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DEPARTMENT OF ENVIRONMENTAL PROTECTION LAND USE MANAGEMENT NEW JERSEY GEOLOGICAL SURVEY SURFICIAL GEOLOGY OF THE BRISTOL QUADRANGLE BURLINGTON COUNTY, NEW JERSEY OPEN-FILE MAP OFM 73 Prepared in cooperation with the U. S. GEOLOGICAL SURVEY NATIONAL GEOLOGIC MAPPING PROGRAM ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! !! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! !! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # # . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! !! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! 74 o 52'30" 40 o 07'30" 50' 47'30" 74 o 45' 40 o 07'30" 5' 2'30" 40 o 00' 74 o 45' COLUMBUS TRENTON WEST MOUNT HOLLY BEVERLY 47'30" 50' 74 o 52'30" 40 o 00' 2'30" 5' Geology mapped 2005. Cartography by S. Stanford and M. Girard. Base from U. S. Geological Survey, 1955. Photorevised 1981. B B' A A' P28 33 Qwf 43 Qcm2 P15 43 Qwf P11 31 Qwf 60 Qcm2 P10 30 Qwf 56 Qcm2 P2 21 Qwf 60 Qcm2 P7 15 Qwf 51 Qcm2 P5 19 Qwf 58 Qcm2 P4 21 Qwf 70 Qcm2 P3 10 fill 35 Qwf R2 20 water 23 Qm 32 Qwf R6 5 water 22 Qm 29 Qwf NJ1 8 fill 28 Qm 37 Qwf NJ17 7 fill 12 Qm 35 Qwf R1 20 water 35 Qwf 27-10779 16 27-4164 30 27-4163 27 27-10765 >45 27-10766 6 fill 20 Qwf 27-10710 24 aft afd afd Qm afd 27-11523 31 27-22 31 27-23 35 27-13235 30 27-4426 22 27-4411 30 Qwf 27-10670 50 27-4436 29 27-9018 34 27-10417 22 27-7281 29 27-1773 31 27-1772 28 27-7271 28 Qwf Qm Tp Qwcp Qtu Qtu Qtu Qm Qal 27-11562 13 27-11621 13 18 >17 >33 18 8 0 22 20 27-6930 15 27-6794 4 27-7693 25 27-10542 16 fill 29 Qm 61 Qwf 27-10549 27 fill >52 Qwf 27-10530 37 27-10541 37 28-1851 12 28-22027 10 28-17612 15 15 Qwcp Qal Qal Qwcp Qwcp Qal Qtu Qtu Qm Qst Tp Qwcp Qal afd Qst Qtu Qtu 28-20985 8 28-15073 9 28-22364 12 28-7292 8 28-16615 20 28-22786 19 28-18563 17 5 Qtl 28-1731 10 5 10 10 Qal Qwcp Qwcp 27-9633 35 27-7399 7 27-9707 11 27-7701 25 28-8206 20 28-30319 20 9 3 Qtu Qtu Qwcp Qwcp 27-9813 25 27-11765 44 13 27-6217 12 Qtu Qal >17 5 Qe Qtu Qtu 0 6 27-2902 20 >22 27-4601 42 27-10556 >40 27-6045 47 27-6351 21 27-4690 44 27-4698 38 27-4697 46 27-7279 37 27-7280 45 27-7278 45 27-7275 40 27-7274 40 27-7272 43 27-7270 37 27-7273 48 27-209 30 27-3568 30 27-34-918 45 27-467 36 27-738 >41 27-4927 41 27-4845 47 27-737 >47 27-685 47 27-600 >49 27-4848 52 27-651 36 27-4846 48 Qwf afd Qwf afd afd afd Qwf Qtl Qcm2 Qwf Qm TP39 26 water 33 Qm CB7 14 water 39 Qm TP38 27 water 32 Qm Qm TP37 22 water 31 Qm TP36 29 water 38 Qm CB77 16 water 24 Qm TP35 27 water 28 Qm 22-34-846 17 27-119 26 27-4750 47 27-11740 3 fill 8 Qm 36 Qwf 27-11329 35 27-11328 22 27-10665 30 27-7514 34 27-5343 42 27-11280 28 >17 23 27-11984 48 27-9183 43 >23 25 >18 27-9860 23 27-9808 11 27-1636 30 27-11095 28 27-8560 30 27-6575 25 3 5 7 Qtl Qtu Qal Qtu Qtu Qtl Qwcp Tp Qcm1 Qwcp 8 5 Qtu Qwcp Qtu Qtu Tp Tp Qwcp Qwcp Qtu Qal aft aft aft aft Qtu Qtl Qtl Qal Qal Tp Qwcp Qwcp Qtu Qtu Qtu Qtu Qwcp Qcm1 Qcm1 Qtu Qtu Qtu Qtu Tp Qtl Qtl 7 0 8 3 Qcm1 Qal Qcm1 3 3 9 9 3 21 4 13 27-5952 8 27-11564 19 27-5975 16 27-9762 15 27-1635 12 27-9872 9 27-10316 12 27-10002 11 27-8495 20 27-9824 16 27-10740 8 B1 19 B24 13 8 B5 12 B29 28 27-6673 0 Qtu Qwcp Qm Qcm2 Qtu Qtu Qtl Qal Qal Qal Tp Qcm1 Qal Qtu Qtl Qtu Qwf Qwf Qm aft aft 27-8949 38 BC >21 BP >21 27-5069 30 Qe 10 >20 Qcm2 Qcm2 Qcm1 Qcm1 Qcm1 Qwcp Qe-Qcm1/Tp 27-9896 17 27-5155 8 27-5009 12 20 10 6 4 27-10144 12 27-5727 13 5 5 Qe-Qcm1/Tp Qcm1 Qwcp Qal Qal Qcm1 Qe-Qcm1/Tp Tp Qcm1 Qtu Qal Qcm1 Qwcp Qe-Qcm1/Tp Tp Qtu Qtu Qwcp Tp Qcm1 2 Qwcp Qal Qtu Qtu Qcm1 Qtu Qtu Qwcp Qtl 2 12 9 32 15 7 4 1 5 9 3 5 10 10 9 11 3 Qcm1 Qcm1 Qtu Qtu Qtu Qtu Qal Qal Qtu Tp Qwcp Tp Qwcp 27-9376 0 4 0 4 8 Qcm1 Qal Qwcp Qcm1 Qtu Qtu Qtl Qtu Qtu Qwcp 3 27-8386 20 0 18 6 3 Qwcp Tp Qtu Qcm1 Qcm1 Tp Qwcp Qwcp Qal Qcm1 Qcm2 Qcm2 Qtl Qtu Qtu Qcm2 Qcm1 Qwcp 5 7 2 9 Qwcp Tp Tp Qe-Qcm1/Tp Qcm1 Qcm1 Qwcp Qtu Qtu Qal Qwcp Qwcp Tp Qtu Qtu Qcm1 Qal Qcm1 Qal Qcm1 Qtu Qal Qtu 3 2 0 0 0 4 0 17 32 7 10 10 4 14 0 Qwcp Qwcp Qtu Qtu Qtu Qcm1 Qwcp Qcm1 Qwcp Qwcp Qwcp Qtu Qal Tg Qtu Qtu Qal Qcm1 Qcm1 Qcm1 Qcm1 12 Qtu 47-4 >40 Qm 27-5416 8 Qtu Qtu Qe-Qcm1/ Tp Qwcp 10 0 3 27-9612 10 fill 15 Qm 44 Qwf >20 8 8 8 >8 0 0 150 A 100 ELEVATION (feet) 50 0 -50 VERTICAL EXAGGERATION 40X DELAWARE RIVER CONRAIL RR US ROUTE 130 27-4848 27-4846 27-4845 27-9612 27-10665 27-11329 Qm Qwf Qm afd Qwf Coastal Plain Formations Qtl Qal Qm Qal Qcm2 ASSICUNK CREEK OLD YORK ROAD Qcm1 Tp BEND IN SECTION INTERSTATE ROUTE 295 Qcm1 Qtu Qal Qtu Qe-Qcm1 Tp NJ TURNPIKE Tp BEND IN SECTION 27-9367 BURR ROAD Qtu Qal Qcm1 Qcm1 Qcm1 Tg WOODLANE ROAD MT HOLLY Coastal Plain Formations Coastal Plain Formations 150 100 50 0 -50 A' Qtu B 150 100 50 0 -50 ELEVATION (feet) -100 VERTICAL EXAGGERATION 40X Bedrock Qwf Qcm2 P15 P11 P10 P2 P7 P5 P4 P3 R1 R2 R6 NJ1 NJ17 AMTRAK DELAWARE RIVER RIVER ROAD Qwf 27-10417 27-10670 27-4436 27-9018 Qwf Coastal Plain Formations Qtu CONRAIL US ROUTE 130 BEND IN SECTION 27-11184 27-6217 Qal Qal Qtu OLD YORK ROAD Tp Qcm1 INTERSTATE ROUTE 295 NJ TURNPIKE Tp Tp B' 150 100 50 0 -50 -100 Coastal Plain Formations Qm 20-30 feet of stream incision in main Delaware valley 5-20 feet of tributary stream incision, as much as 30 feet of stream incision in main Delaware valley 20-30 feet of stream incision erosion and stream incision weathering and extensive erosion, new drainage established weathering and extensive erosion CORRELATION OF MAP UNITS Holocene late middle early Pliocene Pleistocene late Miocene Qm Qal Qst Qwf Qtl Qe Qtu Qcm2 Qcm1 Tp Tg aft afd INTRODUCTION Surficial materials in the New Jersey part of the Bristol quadrangle include artificial fill and fluvial, glaciofluvial, eolian, estuarine, and salt-marsh deposits. They are as much as 70 feet thick beneath and adjacent to the Delaware River but are generally less than 30 feet thick elsewhere. They record seven main periods of deposition, separated by six episodes of valley erosion. The deposits are described below. The age of the deposits and the episodes of valley erosion are shown on the correlation chart. The underlying bedrock and Coastal Plain formations were mapped by Owens and Minard (1964). DESCRIPTION OF MAP UNITS ARTIFICIAL FILL--Sand, silt, gravel, clay; gray to brown; demolition debris (concrete, brick, wood, metal, etc.), cinders, ash, slag, glass. Unstratified to weakly stratified. As much as 20 feet thick. Chiefly in highway and railroad embankments and filled marshes and flood plains. Many small areas of fill, particularly along streams in urban areas, are not mapped. Extent of fill based in part on position of shorelines and salt marshes shown on topographic manuscript map sheets 54 and 58 (N. J. Geological Survey, c. 1880). DREDGE SPOILS--Fine-to-medium sand, silty fine-to-medium sand, minor coarse sand; gray, very pale brown; pebble-to-cobble gravel; minor red, yellow, and white clay, and fragments of schist and gneiss. Gravel consists chiefly of white to gray quartz and quartzite, gray siltstone and sandstone, minor gray chert and gneiss, and minor red siltstone and sandstone. Unstratified to weakly stratified, locally thinly bedded to laminated. May contain minor amounts of demolition debris. As much as 30 feet thick. In disposal cells along the Delaware River. Consist largely of sediment excavated from units Qm and Qwf, and from the underlying Potomac Formation of Cretaceous age, and from schist and gneiss bedrock, during dredging of ship channels. TRASH FILL--Trash mixed and covered with silt, clay, sand, and minor gravel. As much as 60 feet thick. In solid-waste landfills. Small areas of trash fill may be included within artificial fill. ALLUVIUM--Sand, silt, minor clay and peat; brown, yellowish-brown, gray; and pebble gravel. Contains varied amounts of wood and fine organic matter. Sand and silt are unstratified to weakly stratified. Gravel occurs in unstratified to weakly stratified beds generally less than 2 feet thick. Sand consists chiefly of quartz with some glauconite, gray siltstone fragments, and mica. Gravel consists chiefly of white, gray, and yellow-stained quartz and quartzite, and a trace of gray siltstone and chert. Sand and gravel beds may be locally cemented with iron. Total thickness of deposit as much as 15 feet. Deposited in modern flood plains and stream channels, and in former flood plains and channels now covered by salt-marsh and estuarine deposits. Beneath the Delaware River, alluvium underlies estuarine deposits (unit Qm) but cannot be distinguished lithically from the underlying and adjoining glaciofluvial deposit (unit Qwf) and so is included with Qwf on sections AA’ and BB’. SALT-MARSH AND ESTUARINE DEPOSITS--Silt, sand, peat, clay; brown, dark-brown, gray, black; and minor pebble-to-cobble gravel. Contain abundant organic matter. As much as 30 feet thick. Deposited in salt marshes, tidal flats, and tidal channels during Holocene sea-level rise, chiefly within the past 10,000 years. POSTGLACIAL STREAM-TERRACE DEPOSIT--Fine-to-medium sand, minor coarse sand and silt; yellowish-brown, brown, grayish-brown. May include pebble-to-cobble gravel at base. Sand and gravel composition as in unit Qwf. As much as 20 feet thick (estimated). Forms terrace at Newbold Island with a surface 5-10 feet above the Delaware estuary. Deposited by the Delaware River as it downcut into deposit Qwf in postglacial time, about 15,000 to 10,000 years ago. Deposit is a veneer on a strath cut into unit Qwf. This deposit was mapped as part of “Graywacke 1” by Owens and Minard (1975) and was included with the “Van Sciver Lake beds” by Owens and Minard (1979), who considered the beds to be interglacial estuarine deposits of Sangamonian age. Newell and others (2000) also mapped the deposit as the “Van Sciver Lake beds” but considered it to be a fluvial or glaciofluvial deposit of late Wisconsinan age. Because this deposit lies upon a terrace eroded into the glaciofluvial deposits, and is in turn overlain by the modern estuarine deposit, it is a postglacial alluvial deposit. Because the age and origin of the deposit differ from those proposed for the “Van Sciver Lake beds”, that name is not used here. EOLIAN DEPOSITS--Fine-to-medium sand, yellowish-brown to very pale brown. Sand consists chiefly of quartz with some glauconite and gray siltstone fragments, and minor mica. As much as 15 feet thick. These are windblown sediments forming low dunes, derived from underlying and adjacent surficial deposits. GLACIOFLUVIAL DEPOSIT--Fine-to-medium sand, minor coarse sand; yellowish-brown, light reddish-brown, grayish-brown; pebble gravel, minor cobble gravel. Sand consists chiefly of quartz and gray siltstone fragments with a little glauconite, feldspar, and a few red siltstone fragments. Gravel consists chiefly of white and gray quartz and quartzite, gray siltstone and sandstone, minor red siltstone and sandstone, and minor gray chert and gneiss. As much as 50 feet thick. Laid down by glacial meltwater descending the Delaware Valley during the late Wisconsinan glaciation, about 20,000 to 15,000 years ago. Forms a terrace along the Delaware River with a surface elevation of 25 feet in the Florence area, declining to 15 feet in the Burlington area. This deposit was informally termed the “Trenton Gravel” by Cook (1880) and Lewis (1880). It was later mapped as “Graywacke 1” and “Graywacke 2” by Owens and Minard (1975) and named the “Van Sciver Lake” and “Spring Lake” beds by Owens and Minard (1979). “Graywacke 1” and “Van Sciver Lake beds” refer to deposits forming the lowest terrace in the Trenton area, which is equivalent to unit Qst here. “Graywacke 2” and “Spring Lake beds” refer to deposits forming the higher terrace in the Trenton area, which is equivalent to unit Qwf here. Lewis (1880), Owens and Minard (1979), Berg and others (1980), and Newell and others (2000), applied the names “Trenton Gravel”, “Spring Lake beds”, and “Van Sciver Lake beds” to sediments now known to include glaciofluvial, interglacial estuarine, and postglacial alluvial deposits. Because these deposits are mapped separately here as units Qwf, Qcm2, and Qst, respectively, the names “Trenton Gravel”, “Spring Lake beds”, and “Van Sciver Lake beds” are not used. LOWER STREAM-TERRACE DEPOSITS--Fine-to-coarse sand, minor silt; yellow, yellowish-brown, light gray; pebble gravel. Sand consists chiefly of quartz, with some glauconite, and minor gray siltstone fragments and mica. Gravel consists chiefly of white, gray, and yellow-stained quartz and quartzite. As much as 40 feet thick in the East Burlington area, generally less than 10 feet thick elsewhere. Form stream terraces with surfaces 5 to 15 feet above modern flood plains. UPPER STREAM-TERRACE DEPOSITS--Fine-to-medium sand, minor silt and coarse sand; yellow, reddish-yellow, brownish-yellow, light-gray, locally olive-yellow; pebble gravel. Sand consists chiefly of quartz with some glauconite, gray siltstone fragments, minor mica and a trace of red siltstone fragments and feldspar. Gravel consists chiefly of white, gray, and yellow- stained quartz and quartzite. As much as 40 feet thick. The deposits form a fluvial plain in the Delaware Valley between Kinkora and East Burlington, with a surface elevation of 55 to 35 feet, and form stream terraces in tributary valleys that are on grade with the plain in the Delaware Valley. The surfaces of the tributary terraces are 15 to 30 feet above modern flood plains. The plain and terraces grade downvalley to, or are onlapped by, the Cape May Formation, unit 2 (unit Qcm2), and so are contemporaneous with, or slightly older than, the Cape May 2. CAPE MAY FORMATION (Salisbury and Knapp, 1917)--Fine-to-medium sand, minor coarse sand and silt; yellow, brownish-yellow, reddish-yellow, very pale brown, light gray; minor pebble gravel, trace of cobble gravel. Unstratified to well-stratified. Sand consists of quartz with a little glauconite and a trace of mica, feldspar, and gray siltstone fragments. Gravel consists chiefly of white, gray, and yellow-stained quartz and quartzite, and a trace of gray and red siltstone and sandstone. As much as 30 feet thick. The Cape May Formation, unit 2 (Qcm2) (Newell and others, 2000) forms a terrace with a maximum surface elevation of about 35 feet. Fossils, pollen, and amino-acid racemization ratios in shells from this unit elsewhere in the Delaware estuary and Delaware Bay area indicate that it is an estuarine or fluvial-estuarine deposit of Sangamon age (about 125,000 years ago), when sea level was 20 to 30 feet higher than at present in this region (Woolman, 1897; Newell and others, 1995; Lacovara, 1997; Wehmiller, 1997). The Cape May Formation, unit 1 (Qcm1) (Newell and others, 1995) is an older estuarine or fluvial-estuarine deposit of uncertain age that forms an extensively eroded terrace with a top elevation of about 70 feet. Patches of slightly glauconitic yellowish-brown fine-to-medium sand occur as veneers on surfaces higher than this terrace, at elevations as high as 100 feet. These are included in unit Qcm1 but they may consist of windblown or slopewash deposits rather than estuarine and fluvial-estuarine sediments. Because unit Qcm1 is at higher elevation than Sangamon-age deposits, it was laid down during a pre-Sangamon interglacial sea-level highstand and is of early or middle Pleistocene age (Lacovara, 1997; O’Neal and McGeary, 2002). Areas symboled as “Qe-Qcm1/Tp” indicate extent of Cape May Formation, unit 1, and eolian deposits, less than 5 feet thick overlying Pensauken Formation. Salisbury and Knapp (1917) included stream-terrace and glaciofluvial deposits within the Cape May Formation; here they are mapped separately as the upper and lower stream-terrace deposits (units Qtl and Qtu) and glaciofluvial deposit (unit Qwf) because they differ in age and origin from the Cape May Formation. In Pennsylvania, deposits correlative with the Cape May are mapped as “Trenton Gravel” (Berg and others, 1980). As described above for unit Qwf, the “Trenton Gravel” at its type area is a glaciofluvial deposit, not an interglacial estuarine deposit. Because the glaciofluvial and interglacial estuarine deposits are mapped separately here, the name “Trenton Gravel” is not used. PENSAUKEN FORMATION (Salisbury and Knapp, 1917)--Fine-to-coarse sand to clayey sand, minor silt and very coarse sand; reddish-yellow to yellow; pebble gravel. Unstratified to well stratified, commonly with tabular, planar cross-beds in sand. Pebble gravel occurs as thin layers (generally less than 3 inches thick) within the sand and as thicker, unstratified beds in places at the base of the formation, where it may include cobble gravel. Sand consists chiefly of quartz with some feldspar, mica, and glauconite, and a few rock fragments (chert and shale) (Bowman and Lodding, 1969; Owens and Minard, 1979). The feldspar is partially or fully weathered to white clay. Gravel consists chiefly of yellow, reddish-yellow (from iron-staining), white, or gray quartz and quartzite; a little brown to gray chert and reddish-brown ironstone; and a trace of brown, reddish- brown, and gray sandstone and shale, and white-to-gray gneiss. The chert, sandstone, shale, and gneiss commonly are partially weathered or fully decomposed. As much as 40 feet thick. Occurs as erosional remnants capping uplands. Elevation of the base of the deposit ranges from 90 to 100 feet in the Jacksonville area to 60 to 70 feet in the belt trending southwestward from Kinkora through Bustleton, Springside, and Deacons, to Willingboro, with a channel as low as 30 feet at Rancocas. The variation in basal elevation records thickening of the deposit towards the axis of the Delaware Valley, which roughly coincides with the former axis of the Pensauken river valley, and northeast- southwest-trending fluvial channeling into the underlying substrate of Coastal Plain formations. Regional paleoflow data (Owens and Minard, 1979; Martino, 1981; Stanford and others, 2002), and the provenance of the sand and gravel in the formation, indicate that the Pensauken was deposited by a large river flowing southwesterly from the New York City area to the Delmarva Peninsula. The map area is in the southeastern part of the former river valley. The age of the Pensauken is not firmly established. Berry and Hawkins (1935) describe plant fossils from the Pensauken near New Brunswick, New Jersey that they consider to be of early Pleistocene age. Owens and Minard (1979) assign a late Miocene age based on correlation with units in the Delmarva Peninsula. Pollen from a black clay bed within the Pensauken near Princeton, New Jersey, includes cool-temperate species and a few pre-Pleistocene taxa. This assemblage suggests a Pliocene age (Stanford and others, 2002). The Pensauken is overlain by late Pliocene or early Pleistocene till in Somerset County, New Jersey, and lies in a valley deeply eroded into middle and late Miocene marine and fluvial deposits. These relationships indicate a Pliocene age (Stanford, 1993). UPLAND GRAVEL—Medium-to-coarse sand, reddish-yellow to reddish-brown, and pebble gravel. Unstratified, iron-cemented in places. Sand and gravel consist of quartz. As much as 10 feet thick. Caps summit of Mount Holly, above an elevation of 160 feet. Erosional remnant of a fluvial deposit older than the Pensauken Formation. OUTCROP OF COASTAL PLAIN FORMATIONS--Exposed formations of Cretaceous age. Soil zone generally includes some lag pebbles from eroded surficial deposits. May include thin, patchy colluvial, alluvial, or eolian sediments less than 3 feet thick. MAP SYMBOLS Contact--Solid where well-defined by landforms; dashed where approximate; short-dashed where featheredged or gradational; dotted where exposed in former sand pits. Thickness of surficial material in well or boring--Location accurate to within 200 feet. Upper number is identifier; lower number is thickness in feet of surficial material, inferred from driller’s or engineer’s log. Where multiple surficial units were penetrated, the depth (in feet below land or water surface) of the base of the unit is indicated next to the unit symbol. A “>” indicates that base of unit was not reached at depth shown. Identifiers of the form 27-xxxx or 28- xxxx are well permits issued by the N. J. Department of Environmental Protection, Bureau of Water Allocation. Identifiers prefixed by P, R, and NJ are test borings for the Pennsylvania Turnpike bridge. Identifiers prefixed by CB and TP are test borings for channel dredging made by the U. S. Army Corps of Engineers. Identifiers prefixed by B and BC are test borings on file at the N. J. Geological Survey. Identifiers of the form 27-xx-xxx are N. J. Atlas Sheet coordinates of records of wells or borings in the permanent note collection of the N. J. Geological Survey. Thickness of surficial material in well or boring--Location accurate to within 500 feet. Identifiers and thickness values as above. Thickness of surficial material in power-auger boring--From Owens and Minard (1964). Thickness of surficial material in former sand and gravel pit--From Owens and Minard (1964). Surficial material observed in exposure, excavation, or hand-auger hole. Thickness of surficial material observed in former exposure--From permanent note collection of the N. J. Geological Survey. Fluvial scarp--Line at top, ticks on slope. Marks late Wisconsinan channel cut into upper stream terrace deposits by Assicunk Creek near Burlington. Excavation perimeter--Line at limit of large excavation. Slump scarp and block--Line at base of scarp, barbs on slope. Slump block lies between base of scarp and river. Slump is in Potomac Formation clay along Delaware River in Florence. Sand pit--Inactive in 2004. Shallow topographic basin--Line at rim, pattern in basin. Depth generally less than 5 feet. Most were formed by melting of permafrost about 18,000 to 15,000 years ago. Some may have formed from wind erosion. Drawn from air photos taken in 1979. REFERENCES Berg, T. W., Edmunds, W. E., Geyer, A. R., Glover, A. D., Hoskins, D. M., MacLachlan, D. B., Root, S. I., Sevon, W. D., and Socolow, A. A., compilers, 1980, Geologic map of Pennsylvania: Pennsylvania Geologic Survey, Fourth Series, scale 1:250,000, 2 sheets. Berry, E. W., and Hawkins, A. C., 1935, Flora of the Pensauken Formation in New Jersey: Geological Society of America Bulletin, v. 46, p. 245-252. Bowman, J. F., and Lodding, William, 1969, The Pensauken Formation--a Pleistocene fluvial deposit in New Jersey, in Subitzky, Seymour, ed., Geology of selected areas in New Jersey and eastern Pennsylvania and guidebook of excursions: New Brunswick, N. J., Rutgers University Press, p. 3-6. Cook, G. H., 1880, Surface geology--report of progress: N. J. Geological Survey Annual Report for 1880, p. 14-97. Lacovara, K. J., 1997, Definition and evolution of the Cape May and Fishing Creek formations in the middle Atlantic Coastal Plain of southern New Jersey: unpublished PhD dissertation, University of Delaware, Newark, Delaware, 243 p. Lewis, H. C., 1880, The Trenton Gravel and its relation to the antiquity of man: Proceedings of the Academy of Natural Sciences of Philadelphia, Part 2, April to September 1880, p. 296-309. Martino, R. L., 1981, The sedimentology of the late Tertiary Bridgeton and Pensauken formations in southern New Jersey: unpublished PhD dissertation, Rutgers University, New Brunswick, N. J., 299 p. Newell, W. L., Powars, D. S., Owens, J. P., and Schindler, J. S., 1995, Surficial geologic map of New Jersey: southern sheet: U. S. Geological Survey Open File Map 95-272, scale 1:100,000. Newell, W. L., Powars, D. S., Owens, J. P., Stanford, S. D., and Stone, B. D., 2000, Surficial geologic map of central and southern New Jersey: U. S. Geological Survey Miscellaneous Investigations Map I-2540-D, scale 1:100,000. New Jersey Geological Survey, c. 1880, Topographic map sheets 54 and 58: unpublished maps on file at N. J. Geological Survey: scale 1:21,120. O’Neal, M. L., and McGeary, S., 2002, Late Quaternary stratigraphy and sea- level history of the northern Delaware Bay margin, southern New Jersey, USA: a ground penetrating radar analysis of composite Quaternary coastal terraces: Quaternary Science Reviews, v. 21, p. 929-940. Owens, J. P., and Minard, J. P., 1964, Pre-Quaternary geology of the Bristol quadrangle, New Jersey-Pennsylvania: U. S. Geological Survey Geologic Quadrangle Map GQ-342, scale 1:24,000. Owens, J. P., and Minard, J. P., 1975, Geologic map of the surficial deposits in the Trenton area, New Jersey and Pennsylvania: U. S. Geological Survey Miscellaneous Investigations Map I-884, scale 1:48,000. Owens, J. P., and Minard, J. P., 1979, Upper Cenozoic sediments of the lower Delaware valley and northern Delmarva Peninsula, New Jersey, Pennsylvania, Delaware, and Maryland: U. S. Geological Survey Professional Paper 1067D, 47 p. Salisbury, R. D., and Knapp, G. N., 1917, The Quaternary formations of southern New Jersey: N. J. Geological Survey Final Report, v. 8, 218 p. Stanford, S. D., 1993, Late Cenozoic surficial deposits and valley evolution of unglaciated northern New Jersey: Geomorphology, v. 7, p. 267-288. Stanford, S. D., Ashley, G. M., Russell, E. W. B., and Brenner, G. J., 2002, Rates and patterns of the late Cenozoic denudation in the northernmost Atlantic Coastal Plain and Piedmont: Geological Society of America Bulletin, v. 114, p. 1422- 1437. Wehmiller, J. F., 1997, Data report: aminostratigraphic analysis of mollusk specimens: Cape May Coast Guard station borehole, in Miller, K. G., and Snyder, S. W., eds., Proceedings of the Ocean Drilling Program: Scientific Results, v. 150x, p. 355-357. Woolman, Lewis, 1897, Stratigraphy of the Fish House black clay and associated gravels: N. J. Geological Survey Annual Report for 1896, p. 201-254. 7000 FEET 1000 1000 0 2000 3000 4000 5000 6000 .5 1 KILOMETER 1 0 SCALE 1:24 000 1/2 1 0 1 MILE MAGNETIC NORTH APPROXIMATE MEAN DECLINATION, 1981 TRUE NORTH LOCATION IN NEW JERSEY 11.5 O CONTOUR INTERVAL 20 FEET NATIONAL GEODETIC VERTICAL DATUM OF 1929 SURFICIAL GEOLOGY OF THE BRISTOL QUADRANGLE BURLINGTON COUNTY, NEW JERSEY by Scott D. Stanford 2008 Research supported by the U. S. Geological Survey, National Cooperative Geologic Mapping program, under USGS award number 05HQAG0026. The views and conclusions contained in this document are those of the author and should not be interpreted as necessarily representing the official policies, either expressed or implied, of the U. S. Government. afd aft Qal Qm Qst Qe Qwf Qtl Qtu Qcm2 Qcm1 Qe-Qcm1/ Tp Tp Tg Qwcp ! 27-5069 30 . 27-4750 47 #20 ! 10 ! # 15

SURFICIAL GEOLOGY OF THE BRISTOL … · 27-10417 27-10670 27-4436 27-9018 Qwf Coastal Plain Formations Qtu CONRAIL US R OUTE 130 BEND IN SECTION 27-11184 Qal 27-6217 Qtu ... are sh

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Page 1: SURFICIAL GEOLOGY OF THE BRISTOL … · 27-10417 27-10670 27-4436 27-9018 Qwf Coastal Plain Formations Qtu CONRAIL US R OUTE 130 BEND IN SECTION 27-11184 Qal 27-6217 Qtu ... are sh

DEPARTMENT OF ENVIRONMENTAL PROTECTIONLAND USE MANAGEMENTNEW JERSEY GEOLOGICAL SURVEY

SURFICIAL GEOLOGY OF THE BRISTOL QUADRANGLEBURLINGTON COUNTY, NEW JERSEY

OPEN-FILE MAP OFM 73

Prepared in cooperation with theU. S. GEOLOGICAL SURVEY

NATIONAL GEOLOGIC MAPPING PROGRAM

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74o52'30"40o07'30" 50' 47'30" 74o45'

40o07'30"

5'

2'30"

40o00'74o45'

CO

LU

MB

US

TRENTON WEST

MOUNT HOLLY

BE

VE

RLY

47'30"50'74o52'30"40o00'

2'30"

5'

Geology mapped 2005.Cartography by S. Stanford and M. Girard.

Base from U. S. Geological Survey, 1955.Photorevised 1981.

B

B'

A

A'

P2833 Qwf43 Qcm2

P1543 Qwf

P1131 Qwf60 Qcm2

P1030 Qwf56 Qcm2

P221 Qwf60 Qcm2

P715 Qwf51 Qcm2

P519 Qwf58 Qcm2

P421 Qwf70 Qcm2

P310 fill35 Qwf

R220 water23 Qm32 Qwf

R65 water22 Qm29 Qwf

NJ18 fill28 Qm37 Qwf

NJ177 fill12 Qm35 Qwf

R120 water35 Qwf

27-1077916 27-4164

30

27-416327

27-10765>45

27-107666 fill20 Qwf

27-1071024

aft

afd

afd

Qm

afd

27-1152331

27-2231

27-2335

27-1323530

27-442622

27-441130

Qwf

27-1067050

27-443629

27-901834

27-1041722

27-728129

27-177331

27-177228

27-727128

Qwf

Qm

Tp

Qwcp

Qtu

Qtu

Qtu

Qm

Qal

27-1156213

27-1162113

18

>17

>33

18

8

0

22

20

27-693015

27-67944

27-769325

27-1054216 fill29 Qm61 Qwf

27-1054927 fill>52 Qwf

27-1053037

27-1054137

28-185112

28-220271028-17612

15

15

Qwcp

QalQal

Qwcp

Qwcp

QalQtu

Qtu

Qm

Qst

Tp

QwcpQal

afd

Qst

Qtu

Qtu

28-209858

28-150739

28-2236412

28-72928

28-166152028-2278619

28-1856317

5

Qtl

28-173110

5

10

10Qal

Qwcp

Qwcp

27-96333527-7399

7

27-970711

27-770125

28-820620

28-3031920

93

Qtu

Qtu

Qwcp

Qwcp27-981325

27-1176544

1327-621712

Qtu

Qal

>17 5

Qe

Qtu

Qtu

06 27-2902

20

>22 27-460142

27-10556>40

27-604547

27-635121

27-469044

27-469838

27-469746

27-727937

27-728045

27-727845

27-727540

27-727440

27-727243

27-727037

27-727348

27-20930

27-356830

27-34-91845

27-4673627-738

>4127-492741

27-484547

27-737>47

27-6854727-600

>4927-484852

27-65136 27-4846

48

Qwf

afd

Qwf

afd

afdafd

Qwf

Qtl Qcm2Qwf

Qm

TP3926 water33 Qm

CB714 water39 Qm

TP3827 water32 Qm

Qm

TP3722 water31 Qm

TP3629 water38 Qm

CB7716 water24 Qm

TP3527 water28 Qm

22-34-84617

27-11926

27-475047

27-117403 fill8 Qm36 Qwf

27-1132935

27-1132822

27-1066530

27-751434

27-534342

27-1128028

>17

23

27-1198448

27-918343

>23

25

>18

27-986023 27-9808

11

27-163630

27-1109528

27-856030

27-657525

3

5

7

Qtl

Qtu

Qal

Qtu

Qtu

Qtl

Qwcp

Tp

Qcm1

Qwcp

8

5

Qtu

Qwcp

Qtu

Qtu

Tp

Tp

Qwcp

Qwcp

Qtu

Qal

aft

aft

aft

aft

Qtu

QtlQtl

Qal

Qal

TpQwcp

Qwcp

Qtu

Qtu

Qtu

QtuQwcp

Qcm1

Qcm1

QtuQtu

QtuQtu

Tp

QtlQtl

70

8

3

Qcm1

Qal

Qcm1

3

39

9

3

21

4

13

27-59528

27-1156419

27-597516

27-976215

27-163512

27-98729

27-1031612

27-1000211

27-849520

27-982416

27-107408

B119

B24138

B512

B2928

27-66730

Qtu

QwcpQm

Qcm2

Qtu

Qtu

Qtl

Qal

Qal

Qal

Tp

Qcm1Qal

Qtu

Qtl

Qtu

Qwf

Qwf

Qm

aft

aft

27-894938

BC>21

BP>21

27-506930

Qe

10

>20

Qcm2 Qcm2

Qcm1

Qcm1

Qcm1Qwcp

Qe-Qcm1/Tp27-989617

27-51558 27-5009

12

2010

6

4

27-1014412

27-572713

5

5

Qe-Qcm1/Tp

Qcm1

Qwcp

Qal

QalQcm1

Qe-Qcm1/Tp

Tp

Qcm1

Qtu

Qal

Qcm1

Qwcp

Qe-Qcm1/Tp

Tp

Qtu

Qtu

Qwcp

Tp

Qcm1

2

Qwcp

QalQtu

Qtu

Qcm1

Qtu

Qtu

Qwcp

Qtl

2

12

9

32

15

7

4

1

59

3

510

109

11

3

Qcm1

Qcm1

Qtu

Qtu

Qtu

Qtu

Qal

Qal

Qtu

TpQwcp

Tp

Qwcp

27-93760

4

0

4

8

Qcm1

Qal

Qwcp

Qcm1

Qtu

Qtu

Qtl

Qtu

Qtu

Qwcp

3

27-838620

0

18

6

3

Qwcp

Tp

Qtu

Qcm1

Qcm1

Tp

Qwcp

Qwcp

Qal

Qcm1

Qcm2

Qcm2

Qtl

Qtu

QtuQcm2

Qcm1

Qwcp

5

7

2

9

Qwcp

Tp

Tp

Qe-Qcm1/TpQcm1

Qcm1

Qwcp

Qtu

Qtu

Qal

Qwcp

Qwcp

Tp

Qtu Qtu

Qcm1

Qal

Qcm1

Qal

Qcm1

Qtu

Qal

Qtu

3

2

0

0

0

4

017

32

7

10

10 4

14

0

Qwcp

QwcpQtu

QtuQtu

Qcm1

Qwcp

Qcm1

Qwcp Qwcp

Qwcp

Qtu

Qal

Tg

Qtu

Qtu

Qal

Qcm1

Qcm1

Qcm1

Qcm112

Qtu

47-4>40

Qm

27-54168

Qtu

Qtu

Qe-Qcm1/Tp

Qwcp

10

03

27-961210 fill15 Qm44 Qwf

>20

8

88

>8

0

0

150

A

100

EL

EVA

TIO

N (

feet

)

50

0

-50VERTICAL EXAGGERATION 40X

DE

LA

WA

RE

RIV

ER

CO

NR

AIL

RR

US

RO

UT

E 1

30

27-4

848

27-4

846

27-4

845

27-9

612

27-1

0665

27-1

1329

Qm Qwf Qm

afdQwf

Coastal Plain Formations

Qtl

Qal Qm

Qal

Qcm2

AS

SIC

UN

K C

RE

EK

OL

D Y

OR

K R

OA

D

Qcm1Tp

BE

ND

INS

EC

TIO

N

INT

ER

STA

TE

RO

UT

E 2

95

Qcm1

QtuQal

Qtu

Qe-Qcm1

Tp

NJ

TU

RN

PIK

E

Tp

BE

ND

INS

EC

TIO

N

27-9

367

BU

RR

RO

AD

Qtu

Qal

Qcm1Qcm1

Qcm1

Tg

WO

OD

LA

NE

RO

AD

MT

HO

LLY

Coastal Plain FormationsCoastal Plain Formations

150

100

50

0

-50

A'

Qtu

B150

100

50

0

-50

EL

EVA

TIO

N (

feet

)

-100VERTICAL EXAGGERATION 40X

Bedrock

Qwf

Qcm2

P15

P11 P10

P2

P7

P5

P4

P3

R1 R2

R6

NJ1

NJ1

7

AM

TR

AK

DE

LA

WA

RE

RIV

ER

RIV

ER

RO

AD

Qwf

27-1

0417

27-1

0670

27-4

436

27-9

018

Qwf

Coastal Plain Formations

Qtu

CO

NR

AIL

US

RO

UT

E 1

30

BE

ND

INS

EC

TIO

N27

-111

84

27-6

217

Qal Qal

Qtu

OL

D Y

OR

K R

OA

D

Tp

Qcm1

INT

ER

STA

TE

RO

UT

E 2

95

NJ

TU

RN

PIK

E

Tp

Tp

B'150

100

50

0

-50

-100

Coastal Plain Formations

Qm

20-30 feet of stream incision inmain Delaware valley

5-20 feet of tributary stream incision,as much as 30 feet of stream incisionin main Delaware valley

20-30 feet of stream incision

erosion and stream incision

weathering and extensive erosion,new drainage established

weathering and extensive erosion

CORRELATION OF MAP UNITS

Holocene

late

middle

early

Pliocene

Pleistocene

late Miocene

QmQal

Qst

Qwf Qtl Qe

QtuQcm2

Qcm1

Tp

Tg

aft afd

INTRODUCTION

Surficial materials in the New Jersey part of the Bristol quadrangle include artificial fill and fluvial, glaciofluvial, eolian, estuarine, and salt-marsh deposits. They are as much as 70 feet thick beneath and adjacent to the Delaware River but are generally less than 30 feet thick elsewhere. They record seven main periods of deposition, separated by six episodes of valley erosion. The deposits are described below. The age of the deposits and the episodes of valley erosion are shown on the correlation chart. The underlying bedrock and Coastal Plain formations were mapped by Owens and Minard (1964).

DESCRIPTION OF MAP UNITS

ARTIFICIAL FILL--Sand, silt, gravel, clay; gray to brown; demolition debris (concrete, brick, wood, metal, etc.), cinders, ash, slag, glass. Unstratified to weakly stratified. As much as 20 feet thick. Chiefly in highway and railroad embankments and filled marshes and flood plains. Many small areas of fill, particularly along streams in urban areas, are not mapped. Extent of fill based in part on position of shorelines and salt marshes shown on topographic manuscript map sheets 54 and 58 (N. J. Geological Survey, c. 1880).

DREDGE SPOILS--Fine-to-medium sand, silty fine-to-medium sand, minor coarse sand; gray, very pale brown; pebble-to-cobble gravel; minor red, yellow, and white clay, and fragments of schist and gneiss. Gravel consists chiefly of white to gray quartz and quartzite, gray siltstone and sandstone, minor gray chert and gneiss, and minor red siltstone and sandstone. Unstratified to weakly stratified, locally thinly bedded to laminated. May contain minor amounts of demolition debris. As much as 30 feet thick. In disposal cells along the Delaware River. Consist largely of sediment excavated from units Qm and Qwf, and from the underlying Potomac Formation of Cretaceous age, and from schist and gneiss bedrock, during dredging of ship channels.

TRASH FILL--Trash mixed and covered with silt, clay, sand, and minor gravel. As much as 60 feet thick. In solid-waste landfills. Small areas of trash fill may be included within artificial fill.

ALLUVIUM--Sand, silt, minor clay and peat; brown, yellowish-brown, gray; and pebble gravel. Contains varied amounts of wood and fine organic matter. Sand and silt are unstratified to weakly stratified. Gravel occurs in unstratified to weakly stratified beds generally less than 2 feet thick. Sand consists chiefly of quartz with some glauconite, gray siltstone fragments, and mica. Gravel consists chiefly of white, gray, and yellow-stained quartz and quartzite, and a trace of gray siltstone and chert. Sand and gravel beds may be locally cemented with iron. Total thickness of deposit as much as 15 feet. Deposited in modern flood plains and stream channels, and in former flood plains and channels now covered by salt-marsh and estuarine deposits. Beneath the Delaware River, alluvium underlies estuarine deposits (unit Qm) but cannot be distinguished lithically from the underlying and adjoining glaciofluvial deposit (unit Qwf) and so is included with Qwf on sections AA’ and BB’.

SALT-MARSH AND ESTUARINE DEPOSITS--Silt, sand, peat, clay; brown, dark-brown, gray, black; and minor pebble-to-cobble gravel. Contain abundant organic matter. As much as 30 feet thick. Deposited in salt marshes, tidal flats, and tidal channels during Holocene sea-level rise, chiefly within the past 10,000 years.

POSTGLACIAL STREAM-TERRACE DEPOSIT--Fine-to-medium sand, minor coarse sand and silt; yellowish-brown, brown, grayish-brown. May include pebble-to-cobble gravel at base. Sand and gravel composition as in unit Qwf. As much as 20 feet thick (estimated). Forms terrace at Newbold Island with a surface 5-10 feet above the Delaware estuary. Deposited by the Delaware River as it downcut into deposit Qwf in postglacial time, about 15,000 to 10,000 years ago. Deposit is a veneer on a strath cut into unit Qwf.

This deposit was mapped as part of “Graywacke 1” by Owens and Minard (1975) and was included with the “Van Sciver Lake beds” by Owens and Minard (1979), who considered the beds to be interglacial estuarine deposits of Sangamonian age. Newell and others (2000) also mapped the deposit as the “Van Sciver Lake beds” but considered it to be a fluvial or glaciofluvial deposit of late Wisconsinan age. Because this deposit lies upon a terrace eroded into the glaciofluvial deposits, and is in turn overlain by the modern estuarine deposit, it is a postglacial alluvial deposit. Because the age and origin of the deposit differ from those proposed for the “Van Sciver Lake beds”, that name is not used here.

EOLIAN DEPOSITS--Fine-to-medium sand, yellowish-brown to very pale brown. Sand consists chiefly of quartz with some glauconite and gray siltstone fragments, and minor mica. As much as 15 feet thick. These are windblown sediments forming low dunes, derived from underlying and adjacent surficial deposits.

GLACIOFLUVIAL DEPOSIT--Fine-to-medium sand, minor coarse sand; yellowish-brown, light reddish-brown, grayish-brown; pebble gravel, minor cobble gravel. Sand consists chiefly of quartz and gray siltstone fragments with a little glauconite, feldspar, and a few red siltstone fragments. Gravel consists chiefly of white and gray quartz and quartzite, gray siltstone and sandstone, minor red siltstone and sandstone, and minor gray chert and gneiss. As much as 50 feet thick. Laid down by glacial meltwater descending the Delaware Valley during the late Wisconsinan glaciation, about 20,000 to 15,000 years ago. Forms a terrace along the Delaware River with a surface elevation of 25 feet in the Florence area, declining to 15 feet in the Burlington area.

This deposit was informally termed the “Trenton Gravel” by Cook (1880) and Lewis (1880). It was later mapped as “Graywacke 1” and “Graywacke 2” by Owens and Minard (1975) and named the “Van Sciver Lake” and “Spring Lake” beds by Owens and Minard (1979). “Graywacke 1” and “Van Sciver Lake beds” refer to deposits forming the lowest terrace in the Trenton area, which is equivalent to unit Qst here. “Graywacke 2” and “Spring Lake beds” refer to deposits forming the higher terrace in the Trenton area, which is equivalent to unit Qwf here. Lewis (1880), Owens and Minard (1979), Berg and others (1980), and Newell and others (2000), applied the names “Trenton Gravel”, “Spring Lake beds”, and “Van Sciver Lake beds” to sediments now known to include glaciofluvial, interglacial estuarine, and postglacial alluvial deposits. Because these deposits are mapped separately here as units Qwf, Qcm2, and Qst, respectively, the names “Trenton Gravel”, “Spring Lake beds”, and “Van Sciver Lake beds” are not used.

LOWER STREAM-TERRACE DEPOSITS--Fine-to-coarse sand, minor silt; yellow, yellowish-brown, light gray; pebble gravel. Sand consists chiefly of quartz, with some glauconite, and minor gray siltstone fragments and mica. Gravel consists chiefly of white, gray, and yellow-stained quartz and quartzite. As much as 40 feet thick in the East Burlington area, generally less than 10 feet thick elsewhere. Form stream terraces with surfaces 5 to 15 feet above modern flood plains.

UPPER STREAM-TERRACE DEPOSITS--Fine-to-medium sand, minor silt and coarse sand; yellow, reddish-yellow, brownish-yellow, light-gray, locally olive-yellow; pebble gravel. Sand consists chiefly of quartz with some glauconite, gray siltstone fragments, minor mica and a trace of red siltstone fragments and feldspar. Gravel consists chiefly of white, gray, and yellow-stained quartz and quartzite. As much as 40 feet thick. The deposits form a fluvial plain in the Delaware Valley between Kinkora and East Burlington, with a surface elevation of 55 to 35 feet, and form stream terraces in tributary valleys that are on grade with the plain in the Delaware Valley. The surfaces of the tributary terraces are 15 to 30 feet above modern flood plains. The plain and terraces grade downvalley to, or are onlapped by, the Cape May Formation, unit 2 (unit Qcm2), and so are contemporaneous with, or slightly older than, the Cape May 2.

CAPE MAY FORMATION (Salisbury and Knapp, 1917)--Fine-to-medium sand, minor coarse sand and silt; yellow, brownish-yellow, reddish-yellow, very pale brown, light gray; minor pebble gravel, trace of cobble gravel. Unstratified to well-stratified. Sand consists of quartz with a little glauconite and a trace of mica, feldspar, and gray siltstone fragments. Gravel consists chiefly of white, gray, and yellow-stained quartz and quartzite, and a trace of gray and red siltstone and sandstone. As much as 30 feet thick. The Cape May Formation, unit 2 (Qcm2) (Newell and others, 2000) forms a terrace with a maximum surface elevation of about 35 feet. Fossils, pollen, and amino-acid racemization ratios in shells from this unit elsewhere in the Delaware estuary and Delaware Bay area indicate that it is an estuarine or fluvial-estuarine deposit of Sangamon age (about 125,000 years ago), when sea level was 20 to 30 feet higher than at present in this region (Woolman, 1897; Newell and others, 1995; Lacovara, 1997; Wehmiller, 1997). The Cape May Formation, unit 1 (Qcm1) (Newell and others, 1995) is an older estuarine or fluvial-estuarine deposit of uncertain age that forms an extensively eroded terrace with a top elevation of about 70 feet. Patches of slightly glauconitic yellowish-brown fine-to-medium sand occur as veneers on surfaces higher than this terrace, at elevations as high as 100 feet. These are included in unit Qcm1 but they may consist of windblown or slopewash deposits rather than estuarine and fluvial-estuarine sediments. Because unit Qcm1 is at higher elevation than Sangamon-age deposits, it was laid down during a pre-Sangamon interglacial sea-level highstand and is of early or middle Pleistocene age (Lacovara, 1997; O’Neal and McGeary, 2002). Areas symboled as “Qe-Qcm1/Tp” indicate extent of Cape May Formation, unit 1, and eolian deposits, less than 5 feet thick overlying Pensauken Formation.

Salisbury and Knapp (1917) included stream-terrace and glaciofluvial deposits within the Cape May Formation; here they are mapped separately as the upper and lower stream-terrace deposits (units Qtl and Qtu) and glaciofluvial deposit (unit Qwf) because they differ in age and origin from the Cape May Formation. In Pennsylvania, deposits correlative with the Cape May are mapped as “Trenton Gravel” (Berg and others, 1980). As described above for unit Qwf, the “Trenton Gravel” at its type area is a glaciofluvial deposit, not an interglacial estuarine deposit. Because the glaciofluvial and interglacial estuarine deposits are mapped separately here, the name “Trenton Gravel” is not used.

PENSAUKEN FORMATION (Salisbury and Knapp, 1917)--Fine-to-coarse sand to clayey sand, minor silt and very coarse sand; reddish-yellow to yellow; pebble gravel. Unstratified to well stratified, commonly with tabular, planar cross-beds in sand. Pebble gravel occurs as thin layers (generally less than 3 inches thick) within the sand and as thicker, unstratified beds in places at the base of the formation, where it may include cobble gravel. Sand consists chiefly of quartz

with some feldspar, mica, and glauconite, and a few rock fragments (chert and shale) (Bowman and Lodding, 1969; Owens and Minard, 1979). The feldspar is partially or fully weathered to white clay. Gravel consists chiefly of yellow, reddish-yellow (from iron-staining), white, or gray quartz and quartzite; a little brown to gray chert and reddish-brown ironstone; and a trace of brown, reddish-brown, and gray sandstone and shale, and white-to-gray gneiss. The chert, sandstone, shale, and gneiss commonly are partially weathered or fully decomposed. As much as 40 feet thick. Occurs as erosional remnants capping uplands. Elevation of the base of the deposit ranges from 90 to 100 feet in the Jacksonville area to 60 to 70 feet in the belt trending southwestward from Kinkora through Bustleton, Springside, and Deacons, to Willingboro, with a channel as low as 30 feet at Rancocas. The variation in basal elevation records thickening of the deposit towards the axis of the Delaware Valley, which roughly coincides with the former axis of the Pensauken river valley, and northeast-southwest-trending fluvial channeling into the underlying substrate of Coastal Plain formations. Regional paleoflow data (Owens and Minard, 1979; Martino, 1981; Stanford and others, 2002), and the provenance of the sand and gravel in the formation, indicate that the Pensauken was deposited by a large river flowing southwesterly from the New York City area to the Delmarva Peninsula. The map area is in the southeastern part of the former river valley.

The age of the Pensauken is not firmly established. Berry and Hawkins (1935) describe plant fossils from the Pensauken near New Brunswick, New Jersey that they consider to be of early Pleistocene age. Owens and Minard (1979) assign a late Miocene age based on correlation with units in the Delmarva Peninsula. Pollen from a black clay bed within the Pensauken near Princeton, New Jersey, includes cool-temperate species and a few pre-Pleistocene taxa. This assemblage suggests a Pliocene age (Stanford and others, 2002). The Pensauken is overlain by late Pliocene or early Pleistocene till in Somerset County, New Jersey, and lies in a valley deeply eroded into middle and late Miocene marine and fluvial deposits. These relationships indicate a Pliocene age (Stanford, 1993).

UPLAND GRAVEL—Medium-to-coarse sand, reddish-yellow to reddish-brown, and pebble gravel. Unstratified, iron-cemented in places. Sand and gravel consist of quartz. As much as 10 feet thick. Caps summit of Mount Holly, above an elevation of 160 feet. Erosional remnant of a fluvial deposit older than the Pensauken Formation.

OUTCROP OF COASTAL PLAIN FORMATIONS--Exposed formations of Cretaceous age. Soil zone generally includes some lag pebbles from eroded surficial deposits. May include thin, patchy colluvial, alluvial, or eolian sediments less than 3 feet thick.

MAP SYMBOLS

Contact--Solid where well-defined by landforms; dashed where approximate; short-dashed where featheredged or gradational; dotted where exposed in former sand pits.

Thickness of surficial material in well or boring--Location accurate to within 200 feet. Upper number is identifier; lower number is thickness in feet of surficial material, inferred from driller’s or engineer’s log. Where multiple surficial units were penetrated, the depth (in feet below land or water surface) of the base of the unit is indicated next to the unit symbol. A “>” indicates that base of unit was not reached at depth shown. Identifiers of the form 27-xxxx or 28-xxxx are well permits issued by the N. J. Department of Environmental Protection, Bureau of Water Allocation. Identifiers prefixed by P, R, and NJ are test borings for the Pennsylvania Turnpike bridge. Identifiers prefixed by CB and TP are test borings for channel dredging made by the U. S. Army Corps of Engineers. Identifiers prefixed by B and BC are test borings on file at the N. J. Geological Survey. Identifiers of the form 27-xx-xxx are N. J. Atlas Sheet coordinates of records of wells or borings in the permanent note collection of the N. J. Geological Survey.

Thickness of surficial material in well or boring--Location accurate to within 500 feet. Identifiers and thickness values as above.

Thickness of surficial material in power-auger boring--From Owens and Minard (1964).

Thickness of surficial material in former sand and gravel pit--From Owens and Minard (1964).

Surficial material observed in exposure, excavation, or hand-auger hole.

Thickness of surficial material observed in former exposure--From permanent note collection of the N. J. Geological Survey.

Fluvial scarp--Line at top, ticks on slope. Marks late Wisconsinan channel cut into upper stream terrace deposits by Assicunk Creek near Burlington.

Excavation perimeter--Line at limit of large excavation.

Slump scarp and block--Line at base of scarp, barbs on slope. Slump block lies between base of scarp and river. Slump is in Potomac Formation clay along Delaware River in Florence.

Sand pit--Inactive in 2004.

Shallow topographic basin--Line at rim, pattern in basin. Depth generally less than 5 feet. Most were formed by melting of permafrost about 18,000 to 15,000 years ago. Some may have formed from wind erosion. Drawn from air photos taken in 1979.

REFERENCES

Berg, T. W., Edmunds, W. E., Geyer, A. R., Glover, A. D., Hoskins, D. M., MacLachlan, D. B., Root, S. I., Sevon, W. D., and Socolow, A. A., compilers, 1980, Geologic map of Pennsylvania: Pennsylvania Geologic Survey, Fourth Series, scale 1:250,000, 2 sheets.

Berry, E. W., and Hawkins, A. C., 1935, Flora of the Pensauken Formation in New Jersey: Geological Society of America Bulletin, v. 46, p. 245-252.

Bowman, J. F., and Lodding, William, 1969, The Pensauken Formation--a Pleistocene fluvial deposit in New Jersey, in Subitzky, Seymour, ed., Geology of selected areas in New Jersey and eastern Pennsylvania and guidebook of excursions: New Brunswick, N. J., Rutgers University Press, p. 3-6.

Cook, G. H., 1880, Surface geology--report of progress: N. J. Geological Survey Annual Report for 1880, p. 14-97.

Lacovara, K. J., 1997, Definition and evolution of the Cape May and Fishing Creek formations in the middle Atlantic Coastal Plain of southern New Jersey: unpublished PhD dissertation, University of Delaware, Newark, Delaware, 243 p.

Lewis, H. C., 1880, The Trenton Gravel and its relation to the antiquity of man: Proceedings of the Academy of Natural Sciences of Philadelphia, Part 2, April to September 1880, p. 296-309.

Martino, R. L., 1981, The sedimentology of the late Tertiary Bridgeton and Pensauken formations in southern New Jersey: unpublished PhD dissertation, Rutgers University, New Brunswick, N. J., 299 p.

Newell, W. L., Powars, D. S., Owens, J. P., and Schindler, J. S., 1995, Surficial geologic map of New Jersey: southern sheet: U. S. Geological Survey Open File Map 95-272, scale 1:100,000.

Newell, W. L., Powars, D. S., Owens, J. P., Stanford, S. D., and Stone, B. D., 2000, Surficial geologic map of central and southern New Jersey: U. S. Geological Survey Miscellaneous Investigations Map I-2540-D, scale 1:100,000.

New Jersey Geological Survey, c. 1880, Topographic map sheets 54 and 58: unpublished maps on file at N. J. Geological Survey: scale 1:21,120.

O’Neal, M. L., and McGeary, S., 2002, Late Quaternary stratigraphy and sea-level history of the northern Delaware Bay margin, southern New Jersey, USA: a ground penetrating radar analysis of composite Quaternary coastal terraces: Quaternary Science Reviews, v. 21, p. 929-940.

Owens, J. P., and Minard, J. P., 1964, Pre-Quaternary geology of the Bristol quadrangle, New Jersey-Pennsylvania: U. S. Geological Survey Geologic Quadrangle Map GQ-342, scale 1:24,000.

Owens, J. P., and Minard, J. P., 1975, Geologic map of the surficial deposits in the Trenton area, New Jersey and Pennsylvania: U. S. Geological Survey Miscellaneous Investigations Map I-884, scale 1:48,000.

Owens, J. P., and Minard, J. P., 1979, Upper Cenozoic sediments of the lower Delaware valley and northern Delmarva Peninsula, New Jersey, Pennsylvania, Delaware, and Maryland: U. S. Geological Survey Professional Paper 1067D, 47 p.

Salisbury, R. D., and Knapp, G. N., 1917, The Quaternary formations of southern New Jersey: N. J. Geological Survey Final Report, v. 8, 218 p.

Stanford, S. D., 1993, Late Cenozoic surficial deposits and valley evolution of unglaciated northern New Jersey: Geomorphology, v. 7, p. 267-288.

Stanford, S. D., Ashley, G. M., Russell, E. W. B., and Brenner, G. J., 2002, Rates and patterns of the late Cenozoic denudation in the northernmost Atlantic Coastal Plain and Piedmont: Geological Society of America Bulletin, v. 114, p. 1422-1437.

Wehmiller, J. F., 1997, Data report: aminostratigraphic analysis of mollusk specimens: Cape May Coast Guard station borehole, in Miller, K. G., and Snyder, S. W., eds., Proceedings of the Ocean Drilling Program: Scientific Results, v. 150x, p. 355-357.

Woolman, Lewis, 1897, Stratigraphy of the Fish House black clay and associated gravels: N. J. Geological Survey Annual Report for 1896, p. 201-254.

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byScott D. Stanford

2008

Research supported by the U. S. Geological Survey, National Cooperative Geologic Mapping program,under USGS award number 05HQAG0026. The views and conclusions contained in this document are

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QTu QTu Qtr QTu · 2009. 12. 30. · QTu Th To Qu FGS051693 OPEN FILE MAP SERIES NO. 39 Th Th QTu Th QTu Th QTu QTu FLORIDA COUNTY GEOLOGIC MAP OF BY 1992 WALTER SCHMIDT STATE GEOLOGIST

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