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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, 1999 TRUE NORTH LOCATION IN NEW JERSEY 13 O CONTOUR INTERVAL 20 FEET NATIONAL GEODETIC VERTICAL DATUM OF 1929 SURFICIAL GEOLOGY OF THE BEVERLY AND FRANKFORD QUADRANGLES BURLINGTON COUNTY, NEW JERSEY Base from U. S. Geological Survey Frankford quadrangle (1997) and Beverly quadrangle (1995) Geology mapped 2004-2005 Cartography by S. Stanford and M. Girard 2'30" CAMDEN 57'30" 75 o 00' 55' MOORESTOWN 74 o 52'30" 40 o 00' BRISTOL 5' 74 o 52'30" 75 o 00' 40 o 00' 2'30" by Scott D. Stanford 2008 Research supported by the U. S. Geological Survey, National Cooperative Geologic Mapping program, under USGS award number 04HQAG0043. 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. DEPARTMENT OF ENVIRONMENTAL PROTECTION LAND USE MANAGEMENT NEW JERSEY GEOLOGICAL SURVEY SURFICIAL GEOLOGY OF THE BEVERLY AND FRANKFORD QUADRANGLES BURLINGTON COUNTY, NEW JERSEY OPEN-FILE MAP OFM 70 Prepared in cooperation with the U. S. GEOLOGICAL SURVEY NATIONAL GEOLOGIC MAPPING PROGRAM . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. . . . . . . . . . . . . . . . .. . . . . . . . . . . . . . . . . . . ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! !! ! ! ! ! ! ! !! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! ! B Qtl Qm Qm B1 10 fill 38 Qcm2 B2 38 Qcm2 B5 35 Qcm2 B4 41 Qcm2 B7 25 water 42 Qm 44 Qal B8 23 water 48 Qm 58 Qal B9 39 water 57 Qm 59 Qal B10 35 water 56 Qm 59 Qal B11 24 water 27 Qm 40 Qwf B12 7 water 18 Qm 49 Qwf B13 7 water 18 Qm 39 Qwf B14 16 Qm 58 Qwf B15 14 Qm 28 Qwf B16 19 Qm 25 Qtl B6 35 water 39 Qal B25 25 water 48 Qm 54 Qal B24 27 water 43 Qm 55 Qal B23 28 water 53 Qm 55 Qal B22 38 water 58 Qm 59 Qal B21 27 water 37 Qm 48 Qal B20 6 water 19 Qm 36 Qwf B19 16 Qm 42 Qwf B18 12 Qm 22 Qwf B17 9 Qm 19 Qwf 27-7722 8 fill 19 Qm 40 Qwf 27-7725 30 Qm 38 Qtl afd afd 27-9694 40 27-1583 34 27-2694 31 27-6880 23 27-11418 24 31-4864 34 Qcm2 Qcm2 Tp 27-775 11 27-1008 32 Tp B' Qwcp Qcm2 Qm Qal Qwcp Qal 27-3047 9 27-9569 16 27-11687 12 27-9278 14 27-10023 15 Tp 27-5012 25 27-11027 6 fill 25 Qm 23 Qcm2 27-7211 19 Qwcp Qcm2 Tp . 27-690 26 27-7439 25 27-7398 24 27-7504 24 27-7440 13 27-7565 20 27-6413 17 27-6412 16 27-10405 38 27-776 8 aft aft Qal Qwcp Tp Qe-Qcm1/Tp Qcm1 27-8154 19 Qtu Tp Qcm1 Qwcp Qtu Qcm1 Tp Qtu Qtu Qal Qcm1 27-10093 18 27-2642 16 27-1542 15 31-4059 12 Qtu Qtu Qcm1 Tp Qe-Qcm1/Tp 27-6429 16 27-3280 9 27-1010 14 27-1001 14 27-3279 19 27-4568 10 27-7063 13 27-8497 22 27-9325 23 27-7670 34 27-10265 24 27-1533 25 27-8533 12 27-10745 17 27-11919 18 27-7128 17 27-4534 14 27-10043 11 29-6043 23 27-7755 20 27-10810 17 27-9760 16 Qcm1 Tp Qcm2 Qcm2 Qcm1 Qm Qal C' Qal Tp Qal 27-9874 16 27-8355 9 Qcm1 Qm JPO 9 10 27-7497 25 27-7690 12 27-11933 24 27-6828 25 27-7059 25 27-7813 25 27-6676 23 27-7330 25 27-9041 23 27-9074 12 27-9002 29 27-8438 23 27-8435 29 27-8434 35 27-8381 20 27-9572 15 Qcm2 Qcm2 Qal aft Qcm2 Qal Qtl Qcm2 Qal 27-4616 11 27-10750 20 Qwcp Tp Tp 27-1579 20 Qwcp Tp Qcm1 Tp Qcm1 Qe Qe Qal Qcm2 Qcm2 Qm Qcm2 27-2970 30 Qal 27-11910 8 Qal Qwcp 27-3216 21 27-1381 21 27-1382 20 27-9830 6 27-3474 25 27-1466 14 27-211 14 28-1943 18 27-5202 27 27-1206 12 28-2954 20 27-1488 15 27-2613 19 27-1916 19 27-2435 24 27-3177 10 27-1395 20 27-1119 15 27-3264 12 27-1796 24 Qe-Qcm1/Tp Qcm1 Qcm1 27-3079 6 27-1422 18 27-2835 18 27-2950 8 27-1355 20 27-2688 11 27-4247 17 27-4680 21 Qcm1 Qcm2 Qe-Qcm1/Tp Qal Qwcp 27-11811 15 27-11813 20 27-3080 20 28-1874 37 27-2023 20 27-1504 39 27-232A 14 27-11974 34 27-12039 9 27-2611 22 27-977 12 27-1394 32 27-12033 32 DM5 35 DM4 16 DM8 8 DM7 8 DM6 18 27-11119 15 DM2 14 DM3 10 27-238 26 31-18745 18 31-18744 24 27-7380 54 DM1 >35 27-11365 18 27-11125 30 27-7884 13 27-2743 15 27-2742 18 Qtl Qm Qcm1 Qcm2 Qm Qcm2 Qm J3 30 water 47 Qm J4 35 water 43 Qm J7 24 water 41 Qm 27-43-173 21 J8 19 water 41 Qm J32B 30 water 38 Qm J9 19 water 41 Qm J10 22 water 37 Qm J11 25 water 33 Qm Qm afd afd afd afd afd afd afd afd Qtl Qtl Qm Qcm2 Qe 27-5033 25 27-1255 35 27-1433 >47 27-602 32 27-1993 20 27-1429 24 27-1332 34 27-1308 14 27-1529 39 27-43-281 30 JPO11 10 27-2775 34 27-1955 30 27-7748 37 27-9357 25 27-10933 15 27-5076 28 27-2299 15 27-7713 32 27-9642 26 27-4851 32 27-2546 34 Qcm2 Qm Qtl Qtl Qcm2 Qal Qal 27-7856 13 27-7841 20 27-7141 40 27-9217 8 JPO 9 32 27-1508 26 27-2709 29 Qcm2 Tp Qcm1 Qwcp Qcm2 Qm Qwcp Qal 27-2941 15 27-9561 11 27-894 32 Qcm1 Qcm1 Qcm2 27-1615 12 Qal Qwcp Qcm2 Qwcp Qcm2 Qcm1 Qwcp Qal Qcm2 27-8534 6 Qcm2 27-14629 <34 27-2723 <34 Qal Qe- Qcm1/Tp A' Qcm1 Qcm1 27-1689 15 27-10673 17 27-3323 9 27-11227 34 12 Qcm 15 Tp 27-8059 14 27-3548 18 27-4659 48 27-10439 21 27-4050 9 27-5315 7 Qcm2 Qcm1 Qcm1 Qcm2 27-9060 47 27-2646 43 27-9185 48 27-9308 31 27-2592 37 27-2612 45 27-10536 27 27-11891 45 27-11808 22 27-1452 30 27-9908 15 27-11476 18 27-3379 40 27-7164 >32 JPO4 17 Qcm 27 Tp Qcm2 15 Qcm2 Tp 27-12073 20 JPO10 44 Qm 27-43-218 20 Qe Qal Qtl Qm Qtl afd CB71 32 water 37 Qm CB41 26 water 41 Qm J27 21 water 36 Qm CB4 29 water 36 Qm J28 30 water 43 Qm CB72 27 water >45 Qm 27-1528 51 27-4505 53 27-2989 56 27-356 58 27-5385 18 Qcm2 Qal Qm Qcm2 Qe CB42 21 water 36 Qm CB5 22 water 35 Qm TP25A 26 water 34 Qm TP26 24 water >40 Qm 27-991 36 27-10874 13 27-10875 8 27-10876 5 27-13641 31 Qe 27-34-788 30 Qcm2 Qwf 27-6855 20 27-4379 24 27-4380 68 27-3695 46 TP28A 30 water 31 Qm TP30 28 water 29 Qm TP29 23 water 37 Qm TP27 27 water 35 Qm CB6 28 water 35 Qm 27-3820 24 27-3817 25 27-8746 40 27-8747 40 27-3815 22 27-3816 25 27-5426 44 27-3694 42 27-5314 33 27-8171 24 Qwf Qm afd afd A C 27-6943 22 27-3089 8 0 20 40 -20 -40 -60 -80 ELEVATION (feet) 60 80 100 120 A DELAWARE RIVER BURLINGTON AVENUE PINE STREET CONRAIL RR Qtl Qm Qm Qal Qcm2 Qcm2 Bedrock VERTICAL EXAGGERATION 50X J28 27-1528 27-356 27-2789 Qcm1 Tp 27-9060 27-2646 27-9185 Coastal Plain Formations BEND IN SECTION COOPER STREET US ROUTE 130 27-3548 27-8059 Tp Qcm2 Qcm1 LEVITT PARKWAY WILLINGBORO PARKWAY SALEM ROAD 27-2723 27-14629 Tp Qcm1-Qe A' 120 100 80 60 40 20 0 -20 -40 -60 -80 0 20 40 -20 -40 -60 -80 ELEVATION (feet) 60 80 100 120 C C' 120 100 80 60 40 20 0 -20 -40 -60 -80 DELAWARE RIVER CONRAIL RR CHESTER AVENUE GREENWOOD AVENUE 27-5033 J32B 27-1332 27-1308 27-977 27-12039 27-2023 27-1504 27-232A 27-11974 afd Qm Qm Qcm2 Qal Qwf Qtl Qcm2 Qcm1 Bedrock VERTICAL EXAGGERATION 50X Coastal Plain Formations Qcm1-Qe 27-3177 27-1395 27-2435 27-1119 US ROUTE 130 HARTFORD ROAD 27-3279 27-1001 Tp Qcm1 Tp Tp Qcm1-Qe 27-7063 27-8497 HARTFORD ROAD COX ROAD 0 20 40 -20 -40 -60 -80 ELEVATION (feet) 60 80 100 B VERTICAL EXAGGERATION 50X B' 100 80 60 40 20 0 -20 -40 -60 -80 BEND IN SECTION DELAWARE RIVER B1 B2 B4 B5 B6 B7 B25 B24 B23 B9 B22 B10 B21 B11 B12 B20 B13 B14 B18 B17 B15 B16 B19 Qcm2 Qwf Qm Qal afd Qm Qtl Qcm2 Bedrock Coastal Plain Formations 27-9694 27-2694 27-6880 CONRAIL RR HIGHLAND AVENUE 31-4864 Tp Qm Qal Qtl Qtu Qcm2 Qcm1 Tp 5-40 feet of tributary stream incision, as much as 60 feet of stream incision in main Delaware Valley 20-50 feet of stream incision erosion and stream incision weathering and extensive erosion, new drainage established CORRELATION OF MAP UNITS Holocene late middle early Pliocene Pleistocene aft afd Qwf Qe afd aft Qal Qm Qe Qwf Qtl Qtu Qcm2 Qcm1 Tp Qe- Qcm1/Tp Qwcp ! 27-5314 33 . 27-3695 46 ! ! ! 12 Qcm 15 Tp INTRODUCTION Surficial sediments in the New Jersey part of the Beverly and Frankford quadrangles include artificial fill and fluvial, estuarine, and salt-marsh deposits. They are as much as 60 feet thick beneath and adjacent to the Delaware River but are generally less than 30 feet thick elsewhere. The deposits are described below. They record five main periods of deposition, separated by four episodes of valley erosion. The age of the deposits and the erosion intervals are shown on the correlation chart. The underlying bedrock and Coastal Plain formations are mapped by Stanford and Sugarman (2008). 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 or 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 natural deposits beneath fill and dredge spoils is based in part on the position of shorelines and salt marshes shown on topographic map sheet 58 (N. J. Geological Survey, 1906, scale 1:21,120). DREDGE SPOILS--Fine-to-medium sand, silty fine-to-medium sand, minor coarse sand; gray, very pale brown; minor pebble-to-cobble gravel, and fragments of schist and gneiss. Chiefly 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 from units Qm and Qal, and underlying schist and gneiss bedrock, excavated during dredging of shipping channels. TRASH FILL--Trash mixed and covered with silt, clay, sand, and minor gravel. As much as 40 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 variable amounts of wood and fine organic matter. Sand and silt is massive to weakly stratified. Gravel occurs in massive to weakly stratified beds generally less than 2 feet thick. Sand is chiefly quartz with some glauconite and mica. Gravel is chiefly white, gray, and yellow- stained quartz and quartzite, and a trace of gray chert. Sand and gravel may be locally cemented with iron. As much as 15 feet thick. Deposited in modern floodplains and stream channels, and in former floodplains and channels beneath estuarine deposits before Holocene sea-level rise. Beneath the Delaware River (sections AA', BB', CC'), alluvium includes pebble-to-cobble gravel derived, in part, from erosion and reworking of unit Qwf. This gravel is exposed in dredge spoils and includes much gray and red siltstone and sandstone, and minor gray gneiss and schist, in addition to the quartz, quartzite, and chert that constitute the gravel fraction of alluvium in tributary valleys. SALT-MARSH AND ESTUARINE DEPOSITS--Silt, sand, peat, clay; brown, dark-brown, gray, black; and minor pebble 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 8,000 years. EOLIAN DEPOSITS--Fine-to-medium sand, yellowish-brown to very pale brown. Sand is chiefly quartz with some glauconite and mica. As much as 15 feet thick. Form low dunes. These are windblown sediments reworked from the underlying and adjacent Cape May Formation. GLACIOFLUVIAL DEPOSITS--Fine-to-medium sand, minor coarse sand; yellowish-brown, light reddish-brown, grayish-brown; pebble gravel, minor cobble gravel. Sand is chiefly quartz and gray siltstone fragments with a little glauconite, feldspar, and a few red siltstone fragments. Gravel is chiefly white and gray quartz and quartzite; gray chert, siltstone, and sandstone; minor red siltstone and sandstone and gray gneiss. As much as 40 feet thick. Laid down by glacial meltwater descending the Delaware Valley during the late Wisconsinan glaciation, between 20,000 to 15,000 years ago. Form a terrace along the Delaware River at a surface elevation of 10 to 15 feet in the Burlington area. Eroded remnants of the deposits are covered by estuarine sediments downstream from Burlington (sections BB', CC'). The glaciofluvial deposits are equivalent to the Trenton Gravel of Lewis (1880) and Cook (1880), later termed the Van Sciver and Spring Lake beds by Owens and Minard (1979), all named for exposures in the Trenton area, 10 miles northeast of Burlington. Because these names were also used for older, interglacial estuarine deposits elsewhere in the Delaware Valley that are now included in the Cape May Formation, they are not used here. LOWER TERRACE DEPOSITS--Fine-to-coarse sand, minor silt; yellow, yellowish-brown, light gray; pebble gravel. Sand is chiefly quartz, with some glauconite and mica, and minor feldspar and, in deposits along the Delaware River, gray siltstone fragments. Gravel is chiefly white, gray, and yellow-stained quartz and quartzite, and a trace of gray chert. In deposits along the Delaware River, gravel also includes some gray siltstone, and minor red siltstone and gray gneiss and schist. As much as 30 feet thick along the Delaware River, 15 feet thick along Rancocas Creek. Form stream terraces with surfaces 5 to 20 feet above the modern estuary. UPPER TERRACE DEPOSITS--Fine-to-medium sand, minor silt and coarse sand; yellow, reddish-yellow, brownish-yellow, light-gray, locally olive-yellow; and pebble gravel. Sand is chiefly quartz with some glauconite and mica and a trace of feldspar. Gravel is chiefly white, gray, and yellow-stained quartz and quartzite, and a trace of gray chert. As much as 25 feet thick. Form stream terraces with surfaces 15 to 30 feet above modern flood plains. 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 cobble gravel. Unstratified to well- stratified. Sand is quartz with a little glauconite and a trace of mica, chert, feldspar, and gray siltstone fragments. Gravel is chiefly white, gray, and yellow- stained quartz and quartzite, gray chert, and a trace of gray and red siltstone and sandstone. As much as 50 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 and fluvial-estuarine deposit of Sangamonian 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 and fluvial-estuarine deposit of uncertain age that forms a terrace with a maximum elevation of about 70 feet. Because it 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). Salisbury and Knapp (1917) included stream terrace deposits within the Cape May Formation; here they are mapped separately as the upper and lower terrace deposits (units Qtl and Qtu) because they differ in age and origin from the Cape May Formation. PENSAUKEN FORMATION (Salisbury and Knapp, 1917)--Fine-to-coarse sand to clayey sand, minor silt and very coarse sand; reddish-yellow to yellow; and 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, massive beds in places at the base of the formation, where it may include some cobble gravel. Sand is chiefly quartz with some feldspar, mica, and glauconite, and a few rock fragments (chert and shale) (Bowman and Lodding, 1969; Owens and Minard, 1979). Feldspar is partially or fully weathered to a white clay. Gravel is chiefly 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 generally 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 40 to 60 feet in the southeastern corner of the map area to 70 to 80 feet in the Fairview-New Albany area, to sea level, or slightly below, adjacent to the Delaware River between Beverly and Palmyra, where the Pensauken is locally preserved in erosional remnants beneath the Cape May Formation. The variation in basal elevation reflects overall 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 Cretaceous formations. Regional paleoflow data (Owens and Minard, 1979; Martino, 1981), and the provenance of the sand and gravel, 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 central and southeastern parts of the former river valley. The age of the Pensauken is not firmly established. Berry and Hawkins (1935) described plant fossils from the Pensauken near New Brunswick, New Jersey that they considered to be of early Pleistocene age. Owens and Minard (1979) assigned a late Miocene age, based on correlation to 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). A Pliocene age is also consistent with the geomorphic and stratigraphic relation of the Pensauken to late Pliocene or early Pleistocene till and to middle and late Miocene marine and fluvial deposits in central New Jersey (Stanford, 1993). THIN EOLIAN DEPOSITS AND CAPE MAY FORMATION, UNIT 1, OVERLYING PENSAUKEN FORMATION--Fine-to-medium sand, yellowish- brown to very pale brown, as in units Qe and Qcm1, less than 6 feet thick, over 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, featheredged, or gradational; dotted where concealed by water or 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. In well logs, contact with underlying bedrock or Cretaceous formation placed at report of change from yellow or brown sand or sand and gravel to white, gray, green, or red clay and sand. Where logs are of sufficient detail to identify multiple surficial units, 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. A "<" indicates that base of unit is shallower than depth shown. Identifiers of the form 27-xxxx or 31-xxxx are well permits issued by the N. J. Department of Environmental Protection, Bureau of Water Allocation. Identifiers prefixed by B are test borings for the Tacony-Palmyra bridge. Identifiers prefixed by J, CB, and TP are test borings for channel dredging from the U. S. Army Corps of Engineers. Identifiers prefixed by JPO are auger borings recorded on unpublished field maps of J. P. Owens (U. S. Geological Survey) on file at the N. J. Geological Survey. Identifiers prefixed by DM are test borings made in 1958 by the Dames and Moore Co. (provided by J. A. Fischer) 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. Surficial material observed in exposure, excavation, or hand-auger hole Surficial material observed in former exposure--From permanent note collection of the N. J. Geological Survey. Excavation perimeter--Line at limit of excavation. Sand pit--Inactive in 2004. Shallow topographic basin--Line at rim, pattern in basin. Depth generally less than 5 feet. Most basins were likely formed by melting of permafrost after the last glacial maximum about 20,000 years ago, some may have been formed by wind erosion or ground-water processes. Drawn from air photos taken in 1979. Pensauken Formation subcrop--Pensauken Formation formerly observed underlying Cape May Formation in excavation. Depth, in feet below land surface, of base of unit indicated next to unit symbol. From permanent note collection of the N. J. Geological Survey. REFERENCES 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 Ph.D. 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 Ph.D. 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. 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., 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 1067 D, 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. Stanford, S. D. and Sugarman, P. J., 2008, Bedrock geology of the Beverly and Frankford quadrangles, Burlington County, New Jersey: N. J. Geological Survey Open-File Map OFM 71, scale 1:24,000. 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.

SURFICIAL GEOLOGY OF THE BEVERLY AND FRANKFORD … · Surficial sediments in the New Jersey part of the Beverly and Frankford quadrangles include artificial fill and fluvial, estuarine,

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Page 1: SURFICIAL GEOLOGY OF THE BEVERLY AND FRANKFORD … · Surficial sediments in the New Jersey part of the Beverly and Frankford quadrangles include artificial fill and fluvial, estuarine,

7000 FEET1000 10000 2000 3000 4000 5000 6000

.5 1 KILOMETER1 0

SCALE 1:24 0001/ 21 0 1 MILE

MA

GN

ET

IC N

OR

TH

APPROXIMATE MEANDECLINATION, 1999

TR

UE

NO

RT

H

�

LOCATION IN NEW JERSEY

13O

CONTOUR INTERVAL 20 FEET

NATIONAL GEODETIC VERTICAL DATUM OF 1929

SURFICIAL GEOLOGY OF THE BEVERLY AND FRANKFORD QUADRANGLES

BURLINGTON COUNTY, NEW JERSEY

Base from U. S. Geological Survey Frankford quadrangle (1997) and Beverly quadrangle (1995) Geology mapped 2004-2005Cartography by S. Stanford and M. Girard

2'30" CAMDEN 57'30"75o00' 55'MOORESTOWN 74o52'30"40o00'

BR

ISTO

L

5'

74o52'30"

75o00'

40o00'

2'30"

byScott D. Stanford

2008

Research supported by the U. S. Geological Survey, National Cooperative Geologic Mapping program,under USGS award number 04HQAG0043. 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.

DEPARTMENT OF ENVIRONMENTAL PROTECTIONLAND USE MANAGEMENTNEW JERSEY GEOLOGICAL SURVEY

SURFICIAL GEOLOGY OF THE BEVERLY AND FRANKFORD QUADRANGLESBURLINGTON COUNTY, NEW JERSEY

OPEN-FILE MAP OFM 70

Prepared in cooperation with theU. S. GEOLOGICAL SURVEY

NATIONAL GEOLOGIC MAPPING PROGRAM

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B

Qtl

Qm

Qm

B110 fill38 Qcm2

B238 Qcm2

B535 Qcm2

B441 Qcm2

B725 water42 Qm44 Qal

B823 water48 Qm58 Qal

B939 water57 Qm59 Qal

B1035 water56 Qm59 Qal

B1124 water27 Qm40 QwfB127 water18 Qm49 Qwf

B137 water18 Qm39 Qwf

B1416 Qm58 Qwf

B1514 Qm28 Qwf

B1619 Qm25 Qtl

B635 water39 Qal

B2525 water48 Qm54 Qal

B2427 water43 Qm55 Qal

B2328 water53 Qm55 Qal

B2238 water58 Qm59 Qal

B2127 water37 Qm48 Qal

B206 water19 Qm36 Qwf

B1916 Qm42 Qwf

B1812 Qm22 QwfB17

9 Qm19 Qwf

27-77228 fill19 Qm40 Qwf

27-772530 Qm38 Qtl

afd

afd

27-969440

27-158334

27-269431

27-688023

27-1141824

31-486434

Qcm2

Qcm2Tp

27-77511

27-100832

Tp

B'

Qwcp

Qcm2

Qm

QalQwcp

Qal

27-30479

27-956916

27-1168712

27-927814

27-1002315

Tp

27-501225

27-110276 fill25 Qm23 Qcm2 27-7211

19

Qwcp

Qcm2

Tp

.27-69026

27-743925 27-7398

24

27-750424

27-744013 27-7565

20

27-641317

27-641216

27-1040538

27-7768

aft

aft

Qal

Qwcp

Tp

Qe-Qcm1/Tp

Qcm1

27-815419

Qtu

Tp

Qcm1

Qwcp

Qtu Qcm1

Tp

Qtu

Qtu

Qal

Qcm1

27-1009318

27-264216

27-154215

31-405912

Qtu

Qtu

Qcm1

Tp

Qe-Qcm1/Tp

27-642916

27-32809

27-101014

27-100114

27-327919

27-456810

27-706313 27-8497

22

27-932523

27-767034

27-1026524

27-153325

27-853312

27-1074517

27-1191918

27-712817 27-4534

1427-1004311

29-604323

27-775520

27-1081017

27-976016

Qcm1

Tp

Qcm2

Qcm2

Qcm1

Qm

Qal

C'Qal Tp

Qal

27-987416

27-83559

Qcm1

Qm

JPO 910

27-749725

27-769012

27-1193324

27-682825

27-705925

27-781325

27-667623

27-733025 27-9041

23

27-907412

27-900229

27-843823 27-8435

29

27-843435

27-838120

27-957215

Qcm2

Qcm2

Qal

aft

Qcm2

Qal

Qtl

Qcm2

Qal

27-461611

27-1075020

Qwcp

Tp

Tp

27-157920

QwcpTp

Qcm1

Tp

Qcm1

Qe

Qe

Qal

Qcm2

Qcm2QmQcm2

27-297030

Qal

27-119108

Qal

Qwcp

27-321621

27-138121

27-138220

27-98306

27-347425

27-146614

27-21114

28-194318

27-520227

27-120612

28-29542027-1488

15

27-26131927-1916

19

27-243524

27-31771027-139520

27-111915

27-326412

27-179624

Qe-Qcm1/Tp

Qcm1

Qcm1

27-30796

27-142218

27-283518

27-29508

27-135520

27-268811

27-424717

27-468021

Qcm1

Qcm2

Qe-Qcm1/Tp

Qal

Qwcp

27-1181115

27-1181320

27-308020

28-187437

27-202320 27-1504

39

27-232A14

27-1197434

27-120399

27-261122

27-97712

27-139432

27-1203332

DM535

DM416

DM88

DM78

DM61827-11119

15

DM214

DM310

27-23826

31-1874518

31-1874424

27-738054

DM1>35

27-1136518

27-1112530

27-788413

27-27431527-2742

18

Qtl

Qm

Qcm1

Qcm2

Qm

Qcm2

Qm

J330 water47 Qm

J435 water43 Qm

J724 water41 Qm

27-43-17321 J8

19 water41 Qm

J32B30 water38 Qm

J919 water41 Qm

J1022 water37 Qm

J1125 water33 Qm

Qm

afd

afd

afd

afdafd

afd

afd

afd

Qtl

Qtl

Qm

Qcm2

Qe

27-503325

27-125535

27-1433>47

27-60232

27-199320

27-142924

27-133234

27-130814

27-152939

27-43-28130

JPO1110

27-277534

27-195530 27-7748

3727-935725

27-1093315

27-507628

27-229915

27-771332

27-964226

27-485132

27-254634

Qcm2

Qm

Qtl

Qtl

Qcm2

Qal

Qal

27-785613

27-784120

27-714140

27-92178

JPO 932

27-150826

27-270929

Qcm2

Tp

Qcm1

Qwcp

Qcm2

QmQwcp

Qal

27-294115

27-956111

27-89432

Qcm1

Qcm1

Qcm2

27-161512

Qal

Qwcp

Qcm2

Qwcp

Qcm2

Qcm1

Qwcp

Qal

Qcm2

27-85346

Qcm2

27-14629<34

27-2723<34

Qal

Qe-Qcm1/Tp

A'

Qcm1

Qcm1

27-168915

27-1067317

27-33239

27-1122734

12 Qcm15 Tp

27-805914

27-354818

27-465948

27-1043921

27-40509

27-53157

Qcm2

Qcm1

Qcm1

Qcm2

27-906047

27-264643

27-918548

27-930831

27-25923727-2612

45

27-1053627

27-1189145

27-1180822

27-145230

27-99081527-11476

18

27-337940

27-7164>32JPO4

17 Qcm27 Tp

Qcm2

15 Qcm2Tp

27-1207320

JPO1044

Qm

27-43-21820

Qe

Qal

Qtl

Qm

Qtlafd

CB7132 water37 Qm

CB4126 water41 Qm J27

21 water36 Qm

CB429 water36 Qm

J2830 water43 Qm

CB7227 water>45 Qm

27-152851

27-45055327-2989

56

27-35658

27-538518

Qcm2

QalQm

Qcm2

Qe

CB4221 water36 Qm

CB522 water35 Qm

TP25A26 water34 Qm

TP2624 water>40 Qm

27-99136

27-1087413

27-108758

27-10876527-1364131

Qe27-34-78830

Qcm2 Qwf

27-685520

27-437924

27-438068 27-3695

46

TP28A30 water31 Qm

TP3028 water29 Qm

TP2923 water37 QmTP27

27 water35 Qm

CB628 water35 Qm

27-382024

27-381725

27-874640 27-8747

40

27-381522

27-381625

27-542644

27-369442

27-531433

27-817124

QwfQm

afd

afd

A

C

27-694322

27-30898

0

20

40

-20

-40

-60

-80

EL

EVA

TIO

N (

feet

)

60

80

100

120A

DE

LA

WA

RE

RIV

ER

BU

RL

ING

TON

AV

EN

UE

PIN

E S

TR

EE

T

CO

NR

AIL

RR

Qtl

Qm

Qm

Qal

Qcm2

Qcm2

Bedrock

VERTICAL EXAGGERATION 50X

J28

27-1

528

27-3

5627

-278

9

Qcm1

Tp

27-9

060

27-2

646

27-9

185

Coastal PlainFormations

BE

ND

INS

EC

TIO

N

CO

OP

ER

ST

RE

ET

US

RO

UT

E 1

30

27-3

548

27-8

059

Tp

Qcm2

Qcm1

LE

VIT

T P

AR

KW

AY

WIL

LIN

GB

OR

O P

AR

KW

AY

SA

LE

M R

OA

D

27-2

723

27-1

4629

Tp

Qcm1-Qe

A'120

100

80

60

40

20

0

-20

-40

-60

-80

0

20

40

-20

-40

-60

-80

EL

EVA

TIO

N (

feet

)

60

80

100

120C C'

120

100

80

60

40

20

0

-20

-40

-60

-80

DE

LA

WA

RE

RIV

ER

CO

NR

AIL

RR

CH

ES

TE

R A

VE

NU

E

GR

EE

NW

OO

D A

VE

NU

E

27-5

033

J32B

27-1

332

27-1

308

27-9

77

27-1

2039

27-2

023

27-1

504

27-2

32A

27-1

1974

afd

QmQm

Qcm2

Qal

Qwf

Qtl Qcm2

Qcm1

Bedrock

VERTICAL EXAGGERATION 50X

Coastal PlainFormations

Qcm1-Qe 27-3

177

27-1

395

27-2

435

27-1

119

US

RO

UT

E 1

30

HA

RT

FO

RD

RO

AD

27-3

279

27-1

001

Tp

Qcm1

Tp Tp

Qcm1-Qe

27-7

063

27-8

497

HA

RT

FO

RD

RO

AD

CO

X R

OA

D

0

20

40

-20

-40

-60

-80

EL

EVA

TIO

N (

feet

)

60

80

100B

VERTICAL EXAGGERATION 50X

B'100

80

60

40

20

0

-20

-40

-60

-80

BE

ND

INS

EC

TIO

N

DE

LA

WA

RE

RIV

ER

B1

B2

B4

B5

B6

B7

B25

B24

B23

B9

B22

B10

B21

B11

B12

B20

B13

B14

B18

B17

B15

B16

B19

Qcm2

Qwf

Qm

Qal

afd

Qm

Qtl

Qcm2

Bedrock

Coastal PlainFormations

27-9

694

27-2

694

27-6

880

CO

NR

AIL

RR

HIG

HL

AN

D A

VE

NU

E

31-4

864

Tp

QmQal

Qtl

QtuQcm2

Qcm1

Tp

5-40 feet of tributary stream incision,as much as 60 feet of stream incision in main Delaware Valley

20-50 feet of stream incision

erosion and stream incision

weathering and extensive erosion,new drainage established

CORRELATION OF MAP UNITS

Holocene

late

middle

early

Pliocene

Pleistocene

aft afd

Qwf Qe

afd

aft

Qal

Qm

Qe

Qwf

Qtl

Qtu

Qcm2

Qcm1

Tp

Qe-Qcm1/Tp

Qwcp

!27-531433

.27-369546

!

!

!12 Qcm15 Tp

INTRODUCTION

Surficial sediments in the New Jersey part of the Beverly and Frankford quadrangles include artificial fill and fluvial, estuarine, and salt-marsh deposits. They are as much as 60 feet thick beneath and adjacent to the Delaware River but are generally less than 30 feet thick elsewhere. The deposits are described below. They record five main periods of deposition, separated by four episodes of valley erosion. The age of the deposits and the erosion intervals are shown on the correlation chart. The underlying bedrock and Coastal Plain formations are mapped by Stanford and Sugarman (2008).

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 or 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 natural deposits beneath fill and dredge spoils is based in part on the position of shorelines and salt marshes shown on topographic map sheet 58 (N. J. Geological Survey, 1906, scale 1:21,120).

DREDGE SPOILS--Fine-to-medium sand, silty fine-to-medium sand, minor coarse sand; gray, very pale brown; minor pebble-to-cobble gravel, and fragments of schist and gneiss. Chiefly 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 from units Qm and Qal, and underlying schist and gneiss bedrock, excavated during dredging of shipping channels.

TRASH FILL--Trash mixed and covered with silt, clay, sand, and minor gravel. As much as 40 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 variable amounts of wood and fine organic matter. Sand and silt is massive to weakly stratified. Gravel occurs in massive to weakly stratified beds generally less than 2 feet thick. Sand is chiefly quartz with some glauconite and mica. Gravel is chiefly white, gray, and yellow-stained quartz and quartzite, and a trace of gray chert. Sand and gravel may be locally cemented with iron. As much as 15 feet thick. Deposited in modern floodplains and stream channels, and in former floodplains and channels beneath estuarine deposits before Holocene sea-level rise. Beneath the Delaware River (sections AA', BB', CC'), alluvium includes pebble-to-cobble gravel derived, in part, from erosion and reworking of unit Qwf. This gravel is exposed in dredge spoils and includes much gray and red siltstone and sandstone, and minor gray gneiss and schist, in addition to the quartz, quartzite, and chert that constitute the gravel fraction of alluvium in tributary valleys.

SALT-MARSH AND ESTUARINE DEPOSITS--Silt, sand, peat, clay; brown, dark-brown, gray, black; and minor pebble 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 8,000 years.

EOLIAN DEPOSITS--Fine-to-medium sand, yellowish-brown to very pale brown. Sand is chiefly quartz with some glauconite and mica. As much as 15 feet thick. Form low dunes. These are windblown sediments reworked from the underlying and adjacent Cape May Formation.

GLACIOFLUVIAL DEPOSITS--Fine-to-medium sand, minor coarse sand; yellowish-brown, light reddish-brown, grayish-brown; pebble gravel, minor cobble gravel. Sand is chiefly quartz and gray siltstone fragments with a little glauconite, feldspar, and a few red siltstone fragments. Gravel is chiefly white and gray quartz and quartzite; gray chert, siltstone, and sandstone; minor red siltstone and sandstone and gray gneiss. As much as 40 feet thick. Laid down by glacial meltwater descending the Delaware Valley during the late Wisconsinan glaciation, between 20,000 to 15,000 years ago. Form a terrace along the Delaware River at a surface elevation of 10 to 15 feet in the Burlington area.

Eroded remnants of the deposits are covered by estuarine sediments downstream from Burlington (sections BB', CC'). The glaciofluvial deposits are equivalent to the Trenton Gravel of Lewis (1880) and Cook (1880), later termed the Van Sciver and Spring Lake beds by Owens and Minard (1979), all named for exposures in the Trenton area, 10 miles northeast of Burlington. Because these names were also used for older, interglacial estuarine deposits elsewhere in the Delaware Valley that are now included in the Cape May Formation, they are not used here.

LOWER TERRACE DEPOSITS--Fine-to-coarse sand, minor silt; yellow, yellowish-brown, light gray; pebble gravel. Sand is chiefly quartz, with some glauconite and mica, and minor feldspar and, in deposits along the Delaware River, gray siltstone fragments. Gravel is chiefly white, gray, and yellow-stained quartz and quartzite, and a trace of gray chert. In deposits along the Delaware River, gravel also includes some gray siltstone, and minor red siltstone and gray gneiss and schist. As much as 30 feet thick along the Delaware River, 15 feet thick along Rancocas Creek. Form stream terraces with surfaces 5 to 20 feet above the modern estuary.

UPPER TERRACE DEPOSITS--Fine-to-medium sand, minor silt and coarse sand; yellow, reddish-yellow, brownish-yellow, light-gray, locally olive-yellow; and pebble gravel. Sand is chiefly quartz with some glauconite and mica and a trace of feldspar. Gravel is chiefly white, gray, and yellow-stained quartz and quartzite, and a trace of gray chert. As much as 25 feet thick. Form stream terraces with surfaces 15 to 30 feet above modern flood plains. 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 cobble gravel. Unstratified to well-stratified. Sand is quartz with a little glauconite and a trace of mica, chert,

feldspar, and gray siltstone fragments. Gravel is chiefly white, gray, and yellow-stained quartz and quartzite, gray chert, and a trace of gray and red siltstone and sandstone. As much as 50 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 and fluvial-estuarine deposit of Sangamonian 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 and fluvial-estuarine deposit of uncertain age that forms a terrace with a maximum elevation of about 70 feet. Because it 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). Salisbury and Knapp (1917) included stream terrace deposits within the Cape May Formation; here they are mapped separately as the upper and lower terrace deposits (units Qtl and Qtu) because they differ in age and origin from the Cape May Formation.

PENSAUKEN FORMATION (Salisbury and Knapp, 1917)--Fine-to-coarse sand to clayey sand, minor silt and very coarse sand; reddish-yellow to yellow; and 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, massive beds in places at the base of the formation, where it may include some cobble gravel. Sand is chiefly quartz with some feldspar, mica, and glauconite, and a few rock fragments (chert and shale) (Bowman and Lodding, 1969; Owens and Minard, 1979). Feldspar is partially or fully weathered to a white clay. Gravel is chiefly 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 generally 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 40 to 60 feet in the southeastern corner of the map area to 70 to 80 feet in the Fairview-New Albany area, to sea level, or slightly below, adjacent to the Delaware River between Beverly and Palmyra, where the Pensauken is locally preserved in erosional remnants beneath the Cape May Formation. The variation in basal elevation reflects overall 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 Cretaceous formations. Regional paleoflow data (Owens and Minard, 1979; Martino, 1981), and the provenance of the sand and gravel, 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 central and southeastern parts of the former river valley.

The age of the Pensauken is not firmly established. Berry and Hawkins (1935) described plant fossils from the Pensauken near New Brunswick, New Jersey

that they considered to be of early Pleistocene age. Owens and Minard (1979) assigned a late Miocene age, based on correlation to 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). A Pliocene age is also consistent with the geomorphic and stratigraphic relation of the Pensauken to late Pliocene or early Pleistocene till and to middle and late Miocene marine and fluvial deposits in central New Jersey (Stanford, 1993).

THIN EOLIAN DEPOSITS AND CAPE MAY FORMATION, UNIT 1, OVERLYING PENSAUKEN FORMATION--Fine-to-medium sand, yellowish- brown to very pale brown, as in units Qe and Qcm1, less than 6 feet thick, over 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, featheredged, or gradational; dotted where concealed by water or 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. In well logs, contact with underlying bedrock or Cretaceous formation placed at report of change from yellow or brown sand or sand and gravel to white, gray, green, or red clay and sand. Where logs are of sufficient detail to identify multiple surficial units, 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. A "<" indicates that base of unit is shallower than depth shown. Identifiers of the form 27-xxxx or 31-xxxx are well permits issued by the N. J. Department of Environmental Protection, Bureau of Water Allocation. Identifiers prefixed by B are test borings for the Tacony-Palmyra bridge. Identifiers prefixed by J, CB, and TP are test borings for channel dredging from the U. S. Army Corps of Engineers. Identifiers prefixed by JPO are auger borings recorded on unpublished field maps of J. P. Owens (U. S. Geological Survey) on file at the N. J. Geological Survey. Identifiers prefixed by DM are test borings made in 1958 by the Dames and Moore Co. (provided by J. A. Fischer) 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.

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

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

Excavation perimeter--Line at limit of excavation.

Sand pit--Inactive in 2004.

Shallow topographic basin--Line at rim, pattern in basin. Depth generally less than 5 feet. Most basins were likely formed by melting of permafrost after the last glacial maximum about 20,000 years ago, some may have been formed by wind erosion or ground-water processes. Drawn from air photos taken in 1979.

Pensauken Formation subcrop--Pensauken Formation formerly observed underlying Cape May Formation in excavation. Depth, in feet below land surface, of base of unit indicated next to unit symbol. From permanent note collection of the N. J. Geological Survey.

REFERENCES

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 Ph.D. 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 Ph.D. 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.

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., 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 1067 D, 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.

Stanford, S. D. and Sugarman, P. J., 2008, Bedrock geology of the Beverly and Frankford quadrangles, Burlington County, New Jersey: N. J. Geological Survey Open-File Map OFM 71, scale 1:24,000.

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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