DEPARTMENT OF ENVIRONMENTAL PROTECTION
WATER RESOURCES MANAGEMENT
NEW JERSEY GEOLOGICAL AND WATER SURVEY
Prepared in cooperation with the
U.S. GEOLOGICAL SURVEY
NATIONAL GEOLOGIC MAPPING PROGRAM
BEDROCK GEOLOGIC MAP OF THE HAMBURG QUADRANGLE
SUSSEX COUNTY, NEW JERSEY
GEOLOGIC MAP SERIES GMS 14-3
RT
O
(P
48
6
23
68
40
Omr
64
45
1
55
13
4
67
72
20
45
22
73
42
5’
44
85
25
41
7
22
19
41
20
52
90
46
7
30
12
15
47
57
69
38
1
76
20
Omr
90 87
73
10
65
22
20
Omb
50
57
67
60
45
82
TH
RU
_a
30
38
47
38 40
SW
AM
30
P
48
53
66
70
Oj
SOl
Ow 27
?
44
20
33
74
42 38
54
19
72
18
88
52
O_e
7515
43 Oo
27
27
13
33
30
18
32
32
Oj
40
35 72
44
42
26
35
25
44
41
57
44
21
42
70 52
38
43
38
29
46
_l
_a
75
SOl
43
29
31
42
32
23
50
Ylb
37
_h
Ym
SOl
Ylo
10
56
25
47
Yps
87
66
82
75
36
SOl
41
30
60
39
28
42
62
53 47
Ymh
Ypa
10’
Ybs
51
Yff
41
37
74
25
42
FOLDS
36
Antiform
Synform
Ymh
Ybh
Overturned synform
26
Yk
Ymh
40
Ylb
35
59
66
36
54
40
74
78 76
27
67
37
Ypg
41
51
Ybh
86
61
83
61
76
63
(FRANKLIN)
Ylo
86
54
Ylb
Ylo
Ymh
47
57
34
58
47
51
46
46
Ybh
77
36
Ylb
64
54
Vertical
64
Ylo
59
Reviewed by A. A. Drake, S.D. Stanford and M.J. Hozik
(N
Bearing and plunge of intersection of bedding and cleavage in Paleozoic rocks
18
_h
Bearing and plunge of mineral lineation in mesoproterozoic rocks
OTHER FEATURES
Fe
Abandoned mine - Fe, magnetite; H, hematite; L, limonite and brown hematite
R
Active rock quarry
Bore hole and Figure 12
10
Figures 10, 11, 13, 14
Yps
Yk
Ym
Sequence at Wantage (Upper Ordovician) (Monteverde and Herman, 1989) – Interbedded,
very-thin- to medium-bedded limestone, dolomite, siltstone, and argillite. Upper carbonate
facies is yellowish-brown to olive-gray-weathering, medium- to dark-gray, very-fine- to finegrained, laminated to medium-bedded limestone and dolomite. Rounded quartz sand occurs
locally as floating grains and in very thin lenses. Lower clastic facies contains medium-gray,
grayish-red to grayish-green, thin- to medium-bedded mudstone, siltstone, and fine-grained
to pebbly sandstone. Fine-grained beds commonly contain minor disseminated, subangular
to subrounded, medium-grained quartz sand and pebble-sized chert. Some coarse-grained
beds are cross-bedded. Unit is restricted to lows on the paleoerosion surface of the Middle
Ordovician unconformity. North American Midcontinent province conodonts within the
carbonate facies, identified by Harris and others (1995, p. 6) indicate a Rocklandian or
Kirkfieldian age. Unit may be as much as 150 feet thick in the quadrangle.
15
N = 886
Circle = 17%
N = 817
Circle = 19%
Figure 9. Rose diagram of joint strikes in the Proterozoic rocks.
N
20
15
Pyroxene alaskite (Mesoproterozoic) – Light-gray or tan-weathering, greenish-buff to lightpinkish-gray, medium- to coarse-grained, massive, foliated granite composed of mesoperthite
to microantiperthite, oligoclase, and quartz. Commonly contains clinopyroxene, titanite and
magnetite.
10
5
Pyroxene monzonite (Mesoproterozoic) – Gray to buff or tan-weathering, greenishgray, medium- to coarse-grained, massive, foliated rock composed of mesoperthite to
microantiperthite, oligoclase, clinopyroxene, titanite and magnetite. May contain sparse to
moderate amounts of hornblende where in contact with rocks of the Byram Intrusive Suite.
5
%
20
15
10
10
15
20
5
5
Map Area
10
Potassic feldspar gneiss (Mesoproterozoic) – Light-gray- or pinkish-buff-weathering,
pinkish-white or light-pinkish-gray, medium-grained and locally coarse-grained, foliated
gneiss composed of quartz, microcline microperthite, and oligoclase. Commonly contains
biotite, garnet, sillimanite, and magnetite.
15
20
Microcline gneiss (Mesoproterozoic) – Pale pinkish-white-weathering, tan to pinkishwhite, fine- to medium-grained, layered and foliated rock composed of quartz, microcline
microperthite, oligoclase, and biotite. Common accessory minerals include garnet, magnetite
and sillimanite. Locally contains conformable clots and lenses of partial melt. Well exposed
on Pochuck Mountain, where unit is intercalated with amphibolite.
Ymp
Clinopyroxene-quartz-feldspar gneiss (Mesoproterozoic) – Pinkish-gray- or pinkish-buffweathering, white, pale-pinkish-white, or light-gray, medium-grained and locally coarsegrained, foliated gneiss composed of quartz, microcline, oligoclase, clinopyroxene, and
trace amounts of epidote, biotite, titanite, and magnetite.
N = 314
Circle = 29%
Figure 4. Rose diagram of cleavage strikes in the Paleozoic rocks.
15
10
5
5
%
10
15
5
10
15
Pyroxene-epidote gneiss (Mesoproterozoic) – Light greenish-gray to greenish-pinkweathering, pale pinkish-white to light-gray to light-greenish-gray, medium-grained, layered
and foliated gneiss composed of quartz, oligoclase, pyroxene, epidote, microcline, titanite,
and magnetite. Locally contains scapolite and trace amounts of calcite. Unit grades into
clinopyroxene-quartz-feldspar gneiss with a decrease in epidote.
5
10
Map Area
15
N = 315
Circle = 20%
Figure 5. Rose diagram of cleavage dips in the Paleozoic rocks.
Magmatic Arc Rocks
N
Losee Metamorphic Suite (Drake, 1984; Volkert and Drake, 1999)
Ylb
Ylh
Yh
Quartz-oligoclase gneiss (Mesoproterozoic) – White-weathering, light-greenish-gray,
medium- to coarse-grained, foliated gneiss composed of oligoclase or andesine, quartz,
and varied amounts of hornblende, biotite and clinopyroxene. Locally intercalated with
amphibolite.
15
10
Biotite-quartz-oligoclase gneiss (Mesoproterozoic) – White- or light-gray-weathering,
medium-gray or greenish-gray, medium- to coarse-grained, layered and foliated gneiss
composed of oligoclase or andesine, quartz, biotite, and local garnet. Some outcrops
contain hornblende.
FEET
600
Hornblende-quartz-oligoclase gneiss (Mesoproterozoic) – Unit consists of two main
variants. At Hamburg Mountain, unit is white weathering, light-greenish-gray, medium- to
coarse-grained, foliated gneiss containing oligoclase or andesine, quartz, hornblende, and
magnetite. This variant is spatially associated with quartz-oligoclase gneiss. At Pochuck
Mountain, unit is gray-weathering, greenish-gray, medium-grained, well-layered gneiss
containing oligoclase or andesine, quartz, hornblende, biotite, and magnetite. This variant
is interlayered with biotite-quartz-plagioclase gneiss and amphibolite. Both variants contain
local clinopyroxene.
Ya
Ysk
Allentown Dolomite (Upper Cambrian) (Wherry, 1909) – Upper sequence is light- to
medium-gray-weathering, medium-light- to medium-dark-gray, fine- to medium-grained,
locally coarse-grained, medium- to very-thick-bedded dolomite; local shaly dolomite near
the bottom. Floating quartz sand and two sequences of medium-light- to very-light-gray,
medium-grained, thin-bedded quartzite and discontinuous dark-gray chert lenses occur
directly below upper contact. Lower sequence is medium- to very-light-gray weathering,
light- to medium-dark-gray, fine- to medium-grained, thin- to medium-bedded dolomite
and shaly dolomite. Weathered exposures characterized by alternating light- and darkgray beds. Ripple marks, oolites, algal stromatolites, cross-beds, edgewise conglomerate,
mud cracks, and paleosol zones occur throughout but are more abundant in the lower
sequence (fig. 11). Unit grades down into the Leithsville Formation. Howell (1945) describes
Trempealeauian (Late Cambrian) faunas, in the upper part of the formation, from Newton
and Blairstown, New Jersey. At Carpentersville the lower part contains a trilobite fauna of
Dresbachian (early Late Cambrian) age (Weller, 1903; Howell, 1945). Unit is approximately
1,800 ft. thick in map area.
Yu
15
15
10
5
%
5
10
HB-3
Amphibolite (Mesoproterozoic) – Grayish-black, fine- to medium-grained, foliated rock
composed of hornblende, andesine and local clinopyroxene. Most amphibolite is interpreted
to be metavolcanic, and amphibolite east of Glenwood Lake contains relict pillow structures
(Hague and others, 1956; Volkert and others, 1986). Some amphibolite layers within
metasedimentary rocks may be metasedimentary in origin. Unit is associated with rocks of
the Losee Suite and with supracrustal rocks; both types are shown undivided on the map.
Unit is exposed throughout Pochuck Mountain.
N
_r
_a
Hardyston Quartzite
Mesoproterozoic rocks undivided
100
0
100
200 FEET
6
4
Mesoproterozoic rocks, undifferentiated – Shown in cross section only.
6
%
10
8
8
10
6
4
6
N
8
20
N = 608
Circle = 11%
15
10
Figure 7. Rose diagram of joint strikes in the Paleozoic rocks.
10
Map Area
5
N
%
20
15
15
20
5
10
5
5
4
10
3
15
2
Figure 13. Angluar unconformity at hammerhead between Hardyston Quartzite (top right) and biotite-quartz-oligoclase gneiss (lower left). (Richard Volkert)
20
N = 781
Circle = 23%
East Fault
Pochuck Fault
Lake Panorama Fault
A’
FEET
FEET
B
%
3
5
4
3
4
5
2
Figure 2. Rose diagram of bedding strikes in the Paleozoic rocks. N is the number of surfaces analyzed on this and subsequent figures.
Chestnut Hill Formation (Neoproterozoic) – Interbedded sequence of reddish-brown, gray,
or buff, medium-grained, thin-bedded quartz-pebble conglomerate, ferruginous sandstone,
chloritic siltstone, quartzite, and phyllite. Thickness in the map area ranges from 20 to 50
feet.
3
4
Map Area
_a
B’
FEET
Oo
O_e
O_e
Ylo
Ya
Ym
Yp
_l
Yff
_a _a
Yu
Yu
Ya
Ymp
Ylh
Yu
Yff
-1,000
-1,000
_h
_h
_r
_a
_l
Yu
Omr
Oj
O_e
Omb
Oo
-2,000
-3,000
-2,000
-3,000
Omb
Oj
_r
_a
_a
Oo
O_e
_r
_l
_h
_h
Ylb
_h
Ym
Ylo
Ymh
_l
_h
_h
Ybh
Ybs
Ym
Ylb
Yu
Yu
Ylb
Ylo
Ylo
_l
_l _a
_l
Ylo
Ym
1,000
Ylo
Yp
_h
_r
Oo
Ya
Ym
O_e
SEA LEVEL
Yp
_l
?
_a
Oj
_r
_h
_a
Yfw
Yu
SEA LEVEL
Oo O_e
?
O_e
_r
Ylb
Ylh
_h
_l
O_e
Oo
_l _h
_l
_r
Yp
Omb
Ow
Oj Oo O_e
Ym
_l
Omb
1,000
Ylb
Yff
Yff
Ym
Ybh
Ype
-100
-200
-300
-400
Figure 12. Cross section, based on five New Jersey Zinc (NJZ) Company borings, showing an open
fold in the Hardyston Quartzite and Leithsville Formation. Note the green siltstone maker bed of NJZ
is the middle sequence of the Leithsville. Revised from New Jersey Zinc Company drawings (1953)
on file at the New Jersey Geological and Water Survey.
8
Hornblende-pyroxene skarn (Mesoproterozoic) – Greenish-black, medium- to coarsegrained, poorly foliated rock composed mainly of hornblende and clinopyroxene. Grades
into massive, dark-green, nearly monomineralic clinopyroxene skarn, with both rock types
spatially associated with quartz-poor pyroxene gneiss. Unit occurs as a single body on
Pochuck Mountain.
Hardyston Quartzite (Lower Cambrian) (Wolff and Brooks, 1898) – Medium- to light-gray,
fine- to coarse-grained, medium- to thick-bedded quartzite, arkosic sandstone and dolomitic
sandstone. Unconformably overlies Neoproterozoic and Mesoproterozoic rocks (fig. 13).
Elsewhere, contains Scolithus linearis(?) and fragments of the trilobite Olenellus thompsoni
of Early Cambrian age (Nason, 1891; Weller, 1903). Thickness in map area ranges from 5
to 100 feet but rarely exceeds 20 feet.
?
-3,000
_h
_a
O_e
O_e _r
arker
Figure 8. Rose diagram of joint dips in the Paleozoic rocks.
1,000
_a
ne m
5
1,000
Oj
siltsto
-400
Ypa
-2,000
green
Pleistocene deposits
10
2,000
Oo
100
Horizontal scale
2,000
Omb
arker
Leithsville Formation
-300
2,000
Omr
ne m
SEA LEVEL
-100
2,000
-1,000
siltsto
SEA LEVEL
N = 722
Circle = 19%
-200
10
300
200
green
Figure 6. Rose diagram of foliation strikes in the Proterozoic rocks.
5
500
15
3,000
Oj
Map Area
100
Hypersthene-quartz-plagioclase gneiss (Mesoproterozoic) – Gray or tan-weathering,
greenish-gray to greenish-brown, medium-grained, greasy-lustered, foliated gneiss
composed of andesine or oligoclase, quartz, clinopyroxene, hornblende, and orthopyroxene.
Commonly intercalated with amphibolite and mafic-rich quartz-plagioclase gneiss.
Leithsville Formation (Middle and Lower Cambrian) (Wherry, 1909) – Upper sequence,
seldom exposed, is mottled, light- to medium-dark-gray-weathering, medium- to mediumdark-gray, fine- to medium-grained, medium- to thick-bedded dolomite, locally pitted and
friable. Middle sequence is grayish-orange to light- to dark-gray to grayish-red to lightgreenish- to dark-greenish-gray-weathering, aphanitic to fine-grained, thin- to mediumbedded dolomite, argillaceous dolomite, dolomitic shale, quartz sandstone, siltstone and
shale (fig. 12). Lower sequence is light- to medium-gray-weathering, medium-gray, fine- to
medium-grained, thin- to medium-bedded dolomite. Quartz-sand lenses occur near lower
gradational contact with Hardyston Quartzite. Archaeocyathids of Early Cambrian age
were found in the formation nearby in Franklin, New Jersey, suggesting an intraformational
disconformity between Middle and Early Cambrian time (Palmer and Rozanov, 1967;
McMenamin and others, 2000). Unit also contains Hyolithellus micans (Offield, 1967;
Markewicz, 1968). Howell (1945) identified as a Dresbachian (early Late Cambrian) fauna
in the shaly member of the Leithsville Formation at Peapack, New Jersey. Thickness is
approximately 600 feet in map area.
600
400
200
10
FEET
HB-4
300
3,000
SEA LEVEL
HB-1
HB-2
HB-5
400
3,000
Oo
500
5
Other Rocks
Rickenbach Dolomite (Upper Cambrian) (Hobson, 1957) – Upper part is medium- to darkgray, fine- to coarse-grained, medium- to thick-bedded dolomite, locally fetid, and weathers
to a mottled surface. Contains pods and lenses of dark-gray to black chert near the upper
contact and a distinctive thinly interbedded sequence of medium-grained dolomite with
up to seven thin convex upward black chert layers occurs about 50 to 75 feet below the
contact. Lower part is medium- to dark-gray, fine- to medium-grained, thin- to mediumbedded dolomite. Floating quartz sand grains and quartz-sand stringers occur in the basal
part of unit. Lenses of light-gray, coarse- to very-coarse-grained dolomite locally occur
throughout the unit. Lower contact with the Allentown is placed at top of distinctive mediumgray quartzite. Contains conodonts of Cordylodus proavus to Cordylodus lindstomi zones
of North American Midcontinent province, as used by Sweet and Bergstrom (1986). Unit
correlates to Beekmantown Group, lower part of Drake and others (1996) (fig. 1). Unit may
be as much as 300 ft. thick in the quadrangle.
Figure 11. Stromatolites on a glacially polished bedding plane surface in the Allentown Dolomite.
The near horizontal lines (grooves) which parallel the hammerhead are glacial striae. (Donald
Monteverde)
3,000
Omr
Figure 10. Cross cutting relationships between a Lamprophyre dike striking N30oW and dipping 90o
cutting microcline gneiss and fault related breccia veins striking N70oE and dipping 70oS. Notice the
sharp contact between the dike and the country rock. (Richard Volkert)
N
Yff/Yfw Franklin Marble and Wildcat Marble (Mesoproterozoic) – White- to light-gray-weathering,
white or grayish-white, coarse-crystalline, calcitic to locally dolomitic marble with accessory
graphite, phlogopite, amphibole, clinopyroxene and chondrodite. Separated by New Jersey
Zinc Company geologists (Hague and others, 1956) into a lower Franklin marble layer
(Yff) and an upper Wildcat marble layer (Yfw), separated by gneiss. Locally contains relict
karst features in the form of bedrock pinnacles, solution caves, and paleo-solution breccia.
Franklin Marble layer is host rock for Zn-Fe-Mn deposits at the Franklin and Sterling Hill
mines to the south, in the Franklin quadrangle.
Epler Formation (Lower Ordovican and Upper Cambrian) (Hobson, 1957) – Upper part is
light-olive- to dark-gray, fine- to medium-grained, thin- to thick-bedded, locally laminated
dolomite. Middle part is olive-gray, light-brown, or dark-yellowish-orange-weathering, darkgray, aphanitic to fine-grained, laminated to medium-bedded dolomite and light-gray to
light-bluish-gray-weathering, medium- to dark-gray, fine-grained, thin-to medium-bedded
limestone, that is characterized by mottling and reticulate dolomite and light-olive-gray
to grayish-orange-weathering, medium-gray dolomitic shale laminae surrounding the
limestone lenses. Limestone grades laterally and down section into medium-gray, finegrained dolomite. Lower part is medium-light- to dark-gray, aphanitic to medium-grained,
laminated to medium-bedded dolomite. Contains white and dark-gray chert lenses. Lower
contact with the Rickenbach is placed at the transition from a massive, finely laminated,
very-fine-`grained, dark gray dolomite to the underlying massive light gray, medium to
coarse grained pitted dolomite. Contains conodonts of Cordylodus lindstomi to Rossodus
manitouensis zones of the North American Midcontinent province as used by Sweet and
Bergstrom (1986). The Cambrian-Ordovician boundary, based on the final acceptance of
the Global Stratotype Section and Point base (GSSP) for the Ordovician, at Green Point,
Newfoundland (Cooper and others, 2001), now occurs within the lower third of the Epler,
at the top of the Cordylodus lindstromi zone, within the fauna B as used in Karlins and
Repetski (1989). Unit correlates to Beekmantown Group, lower part of Drake and others
(1996) (fig. 1). Unit is approximately 420 feet thick in map area.
15
Figure 3. Rose diagram bedding dips in the Paleozoic rocks.
2014
Route 23
A
6
12
Pyroxene granite (Mesoproterozoic) – Light-gray to buff or white-weathering, greenishgray, medium- to coarse-grained, massive, foliated granite composed of mesoperthite
to microantiperthite, quartz, oligoclase, and clinopyroxene. Commonly contains titanite,
magnetite, apatite, and pyrite. Sparse to moderate amounts of hornblende may be present
where in contact with rocks of the Byram Intrusive Suite. Unit includes small bodies of
pegmatite too small to be shown on the map.
Hornblende-quartz-feldspar gneiss (Mesoproterozoic) – Pinkish-gray to buff-weathering,
light-pinkish-white to pinkish-gray, medium-grained, massive to moderately well layered and
foliated gneiss containing microcline, quartz, oligoclase, hornblende, and magnetite. Locally
contains garnet and biotite.
Ylo
15
12
9
9
Yp/Yap Pyroxene gneiss (Mesoproterozoic) – White- or tan-weathering, greenish-gray, mediumgrained, layered and foliated gneiss containing oligoclase, clinopyroxene, and titanite. Locally
contains quartz, epidote, scapolite, or calcite. Mafic variants (Yap) containing abundant
hornblende, clinopyroxene, and titanite are interlayered with quartz-poor pyroxene gneiss.
Unit is spatially associated with amphibolite and marble.
Ontelaunee Formation (Lower Ordovician) (Hobson, 1957) – Upper beds, locally preserved,
are light- to medium-gray to yellowish-gray-weathering, light- to medium-gray, aphanitic to
medium grained, thin- to thick-bedded, locally laminated, dolomite, slightly fetid. Mediumto dark-gray, fine-grained, medium-bedded, sparsely fossiliferous limestone lenses occur
locally. Lower beds are medium- to dark-gray, medium- to coarse-grained, medium- to thickbedded dolomite, strongly fetid, and weather to a mottled surface. Contains pods and lenses
of white, dark-gray to black chert. Cauliflower-textured black chert beds of varied thickness
occur locally. Lower contact gradational and placed at top of laminated to thin-bedded
dolomite of the Epler Formation. Contains conodonts high in the Rossodus manitouensis
zone to Oepikodus communis zone of the North American Midcontinent province as used by
Sweet and Bergstrom (1986). Unit correlates to Beekmantown Group, upper part of Drake
and others (1996) (fig. 1). Thickness ranges from 0 to 400 feet in map area.
12
10
Hornblende monzonite (Mesoproterozoic) – Tan to buff-weathering, pinkish-gray or
greenish-gray, medium- to coarse-grained, foliated monzonite and, less commonly, quartz
monzonite composed of microcline microperthite, oligoclase, hornblende, and magnetite.
Locally contains quartz. Sparse to moderate amounts of clinopyroxene may be present
where in contact with rocks of the Lake Hopatcong Intrusive Suite.
Ymh
Ype
15
5
Back-Arc Basin Supracrustal Rocks
Jacksonburg Limestone (Upper Ordovician) (Spencer and others, 1908, Miller,
1937) – Medium-dark-gray-weathering, medium- to dark-gray, laminated to thin-bedded,
argillaceous limestone (cement-rock facies) and minor arenaceous limestone. Grades
downward into medium-bluish-gray-weathering, dark-gray, very-thin- to medium-bedded,
commonly fossiliferous, interbedded fine- and medium-grained limestone and pebble-andfossil limestone conglomerate (cement-limestone facies). At places, the basal sequence
contains a thick- to very-thick-bedded dolomite cobble conglomerate that has a limestone
matrix. Locally, lower contact is conformable on the discontinuous carbonate facies of
“Sequence at Wantage”. Elsewhere, it is unconformable on rocks of the Beekmantown
Group or the clastic facies of “Sequence at Wantage”. Weller (1903), based on extensive
fossil collections from numerous localities throughout the region, correlated this unit to the
lower Trenton of New York. Unit contains North American Midcontinent province conodont
zones Phragmodus undatus to Aphelognathus shatzeri that range from Rocklandian to
Richmondian ages (Sweet and Bergstrom, 1986). Harris and others (1995, p. 6) indicate
the Jacksonburg is no older than the Plectodina tenuis zone (Kirkfieldian Stage). Unit is as
much as 200 feet thick in the quadrangle.
9
%
15
5
10
Microperthite alaskite (Mesoproterozoic) – Buff or pale-pinkish-white-weathering, pinkishgray to light-grayish-tan, or pinkish-white, medium- to coarse-grained, foliated granite
composed of microcline microperthite, quartz, and oligoclase, Locally contains hornblende
and magnetite.
NEW JERSEY HIGHLANDS
Zch
15
10
N= 607
Circle = 6%
Pochuck Mountain
N O R TH
HB-1
Ypa
5
%
Richard F. Dalton1, Richard A. Volkert1, Donald H. Monteverde1,
Gregory C. Herman1, and Robert J. Canace2
New Jersey Geological and Water Survey, Trenton, New Jersey 08625
Ridge & Valley Conservancy, Blairstown, New Jersey 07825
FEET
20
Form line showing foliation in Mesoroterozoic rocks. Shown in cross section only.
Crooked Swamp Fault
ET IC
TRUE NORTH
MAGN
2
LINEAR FEATURES
by
APPROXIMATE MEAN
DECLINATION, 1994
Strike and dip of parallel bedding and slaty cleavage
Research supported by the U. S. Geological Survey, National Cooperative
Geologic Mapping Program, under U.S.G.S. 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.
Wallkill River
N
EA
S
T)
CONTOUR INTERVAL 20 FEET
Strike and dip of cleavage in Paleozoic rocks
6
Bedrock Geologic Map of the Hamburg Quadrangle
Sussex County, New Jersey
13°
1
20
Digital cartography by R.S. Pristas
Polyconic projection. 1927 North American datum 10,000-foot grid
based on New Jersey coordinate system 1000-meter Universal
Transverse Mercator grid ticks, zone 18.
LOCATION IN
NEW JERSEY
)
1 KILOMETER
D
0
.5
7000 FEET
Overturned
N
LA
6000
65
D
Bedrock geology mapped by F.J. Markewicz and R.F. Dalton, 1968-1973;
R.J. Canace 1980-1988;
R.F. Dalton, R.J. Canace, R.A. Volkert, D.H. Monteverde and G.C. Herman,1994-1995;
R.F. Dalton, R.A. Volkert, D.H. Monteverde, G.C. Herman and R.J Canace, 2012-2013
N
Topography from aerial photographs by stereophotogrammetric
methods. Aerial photographs taken 1942 and 1951. Field check 1943.
Culture revised by the United States Geological Survey 1954.
5000
Vertical
U
1
4000
Inclined
41o07’30”
74o30’
1 MILE
3000
2000
40
Yh
Yh
71
_l
Strike and dip of beds
FO
EW
1000
0
Inclined
(N
1000
62
74
70
32’30”
0
Strike and dip of crystallization foliation
75 86
Ylb
34
PLANAR FEATURES
Yh
SCALE 1:24 , 000
2
Gently inclined to recumbent syncline
Ypa
Yk
46
41
48
Gently inclined to recumbent anticline
B’
Ymh
_a
Syncline
Ybh
Ylh
Ybs
Anticline
65 72
Ylo
71
25
Ybh
86
54
Folds in Paleozoic rocks showing trace of axial surface, direction and dip of limbs, and direction of
plunge. Folds in bedding and/or cleavage. Dotted where concealed.
Ylo
Ypa
35
50
14
Minor asymmetric fold
40
22
76
71
_r
Overturned antiform
47
78
73
76
Control by USC&GS and New Jersey Geodetic Survey
Folds in Proterozoic rocks showing trace of axial surface, direction and dip of limbs, and direction
of plunge. Dotted where concealed.
36
Ylb
Ymh
Ybs
Ybs
Ype
Ybh
.5
Reverse fault - U, upthrown side; D, downthrown side
Brittle deformation zone
28
Ybs
76
1
Normal fault - U, upthrown side; D, downthrown side
D
U
62 56 54
51
67
54
43
35’
Topographic base mapped by the Army Map Service.
Edited and published by the United States Geological Survey
U
D
Ypg
Bushkill Member of Martinsburg Formation (Upper Ordovician) (Drake and Epstein,
1967) – Medium- to medium-dark-gray-weathering, dark-gray to black, thinly-laminated to
medium-bedded shale and slate; less abundant medium-gray to brownish-gray-weathering,
dark-gray to black, laminated to thin-bedded, graywacke siltstone. Unit forms fining-upward
sequences characterized by either basal cross-bedded siltstone grading upward through
planar laminated siltstone into slate, or laminated siltstone grading upward into slate.
Locally, some of the fining-upward cycles may have a lower planar laminated siltstone
beneath the cross-bedded layer. Complete cycles may be an inch to several feet thick
and slate comprises the thickest part. Lower contact with the Jacksonburg Limestone
is gradational, but commonly disrupted by thrust faulting. Parris and Cruikshank (1992)
showed that regionally, the unit contains graptolites of zones Diplograptus multidens to
Corynoides americanus (Riva, 1969, 1974), which they correlated with the Climacograptus
bicornis zone to Climacograptus spiniferus subzone of Orthograptus amplexicaulis (Berry,
1960, 1971, 1976; Finney, 1986) indicating a lower Shermanian (Caradocian) age.
Parris and others (2001) described a graptolite and shelly fauna about 30 feet above the
Jacksonburg Limestone from a site adjacent to the map area and indicated that the basal
Bushkill correlates with the Corynoides americannus Subzone, slightly younger than the
Climacograptus bicornis zone (Berry, 1960, 1971, 1976; Finney, 1986). Unit approximately
1,500 feet thick.
Beekmantown Group – Ontelaunee and Epler Formations and Rickenbach
Dolomite (Lower Ordovician and Upper Cambrian)
Oo
5
Lake Hopatcong Intrusive Suite (Drake and Volkert, 1991)
Kittatinny Supergroup (Lower Ordovician and Cambrian)
Fault - Dotted where concealed. Queried where uncertain.
Ymh
Yk
49
26
Ontelaunee Formation
Epler Formation
Rickenbach Formation
Rickenbach Dolomite
Stonehenge Formation
Beekmantown Group
Beekmantown Group, upper part
Beekmantown Group, lower part
Epler Formation
Rickenbach Formation
Allentown Dolomite
Allentown Formation
Allentown Dolomite
Leithsville Formation
Contact - Dotted where concealed. Queried where uncertain.
78
73
74

70
65
65
76
_l
EXPLANATION OF MAP SYMBOLS
Ybh
Ypg
61
34
52

Ow
CAMBRIAN
Inclined thrust fault - teeth on upper plate
73
78
Ybs
18
70
79
Ybh
56
_a
CAMBRIAN
ORDOVICIAN
O_e
Yps
Yps
70
36
86
Ybs
56
86
73
Ybh
50
53
61
80
61
SOl
35
Ybh
Yk
23
67
28
41o07’30”
74o37’30”
81
39
68
85
56
_l
_r
O_e
Figure 1. Nomenclature of Paleozoic carbonate rock of previous workers, shown in the columns on
left. This map follows the scheme proposed by Markewicz and Dalton (1977), along with the revised
ages of the carbonate rocks due to changes in the International Stratigraphic Time Scale (U.S. Geological Survey, 2010) shown in the column on right. Dashed line indicates the Cambrian-Ordovician
boundary which has been raised stratigraphically based on the acceptance of a Global Stratotype
Section and Point for the base of the Ordovician System.
38
83
74
43
Yp
39
Ybs
61
43
56
33
_a
79
81
85
Fe
86
69
13
37
42
71
O_a
ORDOVICIAN
34
56
83
57
37
Ylb
_l
76
Ybh
42
39
11 42
38
69
56
54
66
_h
19
68
59
49
59
69
85
MB
U
Ya
Ybh
57
78
Ybs
64
Ybs
56
Ypg
Ybs
Ybs
29
33
29
74
69
66
75
U
D
19
Ym
70
81
SOl
86
Ypg
62
71 57








Oo
73
29
49
79 61
SOl
60 81
HA
25
34
_h
SOl
75
71
Yff
33
RG
K
55
37
Yff
SOl
86
24
_r
46
Ya
66 73
82
80
Ybs
Ybs
Ypg
76
67
59
31
84
56
49
75
Ym
71
36
26
67
74
Oo
Oe
Or
Or*
Os
Ob
Obu
Obl
O_e
_r
O_a
_a**
_a
_l
44
78
SOl
_l
_l
PO
CH
UC
46 48
48
35 63
48
30
80
74
74
_l
This Map
82
46
34
83
81
67
82
35
SOl
68
77
84
Yff
SOl
72
78
76
Yk
Ype
Ybh
Yba
77
43
40
77
90 65
51 30
Zch
_h
SOl
HB-1
HB-5
HB-4
O_e
25
20
71
70
42
SOl
78
70
45
38
47
64
47
34
46
38
34
_l
_l
54
Ymp
21
66
80
81
44
37
SOl
_a
HB-2
63
36
30
39
39
76
81
19
Ybs
79
44
Ymh
55
84
75
79
Ybh
24
43
84
77
Yk
26
50
51
86
71
69
68
O_a
_l
84
44
86
61
78
64
Yk
85
64
Ym
66
73
46
56
66
86 81
72 62
79
74
71
Ymh
81
66
64
74
82
Ylb
12
Ymh
H
T
UL
FA
Ymh
59 48 36
85
Yp
69
_a**
24
77
66
31
32
42
73
78
67
59
68
SOl
_h
82
44
Ylb
46
33
30
21
27
28
Ymh
Yk
83
86
53
SOl
19
19
_h
86
56
Ym
D
68
59
85
_l
Ymh
39
18
10
43 62
60

_h
15
60
13
59
20
51
SOl
U
84
21
34
_l
43
51
Yff
55
_l
_l
Or
_l
_h
Yff
Ym
_h
79
71
35
Zch
Yff/Yfw
Oj

Obl
_l
_l
76
71
46
Ylb
72
SOl
SOl
49
Ylb
H
24
59
SOl
77
Ype
Yp/Yap

Oe
Os
_a
9
61
Yff
A’
_a
15
76
SOl
Fe
Ymp
Ysk
Obu
Or
Oo
Oe
Or*
64
76
60
81
Ya
_a
87
70
69
_h
81 76
18
8
74
L
SOl
_h
16
65
83
68
70
Yff
86
Ymh
Other Rocks
31
SOl
Ym
Drake and
Markewicz Lyttle (1985)
and Dalton Volkert and
Drake
Drake and
(1965 and1969) (1977) others (1989) others (1996)
44
85
66
86
12
Yp
66
79
Yff
Ylb
66
69
61
64
_l
50
40
55
Oo
47
47 30 34
45
83
81
_l
69
56
HB-3
28
9
90
40
38
Ylo
_h
74
57
Yk
_a
Yp
69Ym
71
85
82
71
Yh
12’30”
3
19
53
38
69
Yp
Ypa
60
51
74
79
SOl
SOl
61
_a
74
76
33 47
87
74
65
70
75
77
52
_a
57
SOl
42
45
70
SOl
81
45
60
69
41
54
68
56
Ym
51
57
61
Ym
60
14
65
22
?
40
Yp
73
_l
10
86
37
45
64
73
39
55
36
53
19
47
26
28 32
35
27
33
38
25
26
58
61
47
67 78
73
SOl
87
43
29
42
60
66
28
48
60
47
88
24
_l
45
50 35
50
75
31
41
77
48
41
78
35
33
30
37
84
32
27
57
?
OO
KE
D
63
62
65
CR
87
60
46
35
Oo
Oj
Ow
Omb
38 40 30
25
76
37
43
_l
SOl
44
68
74
_h
63
66
_h
54
62
68
Ya
SOl
56
40
37
51
35
SOl _r
Ylo
71
51
SOl
Ypa
65
60
70
43
15
42
71
49
52
56
56
Ylb
45
Ym
SOl Ym
60
31
71
57
57
56
69
D
SOl
46
31 Ow
63
7732
80
_l
46
59
77
37
5
67
58
76
42
82
13
66
76
Ylh
10
51
43
Ylb
Back Arc Supracrustal Rocks
_r
9
86
54
Ym
Ylh
Yp
72
73
67
74
86
14
71
Yp
_h
39
Oo
41
67
_l
O_e
88
28
41
55
31
42
53
33
40
38
_a
81
Ow
73
56
31
O_e
57
62
71
55
62
75
Omb
Oj
62
32
36
55
34
ST
43 35
_r
51
46
45
80
Yfw
Fe
78
62
70
79
71
Ym
44
SOl
33
54
68
O_e
10
50
82
77
75
65
59
80
78
65
81
74 64
64
32
68
75
67
Ylb
36
72 13
48
40
10’
_a
Oo
43
48
50
_r
45
53
62
25
71
Ymp
83
Ysk
47
63
62
62
42
63
_r
Ya
Ylb
35
O_e
O_e
46
18
O_e _r
60
68
65
54
Oj
40
9
34
53
70
42
75
Ya
Ylo
11
Ym
81
84
82
34
36
U
27
43
Ym
MESOPROTEROZOIC
86
83
86
Losee Metamorphic Suite
Oj
49
33
40
_l
_a
_r
_a
47
Oo
37
41 31
40
80
1
77
68
17
78
65
_r
48
40
25
O_e
85
76
90 20
73
61
74
Oo
O_e
_h
34
48
83
75
Ylo
35
67
83
79
82

Intrusive Contacts
74
Ya
Ylh
Yps
Ypa
Ypg
Magmatic Arc Rocks
31
81 34
87
25
28
73
84
71 64
26
22
_a
52
71
Ylo
77
86
25
O_e
81
80
Ylb
30
Oj
?
(BRANCHVILLE)
_a
24
45
37
45
4
20
53
69 64
52
Yp
51
SOl
53
75
25
72
13
_a
35
FA
UL
T
59
Omr
47
67
82
44
62
32
36
Lake Hopatcong Intrusive Suite
Ybs
Yu
Omb
Yff
49
_l
_l
77
_a
5
55
47
4
27
16
67
Omb
21
53
73
71
27
25
76
2
70
47
24
83
_r
14
12
_r
82
43
B
11
58
68
6
4
86
53 32
22
3
70
51
1
89
3
51
32
32
_a
20
70
40
52
63 27 29
63 53
36
41
22
43
25
19
30
37
52
48
Ylb Ym
Ylh
39
34
50 45
_a
32
36
29
24
36
25
Ylo
35
35
FA
U
LT
45
29
28
66
48
22
83
42
O_e
36
34
31
47
25
O_e
_r
43
33
29
53
15
11
74
Yba
Ybh
73
51
75
25
51
Ym
71 31
39
51
39
75
_a
22
Byram Intrusive Suite
25
_h
_a
_a
46
32
64
59
33
60
34
10
10
35
35
4
85
_a 35
O_e
?
?
77
?
54
Intrusive Contacts
28
72

Ygm
Ya
Vernon Supersuite
Ymp
15
31
71
30
Unconformity
Ym
Ygm
49
72
CR
3
54
23
_r
18
30
38
30
45
21
49
Ya
54
82
35
_a
O_e
10
79
63
O_e
40
18
Ym
36
64
31
7
_a
_l

52
Ym
_a
45
15
43
Omb
1
14
23
81
Ylo
35
60
31
62
15
31
39
_a
54
51
22
1
66
Oo
39
38
_r
38
40
45
17
69
45
25
44
20
52
1
18 55
38
15
44
EA
ST
46
11
30
60
53 82
65
45
35
37
20
74
73
O_e
OO
K
51
78
40
85
86
53
49
55
35
NEOPROTEROZOIC
Ybs
6
Hamburg Mountains
47
57
Oo
11
_h
_a
_a

Zch
10
Gravel Pit
23
13
54
Omb

26
54
26
NEW JERSEY HIGHLANDS
9
Route 23
62
15
30
70
67
30 32
35
37 30
43
83
25 29
46
44
31
79
41
59
45
Ya
Ym
46
44
31 48
44

Unconformity
12
15
N.Y.S.&W Railroad
48 49
51
72 15
58
43
9
Ylb
Yba
East Fault
2
80
SOl
36
49
Yap
41
35
_r
48
84
6
15
Hornblende granite (Mesoproterozoic) – Pinkish-gray to buff-weathering, pinkish-white
or light-pinkish-gray, medium- to coarse-grained, foliated granite and sparse granite
gneiss composed principally of microcline microperthite, quartz, oligoclase, hornblende,
and magnetite. Some variants are quartz syenite or quartz monzonite. Locally contains
clinopyroxene where in contact with rocks of the Lake Hopatcong Intrusive Suite. Unit
includes small bodies of pegmatite too small to be shown on the map.
Hamburg Fault
37
5
1
32
Oj
65
70
57
76
65
85
Omr
24
O_e
39
83
54
_h
Pochuck Fault
71
42
24
39
80
55
9
34 20

Ylb
64
34
_l
Quarry Fault
17
69
47
56
Oo
79
80
61
29
6
13
42
78
24
CAMBRIAN
Wallkill River
17
74
61
87 70
42
12
5
17
47
80
82
29 80

Crooked Swamp Fault
9
13
71 80
37
84
18
2
26
18
47
46
52
79
Ym
21
35
Ybh
Ramseyburg Member of the Martinsburg Formation (Upper Ordovician) - (Drake and
Epstein, 1967) – Interbedded medium- to dark-gray to brownish-gray, fine- to mediumgrained, thin- to thick-bedded, locally quartz-rich, greywacke, sandstone and siltstone and
medium- to dark-gray, laminated to thin-bedded shale and slate. Unit forms fining-upward
sequences characterized by basal cross-bedded sandstone to siltstone grading upward
through planar laminated siltstone into shale or slate. Locally, some of the fining-upward
cycles may have a lower, medium- to thick-bedded, graded sandstone unit overlain by
planar laminated sandstone to siltstone beneath the cross-bedded layer. Complete cycles
may be an inch to several feet thick. Basal scour, sole marks, and soft-sediment distortion
of beds are common in quartzose and graywacke sandstones. Lower contact with the
Bushkill Member is placed at base of lowest thick- to very-thick-bedded graywacke, but
contact locally grades through sequence of dominantly thin-bedded slate and minor thin- to
medium-bedded discontinuous and lenticular graywacke beds in the Bushkill. Parris and
Cruikshank (1992) correlated unit with Orthograptus ruedemanni zone to lowest part of
Climacograptus spiniferus zone of Riva (1969, 1974) indicating an upper Shermanian age
(Caradocian). Unit is approximately 3,500 feet thick.
Beaver Run
3
53
81
_r
_a
Vernon Valley
70
Oj
79
71
Yp

6
39
63
Kittatinny
Supergroup
56
Ya


O_e
Ob
15
61
46 Ymp
Ym
Ym
22
Oo
20
31
30
(WAWAYANDA)
7
86
Omb
3
60
26
Ym
Ymp
36
86
52
72
20
51
67
13
8
33
73
_a
63
36
30

23
35
U
D
5
11
83
60
86
Yap
Ygm
LT
64
67
31
56
ORDOVICIAN
Unconformity
FA
U
15
11
17
U
D
73
Ya

Ow
11
26
Ym
Ylo
Ylo
_l
34
36
18
74
36
U
D
20
31
Omr
N
N
Byram Intrusive Suite (Drake and others, 1991b)
Kittatinny Valley Sequence
Oj
26
41
62
_h
24
Yp
FAU
LT
3
34
59
44
18 58
O_e
_a

Omr
Mount Eve Granite (Mesoproterozoic) – Pinkish-gray- to buff-weathering, pinkish-white
or light-pinkish-gray, medium- to coarse-grained, massive, unfoliated granite composed
principally of microcline microperthite, quartz, oligoclase, hornblende, and biotite. Locally
contains xenoliths of foliated country rock. Unit includes bodies of pegmatite too small to be
shown on the map.
Vernon Supersuite (Volkert and Drake, 1998)
VALLEY AND RIDGE
Omb
59
41 50
Lamprophyre dikes (Lower Silurian and Upper Ordovician) – Light-medium- to mediumdark-gray, fine-grained to aphanitic dikes and small intrusive bodies of mainly alkalic
composition. Contacts are typically chilled and sharp against enclosing country rock (fig.
10). Dikes intrude rocks that are Mesoproterozoic through Ordovician in age.
KITTATINNY VALLEY SEQUENCE
36
38
SOl
SILURIAN and
ORDOVICIAN
Intrusive Contacts
Ym
25
22
FAULT
24
9
35
68
64
16 84
Ya
Ym
60

Ylb
Ym

SOl
Yfw
U
D
8
14
42
65
63
74

Ym
Yk
Ygm
55
74
Yap
36
EA
ST
22
10
59
Ym
Ygm
Beemerville Intrusive Suite (Drake and Monteverde, 1992)
Beemerville Intrusive Suite
37
2936
29
DESCRIPTION OF MAP UNITS
VALLEY AND RIDGE
UC K
38
8
7
37
59
63
Ow
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Figure 14. Pink-granite pegmatite cutting folded foliation of biotite-quartz-oligoclase gneiss at the
Hamburg Quarry. (Richard Volkert)
NEW JERSEY GEOLOGICAL AND WATER SURVEY
GEOLOGIC MAP SERIES GMS 14-3
BEDROCK GEOLOGIC MAP OF THE HAMBURG QUADRANGLE
SUSSEX COUNTY, NEW JERSEY
by
Richard F. Dalton1, Richard A. Volkert1, Donald H. Monteverde1,
Gregory C. Herman1, and Robert J. Canace2
1
New Jersey Geological and Water Survey, Trenton, New Jersey 08625
2
Ridge & Valley Conservancy, Blairstown, New Jersey 07825
Booklet accompanies the map
Bedrock Geologic Map of the Hamburg Quadrangle
Sussex County, New Jersey
scale 1:24,000
(GMS 14-3)
Prepared with support from the
U.S. Geological Survey
National Cooperative Geologic Mapping Program, Award Number 05HQAG0026
STATE OF NEW JERSEY
Chris Christie, Governor
Kim Guadagno, Lieutenant Governor
Department of Environmental Protection
Bob Martin, Commissioner
Water Resources Management
Daniel Kennedy, Assistant Commissioner
Geological and Water Survey
Karl Muessig, State Geologist
NEW JERSEY DEPARTMENT OF ENVIRONMENTAL PROTECTION
The mission of the New Jersey Department of Environmental Protection is to assist the residents of New Jersey in
preserving, sustaining, protecting and enhancing the environment to ensure the integration of high environmental
quality, public health and economic vitality.
NEW JERSEY GEOLOGICAL AND WATER SURVEY
The mission of the New Jersey Geological and Water Survey is to map, research, interpret and provide scientific
information regarding the state’s geology and ground-water resources. This information supports the regulatory and
planning functions of DEP and other governmental agencies and provides the business community and public with
information necessary to address environmental concerns and make economic decisions.
For more information, contact:
New Jersey Department of Environmental Protection
New Jersey Geological and Water Survey
P.O. Box 420, Mail Code 29-01
Trenton, NJ 08625-0420
(609) 292-1185
http://www.njgeology.org/
Cover photo:
This photograph shows a west-east trending wall (left to right) of the Franklin Marble exposed in a quarry at
McAfee. Here the Franklin displays an atypical high density of near-vertical northeast-trending jointing paralleling
the trend of the nearby Hamburg Fault which is about five hundred feet east of the quarry. Elsewhere Franklin joints
are much wider spaced. A large block of gneiss within the marble is evident on the west side of the bedrock
exposure. Note people outlined by a circle for scale. (Richard Dalton)
INTRODUCTION
U.S. Geological Survey (Charles Milton, written
communication, 1972), yields a K-Ar cooling age of
422 ± 14 Ma. More recently, titanite from nepheline
syenite at Beemerville yields a Thermal Ionization
Mass Spectrometry (TIMS) U-Pb crystallization age
of 447 ± 2 Ma (Ratcliffe and others, 2012).
The Hamburg quadrangle is located in
northeastern Sussex County, where it spans the border
between the New Jersey Highlands and the Kittatinny
Valley segment of the Appalachian Valley and Ridge
physiographic provinces. Mesoproterozoic rocks of
the Highlands underlie the eastern part of the
quadrangle, and lower Paleozoic rocks of the Valley
and Ridge underlie the western part. All geologic age
designations conform to U.S. Geological Survey
Geologic Names Committee (2010) Fact Sheet 20103059.
Cambrian and Ordovician rocks of the
Kittatinny Valley sequence crop out in lowland areas
mainly west of Pochuck Mountain and are preserved
along faults north and west of Hamburg Mountain.
These rocks previously were considered part of the
Lehigh Valley sequence of MacLachlan (1979), but
were later reassigned to the Kittatinny Valley
sequence by Drake and others (1996). They consist of
the Hardyston Quartzite; the Kittatinny Supergroup
(fig. 1 on map), which includes the Leithsville
Formation, Allentown Dolomite, and Beekmantown
Group; the Sequence at Wantage; the Jacksonburg
Limestone; and the Martinsburg Formation. These
sedimentary rocks record the formation of the eastern
Laurentian passive margin and the approaching
Taconic orogenic events. Hardyston sandstone marks
the beginning of a major marine transgression along
the entire eastern Laurentian margin. Conditions of
the margin evolved to allow deposition of shallow
water carbonate rocks of the Kittatinny Supergroup.
Dominated by dolomite these units were originally
deposited as limestones. Few limestone beds remain
and can only be found in the Beekmantown Group
sediments. The secondary dolomitization locally still
preserves some of the original sedimentology, such as
oolites and cross beds. The approaching Taconic
orogenic event is first noted by uplift and erosion of
the Kittatinny Supergroup as the peripheral bulge of
the approaching foreland basin arrives. The margin
subsequently resubmerged as evidenced by deposition
of the Sequence at Wantage and Jacksonburg
Limestone. The foreland basin continued to deepen
allowing the flysch deposition of the Martinsburg
Formation.
This map provides detailed geologic information
on the distribution and lithologic character of the
various bedrock types and the structures that affect
them. It provides a geologic framework for geologic
and environmental investigations, as well as for the
hydrogeologic characterization of the Cambrian
through Ordovician carbonate rocks that constitute
the most productive bedrock aquifer in the map area.
Additionally, new interpretations of bedrock geologic
relationships have rendered some previous work
obsolete. Therefore, the interpretations presented here
supersede those shown on previous bedrock geologic
maps of the quadrangle.
Previous work on the bedrock geology of the
quadrangle includes that of Bayley and others (1914),
Hague and others (1956), Buddington and Baker
(1961), and Drake and others (1996). In addition to
the previous bedrock mapping, Stanford and others
(1998) mapped the surficial deposits of the
quadrangle.
STRATIGRAPHY
Paleozoic rocks
The youngest Paleozoic rocks in the quadrangle
include lamprophyre dikes and related rocks of Lower
Silurian to Upper Ordovician age of the Beemerville
Intrusive Suite (Drake and Monteverde, 1992) that
intrude rocks ranging from Upper Ordovician through
Mesoproterozoic age mainly in the southern half of
the map, from McAfee south to Hardistonville. Dikes
strike predominantly northwest. Biotite from
nepheline syenite at Beemerville yields an Rb-Sr and
K-Ar cooling age of 435 ± 20 Ma (Zartman and
others, 1967). Eby (2004) obtained a titanite fissiontrack age from nepheline syenite at Beemerville of
420 ± 6 Ma. Biotite in a minette dike from the
adjacent Branchville quadrangle, collected by the
New Jersey Geological Survey and analyzed by the
The Taconic collisional event caused cessation of
sedimentation as the region was uplifted and deformed. Folding and minor faulting of the sedimentary rocks in the mapped region mark the Taconian
event. Subsequent deformation of the younger Alleghanian orogenic event left a much stronger deformational impact on the geology of the mapped area as
evidenced by more intense folding and thrust faulting.
Neoproterozoic rocks
Unmetamorphosed coarse- to fine-grained clastic
rocks, and less abundant felsic volcanic rocks, of the
1
Chestnut Hill Formation of Neoproterozoic age
(Drake, 1984; Gates and Volkert, 2004) are sparsely
preserved throughout the New Jersey Highlands. In
the map area they crop out at two places near
McAfee, where they host small deposits of hematite,
and at a single location on Pochuck Mountain, east of
Wallkill Lake. At McAfee the Chestnut Hill Formation unconformably overlies Mesoproterozoic
Franklin Marble and is unconformably overlain by
the Lower Cambrian Hardyston Quartzite. On Pochuck Mountain the Chestnut Hill unconformably
overlies Mesoproterozoic gneiss. Rocks of the Chestnut Hill Formation were formed from alluvial, fluvial,
and lacustrine sediments, and volcanic rocks deposited in a series of small sub-basins along the eastern
Laurentia rifted margin, in the present-day Highlands
(Volkert and others, 2010a).
others, 2010b) that overlap ages of rocks of the Losee
Suite.
Granite and related rocks of the Byram and Lake
Hopatcong Intrusive Suites intrude rocks of the Losee
Metamorphic Suite and supracrustal rocks. Plutonic
variants of both granite suites are abundantly exposed
on Hamburg Mountain, near Vernon, which is designated as the type section of the Vernon Supersuite
(Volkert and Drake, 1998). Byram and Lake
Hopatcong rocks form a complete differentiation series that includes monzonite, quartz monzonite, granite, and alaskite, all of which have a distinctive Atype geochemical composition (Volkert and others,
2000). Granites of both suites yield similar U-Pb
(SHRIMP) zircon ages of 1188 ± 6 to 1182 ± 11 Ma
(Volkert and others, 2010b).
Mesoproterozoic rocks
The youngest Mesoproterozoic rocks in the area
are post-orogenic potassic granites and granite
pegmatites that are undeformed, contain xenoliths of
foliated gneiss, and intrude other Mesoproterozoic
rocks in the map area as tabular to irregular bodies
that are discordant to metamorphic foliation. The
most abundant of these is the Mount Eve Granite that
forms two prominent intrusive bodies known as
Mount Adam and Mount Eve directly north of the
map area, as well as more than 30 smaller bodies in
adjacent areas. In the Hamburg quadrangle, Mount
Eve Granite is confined to the northern part of
Pochuck Mountain, whereas pegmatites are more
widespread. Mount Eve Granite has an A-type
geochemical composition that is similar to that of the
Byram and Lake Hopatcong rocks (Gorring and
others, 2004) and compositions that range from
granite to syenogranite (Drake and others, 1991a).
Mesoproterozoic rocks in the map area consist of
an assemblage of granites, gneisses, and marble. Most
Mesoproterozoic rocks were metamorphosed to granulite facies during the Ottawan orogeny at 1045 to
1024 Ma (Volkert and others, 2010b). Temperature
estimates for this high grade metamorphism are constrained from regional calcite-graphite geothermometry to 769oC (Peck and others, 2006).
The oldest Mesoproterozoic rocks in the area are
calc-alkalic rocks of the Losee Metamorphic Suite
that formed in a continental-margin magmatic arc,
and a thick assemblage of supracrustal metavolcanic
and metasedimentary rocks that formed in a back arc
basin inboard of the Losee arc (Volkert, 2004). The
Losee Metamorphic Suite includes plutonic rocks that
are tonalite gneiss and diorite gneiss, and a layered
sequence of metamorphosed volcanic rocks formed
from dacite, andesite, rhyolite, and basalt protoliths
(Volkert and Drake, 1999). Rocks of the Losee
Metamorphic Suite yield sensitive high-resolution ion
microprobe (SHRIMP) U-Pb zircon ages of 1282 ± 7
to 1248 ± 12 Ma (Volkert and others, 2010b).
Mount Eve Granite from Mount Adam yields a
zircon U-Pb age of 1020 ± 4 Ma (Drake and others,
1991a), and from Mt. Eve a zircon U-Pb age of 1019
± 4 Ma (Volkert and others, 2010b). Small bodies of
granite north of the map area yield a zircon U-Pb age
of 1004 ± 3 Ma, and pegmatites from elsewhere in the
Highlands yield zircon U-Pb ages of 990 to 986 ± 4
Ma (Volkert and others, 2005).
Rocks of the Losee Metamorphic Suite are
spatially and temporally associated with supracrustal
rocks that include a bimodal suite of felsic and mafic
metavolcanic rocks that are rhyolite gneiss and
amphibolite, respectively, and metasedimentary rocks
that include quartzofeldspathic gneisses, calc-silicate
rocks, and marble. Metavolcanic rocks are most
abundant in the area of Pochuck Mountain.
Supracrustal rhyolite gneiss yields U-Pb (SHRIMP)
zircon ages of 1299 ± 8 to 1251 ± 6 Ma (Volkert and
STRUCTURE
Paleozoic bedding and cleavage
Bedding in the Paleozoic formations is fairly
uniform and strikes northeast at an average of
N.36oE. (fig. 2 on map). Most beds are upright and
dip northwest and less commonly southeast (fig. 3 on
2
map), and locally are overturned steeply southeast.
Beds range in dip from 3o to 90o and average 44o.
are given in Bayley (1910). Limonite and brown
hematite deposits were mined at the Pochuck and
Edsall mines in the 19th century (Bayley, 1910), most
likely from Mesoproterozoic rocks as well, although
descriptions of the host rocks are ambiguous and no
dump material is available for inspection. Earthy
hematite was mined during the 19th century from
Neoproterozoic rocks of the Chestnut Hill Formation
at the Cedar Hill and Simpson mines. Detailed
descriptions of these mines are given in Bayley
(1910) and Volkert and others (2010a).
Cleavage develops in finer grained sedimentary
rocks or where localized faulting is present. Average
strike of cleavage is N.39oE. (fig. 4 on map), and dips
range from 10o to 90o and average 56o. Generally
cleavage is southeast dipping (fig. 5 on map) but
some vertical to northwest dips occur. Locally a
crenulation cleavage or second spaced cleavage has
been observed in some units in the map area.
Mesoproterozoic marble was quarried mainly
during the 19th and early 20th centuries at numerous
locations from McAfee south to Hardistonville.
Rocks of the Losee Metamorphic Suite are presently
being quarried north of Hamburg. Paleozoic dolomite
is currently commercially quarried from a single
location near the edge of the map at Beaver Run.
Numerous small farm quarries in the dolomite were
encountered during mapping of the quadrangle.
Proterozoic foliation
Crystallization foliation in the Mesoproterozoic
rocks is formed by the parallel alignment of
constituent mineral grains and it defines the trend of
the bedrock units. Foliations strike mainly northeast
at an average of N.25oE. (fig. 6 on map). They dip
southeast, and locally northwest, at 11o to 90o and
average 59o.
Joints
Deposits of sand and gravel of glaciogenic origin
were mined from numerous locations throughout the
map area.
Joints are a common feature in Paleozoic and
Mesoproterozoic rocks. They are characteristically
planar, moderately well formed, and moderately to
steeply dipping. Surfaces are typically unmineralized,
except near faults, and are smooth and, less
commonly, slightly irregular. Joints are variably
spaced from a foot to tens of feet. Those developed in
massive rocks, such as Mesoproterozoic granite or
Paleozoic carbonate and quartzite, tend to be more
widely spaced, irregularly formed and discontinuous
than joints in Mesoproterozoic layered gneisses and
fine-grained Paleozoic rocks. Joints formed near
faults are spaced 2 feet or less.
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CONSTRUCTION OF MAP
Bayley, W.S., 1910, Iron mines and mining in New
Jersey: New Jersey Geological Survey, Final
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1914, Description of the Raritan quadrangle,
New Jersey: U.S. Geological Survey Geologic
Atlas Folio 191, 32 p.
In the Paleozoic rocks, northwest-trending cross
joints are the most common. They strike an average
of N.56oW. (fig. 7 on map), and dip mainly northeast
at an average of 69o (fig. 8 on map). The dominant
joint trend in Mesoproterozoic rocks strikes
northwest at an average of N.64oW. (fig. 9 on map),
and dips southwest, and less commonly, northeast. A
subordinate set strikes about N.15oE. and dips
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_______, 1971, Late Ordovician graptolites from
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ECONOMIC RESOURCES
Mesoproterozoic rocks in the quadrangle host
economic deposits of magnetite that were mined
mainly during the early 19th century at the Copperas
or Green and Bird mines. Descriptions of these mines
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3
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_______, 1991b, The Byram Intrusive Suite of the
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Eve Granite: implications for late- to postOttawan tectonics in the New Jersey/ Hudson
Highlands, in Tollo, R.P., Corriveau, L.,
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map of the Blairstown quadrangle, Warren
4
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J.P.,
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faunas of New Jersey: Geological Society of
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Martinsburg Formation in the Delaware Water
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contact and significance of Hyolithellus micans
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Rader, E.L., 2006, Calcite-graphite thermometry
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and applied geology of the Lower Paleozoic
carbonates in northwestern New Jersey: in 42nd
Annual Field Conference of Pennsylvania
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Amelin, Y., Merguerian, C. and Panish, P. T.,
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Paleozoic environments of deposition and the
discontinuous sedimentary deposits atop the
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