DEPARTMENT OF ENVIRONMENTAL PROTECTION Prepared in cooperation with the GEOLOGIC MAP OF THE PORTION WATER RESOURCES MANAGEMENT U.S. GEOLOGICAL SURVEY OF THE LUMBERVILLE QUADRANGLE NEW JERSEY GEOLOGICAL AND WATER SURVEY NATIONAL GEOLOGIC MAPPING PROGRAM HUNTERDON COUNTY, NEW JERSEY

GEOLOGIC MAP SERIES GMS 18-2

N FRENCHTOWN PITTSTOWN 75o05’00 75o02’0 75o00’ o o 0 0’00 A 0 0’00 Contour Plot ately sorted, weakly stratified. Deposits along Lockatong Creek are chiefly flag- 8 5 7 8 7 INTRODUCTION CORRELATION OF MAP UNITS Qe p Qal p 9 D F Fishing 6 8 p 16

R 200 7 4 D stone gravel composed of gray and red mudstone, with a matrix of reddish-brown FARM Qcs 8 11 14 L RD 8 4 40 R 12 The Lumberville 7.5-minute topographic quadrangle lies within the Piedmont R 300 L Island Qw 4 8 10 Qcal 10 Qcal 0 p Qcal E U Qst 4 N 10 to grayish-brown silt, and are generally less than 10 feet thick. They form terraces H 50 M S 5 0 O 6 SURFICIAL 2 8 I physiographic province, Hunterdon County, west central New Jersey and Bucks E 300 Qal 5 6 HO 4 6 R N 5 to 10 feet above the modern floodplain and are likely of late Wisconsinan age. T Qcal SES Percent D  T 10 H U R O 500 per 1% area County, . The region has not succumbed to the “growing” pressures E Qcal pg E p K T 9 B Deposits along the Delaware River are chiefly yellowish-brown silt and fine sand L  6 5 E Qcal Qal A Holocene N 5 10 15 from suburban development and continues to maintain a rural character. The Del-  Qcal D W 7 R as much as 25 feet thick that form a terrace 15 to 20 feet above the modern flood- E p D P Qcal Qa Qal Qcal p aware River bisects the quadrangle in a north-south direction before swinging in a O  5 plain. They rest on a strath cut into the glaciofluvial gravel (unit Qwf) and so are of R C E 8 12 FAIRVIEW RD more easterly direction down stream. N Qst T 7 0 postglacial age. E Qcal 50 0 5 R 00 pg 0 2 T  lateR Pleistocene 7 1 0 1 0 D H p 200 0 10 pg 5 A 0 The bedrock controls the variable topography in the quadrangle. The Qe p T Qw C 11 Shale, , and Mudstone Colluvium - Silt, sandy silt, clayey silt, red- 300 Qcal H Hunterdon Plateau occupies the northern section of the quadrangle with topo- Qcs  E Qcs Qal R dish-brown to yellowish-brown, with some to many subangular flagstones, chips, erosion Qcs p 300 pg 2a graphic elevations ranging from about 400 to 500 feet. The surface water drainage  Qal p R TINICUM D N = 35 and pebbles of red and gray shale, mudstone, and minor sandstone. Poorly sorted, 200 CRE Qst D patterns on the plateau dominantly align in a northeast-southwest direction which 300 E Qcal pg Qcal KE R Qi middle Pleistocene 2 DY nonstratified to weakly stratified. Flagstones and chips have strong slope-parallel  N Camp 8 pg P Qal 00 L 0 O parallels the bedrock strike. Lockatong Creek transects the plateau with a south- 4 R 0 alignment of a-b planes. The unit is as much as 30 feet thick and forms footslope A 1 Wilson 7 9 N erosion  D pg  E wardly trend and drains into the Delaware River. Abundant rock ledges frequently C Qcal aprons along base of hillslopes. It is chiefly of late Wisconsinan age. early Pleistocene- HIDDEN crop out along its banks. The quadrangle has more muted topography in the south 0 Qw Qcal Qps  0 Contour Plot 3 5 Pliocene 10

 with topographic elevations ranging from about 100 to 200 feet. D N pg BREEZE R 8

NT L D Marshall OI Eolian Deposits - Silt and very fine-to-fine sand, reddish yellow. Well-sorted, non- Qcal ERTOWN P 8 6

R RB

Qe BA n Y 4

T Barbertown R stratified. As much as 3 feet thick. These are windblown deposits blown from the Y i Island Qcs 8 p u 2 E n B U BEDROC D i pg 13 R Percent c 0 L R u r The bedrock within the Mesozoic-aged was formed by the depo- m C E B

0 L p D R L y per 1% area N 9 ION N 1 STAT glaciofluvial plain in the Delaware River valley. A R D WOO L d Qw KING A V O I sition of sediments and subsequent intrusion of within a half-graben rift 0 7 d T

NEWAR BASIN Vansant H 0 S

E 3 2 Qal 7 u S 0 W L

G 0 O N M

basin formed during the breakup of the Pangea . The Newark basin D Airport L 0 5 10 15 I 0 L Qal Pinkertons Island 12 4

Late Wisconsinan Glaciofluvial Deposit - Pebble-to-cobble gravel and pebbly R O 13 pg Qcal  H Qal 0 Qcs is filled with - sedimentary and igneous rocks that have been tilted, Qwf 0 0 0 sand, moderately to well-sorted and stratified. Sand is yellowish brown, brown, 1 4 faulted, and locally folded (Schlische, 1992; and Olsen and others, 1996). Most 9 light gray. Gravel includes chiefly red and gray mudstone and sandstone; gray, STA 5 10 M Qcal U

JURASSIC 0 tectonic deformation is probably to Middle Jurassic age (Lucas and  C Qal D AF 0 Shyhawks Island 9 ong l t C D white, and purplish-red and ; and some gray and white FER Cr 1 ka r T T oc Y others, 1988; de Boer and Clifford, 1988). Southeast-dipping normal faults along Sundale Y R 200 inicum Qst L D Qal 5 7 p R and dark-gray chert. Gneiss clasts are unweathered or have a very thin 0 U

0 12 N D p 15 the basin’s northwestern margin primarily influenced the basin morphology, sed- 1

 0 0 R Walls 0 weathered rind. It is as much as 40 feet thick and forms an eroded plain in the J d R

0 3 Qal D

iment deposition patterns, and the orientation of secondary structures within the 3 Y 9 r 2b

 R Island I 13 Delaware River valley with a top surface between 30-60 feet above the modern O e Qcal B 8 N = 199 A 0 11 A 8 O v basin. Episodic, periodic motion on these faults also influenced the position where OLLOW RD 0 C Qcs R i H T 1 C floodplain. Deposited by glacial meltwater descending the Delaware River valley RK C A N 6 R sediment was input to the basin from the Highlands to the northwest, and resulted D N R O E U S 7 F O 9 T during the late Wisconsinan glaciation. Frankenfield Covered Bridge 0 O e R M 0 K N in having a general sediment dispersal pattern parallel to the basin’s long axis r D DQUARTE 3 C D K p D EA RS a 11 R H R 2 R Qcs N

Q U (northeast-southwest). Intrabasinal faulting also occurred during active deposition D 00 W E w 5 Contour Plot Illinoian Glaciofluvial Deposit - Pebble-to-cobble gravel, silty sand, sandy silt, U Qal B TO a A T K (Schlische, 1992, 1993). Differential fault slip along individual segments of the N l C Qif I L O l 14 L N e L R 13 moderately to poorly sorted and stratified. Matrix is reddish-brown to brown. Grav- 0 pg L E Intrusive Contact U D Qcal 12 0 11 O8 border and intrabasinal fault systems resulted in having a series of depressions N M D 9 O 10 0 2 500 I 0 H W el includes chiefly red and gray mudstone and sandstone; gray, purplish-red, and E 2 pg G 6 H N (synforms) and ridges (antiforms) oriented normal to the fault trends along their X 9 p KI 4 E pg r lr 2 white quartzite and conglomerate; and some gray and white gneiss and dark gray D Treasure C Percent p 10 length (Schlische, 1995). Sediment thickening into the fold troughs indicates the Smithtown Qal d RD per 1% area chert. Gneiss and sandstone clasts have thick weathered rinds or are decom- n Island r RD Lily █ fo FO Qcal syndepositional nature of these regional fold structures. Tectonic deformation and 300 r AR lr TRIASSIC 0 18 8 a W 5 10 15 20 posed. As much as 20 feet thick. Forms terrace remnants in the Delaware River  0 Qst W

Conormable Valley 2 10 synchronous sedimentation continued into the Middle Jurassic at which time ex- B 300 Qa Qal Fly-N-D valley with a top surface between up to 100 feet above the modern floodplain. Hoge 8 Qcs Eagles A R pg 8 Kingwood tensional faulting and associated tilting and folding ceased. At this stage, the basin lh Farm Airport pg B Landing Strip Airport M Lair Airport E Deposited by glacial meltwater descending the Delaware River valley during the 30 1 0 U 0 0 R 0 3 l likely experienced a period of post-rift contractional deformation and localized ba- N T I 0 Qcs C 0 O Illinoian glaciation. lr I 40 9 W l T PA sin inversion, which have been recognized in other Mesozoic rift basins (de Boer inicum Cr L l l Resolution 0 N RD 40 200 Rush 7 I and Clifford, 1988; Withjack and others, 1995; R. Schlische, 1996, oral commun.). Island D Qcal Qal - Pebble-to-cobble gravel, minor boulder gravel, in a matrix E Pre-Illinoian Gravel L N Island ED LN L ERB Subsequent erosion of Mesozoic rocks was followed by flexural loading of the Qps Conormable 400 L 10 8 Qa FEATH 2c Qcal R of clayey silt to sandy silt. Poorly sorted, nonstratified to poorly stratified. Matrix 5 Qal A p D N = 172

D passive margin by -age sediments of the Coastal Plain sequence. E I Qal p R is reddish-yellow to yellowish-brown. Gravel includes chiefly red and gray mud- G 11 D Y sr N Y I Qcal E sa 10 R

L 11 stone and sandstone; gray, purplish-red, and white quartzite and conglomerate; B A E Qal L TWIN LEAR RD 15

A

Stratigraphy 0 S

V lr and some gray and white gneiss and dark gray chert. Gneiss and sandstone clasts V 10 0 N 5 l Y 0 Unconormity  L 0 pg l L R 4

I 11 N Contour Plot

Surficial deposits in the Lumberville quadrangle include fluvial, colluvial, Qcal H D L

have thick weathered rinds or are fully decomposed. Quartzite clasts at and near L R Y E I lr L Qcal K RD 4 L l 34 and windblown sediment. The oldest surficial deposit in the quadrangle is deep- the surface are varnished and pitted. As much as 15 feet thick. Caps a bedrock HORN S J RD12 O W O LO E R 30 HOL AW C R pg N G S D 24 N R O A L B ly weathered fluvial gravel (unit Qps) on a bedrock bench about 130 feet above bench near Raven Rock that is 130 feet above the modern floodplain of the Dela- D W 14 16 I W R R 11 Qa Y 8 N Devils Tea ELL RD D B 9 10 BLE ID 0 R 2 the Delaware River near Raven Rock. An erosional lag of quartzite cobbles on a 3 E 8 11 TUM 50 E ware River. Deposited either during or before the pre-Illinoian glaciation. 0 E 8 5 Percent 0 Table 11 M 1 8 A Qal lr per 1% area N Qcal 9 similar bench half-a-mile to the east (open-dot pattern on map) is of similar age P 8 E o BRICK CHURCH RD o 0 8 R 0 27’0 0 27’0 Qcs 0 7 pg C PIC Qcal 1 NI and origin. This deposit is an erosional remnant of fluvial gravel laid down by the 13 00 C GR Diabase (Lower Jurassic and Upper Triassic) - Fine-grained to aphanitic dikes (?) D 2 p Idell OV l 0 E E R 10 20 30 40 50 J^d 0 L Qst 9 10 D Delaware River that may be equivalent to the Pensauken Formation, a Pliocene and sills and medium-grained, discordant, sheet-like intrusion of dark-gray to dark 3 Qal 11 Hillpot r l #"! C 13 fluvial deposit in central New Jersey that formerly extended up the Delaware Valley greenish-gray, sub-ophitic diabase; massive-textured, hard, and sparsely frac- Cem wn R EPLANATION OF MAP SYMBOLS o 9 D E t h N R from the Trenton area. Alternatively, it may be an erosional remnant of pre-Illinoian tured. Composed dominantly of , clinopyroxene, opaque and D it W 4 lr TO H m 0 Tumble Qa LL 500 00 S 0 I glaciofluvial gravel laid down during a glaciation in the early Pleistocene that ad- I 4 M locally . Contacts are typically fine-grained, display chilled, sharp margins L Surficial Map Symbols 8 L Falls Qa 11 vanced to the vicinity of Riegelsville, about 15 miles upvalley from Raven Rock. and may be vesicular adjacent to enclosing sedimentary rock. Exposed in Bryam R Walls l D 00 C 18 Contact - Contacts o units Qal, Qst, Qw, Qi, and Qps are well-deined4 A l Qcal Qcal MILLTOWN Both the Pensauken Formation and the pre-Illinoian glacial deposits are deeply Diabase sheet that intrudes Lockatong Formation located on Route 29 edge of the 00 F Island 10 3 F 2d

by landorms and are drawn rom 1:12,000 stereo airphotos. Contacts o E 8 10 H weathered and are similarly preserved on bedrock straths between 100 and 150 R N = 22

mapped area. E

other units are drawn at slope inlections and are eather-edged or T W Y Qcs feet above the present Delaware River. After deposition of these gravels, the Dela- 13 lr I R gradational. D RD 9 Qal T D R T N 3 LD l W 0 ware River and its tributaries deepened their valleys by 50 to 100 feet into bedrock, - (Upper Triassic) (Olsen, 1980a) - Interbedded sequence O O lr R Passaic Formation T 0 H Qal D ^p - Scattered cobbles o gray and IwhiteT uartzite and in the early and middle Pleistocene (2.5 million ago [2.5 Ma] to 125,000 Gravel lag M 2 lr 9 of reddish-brown to maroon and purple, fine-grained sandstone, siltstone, sha- S 500 Qcal 500 13 uartzite-conglomerate let 4rom00 T ierosionnicum o unit Qps Windward Farms Airport l years ago [125 ka]). 13 Qal ^pg ly siltstone, silty mudstone and mudstone, separated by interbedded olive-gray, E 2 LN Contour Plot IDG 14 R STOCKTON BEDMINSTER l dark-gray, or black siltstone, silty mudstone, shale and lesser silty argillite. Red- Gravel lag - Scattered pebbles and cobbles o gray and white uartzite B 8 2 14 4 l 5 0 0 Qcal 0 0 A glaciation in the middle Pleistocene, probably during the Illinoian Stage at and uartzite-conglomerate, red and gray mudstone and sandstone, and H 2 dish-brown siltstone is medium- to fine-grained, thin- to medium-bedded, planar to RD W 1 TUMBLE FALLS RD Qal 0 lr W O U weathered gray LgneissO let rom erosion o unit Qi. R 0 around 150 ka, advanced to the vicinity of Phillipsburg, about 25 miles upvalley cross-bedded, micaceous, locally containing mud cracks, ripple cross-lamination, L M 6 O A N K H N B 14 Qcal D Qcs 16 Qcal AR SV R T from Raven Rock. Glaciofluvial gravel laid down during this glaciation (unit Qif) root casts and load casts. Shaly siltstone, silty mudstone, and mudstone form D I U Gravel lagE - Scattered pebbles and cobbles o gray and whiteLL uartzite Prahls T 0 E E S 5 10 15 20 25 30 35 C forms a terrace that is as much as 100 feet above the Delaware River east of Ra- 00 R I Qst Qcal 27 rhythmically fining-upward sequences up to 15 feet thick. They are fine-grained, 4 D R and uartzite-conglomerate, red and gray mudstone and sandstone, and W Island K 3 2 T Qal 0 l D D 0 S ven Rock, where the valley widens and terraces are protected from erosion. Else- very-thin- to thin-bedded, planar to ripple cross-laminated, fissile, locally biotur- gray gneiss let rom erosion o unit Qw. R L 18 21

Y A R O Qcs l Qcs 18 R O C where in the Delaware Valley, erosion following this glaciation removed the Illinoian lr E bated, and locally contain evaporate minerals. Gray bed sequences (^pg) are T Qst N Qal Qcal 15 O 12 D Fluvial scarp - Line at top, ticks on slope. Marks ormer channels on40 0 Point E 12 gravel. During the late Wisconsinan glaciation, which reached its maximum extent C l F medium- to fine-grained, thin- to medium-bedded, planar to cross-bedded silt- 14

0

O B terrace suraces in Delaware Valley. Pleasant Qcal 0 00 6

Y 4 at about 25 ka, glaciofluvial gravel was again laid down in the Delaware Valley (unit stone and silty mudstone. Gray to black mudstone, shale and argillite are lam- 4 Qcs R

A 8 0 LN 10 Qwf). This gravel was deposited between about 30 and 20 ka as the glacier ad- inated to thin-bedded, and commonly grade upwards into desiccated purple to 0 OD M Percent 3 O 19 per 1 area RW K vanced into, and then retreated from, the Delaware Valley, reaching as far south as Bedrock Map Symbols EE 15 I reddish-brown siltstone to mudstone. Thickness of gray bed sequences ranges D N Qst 2e D l G 16 N = 433 A W the Belvidere area, about 35 miles upvalley from Raven Rock. Erosional remnants from less than 1 foot to several feet thick. Unit is approximately 11,000 feet thick R D S Qst R TO 1 17 Qcs K O E VE 0 Qal 1 15 ContactH - Solid whereG location known to be accurate. DashedR where 2 0 11 O of this gravel form terraces up to 60 feet above the river east of Raven Rock, on 4 lh P 0 but the upper contact is a nonconformity with the Orange Mountain that can O D A D I R 0 0 L 13 Stover R K 0 Stereonet (left and middle) and rose diagram (right) analysis of fracture trends from surface exposures in the Diabase (2a), Passaic R Figure 2. L R 5 both sides of the river near Marshall Island, and at Point Pleasant and Lumberville, approximately locatedB dotted where concealed. 0 Qal O D E D 30 be found on the Stockton quadrangle to the east of the map area (Monteverde and Cr G 17 W n Myers N o l (2b), Lockatong (2c), and Stockton (2d). Additional Stockton data (2e) collected in Wickecheoke Creek in the Stockton quadrangle as a class ck 00 ID Qa 13 NG RD Qcs O 3 O i R OCKAT Pennsylvania. Elsewhere in the Delaware Valley, the gravel underlies sand of the R h L

others, 2015). Mill R o B 16 I D T 20 Qa assignment under Prof. Michael Hozik of Stockton University. “N” values list the number of bedding orientations analyzed on individual plots 0 lh 18 postglacial terrace deposit (unit Qst), and, in places, for example along the east 14 14 Qst 0 B 0 on each row. The left hand lower hemisphere, equal area stereonet graphs displays contoured poles to fractures using 1% area contours with D R T J d 3 I o 17 bank of the river north of Shyhawks Island, colluvium (unit Qcs). Silt and fine sand Fault - Dashed where approximately located. R D h Lockatong Formation (Upper Triassic) (Kummel, 1897) - Cyclically deposited G a 2% contour interval. The middle lower hemisphere, equal area stereonet presents all fracture planes. Rose diagrams display fracture dip 0 K i ^l 30 R E c o A N k 12 P 1 17 blown from the glacial terrace on the east side of the river near Marshall Island sequences of mainly gray to greenish-gray, and in upper part of unit, locally red- S E 4 L direction using 10 sectors. Note difference in scale between the rose diagrams. Plots created using software from Allmendinger and others TAT 0 300 Y o 0 lh Cabin N n 0 IN l Qcal 12 (2013) and Caroza and Allmendinger (2013). form a thin sheet of windblown sediment on the adjacent hillslope (unit Qe). ^lh dish-brown siltstone to silty argillite (^lr) and dark-gray to black shale and mud- 40 SK D C R R u n C o v e r e d B r iPlanardge features R ILL O M

r S stone. Siltstone is medium to fine grained, thin-bedded, planar to cross-bedded D 13 PLE G 12 lh RIM 12 Qcal ^lr E l ST After the late Wisconsinan glaciation the Delaware River again eroded the 11 0 R with mud cracks, ripple cross-laminations and locally abundant pyrite. Shale and 0 S L

Strike and dip of inclined beds 4 R D 18 Qcal o glaciofluvial gravel and deposited sand and silt on the eroded gravel toforma mudstone are very thin bedded to thin laminated, platy, locally containing desic- c k N n 19 a postglacial terrace (unit Qst) which is between 15 and 20 feet above the modern cation features. Thermally altered to dark gray to black (^lh) where in- u C N 11 sr R Other featuresO L 15 t C n V Qcal o abi E D lh floodplain. The postglacial terrace began to accumulate around 12 ka, when ero- R Qst W Qcs Qal n truded by diabase. Thickness of hornfels directly related to thickness of intruded ED A 0 A H 0 S 13 g Qcs Contour Plot B 1 R L sion of the glacial gravel was completed. Minor deposition on the terrace during diabase (Van Houten, 1969). Lower contact gradational into Stockton Formation I T D 14 C Abandoned rock uarry G E 0 24 10 R Qcal E r 1 0 large floods continues today. R TOHIC 0 S 8 and placed at base of lowest continuous black siltstone bed (Olsen, 1980). Maxi- KON HILL 2 J d D RD 0 RD Qal L lh OMPF TAVERN 6 N T mum thickness of unit regionally is about 2,200 feet (Parker and Houghton, 1990). 8 S 4 Diabase float station Qcs 22 200 2 In tributary valleys during the late Wisconsinan glacial period, and during ear- Smiths 28 sr Qa Percent D B7 12 16 per 1% area R 12 13 J d 14 Qcal 10 Corner D 18 lh Qcs lier periods of cold climate, permafrost and reduced tree cover led to increased D Stockton Formation (Upper Triassic) (Kummel, 1897) - Unit is interbedded se- N 12 Hornfels float station R A 15 5 10 ^sr Z L 9 0 0 Qst 9 L 0 4 O E 3 0 20 erosion on hillslopes. This sediment aggraded in alluvial plains (now terraces) and quence of gray, grayish-brown, or slightly reddish-brown, coarse- to fine-grained, L L 0 I A V 15 10 B2 O H R 25 J d 14 fans in valley bottoms (units Qst, Qaf), and in colluvial deposits on footslopes (unit D R Point Byram 12

^sa thin- to thick-bedded, poorly sorted, planar to trough cross-bedded, and ripple Drillers log - Used to proect grayZ bed and other characteristic beds to G Qal 2 B6 17 T

N Pleasant RD Qcs

Qcs). By 14 ka, permafrost had melted and tree cover was reestablished. Streams cross laminated arkosic sandstone (^sa), and reddish-brown clayey fine-grained, surace. E 12 L Qw 10 16 12 Qa H 0 13 11 00 Qal

eroded into the valley-fill sediments to form modern floodplains. Channel and over- sandstone, siltstone and mudstone (^sr). Coarser units commonly occur as lens- C 0 l 4 11 S 3 Qal Qcs R 14 I bank deposits have aggraded in these floodplains within the past 14 ka (unit Qal). B 0 es and are locally graded. Finer units are bioturbated sequences that fine upward. 0 3 V L Qa 500 2 0 E 7 1 U 0 R sa RD l 10 Qa In headwater areas during this same time, colluvium and weathered rock material Arkosic sandstone units are deeply weathered and more common in the lower half; Location of photo E B E Qcs 13 sr R Qa have been incised, washed, and winnowed by runoff and groundwater seepage siltstone and mudstone are generally less weathered and more common in upper D Qw 14 R R Qcs sr 3a Y R BYR N = 68 (unit Qcal). E AM L 24 half. Lower contact, located outside of mapped area, is an erosional unconformi- L G N CA T 40 G N 25 Diabase borehole B7 RV N OLL 0 ER GA o A E SVI TE 0 25’00 W P W Qst 12 sr o ty. Thickness is approximately 4,500 feet. LLE RD E S D Qcs 0 25’00 R IK R E RAVEN ROCK D P JE Qal Qcs RD N Bedrock units range in age from the to Late Triassic (Olsen, T Y N R Qst Wismer N R N S 9 0 Qal Qst Qal s R A R E 2 12 30 de u S E S Y 1980a, 1980b) and consist of a sequence of alluvial to lacustrine sedimentary d n A 0 F Y Contour Plot

REFERENCES CITED AND USED IN CONSTRUCTION OF MAP e E 0 L N L 19 Qa Qcal Qi 4 V sa G P A Qst rocks that are locally intruded by igneous rocks. Sedimentary rocks cover the ma- N sa 24 T IA N 20 Allmendinger, R. W., Cardozo, N. C., and Fisher, D., 2013, Structural Geology Al- I 14 11 8 P 16 jority of the mapped area. The basal Stockton Formation, located just to the south O A P r D U 12 gorithms: Vectors & Tensors, Cambridge, , Cambridge University R Contour Plot Qal Qcs C Qps L P W Qw 8 in the Stockton quadrangle is dominantly an alluvial sequence of red, light-brown, M M IS y 100 A' 4 U 90 M r I Press, p. 289. E T E Percent gray, and buff sandstone, arkosic sandstone, and conglomerate. Red sandstone, S 80 R o 25 Qal R per 1% area R k Qst Cardozo, N., and Allmendinger, R. W., 2013, Spherical projections with OSXSte- 70 D Qi R c D siltstone and mudstone are more common in the upper half of the Stockton (Mc- 60 i 1 0 Raven Rock reonet: Computers & Geosciences, v. 51, p. 193 - 205, doi: 10.1016/j. 50 4 0 Bulls H 0 2 5 10 Laughlin, 1945, 1959). These two rock assemblages form a sequential pattern, 40 0 cageo.2012.07.021. 30 Island sa Qw basal arkose-dominated overlain by red sandstone-shale dominated, that is re- 20 de Boer, J.Z., and Clifford, A.E., 1988, Mesozoic tectogenesis: Development and 10 n Qal Qal Ru 10 20 30 40 50 Qst peated through the Stockton. Two such sequences, forming the upper Raven Rock Percent es r 0 dd PO Qal ive Qw deformation of “Newark” rift zones in the Appalachains (with special em- 0 per 1%G areae Qst R 5 Qst re and Cuttalossa members of the Stockton (McLaughlin, 1945; Johnson and Mc- Qw D wa phasis on the Hartford basin, Connecticut), in, Manspeizer, W., ed., Trias- e ela Laughlin, 1957; Olsen and others, 1996) crop out in the mapped area. Member 200 Lumberville H la D sic-Jurassic rifting: , NY, Elsevier, p. 275-306. U w 0 a l contacts are covered and inferred. 30 N r na Qst Hager-Richter Geoscience Inc., 2017, Borehole geophysical logging - data report Qcs T E e a Ca Qal Qst B R nd R ritan Hinkletown r U D a 0 boreholes B-6 & B-7 Route 29 Rockfall Mitigation, Kingwood, New Jer- C C ON 20 3b N = 82 The overlying Lockatong Formation, dominated by black shale and argillite g K S CO in C Lockatong Fm borehole B sey, Consulting Report, 15 pages. F s O and the Passaic Formation, dominantly red, and less commonly gray, and black s O D Qa Herman, G.C., Houghton, H.F., Monteverde, D.H., and Volkert, R.A., 1992, Bed- u L 1 1a L Passaic Fm bedding 0 c O 0 shale, and siltstone were deposited in lacustrine environments. The red and gray D N = 20 300 N well K a rock geologic map of the Pittstown and Flemington quadrangles, Hunter- D D U R n to black bedrock units display a cyclical pattern at four different scales related to R D n Contour Plot W H N don and Somerset Counties, New Jersey, New Jersey Geological Survey, I A 00 L A L u 2 both thickness and duration of sedimentary environment (Olsen and others; 1996). D M N E 0 W V a SON 14 Open-file Map, OFM 10, scale 1: 24,000. O R O 0 AX H

D P P I O R 4 RD L C 12 Olsen and Kent (1995) and Olsen and others (1996) show that these cycles reflect D G E L O 10 X G R M Houghton, H.F., Herman, G.C., and Volkert, R.A., 1992, Igneous rocks of the D A D IN MILL R T F 8 climatic variations influenced by celestial mechanics (Milankovitch orbital cyclici- G RETZ I O 6 Contour Plot F M RT Flemington fault zone, central Newark basin, New Jersey: , R 4

0 R M A D

0 2 ty). The basic (Van Houten) cycle correlates to the 20,000-yr climatic precession 90 O Y 3 E D Percent structure, and stratigraphy, in, Puffer J.H., and Ragland, P.C., eds., East- 80 R R per 1% area cycle and consists of about 20 feet of lacustrine sediments deposited in a shallow- 70 R 00 N D 2 O ern North American Mesozoic Magmatism: Geological Society of America 60 S 5 10 15 20 25 30 ing-upward environment. Four to six Van Houten cycles combine to form a Short BELMONT M 50 X AN A O P

Special Paper 268, p. 219-232. R 40 o D 0 o G D R 0 R 30 0 22’0 3 0 22’0 Modulating Cycle, approximately 95,000-125,000 duration (Olsen and others, o o R o W E LAMBERTVILLE Hozik, M. J., and Columbo, R., 1984, Paleomagnetism in the central Newark ba- 20 75 05’00 75 02’0 E 75 00’ I T S D E 0 10 M A R 0 1996). McLaughlin cycle forms the next higher level cycle and contains four Short N 3 5 10 15 E G LE BUCKINGHAM D R L A H sin, in, Puffer, J. H., ed., Igneous rocks of the Newark basin: Petrology, Percent R D R L D I R D L L Modulating Cycles. The 413,000-year eccentricity of the earth’s orbit controls this per 1% area W O Y D E T L R mineralogy, ore deposits, and guide to field trip: Geological Association of A C E U E E H R R A depositional pattern. A McLaughlin cycle forms the basis of the different Passaic S E F D L D SH L IE New Jersey 1st Annual Field Conference, p. 137-163. A O F L R R D Formation members (Olsen and others, 1996). Olsen and others (1996) delineate B Produced by the Geological Survey T D Bedrock geology mapped by D.H. Monteverde, E R SCALE 1:24 000R 1 1 Husch, J., 1988, Significance of major- and trace-element variation trends in Me- K D , C I North American Datum of 1983 (NAD83) U G.C. Herman and R.W. Witte , 2017. 0 T Aerequus a final thickest cycle, Long Modulating Cycle, as composed of four McLaughlin 0 P TA 5 World Geodetic System of 1984 (WGS84). Projection and L Surfical geology mapped by S.D. Stanford, 2014. N = 16 sozoic diabase, west central New Jersey and eastern Pennsylvania, in, T D 0 1 0.5 0 KILOMETERS 1 O 2 Airport N 0 S 3c cycles and representing the 1.6-2.0 million-year eccentricity cycle. R 1,000-meter grid: Univeral Transverse Mercator, Zone 18T4 S A Y A 1 Froelich, A. and Robinson, G., eds., Geology of the Early Mesozoic Ba- S 10,000-foot Ticks: Pennsylvania Coordinate System of 1983 Retired, New Jersey Geological and Water Survey Passaic Fm well K R M R A R 1000 500 0 METERS 1000 2000D E 0 I D E (south zone), New Jersey Coordinate System of 1983 D L F 0 sins of Eastern North America. United States Geological Survey Bulletin, P R 3 D Carvers Ridge P 1 0.5 0 2 O L L Digital cartography by R.S. Pristas A single diabase body, called the Byram Diabase (Van Houten, 1969; Olsen T L E T I r T no. 1776, p. 141-150. E H Passaic Fm bedding M T R C N O Figure 3. Fracture data collected from a 75.5 ft deep borehole in diabase (3a, Borehole B9) and a 48.5 ft borehole in Lockatong Formation (3b, I C D N and others, 1996) and Point Pleasant diabase (Husch, 1988) intrudes Triassic sed- S Y y N = 118 N 0 R LN MILES 1b L E O Imagery...... NAIP, July 2010 0 Reviewed by Michael J. Hozik and Gary M. Fleeger N L n E 3 L N SUGAN RD Johnson, M.E., and McLaughlin, D. B., 1957, Triassic formations of the Delaware i P IL Borehole B9) using downhole optical televiewer logs recorded and interpreted by Hager-Richter Geoscience (2017). Fracture data in 610 ft. R 1000 0 1000 2000IL 3000 4000 5000 6000 7000 8000 9000 10000 iment in the Lumberville quadrangle. This intrusive body has the same magmatic U m R Roads...... ©2006-2012 TomTom C D M Valley, in, Dorf, E., ed., Guidebook for field trips: Geological Society of a Names...... GNIS,0 2013 Research supported by the U. S. Geological Survey, deep borehole in the basal Passaic Formation (3c, well K) collected from downhole optical televiewer logs. Each row of three plots displays the N h 0 Carversville W source as the Orange Mountain Basalt based on geochemical and paleomagnetic s 5 A FEET N e Hydrography...... National Hydrography Dataset, 2010 S NationalF Cooperative Geologic Mapping Program, same data in different methods. The left hand lower hemisphere, equal area stereonet graphs poles to fractures using 1% area contours with a America, Annual Meeting, Atlantic City, New Jersey, Trip 2, p. 31-68. B data (Hozik and Colombo, 1984; Husch, 1988; Houghton and others, 1992). Limit- R N Contours...... National Elevation Dataset, 2011 under U.S.G.S. award numbers G16AC00284 and G14ACC00238. A r D 400 2% contour interval. The middle lower hemisphere, equal area stereonet presents all fracture planes and the rose diagrams on the right display Kummel, H.B., 1897, The Newark system, report of progress, New Jersey Geo- N Contour Plot Boundaries...... Census, IBWC, IBC,USGS, 1972 - 2012 R The views and conclusions contained in this document

C B LE AQ o

ed thermally metamophosed sediments surround the diabase intrusions and have H A IL UET CONTOUR INTERVAL 20 FEET fracture dip direction using 10 sectors. “N” value is the number of fracture orientations analyzed on individual plots on each row.

L V ON are those of the author and should not be

R N B RS G logical Survey, Annual Report to the State Geologist for the year 1896, D

80 E VE RD NORTH AMERICAN VERTICAL DATUM OF 1988 interpreted as necessarily representing the official been discussed by Van Houten, (1969, 1971, 1980, 1987). R R r

70 S CA policies, either expressed or implied, of the U. S. Government. p. 25-88. C 60 LO RD L SI N C

50 N R

I g Kummel, H.B., 1898, The Newark System of New Jersey, New Jersey Geological 40 T This map was produced to conform with the E C W A T n Structure 30 E 0 M AN RD I 0 i National Geospatial Program US Topo Product Standard, D2011. Survey, Annual Report to the State Geologist for the year 1897, p. 25- RY 20 H 3 R E s R n IC A metadata file associated with this product is draft versionE 0.6.11 Y █ 10 R s L Newark Basin rocks show limited signs of structural deformation except near 300 IL R 159. u V D n█ Percent R c S Solebury per 1% area D C 400 5 10 15 20 25 30 D R I the diabase intrusion where several small faults are present (photo 1). The sed- Lucas, M., Hull, J., and Manspeizer, W., 1988, A foreland-type fold and related a N 500 W L TA n L M A IE I AR H iments uniformly strike northeast-southwest and dip northwest, forming a gentle V n M A C 0 r structures in the Newark Rift Basin, in, Manspeizer, W., ed., Triassic-Ju- E 13° C E 0 u W K 4 C G a A M D D 0 homocline (figure 1). Surface data from Stockton and Lockatong Formations have I D P S a 0 rassic rifting, continental breakup and the origin of the Atlantic Ocean 0 R R R s 3 0 MAGNETICNORT 4 TRUE NORT H L o 0 almost identical bedding trends with the Passaic Formation showing a wider range L l 0 and passive margins, part A, Elsevier Science Publishers, New York, p. I a 4 M t Cottageville S S t of orientations. Downhole bedding trends in the Passaic display a slightly more 40 T R u 307-332. 0 R E EE V C T O northern strike trend. McLaughlin, D. B., 1945, Type sections of the Stockton and Lockatong formations, R T D SH Peters Corner Proceedings of the Pennsylvania Academy of Science, v. 19, p.102-113.

V APPROXIMATE MEAN

Fracture orientations show a wider variability across the three sedimentary McLaughlin, D. B., 1946, The Triassic rocks of the Hunterdon Plateau, New Jersey, A Locktong Fm bedding Plumstead R 0

1c L N = 82D DECLINATION, 1994 formations (figure 2). Stockton fractures have the tightest range of orientations, L W Proceedings of the Pennsylvania Academy of Science, v. 20, p. 89-98. E E Y I LOCATION IN V E with a dominant trend of 036/74SE. This tight density is possibly due to the smaller McLaughlin, D. B., 1959, Mesozoic rocks, in, Willard, B., et al., Geology and min- P N A G NEW JERSEY R ID number of recorded fractures (22) as compared to the Lockatong (172) and Pas- eral resources of Bucks County, Pennsylvania, Pennsylvania Geological K R R D saic (199). Lockatong fractures display a nearly identical dominant trend as the Survey, Bulletin C-9, p. 55-114. Contour Plot Stockton. Two other subsidiary trends of 027/79SE and 115/87NE are also present Monteverde, D.H., Herman, G.C., Stanford, S.D., and Spayd, Steven, 2015, Geo- 70 60 in the Lockatong. Passaic data have the larger variation. A somewhat dominant logic map of the Stockton Quadrangle, Hunterdon County, New Jersey, 50 40 trend of 006/87SE is supplemented with weaker trends of 032/84SE, 045/86SE New Jersey Geological and Water Survey, Geologic Map Series, GMS 30 20 and 069/87SE. The intrusive diabase has the widest range of fracture orientations 15-1, scale 1: 24,000. 10 of all the units. Again, this range could be due to a small amount of data (35). Olsen, P.E., 1980a, The latest Triassic and Early Jurassic formations of the New- Percent per 1% area 5 10 15 20 25 30 35 Geologic Map of the New Jersey These overall trends mimic the dominant Newark Basin orientation in the eastern ark basin (eastern North America, ): Stratigraphy, section of the western fault block. The Flemington - Dilts Corner - Furlong faults structure, and correlation: New Jersey Academy of Science, Bulletin, v. crop out to the east and south of the mapped area and mark the eastern boundary 25, p. 25-51. Portion of the Lumberville Quadrangle, Hunterdon County, New Jersey of this block (Herman and others, 1992; Monteverde and others, 2015). Olsen, P.E., 1980b, Fossil great lakes of the Newark Supergroup in New Jersey; in, Manspeizer, W., ed., Field studies of New Jersey geology and guide There is a wide variability between surface trends and those measured in two to field trips: 52nd annual meeting of the New York State Geological As- shallow boreholes, one in the diabase intrusive and the other in Lockatong hornfels sociation, p. 352-398. Stockton Fm bedding by zone (figures 2 and 3). Optical televiewer downhole data is shown in figure 3. Olsen P.E. and Kent D.V., 1995: Milankovitch climate forcing in the tropics of Pan- 1d N = 22 gea during the Late Triassic. Palaeogeography, Palaeoclimatology, Pa- No strong deformational fabric exists over the mapped region with the excep- laeoecology, v. 122, 1-26. Stereonet (left) and rose diagram (right) analysis of bedding trends from downhole data from well K 1 Photo 1: Exposure of the Lockatong Argillite displaying west dipping (to the left) beds with a spaced tion of the region of the Byram . Previous workers have mapped a single fault Olsen, P.E., Kent, D.V., Cornet, Bruce, Witte, W.K., and Schlische, R.W., 1996, Figure 1. in the Passaic (1a), surface exposures in the Passaic (1b), Lockatong (1c) and Stockton (1d) Formations. “N” Donald H. Monteverde, Ron W. Witte , Scott D. Stanford near vertical fracture pattern. One foot bar for scale. along the sill’s northwestern boundary with the Lockatong (Kummel, unpublished High-resolution stratigraphy of the Newark rift basin (early Mesozoic, values list the number of bedding orientations analyzed on individual plots on each row. The left hand lower 1 data, ca 1890; Van Houten, 1969, 1980, 1987; Houghton, unpublished data, ca eastern North America): Geological Society of America, Bulletin, v. 108, hemisphere, equal area stereonet graphs displays both bedding planes and contoured poles to fractures using and Gregory C. Herman 1985). However, the northern Lockatong/diabase contact was not exposed during p. 40-77. 1% area contours with a 2% contour interval. Rose diagrams display bedding dip direction using 10o sectors. field research for this map. Two other fault trends were recorded within the diabase Olsen, P.E., Schlische, R.W., and Gore, P.J., 1989, Tectonic, depositional, and pa- and the Lockatong hornfels. An older nearly east-west trend with a southern dip leoecological history of Early Mesozoic rift basins in eastern North Amer- occurred separating the hornfels on the north from the diabase to the south. This ica: Field trip guidebook T351, American Geophysical Union, 174 pages. 2018 fault can be seen on a road cut (photo 2) and wrapping around to paralleling the Parker, R.A., and Houghton, H.F., 1990, Bedrock geology of the Rocky Hill quad- stream. Motion direction on this fault suggests normal sense of offset. A younger rangle, New Jersey, US Geological Survey, Open-File Report 90-219, trend observed at several different locations within the diabase was orientated scale 1:24,000. nearly north-south and dipped steeply east to vertical. Slickenlines were oriented Schlische, R.W., 1992, Structural and stratigraphic development of the Newark nearly horizontal and displayed a left lateral offset. Most of these features are too extensional basin, eastern North America: Evidence for the growth of the small for accurate depiction on this scale map. basin and its bounding structures; Geological Society of America, Bulle- tin, v.104, p.1246-1263. DESCRIPTION OF MAP UNITS Schlische, R.W., 1993, Anatomy and evolution of the Triassic-Jurassic continental Alluvium - Silt, pebble-to-cobble gravel, minor fine sand and clay. Moderately to rift system, eastern North America; Tectonics, v.12, p.1026-1042. A A’ Qal Schlische, R.W., 1995, Geometry and origin of fault-related folds in extensional well-sorted and stratified. Contains minor amounts of organic matter. Color of fine FEET FEET Fairview Road Kingwood Station Road K Well Idell n n sediment is reddish brown, grayish brown, and brown, locally yellowish-brown. settings, American Association of Petroleum Geologists Bulletin, v.79, p. n 1661-1678. 1,000 1,000 Gravel in tributary valleys is dominantly subangular to angular flagstones and ^pg ^p ^p ^pg ^pg chips of red and gray shale and mudstone with minor subrounded to rounded Van Houten, F.B., 1969, Late Triassic Newark Group, north central New Jersey Diabase and adjacent Pennsylvania and New York, in, Subitzky, S., ed., Geology ^p pebbles and cobbles of red and gray sandstone. Gravel in the main Delaware ^pg Valley includes cobbles and boulders of red and gray sandstone; gray, red, and of selected area in New Jersey and eastern Pennsylvania and guidebook SEA LEVEL ^p SEA LEVEL of excursions: Rutgers University Press, New Brunswick, New Jersey, p. ^pg brown quartzite and quartzite-conglomerate; gray and white gneiss; and dark gray ^p 314-347. ^p chert. Silt, fine sand, and clay occur as overbank deposits on floodplains along ^pg ^pg Van Houten, F.B., 1971, Contact metamorphic assemblages, Late Triassic ^l hornfels low-gradient stream reaches. Overbank sediments are sparse or absent along -1,000 ^lr ^l -1,000 Newark Group, New Jersey: Contributions to Mineralogy and Petrology, ^lr ^sa steeper stream reaches. Gravel is deposited in stream channels and is the domi- ^l nant floodplain material along steeper stream reaches. Flagstone gravel typically v. 30, p. 1-14. ^lr Lockatong Fm hornfels ^sa ^sr Van Houten, F.B., 1980, Late Triassic part of Newark Supergroup, Delaware River ^l ^l ^sr shows strong imbrication. As much as 10 feet thick. Many stream channels are -2,000 ^sr ^sa ^sr -2,000 floored by bedrock, particularly in steep reaches. section, west-central New Jersey, in, Manspeizer, W., ed., Field studies of ^sa ^lr ^sr New Jersey geology and guide to field trips, 52nd Annual meeting of the ^sa ^sr New York State Geological Association, Newark, New Jersey, Rutgers, Colluvium and Alluvium, Undivided - Interbedded alluvium as in unit Qal and ^sa Photo 2: Photo looking east along Route 29 shows fault contact between the diabase to the right Qcal -,000 -,000 colluvium as in unit Qcs in narrow headwater valleys. As much as 10 feet thick University, p. 246-276. ^sr (south) and the Lockatong hornfels below and to the left (north). Indicators suggest normal motion Van Houten, F.B., 1987, Late Triassic cyclic sedimentation; upper Lockatong ^sa on the fault. A small hornfels block lies above the fault but its contact relationship with the diabase Deposits - Flagstone gravel as in unit Qal and minor reddish-brown and lower Passaic formations (Newark Supergroup), Delaware Valley, Paleozoic- rocks, undivided cannot be discerned due to cover. Kummel (1898) described the overall contact between the diabase and the Lockatong here as unconformable with some note of shearing. His figure depicts the hornfels Qaf to grayish-brown silt and fine sand. Moderately sorted and stratified. As much as west-central New Jersey, in, Roy, D.C., ed., Northeastern section of the -,000 -,000 block above the fault shown above as a complete continuation of the hornfels body suggesting the 15 feet thick. Form fans at mouths of steep tributary streams. Geological Society of America, Centennial field guide, v. 5, p. 81-86. Withjack, M. O., Olsen, P. E., and Schlische, R. W., 1995, Tectonic evolution of contact has a stair step trace. Van Houten (1969) characterizes the overall contact as a fault with hornfels both below and above the fault. Van Houten (1987) depicts the small hornfels body above Stream-Terrace Deposits - Silt, fine sand, and pebble-to-cobble gravel, moder- the Fundy basin, Canada: Evidence of extension and shortening during the fault shown above as a xenolith. Rock hammer in circle for scale. Qst passive-margin development: Tectonics, v. 14, p. 390-405.