60
˛s
˛s
0.5
0
2000
3000
llll
l
lll
llll
ll
llll
llll
llll
llll
ll
5
2
27
late
SAN ANTONITO (NM 44) 4.7 MI.
MADRID 29 MI.
13
81
28
5
5000
6000
7
6
middle
Pleistocene
Neogene (Tertiary & Quaternary)
early
Miocene
Triassic
6
0
Xp
Xdt
20
Xmv
38
76
˛mu
˛ml
˛mu
˛ml
E XPLANATION OF M AP S YMBOLS
13
38
˛s
B
75
B'
Qay
12
22
47
˛s
48
65
44
50
45 Xmv
64
45
59
Xla
Xmv
59
Qay
5
af
˛ml
af
˛ml
Qay
40
QHa
45
44
43 42
71
Xcm
Ys
Qay
˛ml ˛s
3
71
72
˛ml
˛mu
Qpy
˛s
Xq
3
Qay
5
˛ml
25'
40
54
52
Normal fault —Tic showing dip, arrow showing trend and plunge of slickensides where measurable; solid where
exposed, dashed where approximately located, dotted where concealed, queried where inferred; ball and
bar on downthrown side, upthrown (U) and downthrown (D) sides indicated where concealed and/or interpreted
50
Xla
Xla
60
15
Xmv
˛mu
30
38
74000m N.
˛ml
3
73
3
74000m E.
35° 00'
106° 22' 30"
Geology of Tijeras quadrangle,
Bernalillo County, New Mexico
NEW MEXICO
QUADRANGLE LOCATION
NATIONAL GEODETIC VERTICAL DATUM OF 1929
68
86
Moenkopi Formation — A recessive-weathering, dark red-colored micaceous shale, silty shale and thinbedded feldspathic sandstone. Approximately 200 ft (60 m) thick.
Yeso Formation, upper limestone unit — Intervals of massive or algal/cryptalgal-laminated limestone
within the upper part of the Yeso Formation. The limestones are typically micritic, fenestral fabrics are
commonly preserved, and they contain abundant quartz sand. Differentiated where possible east of the
Village of Cañoncito. Generally less than 16 feet (5 m) thick.
Slickensides on fault or minor fault
Minor fold axis, trend and plunge, with map view sketch of fold
54
Upper and Middle Pennsylvanian
San Andres and Glorieta Formations, undivided — The upper two lithostratigraphic units of the Permian
are complexly interleaved. The lithotypes, which may not strictly correlate with formations of the same names,
are gray limestone (San Andres, Ps) and white quartz arenite (Glorieta, Pg). These were differentiated where
possible.
San Andres Formation — Light gray and less commonly tan colored, medium- to thick-bedded limestone.
The limestones are mostly micrites or skeletal wackstones, commonly with some component of quartz sand.
The San Andres Formation is interbedded with the Glorieta Formation (Pg) with a total upper Permian (Ps and
Pg) thickness of approximately 400 ft (120 m).
˛m u
Glorieta Formation — White and pink (along the contact with the underlying Yeso Formation), massive or
plane-bedded to low-angle planar cross-stratified quartz arenite. Locally, the sandstones are extensively
bioturbated by Macaronichnus, and near the contact with Yeso Formation they are feldspathic. The sandstones
are typically well sorted, but a thin, feldspathic quartz-pebble conglomerate occurs just below the base of the
lowermost San Andres Formation limestone in the Arroyo Armijo area along the boundary between Sandia
Park and Sandia Crest quadrangles. These sandstones and the limestones of the San Andres Formation are
interbedded with each sandstone bed generally less than 30 ft (10 m) thick.
P
Lower Permian
˛m l
˛s
PROTEROZOIC ROCKS
Mesoproterozoic igneous rocks
Madera Formation, lower gray limestone — A sequence of often fossiliferous and massively bedded
cliff-forming wavy laminated and cherty micritic limestone interbedded with shales. Shale is particularly
abundant near the base of this member where it grades into the Sandia Formation. Generally correlative
with the Los Moyos Limestone of Myers and McKay (1976).
Sandia Formation — Consists of a variety of lithologies including, in descending stratigraphic order: interbedded
brown claystone and gray limestone, massive gray limestone, and a lower olive-brown to gray, subarkosic,
fine- to coarse-grained sandstone. The contact with overlying Madera Formation (˛m) is chosen at the base
of the lowest thick, ledge-forming limestone. The lower contact is unconformable with the Arroyo Peñasco
Group or Proterozoic crystalline rocks. Isolated thin outcrops in Tijeras Canyon of sandstone and limestone
from the Espiritu Santo Member of the Arroyo Peñasco Group (see Szabo, 1953; Armstrong, 1967; Armstrong
and Mamet, 1974, Kelley and Northrop, 1975) generally remain undifferentiated from the Sandia Formation.
Limestone in the Sandia Formation is distinct from limestone in the overlying Madera Formation as they are
typically thinner-bedded, clast-supported, greenish, and contain abundant siliciclastic material. Approximately
170 ft (50 m) thick.
Aplite dikes — Light colored, fine- to medium-grained, and often sugary-textured aplite dikes consist of quartz,
orthoclase, accessory muscovite, and in places are garnet-bearing (Kelley and Northrop, 1975). These dikes
are generally thin planar dikes but may also be pods and stringers (up to approximately 500 ft, or 150 m, in
diameter); interpreted to be coeval with the Sandia granite (Ys).
Ya
Yp
Pegmatite dikes — Pegmatite dikes, pods, and lenses ranging from <1 in to >50 ft (<30 cm to >15 m) in
thickness and up to about 3,000 ft (915 m) in length; interpreted to be coeval with the Sandia granite (Ys).
Yps
Sandia granite porphyry — Fine- to med- grained phase of the Sandia granite (Ys) with scattered K-feldspar
phenocrysts (up to several cm). Interpreted to be coeval with the intrusion of the Sandia granite.
.
Sandia granite — Mainly megacrystic biotite monzogranite to granodiorite. K-feldspar megacrysts, up to
several cm long, are commonly aligned in a magmatic foliation; contains numerous ellipsoidal enclaves of
microdiorite, fine-grained granite, and gabbro (interpreted to be mingled mafic magmas, Ye), and xenoliths
of quartzite, mica schist, and mafic metavolcanic rock. Pegmatites (Yp), aplites (Ya), and quartz veins are
ubiquitous. Various dates are available from geochronologic sample Locality 3: U-Pb zircon plus sphene
1,455±12 Ma (Tilton and Grunenfelder, 1968, recalculated by S. Getty, unpublished); U-Pb zircon of 1,437±47
Ma (Steiger and Wasserburg, 1966, recalculated in Kirby et al., 1995); U-Pb zircon of 1,446±26 Ma (D.
Unruh, unpublished data); Locality 3 also has 40Ar/39Ar analyses from hornblende of 1,422±3 Ma (Kirby
et al., 1995); Locality 2 has an 40Ar/39Ar date of 1,423 ±2 Ma (Karlstrom et al., 1997b).
.
Ys
Madera Formation, upper arkosic limestone — A gray, greenish-gray, olive-gray, tan and buff-brown
fossiliferous limestone (comprises slightly more than half of member) interbedded with intervals of subarkosic sandstone and mudstone. The limestone is thinly to thickly bedded and massive, with sparsely
disseminated chert. Sandstones and mudstones vary from reddish-brown to maroon to greenish-gray
and gray. Sandstones and arkosic sandstones, while sometimes lenticular and laterally discontinuous,
can be often traced over distances of several kilometers (see Read et al., 1998). These arkosic sandstones
are typically coarse- to medium-grained and often contain granules and pebbles. The base of this member
is defined as the first occurrence of a thick and relatively continuous arkosic sandstone bed. Petrified
wood is seen locally throughout this member.
Yss
Ye
Xcf
Sheared Sandia granite — Plastically deformed megacrystic monzogranite to granodiorite, enriched
in biotite due to depletion of quartz-feldspar from the matrix.
Mafic enclaves — Cross section only. A high density of ellipsoidal enclaves of microdiorite. These mafic
enclaves often define magmatic foliation within the Sandia granite.
Xcm
Xcc
Xq
Xp
Xla
Xdt
Xmv
Paleoproterozoic rocks
Xlg
Xmg
Leucocratic granite and aplitic granite — Light-colored biotite-poor granite in dikes and pods within the
Manzanita granite.
Manzanita granite — Strongly foliated very coarse-grained biotite monzogranite (biotite is chloritized). UPb zircon date of 1,645 ±16 Ma (Brown et al., 1999) from the Mt. Washington 7.5-minute quadrangle
(Karlstrom et al., 1997a).
Xr
Horizontal bedding; overturned bedding
Fine-grained Cibola granite — Leucocratic two-mica granite.
45
Strike and dip of S1 foliation, arrow indicates trend and plunge of lineation defined by elongate minerals and
stretched grains
75
Strike and dip of S2 foliation
56
Magmatic foliation in granite defined by alignment of mafic enclaves
22
Medium-grained Cibola monzogranite — Equigranular, medium-grained, two-mica monzogranite;
average grain size is 1-3 mm.
Magmatic foliation in granite defined by alignment of feldspar megacrysts
23
Strike and dip of pegmatite or aplite dikes and veins
Coarse-grained Cibola monzogranite — Two-mica monzogranite, contains scattered cm-size phenocrysts.
A, S, K
Xms
Mica schist, quartz-muscovite schist, and phyllite — Commonly rust red from hematitic staining, strongly
crenulated and commonly crowded with boudinaged and folded stringers and lenses of vein quartz. Includes
Coyote schist and Coyote phyllite of Cavin (1985).
Metamorphic mineral occurrences and assemblages: K = kyanite; A = andalusite; A,S = andalusite + sillimanite;
A,S,K = andalusite+sillimanite+K-spar; A,St,Cd = andalusite+staurolite+chloritoid; A,S,Cd =
andalusite+sillimanite+chloritoid; S,K = sillimanite+K-spar
Prospect
Quartzite — Thick-bedded to massive and gray to milky-white quartz arenite with crossbedding and bedding
defined by bands of iron oxides. Pelitic partings and interbeds contain aluminum silicates. Includes Cerro Pelon
and Coyote quartzites of Cavin (1985) and Cibola quartzite of Connolly (1981). Locality 4 has an 40Ar/39Ar
date of 1,423±2 Ma (Kirby et al., 1995).
lll
l
ll
ll
5
Quarry
Geochronologic sample location (U-Pb, 14C, etc.; see table and unit descriptions)
Exploratory or groundwater monitoring well, including abbreviation
4H
Chlorite-amphibole phyllite and schist — Metasedimentary and volcaniclastic rocks that grade from mafic
metavolcanics to lithic arenites. Includes metasedimentary rocks of the Tijeras greenstone of Connolly (1981)
and part of the Coyote phyllite of Cavin (1985).
Metamorphosed lithic arenite — Quartz schist, quartz-chlorite schist, and quartzite (Xq), interlayered with
volcaniclastic schists (Xp); quartzite locally contains alumino-silicates. Includes the Tijeras quartzite of Connolly
(1981) and the Isleta metasediments of Parchman (1981).
Metamorphosed dacitic tuff — Gray to light green metavolcanic and volcaniclastic schist and phyllite with
local fragments of phyllite, chlorite phyllite, greenstone, and jasper.
Mafic metavolcanic rocks — Heterogeneous unit consisting of massive to schistose metabasalt and metaandesite with subordinate chlorite phyllite and schist of volcaniclastic origin. Coarse dioritic units may locally
intrude the volcanic rocks. Includes the Tijeras greenstone of Connolly (1981), Coyote greenstone of Cavin
(1985), and Isleta metavolcanics of Parchman (1981).
Metarhyolite and to felsic metavolcanic rock — Coarse-grained, buff to reddish-orange felsic metavolcanic
rock, commonly banded, locally contains quartz and feldspar phenocrysts. Includes Tijeras felsic metavolcanics
of Connolly, (1981).
.
Strike and dip of joint or fracture; vertical joint or fracture
80
l
Madera Formation, undivided — Two informal members, an arkosic limestone and a gray limestone, are
recognized but not differentiated. The upper and lower members are respectively generally correlative to the
Wild Cow Formation and Los Moyos Limestone (Formation) of the Madera Group of Myers and McKay (1976).
These informal member names are used because the units were lithostratigraphically defined on the Sedillo
(Read et al., 1999) and Tijeras (Karlstrom et al., 1994) 7.5-minute quadrangles rather than biostratigraphically
defined and may therefore not strictly correlate with the units defined by Myers and McKay (1976). The Madera
Group nomenclature was abandoned because of the gradational contacts between members and the difficulty
of distinguishing these contacts in the field. Total thickness is approximately 1,320 ft (402 m) near Cedro Peak
to the southeast (Myers and McKay, 1976) and 1,260 ft (385 m) on the Crest of Montezuma (Picha, 1982)
to the north (consistent with thickness estimates based on map relationships in the study area).
.
Strike and dip of bedding
85
Xc
Overturned syncline —Trace of axial plane showing direction of plunge; dashed where approximately located,
dotted where concealed, queried where inferred
Breccia or gouge zones
30
Cibola granite, undivided — Biotite-muscovite monzogranite with U-Pb dates of 1,632 ±45 Ma (geochronologic
sample Locality 5), from north of the Tijeras fault and 1,659±13 Ma (Locality 6) from south of the Tijeras fault
(D. Unruh, 1998 unpublished data).
Overturned anticline—Trace of axial plane showing direction of plunge; dashed where approximately located,
dotted where concealed, queried where inferred
Shear zone—Tic showing dip
65
Biotite granite — Biotite-rich, medium-grained, massive to foliated granite; occurs as mixed zones in the
Manzanita granite.
Thrust fault —Tic showing dip; solid where exposed, dashed where approximately located, dotted where
concealed; triangular teeth on upthrown side of thrust
Syncline— Trace of axial plane showing direction of plunge; dashed where approximately located, dotted
where concealed, queried where inferred
June 1, 1994
5 April 2000 Revision
Xbg
Reverse fault —Tic showing dip; solid where exposed, dashed where approximately located, dotted where
concealed; square teeth on upthrown side
Anticline — Trace of axial plane showing direction of plunge; dashed where approximately located, dotted
where concealed, queried where inferred
10
l ll
Pyc
Location of geologic cross section
Geologic contact —solid where exposed, dashed where approximately located; dotted where concealed
.
Geologic contact based upon interpretation of aerial photography
15
1 KILOMETER
Arroyo Peñasco Group, Espiritu Santo Formation(?) — A poorly exposed outcrop of sandstone and
limestone along a splay of the Tijeras fault. Several measured sections of thin remnants of the Arroyo Peñasco
Group were described by Szabo (1953) and Armstrong (1967) but remain undifferentiated on this map (see
the Sandia Formation description above).
Xcc
Xla
Mississippian
Ma
Xcm
Xq
55
The sandstones are cross-stratified (typically trough and wedge-planar geometries) and the finer grained rocks
are commonly ripple cross-laminated. In addition, mud-chip clasts and plant debris are common. The upper
contact with the Yeso Formation (Py) is conformable but difficult to distinguish in the field. The lower contact
with the Madera Formation (˛ m) is gradational with interbedded limestone and reddish-brown mudstone. The
top of the lowermost laterally continuous and relatively thick limestone bed is chosen as the Madera Formation
contact. Total thickness for the Abo and Yeso formations combined is approximately 1,300 ft (400 m).
Xcf
Xms
Qay
Mapping of this quadrangle was funded by a matching-funds grant from the 1994 STATEMAP
program of the National Geologic Mapping Act coordinated by the U.S. Geological Survey
and the New Mexico Bureau of Mines and Mineral Resources.
Chinle Group, Agua Zarca Formation — The only distinct sub-unit of the Chinle Group recognized
during this study (differentiated where possible). It is a tan- to light-grayish pink, resistant, thin- to mediumbedded quartz arenite and feldspathic arenite. The lower contact with the underlying Moenkopi Formation
(ˇm) is disconformable. The unit is about 350 ft (105 m) thick.
Xbg
Xlg
4
˛ml
?
Xc
Qca
Xmg
Qay
7000 FEET
Yss
44
Xmg ˛s
CONTOUR INTERVAL 40 FEET
UTM GRID AND 1972 MAGNETIC NORTH
DECLINATION AT CENTER OF SHEET
CENOZOIC
Cret aceous
5
˛ml
Qay
Qca
Xmg
231 MILS
0.5
Pliocene
EDGEWOOD 13 MI.
MADRID 29 MI.
2
4
QHa
15 MILS
1
Permian
llll
l l ll
3
6
8
1 MILE
4000
Jurassic
llll
l ll l
l
ll
l l ll
llll
ll
˛mu
6
?
5
Penn.
l
l
ll
7
Qay
Xla
0
1000
Miss.
lll
lll l
ll l
ll
l l l l l l
1000
13°
Mesoproterozoic
ll
l l ll
l llll
ll
llll
l l l l l l l l l l l l l l l l l
l l
l l
l l l l
1
PALEOZOIC
l l l ll l
l
ll
l l ll
ll
l lllll
(SEDILLO)
l
llll
ll
ll
l
ll
lll l
llll
llll
l llll
l l ll
l
llll
7
SCALE 1:24,000
GN
MESOZOIC
l
ll
ll
l l ll
l
l
l l ll
ll
lll
ll
ll
ll
llll
lll l
lll l
l ll
ll
6
13
Ya
Qay
7
3 6
PROTEROZOIC
us
thr
Qay
6
8
7
˛ml
Qca
28
32
70
(MOUNT WASHINGTON)
74
13
3
Yps
Yp
Xmg
7
15
83
lll l
NE
PA
RK
)
Xmg
Xmv
Ye
16
5
Xmv
44
Xcm
Qvm2
55
Qvm2
24
PLUTONIC
Ys
80
QHa
Qay
78
METAVOLCANIC
3
7
2
7
METASEDIMENTARY
Xmv
Xcm Xcm
48
55
˛ml
8
Ma
llll
NM B
ur
e
(S
AN
DI
A
r
Qay
45
Xmg
˛ml
7
ESCABOSA 11 MI.
MOUNTAINAIR 50 MI.
t
ul
fa
V
l
ne
zo
l l l l
l
l l l
l l
l l
l l
l l l
l l
l l l
ras
t zon
e – Four
H ills s t r a nd
faul
dia
San
)
Tij
e
INTERSTATE 25 8 MI.
(ALBUQUERQUE EAST)
l l
NG
llll
ll l
lll
ll
RI
lll l
SP
ll
BB
EL
L
˛mu
˛m u
˛s
)
SA
(H
U
ll
ll
85
llll
5
18
10
3
MN
0° 50'
46
T. 9 N.
8
7
6
63
Xcm
67
Xlg
A'
ll
68
l
3
R. 5 E.
Xcm
Xmv
Xmg
Xmg
Xcm
6
e
53
˛s
02' 30"
38
10
˛s
63
mixed zone
Xcm
Xmg
T. 10 N.
7
6
Pyc
˛m l
BO
CA
K. E. Karlstrom: mapping and compiliation of Proterozoic rocks, cross sections; S. D.
Connell and D. W. Love: Quaternary mapping and unit descriptions (Connell); C. A.
Ferguson and G. R. Osburn: Phanerozoic mapping and stratigraphy, (northeastern
area of quad), unit descriptions, correlations, and regional structural interpretation; A.
S. Read: differentiation of the Madera formation (southeastern area of quad), final map
and cross section compilation; and P. W. Bauer: intellectual contributions.
27' 30"
R. 4.5 E.
˛s
˛m 15
20
8
81
˛m
S
(E
Base from U.S. Geological Survey 1954, photorevised 1961
Polyconic projection, 1927 North American datum, 10,000-foot grid based on New
Mexico coordinate system, cental zone
1000-meter Universal Transverse Mercator grid ticks, zone 13, shown in blue
R. 4 E.
25
9
Qay
34
55 31 50 Xp
52
25
7
5
27
32
56
Xla
˛s
71
78
Xmv
l
66
Xcm
an
af
Xcm
ll l l ll
3
65
52
Xcm
Xcm
60
Xmv
65
54
l ll
3
Xp
l l l ll
430 000 FEET
Qca
Qay
53 Xms
Xq
35
Xp
l
64
Xq
Xms
M
Xcm
lll
3
Qpm2
74
16
ll
QHa
Xq Xcm
llll
Qay
Xcm
76
Qvm2
Xq af
ll
Qay
z
an
lll
35° 00'
106° 30'
S,K
Xla
Qvm1
Qay
50
50
Qay
Qpx3
Xq
48
68
i t a af
˛s
Xmg
Qvm2
ll
74
34
Qay
75
af
Qay
Xmg
l lll
38
Qvm2
ea
46
QHa
lll
45
Xmv
50
QHa
Qay
60
40
Qvm3
71
Xq
24
6
62
Pay
Xr
Qay
sh
55
17
5
Pg
Qay
49
Qvm2
44
40
Qay
Xms
Xq
18
Xq
Ys
Xcm
20
QHa
36
˛m
80
af
l
Xmv
Ys
Xcm
Xq
Xms
52
l
˛m
Xms
55
Xq
Qpy
40
31
Xq
˛s
Xms
Xq
5m
85
12
Ps
Psg
8
5
5
ˇz
24
24
30
5
QHa
64
60
35
48
ll
56
Xmv
ll
24
Xq
l
66
Qpy
75
82
16
30
˛m
Qpx3
˛m
68
ll
l
Xcm
40
6
Xq
Xmv
Xq
Qca
Xq
ll
54
Xcm
29
l ll
Xcm
Xmv
49
Qca
Xms
31
54
Xq
˛s?
af
35
9
79
Qay
5
Qvm2
43
76
48
ll
Xmv
Qpy
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20
55 76
50
80
2 46
ll
40 45
Xms
71
Qay
32
˛s
n
zo
52
65
Xcm
76
47
45
Qvm Xmv
l
75
36
Qay
58
38
Xcm Xq
Xcm
lll
Xcm
48
llll
Xcm
QHa
˛m
Qpx3
˛m
llll
Qpm3
˛m
llll
Qca
82
74
Xmv
llll
Xmv
QHa
45
56
75
˛ml
15
32
38
17
5m
8 3
59
30
42
58
70
llll
Ys
Ys
58
50
Xmv
30
Xq
75
63
ll
61
70 70
50
Xcm
66
47
Xms
Xms
22
38
27
78
6
45
˛ml
Xq
62
16
25
Qvm2
64
71
57
67
43
Xla
24
Qay
˛s
28
9
24
25
36
˛s
Xq
43
75
75
Qca
60
84
˛s
23
63
35
˛ml
27
31
32
12
33
˛s
38
42
29
Je
50
37
D
U
22
11
Jt
Je-t
ˇm
43
15
23
B'
80
17
QHa
Qay
80
75
40
45
43
4
57
40
66
Xq
64
76
77
50
35
45
25
55
51
Xcm
68
70
72
43
63
38
Xms
ll
1 460 000
FEET Qpy
Qvm3
Qay
50 51
67
75
72
59
Xms
Qay
43
58
15
15
79
30
ll l l
˛ml
20
78
8
Qay
58
66
62
55
l l ll
l Tmi
l
36
Xms
56
80
51
60
Qpx3
˛m
Xmv
55
Xq
llll
l
42
54
86
10 25
l
25
16
8
9
ll
60 45 32
67
62
ll
l
58
Xq 56
Qvm2
Xq
18
50
46
ll l l
l
Xms
l
l
22
l
55
˛s
42
72
60
D
Qpx3
Ys
Qvm
l l
l l
l l
l l
Tmi l l
73
68
l
63
17 14
5
Jm
30
38
82
Xq
Xms
38
5
˛s
78
46
38
Xla
15
32
63
37
U
Qay
42
Xmv
80
15
18
6
Qay
Xmv
14
14
13
10
?
Qvm2
Xmv
Xla
Qvm2
63
61
84
Xms
30
46
Xmv
Ys
68
39
57
l l
l l
l l
l l Tmi
l l
l
Qay
53
QHa
ll l
Qpy
Ys
Qpm3
i
Qay
˛s
49
51
52 64
?
62
86
Qvm2
44
12
11
Kms
Kvm
ˇc
12
17
Km
Kvt
Kd
16
˛ml
10
60
QHa
Xms
Qay
?
Qay
Xms
65
43
41
55
49
K
lll
l
QHa
t
51
lll
Ys
en
nc
Xms
60
71
47
Xq
22
QHa
Kvs
20
4
10
Xms
˛s
54
44
e
or
Mo
l ll l l l l
ll
76
30
ll ll
38
QHa
llll
Qpy
?
?
lllll
Ys
Ys
Ys
50
35
l l
l l
l l
l l
l l
l l
l l
l
l l
35
l
l l
l
l
l l
l
l l Tmi
l
l l l l
l
l l l ll l l
35
l
20
l
l
l
l
l
20
l
l
l
l
l
l Tmi
l
l
l
l
l
l
l
l
l
l
l l
l l
l
Xmv
˛s
Xms
71
˛ml
10
l
10
˛s
37
K
l
l l l l
l l l ll l ll l l l l l l l l l
l l
l
Qpm3
Mancos Shale, sandstone unit — A discontinuous, <5 meter-thick interval of medium-bedded, resistant,
non-argillaceous sandstone with abundant vertical burrows. In the northerly adjacent Sandia Park
quadrangle, this sandstone unit overlies a fossiliferous shale containing late Turonian guide fossils. The
sandstone may correlate with the Tocito sandstone, and it appears to pinch-out to the south were its
approximate stratigraphic position is occupied by a massive, non-calcareous sandstone body interpreted
as the northern pinch-out of the Gallup Sandstone.
Abo and Yeso Formations, undivided — The lower two lithostratigraphic units of the Permian represent a
red-colored feldspathic to quartzose siliciclastic sequence that, because of generally poor exposure, was
mapped as a single unit throughout the study area. The Yeso Formation is a reddish to pink or tan-colored,
medium- to thin-bedded, feldspathic sandstone, shale and silty shale with interbedded massive or laminated
micritic gray or tan limestone (Pyc) near the top. The sandstones are typically cross-stratified and/or crosslaminated and virtually identical to those within the underlying Abo formation except that, rarely, salt hopper
casts and molds are present. The Abo Formation is a red and locally tan-colored (particularly near the base),
medium- and thin-bedded arkose and feldspathic sandstone interbedded with red, micaceous siltstone and
shale, commonly with green reduction spots. The lowermost arkoses are typically lighter-colored and coarsergrained than the younger feldspathic sandstones, and at least one of them is strongly bioturbated (Macaronichnus).
Xr
l ll l l
20
Qpy
Xcm
50
llll
74
70
ll
68
63
9
17
Xms
68
17
11
˛s
˛s
38
39
˛ml
12
20
QHa
80
20
36
6
5
Xms
Xms
˛s
t
lll
56
73
ll l l
Ys
Xmv
54
74
Xcm
49
59
65
64
69
llll
81
Xmv
Xcm
73
Xla
72
Xcm
t
ul
fa
70
60
27
16
l l ll
20
˛s
20
65
81
Xcm
Ys
60
llll llll
Xcc
81
Yss
Ys
Xmv
2
81
11
˛mu
80
15
˛ml
14
13
Qay
8
8
˛ml
Xq
81
ll
5
24
20
Xms
10
88
10
11
5
5
8
38
6
10
7
37
77
50
ll
5
6
5
55
74
70
l ll
l
ll
10
17
10
75
15
3
˛mu
21
12
3
15
88
4
4
QHa
21
Kv
17
9 6
5
4
16
6
35
13
ll
llll
l
8
13
˛s
80
ll
78
18
38
83
85
85
l
Ys
Qpm3
78
40
l
Pay
25
12
18
13
8
15
30
10
9
5
30
llll
6
80
85
lll
Qpx3
Ys
27
5
85
ll
˛mu
9
14
62
7
6
7
l l ll
10
10
7
40
40
50
ll
Qay
11
11
18
43
l l ll
53
Qpy
Ys
lll
Ys
17
15
50
85
QHa
llll
46
Xla
72
llll
73
Ys
15
26
53
˛mu
33
Qvmt 24
38
7
Tmi
55
11
25 11
4
4
ll
l
˛mu
9
14
6
6
40
64
A,S,K
40
77
58
56
8
40
33
88
ll
10
7
l lll
13
˛ml
34
12
11
10
66
Xp
59
20
30
70
50
6
4
21
Xmv
60
75
62
64
5
6
19
16
64
Xcc
Yss
QHa
64
38
Mesaverde Group, marine shale unit — Shale and mudstone with thin-bedded, commonly limonitic
siltstone interbeds. Characterized by a lack of coal seams and abundant woody debris, and by the
presence of molluscan fossils and shell fragments. These rocks correlate partially with the marine
sandstone and shale unit (Kvm) of the northerly adjacent Sandia Park quadrangle.
.
78
8
lll
˛mu
70
8
65
Xla
5
12
l
af
Tmi
11
10
14
˛s
65
65
Xla
Xcm
Ys
54
35
˛m
Pay
Xla
Qay
Qpx3
Ys
70
65
55
79
66
l
Qpy
Ys
Xp
11
23
48
10
85
21
70
Xcm
8
18
8
25
77
68
6
Paleogene
8
6
14
18
70
30
68
64
45
Qpy
4
ll
l
62
70
Xp
45
Xmv
62
45
Tmi
86
l ll l
l
62
31
Ys
14
l l ll
36
61
25
22
65
78
70
82
Qpx3
Ys
Xcm
Ys
TmiYss
Xcm
25
28
53
Qay
Ys
62
QHa
76
65
50
28
70
˛ml
80
Xla
12
2
17
5
lll
Mesaverde Group, terrestrial shale unit — Shale and mudstone with thin-bedded siltstone interbeds.
Characterized by the absence of marine fossils, abundant woody debris and common association with
coal seams. These rocks correlate partially with the terrestrial sandstone and shale unit (Kvt) of the
Sandia Park quadrangle to the north-east (Ferguson et al. 1996).
PALEOZOIC ROCKS
Upper Permian
Pg
17
Qpm3
70
25
17
l l
l
10
8
˛mu
25
Xcm
Xcm
Yss
6
15
15
3
4
15
˛mu
4
20
˛mu
Qay
19
18
2
4
8
Pay
15
18
25
66
70
8
Pay
af
24
2
87
Qay
7
20
20
8
82
25
7
ll
13
20
6
38
10
31
21
˛ml
10
l l ll
22
7
80
˛s
65
l
Pay
12
7
8
12
18
25
Qpx2
Xp
74
Qpx2
Xcm
38
75
Xp
1m
25
20
18
10
12
36
8
19
80
10
35
55
65
4
16
12
12
25
12
? ?
QTsp
14
22
8
5
9
55
88
ll l
24
10
15
78
70
47
23
28
65
70
QHao
Tmi
22
20
70
ll
QTpx
11
42
18
l
˛mu
89
7
l
Ys
39
T. 10 N.
Middle and Lower Triassic
Ps
17
Chinle Group, undivided (probably Petrified Forest Formation) — Mudstone with lenticular beds of
lavender-gray sandstone; mudstones are reddish-brown to orange-tan in the upper part, and purple to reddishbrown in the lower part. Green reduction spots are common, as are local limestone-pebble conglomerate
lenses, particularly near the base of the unit. Total Chinle Group thickness is about 1,300 ft (400 m).
.
ˇz
Psg
12
QHao
47
36
60
10
20
18
6
Qay
25
lll
Qay
Ys
l
Qpm3
Ys
Qpx2
Ys
28
Tmi
75
af
Qpx 1
10
Qay 19
17
QTt
8
12
17
? ?
QHa
15 18
Pay
Qpx 2
Qvm 1
Pay
7
ll
10
4
85
53
70
ll
l l
15
34
ll
ll
l
78
18
Tmi
Xla
10
7
43
53
87
15
16
85
Xmv
65
ll
ll
6
˛ml
28
53
Xq
57
l
38
Ys
Ys
33
Qca
70
50
9
Qvm t1
10
15
8
Qpm1
Qvm t
C'
05'
20
18
52
? ?
Qvm 2
QTp
Pay
10
12
34
5
Xcm
ll
ll
l
23
62
63
Xq
QHa
Xd
Qpx2
Xp
ll
42
˛s
75
Qpx2
Xp
l ll
˛mu
28
29
60
Xp
A
50 33
49
58
Xcc
Qpx2
Ys
Qpx2
Ys
l
l
Mesaverde Group, sandstone unit — Feldspathic arenite to quartz arenite, locally with abundant
dark-colored chert grains. Four types of sandstones are included in this unit: 1) resistant, medium- to
thick bedded, trough and wedge-planar cross-stratified, light-colored sandstones, 2) recessive, massive
or flaggy-weathering, argillaceous, greenish-brown colored sandstones and siltstones with abundant
woody debris and mud chip clasts, 3) resistant, clean (non-argillaceous), well-sorted, light-colored, planarbedded to low-angle cross-stratified sandstone, and 4) recessive weathering, thin- to medium-bedded,
dark brown to greenish colored, argillaceous and variably calcareous sandstone containing abundant
molluscan shell fragments (chiefly bivalves). The first two lithotypes were mapped as terrestrial sandstones
(Kvt) in the northerly adjacent Sandia Park quadrangle (Ferguson et al. 1996), and interpreted as alluvial,
or distributary channel sandstones. The third type, which is also characterized by the upper shoreface
environment restrictive trace fossil Macaronichnus (c.f. Mieras et al., 1993), is interpreted as a shoreface
or beach sandstone which were mapped as Kvs in the Sandia Park quadrangle to the northeast. The
fourth type is a marine sandstone that was mapped as part of a marine sandstone and shale unit (Kvm)
in the Sandia Park quadrangle.
19
70
14
Qpx2
Ys
QHao
l
T. 9 N.
Upper Triassic
ˇm
Tmi
9
QTpx
Ys
58
71
Qvmt1
Xla
A
70
52
64
Xcc
43
22
19
Ys
68
16
88
50
61
Qayt
˛ml
ll
14
12
12
21
32
11
12
l
ll
24
65
A,St,Cd
Xla
70
Xp
Qayt
48
Xmv
Qpx2
Xmv
65
65
65
64
78
30
Ys
33
Qay
35
Yss 58
Qvm
14
23
l
02' 30"
Ys
81
14
QTpx
Ys
63
57 33
62
Qvmt
19
48
llll
24
46
84
QHa
QHa
51
67
62
A
Qca
87
Qvmt2 Xp
Qpm3
Xcm
ll
65
80
af
68
75
65
Xp
Qvmt2
Xq
Xcm
79
Ys
QTpx
Ys
Xla
Qvmt1c
Xcm
54
60
Qayt
Qayt
Yss
58
65
22
52
Qay
60
47
36
70
66
63
l
Qay
T. 10 N.
Entrada Formation — A poorly exposed, light green-colored, massive (bioturbated?) sandstone unit that rarely
displays high-angle cross-stratification.
ˇc
QHao
38
78
D U
Qayt
Qay
44
56
QHao
Xq
16
Qay
Qay Xcc
55
Qvmt2
Ys
Qayt
QHa
Qpx2
Xmv
65
QHa
Qayt
Qca
af
49
78
Qayt
af
af
Ys
66
af
QHa
Qpx3
Ys
44
54 55
32
21
49
58
Qayt
3
QHao
36
75
80
Qvmt2
Qayt
13
15
˛ml
7
ll
QHa
14
12
18
25
22
84
12
52
23
17
Qca
10
18
Qvm t2
Qpo
7
14
44
Qpo
50
7
Pay
12
7
14
˛s
Xla
85
70
Xmv
52
34 39
51
35
36
38
50
33
Qay
Ys
Qpx1
Ys
QHao
12
Yss
38
44
Xcc
Xcm
Qvmt2
26
33
54
63
Ys
27
Qpm3
Qca
Pay
12
30
80
79
41
50
12
af
13
Qayt
Qay
Xmv
76
af
12
8
Qpo
17
Pay
11
20
Pay
38
Kvs
Qpo
18
33
32
31
30
QHa
Psg
7
Qvmt
Pay
QHa
˛mu
30
29
15
13
65
55
42
Xcm 36
A,S,Cd
47
Xcc
32
Xcm
Qpx3
Ys
Qpx3
Ys
72
28
10 4 Tmi
18
20
50
˛ml
QTp
Pay
23
60
54
41
23
?
42
35
7
Pay
30
Kvs
Qvmt
8
33
8
65
6
6 15
12
41
58
Pay
43
Pay
Qayt
45
50
Qvmt2
Xmv
56
72
50
30
af
Qca
42
32
44
46 41
40
Qayt
Qay
QHa
Ys
Qay
Ys
Qpx2
Ys
Ys
Qvmt2
Ys
15
33
18
12
76
Qpx2
Ys
QHa
Ys
Qpx2
Ys
Qay
QTsp
15
12
45
60
Qpx2
Ys
12
15
Qayt
Qayt
43
Qay
Qpx1
Ys
Xq
Xcc
85
60
46
A,S
31
53
Ys
Ys
Todilto Formation (chiefly Luciano Mesa Member) — In most areas the only part of this unit that is exposed
is the Luciano Mesa Member, a laminated, fetid, dark-gray, micritic limestone. Laminations in the limestone
appear to be algal in origin and consistently lack of macrofossils. Rarely, the overlying Tonque Arroyo Member,
a thin-bedded to laminated gypsum unit is preserved.
Je
Qay
Ys
Ys
5
Qay
Qayt
af
1
Ys
Ys
Qpx2
Ys
Qpx3
Ys
Yss
46
Xcm
Ya
Yss
Qpx3
Ys
46
Xcm
75
Pay45
Tmi
Kvs
Qvm?
af
25
QHa
55
43
Xmv
Qayt
44
28
75
40 71
55
72
50
80 66
llll
Qayt
Ys
80
Qpm3
QHa
Qay
42
41 31
55
78
29
l
Ys
26
Ys
Ys
54
55
70
34 26
ll
af
38
Entrada and Todilto Formations, undivided — Cross section only. Estimated total thickness is up to 100 ft
(30 m).
Jt
Ys
18
Qay
Ys
24
18
53
20
af
Qpx2
Ys
Ys
QHao
Qca
4
10
Ys
50
3523
Kvs
Kvm 30
60
75
65
85
55
9
6
68
Kvm Kvs
72
17
Kvs
QTp
65
61
70
QHa
50
Qvm
85
ˇc
49
Pay
Psg
Kvm
QTp
66
29
30
76
77
Qay
40 34
Qca
Kd
77
78
60
Ma
˛m
Qca
Xcf
Xcm
Xcf
39 31
Qvmt1
Xcm
82
A,S 14
35
Xcm
26 23
20
55
80
53
29
56
43
75
25
Qay
25
53
58
Qtr
Qay
Xcm
86
5
Xq
29
56
25
25
58
60
49
52
48 77
42 72
Qca
42
Qca Qtr 52 80
68
ˇc
28
55
11
12
15
58
58
80
69
63
72
QTp
QTp
30
67
67
Km
Kd 35
Km
Jm
31
47
62
63
Kvt
75
Kvs
69
Kvs 80
68
88
QHao
Pay
23
49 50
QTp ˛m 5461
63
27 18
30
69
34
65 30 39
13 29
Pay
57
38 65
68
Qpm
Xcm
49 48
73
54
Qpo 58
80
10
51
26
Pay
55
52
Qca ˛m
18
22
QTp
85
˛m
58
Qpo
55
Pay
˛m
33
56
9
31
55
58
80
80
71
Ya
Xcm
5 4 70
49
32
29
Ys
16
86
Qay
Ys
73
49
41
42
60
QHao
Ys
Morrison Formation, undivided — Three members are commonly recognized in northern New Mexico but
are not differentiated in this map area. In descending stratigraphic order, the members are: the Jackpile
Sandstone, the Brushy Basin Shale, and the Salt Wash Sandstone (the Westwater Canyon Sandstone of former
usage, Lucas et al., 1995). The Recapture Shale member has been redefined by Lucas et al. (1995) as the
Summerville Formation of the upper San Raphael Group (Lucas and Anderson, 1997). Due to poor exposure
in the study area, these units are not differentiated. Medium- to thick-bedded, light-colored, generally poorlysorted, feldspathic sandstones, with green and red shaley interbeds. Sandstones contain abundant quartz
granules and greenish mud-chip clasts, and the feldspar grains are typically strongly altered to white clay
minerals. The upper part of this unit, in some areas, is a moderately to well-sorted, moderately bioturbated
feldspathic sandstone which may be equivalent to the Jackpile Member. Abundant dark grayish-green shaley
intervals with thin dark-colored micritic limestones are present in some areas near the base of the map unit.
Total thickness is approximately 500 ft (150 m).
Jet
22
Qay
Qay
Upper Jurassic
Jm
4
Ys
Qca
82
Ys
Ys
Qvmtc
Qpx2
Ys
QHa
62
Ys
36 5
47
8
Qpx3
Ys
QHa
Yss
82
Qca
˛m
80
35
Qvmt2
5
51
22
79
57
Xq
45
50
80
˛m
23 63
65 67
45
87 57 73
40
70
Pay
19 22
21
82
45
Xcc
58
77
Qay
Qvmt2
Qvmt2 Qvmt1
25
Ys
13
86
Qpx3
Ys
Ys
81
Xq
35
Xcm
Qay
35
Jm
l
6
34
˛s
57
lll
Yps
Qpx2
Ys
Qay
14
14
11
64
l
5
Xcm
ll
38 10
15
l l l
19
Qvmt2
Qayt
af
af
QTsp
Qvmt2
10
˛s
Qca
Km
80
71
67
85
81
Qvmt3
Kd
Kvt
65
Km
82
QHao
53
78
76
Jm
Km
64
71
80
Qca
Km
Km
Qca
Km
71
Jm 30
50 51
88 83
28 58 80
37 7685
80
85 64
8
10
14
Qca
Xcm
l
l l
Ys
Qvmt2
9
28
64
17
ll l
Ys
45
35 68
52
Yps
5
QHa
QHao
Yps
41
15
15
16 49
17
22
l
?
QHao
Qayt
20
af
Qvmt2 Qayt QHao
15
20
Pay Ps
ˇc
Kvs
79
65
85
70
81
83
63
38
78
Km
Kd
Jm
77
Jm
ˇz
ˇc
81
79
85
83
Qay
ˇc
81
13
22
20
Ys
18
l l l l
l
l
l
l l
l l l
l l l
l l l
l
Older subunit (middle Pleistocene) — Poorly to moderately consolidated deposits of light- to strongbrown (7.5YR) and very pale-brown to light-gray (7.5-10YR), poorly to moderately stratified and sorted,
sand clayey sand and gravel. Deposit surface (top) is dissected and commonly exhibits erosional ridgeand-ravine topography. Moderately well developed soils with Stage III+ carbonate morphology and
many moderately thick clay films. Correlative to the geomorphic surface Q6 of Connell (1995, 1996)
and to stream alluvium of Tijeras Canyon (Qpmt1). Generally correlative to units P3-P4 of Thomas et al.
(1995).
Ys
Qvmt2
29
45
50
36
73 44
8075
56
ˇc
51
84
74
Qsct
? ?
QHao
Kd
Km
Qca
Jm
82
69
ˇc
Qvmt3
Qpm2
Km
86
65
QHao
Ps
10
23
55
73
12
20 51 25
3
13
l
Qpm1
af
?
Qvmt2
Dakota Formation — Medium-bedded, pervasively silica-cemented, plane-bedded to tabular cross-stratified,
quartz arenite, typically with abundant vertical, lined burrows, many of which are Diplocraterion traces.
Approximately 300 ft (90 m) thick.
Kd
Youngest subunit (upper Pleistocene) — Poorly consolidated and poorly to moderately sorted graybrown to reddish-brown, subangular to subrounded, pebble to cobble gravel with silty sand interbeds.
Inset against middle subunit Qpm2. Soils are moderately developed and exhibit Stage II carbonate
morphology. A radiocarbon date of more than 21,000 years BP reported by Thomas et al. (1995, p.
2-36, unit Pf5) indicates a late Pleistocene age. Correlative to stream alluvium of Tijeras Canyon (Qpmt3),
and generally correlative to units P5-P6 of Thomas et al. (1995).
Younger subunit (upper to middle Pleistocene) — Poorly to moderately consolidated and poorly to
moderately sorted deposits of very pale-brown to strong yellowish-brown (7.5-10YR), poorly to moderately
stratified and sorted, silty clay and loamy sand and gravel. Deposit surface (top) along the mountain
front is slightly to moderately dissected and exhibits subdued bar and swale topography on interfluves.
Soils are moderately developed and possess Stage II to III carbonate morphology and few to common,
thin to moderately thick clay films. Correlative to the geomorphic surface Q7 of Connell (1995, 1996).
Correlative to stream alluvium of Tijeras Canyon (Qpmt2), and generally correlative to unit P5 of Thomas
et al. (1995).
af
Ys
Ys
41
75
26
QHa
QTp
l l
lll l
4H
Qvmt1
Qvmt2
Qpm2
85
9
Ys
22
26
5
l l l l l l l l
l l l ,
l
l
l l
l l
l l
l
Qpm2
af
Tmi
30
84
80
14
44
l l l l
l l l l l
l
l
l l l
l l
l l
Qpm3
Qpx2
Ys
Ys
af
QHa
75
25
33
70
l l l l l l l
l
Middle eastern-margin piedmont alluvium, undivided (upper to middle Pleistocene) — Poorly to
moderately consolidated deposits of very pale-brown to strong-brown and light-gray (7.5-10YR) sand and siltyto clayey-sand, and gravel. Deposit surface (top) is 30-165 ft (9-50 m) above local base level. Gravel clasts
are predominantly subangular granite and schist with minor subrounded limestone derived from the western
front of the Sandia Mountains and Four Hills salient. Slightly to moderately dissected deposit surface exhibits
subdued constructional bar-and-swale topography on interfluves. Weakly developed soils exhibit Stage II to
III+ carbonate morphology and minor to moderate clay film development. Locally divided into three subunits
(Qpm1, Qpm2, and Qpm3). Variable thickness from 0-30 ft (0-9 m).
Qpm
Ys
Qpm1
QTsp
44
Yps
Yps
Yps
70
73
35 45
65
13
15
20
42
22
˛m
Ys
25
l l
l l l
Younger eastern-margin piedmont alluvium (Holocene to uppermost Pleistocene) — Poorly to moderately
sorted and stratified gravel, sand with minor silt-clay mixtures inset against eastern-margin piedmont alluvium
(Qpm). Deposit surface (top) is moderately dissected and exhibits well developed to subdued bar-and-swale
topography. Soils possess Stage I to II carbonate morphology and weakly to moderately developed clay
films. Generally correlative to units H7-H9 of Thomas et al. (1995). Variable thickness from 0-30 ft (0-9 m).
48
Qay
af
QTsp
24
89
12
Ys
5
8
QTp
13
20
Tmi
8
40
30
2560
˛s
50
83 19
53
Je
Jt
68
72
80
64
74 74
34 71
82
55 42
QTp
51 69 ˇm
18
Tmi
14
l l l l l l l l l l l l l l l l l l l l l l l l l
l l l l
l l l
l
l l
l l l l l l
l l l l l l l l l l l l l l l l
Kms
Eastern-margin piedmont slope deposits
Qpy
Ys
74
28
QHa
Mancos Shale, undivided — Dark gray shale, slightly calcareous shale, and septarian nodule-bearing shale,
with rare, thin, black micrite beds and at least two ~10 ft-thick (3-4 m), medium-bedded calcareous sandstone
intervals. The micrites and sandstones are typically fossiliferous yielding abundant molluscan shell fragments
indicating a late Turonian age for the youngest part of the sequence. Total thickness is approximately 1,300
ft (400 m).
Km
Well cemented stream alluvium, undivided (middle Pleistocene) — Indurated, scattered lensoidal
accumulations of calcium-carbonate cemented, subangular to subrounded pebbly sandstone and pebble to
cobble conglomerate. Unconformably overlying pediments developed on Sandia granite (Ys). Probably
correlative to older subunit of the alluvium of Tijeras Creek (Qvmt1). Unit is less than 6 ft (2 m) thick.
Typically contains poorly to moderately sorted and stratified, clast- and matrix-supported sand and gravel with
minor muddy sand interbeds associated coalescent range-front alluvial fans in the Sandia Mountains and Four
Hills salient. Deposits unconformably overlie Santa Fe Group deposits and older rocks, and are differentiated
on the basis of inset relationships and soil-morphology. Clasts are commonly angular to subangular granite
with minor subrounded limestone.
76
Yps
60
Pyc
Pay
˛m
11
42
Yps
42
Ys
Tmi
Ys
50
24
Ys
Qvmt2
38
l l l
l
Qvmtc
36
4
Qpy
26
5
l l l l l l l l l l
l l l l l l l l l l l l l l l l l l l l l l l
Qvm t1
Older subunit (middle Pleistocene) — Moderately consolidated pebble to cobble gravel. Deposits
surface (top) is approximately 50-55 ft (15-17 m) above Tijeras Creek and represents the highest stream
gravel west of Seven Springs in Tijeras Canyon. Unit is locally overlain by about 5 ft (1.5 m) of grus
where inset against the Sandia granite (Ys). Soils locally exhibit Stage III carbonate morphology. Clasts
are dominated by granite, with local accumulations of metavolcanic, gneiss, sandstone and limestone.
Correlative to eastern-margin piedmont alluvium (Qpm1) and units Qf1a and Qa1 of Smith et al. (1982),
and generally correlative to units P3-P4 of Thomas et al. (1995).
88
32 66
Qvmt1
Yps
QHa
9
14
Ys
Tmi
58
Ys
QTsp
51
34
l l l l l l
l l l l l l l l l l l l
Qvm t2
20
42
Ys
67
80
60
Yps
54
22
Yps
10
15
Tmi
l l l l l l l l
l l l
ll
l
Kvm
Youngest subunit (upper Pleistocene) — Poorly to moderately consolidated deposits of sandy gravel
and cobble to boulder gravel. Unconformably overlies crystalline rocks with an irregular contact. Inset
against stream alluvium of units Qvmt1 and Qvmt2. Correlative to eastern-margin piedmont alluvium
(Qpm3) and units Qf1b and Qf2 of Smith et al. (1982), and generally correlative to unit P6 of Thomas
et al. (1995).
Middle subunit (upper to middle Pleistocene) — Moderately consolidated deposits of sandy to
cobbly gravel, with local accumulations of boulders. Minor light-brown to reddish-brown silty sand
interbeds. Clasts are composed of rounded to subangular limestone, granite, quartzite and sandstone.
Basal contact is irregular and sits about 50 ft (15 m) above top of the youngest stream alluvium (QHa).
Inset against stream alluvium of unit Qvmt1 and pediment surface Qpx1 and forms gravelly alluvium
within Tijeras Canyon. Two terraces are recognized near Seven Springs, but not differentiated. Soils
are moderately developed and exhibit Stage II to III carbonate morphology in gravel. Surface is typically
overlain by thin (<1 ft) layer of grus where inset against the Sandia granite (Ys). Correlative to easternmargin piedmont alluvium (Qpm2) and units Qf1a and Qa1 of Smith et al. (1982), and generally
correlative to unit P5 of Thomas et al. (1995).
33
63
Ys
Qpx2
Ys
52
Tmi
Ys
D U
l
Qvm t3
84
62
Ys
l
Qvm t
50
53
?
Qpx2
Ys
?
57
72
Yps
Qca
73
ˇm
ˇz
35 53
40
ˇc
Qvm 3
Qvm t3
Qpx 3
Kd
74
74
Qpm3
Qvm
80
79
81
Pyc
46
54
Ps
52
45
21
l
Kvt
Typically contains moderately to well sorted and stratified, clast- and matrix-supported sand and gravel with
minor muddy sand interbeds associated with the Tijeras Creek drainage. Deposits are differentiated into a
trunk stream that interfingers with steeper tributary drainages to Tijeras Canyon (unit Qay). Clasts are commonly
subangular to subrounded granite, metarhyolite, limestone, yellowish-brown and reddish-brown sandstone
derived from the headwaters of the Tijeras Canyon drainage-basin. Unconformably overlie Santa Fe Group
deposits and older rocks, and are differentiated on the basis of inset relationships and soil-morphology.
Middle stream alluvium of Tijeras Canyon, undivided (upper to middle Pleistocene) — Moderately to
well-consolidated gravelly alluvium containing subrounded to subangular clasts of limestone with minor
sandstone, gneiss and metavolcanic rocks. Unit represents former position of the ancestral Tijeras and Madera
Creeks and is differentiated into three subunits on the basis of inset relationships. Soils are moderately to well
developed and possess Stage II to III calcic horizons in Tijeras Canyon (Smith et al., 1982). This unit commonly
contains unmapped inclusions of younger stream alluvium (Qay, Qayt, and QHa). Thickness is variable from
0-15 ft (0-5 m).
49
l l l l l l l l l l l l l l l
l
Kvs
Youngest stream alluvium, undivided (Historic to upper Holocene) — Unconsolidated deposits of brown,
light gray-brown, and yellowish-brown (10YR) sand, silty to clayey sand, and gravel. Underlies modern arroyos
and inset against younger stream alluvium (Qay). Color and clast composition varies with drainage-basin
composition, but gravel typically contains limestone, gneiss, quartzite, sandstone, granite and metarhyolite.
Deposit surface exhibits no pedogenic development, and unit locally forms small alluvial fans within low-order
tributary drainages of Madera and Tijeras Canyons. Locally divided into an older terrace (QHao) on the basis
of inset relationships. Deposits locally contain asphalt fragments and construction debris. The age is constrained
by radiocarbon dates ranging between 1,000 to 3,000 years BP (Thomas et al., 1995, p. 2-37 and 2-43).
Correlative to units H8 and H9 of Thomas et al. (1995), and correlative to geomorphic surface Q9 of Connell
(1995, 1996). Variable thickness from 0-10 ft (0-3 m).
Younger stream alluvium of Tijeras Canyon (Holocene) — Deposits contain variable proportions of gneiss,
limestone, sandstone and minor granite within the Tijeras drainage. Locally includes undivided stream alluvium
(QHa) in narrow arroyos. A minimum age is constrained by a radiocarbon date of 1,790 ±90 years BP (Locality
1, Beta Analytic Labs No. 104958) near the top of the deposit. Correlative to unit H7 of Thomas et al. (1995)
and unit Qa2 of Smith et al. (1982), and correlative to geomorphic surfaces Q8 and Q9 of Connell (1995,
1996). Variable thickness from 0-20 ft (0-6 m).
50 64
25
36
QHa
Ys
?
Mesaverde Group, undivided — A complex unit of marine, marginal marine, and fluvial sandstones, shales,
and siltstones with several intervals of coal-bearing strata. The sequence is divided into three interbedded map
units: sandstone (Kvs), marine shale (Kvm) and terrestrial shale (Kvt). Note that these subdivisions are defined
differently from the three subdivisions of the Mesaverde Group as recognized in the northerly adjacent Sandia
Park quadrangle; marine sandstone and shale (Kvm), terrestrial sandstone and shale (Kvt), and shoreface
sandstone (Kvs). The exposed thickness of the incomplete Mesaverde Group section is approximately 1,400
ft (430 m).
Kv
Alluvium of Tijeras Creek
Qay t
Ys
65
Pyc
50
Ys
Yps
48
36
31
MESOZOIC ROCKS
Cretaceous
Typically contains poorly to well sorted and stratified, clast- and matrix-supported sand and gravel with minor
muddy sand interbeds associated with modern and late Pleistocene entrenched arroyos and streams originating
in the Sandia and Manzanita Mountains. Deposits unconformably overlie Santa Fe Group deposits and older
rocks, and are differentiated on the basis of inset relationships and soil-morphology.
.
Younger stream alluvium (Holocene to uppermost Pleistocene) — Poorly consolidated deposits of lightbrown to dark-gray, fine-grained silty sand with minor pebbly sand and clayey sand interbeds; pebble lenses
are common along basal contact. Unit forms broad terraces ranging from 8-30 ft (3-9 m) above Tijeras and
Madera Creeks. Two terrace levels are locally recognized, but not differentiated, within Tijeras Canyon. Clasts
are chiefly rounded limestone with minor granite, metavolcanic and gneiss within Madera Canyon. The trunk
stream of the Tijeras Canyon drainage is divided into unit Qayt. Locally includes undivided stream alluvium
(QHa) in narrow arroyos. Soils are weakly developed and exhibit Stage I and II carbonate morphology.
Deposit age is constrained by a radiocarbon of about 10,000 years BP (Thomas et al., 1995, p. 2-43).
Correlative to unit H7 of Thomas et al. (1995), and correlative to geomorphic surfaces Q8-Q9 of Connell
(1995, 1996). Variable thickness from 0-20 ft (0-6 m).
10
Qpx3
Ys
Ys
˛m
65
55
45 64
27
47
Km
? ?
70
84
72
81
67
85
82
Qca
QHao
ˇc
69 23
85
Pay 48
63 54
18
Yps
10
Qay
Yps
Ys
˛m
D U
15
l l l l l l
l l l l l l l
Ys
71
Yps
6
Tmi
˛m
7
4
Pg
20
Qay
Kd Qpm3
53
80
ˇm
60
68
84
47
72
52 69
27
QTp
59
4
Qay
14
5
5514
39
31
56
45
45
Pg
Pyc
15
Pyc
24
Qpx2
Ys
Stream-valley Alluvium
Qay
Ys
83
79
QHao
36
25
46
4
Mafic to intermediate dikes (Oligocene?) — Generally deeply weathered mafic to intermediate, steeply
dipping, north trending dikes. Dikes are probably correlative to an Oligocene mafic to intermediate dike
exposed on the northern flank of the Sandia Mountains (cf., Connell et al., 1995).
.
Tmi
34
59
Ys
Ys
Yps
Yps
63 32
37
ˇc
85
QHa
70
Jm 61
Jt
ˇz
26
35
Qay 55
20
38
Qpm3
56
38
32
ˇm
Pay
30
32
38
Ps
42
13
Ps Pg
42
QTp
Qca
70 44
12
Ys
Tmi
Qpx3
Ys
34
Ys
Tertiary Intrusives
l l l l l l l l
QHa
64
Oldest pediment surface — Deeply dissected and commonly grussified, formerly extensive south-sloping
surface of erosion cut mostly upon Sandia granite (Ys). Surface projects about 120-200 ft (35-60 m) above
Tijeras Creek. Probably correlative to the basal contact of old eastern-slope alluvium (QTp).
.
QTpx
Yps
Yps
5
Tmi
75
˛m
8
Pyc
13
Pg
80
˛s
11
Ys
Qpm
Older pediment surface — Broad, relatively low relief erosional surface on Sandia granite (Ys). Surface
projects to the basal contact of eastern-margin piedmont alluvium (Qpo). Surface projects between 50-100
ft (15-30 m) above Tijeras Creek.
Qpx3
Yps
Qpx2
Ys
38
QHa
D U
6
38
14
34
28
30
25 30
42 Ps
Tmi
Qpx3
Ys
83
Middle pediment surface — Broad, relatively low relief erosional surface on the Sandia granite (Ys). Surface
is lower than the pediment surface of Qpx1 and correlated to the base of older eastern-margin piedmont
alluvium (Qpo). Surface projects between 50-100 ft (15-30 m) above Tijeras Creek.
.
Artificial fill (Historic) — Dumped fill and areas affected by human disturbances. Locally mapped where
areally extensive or geologic contacts are obscured.
.
Travertine and spring deposits (upper Pleistocene to upper Pliocene?) — Light-gray nodular to massive
constructional mounds of travertine interlayered with mudstone and conglomerate derived from local upland
sources. Unit is commonly associated with springs along the eastern dip-slope of the Sandia Mountains. Variable
thickness, ranging from 3-30 ft (1-10 m).
QHa
QTp
30
31
8
75
QHa
58
80
48
64
ˇz Jm
49
Qayt
Km
71
45
Kd75 26 Jm
ˇc
QHao
14
65
45
QTp
34
88 78
Qca
32
Qca
Qpy
41
75
Qpo
10
32
Qca
48
2
Qpo
Pg
35
Pg
26
20
ˇc
18
28 15
Pg
Qpo
Qca
Qay
37
36
IGNEOUS
af
QHao
QHa
Holocene
Qca
Qay
ˇc
32
28
Ps
33
Pg 31
20 24
77
18
38
Younger pediment surface — Exposed erosional surface between Sandia granite (Ys) and overlying younger
stream alluvium (Qay).
Qpx1
UNIT DESCRIPTIONS
QTt
Ys
Yps
Qpx3
Ys
Ys
68
QTp
Ys
Qpm2
QHa
37
Pay
75
10
Yps
D U
Ys
Qca
30
Yps
?
Qca
41
39
20
SEDIMENTARY
36
Ps
39 32
QTp
Qay
Yps
Ys
Qpm2
55
ˇc 53
55
15
Qca
30
ˇc
41
Pg
Qpo
49
Qca
29
25
26
75
64
43
17
ˇc
QTp
24
51
Ys
25
14
Qpm
Pediments, as mapped within the study area, are areally extensive, low-relief surfaces of erosion that were
probably cut by fluvial processes. Pediments grade to the former levels of major piedmont drainages and have
smooth, generally concave-up, surfaces that are commonly marked by tors and corestones. They are primarily
developed on Sandia granite (Ys), but are rarely preserved on Madera Formation, quartzite and metavolcanic
rocks. Pediments are also recognized as short benches preserved on spur ridges along the northwestern slope
of Cerro Pelon. Two generations of weathering rinds developed on corestones indicate that these surfaces
have experienced multiple periods of erosion (Smith et al., 1982), resulting in the formation of broad weatheringlimited slopes underlain by grus and Sandia granite. Up to 15 ft (4.5 m) of grussified granite, and rare
interbedded pebble lenses of weathered granite are locally preserved on pediment slopes. Locally divided
into four units on the basis of inset relationships and height above local base level.
.
Qpx2
Colluvium and alluvium, undivided (Holocene to upper-middle Pleistocene) — Poorly consolidated,
poorly sorted and stratified, fine- to coarse-grained, clast- and matrix-supported deposits derived from a variety
of mass-movement hill slope processes, including debris flow, shallow slump and creep. Gravel clasts are
typically angular to subangular and composition reflects local provenance. Soils locally exhibit Stage I to III
carbonate morphology. Clasts are typically angular and composition generally reflects local provenance.
Commonly surrounds small undivided inliers of Madera Formation limestone on the eastern dip-slope of the
Sandia Mountains. Differentiated where areally extensive, thick, or where geologic contacts are obscured.
Variable thickness, up to 12 ft (4 m).
10
Qay
Pediments
The map has not been reviewed according to New Mexico Bureau of Mines and Mineral Resources standards. Revision of the
map is likely because of the on-going nature of work in the region. The contents of the report and map should not be considered
final and complete until reviewed and published by the New Mexico Bureau of Mines and Mineral Resources. The views and
conclusions contained in this document are those of the authors and should not be interpreted as necessarily representing the
official policies, either expressed or implied, of the State of New Mexico and the U.S. Government.
.
Qca
21
Yps
14
32
47
9
Qpm
D U
5
73
l l
l l l l
l l l l
l l
l l
l l
l l
84
46
34
39
l
38
Yps
5
Ps
87
50
14
Qca
19
23
Pay
14
l l l l
l l l l
l l
l l
B
Ys
86
67
38
Qca
Tmi
QHao
Pg
20
60
46
19
strand
Qpm
75
Yps
ll
85
Tmi
Qay
Epoch
33
7
Pg
Ps
20
QHa
Qay
QTp
20
QHa
36
25
21
l
38
9
38
Pyc
24
ll l l
QHa
55
32
38
57
˛m
4
ll
Qpm
Tmi
Qay
ˇc
Ps
Qca
31
Pay
81
˛m
l
Qpy
Qpm
22
7
Yps
Ps
33
65
59
5
QTp
Qca
25 84
ll
86
Younger subunit (upper to middle Pleistocene) — Poorly to moderately consolidated and poorly to
moderately sorted deposits of very pale-brown to strong yellowish-brown (7.5-10YR), poorly to moderately
stratified and sorted, silty clay and loamy sand and gravel. Soils are moderately developed and possess
Stage II to III carbonate morphology and few to common, thin to moderately thick clay films. Probably
correlative to stream alluvium of Tijeras Canyon (Qpmt1), and generally correlative to units P5-P6 of
Thomas et al. (1995).
Older subunit (middle Pleistocene) — Poorly to moderately consolidated deposits of light- to strongbrown (7.5YR) and very pale-brown to light-gray (7.5-10YR), poorly to moderately stratified and sorted,
sand clayey sand and gravel. Deposit surface (top) is dissected and commonly exhibits erosional ridgeand-ravine topography. Moderately well developed soils with Stage III+ carbonate morphology and
many moderately thick clay films. Probably correlative to stream alluvium of Tijeras Canyon (Qpmt1),
and generally correlative to units P3-P4 of Thomas et al. (1995).
Ys
64
34
27
U NITS
OF
1 500 000
FEET
36
15
14
ˇz
30
ˇm
10
Pg
17
C ORRELATION
Qay
42 25
21
Ps
Pay
28
Ps
30
Qay
ˇm 14
Ps
23
17
QHa
Pay
Ys
Yps
74000m E.
Qca
25
31
15
l
Qpy
38
10
23
67
lll
Youngest subunit (upper Pleistocene) — Poorly consolidated and poorly to moderately sorted graybrown to reddish-brown, subangular to subrounded, pebble to cobble gravel with silty sand interbeds.
Inset against middle subunit Qvm2. Soils are moderately developed and exhibit Stage II carbonate
morphology. A radiocarbon date of more than 21,000 years BP reported by Thomas et al. (1995, p.
2-36, unit Pf5) indicates a late Pleistocene age. Probably correlative to stream alluvium of Tijeras Canyon
(Qpmt1), and generally correlative to units P5-P6 of Thomas et al. (1995).
QTp
32
Pay
106° 22' 30"
35° 07' 30"
3
Ps
50
strand
A geologic map displays information on the distribution, nature, orientation and age relationships of rock and deposits and the
occurrence of structural features. Geologic and fault contacts are irregular surfaces that form boundaries between different types
or ages of units. Data depicted on this geologic quadrangle map are based on reconnaissance field geologic mapping, compilation
of published and unpublished work, and photogeologic interpretation. Locations of contacts are not surveyed, but are plotted
by interpretation of the position of a given contact onto a topographic base map; therefore, the accuracy of contact locations
depends on the scale of mapping and the interpretation of the geologist(s). Any enlargement of this map could cause misunderstanding
in the detail of mapping and may result in erroneous interpretations. Site-specific conditions should be verified by detailed surface
mapping or subsurface exploration. Topographic and cultural changes associated with recent development may not be shown.
38
l
Qpm
Piedmont deposits (lower Pleistocene to Miocene) — Subhorizontally stratified to slightly east-tilted, reddishbrown to yellowish-brown and very pale-brown (7.5-10YR) conglomerate, gravelly sandstone, and sandstone
with subordinate siltstone and rare mudstone. Conglomerate clasts are predominantly composed of subangular
to subrounded granite with subordinate metamorphic rocks, and minor subrounded limestone. Unconformably
overlies Sandia granite (Ys) and is unconformably overlain by eastern-margin piedmont alluvium. A monitoring
well (4H) near the intersection of Tijeras Creek and Four Hills Road (Richey, 1991) encountered 69 ft (21 m)
of eastern-margin piedmont alluvium and Santa Fe Group piedmont deposits just west of the Sandia fault.
These deposits interfinger with and overlie early Pleistocene (Irvingtonian land mammal “age”) fluvial deposits
of the ancestral Rio Grande near the mouth of Tijeras Arroyo (see Lucas et al., 1993). May be correlative with
piedmont-slope and alluvial fan deposits of the Sierra Ladrones Formation (Machette, 1978) exposed at the
southern margin of the Albuquerque Basin. Estimated hydraulic conductivity is low. Base is not exposed, but
deposit thickens to the west across the Sandia fault zone to where it is several thousand feet thick.
COMMENTS TO MAP USERS
af
10
82 7
Ys
Digital Cartography
Thin surficial deposits derived from wind and mass-movement processes, or extensive areas disturbed by openpit aggregate mining or construction.
41 42
QHa
87000m N.
Old eastern-slope alluvium (lower Pleistocene to upper Pliocene(?)) — Moderately consolidated and
poorly to moderately sorted gravel that forms the highest gravel preserved along the southeastern flank of the
Sandia Mountains. Locally contains two undivided subunits. Contains subrounded to subangular clasts of
limestone with minor (< 5%) sandstone and highly weathered, grussified granite and metamorphic rocks. The
basal contact is about 40-200 ft (12-60 m) above local base level. Deposits cover a formerly areally extensive
pediment developed along the southeastern flank of the Sandia Mountains that may be correlative to the Tuerto
gravel of Stearns (1953). Deposit surface (top) is dissected and soils are generally stripped, but locally exhibit
Stage III+ carbonate morphology. Variable thickness from 0-30 ft (0-10 m).
QTsp
73
l
14
05'
CENOZOIC DEPOSITS
Neogene (Quaternary and Tertiary) System
Colluvial, landslide, eolian, and anthropogenic deposits
Yps
43
38
460 000 FEET
3
42 18
l lll
Qpy
Older eastern-slope alluvium (middle to lower Pleistocene) — Poorly to moderately consolidated deposits
of yellowish-brown (10YR), poorly to moderately sorted and stratified, gravel and sand with thin silty-clay
interbeds. Forms alluvial fans that developed along relatively steep tributary drainages to the Arroyo de San
Antonio and Tijeras Creek. Gravel clasts are predominantly subrounded limestone with a greater proportion
of sandstone that in old eastern-slope alluvium (QTp). Overlies a formerly extensive erosional surface (pediment)
developed on the eastern dip-slope of the Sandia mountains. Deposit surface (top) is dissected and soils are
generally stripped, but locally exhibit Stage III carbonate morphology. Deposits grade to high pediment surface
QTpx in Tijeras Canyon. Variable thickness from 0-16 ft (0-5 m).
QTp
5
17
Eastern-slope alluvium
Qpo
72
˛s
l l l l l l l l
Qvm1
3
71
l
59
Sandia fault zone – West Embudo
Qvm2
3
25'
ll
Yps
Santa Fe Group
Special thanks to Mr. Joe Rogers, Mr. Larry Rainosek, Mr. Richard Nieto (Carnuel Land Grant Association), Mr. Ray McDaniels
(Acequia Madre de Carnuel Community Ditch Association) and Mr. Chris Jinzo and Mr. Gary Hefkin of the Acequia Madre de
San Antonio Community Ditch Association for logistical assistance and access to their lands during this study.
.
C
(SANDIA CREST)
43
S an d i a fa u lt z o n e – Ea s t Embud o
Qvm3
1 Department
David J. McCraw
Mark M. Mansell
Glen E. Jones
68
Ys
Middle stream alluvium of Madera Canyon, undivided (upper to middle Pleistocene) — Poorly to
moderately consolidated deposits of very pale-brown to strong-brown and light-gray (7.5-10YR) sand and siltyto clayey-sand, and gravel. Deposit top is 30-165 ft (9-50 m) above local base level. Gravel clasts are
predominantly subangular granite and schist with minor subrounded limestone derived from the western front
of the Sandia Mountains and Four Hills salient. Slightly to moderately dissected deposit surface exhibits subdued
constructional bar-and-swale topography on interfluves. Weakly developed soils exhibit Stage II to III+ carbonate
morphology and minor to moderate clay film development. Locally divided into three subunits (Qvm1, Qvm2,
and Qvm3). Variable thickness from 0-30 ft (0-9 m).
Qvm
Plate I of II.
5 April 2000 Revision
of Earth and Planetary Sciences, University of New Mexico, Albuquerque, NM 87131
2 New Mexico Bureau of Mines and Mineral Resources, Albuquerque, NM 87106
3 Arizona Geological Survey, 416 W. Congress, #100, Tucson, AZ 85701
4 New Mexico Bureau of Mines and Mineral Resources, Socorro, NM 87801
5 Department of Earth and Planetary Sciences, Washington University, St. Louis, MO 63130
6 Department of Earth and Environmental Science,
New Mexico Institute of Mining and Technology, Socorro, NM 87801
7 William Lettis & Associates, Inc., 1777 Botelho Dr., Suite 26 2, Walnut Creek, CA 945 96
3
QHa
Typically contains poorly to well sorted and stratified, clast- and matrix-supported sand and gravel with minor
muddy sand interbeds associated with modern and late Pleistocene entrenched arroyos and streams originating
in the northern Manzanita Mountains. Deposits unconformably overlie pre-Cenozoic rocks, and are differentiated
on the basis of inset relationships and soil-morphology. Clasts are commonly angular to subrounded limestone,
metarhyolite, gneiss, and quartzite.
Geology of the Tijeras quadrangle,
Bernalillo County, New Mexico
by
1
Karl E. Karlstrom , Sean D. Connell 2 , Charles A. Ferguson 3 ,
Adam S. Read 4 , Glenn R. Osburn 5 , Eric Kirby 1 , John Abbott 6 ,
Christopher Hitchcock 7 , Keith Kelson 7 , Jay Noller 7 ,
Thomas Sawyer 7 , Steven Ralser 6 , David W. Love 4 ,
Matthew Nyman 1 , and Paul W. Bauer 4
66
Qpm
EMA
Dr. Paul W . Bauer
Geologic Mapping
Program Director
Dr. Peter A. Scholle
Director and State Geologist
27' 30"
3
65
ll
lll l
AT
3
ll l
nce fo r t h e 21st
Cen
64000m E.
l
Scie
Alluvium of Madera Canyon
3
R. 5 E.
lll
T
y
tur
106° 30'
35° 07' 30"
I
Tec h
S
rth
ME X
l ll l l l l
l l
l l
l l
Me x i c o
W
NEW MEXICO
A
ll l llll
e
TIJERAS QUADRANGLE
l ll
al
R
CO
Ne w
Ea
e s & Mi n e r
ces
ur
so
a
in
fM
uo
MEXICO INSTITUTE OF MINING & TECHNOLOGY
S)
TA
CI
LA
(P
A DIVISION OF NEW
NMBMMR Open File Map Series
OF–GM–4
Map last modified 5 April 2000
Plate I of II.
Paleoproterozoic
NEW MEXICO BUREAU OF MINES AND MINERAL RESOURCES
Table of Geochronologic Samples
Locality
Date
1
2
3
1,790 ±90 BP
1,423±2 Ma
1,455±12 Ma
1,437±47 Ma
1,446±26 Ma
1,422±3 Ma
1,423±2 Ma
1,632±45 Ma
1,659±13 Ma
4
5
6
Formation
Method
Qayt
Xcm(sz)
Ys
Ys
Ys
Ys
Xq
Xcm
Xcm
14C
40Ar/39Ar
(whole rock)
U-Pb zircon + sphene
U-Pb zircon
U-Pb zircon
40Ar/39Ar (hornblende)
40Ar/39Ar (muscovite)
U-Pb zircon
U-Pb
Reference
Sample No. Beta-104958 (this study)
Karlstrom et al. (1997 b)
Tilton and Grunenfelder (1968 ), recalculated by S. Getty (unpubl.)
Stieger and Wasserburg (1966 ), recalculated in Kirby et al. (1995 )
D. Unruh, (unpublished); Karlstrom (1999)
Kirby et al. (1995 )
Kirby et al. (1995 )
D. Unruh, (unpublished); Karlstrom (1999)
D. Unruh, (unpublished); Karlstrom (1999)