. Supracrustal rocks were deposited in a back-arc basin inboard of the Losee arc (Volkert, 2004). Microcline gneiss yields U-Pb SHRIMP zircon ages of 1299 to 1251 Ma (Volkert and others, 2010) that closely overlap the age of rocks of the Losee Suite. Granite and related rocks of the Byram and Lake Hopatcong Intrusive Suites, that together comprise the Vernon Supersuite (Volkert and Drake, 1998), are abundantly exposed in the area where they intrude Losee Suite and supracrustal rocks. Byram and Lake Hopatcong rocks form a complete differentiation series that includes monzonite, quartz monzonite, granite, and alaskite, all of which have a distinctive A-type geochemical composition (Volkert and others, 2000). Granites of both suites yield similar U-Pb SHRIMP zircon ages of 1188 to 1182 Ma (Volkert and others, 2010). The youngest Mesoproterozoic rocks are postorogenic potassic granites and granite pegmatites that are undeformed, contain xenoliths of foliated gneiss or marble, and intrude other Mesoproterozoic rocks in the map area as small, tabular to irregular bodies that are discordant to metamorphic foliation. The most abundant of these is the Mount Eve Granite which forms two prominent intrusive bodies known as Mt. Adam and Mt. Eve in the Pine Island quadrangle, as well as more than 30 smaller bodies in adjacent quadrangles (Gorring and others, 2004). A sample of Mount Eve Granite collected from Mt. Adam yielded a zircon U-Pb thermal ionization mass spectrometry (TIMS) age of 1020 Ma (Drake and others, 1991a) and a sample collected from Mt. Eve yielded a zircon SHRIMP age of 1019 Ma (Volkert and others, 2010). Other small bodies of granite from the Pine Island quadrangle yielded a zircon U-Pb TIMS age of 1004 Ma (Volkert and others, 2005). Granite pegmatites intrude Mesoproterozoic rocks in the map area as small, tabular to irregular bodies that are highly discordant to crystallization foliation. Elsewhere in the Highlands these pegmatites have yielded zircon U-Pb ages of 990 to 965 Ma (Volkert and others, 2005). STRUCTURE Paleozoic bedding Bedding in the Middle Paleozoic rocks is fairly uniform and strikes northeast from N.12 o E. to N.50 o E. and averages N.33 o E. Most beds are upright and dip southeast and, less commonly, northwest, although locally they are overturned. The dip of all beds in the Middle Paleozoic rocks ranges from 34 o to 90 o and averages 71 o (Barnett, 1976; Herman and Mitchell, 1991). Bedding in the Lower Paleozoic rocks forms two populations, one that strikes northeast (N.10 o E.to N.65 o E.) and one that strikes northwest (N.44 o W. to due East) (fig. 1). Most beds dip northwest and, less commonly, southeast. The dip of all beds in Lower Paleozoic rocks ranges from 4 o to 90 o and averages 26 o . Proterozoic foliation Crystallization foliation, formed by the parallel alignment of mineral grains in the Mesoproterozoic rocks, defines the trend of the bedrock. It is an inherited feature from compressional stresses during granulite-facies metamorphism that deformed the rocks between 1045 and 1024 Ma (Volkert and others, 2010). Foliations in the Wawayanda quadrangle strike mainly northeast at an average of N.25 o E. (fig. 2), but locally, in the hinges of folds, they strike northwest due to deformation of the rocks during folding. Foliations dip southeast and, less commonly, northwest at 12 o to 90 o and average 66 o . Northwest-striking foliations dip gently to moderately northeast. Foliations in the Pine Island quadrangle are more varied due to the extent of folding of the rocks. Here, foliations fall into three main groups that average N.15 o E., N.15 o W., and N.65 o W. (fig. 3). Northeast-striking foliations dip mainly southeast and northwest-striking foliations dip mainly southwest. The dip of all foliations ranges from 5 o to 85 o and averages 22 o , but most dips are less than 40 o . Folds Folds in the Lower Paleozoic rocks were formed during the Taconian and Alleghanian orogenies at about 450 Ma and 250 Ma, respectively, and in the Middle Paleozoic rocks during the Alleghanian orogeny. Folds in the Middle Paleozoic rocks have axial surfaces that trend northeast, and they are open to tight, upright to locally overturned, and gently inclined to recumbent anticlines and synclines (Barnett, 1976; Herman and Mitchell, 1991). Most folds plunge gently southwest. Folds in the Lower Paleozoic rocks have northeast-trending axial surfaces, and they are open, upright to locally overturned and form gently north-plunging anticlines and synclines. Folds that deform Mesoproterozoic rocks originated during the Ottawan phase of the Grenville orogeny. They deform earlier-formed planar metamorphic fabrics and, therefore, postdate the develop- ment of crystallization foliation. Characteristic fold patterns are broad, open, northwest-verging to locally upright, northeast-plunging antiforms and synforms. Mineral lineation plunges parallel to the axes of major folds. Plunges range from 7 o to 52 o and average 26 o to N.36 o E. Faults The structural geology of the bedrock units is dominated by northeast-trending faults that deform Mesoproterozoic and Paleozoic rocks. These faults were active during the Grenville, Taconic and Allegha- nian compressional orogenies and during Neoproterozoic and Mesozoic extensional events. From the northwest, they include the Glenwood, East, Vernon, DeKay, Highland Lake, Wawayanda Lake, Laurel Pond, and Reservoir fault. Most faults exhibit brittle deformation features that include brecciation, recrystallization, and low- temperature retrogression of mafic minerals, chlorite or epidote-coated slickensides, and closely-spaced fracture cleavage. Ductile deformation features include mylonite, shear band foliation, and boudinage. On some faults these are locally overprinted by brittle deformation features. The Glenwood fault extends through the center of Pochuck Mountain where it is bounded by Mesoproterozoic rocks along most of its length almost to Pine Island, and from there, by Paleozoic rocks extending north. The fault strikes about N.15 o E. and dips northwest about 80 o . The latest movement appears to have been reverse with a high-angle oblique component. The fault exhibits brittle deformation features. The East fault borders the west side of Vernon Valley where Mesoproterozoic rocks on the footwall abut Lower Paleozoic rocks on the hanging wall. The fault strikes N.45 o E. and dips about 80 o southeast. In the map area, the latest movement was normal, although along strike to the south, kinematic indicators record steep reverse movement. The fault exhibits brittle deformation features. The Vernon fault extends along the west side of Wawayanda Mountain where it is bounded by Mesoproterozoic rocks along most of its length to the town of Vernon. Here it offsets the contacts of Lower Paleozoic rocks. The fault strikes N.15 o E. and dips southeast at about 60 o . The latest movement appears to have been normal. The fault exhibits brittle deformation features. The DeKay fault extends along the western base of Wawayanda Mountain west to Vernon where it appears to be cut off by the Vernon fault. It is bounded by Mesoproterozoic rocks at its southern end and by Lower Paleozoic rocks at its northern end which are offset. The fault strikes N.40 o E. and dips about 80 o northwest. The latest movement appears to have been normal. The fault exhibits brittle deformation features. The Highland Lake fault extends through the western part of Wawayanda Mountain where it is bounded by Mesoproterozoic rocks. To the south it merges with, or is cut off by, the Vernon fault. To the north its extent is unknown beyond the area of Highland Lake. The fault strikes N.20 o E. to N.40 o E. and dips about 75 o southeast. The latest movement appears to have been normal. The fault exhibits brittle deformation features. The Wawayanda Lake fault extends through the central part of Wawayanda Mountain where it is bounded by Mesoproterozoic rocks. The fault bifurcates east of Highland Lake, and the main segment extends northeastward through Wawayanda Lake. To the north the presence of both fault segments is unknown, however the main segment does not seem to offset the Lower Paleozoic rocks. The fault strikes N.15 o E.to N.35 o E. and dips about 75 o southeast. The latest movement appears to have been normal. The fault exhibits brittle deformation features. The Laurel Pond fault extends along the east side of Wawayanda Mountain where it is bounded by Mesoproterozoic rocks. The strike is somewhat varied and ranges from N.40 o E. to N.70 o E. The dip is about 50 o northwest. The latest movement appears to have been normal. The fault exhibits brittle deformation features. The Reservoir fault extends from New York State southwest to Schooleys Mountain (Drake and others, 1996). In the map area the fault places Paleozoic rocks on the hanging wall against Mesoprotero- zoic rocks on the footwall, but to the south it is bounded by Mesoproterozoic rocks on both sides. The fault strikes N.30 o E. and dips 80 o northwest to vertically. It has undergone multiple reactivations dating from the Proterozoic that reflect a complex deformation history involving normal, right-lateral strike slip, and reverse movement, with the latest movement having been normal. The fault exhibits ductile deformation features that are overprinted by brittle features. Timing of fault movement based on 40 Ar/ 39 Ar isotope analysis yielded disturbed spectra, indicating resetting of amphiboles at about 722 Ma, and biotite inclusions in amphibole at about 322 Ma (Price, 2005), likely due to the effects of hydrothermal fluid movement along the fault. Mesoproterozoic and Paleozoic rocks are also deformed by small faults that strike northeast or northwest. These faults range from a few inches to a few feet wide and are of short length. They are characterized mainly by brittle deformation features. Joints Joints are a common feature in the Paleozoic and Mesoproterozoic rocks. They are best devel- oped in massive rocks such as Paleozoic limestone, dolomite, and sandstone, and in Mesoproterozoic granite and some gneiss. Joints are characteristically planar, moderately well formed, moderately to widely spaced, and moderately to steeply dipping. Their surfaces are typically unmineralized, except near faults, and are smooth or less commonly, slightly irregular. Joints vary in their spacing from one foot to tens of feet apart. Those formed close to faults are spaced two feet or less apart. Joint data for the Middle Paleozoic rocks are shown on the map of Herman and Mitchell (1991) and are not shown here. Joints in the Lower Paleozoic rocks form two populations that have average strikes of N.65 o W. and N.40 o E. (fig. 4). Northwest-striking joints dip mainly southwest, whereas the northeast-striking joints dip mainly southeast. The dip of all joints ranges from 44 o to 90 o and averages 75 o . The dominant joints in Mesoproterozoic rocks are nearly perpendicular to the strike of crystalliza- tion foliation, a consistent feature observed throughout the Highlands (Volkert, 1996). Therefore, the strike of joints is somewhat varied because of folding of the rocks. In the Wawayanda quadrangle the dominant joints strike N.67 o W. on average (fig. 5) and dip 18 o to 90 o mainly southwest at an average of 70 o . In the Pine Island quadrangle principal joint sets were measured that strike northwest at an average of N.70 o W. and northeast at an average of N.20 o E. (fig. 6). Northwest-striking joints dip nearly equally southwest and northeast and northeast-striking joints dip mainly southeast. The dip of all joints ranges from 56 o to 90 o and averages 79 o . ECONOMIC RESOURCES Mesoproterozoic rocks in the map area host economic deposits of iron ore (magnetite) that were mined predominantly during the 19th century. Detailed descriptions of most of the mines are given in Bayley (1910). Mount Eve Granite was formerly quarried at several locations on Mount Adam and Mount Eve for use as dimension stone. Marble was quarried for agricultural use as fertilizer east of Pochuck Mountain and south of Pine Island, and dolomite was quarried in Orange County, N.Y. Deposits of sand and gravel and peat were formerly worked in the area and organic-rich “black dirt” in the area of Pochuck Creek currently supports robust agricultural activity. DESCRIPTION OF MAP UNITS GREEN POND MOUNTAIN REGION Skunnemunk Conglomerate (Middle Devonian) (Darton, 1894) – Grayish-purple to grayish-red, thin- to very thick bedded, locally cross-bedded, polymictic conglomerate and sandstone containing clasts of white vein quartz, red and green quartzite and sandstone, red and gray chert, and red shale; interbedded with medium-gray, thin-bedded sandstone and greenish-gray and grayish-red, mud-cracked shale. Conglomerate and sandstone matrix is primary hematite and microcrystalline quartz. Conglomerate cobbles are as much as 6.5 in. long, and average cobble size is larger in upper part of unit. Lower contact is conformable and gradational as defined by Kümmel and Weller (1902). Unit is about 3,000 ft thick. Bellvale Sandstone (Middle Devonian) (Bellvale Flags of Darton, 1894; Willard, 1937) – Upper beds are grayish-red to grayish-purple sandstone containing quartz pebbles as large 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. Sandstone more common in upper beds and is finer downward. Lower contact conformable with the Cornwall Shale and placed where beds are thicker 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 shale, interbedded with medium-gray and light-olive-gray to yellowish-gray, laminated to very thin-bedded siltstone that is more abundant 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 Formation) Kanouse Sandstone (Kümmel, 1908) – Medium-gray, light-brown, and grayish-red, fine to coarse-grained, thin to thick-bedded sandstone and pebble conglomerate. Basal conglom- erate 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 gradational. 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 probably 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 con- glomerate 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 transitional 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 conformable with Green Pond Conglomerate. Unit is about 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, or is in fault contact with, Mesoproterozoic rocks. Unit is about 1,000 ft. thick. KITTATINNY VALLEY SEQUENCE Epler Formation (Lower Ordovican and Upper Cambrian) (Hobson, 1957) – Upper part is light-olive to dark-gray, fine to medium-grained, thin to thick-bedded, locally laminated dolomite. Middle part is olive-gray, light-brown, or dark-yellowish-orange-weathering, dark-gray, aphanitic to fine-grained, laminated to medium-bedded dolomite, and light-gray to light-bluish-gray-weathering, medium-dark to dark-gray, fine-grained, thin to medium-bedded limestone, that is characterized by mottling and reticulate dolomite and light-olive-gray to grayish-orange-weathering, medium-gray dolomitic shale laminae surrounding the limestone lenses. Limestone grades laterally and down section into medium-gray, fine-grained dolomite. Lower part is medium-light to dark-gray, aphanitic to medium-grained, laminated to medium-bedded dolomite. Contains lenses of white and dark-gray chert. Lower contact is placed at the transition from a massive laminated, very fine-grained, dark-gray dolomite to the underlying massive light-gray, medium to coarse-grained pitted dolomite that occurs about 50 to 75 feet above a thinly interbedded sequence of medium-grained dolomite and as many as seven, thin, black, convex-upward chert layers. Unit contains conodonts of Cordylodus lindstomi to Rossodus manitouensis zones of the North American Midcontinent Province as used by Sweet and Bergstrom (1986). Unit is approximately 420 ft. thick. Rickenbach Dolomite (Upper Cambrian) (Hobson, 1957) – Upper part is medium to dark-gray, fine to coarse-grained, medium to thick-bedded dolomite, locally fetid, mottled, weathered surface. Contains pods and lenses of dark-gray to black chert near the upper contact. Lower part is medium to dark-gray, fine to medium-grained, thin to medium-bedded dolomite. Floating quartz sand grains and quartz-sand stringers occur in the basal part of unit. Lenses of light-gray, coarse to very-coarse-grained dolomite locally occur throughout the unit. Lower contact placed at top of distinctive medium-gray quartzite. Contains conodonts of Cordylodus proavus to Cordylodus lindstomi zones of North American Midcontinent Province, as used by Sweet and Bergstrom (1986). Unit is as much as 200 ft. thick. Allentown Dolomite (Upper Cambrian) (Wherry, 1909) – Upper sequence is light to medium-gray-weathering, medium-light to medium-dark-gray, fine to medium-grained, locally coarse-grained, medium to very-thick-bedded dolomite; local shaly dolomite near the bottom. Floating quartz sand and two intervals of medium-light to very-light-gray, medium-grained, thin-bedded quartzite and discontinuous dark-gray chert lenses occur directly below upper contact. Lower sequence is medium to very-light-gray-weathering, light to medium-dark-gray, fine to medium-grained, thin to medium-bedded dolomite and shaly dolomite. Weathered exposures characterized by alternating light- and dark-gray beds. Ripple marks, ooids, algal stromatolites, cross-beds, edgewise conglomerate, mud cracks, and paleosol zones occur throughout but are more abundant in the lower sequence. Unit grades down into the Leithsville Formation. Elsewhere, contains a trilobite fauna of Dresbachian (early Late Cambrian) age (Weller, 1903; Howell, 1945). Unit is approximately 1,800 ft. thick. Leithsville Formation (Middle and Lower Cambrian) (Wherry, 1909) – Upper sequence, seldom exposed, is mottled, medium-light to medium-dark-gray-weathering, medium to medium-dark-gray, fine to medium-grained, medium to thick-bedded dolomite, locally pitted and friable. Middle sequence is grayish-orange, light to dark-gray, grayish-red, or light- greenish to dark-greenish-gray-weathering, fine-grained, thin to medium-bedded dolomite, ar- gillaceous dolomite, dolomitic shale, quartz sandstone, siltstone and shale. Lower sequence is medium-light to medium-gray-weathering, medium-gray, fine to medium-grained, thin to medium-bedded dolomite. Quartz-sand lenses occur near lower gradational contact with Hardyston Quartzite. Archaeocyathids of Early Cambrian age were found in the formation in Franklin, New Jersey, suggesting an intraformational disconformity between Middle and Early Cambrian strata (Palmer and Rozanov, 1967). Unit also contains Hyolithellus micans (Offield, 1967; Markewicz, 1968). Thickness is approximately 600 ft. Hardyston Quartzite (Lower Cambrian) (Wolff and Brooks, 1898) – Medium to light-gray, fine to coarse-grained, medium to thick-bedded quartzite, arkosic sandstone and dolomitic sandstone. Elsewhere, contains Scolithus linearis(?) and fragments of the trilobite Olenellus thompsoni of Early Cambrian age (Nason, 1891; Weller, 1903). Thickness is as much as 40 ft. Dsk Dbv Dcw Dkec Sbp Sl Sg NEW JERSEY HIGHLANDS Other Rocks Mount Eve Granite (Mesoproterozoic) – Pinkish-gray or buff-weathering ,pinkish-white or light-pinkish-gray, medium to coarse-grained, massive, unfoliated granite composed principally of microcline microperthite, quartz, oligoclase, horblende, and biotite. Locally contains xenoliths of foliated country rock. Includes bodies of pegmatite too small to show on map. Vernon Supersuite (Volkert and Drake, 1998) Byram Intrusive Suite (Drake and others, 1991b) Hornblende granite (Mesoproterozoic) – Pinkish-gray or buff-weathering, pinkish-white or light pinkish-gray, medium to coarse-grained, foliated granite and sparse granite gneiss composed principally of microcline microperthite, quartz, oligoclase, hornblende, and magne- tite. Some variants are quartz syenite or quartz monzonite. Locally contains clinopyroxene where in contact with rocks of the Lake Hopatcong Intrusive Suite. Includes small bodies of pegmatite too small to show on map. Hornblende monzonite (Mesoproterozoic) – Tan or buff-weathering, pinkish-gray or greenish-gray, medium to coarse-grained, foliated monzonite and, less commonly, quartz monzonite composed of microcline microperthite, oligoclase, hornblende, and magnetite. Locally contains quartz. Sparse to moderate amounts of clinopyroxene may be present where in contact with rocks of the Lake Hopatcong Intrusive Suite. Lake Hopatcong Intrusive Suite (Drake and Volkert, 1991) Pyroxene granite (Mesoproterozoic) – Light gray, buff, or white-weathering, greenish-gray, medium to coarse-grained, massive, foliated granite composed of mesoperthite to microanti- perthite, quartz, oligoclase, and clinopyroxene. Commonly contains titanite, magnetite, apatite, and pyrite. Sparse to moderate amounts of hornblende may be present where in contact with rocks of the Byram Intrusive Suite. Includes small bodies of pegmatite too small to show on map. Pyroxene alaskite (Mesoproterozoic) – Light-gray or tan-weathering, greenish-buff or light pinkish-gray, medium to coarse-grained, massive, foliated granite composed of mesoperthite to microantiperthite, oligoclase, and quartz. Commonly contains clinopyroxene, titanite and magnetite. Occurs in a pair of bodies east of Highland Lake. Pyroxene monzonite (Mesoproterozoic) – Gray, buff, or tan-weathering, greenish-gray, medium to coarse-grained, massive, foliated rock composed of mesoperthite to microantiper- thite, oligoclase, clinopyroxene, titanite and magnetite. Locally contains hornblende where in contact with rocks of the Byram Intrusive Suite. Crops east and west of the Vernon fault. Back-Arc Supracrustal Rocks Potassic feldspar gneiss (Mesoproterozoic) – Light-gray or pinkish-buff-weathering, pinkish-white or light pinkish-gray, fine to medium-grained, moderately foliated gneiss and less abundant granofels composed of quartz, microcline microperthite, and varied amounts of biotite, garnet, sillimanite, and magnetite. Locally contains thin, sparsely garnetiferous quartzite layers. Exposed sporadically throughout the map area, but is most abundant in the vicinity of Highland Lake. Microcline gneiss (Mesoproterozoic) – Tan or pale pinkish-white-weathering, light-gray or pinkish-gray, fine to medium-grained, layered and foliated rock composed principally of microcline microperthite, quartz, and oligoclase. Common accessory minerals include biotite, garnet, sillimanite, and magnetite. Unit is well exposed in the northwest part of the map area. Biotite-quartz-feldspar gneiss (Mesoproterozoic) – Gray-weathering, locally rusty- weathering, gray, tan, or greenish-gray, medium to coarse-grained, moderately layered and foliated gneiss containing microcline microperthite, oligoclase, quartz, and biotite. Locally contains garnet, sillimanite, graphite, and opaque minerals. Commonly contains thin layers of quartzite that may contain graphite and biotite. Unit is most abundant north of Upper Greenwood Lake. Hornblende-quartz-feldspar gneiss (Mesoproterozoic) – Pinkish-gray or buff- weathering, pinkish-white or pinkish-gray, fine to medium-grained, moderately well layered and foliated gneiss composed of microcline, quartz, oligoclase, and hornblende. Locally contains garnet, magnetite, and biotite. Unit occurs throughout the map area. Clinopyroxene-quartz-feldspar gneiss (Mesoproterozoic) – Pinkish-gray or pinkish-buff- weathering, white, pale-pinkish-white, or light-gray, fine to medium-grained, moderately foli- ated gneiss composed of quartz, microcline, oligoclase, clinopyroxene, and trace amounts of epidote, biotite, titanite, and opaque minerals. Commonly contains thin layers of amphibolite. Unit is present throughout the map area, but is most abundant south and east of Wawayanda Lake. Pyroxene gneiss (Mesoproterozoic) – White or tan-weathering, greenish-gray, medium- fine to medium-grained, layered and foliated gneiss containing oligoclase and clinopyroxene. Quartz content is highly varied. Contains sparse amounts of epidote, titanite, scapolite, or calcite. Commonly interlayered with pyroxene amphibolite or marble. Unit is abundantly exposed throughout the map area. Marble (Mesoproterozoic) – White or light-gray-weathering, white, grayish-white, or less commonly pinkish-orange, fine to coarse-grained, calcitic to locally dolomitic marble with accessory graphite, phlogopite, chondrodite, and clinopyroxene. Contains pods and lenses of clinopyroxene-garnet skarn, hornblende skarn, and clinopyroxene-rich rock. Divided by Hague and others (1956) into a lower Franklin marble (Yff) and an upper Wildcat marble (Yfw) separated by a layered sequence of gneiss. Locally contains relict karst features in the form of bedrock pinnacles and solution joints and openings. Unit is best exposed in the northwestern part of the map area in Vernon Valley. Amphibolite (Mesoproterozoic) – Grayish-black, medium-fine to medium-grained, foliated rock composed of hornblende and andesine. Some amphibolite also contains abundant clinopyroxene (Yap). Unit is associated with most Mesoproterozoic rocks in the map area. Amphibolite associated with the Losee Suite is metavolcanic in origin, and that associated with supracrustal rocks may be metavolcanic or metasedimentary in origin. All types are shown undifferentiated on the map. Unit is best exposed on Pochuck Mountain. It locally contains relict pillow structures (Hague and others, 1956) and forms a bimodal sequence of volcanic rocks with microcline 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, moderately layered to foliated gneiss composed of oligoclase or andesine, quartz, and local hornblende, biotite, and clinopyroxene. Commonly contains thin, conformable layers of amphibolite. Best exposed north and west of Canistear Reservoir. Biotite-quartz-oligoclase gneiss (Mesoproterozoic) – White or light-gray-weathering, medium-gray or greenish-gray, medium to coarse-grained, layered and foliated gneiss composed of oligoclase or andesine, quartz, and biotite. Some outcrops contain garnet or hornblende. Locally interlayered with amphibolite. Best exposed in the eastern part of the map area. Hornblende-quartz-oligoclase gneiss (Mesoproterozoic) – White-weathering, light greenish-gray, medium to coarse-grained, foliated gneiss containing oligoclase or andesine, quartz, hornblende, and magnetite. Crops out in one small body southwest of Highland Lake. Hypersthene-quartz-plagioclase gneiss (Mesoproterozoic) – Gray or tan-weathering, greenish-gray or greenish-brown, medium-grained, layered and foliated gneiss composed of andesine or oligoclase, quartz, clinopyroxene, hornblende, and hypersthene. Contains thin, conformable layers of amphibolite and mafic-rich quartz-plagioclase gneiss. Crops out near Canistear Reservoir, in the southwestern part of the map area. Diorite (Mesoproterozoic) – Gray or tan-weathering, greenish-gray or greenish-brown, medium to coarse-grained, massive, foliated rock containing andesine or oligoclase, clinopyroxene, hornblende, and hypersthene. Commonly contains thin mafic layers or schlieren having the composition of amphibolite. Crops out in one small body in Orange County, New York. Undifferentiated rocks (Mesoproterozoic) – Shown in cross section only. OCe Cr Ca Cl Ch Yu Ygm Ybh Ybs Ypa Ym Yb Ylb Ypg Yps Yk Ymh Ymp Yp Yff Yfw Ylh Yh Yd Ylo by Richard A. Volkert and Donald H. Monteverde 2014 BEDROCK GEOLOGIC MAP OF THE WAWAYANDA QUADRANGLE AND THE NEW JERSEY PART OF THE PINE ISLAND QUADRANGLE SUSSEX AND PASSAIC COUNTIES, NEW JERSEY AND ORANGE COUNTY, NEW YORK Ya Yap 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, 9 p. Bayley, W.S., 1910, Iron mines and mining in New Jersey: New Jersey Geological Survey Final Report VII, 512 p. 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. Cooper, R.A., Nowlan, G.S., and Williams, S.H., 2001, Global Stratotype Section and Point for base of the Ordovician System: Episodes, v. 24, no. 1, p. 19-28. 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., Aleinikoff, J.N., and Volkert, R.A., 1991a, The Mount Eve Granite (Middle Proterozoic) of northern New Jersey and southeastern New York, in Drake, A.A., Jr., ed., Contributions to New Jersey Geology: U.S. Geological Survey Bulletin 1952, p. C1-C10. _________, 1991b, The Byram Intrusive Suite of the Reading Prong - Age and tectonic environment, in Drake, A.A., Jr., ed., Contributions to New Jersey Geology: U.S. Geological Survey Bulletin 1952, p. D1-D14. 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., Estelle, T.C., and Volkert, R.A., 2004, Geochemistry of the late Mesoproterozoic Mount Eve Granite: implications for late- to post-Ottawan tectonics in the New Jersey-Hudson Highlands, 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. 505-524. Hague, J.M., Baum, J.L., Hermann, L.A., and Pickering, R.J., 1956, Geology and structure of the Franklin-Sterling area, New Jersey: Geological Society of America Bulletin, v. 67, p. 435-474. 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. Hobson, J.P., 1957, Lower Ordovician (Beekmantown) succession in Berks County, Pennslyvania: American Association of Petroleum Geologists Bulletin, v.14, p. 2710-2722. Howell, B.F., 1945, Revision of Upper Cambrian faunas of New Jersey: Geological Society of America Memoir 12, 46 p. Karklins, O.L. and Repetski, J.E., 1989, Distribution of selected Ordovician Conodont fauns in Northern New Jersey, U.S. Geological Survey Map MF-2066, scale 1:185,000. Kümmel, H.B., 1908, Paleozoic sedimentary rocks of the Franklin Furnace quadrangle, New Jersey, in Spencer, A.C., Kümmel, 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. Kümmel, H.B., and Weller, Stuart, 1902, The rocks of the Green Pond Mountain region: New Jersey Geological Survey Annual Report of the State Geologist, 1901, p. 1-51. Markewicz, F.J., 1968, The Hardyston-Leithsville contact and significance of “Hyolithellus micans” in the lower Leithsville Formation: [abs.], New Jersey Academy of Science Bulletin, v. 13, p. 96. Markewicz, F.J., and Dalton, R.F., 1977, Stratigraphy and applied geology of the lower Paleozoic carbonates in northwestern New Jersey: in 42nd Annual Field Conference of Pennsylvania Geologists, Guidebook, 117 p. Nason, F.L., 1891, The Post-Archaen age of the white limestone of Sussex County, New Jersey: New Jersey Geological Survey Annual Report of the State Geologist, 1890, p. 25-50. Offield, T.W., 1967, Bedrock geology of the Goshen-Greenwood Lake area, New York: New York State Museum and Science Service Map and Chart Series, no. 9, 78 p. Palmer, A.R., and Rozanov, A.Y., 1967, Archaeocyatha from New Jersey: Evidence for an intra- formational unconformity in the north-central Appalachians: Geology, v. 4, p. 773-774. 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. Price, R.E., 2005, 40Ar/39Ar evidence for early (700 Ma) Iapetan oblique divergence in the Highlands region, NJ-NY-PA, unpublished MS thesis, Rutgers University, Newark, NJ, 36 p. Rogers, H.D., 1836, Report on the geological survey of the State of New Jersey: Philadelphia, Desilver, Thomas, & Co., 174 p. Sweet, W.C., and Bergstrom, S.M., 1986, Conodonts and biostratigraphic correlation: Annual Review of Earth and Planetary Science, v. 14, p. 85-112. Vanuxem, Lardner, 1842, Geology of New York, part III, comprising the survey of the third geological district: Albany, N.Y., 306 p. 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 Geolo- gists, p. A1-A33. ________, 2004, Mesoproterozoic rocks of the New Jersey Highlands, north-central Appalachians: petrogenesis 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. 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 geochronology, in Tollo, R.P., Bartholomew, M.J., Hibbard, J.P., and Karabinos, P.M., eds., From Rodinia to Pangea: The Lithotectonic 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, 77 p. 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., Zartman, R.E., and Moore, P.B., 2005, U-Pb zircon geochronology of Mesoproterozoic postorogenic rocks and implications for post-Ottawan magmatism and metallogenesis, New Jersey Highlands and contiguous areas, USA: Precambrian Research, v. 139, p. 1-19. Weller, Stuart, 1903, The Paleozoic faunas: New Jersey Geological Survey, Report on Paleontology, v. 3, 462 p. Wherry, E.T., 1909, The early Paleozoics of the Lehigh Valley district, Pennsylvania: Science, new series, v. 30, 416 p. White, I.C., 1882, The geology of Pike and Monroe Counties: Pennsylvania Geological Survey, 2nd series, Report G-6, 407 p. Willard, Bradford, 1937, Hamilton correlation: American Journal of Science, 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. 431-456. ORDOVICIAN SILURIAN DEVONIAN CAMBRIAN MESOPROTEROZOIC UNCONFORMITY UNCONFORMITY Kittatinny Valley Sequence Kittatinny Supergroup NEW JERSEY HIGHLANDS Ygm Dkec Dcw Dsk Dbv Sbp Sl Sg CORRELATION OF MAP UNITS OCe Ca Cr Cl Ch INTRUSIVE CONTACTS Mesoproterozic undivided VALLEY AND RIDGE GREEN POND MOUNTAIN REGION Yk Ym Yb Ymp Ymh Ylh Yh Yd Ylo Ylb Ybh Ybs Ypg Yps Ypa Back Arc Supracrustal Rocks Ya Yap Yp Yff Yfw Magmatic Arc Rocks Vernon Supersuite Byram Intrusive Suite Lake Hopatcong Intrusive Suite Losee Suite Yu INTRUSIVE CONTACTS N % Avg trend = N64 E Sector size = 10 n = 111 o o 3 6 9 12 Figure 1. Rose diagram of bedding strikes in Lower Paleozoic rocks of the Kittatinny Valley sequence. N % 9 12 12 9 6 Avg trend = N67 W Sector size = 10 n = 723 o o Figure 5. Rose diagram of joint strikes in Mesoproterozoic rocks of the Wawayanda quadrangle. N % Avg trend = N06 E Sector size = 10 n = 62 o o 10 4 6 8 Figure 3. Rose diagram of crystallization foliation strikes in Mesoproterozoic rocks of the Pine Island quadrangle. N % Avg trend = N82 W Sector size = 10 n = 95 o o 9 6 12 15 6 3 9 12 15 Figure 6. Rose diagram of joint strikes in Mesoproterozoic rocks of the Pine Island quadrangle. N % 15 5 25 Avg trend = N25 E Sector size = 10 n = 612 o o 20 10 5 10 15 20 Figure 2. Rose diagram of crystallization foliation strikes in Mesoproterozoic rocks of the Wawayanda quadrangle. U U D D 75 M 30 10 20 30 70 EXPLANATION OF MAP SYMBOLS Contact - Dotted where concealed Faults - Dotted where concealed. Queried where uncertain Normal fault - U, upthrown side; D, downthrown side Reverse fault - U, upthrown side; D, downthrown side FOLDS Folds in Proterozoic rocks showing trace of axial surface, direction and dip of limbs, and direction of plunge. Antiform Synform Overturned antiform Overturned synform Minor asymmetric fold Folds in Paleozoic rocks showing trace of axial surface, direction and dip of limbs, and direction of plunge. Folds are in bedding. Anticline Syncline PLANAR FEATURES Strike and dip of crystallization foliation Inclined Vertical Strike and dip of mylonitic foliation Strike and dip of beds - Ball indicates top of beds known from sedimentary structures Inclined Vertical Overturned Strike and dip of spaced cleavage in Paleozoic rocks LINEAR FEATURES Bearing and plunge of mineral lineation in Proterozoic rocks Bearing and plunge of interesection of bedding and cleavage in Paleozoic rocks OTHER FEATURES Abandoned magnetite mine Abandoned quarry 80 R 72 35 72 74 50 86 79 72 39 38 21 76 83 84 78 72 84 52 64 71 70 82 68 61 70 74 M 53 58 37 60 74 62 50 61 87 70 79 75 74 26 A A' B' B VERNON FAULT FAULT LAKE HIGHLAND WAWAYANDA LAKE FAULT 73 ? ? h h h h h h 20 U D 25 17 h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h h M M M M M M M R 69 62 75 85 28 36 35 28 48 29 21 15 10 65 64 61 76 61 53 62 75 73 76 85 84 68 61 81 66 h 86 26 8 53 27 65 46 60 52 49 32 38 60 79 72 57 81 85 82 83 71 72 77 78 82 72 79 83 83 64 63 84 70 71 39 37 51 53 55 56 23 79 79 79 71 70 81 26 54 69 86 68 72 76 58 66 76 85 69 68 65 71 76 75 75 73 70 34 69 44 68 78 36 44 40 21 32 44 47 61 74 62 34 50 30 62 75 76 71 75 70 72 73 69 75 79 54 72 84 58 34 76 57 43 61 55 30 33 44 15 67 79 30 25 52 69 68 35 51 15 13 85 45 11 68 69 26 65 57 72 h 81 67 69 70 30 61 49 85 82 79 82 63 83 76 79 46 60 85 76 85 73 76 67 30 52 88 61 47 24 64 57 82 74 62 60 61 25 30 75 79 39 15 20 11 72 69 67 42 56 67 65 83 60 37 85 31 17 39 54 27 60 65 42 78 12 20 27 64 31 48 47 62 46 55 61 61 63 67 67 75 69 69 80 69 80 75 12 86 81 82 84 71 82 53 82 70 76 68 51 76 70 h 71 66 74 60 63 60 61 54 45 77 61 61 72 66 56 66 71 75 76 h 78 h 85 84 74 80 h h h h h h h 26 21 80 85 h 74 21 65 57 13 22 10 15 15 9 7 19 21 35 30 51 10 25 27 26 19 10 41 28 21 23 20 26 39 8 11 14 19 11 15 31 16 20 17 31 20 63 22 80 85 10 26 34 26 76 51 56 72 76 83 50 34 38 41 72 80 h 35 58 54 60 65 44 20 76 71 50 66 71 86 72 43 68 82 h h 78 72 80 60 65 75 48 77 35 39 51 43 30 16 62 79 84 74 79 76 69 77 79 80 72 M h 69 50 85 h 75 74 53 85 42 59 79 51 54 55 74 86 79 83 86 81 85 83 85 h h h 69 82 33 77 54 83 86 41 h h 77 78 84 81 81 85 80 80 83 63 83 58 75 81 64 76 82 81 40 M 68 81 75 49 65 44 56 47 76 60 96 67 75 75 68 34 27 27 56 55 17 13 75 80 83 78 78 66 65 79 63 78 76 68 77 64 71 79 76 67 50 18 67 82 69 78 81 66 86 62 48 21 54 h 22 20 18 15 43 19 20 13 15 10 5 25 67 29 8 18 10 22 18 55 37 22 15 6 79 55 8 83 78 79 89 81 h h h h h h h h h 70 80 60 80 80 70 75 40 30 52 h 85 h h h 70 20 45 15 11 82 64 21 23 25 16 29 30 76 12 14 86 36 70 33 27 58 16 15 13 9 14 21 13 12 12 10 h 65 60 48 47 34 12 70 38 52 35 56 63 16 15 13 17 14 60 h 18 18 6 10 14 10 12 14 15 18 29 8 25 21 24 11 78 82 56 68 74 63 52 50 U D h h 11 87 87 65 40 77 76 73 83 79 70 78 75 79 72 53 34 65 41 52 66 80 82 76 84 80 85 56 40 80 44 81 73 h h 59 M 61 69 76 73 65 76 10 71 64 87 83 85 80 87 h h 79 57 57 68 71 79 80 44 h 75 82 79 68 80 h 81 74 76 R 10 58 58 60 30 82 74 80 53 30 h h h h 25 71 16 9 14 14 25 67 Ch Ch h 12 42 65 77 79 h 35 h Yp Ybs Ybh Ymh Yps Ylb Ypg Ymh Ymh Ymh Yk Dsk Dbv Dbv Dcw Dkec Sbp Sl Sg Yp Yp Yp Yp Yp Yp Yp Yp OCe Yb Ypg Ylo Ypg Ymp Ymp Ymp Ymp Ymp Ymp Ymh Ymp Ymp Ypg Ylb Ymp Ya Ymh Ylb Ch Cl Cl Cl Cr Ygm Ygm Ygm Ygm Ylb Yfw Yk Ylb Ylb Yp Yfw Yfw Ym Ym Ym Ym Ym Ym Ym Ygm Ygm Ym Yff Yff Ylo Yk Ymh Yff Ybh Ybs Ca Ca Cl Ypg Yps Ymh Ylb Ymh Yb Ylb Ylo Ylo Ylo Ylo Ylb Ybh Ypg Ypg Ymh Ymh Ylo Yk Ymh Ylb Ymp Ymp Ypa Ypa Ymh Ypa Yp Ymh Yb Ylb Ylb Yb Ylo Yap Yap Yb Ylb Ylb Yb Yp Ymh Ymh Ymh Yd Ybh GLENWOOD FAULT D U EAST FAULT U D D U DEKAY FAULT D U ? U D ? RESERVOIR U D FAULT WAWAYANDA LAKE FAULT LAUREL POND FAULT Yp Yh Yh Ylo Ylh Ymh Ylb Ypg Ypg Ylo U D Ymp Ymp Ymh Dsk Ylo Ymp Yp Yb Yp Yp Yp Yp Yp Yp Yp Ypg Ylb Ymh Yk Ymh Yk Yk Yk Yh Ya Ya Ya Ya Ya U D Yp
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41 o 07'30''74 o 30'
10'
74 o 30'
41 o 15' 27' 30''
41o 15'
74 o 22'30''
Prepared in cooperation with theU.S. GEOLOGICAL SURVEY
NATIONAL GEOLOGIC MAPPING PROGRAM
DEPARTMENT OF ENVIRONMENTAL PROTECTIONWATER RESOURCES MANAGEMENTNEW JERSEY GEOLOGICAL AND WATER SURVEY
600050004000300020000 10001000 7000 FEET
01 1 KILOMETER.5
1 MILE01SCALE 1:24 000
(NEWFOUNDLAND)
(WARWIC
K)
(GR
EEN
WO
OD
LAK
E)
(WANAQUE)(FRANKLIN)
(HAM
BUR
G)
(UNIONVILLE) (PINE ISLAND)
Wawayanda, N.J. - N.Y. base map from U.S. Geological Survey, 1954. Pine Island, N.Y. - N.J. base map from U.S. Geolgical Survey, 1969
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 authorsand should not be interpreted as necessarily representing the official
policies, either expressed or implied, of the U. S. Government.
12'30''
27' 30'' 41 o 07'30''
74 o 22'30''
Digital cartography by M.W. Girard
25'
25'
10'
12'30''
BEDROCK GEOLOGIC MAP OF THE WAWAYANDA QUADRANGLE AND NEW JERSEY PART OF THE PINE ISLAND QUADRANGLE
OPEN FILE MAP SERIES OFM 104SUSSEX AND PASSAIC COUNTIES, NEW JERSEY AND ORANGE COUNTY, NEW YORK
LOCATION IN NEW JERSEY
Mesoproterozoic geology mapped by R.A. VolkertLower Paleozoic geology mapped by D.H. Monteverde and R.A. Volkert
Middle Paleozoic geology adopted from Herman and Mitchell (1991) and Barnett (1976)Geology mapped in 1988, 1995, and 2010
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WAWAYANDA QUADRANGLE PINE ISLAND QUADRANGLE
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INTRODUCTION
The Wawayanda and Pine Island quadrangles are located in northeastern Sussex and northwestern Passaic Counties, New Jersey, and southern Orange County, New York. They are situated mainly in the New Jersey Highlands Province. The map area is characterized by rugged uplands with ridge top elevations of as much as 1,480 feet above sea level on Wawayanda and Bearfort Mountains, the highest elevations in the Highlands, and 914 feet above sea level on Pochuck Mountain. Upland areas in the northern part of the area are separated by generally broad, northeast-striking stream valleys, such as Vernon Valley. Pochuck Creek and Wawayanda Creek are the principal streams in these valleys. Elsewhere in the area, uplands are drained by tributary streams that have incised narrow, steep-sided valleys that strike mainly north or northeast.
STRATIGRAPHYPaleozoic rocks
Paleozoic rocks in the map area range in age from Cambrian through Devonian and are subdivided into Middle Paleozoic rocks of the Green Pond Mountain Region that crop out in the area of Bearfort Mountain, and Lower Paleozoic rocks of the Kittatinny Valley sequence that occur in Vernon Valley to the west and north of Wawayanda Mountain. Middle Paleozoic rocks include the 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 origin and stratigraphic relationship of these rocks were discussed by Darton (1894), Kümmel and Weller (1902), and Barnett (1970). Along their western margin, Middle Paleozoic rocks are in fault contact with Mesoproterozoic rocks. Formations of Cambrian and Ordovician age of the Kittatinny Valley sequence include the Kittatinny Supergroup, of which the Leithsville Formation, Allentown Dolomite, Richenbach, and Epler Formations are exposed in the quadrangle. Lower Paleozoic rocks are in unconformable contact with Mesoproterozoic rocks north and west of Wawayanda Mountain, and are in fault contact east of Pochuck Mountain. Based on the final acceptance of the Global Stratotype Section and Point base (GSSP) for the Ordovician at Green Point, Newfoundland (Cooper and others, 2001), the Cambrian-Ordovician boundary in New Jersey is currently accepted as occurring within the lower third of the Epler Formation, at the top of the Cordylodus lindstromi zone, within conodont fauna B as used in Karklins and Repetski (1989). Therefore, the Allentown and Rickenbach Dolomite are currently regarded as Cambrian in age and not Ordovician and Cambrian as shown on previous bedrock geologic maps.
Mesoproterozoic rocks Mesoproterozoic rocks consist of an assemblage of granites, gneisses, and marble. Most Mesoproterozoic rocks were metamorphosed to granulite facies during the Ottawan phase of the Grenville orogeny at 1045 to 1024 Ma (Volkert and others, 2010). The temperature for this high-grade metamorphism is constrained from regional calcite-graphite geothermometry to 769oC (Peck and others, 2006). The oldest Mesoproterozoic rocks in the area consist of the Losee Suite and a thick assemblage of supracrustal metavolcanic and metasedimentary rocks. Rocks of the Losee Suite are calc-alkalic in composition and include various quartz-plagioclase gneisses and amphibolite formed from plutonic and volcanic protoliths in a magmatic arc tectonic setting (Volkert, 2004). Rocks of the Losee Suite yield sensi-tive high-resolution ion microprobe (SHRIMP) U-Pb zircon ages of 1282 to 1248 Ma (Volkert and others, 2010). Spatially and temporally associated with the Losee Suite are supracrustal rocks that include micro-cline gneiss and amphibolite formed from felsic and mafic volcanic protoliths, respectively, and quartzofeld-spathic gneisses, calc-silicate rocks, and marble formed from sedimentary protoliths. Supracrustal rocks were deposited in a back-arc basin inboard of the Losee arc (Volkert, 2004). Microcline gneiss yields U-Pb SHRIMP zircon ages of 1299 to 1251 Ma (Volkert and others, 2010) that closely overlap the age of rocks of the Losee Suite. Granite and related rocks of the Byram and Lake Hopatcong Intrusive Suites, that together comprise the Vernon Supersuite (Volkert and Drake, 1998), are abundantly exposed in the area where they intrude Losee Suite and supracrustal rocks. Byram and Lake Hopatcong rocks form a complete differentiation series that includes monzonite, quartz monzonite, granite, and alaskite, all of which have a distinctive A-type geochemical composition (Volkert and others, 2000). Granites of both suites yield similar U-Pb SHRIMP zircon ages of 1188 to 1182 Ma (Volkert and others, 2010). The youngest Mesoproterozoic rocks are postorogenic potassic granites and granite pegmatites that are undeformed, contain xenoliths of foliated gneiss or marble, and intrude other Mesoproterozoic rocks in the map area as small, tabular to irregular bodies that are discordant to metamorphic foliation. The most abundant of these is the Mount Eve Granite which forms two prominent intrusive bodies known as Mt. Adam and Mt. Eve in the Pine Island quadrangle, as well as more than 30 smaller bodies in adjacent quadrangles (Gorring and others, 2004). A sample of Mount Eve Granite collected from Mt. Adam yielded a zircon U-Pb thermal ionization mass spectrometry (TIMS) age of 1020 Ma (Drake and others, 1991a) and a sample collected from Mt. Eve yielded a zircon SHRIMP age of 1019 Ma (Volkert and others, 2010). Other small bodies of granite from the Pine Island quadrangle yielded a zircon U-Pb TIMS age of 1004 Ma (Volkert and others, 2005). Granite pegmatites intrude Mesoproterozoic rocks in the map area as small, tabular to irregular bodies that are highly discordant to crystallization foliation. Elsewhere in the Highlands these pegmatites have yielded zircon U-Pb ages of 990 to 965 Ma (Volkert and others, 2005).
STRUCTUREPaleozoic bedding
Bedding in the Middle Paleozoic rocks is fairly uniform and strikes northeast from N.12oE. to N.50oE. and averages N.33oE. Most beds are upright and dip southeast and, less commonly, northwest, although locally they are overturned. The dip of all beds in the Middle Paleozoic rocks ranges from 34o to 90o and averages 71o (Barnett, 1976; Herman and Mitchell, 1991). Bedding in the Lower Paleozoic rocks forms two populations, one that strikes northeast (N.10oE.to N.65oE.) and one that strikes northwest (N.44oW. to due East) (fig. 1). Most beds dip northwest and, less commonly, southeast. The dip of all beds in Lower Paleozoic rocks ranges from 4o to 90o and averages 26o.
Proterozoic foliation Crystallization foliation, formed by the parallel alignment of mineral grains in the Mesoproterozoic rocks, defines the trend of the bedrock. It is an inherited feature from compressional stresses during granulite-facies metamorphism that deformed the rocks between 1045 and 1024 Ma (Volkert and others, 2010). Foliations in the Wawayanda quadrangle strike mainly northeast at an average of N.25oE. (fig. 2), but locally, in the hinges of folds, they strike northwest due to deformation of the rocks during folding. Foliations dip southeast and, less commonly, northwest at 12o to 90o and average 66o. Northwest-striking foliations dip gently to moderately northeast. Foliations in the Pine Island quadrangle are more varied due to the extent of folding of the rocks. Here, foliations fall into three main groups that average N.15oE., N.15oW., and N.65oW. (fig. 3). Northeast-striking foliations dip mainly southeast and northwest-striking foliations dip mainly southwest. The dip of all foliations ranges from 5o to 85o and averages 22o, but most dips are less than 40o.
Folds Folds in the Lower Paleozoic rocks were formed during the Taconian and Alleghanian orogenies at about 450 Ma and 250 Ma, respectively, and in the Middle Paleozoic rocks during the Alleghanian orogeny. Folds in the Middle Paleozoic rocks have axial surfaces that trend northeast, and they are open to tight, upright to locally overturned, and gently inclined to recumbent anticlines and synclines (Barnett, 1976; Herman and Mitchell, 1991). Most folds plunge gently southwest. Folds in the Lower Paleozoic rocks have northeast-trending axial surfaces, and they are open, upright to locally overturned and form gently north-plunging anticlines and synclines. Folds that deform Mesoproterozoic rocks originated during the Ottawan phase of the Grenville orogeny. They deform earlier-formed planar metamorphic fabrics and, therefore, postdate the develop-ment of crystallization foliation. Characteristic fold patterns are broad, open, northwest-verging to locally upright, northeast-plunging antiforms and synforms. Mineral lineation plunges parallel to the axes of major folds. Plunges range from 7o to 52o and average 26o to N.36oE.
Faults
The structural geology of the bedrock units is dominated by northeast-trending faults that deform Mesoproterozoic and Paleozoic rocks. These faults were active during the Grenville, Taconic and Allegha-nian compressional orogenies and during Neoproterozoic and Mesozoic extensional events. From the northwest, they include the Glenwood, East, Vernon, DeKay, Highland Lake, Wawayanda Lake, Laurel Pond, and Reservoir fault. Most faults exhibit brittle deformation features that include brecciation, recrystallization, and low-temperature retrogression of mafic minerals, chlorite or epidote-coated slickensides, and closely-spaced fracture cleavage. Ductile deformation features include mylonite, shear band foliation, and boudinage. On some faults these are locally overprinted by brittle deformation features. The Glenwood fault extends through the center of Pochuck Mountain where it is bounded by Mesoproterozoic rocks along most of its length almost to Pine Island, and from there, by Paleozoic rocks extending north. The fault strikes about N.15oE. and dips northwest about 80o. The latest movement appears to have been reverse with a high-angle oblique component. The fault exhibits brittle deformation features. The East fault borders the west side of Vernon Valley where Mesoproterozoic rocks on the footwall abut Lower Paleozoic rocks on the hanging wall. The fault strikes N.45oE. and dips about 80o southeast. In the map area, the latest movement was normal, although along strike to the south, kinematic indicators record steep reverse movement. The fault exhibits brittle deformation features. The Vernon fault extends along the west side of Wawayanda Mountain where it is bounded by Mesoproterozoic rocks along most of its length to the town of Vernon. Here it offsets the contacts of Lower Paleozoic rocks. The fault strikes N.15oE. and dips southeast at about 60o. The latest movement appears to have been normal. The fault exhibits brittle deformation features.
The DeKay fault extends along the western base of Wawayanda Mountain west to Vernon where it appears to be cut off by the Vernon fault. It is bounded by Mesoproterozoic rocks at its southern end and by Lower Paleozoic rocks at its northern end which are offset. The fault strikes N.40oE. and dips about 80o northwest. The latest movement appears to have been normal. The fault exhibits brittle deformation features. The Highland Lake fault extends through the western part of Wawayanda Mountain where it is bounded by Mesoproterozoic rocks. To the south it merges with, or is cut off by, the Vernon fault. To the north its extent is unknown beyond the area of Highland Lake. The fault strikes N.20oE. to N.40oE. and dips about 75o southeast. The latest movement appears to have been normal. The fault exhibits brittle deformation features. The Wawayanda Lake fault extends through the central part of Wawayanda Mountain where it is bounded by Mesoproterozoic rocks. The fault bifurcates east of Highland Lake, and the main segment extends northeastward through Wawayanda Lake. To the north the presence of both fault segments is unknown, however the main segment does not seem to offset the Lower Paleozoic rocks. The fault strikes N.15oE.to N.35oE. and dips about 75o southeast. The latest movement appears to have been normal. The fault exhibits brittle deformation features. The Laurel Pond fault extends along the east side of Wawayanda Mountain where it is bounded by Mesoproterozoic rocks. The strike is somewhat varied and ranges from N.40oE. to N.70oE. The dip is about 50o northwest. The latest movement appears to have been normal. The fault exhibits brittle deformation features. The Reservoir fault extends from New York State southwest to Schooleys Mountain (Drake and others, 1996). In the map area the fault places Paleozoic rocks on the hanging wall against Mesoprotero-zoic rocks on the footwall, but to the south it is bounded by Mesoproterozoic rocks on both sides. The fault strikes N.30oE. and dips 80o northwest to vertically. It has undergone multiple reactivations dating from the Proterozoic that reflect a complex deformation history involving normal, right-lateral strike slip, and reverse movement, with the latest movement having been normal. The fault exhibits ductile deformation features that are overprinted by brittle features. Timing of fault movement based on 40Ar/39Ar isotope analysis yielded disturbed spectra, indicating resetting of amphiboles at about 722 Ma, and biotite inclusions in amphibole at about 322 Ma (Price, 2005), likely due to the effects of hydrothermal fluid movement along the fault. Mesoproterozoic and Paleozoic rocks are also deformed by small faults that strike northeast or northwest. These faults range from a few inches to a few feet wide and are of short length. They are characterized mainly by brittle deformation features.
Joints Joints are a common feature in the Paleozoic and Mesoproterozoic rocks. They are best devel-oped in massive rocks such as Paleozoic limestone, dolomite, and sandstone, and in Mesoproterozoic granite and some gneiss. Joints are characteristically planar, moderately well formed, moderately to widely spaced, and moderately to steeply dipping. Their surfaces are typically unmineralized, except near faults, and are smooth or less commonly, slightly irregular. Joints vary in their spacing from one foot to tens of feet apart. Those formed close to faults are spaced two feet or less apart. Joint data for the Middle Paleozoic rocks are shown on the map of Herman and Mitchell (1991) and are not shown here. Joints in the Lower Paleozoic rocks form two populations that have average strikes of N.65oW. and N.40oE. (fig. 4). Northwest-striking joints dip mainly southwest, whereas the northeast-striking joints dip mainly southeast. The dip of all joints ranges from 44o to 90o and averages 75o. The dominant joints in Mesoproterozoic rocks are nearly perpendicular to the strike of crystalliza-tion foliation, a consistent feature observed throughout the Highlands (Volkert, 1996). Therefore, the strike of joints is somewhat varied because of folding of the rocks. In the Wawayanda quadrangle the dominant joints strike N.67oW. on average (fig. 5) and dip 18o to 90o mainly southwest at an average of 70o. In the Pine Island quadrangle principal joint sets were measured that strike northwest at an average of N.70oW. and northeast at an average of N.20oE. (fig. 6). Northwest-striking joints dip nearly equally southwest and northeast and northeast-striking joints dip mainly southeast. The dip of all joints ranges from 56o to 90o and averages 79o.
ECONOMIC RESOURCES Mesoproterozoic rocks in the map area host economic deposits of iron ore (magnetite) that were mined predominantly during the 19th century. Detailed descriptions of most of the mines are given in Bayley (1910). Mount Eve Granite was formerly quarried at several locations on Mount Adam and Mount Eve for use as dimension stone. Marble was quarried for agricultural use as fertilizer east of Pochuck Mountain and south of Pine Island, and dolomite was quarried in Orange County, N.Y. Deposits of sand and gravel and peat were formerly worked in the area and organic-rich “black dirt” in the area of Pochuck Creek currently supports robust agricultural activity.
DESCRIPTION OF MAP UNITS
GREEN POND MOUNTAIN REGION
Skunnemunk Conglomerate (Middle Devonian) (Darton, 1894) – Grayish-purple to grayish-red, thin- to very thick bedded, locally cross-bedded, polymictic conglomerate and sandstone containing clasts of white vein quartz, red and green quartzite and sandstone, red and gray chert, and red shale; interbedded with medium-gray, thin-bedded sandstone and greenish-gray and grayish-red, mud-cracked shale. Conglomerate and sandstone matrix is primary hematite and microcrystalline quartz. Conglomerate cobbles are as much as 6.5 in. long, and average cobble size is larger in upper part of unit. Lower contact is conformable and gradational as defined by Kümmel and Weller (1902). Unit is about 3,000 ft thick.
Bellvale Sandstone (Middle Devonian) (Bellvale Flags of Darton, 1894; Willard, 1937) – Upper beds are grayish-red to grayish-purple sandstone containing quartz pebbles as large 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. Sandstone more common in upper beds and is finer downward. Lower contact conformable with the Cornwall Shale and placed where beds are thicker 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 shale, interbedded with medium-gray and light-olive-gray to yellowish-gray, laminated to very thin-bedded siltstone that is more abundant 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 Formation)
Kanouse Sandstone (Kümmel, 1908) – Medium-gray, light-brown, and grayish-red, fine to coarse-grained, thin to thick-bedded sandstone and pebble conglomerate. Basal conglom-erate 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 gradational. 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 probably 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 con-glomerate 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 transitional 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 conformable with Green Pond Conglomerate. Unit is about 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, or is in fault contact with, Mesoproterozoic rocks. Unit is about 1,000 ft. thick.
KITTATINNY VALLEY SEQUENCE
Epler Formation (Lower Ordovican and Upper Cambrian) (Hobson, 1957) – Upper part is light-olive to dark-gray, fine to medium-grained, thin to thick-bedded, locally laminated dolomite. Middle part is olive-gray, light-brown, or dark-yellowish-orange-weathering, dark-gray, aphanitic to fine-grained, laminated to medium-bedded dolomite, and light-gray to light-bluish-gray-weathering, medium-dark to dark-gray, fine-grained, thin to medium-bedded limestone, that is characterized by mottling and reticulate dolomite and light-olive-gray to grayish-orange-weathering, medium-gray dolomitic shale laminae surrounding the limestone lenses. Limestone grades laterally and down section into medium-gray, fine-grained dolomite. Lower part is medium-light to dark-gray, aphanitic to medium-grained, laminated to medium-bedded dolomite. Contains lenses of white and dark-gray chert. Lower contact is placed at the transition from a massive laminated, very fine-grained, dark-gray dolomite to the underlying massive light-gray, medium to coarse-grained pitted dolomite that occurs about 50 to 75 feet above a thinly interbedded sequence of medium-grained dolomite and as many as seven, thin, black, convex-upward chert layers. Unit contains conodonts of Cordylodus lindstomi to Rossodus manitouensis zones of the North American Midcontinent Province as used by Sweet and Bergstrom (1986). Unit is approximately 420 ft. thick.
Rickenbach Dolomite (Upper Cambrian) (Hobson, 1957) – Upper part is medium to dark-gray, fine to coarse-grained, medium to thick-bedded dolomite, locally fetid, mottled, weathered surface. Contains pods and lenses of dark-gray to black chert near the upper contact. Lower part is medium to dark-gray, fine to medium-grained, thin to medium-bedded dolomite. Floating quartz sand grains and quartz-sand stringers occur in the basal part of unit. Lenses of light-gray, coarse to very-coarse-grained dolomite locally occur throughout the unit. Lower contact placed at top of distinctive medium-gray quartzite. Contains conodonts of Cordylodus proavus to Cordylodus lindstomi zones of North American Midcontinent Province, as used by Sweet and Bergstrom (1986). Unit is as much as 200 ft. thick.
Allentown Dolomite (Upper Cambrian) (Wherry, 1909) – Upper sequence is light to medium-gray-weathering, medium-light to medium-dark-gray, fine to medium-grained, locally coarse-grained, medium to very-thick-bedded dolomite; local shaly dolomite near the bottom. Floating quartz sand and two intervals of medium-light to very-light-gray, medium-grained, thin-bedded quartzite and discontinuous dark-gray chert lenses occur directly below upper contact. Lower sequence is medium to very-light-gray-weathering, light to medium-dark-gray, fine to medium-grained, thin to medium-bedded dolomite and shaly dolomite. Weathered exposures characterized by alternating light- and dark-gray beds. Ripple marks, ooids, algal stromatolites, cross-beds, edgewise conglomerate, mud cracks, and paleosol zones occur throughout but are more abundant in the lower sequence. Unit grades down into the Leithsville Formation. Elsewhere, contains a trilobite fauna of Dresbachian (early Late Cambrian) age (Weller, 1903; Howell, 1945). Unit is approximately 1,800 ft. thick.
Leithsville Formation (Middle and Lower Cambrian) (Wherry, 1909) – Upper sequence, seldom exposed, is mottled, medium-light to medium-dark-gray-weathering, medium to medium-dark-gray, fine to medium-grained, medium to thick-bedded dolomite, locally pitted and friable. Middle sequence is grayish-orange, light to dark-gray, grayish-red, or light-greenish to dark-greenish-gray-weathering, fine-grained, thin to medium-bedded dolomite, ar-gillaceous dolomite, dolomitic shale, quartz sandstone, siltstone and shale. Lower sequence is medium-light to medium-gray-weathering, medium-gray, fine to medium-grained, thin to medium-bedded dolomite. Quartz-sand lenses occur near lower gradational contact with Hardyston Quartzite. Archaeocyathids of Early Cambrian age were found in the formation in Franklin, New Jersey, suggesting an intraformational disconformity between Middle and Early Cambrian strata (Palmer and Rozanov, 1967). Unit also contains Hyolithellus micans (Offield, 1967; Markewicz, 1968). Thickness is approximately 600 ft. Hardyston Quartzite (Lower Cambrian) (Wolff and Brooks, 1898) – Medium to light-gray, fine to coarse-grained, medium to thick-bedded quartzite, arkosic sandstone and dolomitic sandstone. Elsewhere, contains Scolithus linearis(?) and fragments of the trilobite Olenellus thompsoni of Early Cambrian age (Nason, 1891; Weller, 1903). Thickness is as much as 40 ft.
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NEW JERSEY HIGHLANDSOther Rocks
Mount Eve Granite (Mesoproterozoic) – Pinkish-gray or buff-weathering ,pinkish-white or light-pinkish-gray, medium to coarse-grained, massive, unfoliated granite composed principally of microcline microperthite, quartz, oligoclase, horblende, and biotite. Locally contains xenoliths of foliated country rock. Includes bodies of pegmatite too small to show on map.
Vernon Supersuite (Volkert and Drake, 1998)Byram Intrusive Suite (Drake and others, 1991b)
Hornblende granite (Mesoproterozoic) – Pinkish-gray or buff-weathering, pinkish-white or light pinkish-gray, medium to coarse-grained, foliated granite and sparse granite gneiss composed principally of microcline microperthite, quartz, oligoclase, hornblende, and magne-tite. Some variants are quartz syenite or quartz monzonite. Locally contains clinopyroxene where in contact with rocks of the Lake Hopatcong Intrusive Suite. Includes small bodies of pegmatite too small to show on map.
Hornblende monzonite (Mesoproterozoic) – Tan or buff-weathering, pinkish-gray or greenish-gray, medium to coarse-grained, foliated monzonite and, less commonly, quartz monzonite composed of microcline microperthite, oligoclase, hornblende, and magnetite. Locally contains quartz. Sparse to moderate amounts of clinopyroxene may be present where in contact with rocks of the Lake Hopatcong Intrusive Suite.
Lake Hopatcong Intrusive Suite (Drake and Volkert, 1991)
Pyroxene granite (Mesoproterozoic) – Light gray, buff, or white-weathering, greenish-gray, medium to coarse-grained, massive, foliated granite composed of mesoperthite to microanti-perthite, quartz, oligoclase, and clinopyroxene. Commonly contains titanite, magnetite, apatite, and pyrite. Sparse to moderate amounts of hornblende may be present where in contact with rocks of the Byram Intrusive Suite. Includes small bodies of pegmatite too small to show on map.
Pyroxene alaskite (Mesoproterozoic) – Light-gray or tan-weathering, greenish-buff or light pinkish-gray, medium to coarse-grained, massive, foliated granite composed of mesoperthite to microantiperthite, oligoclase, and quartz. Commonly contains clinopyroxene, titanite and magnetite. Occurs in a pair of bodies east of Highland Lake.
Pyroxene monzonite (Mesoproterozoic) – Gray, buff, or tan-weathering, greenish-gray, medium to coarse-grained, massive, foliated rock composed of mesoperthite to microantiper-thite, oligoclase, clinopyroxene, titanite and magnetite. Locally contains hornblende where in contact with rocks of the Byram Intrusive Suite. Crops east and west of the Vernon fault.
Back-Arc Supracrustal Rocks
Potassic feldspar gneiss (Mesoproterozoic) – Light-gray or pinkish-buff-weathering, pinkish-white or light pinkish-gray, fine to medium-grained, moderately foliated gneiss and less abundant granofels composed of quartz, microcline microperthite, and varied amounts of biotite, garnet, sillimanite, and magnetite. Locally contains thin, sparsely garnetiferous quartzite layers. Exposed sporadically throughout the map area, but is most abundant in the vicinity of Highland Lake.
Microcline gneiss (Mesoproterozoic) – Tan or pale pinkish-white-weathering, light-gray or pinkish-gray, fine to medium-grained, layered and foliated rock composed principally of microcline microperthite, quartz, and oligoclase. Common accessory minerals include biotite, garnet, sillimanite, and magnetite. Unit is well exposed in the northwest part of the map area.
Biotite-quartz-feldspar gneiss (Mesoproterozoic) – Gray-weathering, locally rusty-weathering, gray, tan, or greenish-gray, medium to coarse-grained, moderately layered and foliated gneiss containing microcline microperthite, oligoclase, quartz, and biotite. Locally contains garnet, sillimanite, graphite, and opaque minerals. Commonly contains thin layers of quartzite that may contain graphite and biotite. Unit is most abundant north of Upper Greenwood Lake.
Hornblende-quartz-feldspar gneiss (Mesoproterozoic) – Pinkish-gray or buff- weathering, pinkish-white or pinkish-gray, fine to medium-grained, moderately well layered and foliated gneiss composed of microcline, quartz, oligoclase, and hornblende. Locally contains garnet, magnetite, and biotite. Unit occurs throughout the map area.
Clinopyroxene-quartz-feldspar gneiss (Mesoproterozoic) – Pinkish-gray or pinkish-buff- weathering, white, pale-pinkish-white, or light-gray, fine to medium-grained, moderately foli-ated gneiss composed of quartz, microcline, oligoclase, clinopyroxene, and trace amounts of epidote, biotite, titanite, and opaque minerals. Commonly contains thin layers of amphibolite. Unit is present throughout the map area, but is most abundant south and east of Wawayanda Lake.
Pyroxene gneiss (Mesoproterozoic) – White or tan-weathering, greenish-gray, medium-fine to medium-grained, layered and foliated gneiss containing oligoclase and clinopyroxene. Quartz content is highly varied. Contains sparse amounts of epidote, titanite, scapolite, or calcite. Commonly interlayered with pyroxene amphibolite or marble. Unit is abundantly exposed throughout the map area.
Marble (Mesoproterozoic) – White or light-gray-weathering, white, grayish-white, or less commonly pinkish-orange, fine to coarse-grained, calcitic to locally dolomitic marble with accessory graphite, phlogopite, chondrodite, and clinopyroxene. Contains pods and lenses of clinopyroxene-garnet skarn, hornblende skarn, and clinopyroxene-rich rock. Divided by Hague and others (1956) into a lower Franklin marble (Yff) and an upper Wildcat marble (Yfw) separated by a layered sequence of gneiss. Locally contains relict karst features in the form of bedrock pinnacles and solution joints and openings. Unit is best exposed in the northwestern part of the map area in Vernon Valley.
Amphibolite (Mesoproterozoic) – Grayish-black, medium-fine to medium-grained, foliated rock composed of hornblende and andesine. Some amphibolite also contains abundant clinopyroxene (Yap). Unit is associated with most Mesoproterozoic rocks in the map area. Amphibolite associated with the Losee Suite is metavolcanic in origin, and that associated with supracrustal rocks may be metavolcanic or metasedimentary in origin. All types are shown undifferentiated on the map. Unit is best exposed on Pochuck Mountain. It locally contains relict pillow structures (Hague and others, 1956) and forms a bimodal sequence of volcanic rocks with microcline gneiss.
Magmatic Arc RocksLosee Metamorphic Suite (Drake, 1984; Volkert and Drake 1999)
Quartz-oligoclase gneiss (Mesoproterozoic) – White-weathering, light greenish-gray, medium to coarse-grained, moderately layered to foliated gneiss composed of oligoclase or andesine, quartz, and local hornblende, biotite, and clinopyroxene. Commonly contains thin, conformable layers of amphibolite. Best exposed north and west of Canistear Reservoir. Biotite-quartz-oligoclase gneiss (Mesoproterozoic) – White or light-gray-weathering, medium-gray or greenish-gray, medium to coarse-grained, layered and foliated gneiss composed of oligoclase or andesine, quartz, and biotite. Some outcrops contain garnet or hornblende. Locally interlayered with amphibolite. Best exposed in the eastern part of the map area.
Hornblende-quartz-oligoclase gneiss (Mesoproterozoic) – White-weathering, light greenish-gray, medium to coarse-grained, foliated gneiss containing oligoclase or andesine, quartz, hornblende, and magnetite. Crops out in one small body southwest of Highland Lake.
Hypersthene-quartz-plagioclase gneiss (Mesoproterozoic) – Gray or tan-weathering, greenish-gray or greenish-brown, medium-grained, layered and foliated gneiss composed of andesine or oligoclase, quartz, clinopyroxene, hornblende, and hypersthene. Contains thin, conformable layers of amphibolite and mafic-rich quartz-plagioclase gneiss. Crops out near Canistear Reservoir, in the southwestern part of the map area.
Diorite (Mesoproterozoic) – Gray or tan-weathering, greenish-gray or greenish-brown, medium to coarse-grained, massive, foliated rock containing andesine or oligoclase, clinopyroxene, hornblende, and hypersthene. Commonly contains thin mafic layers or schlieren having the composition of amphibolite. Crops out in one small body in Orange County, New York.
Undifferentiated rocks (Mesoproterozoic) – Shown in cross section only.
OCe
Cr
Ca
Cl
Ch
Yu
Ygm
Ybh
Ybs
Ypa
Ym
Yb
Ylb
Ypg
Yps
Yk
Ymh
Ymp
Yp
Yff Yfw
Ylh
Yh
Yd
Ylo
byRichard A. Volkert and Donald H. Monteverde
2014
BEDROCK GEOLOGIC MAP OF THE WAWAYANDA QUADRANGLE AND THE NEW JERSEY PART OF THE PINE ISLAND QUADRANGLE
SUSSEX AND PASSAIC COUNTIES, NEW JERSEY AND ORANGE COUNTY, NEW YORK
Ya Yap
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, 9 p.Bayley, W.S., 1910, Iron mines and mining in New Jersey: New Jersey Geological Survey Final Report VII, 512 p.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. Cooper, R.A., Nowlan, G.S., and Williams, S.H., 2001, Global Stratotype Section and Point for base of the Ordovician System: Episodes, v. 24, no. 1, p. 19-28.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., Aleinikoff, J.N., and Volkert, R.A., 1991a, The Mount Eve Granite (Middle Proterozoic) of northern New Jersey and southeastern New York, in Drake, A.A., Jr., ed., Contributions to New Jersey Geology: U.S. Geological Survey Bulletin 1952, p. C1-C10._________, 1991b, The Byram Intrusive Suite of the Reading Prong - Age and tectonic environment, in Drake, A.A., Jr., ed., Contributions to New Jersey Geology: U.S. Geological Survey Bulletin 1952, p. D1-D14.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., Estelle, T.C., and Volkert, R.A., 2004, Geochemistry of the late Mesoproterozoic Mount Eve Granite: implications for late- to post-Ottawan tectonics in the New Jersey-Hudson Highlands, 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. 505-524. Hague, J.M., Baum, J.L., Hermann, L.A., and Pickering, R.J., 1956, Geology and structure of the Franklin-Sterling area, New Jersey: Geological Society of America Bulletin, v. 67, p. 435-474.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.Hobson, J.P., 1957, Lower Ordovician (Beekmantown) succession in Berks County, Pennslyvania: American Association of Petroleum Geologists Bulletin, v.14, p. 2710-2722.Howell, B.F., 1945, Revision of Upper Cambrian faunas of New Jersey: Geological Society of America Memoir 12, 46 p.Karklins, O.L. and Repetski, J.E., 1989, Distribution of selected Ordovician Conodont fauns in Northern New Jersey, U.S. Geological Survey Map MF-2066, scale 1:185,000. Kümmel, H.B., 1908, Paleozoic sedimentary rocks of the Franklin Furnace quadrangle, New Jersey, in Spencer, A.C., Kümmel, 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.Kümmel, H.B., and Weller, Stuart, 1902, The rocks of the Green Pond Mountain region: New Jersey Geological Survey Annual Report of the State Geologist, 1901, p. 1-51.Markewicz, F.J., 1968, The Hardyston-Leithsville contact and significance of “Hyolithellus micans” in the lower Leithsville Formation: [abs.], New Jersey Academy of Science Bulletin, v. 13, p. 96.Markewicz, F.J., and Dalton, R.F., 1977, Stratigraphy and applied geology of the lower Paleozoic carbonates in northwestern New Jersey: in 42nd Annual Field Conference of Pennsylvania Geologists, Guidebook, 117 p.Nason, F.L., 1891, The Post-Archaen age of the white limestone of Sussex County, New Jersey: New Jersey Geological Survey Annual Report of the State Geologist, 1890, p. 25-50.Offield, T.W., 1967, Bedrock geology of the Goshen-Greenwood Lake area, New York: New York State Museum and Science Service Map and Chart Series, no. 9, 78 p.Palmer, A.R., and Rozanov, A.Y., 1967, Archaeocyatha from New Jersey: Evidence for an intra- formational unconformity in the north-central Appalachians: Geology, v. 4, p. 773-774.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.Price, R.E., 2005, 40Ar/39Ar evidence for early (700 Ma) Iapetan oblique divergence in the Highlands region, NJ-NY-PA, unpublished MS thesis, Rutgers University, Newark, NJ, 36 p.Rogers, H.D., 1836, Report on the geological survey of the State of New Jersey: Philadelphia, Desilver, Thomas, & Co., 174 p. Sweet, W.C., and Bergstrom, S.M., 1986, Conodonts and biostratigraphic correlation: Annual Review of Earth and Planetary Science, v. 14, p. 85-112.Vanuxem, Lardner, 1842, Geology of New York, part III, comprising the survey of the third geological district: Albany, N.Y., 306 p. 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 Geolo- gists, p. A1-A33.________, 2004, Mesoproterozoic rocks of the New Jersey Highlands, north-central Appalachians: petrogenesis 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. 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 geochronology, in Tollo, R.P., Bartholomew, M.J., Hibbard, J.P., and Karabinos, P.M., eds., From Rodinia to Pangea: The Lithotectonic 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, 77 p.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., Zartman, R.E., and Moore, P.B., 2005, U-Pb zircon geochronology of Mesoproterozoic postorogenic rocks and implications for post-Ottawan magmatism and metallogenesis, New Jersey Highlands and contiguous areas, USA: Precambrian Research, v. 139, p. 1-19.Weller, Stuart, 1903, The Paleozoic faunas: New Jersey Geological Survey, Report on Paleontology, v. 3, 462 p.Wherry, E.T., 1909, The early Paleozoics of the Lehigh Valley district, Pennsylvania: Science, new series, v. 30, 416 p.White, I.C., 1882, The geology of Pike and Monroe Counties: Pennsylvania Geological Survey, 2nd series, Report G-6, 407 p.Willard, Bradford, 1937, Hamilton correlation: American Journal of Science, 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. 431-456.
ORDOVICIAN
SILURIAN
DEVONIAN
CAMBRIAN
MESOPROTEROZOIC
UNCONFORMITY
UNCONFORMITY
Kittatinny Valley Sequence
KittatinnySupergroup
NEW JERSEY HIGHLANDS
Ygm
Dkec
Dcw
Dsk
Dbv
Sbp
Sl
Sg
CORRELATION OF MAP UNITS
OCe
Ca
Cr
Cl
Ch
INTRUSIVE CONTACTS
Mesoproterozicundivided
VALLEY AND RIDGE
GREEN POND MOUNTAIN REGION
Yk Ym Yb YmpYmhYlh Yh YdYlo Ylb
Ybh Ybs Ypg YpsYpa
Back Arc Supracrustal Rocks
Ya YapYp Yff Yfw
Magmatic Arc Rocks
Vernon Supersuite Byram Intrusive Suite Lake Hopatcong Intrusive Suite
Losee Suite
Yu
INTRUSIVE CONTACTS
N
%
Avg trend = N64 ESector size = 10n = 111
o
o
3
6
9
12
Figure 1. Rose diagram of bedding strikes in Lower Paleozoic rocks of the Kittatinny Valley sequence.
N
%
Avg trend = N86 WSector size = 10n = 71
o
o
8 10
10
8
6
Figure 4. Rose diagram of joint strikes in Lower Paleozoic rocks of the Kittatinny Valley sequence.
N
%9 12
12
9
6
Avg trend = N67 WSector size = 10n = 723
o
o
Figure 5. Rose diagram of joint strikes in Mesoproterozoic rocks of the Wawayanda quadrangle.
N
%
Avg trend = N06 ESector size = 10n = 62
o
o
104 6 8
Figure 3. Rose diagram of crystallization foliation strikes in Mesoproterozoic rocks of the Pine Island quadrangle.
N
%
Avg trend = N82 WSector size = 10n = 95
o
o
96 12 15
6
3
9
12
15
Figure 6. Rose diagram of joint strikes in Mesoproterozoic rocks of the Pine Island quadrangle.
N
%15 525
Avg trend = N25 ESector size = 10n = 612
o
o
20 10
5
10
15
20
Figure 2. Rose diagram of crystallization foliation strikes in Mesoproterozoic rocks of the Wawayanda quadrangle.
U
UD
D
75
M
30
10
20
30
70
EXPLANATION OF MAP SYMBOLS
Contact - Dotted where concealed
Faults - Dotted where concealed. Queried where uncertain
Normal fault - U, upthrown side; D, downthrown side
Reverse fault - U, upthrown side; D, downthrown side
FOLDS
Folds in Proterozoic rocks showing trace of axial surface, direction and dip of limbs, and direction of plunge.
Antiform
Synform
Overturned antiform
Overturned synform
Minor asymmetric fold
Folds in Paleozoic rocks showing trace of axial surface, direction and dip of limbs, and direction of plunge. Folds are in bedding.
Anticline
Syncline
PLANAR FEATURES
Strike and dip of crystallization foliation
Inclined
Vertical
Strike and dip of mylonitic foliation
Strike and dip of beds - Ball indicates top of beds known from sedimentary structures
Inclined
Vertical
Overturned
Strike and dip of spaced cleavage in Paleozoic rocks
LINEAR FEATURES
Bearing and plunge of mineral lineation in Proterozoic rocks
Bearing and plunge of interesection of bedding and cleavage in Paleozoic rocks
OTHER FEATURES
Abandoned magnetite mine
Abandoned quarry
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