high aggregate potential in Three Rivers area because of coarser texture there. Low agricultural potential because of gypsic top soil.
Qao1
•
••
•
•
• •
••
••
22
Qay2u
•
••
•••
•••
••••
••••
••••
•••
•••
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••••
•••
•••
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•••
•••
•••
•••
•••
••••
•••
•••
•••
•
•
•
•
9
GODFREY
PEAK
THREE
RIVERS SW
THREE
RIVERS
GOLONDRINA
DRAW
SIERRA
BLANCA
PEAK
RUIDOSO
BITTER
CREEK
TULAROSA NE
CAT
MOUNTAIN
MESCALERO
APACHE
SUMMIT
Qay2u
Qay2u
Qao
Qac
17
Qao
*h
Qao
Qay2u
Qac
Qay2
Qao
106°00'00"W
Qao2
Py
Pa
Qao3
Qao
Qac QTg
Ti
55'00"
Qc
Qc
Qay
Qay
*h
Qao3
52'30"
1.5 MILE
Qary3
1000
Pa
Pa
Qc
1
0.5
0
1000 2000 3000 4000 5000 6000 7000 FEET
0
1 KILOMETER
Qary2
Py
CONTOUR INTERVAL VARIES
Py 33°00'00"N
Pa
Qay
NATIONAL GEODETIC VERTICAL DATUM OF 1929
New Mexico
June 2014
Qay3
by
MALONE
DRAW
DOMINGO
PEAK
HIGH
ROLLS
ALAMOGORDO
NORTH
Shari Kelley, Daniel J. Koning, and Bruce Allen
FIRMAN
CANYON
New Mexico Bureau of Geology and Mineral Resources, Socorro, NM
CLOUDCROFT
S c ie
nce for the
TECH
en
2 1st C
tur
New Mexico Bureau of Geology and Mineral Resources
NEW M EXICO I NSTITUTE OF M INING AND TECHNOLOGY
801 Leroy Place, Socorro, New Mexico 87801-4796 (575) 835-5490
y
MEXI
Qay3r
TA
S
r th
M EXICO
EW
O
C
NEW
Mapping of this quadrangle was funded by a matching-funds grant from the STATEMAP program
of the National Cooperative Geologic Mapping Act, administered by the U.S. Geological Survey,
and by the New Mexico Bureau of Geology and Mineral Resources (Dr. Peter A. Scholle, Director
and State Geologist, Dr. J. Michael Timmons, Geologic Mapping Program Director).
s
urce
eso
lR
ra
Ea
New Mexico Bureau of Geology and Mineral Resources
Open File Report 564
f Geology and
uo
a
Mi
e
r
ne
Bu
http://geoinfo.nmt.edu
P
LOST
RIVER
SABINATA
FLAT
N
TULAROSA
New
Me
xic
o
TULAROSA
PEAK
TEMA
Qay2
This and other STATEMAP quadrangles are (or soon will be) available
for free download in both PDF and ArcGIS formats at:
http://geoinfo.nmt.edu/publications/maps/geologic/ofgm/home.html
A'
Godfrey Hills fault zone
A
Kmd Kth
West
E–E'
Lewelling No. 1
Lewelling No. 2
5,000
feet ASL
4,000
State L.G.
“1453”
QTbf
3,000
Tla
Tlw2a
sharp contact (disconformity?)
Ps
Probable buried normal faults
paralleling Alamogorod fault
2,000
Kt Kmd
Km
Kd l
TRm
Pag
Pag
1,000
Kg
d
Kg
Kmd
Kth
Kml
Kd
TRm
Pag
Kth
Kg
Psf
Kmd
Psr
–1,000
–2,000
TRm
Pag
–3,000
Kmd
–4,000
Kg
Kd
Pag
?
Py
?
?
Kd
?
Py
TRm
Ps
IPh
Py
Py
MS
D
O
XYu
XYu
Psf
Psf
Psf
Psr
2,000
meters ASL
1,500
Py
Py
1,500
Py
Py
Py
Psf
Psr
Psr
Psr
Psr
Py
Kml
Kd
TRm
Pag
Psf
Psf
Psr
Kth
Kml
Kd
TRm
Pag
Kml
Kd
TRm
Pag
Kml
Kd
TRm
Pag
500
Pa
Pa
Pa
Pa
Pa
Pa
Pa
Pb
Pa
Pb
Pb
Pb
Pb
Pb
Pb
Pb
Pb
0
–1,000
–1,500
IPg
IPg
MSD
MSD
O
O
–2,000
No vertical exaggeration
60,000
XYu
TD: 9852 ft depth
30,000
40,000
50,000
West
Desal. Test
Well #4
5,000
(projected
from north,
perpendicular
to profile line)
Pliocene–Pleistocene, gravelly sediment (includes units Qf1 and Qfo in its upper part)
4,000
Upper basin-fill unit
(more coarse-grained to east,
more fine-grained to west)
3,000
1,000
Desal. Test
Well #5
Pliocene–Pleistocene,
gravelly sediment
Psf
Py
Lower coarse interval
Abo Fm.
Lower basin-fill unit
Lower coarse interval
Lower basin-fill unit
10,000
20,000
Py
1,500
Pa
1,000
Pb
Pb
500
˛g
M
˛h
˛b
SD
60,000
˛g
Allen, M.S., and Foord, E.E., 1991, Geological, geochemical and isotopic characteristics of the Lincoln County porphyry belt, New Mexico:
implications for regional tectonics and mineral deposits: New Mexico Geological Society Guidebook 42, pp. 97–102.
Bachman, G.O, 1954, Reconnaissance map of an area southeast of Sierra Blanca in Lincoln, Otero, and Chaves Counties, New Mexico: New
Mexico Geological Society Guidebook 5, p. 94.
0
No vertical exaggeration
70,000
Qay2u
Arkell, B.W., 1983, Geology and coal resources of the Cub Mountain area, Sierra Blanca coal field, New Mexico [Masters Thesis]: Socorro,
NM, New Mexico Institute of Mining and Technology, 104 p.
˛h
˛b
˛g
50,000
Py
Psr
Pa
˛b
40,000
Psf
Tim
Py
˛h
˛h
˛b
30,000
Py
2,000
meters
ASL
REFERENCES
Py
Tid
Pag
Psf
Pb
Holder Fm.
Beeman Fm.
0
Psr
Pb
Undifferentiated pre-rift bedrock
Psf
Ti
Pa
Pa
Bursum Fm.
Undifferentiated pre-rift bedrock
Psr
Psr
Psf
Py
Ti
East
Karst
feature
Maxwell
Spring
Psr
Psr
Psf
Yeso Fm.
Lower transition interval
Undifferentiated
pre-rift bedrock
0
(projected
from south,
perpendicular
to profile line)
Upper basin-fill unit
Lower basin-fill unit
(more coarse-grained to east,
more fine-grained to west)
2,000
Desal. Test
Well #8
Latest Miocene(?) to
Pliocene, coarse sediment
Bachman, G.O., 1960, Southwestern edge of late Paleozoic landmass in New Mexico: U.S. Geological Survey Professional Paper 400 B p.
239–241.
B
Cat
Mountain
Monocline
East
Birkeland, P.W., Machette, M.N., and Haller, K.M., 1991, Soils asBB'
a tool for applied Quaternary geology: Utah Geological and Mineral Survey,
a division of the Utah Department of Natural Resources,Bent
Miscellaneous Publication 91–3, 63 p.B
Cat
Mountain
dome
Psf
Upper basin-fill unit
Upper basin-fill unit (more coarse-grained
to east, and more fine-grained to west)
Temporal
Creek
Desal. test
well #8
(projected
Latest Miocene(?) to
Pliocene, coarse sediment from south,
perpendicular
Desal. test
to profile line)
well #5
Desal. test
well #4
(projected
from north,
perpendicular
to profile line)
Pliocene-Pleistocene, gravelly sediment (includes units Qf1 and Qfo in its upper part)
lower transition interval
Undifferentiate
Yeso Formation
10000
Abo Formation
Py
(Py)
Py
(Pa)
Pa
Pb
tion (Pb)
Pennsylvanian
and
older units
20000
25000
30000
35000
Pb
40000
45000
50000
55000
60000
65000
Pa
COb
6500
4500
4000
Pb
Pb
Blair,
J.G., 1994a, Alluvial fans and their natural distinction
from rivers based on morphology, hydraulic processes, sedimenta3500
PbT.C., and McPherson, Pb
3000
pC
ry processes, and facies assemblages: Journal of Sedimentary
Research,
vol.
A64,
p. 450–489.
2500
2000
1500 in Abrahams, D., and Parsons, A.J., eds., Geomorphology of Desert
Blair, T.C., and McPherson, J.G., 1994b, Alluvial fan processes and forms,
1000
Environments: London, Chapman and Hall, p. 354–402.
500
0
80000P.W. and Lozinsky,
85000
90000
95000Paleozoic uplift in southern New Mexico: New Mexico Geological Society
Bauer,
R.P., 1991, The Bent
dome - part of a major
Pb
Pa
Tita
Pa
Pa
Pa
Pa
Bursum Forma
15000
Py
Psr
Pb
ck
5000
Psf
Psr
Tid
Tid Py
6000 Springs Canyon alluvial fan, Death Valley, California: Sedimentology,
Blair,
facies of the waterlaid Anvil
Py processes andPy
5500
PyT.C., 1999, Sedimentary
Pa
vol. 46, p. 913–940.
5000
Pa
Tig
Py
Tita
k
Undifferentiated pre-rift bedro
0
Tid
d pre-rift bedroc
Lower basin-fill unit
Undifferentiated pre-rift bedrock
Psr
Psf
Tim
Tim
Psf
Psr
Lower basin-fill unit
Lower coarse interval
Psf
Psr
Birkeland, P.W., 1999, Soils and geomorphology: New York, Oxford University
Press, 430 p.
7000
Psr
Psr
Tid
Pliocene-Pleistocene,
gravelly sediment
Lower coarse interval
Lower basin-fill unit (more coarse-grained
to east, and more fine-grained to west)
70000
75000
Guidebook 42, p. 175–182.
ba se of ba
sin fil l fro m
Heal y et al
. (1978)
Ysletano Canyon
Houston Fed. 1A
Trustee No. 1
T–378
T–5424
?
undivided Permian
to Cambrian
sedimentary rocks
Gile, L.H., Hawley, J.W., and Grossman, R.B., 1981, Soils and geomorphology in the Basin
and Range area of Southern New Mexico—Guidebook
1,000
to the Desert Project: New Mexico Bureau of Mines and Mineral Resources, Memoir 39, 222 p.
Holder Formation
Pennsylvanian carbonates, sandstone, shale
Beeman Formation
Mississippian carbonates
Gobbler Formation
50,000
REFERENCES
60,000
70,000
Hook , S.C., and Cobban, W.A., 2012, Evolution of the Late Cretaceous oyster genus Cameleolopha Vyalov 1936 in central New Mexico: New
Mexico Geology, v. 34, no. 3, p. 76-95.
Bachman, G.O., 1960, Southwestern edge of late Paleozoic landmass in New Mexico: U.S. Geological Survey Professional Paper 400 B p.
239–241.
Tularosa NE
Ingram, R.L., 1954, Terminology for the thickness of stratification and parting units in sedimentary rocks: Geological Society of America Bulletin, v.
65, p. 937–938, Table 2.
E'
Alamogordo fault
Bachman, G.O, 1954, Reconnaissance map of an area southeast of Sierra Blanca in Lincoln, Otero, and Chaves Counties, New Mexico: New
Mexico Geological Society Guidebook 5, p. 94.
DesalTest
Test Well
No.No.
1 1
Desal
Well
Hook, S.C., 2010, Flemingostrea elegans, n. sp: guide fossil to marine, lower Coniacian (upper Cretaceous) strata of central New Mexico: New
Mexico Geology, v. 32, no. 2, p. 35–57.
40,000
F
Golondrina
Draw E-W
section
Three Rivers
cross-section
Tim
Tita
Titd
5,000
Kc
Kc
Kc
Kclt
Kclt
Kg
4,000
Kmd
Kth
Kml
3,000
Kc
Kg
Kmd
Kd
TRm
Kml
Kd
TRm
Pag
2,000
Kg
Kc
Kclt
Psf
Pag
Psr
Psf
Py
Psr
Py
1,000
Kmd
Kclt
Kth
Kg
Kth
Pag
Kml
Kd
TRm
Kth
Kg
Kclt
Kth
Kmd
Kmd
Kml
Kd
TRm
Pag
Tim
Kg
Kg
Kmd
Kmd
Kml
Kd
TRm
Pag
Kth Kml
Kd
TRm
Pag
Psf
Psf
Psr
Psf
Kml
Kd
TRm
Pag
Tid
Kg
Tc
Titd
Tim
Tid
Kth
Kth
Kmd
Kml
Kd
TRm
Pag
Kmd
Kml
Kd
TRm
Pag
Psf
Psr
Psf
Kth
Kth
Kmd Kmd Kth
Kml
Kd
TRm
Pag
Kml
Kd
TRm
Pag
Kml
Kd
TRm
Pag
Psf
Psf
Psf
Psr
Psr
Psr
Tita
Psf
Py
Py
Pa
Pa
Py
Pa
Psf
Psf
Psf
Psr
Psr
Psr
Py
Py
Pa
20,000
Pb
Pb Pb
Pb
Pb
Pb
Pb
30,000
The illustrated dikes and sills conceptually capture the range of
dike, sill, and fault interactions observed in the field. Faults cut
sills. Sills tend to form in the Yeso and Crevasse Canyon formations.
The east-west striking faults likely formed in a right-lateral releasing
bend that formed during Laramide deformation. Some faults are filled
with dikes anddisplay no subsequent motion. Some dikes are offset
or truncated by the E-W striking faults, but the dike offset is much less than the
stratigraphic offset. Some dikes are younger than the faults and
are unaffected by faulting.
REFERENCES
Allen, M.S., and Foord, E.E., 1991, Geological, geochemical and isotopic characteristics of the Lincoln County porphyry belt, New Mexico:
implications for regional tectonics and mineral deposits: New Mexico Geological Society Guidebook 42, pp. 97–102.
Arkell, B.W., 1983, Geology and coal resources of the Cub Mountain area, Sierra Blanca coal field, New Mexico [Masters Thesis]: Socorro,
NM, New Mexico Institute of Mining and Technology, 104 p.
Bachman, G.O, 1954, Reconnaissance map of an area southeast of Sierra Blanca in Lincoln, Otero, and Chaves Counties, New Mexico: New
Mexico Geological Society Guidebook 5, p. 94.
Bachman, G.O., 1960, Southwestern edge of late Paleozoic landmass in New Mexico: U.S. Geological Survey Professional Paper 400 B p.
239–241.
Bauer, P.W. and Lozinsky, R.P., 1991, The Bent dome - part of a major Paleozoic uplift in southern New Mexico: New Mexico Geological Society
Guidebook 42, p. 175–182.
Birkeland, P.W., Machette, M.N., and Haller, K.M., 1991, Soils as a tool for applied Quaternary geology: Utah Geological and Mineral Survey,
a division of the Utah Department of Natural Resources, Miscellaneous Publication 91–3, 63 p.B
Pb
IPh
Psf
Psr
Py
g
Kd
Qa
Tim sill
Tita sill
Kml
Qa
I-I’ cross section
QTbf
Pag
Psf
TRm
Kd
Petroglyph horst
QTbf
Kml
Py
Py
Pa
Sedimentology,
60,000
Pa
Pa
Psr
Psr
Kg
Kmd
TRm
Pag
Kml
Psf
Kd
Kml
Kmd
TRm
Kt
Pag
Kd
Psf
Py
Trm
Pag
Py
Pa
Pa
Psr
Kc
Kg
Kmd
Kt
Kml
Kd
TRm
Pag
Kclt
Kg
TRm
Pag
Py
Py
Py
Pa
Kmd
Kt
Kml
Ps
Psf
Psr
1,000
Psf
Psr
500
Koning, D.J., 1999, Fault segmentation and paleoseismicity of the southern Alamogordo fault, southern Rio Grande rift [M.S. thesis]: Albuquerque,
0
University of New Mexico, 286 p.
No vertical exaggeration
Pa
Pa
1,500
Kg
Kt
Kc
Kclt
King, W.E., and Harder, V.M., 1985, Oil and gas potential of the Tularosa Basin–Otero Platform–Salt Basin graben area, New Mexico and Texas:
New Mexico Bureau of Mines and Mineral Resources Circular 198, 36 p. (with plates).
Py
Pa
Pa
Pa
Pa
Pa
Blair, T.C., and McPherson, J.G., 1994a, Alluvial fans and their natural distinction from rivers based on morphology, hydraulic processes, sedimentary processes, and facies assemblages: Journal of Sedimentary Research, vol. A64, p. 450–489.
Blair, T.C., and McPherson, J.G., 1994b, Alluvial fan processes and forms, in Abrahams, D., and Parsons, A.J., eds., Geomorphology of Desert
Environments: London, Chapman and Hall, p. 354–402.
Bauer, P.W. and Lozinsky, R.P., 1991, The Bent dome - part of a major Paleozoic uplift in southern New Mexico: New Mexico Geological Society
Guidebook 42, p. 175–182.
Bull, W.B., 1972, Recognition of alluvial-fan deposits in the stratigraphic record, in Rigby, J.K., and Hamblin, W.K., eds., Recognition of ancient
sedimentary environments: Society of Economic Paleontologists and Mineralogists Special Publication 16, p. 63–83.
Bull, W.B., 1977, The alluvial fan environment: Progress in Physical Geography, vol. 1, p. 222–270.
Compton, R.R., 1985, Geology in the field: New York, John Wiley & Sons, Inc., 398 p.
Bauer, P.W. and Lozinsky, R.P.,F'1991, The Bent dome - part of a major Paleozoic uplift in southern New Mexico: New Mexico Geological Society
Guidebook 42, p. 175–182.North
Koning, D.J., Pazzaglia, F., and Smartt, R., 2002, Alluvial fan stratigraphy along the southern Sacramento Mountains, N.M., and inferences regarding late Quaternary paleoclimate, soils, and sedimentation: New Mexico Geological Society Guidebook 53, p. 289–302.
Bull, W.B., 1972, Recognition of alluvial-fan deposits in the stratigraphic record, in Rigby, J.K., and Hamblin, W.K., eds., Recognition of ancient
2,000of Economic Paleontologists and Mineralogists Special Publication 16, p. 63–83.
sedimentary environments: Society
Koning, D. J., Hallett, B., and Shaw, C., 2007, Preliminary geologic map of the Alamogordo North 7.5-minute quadrangle, Otero County, New
Mexico: New Mexico Bureau of Geology and Mineral Resources OF–GM–153, scale 1:24,000.
Qaof
Tita
Bull, W.B., 1977, The alluvial fan1,500
environment: Progress in Physical Geography, vol. 1, p. 222–270.
Psf
Psr
Koning, D.J., Kempter, K.A., Zeigler, K.E., and Cicoski, C.T., 2011, Preliminary geologic map of the Cub Mountain 7.5-minute quadrangle: New
Mexico Bureau of Geology and Mineral Resources OF–GM–138, scale 1:24,000.
Foord, E.E., and Moore, S.L., 1991, Geology of the Bent Dome, Otero County, New Mexico Geological Society Guidebook 42, p. 171–174.
Kuhle, A.J., and Smith, G.A., 2001, Alluvial-slope deposition of the Skull Ridge Member of the Tesuque Formation, Española Basin, New Mexico:
New Mexico Geology, vol. 23, no. 2, p. 30–37.
Gile, L.H., Peterson, F.F., and Grossman, R.B., 1966, Morphological and genetic sequences of carbonate accumulation in desert soils: Soil
Science, v.
p. exaggeration
347–360. 0
No101,
vertical
Lucas, S.G., and Krainer ,K., 2004, The Red Tanks Member of the Bursum Formation in the Lucero Uplift and regional correlation of the Bursum
Formation in New Mexico: New Mexico Museum of Natural History and Science, Bulletin 25, p. 43–52.
Gile, L.H., Hawley, J.W., and Grossman, R.B., 1981, Soils and geomorphology in the Basin and Range area of Southern New Mexico—Guidebook
to the Desert Project: New Mexico Bureau of Mines and Mineral Resources, Memoir 39, 222 p.
Mack, G.H., Dinterman, P.A., 2002, Depositional environments and paleogeography of the Lower Permian (Leonardian) Yeso and correlative
formations in New Mexico: The Mountain Geologist, v. 39, p.75–88.
Harbour, R. L, 1970, The Hondo Sandstone Member of the San Andres Limestone of south–central New Mexico : U. S. Geological Survey Professional Paper 700–C, p. 175–182.
McManus, C.E.D., and McMillan, N.J., 2002, Subduction or rifting: the Eocene magmas of the Sacramento Mountains, NM: Geological Society
of America Abstracts with Programs, v. 34, no. 6, p. 364.
Hawley, J.W., and Wilson, W.E., 1965, Quaternary geology of the Winnemucca area, Nevada: University of Nevada, Desert Research Institute,
Technical Report no. 5, 66 p.
McMillan, N.J., 2004, Magmatic record of Laramide subduction and the transition to Tertiary extension: Upper Cretaceous through Eocene
igneous rocks of New Mexico: New Mexico Geological Society Special Publication 11, p. 249–270.
500
40,000
Qao3
Hooke, R.L., 1967, Processes on arid-region alluvial fans, Journal of Geology, vol. 75, p. 438–460.
Miller A.K., and Youngquist, W., 1949, American Permian Nautiloids: Geological Society of America Memoir 41, 218 p.
Hook, S.C., 2010, Flemingostrea elegans, n. sp: guide fossil to marine, lower Coniacian (upper Cretaceous) strata of central New Mexico: New
Mexico Geology, v. 32, no. 2, p. 35–57.
Moore, S. L., Foord, E. E., and Meyer, G. A., 1988a, Geologic and aeromagnetic map of a part of the Mescalero Apache Indian Reservation,
Otero County, New Mexico: U.S. Geological Survey Miscellaneous Investigations Series Map I–1775, scale 1:50,000.
Hook , S.C., and Cobban, W.A., 2012, Evolution of the Late Cretaceous oyster genus Cameleolopha Vyalov 1936 in central New Mexico: New
Mexico Geology, v. 34, no. 3, p. 76-95.
Moore, S.L., Foord, E.E., Meyer, G.A., and Smith, G.W., 1988b, Geologic map of the northwestern part of the Mescalero Apache Indian Reservation, Otero County, New Mexico: U.S. Geological Survey Map I–1895, scale 1:24,000.
Ingram, R.L., 1954, Terminology for the thickness of stratification and parting units in sedimentary rocks: Geological Society of America Bulletin, v.
65, p. 937–938, Table 2.
Kelley, V.C., 1971, Geology of the Pecos country, southeastern New Mexico: New Mexico Bureau of Mines and Mineral Resources Memoir 24,
78 pp.
Qaovf
Qao2
Munsell Color, 1994 edition, Munsell soil color charts: New Windsor, N.Y., Kollmorgen Corp., Macbeth Division.
Otte, C., 1959, Late Pennsylvanian and early Permian stratigraphy of the northern Sacramento Mountains, Otero County, New Mexico: New
Mexico Bureau of Mines and Mineral Resources Bulletin 50, 111 p. (with plates).
Kelley, V.C., 1972, Geology of the Fort Sumner sheet, New Mexico: New Mexico Bureau of Mines and Mineral Resources, Bulletin 98, 55 pp.
Pray, L.C., 1961, Geology of the Sacramento Mountains escarpment, Otero County, New Mexico: New Mexico Bureau of Mines and Mineral
Resources Bulletin 35, 144 p. (with plates).
King, W.E., and Harder, V.M., 1985, Oil and gas potential of the Tularosa Basin–Otero Platform–Salt Basin graben area, New Mexico and Texas:
New Mexico Bureau of Mines and Mineral Resources Circular 198, 36 p. (with plates).
Raatz, W.D., 2002, A stratigraphic history of the Tularosa basin area, south–central New Mexico: New Mexico Geological Society Guidebook
53, p. 141–157.
Koning, D.J., 1999, Fault segmentation and paleoseismicity of the southern Alamogordo fault, southern Rio Grande rift [M.S. thesis]: Albuquerque,
University of New Mexico, 286 p.
Ritter, J.B., Miller, J.R., Enzel, Y., Howes, S.D., Nadon, G., Grubb, M.D., Hoover, K.A., Olsen, T., Reneau, S.L., Sack, D., Summa, C.L., Taylor, I.,
Touysinhthiphonexay, K.C.N., Yodis, E.G., Schneider, N.P., Ritter, D.F., and Wells, S.G., 1993, Quaternary evolution of Cedar Creek alluvial fan,
Montana: Geomorphology, vol. 8, p. 287–304.
Koning, D.J., 2009, Radiocarbon age control for Sacramento Mountain-derived alluvial fan deposits near Alamogordo, New Mexico, and related
geomorphic and sedimentologic interpretations [abstract for 2009 NMGS Spring Meeting]: New Mexico Geology, v. 31, no. 2, p. 46.
Koning, D.J., Connell, S.D., Pazzaglia, F.J., and McIntosh, W.C., 2002a, Redefinition of the Ancha Formation and Pliocene–Pleistocene deposition
in the Santa Fe embayment, north–central New Mexico: New Mexico Geology, v. 24, no. 3, p. 75–87.
Koning, D.J., Pazzaglia, F., and Smartt, R., 2002, Alluvial fan stratigraphy along the southern Sacramento Mountains, N.M., and inferences regarding late Quaternary paleoclimate, soils, and sedimentation: New Mexico Geological Society Guidebook 53, p. 289–302.
Koning, D. J., Hallett, B., and Shaw, C., 2007, Preliminary geologic map of the Alamogordo North 7.5-minute quadrangle, Otero County, New
Mexico: New Mexico Bureau of Geology and Mineral Resources OF–GM–153, scale 1:24,000.
Scholle, P.A., Goldstein, R.H., and Ulmer-Scholle, D.S., 2007, Classic Upper Paleozoic reefs and bioherms of west Texas and New Mexico: New
Mexico Bureau of Geology and Mineral Resources Open-file Report 504, 174 p.
Smith, G.A., 2000, Recognition and significance of streamflow-dominated piedmont facies in extensional basins: Basin Research, vol. 12, p.
399–411.
Soil Survey Staff, 1992, Keys to Soil Taxonomy: U.S. Department of Agriculture, SMSS Technical Monograph no. 19, 5th edition, 541 p.
Speer, S.W., 1983, Abo Formation, north–central Sacramento Mountains: An onlapping fluvial clastic wedge: in Guidebook for file trip to the Abo
red beds (Permian), central and south–central New Mexico: Roswell Geological Society and the New Mexico Bureau of Mines and Mineral
Resources, p. 54–72.
Koning, D.J., Kempter, K.A., Zeigler, K.E., and Cicoski, C.T., 2011, Preliminary geologic map of the Cub Mountain 7.5-minute quadrangle: New
Mexico Bureau of Geology and Mineral Resources OF–GM–138, scale 1:24,000.
Stearns, C.E., 1953, Tertiary geology of the Galisteo–Tonque area, New Mexico: Geological Society of America Bulletin, v. 64, p. 459–508.
Kuhle, A.J., and Smith, G.A., 2001, Alluvial-slope deposition of the Skull Ridge Member of the Tesuque Formation, Española Basin, New Mexico:
New Mexico Geology, vol. 23, no. 2, p. 30–37.
Tait, D.B., Ahlen, J.L., Gordon, A., Scott, G.L., Motts, W.S., Spitler, M.E., 1962, Artesia Group of New Mexico and west Texas: Bulletin of the American Association of Petroleum Geologists: vol. 46, no. 4, p. 504–517.
Lucas, S.G., and Krainer ,K., 2004, The Red Tanks Member of the Bursum Formation in the Lucero Uplift and regional correlation of the Bursum
Formation in New Mexico: New Mexico Museum of Natural History and Science, Bulletin 25, p. 43–52.
Udden, J.A., 1914, The mechanical composition of clastic sediments: Bulletin of the Geological Society of America, v. 25, p. 655–744.
Qao1
Foord, E.E., and Moore, S.L., 1991, Geology of the Bent Dome, Otero County, New Mexico Geological Society Guidebook 42, p. 171–174.
Gile, L.H., Peterson, F.F., and Grossman, R.B., 1966, Morphological and genetic sequences of carbonate accumulation in desert soils: Soil
Science, v. 101, p. 347–360.
Gile, L.H., Hawley, J.W., and Grossman, R.B., 1981, Soils and geomorphology in the Basin and Range area of Southern New Mexico—Guidebook
to the Desert Project: New Mexico Bureau of Mines and Mineral Resources, Memoir 39, 222 p.
Harbour, R. L, 1970, The Hondo Sandstone Member of the San Andres Limestone of south–central New Mexico : U. S. Geological Survey Professional Paper 700–C, p. 175–182.
Hawley, J.W., and Wilson, W.E., 1965, Quaternary geology of the Winnemucca area, Nevada: University of Nevada, Desert Research Institute,
Technical Report no. 5, 66 p.
Mack, G.H., Dinterman, P.A., 2002, Depositional environments and paleogeography of the Lower Permian (Leonardian) Yeso and correlative
formations in New Mexico: The Mountain Geologist, v. 39, p.75–88.
McManus, C.E.D., and McMillan, N.J., 2002, Subduction or rifting: the Eocene magmas of the Sacramento Mountains, NM: Geological Society
of America Abstracts with Programs, v. 34, no. 6, p. 364.
Waresback, D.B., 1986, The Puye Formation, New Mexico: analysis of a continental rift-filling volcaniclastic alluvial fan sequence [unpublished
M.S. thesis]: Arlington, University of Texas, 225 p.
Sheetflood deposits, reworking eolian sand, overlying fine-grained older alluvial fan deposits—See descriptions for units Qse (above) and
Qaof (below). Qse is less than 2 m thick. Clastic sediment, alluvial sediment, mostly fine-grained. Societal uses: low potential for aggregate
because of thin nature of Qse. Possible residential development.
Sheetflood deposits, reworking eolian fine-grained sediment, overlying gypsum (Holocene)—See descriptions of Qse (above) and Qgy
(below). Sheetflood deposits are probably more than 20 cm thick. Mapped using air photos where surface has a lighter tone and relatively tanner
to redder colors (as opposed to darker, grayer colors corresponding to Qgy) and a higher shrub density. Clastic sediment, alluvial sediment,
mostly fine-grained. Societal uses: very limited.
Tist
Sheetflood and slopewash deposits, reworking eolian sand, with coppice dunes on the surface (middle Holocene to present)—Similar to unit
Qse (described above), but with 7–10% or greater surface coverage by coppice dunes (unit Qec, as described above). Clastic sediment, alluvial
and eolian sediment. Societal uses: low to moderate potential for aggregate. Possible residential development or agricultural potential.
Miller A.K., and Youngquist, W., 1949, American Permian Nautiloids: Geological Society of America Memoir 41, 218 p.
Moore, S. L., Foord, E. E., and Meyer, G. A., 1988a, Geologic and aeromagnetic map of a part of the Mescalero Apache Indian Reservation,
Otero County, New Mexico: U.S. Geological Survey Miscellaneous Investigations Series Map I–1775, scale 1:50,000.
Moore, S.L., Foord, E.E., Meyer, G.A., and Smith, G.W., 1988b, Geologic map of the northwestern part of the Mescalero Apache Indian Reserva-
Samp e a 410715N
Porphyr c rachydac e uppe Eocene o owe O gocene —D kes and s s o a gh g ay po phy y Rock con a ns 5—15% phenoc ys s o
p ag oc ase e dspa b o e ± ho nb ende and da k g een py oxene 1–10 mm ong se n a ne g a ned ma x Un nc udes amph bo e ch s s
on he sou h s de o Coyo e R dge ha a e 1–5 m h ck These s s a e b ack o da k g een med um g a ned and con a n ~ 30% da k g een
e onga ed amph bo e need es 5% p ag oc ase and 5% po ass um e dspa Un a so nc udes a p om nen 5 km ong and 4 m w de NE end ng
d ke be ween Boone D aw and he Th ee R ve s d a nage
Porphyr c rachyandes e m dd e o uppe Eocene —D kes s s and sma acco hs o a gh g ay o g ay po phy y 5—15% phenoc ys s o
p ag oc ase e dspa da k g een py oxene and po ass um e dspa 1–10 mm ong se n a ne g a ned ma x These n us ve bod es may g ade
n o mo e equ g anu a ex u es T d Syen c and sed men a y xeno hs a e oca y p esen Two c oss cu ng d kes n he C aw o d W ndm a ea
gave ow qua y da es o 36 41 ± 0 41 and 36 90 ± 0 51 Ma UTM 411503E 3684169N NAD 27 D kes a e 0 5–8 m w de
Trachybasa m dd e o uppe Eocene —B ack o da k g een ne g a ned n us ons gene a y d kes w h ba e y d sce n b e need es o
p ag oc ase and py oxene No o v ne obse ved n hand ens Th s ock ype y e ded a ow qua y da e o 34 38 ± 0 76 Ma n he Hamm we
a ea UTM 412704E 3687347N NAD27 D kes a e 1–2 m w de
Porphyr c rachy e Eocene —D kes o gh g ay o da k g ay po phy y w h 15–25% p ag oc ase a hs 10–20 mm ong se n an equ g anu a
o ne g a ned ma x o da k g een py oxene and e dspa The p ag oc ase a hs a e o en d s nc y a gned pa a e o he ma g ns o he d ke
D kes 1–4 m w de
Equ granu ar a ka gabbro d or e or syenogabbro syenod or e m dd e o uppe Eocene —L gh g ay o g ay equ g anu a o s gh y
po phy c ne o med um g a ned sa and peppe co o ed d kes s s and acco hs D kes a e 1–7 m w de Phenoc ys s nc ude p ag oc ase
e dspa and py oxene ± kspa ± b o e ± amph bo e These n us ve bod es may g ade n o mo e po phy c ocks T a and o en con a n xeno
hs o syen e D kes o h s compos on cu s s o megac ys c achybasa T m sou h o Coyo e Peak Th ck s s o h s compos on n he no h
eas e n pa s o he map a ea have cumu a e py oxene a he base Th s un nc udes he a ka d o e o G an e We wh ch s a g een sh g ay
equ g anu a ne o med um g a ned sa and peppe co o ed s w h p ag oc ase e dspa py oxene and b o e phenoc ys s exposed sou h o
G an e We a ong Tempo a C eek nea he moun a n on A 40A /39A age o 38 07 ± 0 64 Ma was de e m ned o b o e om h s n us on
Th s s has py oxene ch cumu a e phase nea he base and s abou 30–35 m h ck A h ck s on he no h s de o Ca Moun a n e u ned a
40
A /39A age o 36 21 ± 0 30 Ma on b o e Th s un a so nc udes b ack o da k g een med um o coa se g a ned 1–3 m h ck s s oca ed on
he sou hwes s de o Ca Moun a n Rock con a ns subequa amoun s o b ack py oxene and p ag oc ase as we as spa se app e g een py oxene
The coa se gabb o g ades upwa d n o a ne o med um g a ned equ g anu a gabb o Exposed ock may deve op a s ong va n sh T d d kes
a e 0 5–7 m w de
n rus ons w h megracrys c a gned p ag oc ase m dd e o uppe Eocene —A d s nc ve n us on gene a y ng d kes ha con a ns 5–25%
euhed a p ag oc ase a hs 5–20 mm ong The g oundmass s gh g ay o da k g ay equ g anu a and composed o dark green pyroxene and
e dspar ha are 0 2–0 4 mm ong The p ag oc ase a hs a e o en d s nc y a gned pa a e o he ma g ns o he d ke No h o Th ee R ve s
a d ke o h s compos on s c osscu by a T d d ke T mp d kes a e 1–4 m w de
Megacrys c a ka gabbro d or e or syenogabbro–syenod or e m dd e o uppe Eocene —G ay o gh g ay o g een sh g ay po phy c
s s d kes and acco hs Th s ock con a ns 5–25% megac ys s o embayed sche mak c subhed a o euhed a ho nb ende o g een py oxene
ha a e up o 2–4 cm ong Loca y b o e phenoc ys s a e p esen The g oundmass cons s s o p ag oc ase w h 15–25% amph bo e and/o py ox
ene g a n s ze s 0 2–0 5 mm ess common y o 1 0 mm These n us ves oca y have xeno hs o p nk coa se g a ned syen e po phy y w h
a ge phenoc ys s o o hoc ase e dspa and ho nb ende Exposed ock common y deve ops a ve y s ong va n sh Many acco hs and s s
cons s o h s ock ype nc ud ng he p om nen N–S dge a he Th ee R ve s Pe og yph s e Th s dge was da ed a 36 32 ± 0 35 Ma Dowe
e a 2002 and was ca ed a achybasa s by McLemo e 2002 A s no h o Boone D aw gave a da e o 3795 ± 0 91 Ma UTM
410998E 3687059N NAD27 The n us on a K y Sp ng s 3717 ± 0 33 Ma UTM 405032E 3680799N NAD27 D kes a e 1–5 m w de
Syen e– rachy e m dd e Eocene —P nk med um g a ned equ g anu a s s and d kes composed o po ass um e dspa p ag oc ase e dspa
py oxene and b o e S s a e <3m h ck and d kes a e ess han 4 m w de Th s un nc udes he syen e o Tempo a C eek wh ch s a an o p nk
equ g anu a o po phy c s ock exposed n he no heas co ne o he map a ea Moo e e a 1988 no h o Tempo a C eek and s add ng
he wes e n bounda y o he Mesca e o Apache nd an Rese va on The mos common phenoc ys s n he s ock a e po ass um e dspa
p ag oc ase e dspa and c nopy oxene Some phases o h s s ock have amph bo e Moo e e a 1988 wh e o he s have spa se phenoc ys s
o qua z D kes w h a ge a gned p ag oc ase phenoc ys s T mp c osscu h s s ock
Sheetflood deposits, reworking eolian sand, with coppice dunes on the surface, overlying younger alluvium—See descriptions of Qsec
(above) and Qay (below). Clastic sediment, alluvial and eolian sediment. Societal uses: low to moderate potential for aggregate. Possible
residential development or agricultural potential.
NEOGENE EXTRUS VE ROCKS OF THE S ERRA BLANCA VOLCAN C F ELD
Sheetflood deposits, reworking eolian sand, with coppice dunes on the surface, overlying older alluvium—See descriptions of Qsec (above)
and Qao (below). Clastic sediment, alluvial and eolian sediment. Societal uses: low to moderate potential for aggregate. Possible residential
development or agricultural potential.
Th s un appears o over e an uncon o m y deve oped a abou he s a g aph c eve o he Buck Pas u e Tu wh ch s no exposed n h s pa c
u a a ea nc udes he 28 2 o 28 8 Ma ackass Moun a n Fo ma on and he 28 8 o 34 3 Lopez Sp ng Fo ma on
Sheetflood deposits, reworking eolian sand, with coppice dunes on the surface, overlying the middle subunit of older alluvium—See
descriptions of Qsec (above) and Qao2 (below).
Thick gypsum accumulation (middle to upper Holocene)—Yellowish-white to pink (7.5YR 7/4) to very pale brown (10YR 7/4) gypsum that has
been subjected to multiple dissolution and precipitation events. These processes have formed a hard crust >10 cm thick on the surface of this deposit. Underneath, gypsum is generally moderately consolidated, massive or in tabular beds (up to 40 cm thick), and consists of silt and very fine- to
coarse-grained sand size, platy crystals (mostly very fine to fine-grained) that are subangular to angular and well-sorted. Locally, this gypsum sand
is planar-laminated to low-angle cross-laminated. Very thin cross-beds, with 30 cm thick foresets, locally seen near base of the deposit. Gypsum
sand may include subordinate plagioclase and quartz, and when dry has a “fluffy” feel. Surface of unit may have microkarst topography where
exposed on slope shoulders. Interpreted to be a relic of an eastward, eolian-driven expansion of the White Sands dune field in the middle to upper
Holocene. Deposit thickens westward and is inferred to interfinger eastward with unit Qay2 (this transitional zone was mapped as Qgyay2).
Deposit overlies Qaof, probably over an unconformity. Lower meter of deposit commonly grades into more siliclastic sand that is clean, fine- to
coarse-grained, and planar-laminated to very thinly bedded (included in unit Qgy). In the southwestern part of the compilation map, the surface of
this unit is marked by minor to abundant sinkholes and similar collapse features, whose locations and extents are shown on the map. These are
probably due to dissolution of gypsum beds several meters below the surface (in underlying Qaof). Flat surfaces are commonly overlain by a
younger veneer of pale brown (10YR 6/3) silt and very fine- to fine-grained sand a few 10s of centimeters thick (unit Qse). Where this surficial
veneer manifests itself on air photos, then this unit is mapped as Qse/Qgy (see above). Unit is also mapped where gypsum forms a hardpan in
low areas. 0.5–4 m thick. Precipitate and eolian sediment, gypsum. Societal uses: potential for gypsum mining.
Gradation-interfingering between gypsum and younger basin-floor deposits (middle to upper Holocene)—Mapped where unit Qgy transitions eastward into unit Qay2. This gradational unit contains about 1/3–2/3 gypsum compared to 2/3–1/3 sediment of Qay2. Surface sediment
commonly consists of pinkish, gypsiferous silt and very fine- to medium-grained sand. Probably 1–3 m-thick. Eolian and clastic sediment. Societal
uses: possible residential development.
GODFREY H LLS GROUP
Tgjvs
Tgjta
Tgjb
Tgjpt
Tgl
Tglta
Travertine (lower Pleistocene? to upper Pliocene?)—Laminated to massive calcium carbonate. On Round Mountain, 10–15 m thick travertine sits
on 3 m of carbonate cemented gravel. Travertine deposits southwest of Mescalero are associated with faults and consist of 1–2 m thick beds of
carbonate overlying the Yeso Formation. Carbonate cemented gravels (with 1 to 2 cm thick CaCO3 rinds) are exposed north of Mescalero. In this
area, the carbonate cemented gravels are covered by younger fans and are being exhumed by down-cutting along the Rio Tularosa. Golden
brown travertine at UTM 419746E 3671012N (NAD27) coats bedding planes in the San Andres Limestone on the escarpment north of Tularosa
Creek. Calcium carbonate. Societal uses: limited.
Spring deposit (Pleistocene)—Banded barite and goethite deposited along a fault (two deposits, UTM 407146E 3681126N and 406950E
3681195N [NAD 27]) 1–2 m thick.
Recent alluvium (0–200 yrs old)—Well-stratified sand, gravel, and silt deposited by arroyo fluvial activity and sheetflooding in modern or historical
times. Sand and gravel characterize this unit in mountain drainages and the proximal portions of alluvial fans, whereas sand, silt, and clay dominate
in distal portions of the alluvial fans. In addition to occupying active arroyo bottoms, this unit commonly comprises relatively small (generally less
than 500 m across) depositional lobes at the mouths of incised channels and extends downslope from these lobes as thin, tabular bodies. Historical deposits of this unit may be present outside the rim of recently incised arroyos. Color of non-gravel fraction varies according to source area,
but generally ranges from reddish-brown in the south to grayish-brown, light grayish-brown, gray, and pale brown in the middle and north. In gravelly sediment, bar and swale topography is present (up to 150 cm relief) and gravel consists of pebbles, cobbles, and boulders. Gravel is subrounded (minor subangular) and very poorly to poorly sorted. Clast composition reflects the source area, and may include sandstone, siltstone, intrusive,
or volcanic rock types. Bedding in gravelly sediment is very thin to thick, horizontal-planar to lenticular to ribbon-like, concave-up channel-fills
(locally cross-stratified). Sand is very fine- to very coarse-grained; mostly medium- to very coarse-grained and moderately to very poorly sorted on
proximate-medial alluvial fans and within the mountains. Sand is mostly very fine- to medium-grained and moderately- to well-sorted on the distal
fan. It is on the distal fan that silt (plus clay) can be abundant. Bed forms in sandy sediment are horizontal-planar to cross-stratified and laminated
to medium-thick; locally internally massive. Historical alluvium away from rocky topographic highs is generally well-stratified sand and subordinate
gravel with a sharp, relatively flat basalt contact. Stratification in sandy or silty sediment is mostly laminated to very thin, horizontal-planar to wavy
to cross-stratified (commonly low-angle foresets or ripple-marked). Surface is sparsely to moderately vegetated. No observable soil development,
desert pavement, nor clast varnish—but an erosional gravel lag may locally be present. The modern to historic age assignment is based on the
presence of post-Native American artifacts in the sediment—including tires, railroad-related coal, and various types of anthrogenic rubbish. This age
interpretation is consistent with the youthful surface of the unit and its geomorphic position (i.e., lying in low topographic areas, or adjacent to or in
active arroyos or intra-fan lobes). Deposit is loose and less than 3 m thick. Clastic sediment, alluvial sediment, mostly coarse-grained. Societal
uses: aggregate at large gully-mouth fan sites.
Recent alluvium with subordinate youngest subunit of younger alluvium—See descriptions for units Qar (above) and Qay3 (below). Clastic
sediment, alluvial sediment, mostly coarse-grained. Societal uses: aggregate.
Younger alluvial fan lithostratigraphic unit (Holocene)—A pale brown (10YR 6/3), light yellowish-brown (10YR 6/4), very pale brown (10YR
7/3–4), pink (7.5YR 7–3/4), grayish (10YR 7/1–2 and 6/1–2), or light brown reddish-yellow (7.5YR 6/4–6) deposit that lacks a well-developed
top soil and whose surface is commonly eroded. Although this unit is gravelly near rocky topographic highs, gravel is subequal to subordinate in
most areas, including alluvial fans downstream of the fan apex. East of the Alamogordo fault, this unit occupies the floors of valleys. Commonly
differentiated into three allostratigraphic subunits that are described below: Qay3, Qay2 (including Qay2u), and Qay1 (from youngest to oldest).
Where extensively present south of the Rio Tularosa in the Sacramento Mountains (southeastern map area), this unit generally consists of structureless, pale reddish-brown, fine-grained sediment (silt, sand, and clay) interbedded with thin, discontinuous beds of clast-supported, angular to
subrounded gravel composed largely of Permian limestone. On alluvial slopes and footwall valleys near Three Rivers, as well as alluvial fans
between Three Rivers and the Rio Tularosa, this unit mostly consists of very fine- to medium-grained sand and clayey-silty fine sand interbedded with
coarse channel-fills of medium- to very coarse-grained sand, pebbly sand, and sandy pebbles. Much of the non-gravelly sediment (especially the
clayey-silty fine sand) is internally massive and weakly modified by pedogenesis (characterized by moderate pedogenic development and Stage
I gypsum ± calcium carbonate accumulation). Within the fine sand, there is typically scattered pebbles and minor, scattered medium to very coarser-grained sand. In the northern map area, surface clasts are subangular to subrounded and composed of igneous rocks and subordinate sedimentary rocks. Greater than 80% of this unit is middle to upper Holocene in age. Moderately to well consolidated and 1–6(?) m thick. Clastic
sediment, alluvial sediment. Societal uses: agriculture and residential development.
Youngest allostratigraphic subunit of younger alluvium (upper Holocene)—Well-stratified sand, silty fine sand, and variable gravel. Near
Temporal Creek and south of the Rio Tularosa, this unit is subsumed into Qay2. Generally occupies arroyo back-fills (generally too small to be
mapped) or sheet-like deposits near recent arroyos or channels (most commonly what is mapped). Unconformably overlies, or is inset into, the
middle subunit of younger alluvium (Qay2). Gravelly beds are more common on the footwall of the Alamogordo fault and in the proximal alluvial
fans. On the distal alluvial fans, gravel interbeds are very minor and the unit is primarily a sand, silty very fine- to fine-grained sand, and silt.
In sandy or silty sediment, stratification is generally horizontal-planar laminated to thinly bedded, with minor wavy laminations or thin cross-bed sets.
Sand is pale brown to very pale brown (10YR 6–7/3) or light yellowish-brown (10YR 6/4), very fine- to very coarse-grained, subrounded to subangular (medium to very coarse sand tends to be more subrounded, very fine to fine sand is generally subangular), well to poorly sorted, and
composed of quartz, subordinate feldspar, and minor volcanic + lithic grains. Surface has very poor soil development, bar and swale topography
less than 50 cm tall, and exhibits no desert pavement development or clast varnishing. This unit may be difficult to differentiated from historic alluvium (Qar), as both appear to have aggraded relatively quickly (at a given location) and lack buried soils (hence the well-developed stratification).
However, in aerial imagery the bar and swale topography on this unit's surface is more vague and subdued, compared with that on Qar. This unit
was deposited in the late Holocene following the widespread middle Holocene aggradation event associated with Qay2. The landscape in the
upper Holocene was characterized by landscape instability, with widespread erosion punctuated by brief, localized back-filling events (Koning,
2009). This unit correlates to the younger Organ alluvium in the Desert Project (Gile et al., 1981). Loose to weakly consolidated. Up to 2 m thick.
Clastic sediment, alluvial sediment. Societal uses: agriculture and residential development.
Twt
Twtr
Twh
Middle subunit of younger alluvium, consisting of pebbly sand capping subdued topographic highs (middle to upper Holocene)—Sandy
upper Qay2 deposits, with minor pebble lenses, underlying subdued topographic highs mantled by an erosional gravel lag. The slightly coarser
texture of the sediment has inhibited erosion, creating topographic highs whose surfaces are 20–150 cm higher than surrounding, eroded Qay2
surfaces. To the north, the sand is yellowish-brown to light yellowish-brown (10YR 5–6/4). To the south, the sand is reddish-brown (5YR 5/3–4),
pale brown (10YR 6/3), or very pale brown (10YR 7/3–4). Sand is very fine- to very coarse-grained (mostly fine- to medium-grained) and similar
to Qay2 sand. Surface gravel consists of very fine to very coarse pebbles and 0–10% cobbles that are subrounded to subangular, generally non- to weakly varnished, and generally lacking coats of calcium carbonate (trace to 10% of clasts exhibit distinctive, thick calcium
carbonate coats on their undersides), that form a weak to moderate pavement (generally greater than 10% clast surface cover). Surface
lacks original bar and swale relief and generally exhibits no to very sparse (<15%) patches of strong gypsum accumulation. The clast armor of the
desert pavement allowed preservation of elongated, slightly higher surfaces that probable coincide with paleo-channels. These highs are generally not as dissected as those underlain by Qfo. Age control for this unit is similar to that discussed for Qay2. Less than 2 m thick. Clastic sediment,
alluvial sediment, mostly coarse-grained. Societal uses: agriculture and residential development.
Older allostratigraphic unit of younger alluvium (lower Holocene)—This unit is only mapped on the proximal alluvial fans, where it is distinguished by a gravelly surface that is generally topographically higher than the surface of Qay2. Clasts on the Qay1 surface are less varnished
than the Qao surface. Sediment exposure is limited, but overall seems to be somewhat coarser-grained than Qay2. Only one exposure found of
this unit, which shows Qay2 inset into Qay1 and Qay1 composed of fine-grained sand with minor (10–15%), narrow, very thin- to thick-bedded,
coarse channel-fills. Sediment is slightly redder than adjoining Qay2 sediment, with colors ranging from reddish-brown to pinkish-white (5YR 5/4
and 7.5YR 8/2). Sediment is internally massive and has experienced cumulic soil development marked by gypsum accumulation (7–10% gypsum
filaments). Sand has 1–30% clay–silt and is very fine- to fine-grained, subangular, well-sorted, and gypsiferous. Sand in channel-fills is reddish-gray
to reddish-brown (5YR 5/2–3), subrounded to subangular, and poorly sorted. Surface is mantled (>50% clast density) by very fine to very coarse
pebbles and minor fine to coarse cobbles. These clasts are non- to moderately varnished. Surface clasts generally lack thick calcium carbonate
coats, are poorly sorted, subangular to subrounded, and composed mostly of limestone. Surface is marked by gypsum accumulation comparable
to a Stage II to II+ carbonate morphology. Desert pavement is moderately to well-developed. Less than 10% strong gypsum accumulation is apparent on the surface. Surface lacks bar and swale topography and is undissectecd. The surface of Qay2 is lower (by ~1 m) or level with this surface.
The aforementioned exposure of Qay1 shows this unit overlying a calcic horizon similar to that seen developed on the Qai deposit. Moderately
to well consolidated and 1.5–2.5 m thick.
Waresback, D.B., and Turbeville, B.N., 1990, Evolution of a Pliocene–Pleistocene volcanogenic alluvial fan: the Puye Formation, Jemez Mountains,
New Mexico: Geological Society of America Bulletin, v. 102, p. 298–314.
Qp
Qtg
Trachy e o rachyandes e ows o he Jackass Moun a n Forma on owe O gocene —L gh o da k g ay ne g a ned ava w h a achy c
ex u e and con o ed p a y ow o a on The un s composed o a se es o h n ows 1–10 m h ck w h basa sco aceous b ecc a and ves cu a
ow ops w h e onga ed ves c es Red o ye ow a e a on o he ow b eaks s common 40A /39A ages o 28 59 ± 0 05 Ma and 28 53 ± 0 03
Ma we e ob a ned om san d ne n a u bed n he un Base s pa eocanyons op e oded 50 m h ck
Brecc a ed porphyr c rachy e o he Jackass Moun a n Forma on owe O gocene —A erna ng gh gray rachyandes e w h ew
phenos <5% p ag oc ase and pyroxene n erbedded w h mono ho og c brecc a w h subround o angu ar c as s n a gh gray ma r x
Base s a and op s e oded n C aw o d Canyon achy c ows b acke he b ecc a un 60–140 m h ck
Pa sades Tu Member o he Jackass Moun a n Forma on owe O gocene —C o m ng we ded u w h p onounced eu ax c o a on and
aphony wea he ng Con a ns < 2% h c agmen s composed o achyandes e and achy e avas Phenoc ys s nc ude p ag oc ase san d ne
py oxene magne e and spa se b o e and ho nb ende The u s gene a y c ys a poo bu he mo e we ded n e va s a e 15–20% phenoc ys s
40
A /39A ages o 28 67 ± 0 07 Ma and 28 66 ± 0 08 Ma we e ob a ned om san d ne n he u Geochem ca y h s u s a achy e Bo h he
op and bo om o h s un s a r y a 25–90 m h ck
Lopez Spr ng Forma on und v ded owe O gocene — n e va o h n o h ck 1–10 m d scon nuous achy e po phy c achyandes e
b o e achydac e and achybasa ows comp ex y n e ca a ed w h vo can c as c sed men s Some exposu es o vo can c as c sed men a e
dom na ed by b o e bea ng achydac e c as s A achydac e cobb e om h s vo can c as c n e va on he Oscu a quad ang e o he no heas
y e ded a b o e 40A / 39A da e o 30 04 ± 0 2 Ma p ov d ng a max mum age o he sed men Th ck nd v dua ows o achyandes e a e shown
a Tg a Mos o he achyandes e ows a e da k g ay o edd sh b own po phy y w h phenoc ys s o p ag oc ase and py oxene n p aces he
ows a e sepa a ed by ne g a ned ed s s one The avas a e pe vas ve y a e ed w h zeo o e n he ves c es One h ck ow n h s o ma on s
exposed n C aw o d Canyon The C aw o d Canyon ow s a ne g a ned suga y ex u ed ava w h con o ed p a y ow o a on Phenoc ys s
nc ude py oxene The base o he C aw o d Canyon ow s cove ed o s pa eova eys cu on Tg sed men s and ava ows The op o he C aw
o d Canyon ow s egu a and n p aces pa eocanyons ed w h sed men cu deep y n o he un The C aw o d Canyon ow un p nches ou
o he eas The Lopez Sp ng Fo ma on s 90–100 m and he C aw o d Canyon ow s 30–40 m h ck
Three R vers Forma on und v ded uppe Eocene poss b y owe O gocene —From younges o o des nc udes he Buck Pas ure Doub e
D amond Argen na Spr ng Tu Tay or We and Ra esnake Canyon members On y he Ra esnake Canyon Membe s p ese ved n h s
a ea
Ra esnake Member o he Three R vers Forma on uppe Eocene —Da k g ay po phy c achyandes e w h phenoc ys s o p ag oc ase and
py oxene p ag oc ase s he dom nan phenoc ys The avas a e va ab y c ys a poo 5% o c ys a ch 30% Modes amoun s o vo can c as c
ma e a p ese ved be ween he ows Hyd omagma c depos s w h sco aceous andes c ap and bombs a e oca ed a UTM 410424E
3692929N and 410256E 3692999N NAD 27 30 m o Ra esnake Membe exposed n he quad ang e
Hog Pen Forma on m dd e? o uppe Eocene —G een o ed vo can c as c o vo can c un con a n ng ow b ecc a and ava ows The ow
b ecc a c as s and ava ows a e composed p ma y o po phy c basa c achyandes e o achybasa w h phenoc ys s o py oxene and
p ag oc ase he py oxene phenoc ys s a e usua y >5 mm and a e no ceab e on wea he ed su aces 40A / 39A ho nb ende da es o 36 57 ±
0 21 o 3701 ± 0 10 Ma we e de e m ned o h s un n a eas no h and eas o he quad ang e Th s un nc udes d s nc ve ho nb ende achydac
e ows ha appea o be w h n he Hog Pen Fo ma on These da k g ay achydac e porphyr es con a n phenoc ys s o p nk a b zed e dspa
py oxene and ho nb ende Two ows sepa a ed by a ow b eak a e p esen on he knob sou h o he Th ee R ve s Road The younge ow d ec y
ove es he o de ow no vo can c as c sed men s a e p ese ved be ween he ows The op o he un s no exposed n h s a ea The base s s
on Sande s Canyon and he ava appea s o have n e ac ed w h we sed men s a one oca y Abou 20 m o he un s exposed
PALEOGENE SED MENTARY ROCKS
Ts
Tc
Sanders Canyon Forma
eas o C aw o d W ndm
Hog Pen Fo ma on ows
s gn can n e nge ng o
Kc
Kclt
Kg
Km
Kmd
Kth
Kml
Kd
^m
Cub Moun a n Forma on owe o m dd e Eocene —Ye ow an sands one n e ca a ed w h ma oon b ck ed and da k g ay muds one and
ye ow g een g een g ay and ed sands one Mud c as cong omera es occu h ghe n he sec on Sands one s med um o coa se g a ned and
s poo y o we so ed w h angu a sand g a ns o qua z e dspa o en a e ed o c ay and b ack h c agmen s Bedd ng s abu a o
c oss bedded o pp e am na ed Nodu a mes one was obse ved a UTM 408650 3688032 NAD 27 and des cca on c acks we e no ed a
UTM 409507 3688048 NAD 27 The d scon o mab e base s oca ed us above a mo ed pa eoso deve oped on cong ome a c sands one
n he op o he C evasse Canyon he op s no exposed The h ckness o he un s poo y cons a ned due o poo exposu e and comp ex
s uc u e The Cub Moun a n Fo ma on s 370–570 m h ck no h o h s a ea
Crevasse Canyon Forma on Uppe C e aceous Con ac an No h Ame can S age —F uv a s a a cons s ng o n e bedded sands one chan
ne s and ne g a ned muds one ch oodp a n depos s ve y m no coa beds Sands one channe
comp exes may be up o 6 m h ck a e
we cemen ed and o m edges Co o s o he sands one ange om pa e ye ow go den gh o ve g ay pa e o ve ve y pa e b own and gh
b own sh g ay Beds a e gene a y angen a o ough c oss s a ed am na ed o ve y h n o h n beds w h subo d na e o subequa ho zon
a p ana bedd ng am na ed o h n Sands one s mos y ne o med um g a ned sub ounded o subangu a we so ed and composed o
qua z e dspa and 5–10% h c g a ns sands one was c ass ed as sub h c o suba kos c by A ke 1983 F oodp a n depos s cons s o
muds one and ve y ne o ne g a ned sands one and s y sands one w h oca ve y m no coa beds Muds one s pa e ye ow o gh g ay o
g ay o gh o ve g ay n co o and oca y ss e Ca bonaceous sha e s da k g ay o b ack n co o Base o un no we exposed on h s quad an
g e bu no ed o be g ada ona n A ke 1983 Nea he op o h s un exposed no h o he Th ee R ve s Pe og yph s e s a ~110 m h ck
n e va cons s ng o edge o m ng sands one ha s angen a c oss s a ed o ho zon a p ana bedded bedd ng s am na ed o h n The sand
n hese edges s wh e o gh g ay med um o coa se g a ned sub ounded o subangu a we so ed and composed o qua z w h 1–5% ma cs
and che y h c g a ns A d s nc ve ~5 6 m h ck pa eoso has deve oped on he op o he C evasse Canyon Fo ma on cons s s o ne o
coa se g a ned sands one ha s n e na y mass ve ke y b o u ba ed and con a ns ~10% pu p sh manganese o on ox de conc e ons The
con ac be ween Kc and Kc s con o mab e Th ckness no we cons a ned due o va ab y n d ps bu on he sca e o 550–700 m
Lower rans ona par o Crevasse Canyon Forma on Uppe C e aceous owe Con ac an No h Ame can S age — n e bedded sands one
and sha e n e p e ed o e ec ma g na ma ne sho e ace o esho e agoona pond and de a c and uv a depos ona env onmen s A ke
1983 Un con o mab y ove es he uppe mos sho e ace sands one assoc a ed w h un Kgs One o mo e coa beds a e p esen nea he base
o he depos n e bedded w h muds one and ve y ne o ne g a ned sands ones h s s ass gned o he D co Membe o he C evasse Canyon
Fo ma on Above h s coa s ano he coa sen ng upwa d eg ess ve sequence ke hose desc bed o Kgs see be ow he nea sho e sands one
n h s n e va s co e a ed w h he Da on Sands one o he C evasse Canyon Fo ma on The uppe con ac o h s un s p aced a h ghes go den
b own h gh y ca ca eous ve y ne o ne g a ned s y sands one bed con a n ng ma ne o b ack sh wa e oss s h s bed s gene a y 30–100
cm h ck Th s go den b own oss e ous sands one s s e a ve y con nuous h oughou he s udy a ea and common y o ms edges Age om
Hook 2010 and Hook and Cobban 2012 50–150 m h ck
Ga up Sands one Uppe C e aceous owe Con ac an No h Ame can S age — n e bedded nea sho e sands ones and deepe wa e sha es
ha d sp ay coa sen ng upwa d eg ess ve sequences n good exposu es o he no h G eg Mack 2010 persona commun ca on Kon ng e
a 2011 These eg ess ve sequences a e ve y ke y p esen n h s quad ang e as we a hough no we exposed G ay o ye ow ma ne sha es
a e ound a he base o he eg ess ve sequence These g ade upwa d n o owe sho e ace sands ones ha a e common y ve y h n y o h ck y
abu a bedded mos y ve y h n o h n beds beds a e n e na y mass ve oca y b o u ba ed and bu owed o ho zon a p ana am na ed o
hummocky am na ed Sand s ve y ne o ne g a ned oca y s y ca ca eous sub ounded o subangu a we so ed and composed o qua z
w h 1–10% h c g a ns Co o s ange om gh g ay o o ve ye ow o pa e o ve o gh ye ow sh b own o pa e b own o pa e ye ow Uppe
sho e ace sands ones a e s gh y coa se mos y ne o med um g a ned and n ve y h n o h ck abu a beds ha a e n e na y ho zon a p a
na am na ed o c oss s a ed angen a ow ang e o ough c oss am na ed o ve y h n y bedded o ese s a e up o 20 cm h ck Sand s
pa e ye ow o gh g ay o pa e b own o wh e sub ounded o subangu a we so ed and composed o qua z w h m no e dspa ? and
1–10% h c g a ns The sands one common y wea he s o a ye ow go den co o The Ga up Sands one g ada ona y ove es he Mancos Sha e
Km o Kmd and s con o mab y ove a n by he C evasse Canyon Fo ma on Kc Oys e beds a e e a ve y common and nc ude a d agnos c
spec es es c ed o he owe Con ac an F em ngos ea e egans Hook 2010 170–180 m h ck
Mancos Sha e und v ded Uppe C e aceous m dd e Cenoman an o owes Con c an No h Ame can S age —F ss e sha e ha s p ana o
wavy am na ed Me amo phosed o b ack o g ay a g e ad acen o acco hs S a a hos s nume ous s s and acco hs emp acemen o a ge
n us ons has o ded and de o med he ad o n ng Mancos Sha e Th s und v ded un nc udes he owe ongue o he Mancos Sha e Km see
be ow he D C oss Tongue Membe o he Mancos Sha e Kmd and he n e ven ng pa e ye ow o wh e ne g a ned sho e ace sands o he
T es He manos Fo ma on Th n mes one and ben on e beds a e oca y p esen n he owe ongue o he Mancos Sha e Km Un grada ona
y over es he Dako a Sands one and g ada ona y unde es he Ga up Sands one Age ass gnmen s om Hook and Cobban 2012
C oss sec on A–A and we da a nd ca e a h ckness o 165–270 m
Mancos Sha e D Cross Tongue Member Uppe C e aceous m dd e Tu on an o owes Con ac an S age —Da k g ay o g een sh g ay o pa e
ye ow ss e sha e s y sha e s s one and c ays one S gh o no e e vescence n hyd och o c ac d T ace o common s de e and/o ca c um
ca bona e cemen ed conc e ons ha a e up o 0 5 m n d ame e occu abou 20 m be ow he con ac w h ove y ng Ga up Sands one Un
e odes ead y Toward op o un g een o b own beds o s s one and ve y ne o ne g a ned sands one become p og ess ve y mo e common
Sha e s me amo phosed o a b ack o g ay a g e mmed a e y ad acen o acco hs o d kes a d ng n he p ese va on o noceram d oss s
Un s g ada ona y ove a n by he Ga up Sands one and unde a n by he T es He manos Fo ma on 70–100 m h ck
Tres Hermanos Forma on uppe C e aceous m dd e Tu on an S age —A ongue o ve y ne o med um g a ned mos y ne g a ned sands one
w h n he Mancos Sha e oca y con a n ng she deb s and che agmen s Co o s ange om pa e ye ow o gh g ay wea he ng o b own
sh ye ow ve y pa e b own o pa e ye ow Sands one s oca y n e bedded w h subo d na e ye ow sha e beds n p aces enses o b o u ba ed
ye ow sh b own sands one occu ha nc ude oys e b va ve and ammon e emnan s Loca y bu ows a e obse ved A p ano convex med
um s zed bbed oys e ca ed Came eo opha be ap ca a con ms hos a g aph c co e a ons w h he T es He manos Fo ma on Hook and
Cobban 2011 10–60 m h ck h nn ng o he no heas Th ckness 15–21 m owa d he no h
Mancos Sha e ower ongue Uppe C e aceous m dd e Cenoman an o owe Tu on an No h Ame can S age —F ss e ca ca eous sha e ha
s p ana o wavy am na ed co o s ange om g ay o gh g ay o gh o ve g ay o gh g een sh g ay Th n beds o mes one B dge C eek
L mes one Membe and ben on e a e oca y exposed L mes one occu s abou 5 m above he base and n he B dge C eek n e va a ew 10s
o me e s h ghe up sec on These ma ne depos s we e mapped as he owe pa o he R o Sa ado Tongue o he Mancos Sha e by Moo e e
a 1988 us eas o he map a ea Un g ada ona y ove es he Dako a Sands one 85–110 m h ck
Dako a Sands one Uppe C e aceous —Wh e c oss s a ed sands one ha s n e ca a ed w h gh g ay o da k g ay sha e and gh gray
s s one o very ne sands one n s uppe ha Sands one s angen a o ough c oss s a ed am na ed o ve y h n beds o n med um o
h ck abu a beds ha a e n e na y c oss s a ed o ho zon a p ana am na ed T ough c oss s a ca on nd ca es a no heas pa eo ow d ec
on Wood agmen s a e oca y obse ved Sand g a ns a e mos y ne o med um g a ned sub ounded o subangu a we so ed and a qua z
a en e Loca y coa se o ve y coa se sand g a ns a e p esen composed o che qua o qua z e M no beds o pebb y sands one occu
nea he base o he un c as s nc ude sub ounded o ounded qua z che and qua z e D s nc ve cy nd ca Oph omo pha nodosa bu ows
a e abundan a he op o he Dako a Sands one Sands one s g ada ona y ove a n by he Mancos Sha e Km The base o he un s scou ed
Loca y he Dako a Sands one s pa eo va eys ha a e up o 6 m deep hese pa eo va ey s cons s o subequa sands one and edd sh b own
muds one Sands one wea he s o o m a pu p sh b own va n sh App ox ma e y 90 m h ck
Moenkop Forma on Uppe T ass c —Redd sh b own o weak ed o p nk sh g ay c oss s a ed ne o coa se g a ned sands one mos y ne
o med um g a ned Va y ng p opo ons o weak ed o edd sh b own sha e c ays one and s s one dec eas ng n abundance o he sou heas
Sands one s common y ough o angen a c oss s a ed am na ed o ve y h n y bedded 10–15 cm h ck o ese s and oca y pp e am na
ed The sand gra ns are subangu ar o rounded modera e y o we sor ed and a h c aren e nc ud ng muscov e and h c ragmen s
Cong ome a c sands ones w h pebb es o che qua z e and qua z a e p esen n a ew oca es The uppe and owe con ac s a e d scon
o mab e The uv a Moenkop Fo ma on scou ed channe s n o he unde y ng G aybu g Fo ma on o he A es a G oup 10–50 m h ck
s
poss b y 70 m h ck nea Th ee R ve s bu h ns o 10 m o he sou heas
PALEOZO C SED MENTARY ROCKS
Pag
Ps
Younger alluvium with subordinate recent alluvium (upper Holocene to present)—See descriptions for Qay and Qar above. Clastic sediment,
alluvial sediment. Societal uses: limited because of higher flooding potential; possible aggregate or agriculture.
Grayburg Forma on Ar es a Group Pe m an —O ange o edd sh b own o gh edd sh b own ve y ne o ne g a ned sands one and
s y c ayey ve y ne o ne g a ned sands one on y m no s s one and sha e Bedd ng s mos y ve y h n o h ck and abu a bu ve y h n o
med um en cu a beds a e oca y p esen M no gh g ay o gh g een sh g ay educ on spo s 0 5–2 0 mm Sands one s subangu a o ound
ed mos y sub ounded we so ed and composed p edom na e y o qua z no h c g a ns and e dspa seems o be ve y m no n e ca a ed
gypsum beds a e mo e common up sec on The gypsum s absen ~10 m be ow he op The gypsum o ms med um o h ck abu a beds ha a e
common y o ded o de o med Base w h unde y ng Fou m e D aw Membe o he San And es L mes one s sha p and has ag g ave The op s
e oded and scou ed by he Moenkop Fo ma on No oss s p ese ved Th s un s ass gned o he G aybu g Fo ma on because o ho og c
cha ac e s cs h ckness and he ac ha h ghe o ma ons o he A es a G oup ex end p og ess ve y sho e d s ances om he deepes pa s o
he De awa e Bas n o he sou h sou heas Ke ey 1971 and 1972 We d d no ecogn ze he Queen Fo ma on o he A es a G oup because
we d d no no e sca e ed a ge ounded os ed qua z g a ns nd ca ve o he uppe pa o h s o ma on Ta e a 1962 O ang sh co o ne
ex u e and qua z a en e compos on and educ on spo s se ve o d e en a e h s un om he ove y ng Moenkop Fo ma on 90–110 m
based on pe o eum we da a nea Th ee R ve s
San Andres Forma on Pe m an —Ke ey 1971 ecogn zed h ee membe s o he San And es Fo ma on n sou h cen a New Mex co The
n e ca a ed mes one and gypsum un n he uppe pa o he San And es Fo ma on be ongs o he Fou m e D aw Membe o Ke ey 1971 The
m dd e pa o he un he Bonney Canyon Membe s oss e ous h n h ck bedded da k g ay mes one The owe pa o he depos he R o
Bon o Membe s composed o med um o h ck bedded da k g ay oss e ous mes one go den an do om e and h n beds o ye ow s s one
and gypsum Ha bou 1971 desc bed a sands one bed w h n he R o Bon o Membe app ox ma e y 30 m above he base o he mes one ha
he named he Hondo Sands one Membe o he San And es Fo ma on n h s a ea on y he Fou m e D aw he Hondo Sands one and he R o
Bon o membe s a e p esen The San And es Fo ma on s 240–250 m h ck based on pe o eum we da a no h o he map bounda y
Psf
Younger subunit of younger alluvium, with subordinate recent alluvium—See descriptions for units Qay2 and Qar above. This unit is common
in the bottom of mountain canyons where Qar is too narrow to differentiate at this map scale. Clastic sediment, alluvial sediment, mostly
coarse-grained. Societal uses: limited because of higher flooding potential.
Younger alluvium and subordinate older alluvium, undivided (middle to upper Pleistocene and Holocene)—See descriptions of Qay (above)
and Qao (below). Clastic sediment, alluvial sediment. Societal uses: possible agricultural potential.
Intermediate alluvium (uppermost Pleistocene)—Light brown to light reddish-brown (5–7.5YR 6/4), clayey-silty very fine- to fine-grained sand
interbedded with lenses of gravel and coarse sand, commonly grading downward into sandy gravel. Variable (but generally minor), scattered
coarser sand and pebbles may be present. Lower sandy gravel is in very thin to medium, lenticular to tabular beds; gravel are clast-supported,
subrounded, and poorly sorted; matrix is pale brown (10YR 6/3), very fine- to very coarse-grained sand that is subrounded, poorly sorted, and
contains abundant lithic grains. A nodular, Stage II to II+ calcic horizon has developed on top of the unit. The calcium carbonate nodules in this
horizon are commonly 0.5–2.0 cm. This calcic horizon is about 10–70 cm thick. Unit is inset into Qao2 and Qao1 and generally overlain by unit
Qay. It commonly fills topographic lows. Only subaerially exposed in a few places because it is generally overlain by unit Qay. Unit is interpreted
to be associated with an interval of limited aggradation and back-filling of arroyos in the latest Pleistocene, which is supported by a radiocarbon
age of 22,580 ± 140 ka from an exposure along Salinas Draw. 1–3 m(?) thick.
Psh
Older alluvium (lower to upper Pleistocene)—Undifferentiated older alluvium recognized by its relatively red hues and abundant gypsum.
Gypsum-cemented rhizoliths are commonly observed. Finer sediment is generally massive or in thick, vague beds, and interbedded with various
proportions of gravelly channel-fills. Unit is commonly subdivided into three allostratigraphic units that are described in detail below: Qao3, Qao2,
and Qao1. Another allostratigraphic unit (Qaovf) is mapped on modern valley floors west of Tularosa, and a fine-grained lithostratigraphic unit
(Qaof) is differentiated on the distal areas of alluvial fans. Moderately to well consolidated and greater than 8 m thick.
Psr
Py
Pa
Pb
Fine-grained, older alluvial fan deposits of intercalated gypsiferous clay, sand, silt, and gypsum on the distal alluvial fans (lower? to upper
Pleistocene)—Intercalated clayey fine sand, clay, silt, very fine- to fine-grained sand, and gypsum. Colors range from reddish-brown to light
reddish-brown (5YR 4–6/4) to pink (5YR 7/3 to 7.5YR 7/4) to reddish-yellow (7.5YR 6/6) and yellowish-red (5YR 4/6). Very thin to thick, tabular
beds that are internally massive and commonly hard; locally planar-laminated. Local calcium carbonate in nodules or thin to thick beds. Sand is
very fine- to coarse-grained (mostly very fine- to medium-grained), moderately to well-sorted, and consists of various proportions of quartz, calcite,
gypsum, feldspar, and minor lithic grains (including granite). Locally, there are minor, meter-scale-thick, sandy pebble to cobble beds interbedded
in the typically fine sediment of this unit. Radiocarbon age of 27,010 ± 160 obtained from gastropod shells from the upper part of this deposit (silt
and clay beds), 1.1–1.3 below Qgy. Base of unit not defined. West of Tularosa, unit is exposed or underlies units Qgy or Qay2. Surface of unit is
comparable to that of Qao. Total basin-floor sediment is several hundred meters thick before Paleozoic bedrock is encountered. Clastic sediment,
alluvial sediment, mostly fine-grained. Societal uses: residential development; high gypsic content of top soil impedes agriculture; buried soils
and variable gravel and clay content reduces aggregate quality.
Older alluvial fan deposits occupying the floors of modern valleys on the distal parts of the alluvial fans, locally capped by a veneer of
recent alluvium (middle to upper Pleistocene to uppermost Holocene)—This unit was applied to valley floors incised below unit Qgy in the southwestern map area. There, lack of exposure commonly presented difficulty in recognizing thin, discontinuous, recent deposits (Qar) versus
fine-grained, older alluvial fan deposits (Qaof). Thus, these units were generally combined on these valley floors. Latest Holocene sediment is light
yellowish-brown (2.5Y 6/3), internally massive, well-sorted, and consists of silty sand composed of gypsum, calcite, quartz(?), and plagioclase).
Clastic sediment, alluvial sediment, mostly fine-grained. Societal uses: very limited because of high flooding potential.
Younger allostratigraphic subunit of older alluvium inset into older deposits (probably upper Pleistocene)—Generally a sandy gravel and
pebbly sand with variable (but commonly subordinate) interbeds of strong brown to reddish-yellow to light brown (7.5YR 5–6/6; 7.5YR 6/4),
gypsiferous sand. The sand is mostly very fine- to fine-grained and contains variable amounts of scattered pebbles (pebbles may also be in thin
lenses) and coarser sand. Differentiated east of the Alamogordo fault, this unit generally occupies paleo-valleys that are inset into older alluvium
(Qao2). Unit locally fines upward from a sandy gravel at its base to clayey very fine- to fine-grained sand at its top. The gravelly sediment exhibits
very thin to medium, horizontal-planar to lenticular beds. Gravel is clast-supported, rounded to subangular (mostly subrounded), poorly sorted, and
includes pebbles with lesser cobbles and boulders. Matrix in gravelly sediment is pale brown to light brownish-gray (10YR 6/2-3), highly gypsiferous, and composed of very fine- to very coarse-grained sand (mostly coarse- to very coarse-grained) that is subrounded, poorly sorted, and
contains abundant lithic grains; beds are very thin to thick and lenticular to tabular. Fine-grained sediment is internally massive and has gypsum
filaments. Locally, sediment extends hundreds of meters away from paleovalleys as a tabular deposit up to a few meters thick. Where unit is not
covered by younger, surficial deposits (e.g. Qse), a strong gypsic-calcic horizon is developed on the surface of the unit (comparable to a Stage
II+ or III morphology in a strictly calcic soil), surface clast varnish is relatively well-developed, and there is a well-developed desert pavement.
Where this unit has been buried or recently exhumed, a nodular, Stage II to II+ calcic horizon may be developed on top of the unit (10–70 cm
thick). Unit partially correlates with Qao on the alluvial fans. No direct age control but inferred to be late Pleistocene. Weakly to moderately
consolidated. South of the Three Rivers drainage, this unit is notably gravelly and 4–14 m-thick. Clastic sediment, alluvial sediment, mostly
coarse-grained. Societal uses: aggregate.
Middle allostratigraphic subunit of older alluvium (middle to upper Pleistocene)—Reddish, gypsiferous, relatively fine-grained sediment
interbedded with coarse channel-fills of sand and gravel. Only differentiated east of the Alamogordo fault. Scoured base of deposit appears to
lie several meters below the base of unit Qao1. Unit locally occupies discrete paleovalleys whose tops are at the same height as adjoining Qao2;
sediment in these paleovalleys generally consists of clast-supported, sandy gravel in very thin to thin, horizontal-planar beds. Unit includes relatively
coarse sediment on the immediate footwall of the Alamogordo fault north of Three Rivers. Color of fine sediment is pink to light brown (7.5YR
6-7/3–4), brown to reddish-yellow (7.5YR 5/4–6/6), light reddish-brown (5YR 6/4), yellowish-red to reddish-yellow (5YR 5–6/6), or brown to
dark grayish-brown (10YR 5/3–4/2). The fine sediment is composed of very fine- to medium-grained sand and clayey-silty fine sand, with minor
medium- to very coarse-grained sand and pebbles (as scattered grains/clasts or in very thin to medium lenses). Very fine- to medium-grained sand
is subangular to subrounded and consists of quartz, 5–15%? feldspar, and 15% volcanic grains. Coarse to very coarse sand is subrounded to angular (mostly subrounded to subangular) and consist of lithic fragments (mostly igneous fragments to the north and mostly Paleozoic sedimentary
detritus to the south). The fine-grained sediment is internally massive, well consolidated, commonly bioturbated, and variably affected by pedogenesis (i.e., illuviated clay and ped development), with common rhizoliths cemented by gypsum and local calcium carbonate nodules. Less commonly,
the fine sediment is in medium to thick, tabular beds. Between Rio Tularosa and Temporal Creek, fine-grained sediment dominates the unit near the
mountain-front, where it is interpreted to have been brought in by eolian processes before being fluvially reworked. Intercalated gravelly channel-fills are up to 1 m thick and contain pebbles with minor cobbles and local boulders. These channel-fills are clast- to matrix-supported (mostly
clast-supported) and in thin to thick, tabular to lenticular beds. Gravel is commonly imbricated, subrounded to subangular, poorly to moderately
sorted, and composed of limestone, sandstone, and igneous clasts (the latter dominating to the north). Sand in the coarse channel fills is generally
horizontal-planar laminated to very thinly bedded, light brown to reddish-yellow (7.5YR 6/4–6) to light yellowish-brown (2.5Y 6/3) to light
gray-grayish-brown (10YR 6/3–5/2 and 10YR 6–7/2), very fine to very coarse-grained (mostly medium- to very coarse-grained), subrounded to
subangular, and moderately to poorly sorted. This channel-fill sand contains up to 3% clay (as sand-size rains or as clay films) and gypsum crystals
may occupy up to 2% of the volume. Near rocky topographic highs, matrix-supported debris flows are interbedded in clast-supported, stream-flow
sediment. The matrix of these gravelly debris flows consist of pink (7.5YR 7/3–4), very fine- to medium-grained sand with subordinate coarser sand.
Where not covered by Qse or Qsec, the surface of Qao2 is characterized by a moderately to well developed desert pavement (containing
well-varnished clasts) and strong gypsum accumulations (comparable to a Stage III morphology in a calcic soil or else a petrogypsic horizon).
Several different erosion surfaces have developed on this unit, which are most obvious immediately adjacent to the Alamogordo fault. Unit probably correlates with much of the older alluvial fan deposits west of the Alamogordo fault (Qao). No direct age control but inferred to be middle to
late Pleistocene. Well consolidated and locally cemented. 3 m to greater than 15 m thick. Clastic sediment, alluvial sediment. Societal uses:
residential development. Low to moderate aggregate potential because of high content of gypsum and fine-grained sediment—moderate to
high aggregate potential in Three Rivers area because of coarser texture there. Low agricultural potential because of gypsic top soil.
Older allostratigraphic subunit of older alluvium (lower to middle Pleistocene)—Generally a sandy gravel with subordinate to subequal
interbeds of clayey-silty, gypsiferous, very fine- to fine-grained sand containing minor medium to very coarse sand. Finer-grained sediment increases
progressively south of the Three Rivers drainage. Gravel contains pebbles with variable cobbles, locally with minor boulders. Gravel are subrounded to subangular, poorly to moderately sorted, and composed of limestone, intermediate to mafic intrusive rocks, and subordinate sandstone (limestone clasts dominate to the south and igneous clasts dominate to the north). Color of sand ranges from pale brown to very pale brown (10YR
6–8/3), pink (5–7.5YR 7/3), or light yellowish-brown to light brown (10–7.5YR 6/4). Sand is very fine to very coarse-grained, subrounded to
subangular, and moderately to poorly sorted. Very fine- to medium-grained sand is composed mostly of subangular to angular gypsum grains,
whereas coarser sand is composed of lithic grains. Base of deposit generally lies several meters above the base of unit Qao2. Surface of unit
typically lies >3 m above the Qao2 surface. Prevalent petrogypsic horizon developed on its surface and very strongly varnished surface
clasts. Moderately consolidated, highly gypsiferous, and variably cemented. Unit is locally strongly cemented near Salinas Draw. 5–25 m-thick.
Clastic sediment, alluvial sediment, mostly coarse-grained. Societal uses: residential development, aggregate potential, low agricultural potential because of gypsic top soil and gravelly texture.
Pediment gravel, undivided (upper Pleistocene)—Thin sandy gravel, generally gypsiferous, that overlies pediment surfaces in the lower part of the
Sacramento Mountains. Surfaces are relatively smooth and exhibit well-varnished desert pavements. Underlying soil generally marked by gypsum
accumulation comparable to a Stage II to III calcium carbonate morphology. Less than 1 m thick. Clastic sediment, alluvial sediment, mostly
coarse-grained. Societal uses: aggregate.
Terrace gravel (Pleistocene)—Gravelly terrace deposits found alongside, and paralleling, modern drainages, including the Three Rivers drainage.
The bases of the terrace deposits (straths) are greater than 2 m above these drainages. The terrace deposit is generally poorly exposed.
Gravel are subrounded to subangular, poorly sorted, and consists of pebbles with subordinate cobbles and 1–10% boulders. Spallation of
exposed clasts results in abundant subangular-angular gravel on the surface. The gravel is clast- to matrix-supported and composed predominately
of intermediate-mafic igneous rocks, with subordinate Paleozoic–Mesozoic sedimentary clasts (mostly sandstone and limestone). The gravel is
interbedded with varying proportions of sand. Sand is very fine- to very coarse-grained, pale brown to very pale brown (10YR 6–8/3; 10YR 7/4),
subangular to subrounded, and moderately to poorly sorted. In at least some deposits, a significant proportion of the sand is composed of gypsum
grains. Deposit also includes fine-grained sediment that is internally massive, brownish–yellow (10YR 6/6), locally clayey-silty, and dominated by
very fine- to fine-grained sand (much of which is gypsum grains); the fine sediment locally contains gypsum-cemented rhizoliths. Surfaces are flat,
on m dd e Eocene — nc udes pu p sh ma oon vo can c as c b ecc a n uded by a NE s k ng d ke abou 2 km sou h
Ma oon s and g ay sands one w h b ack ma c g a ns a e exposed us be ow he d s nc ve ho nb ende achydac e
The owe pa o he Sande s Canyon s umped w h he Cub Moun a n n h s a ea because o poo exposu es and
he un s Vo can c as c b ecc a <10 m h ck
MESOZO C SED MENTARY ROCKS
Youngest subunit of younger alluvium with subordinate recent alluvium (upper Holocene to present)—See descriptions for Qay3 and Qar
above. Clastic sediment, alluvial sediment, mostly coarse-grained. Societal uses: limited because of higher flooding potential; possible aggregate.
Middle allostratigraphic subunit of younger alluvium (middle to upper Holocene)—This subunit underlies the majority of alluvial fan surfaces in
the study area, where it commonly consists of very fine- to medium-grained sand and clayey-silty fine sand—both are interbedded with very thin to
thick, lenticular beds of medium- to very coarse-grained sand, pebbly sand, and sandy pebbles. The proportion of coarse channel-fills progressively decreases westward away from the mountain front. Qay2 also extends into footwall valleys and mountain drainages. Sediment color is generally
pale brown to brown (10YR 5–6/3; 7.5YR 5/4), light yellowish-brown (10YR 6/4), light brown (7.5YR 6/3-4), or pink (7.5YR 7/3–4), with lower
strata commonly being redder. Subunit is generally reddish-brown (5YR 4–5/3–4) where it includes notable amounts of Abo Formation detritus.
Sediment mostly consists of clay, silt, and very fine- to fine-grained sand in the distal part of alluvial fans. However, sediment contains <10% silt-clay
and is dominated by sand and gravel (mostly pebbles and cobbles, with minor boulders) in mountain drainages and the proximal parts of alluvial
fans deposited by small to medium, relatively steep mountain-front drainages. Coarse channel-fills are up to 1 m thick (generally in very thin to
medium, lenticular to tabular beds) and consist of pebbly sand to sandy pebbles-cobbles. In the medial parts of the alluvial fans, sediment typically
consists of a very fine- to medium-grained sand and silty-clayey sand interbedded with pebbly channel-fills. The fine sediment is generally massive
or in thick, vague beds that may be bioturbated or horizontal-planar laminated. Fine sand is mostly moderately to well-sorted, subangular to
subrounded, and composed of quartz, subordinate feldspar, and minor lithic + mafic grains. The finer-grained sediment commonly includes 1–20%,
scattered medium- to very coarse-grained sand and 1–15%, scattered pebbles scattered in a finer-sand matrix (probably via bioturbation).
Most fine-grained sediment intervals are overprinted by a weak, cumulic, buried soil(s); these buried soil horizons commonly exhibit moderate ped
development, weak (Stage I or less) calcic + gypsic soil horizons (characterized by scattered filaments), and no to very weak clay illuviation (mostly as clay bridges). Minor calcium carbonate nodules may be found in lower strata. Much of the fine sediment was likely blown in and then
reworked by sheetflooding during monsoonal thunderstorms. Overall, the finer texture helps in differentiating this subunit from gravelly Qay1 deposits. Subunit may grade laterally up-slope into Qse deposits, but is differentiated from Qse by the presence of local medium to thick, coarse channel-fills.
Vo can c as c sed men o he Jackass Moun a n Forma on owe o uppe O gocene — nc udes an uppe un ha s a he ero h c ands de
depos w h a wh e ashy ma x ha con a ns a ge 1–5 m angu a bou de s o po phy c achyandes e Pa sades Tu and achyandes e
b ecc a 5–15 m h ck The owe un s a sandy ma x suppo ed ca bona e cemen ed cong ome a e ha con a ns uppe achy e ava as he
dom na e c as O he c as s nc ude o de avas and ow banded hyo e The c as s a e angu a and <0 5 m n d ame e Basa cong ome a e has
a ge bou de s o po phy c achyandes e w h abundan p ag oc ase phenoc ys s A h n oca zed u depos w h a basa ye ow b own ash
ow u con a n ng a e ed pum ce and ~15% phenoc ys s o san d ne and qua z unde a n by a b ack v c u w h 35% phenoc ys s o san d ne
qua z and spa se b o e w h ne g a ned edd sh an h c agmen s s p esen a he basa con ac a UTM 409692E 3692960N NAD27
The u y e ded an 40Ar/39Ar age o 28 23 ± 0 06 Ma The basa v c u s 30 cm h ck uppe u s 60 cm h ck 30 m h ck
WALKER GROUP
Recent alluvium with subordinate middle subunit of younger alluvium—See descriptions for units Qar (above) and Qay2 (below). Clastic
sediment, alluvial sediment, mostly coarse-grained. Societal uses: aggregate.
TERRACE AND PEDIMENT DEPOSITS
Wentworth, C.K., 1922, A scale of grade and class terms for clastic sediments: Journal of Geology, v. 30, p. 377–392.
McMillan, N.J., 2004, Magmatic record of Laramide subduction and the transition to Tertiary extension: Upper Cretaceous through Eocene
igneous rocks of New Mexico: New Mexico Geological Society Special Publication 11, p. 249–270.
Hooke, R.L., 1967, Processes on arid-region alluvial fans, Journal of Geology, vol. 75, p. 438–460.
Hook, S.C., 2010, Flemingostrea elegans, n. sp: guide fossil to marine, lower Coniacian (upper Cretaceous) strata of central New Mexico: New
Mexico Geology, v. 32, no. 2, p. 35–57.
Tid
This unit correlates to the Jornada II alluvium in the Desert Project, which is inferred to be upper middle to upper Pleistocene in age (Gile et al.,
1981, Table 9). Radiocarbon dates presented in Koning et al. (2002b) support a Pleistocene age for Qao. Unit almost certainly represents more
than one episode of alluvial aggradation. Clastic sediment, alluvial sediment. Societal uses: residential development; high gypsic content of top
soil impedes agriculture; buried soils and variable gravel and clay content reduces aggregate quality.
Birkeland, P.W., 1999, Soils and geomorphology: New York, Oxford University Press, 430 p.
Blair, T.C., 1999, Sedimentary processes and facies of the waterlaid Anvil Springs Canyon alluvial fan, Death Valley, California: Sedimentology,
vol. 46, p. 913–940.
Titp
Py
Pa
Koning, D.J., Connell, S.D., Pazzaglia, F.J., and McIntosh, W.C., 2002a, Redefinition of the Ancha Formation and Pliocene–Pleistocene deposition
in the Santa Fe embayment, north–central New Mexico: New Mexico Geology, v. 24, no. 3, p. 75–87.
Pb
Pb
Psr
Py
Py
Kml
Kelley, V.C., 1972, Geology of the Fort Sumner sheet, New Mexico: New Mexico Bureau of Mines and Mineral Resources, Bulletin 98, 55 pp.
TRm
Pag
Psf
Psr
QTbf
Blair, T.C., and McPherson, J.G., 1994b, Alluvial fan processes and forms, in Abrahams, D., and Parsons, A.J., eds., Geomorphology of Desert
Environments: London, Chapman and Hall, p. 354–402.
Pa
Pa
Kd
Koning, D.J., 2009, Radiocarbon age control for Sacramento Mountain-derived alluvial fan deposits near Alamogordo, New Mexico, and related
geomorphic and sedimentologic interpretations [abstract for 2009 NMGS Spring Meeting]: New Mexico Geology, v. 31, no. 2, p. 46.
Pa
Pa
Psf
Psr
Kd
Py
Py
Pa
Psf Psf
Psr
Kd
Kd
TRm TRm
Pag Pag
Py
Compton, R.R., 1985, Geology 1,000
in the field: New York, John Wiley & Sons, Inc., 398 p.
Py
Psf
Psr
Py
Kd
Kd
Kd
TRm
TRm
Pag
Pag
Pag
Pag
Psf
Kd
Py
Py
Pa
Pa
Psf
Psr
Pag
Blair, T.C., and McPherson, J.G., 1994a, Alluvial fans and their natural distinction from rivers based on morphology, hydraulic processes, sedimentary processes, and facies assemblages: Journal of Sedimentary Research, vol. A64, p. 450–489.
Pag Titd
Pag
Py
Py
Psr
Pa
10,000
Kd
TRm
Pag
Psr
Psr
Py
Psf
Horse Camp fault zone
Tita
Kth
Tita
Pa
Py
0
Tid
Kml
Kd
TRm
Pag
Py
Psr
Mineral Survey,
Tita
J-J’ cross section
TRm
TRm
2,500
meters ASL
7,000
6,000
50,000
Pag
Tita
vol. 46, p. 913–940.
30,000
South
9,000
feet ASL
8,000
Titb
Tim
Unit underlies topographically high surfaces dissected by gullies (0.5–1.0 m-deep) that have been partly back-filled by Qay deposits. The surface
is smooth and lacks original bar and swale topography. Much of the surface is covered by thin (generally less than 30 cm thick), younger sheetflood deposits (Qse). A thin mantle of younger eolian deposits (Qec and Qsec) is common in the Three Rivers area. Where not mantled by these
younger deposits, the surface manifests a weak to well-developed desert pavement—with moderately to strongly varnished surface clasts exhibiting
calcium carbonate rinds (up to 65% clast coverage). Surface gravel include very fine to very coarse pebbles and 8–10% fine cobbles. A Stage
II+ to III calcic horizon has locally developed on this unit on the Temporal Creek alluvial fan, but generally the unit exhibits a top soil with strong
gypsic + calcic horizon(s) (comparable to a Stage II+ to III morphology in a calcic soil). In areas where the deposit has been stripped, pedogenic
gypsum horizons have been exposed and weathered to form a hard gypsum crust at the surface. In areas of poor exposure on the alluvial fans,
Qao assignment was based on the observation of 10% or greater strong gypsum indications (such as gypsum crusts) on the surface. Base of unit
not defined, but alluvial fan sediment filling the basin here is generally several hundred meters thick.
2,000
Kelley, V.C., 1971, Geology of the Pecos country, southeastern New Mexico: New Mexico Bureau of Mines and Mineral Resources Memoir
24,
meters ASL
78 pp.
Pa
Pag
Tita
20,000
Tita
Sheetflood deposits, reworking eolian sand, overlying middle subunit of older alluvium—Only differentiated where Qse is inferred to be
30–200 cm thick (it is not more than 200 cm thick). See descriptions for units Qse (above) and Qao (below). Clastic sediment, alluvial sediment,
mostly fine-grained. Societal uses: low potential for aggregate because of thin nature of Qse. Possible residential development.
This unit is left undivided on alluvial fans, where it commonly underlies slight topographic highs. There, it consists of interbedded sandy gravel,
gravelly sand, sand, and clayey very fine- to fine-grained sand. Gravel layers are of variable thickness and consist of clast-supported pebbles with
minor cobbles and boulders; clasts are subrounded to subangular and poorly to moderately sorted. Gravel composition varies according to source
area, but typically includes variable limestone, sandstone, and igneous rocks. Clast imbrication indicates a westward flow direction. Bedding within
a gravel layer is tabular to lenticular and up to ~50 cm thick (mostly very thin to thinly bedded). Some beds have abundant cobbles and boulders
(i.e., well-graded pebbles through boulders) in a light brown (7.5YR 6/3–4) to reddish-yellow (7.5YR 6/6), clayey fine sand matrix—these are
debris flows. Clayey-silty, very fine- to fine-grained sand on the alluvial fans is light brown to reddish-yellow to reddish-brown (7.5YR 6/3–6), highly
gypsiferous, and consists of thick, tabular beds; sediment has 10–20% medium- to very coarse-grained sand and 1–10% scattered pebbles; 1–2%
very thin to thin, pebble to cobble lenses are found locally at the base of individual beds. Fine sediment is redder where it contains Abo Formation
detritus (2.5YR 5/4). Fine sediment is very well consolidated and has 10–30% gypsum. Sandy beds are reddish-brown to light brown to brown;
sand is very fine- to very coarse-grained, subangular to subrounded, and moderately to poorly sorted; up to 50% of sand grains may be composed
of gypsum. Fine and sandy beds commonly contain gypsum-cemented rhizoliths or nodules. Sand grains and gravel clasts are commonly covered
by clay coats.
North
Titb
undivided Mesozoic rocks
10,000
Hawley, J.W., and Wilson, W.E., 1965, Quaternary geology of the Winnemucca area, Nevada: University of Nevada, Desert Research Institute,
Technical Report no. 5, 66 p.
Titd
2,000
No vertical exaggeration
90,000
Arkell, B.W., 1983, Geology and coal resources of the Cub Mountain area, Sierra Blanca coal field, New Mexico [Masters Thesis]: Socorro,
NM, New Mexico Institute of Mining and Technology, 104 p.
5000
Pag
upper basin-fill unit, coarse-grained Plio-Pleist?)
Pag
Psf
Psr Psr
4500
Psf
Psr
lower Soils
basin-fill as
unit, a
fine-grained
Birkeland, P.W., Machette,? M.N., and Haller, K.M., 1991,
tool for applied Quaternary
geology:
and
Psf
Psr Utah Geological
Psf
4000
lower basin-fill unit, coarse-grained
Psr
?
Py
PsrPsf
Py
PsrPsf
lower basin-fill unit
3500
a division of the Utah Department
of
Natural
Resources,
Miscellaneous
Publication
91–3,
63
p.B
Py
basin fill (Santa Fe Group)
Py
Psr
3000
Pa
Psr
Pa
Py
2500
Py
undivided Paleozoic rocks
Py
Py
Py
Pb
2000
Birkeland, P.W., 1999, Soils and geomorphology: New York, Oxford University Press, 430 p. PaPb
Pa
1500
Pa
IPh
PaPa
Pa
1000
IPb
Pb
500
Blair, T.C., 1999, Sedimentary processes and facies of the waterlaid AnvilPbSprings
Canyon
alluvial
fan,
Death
Valley,
California:
Pb
IPg Pb
M
Pb
0
Pb
3,000
0
80,000
Hooke, R.L., 1967, Processes on arid-region alluvial fans, Journal of Geology, vol. 75, p. 438–460.
Psf
Psf
lower basin-fill unit, fine-grained
1,000
Harbour, R. L, 1970, The Hondo Sandstone Member of the San Andres Limestone of south–central New Mexico : U. S. Geological Survey Professional Paper 700–C, p. 175–182.
0
Bauer, P.W. and Lozinsky, R.P., 1991, The Bent dome - part of a major Paleozoic uplift in southern New Mexico: New Mexico Geological Society
Guidebook 42, p. 175–182.
upper basin-fill unit, coarse-grained
Qao
500
Allen, M.S., and Foord, E.E., 1991, Geological, geochemical and isotopic characteristics of the Lincoln County porphyry belt, New Mexico:
implications for regional tectonics and mineral deposits: New Mexico Geological Society Guidebook 42, pp. 97–102.
Desal Test Well No. 8
SEO T-71
SEO T-1900
40,000
Abo Fm.
Gile, L.H., Peterson, F.F., and Grossman, R.B., 1966, Morphological and genetic sequences of carbonate accumulation in desert soils: Soil
1,500
Science, v. 101, p. 347–360.
Cambrian–Silurian carbonates and sandstone
Cross section line
30,000
base of cs interval in well is interpreted at 385 ft depth)
T-1797 S-7 (south; projected across probable fault;
20,000
2,000
meters ASL
Bliss
Alkalic mafic sills
undivided Proterozoic
TB-006 (T-25AA)
TB-007 (T-4656)
Cross section line
Cross section line & TB-046 (T-25A)
T-1002
T-3418
T-3390
C'
T-4394
South
T-18
E
5,000
feet ASL
4,000
?
10,000
Yeso Formation
Foord, E.E., and Moore,Permian
S.L., 1991,
Geology of the Bent Dome, Cambrian
Otero County,Yeso
New
Fm. Mexico Geological Society Guidebook 42, p. 171–174.
Proterozoic
diorite
probable normal faults
basin fill (Santa Fe Group)
undivided Mesozoic rocks
?
NE
Permian Bursum Formation
?
?
inferred inversion of a Laramide reverse fault
0
?
?
1,000
Qayo
Qai
Compton, R.R., 1985, Geology in the field: New York, John Wiley & Sons, Inc., 398D'p.
Permian Abo Formation
T-1797 S-7 (north; projected across probable fault)
undivided Permian to Cambrian sedimentary rocks
2,000
0
T–1382
T–796
T–2845
T–4656
T–25A T–2000
T–3418
T–25AA T–4792
Meeks
upper basin-fill unit, cser
gravelly sediment
upper basin-fill unit, finer
3,000
0
T–4971
T–67
T–4394
4,000
Qayr
Bull, W.B., 1977, The alluvial fan environment: Progress in Physical Geography, vol. 1, p. 222–270.
T–1002
T–18
Cross section X–X'
Cross section Y–Y'
T–15
T–1606
T–4514
T–1973
T–3334
T–4689
T–3390
T–2940
T–2827
T–1651 & 1653
T–2903 T–2987
T–1663 & 4992
T–2951, 2926 & 5073
T–30 T–2928 & 4252
T–2088
nine wells
T–5672
T–2643
T–1963
T–5015
T–1158 & 4690
T–2049
gravel beds
T–3717
T–4876
T–5687
T–5104
5,000
T–4932
T–5065
T–5048
7,000
feet ASL
6,000
T–2420 & 1426
T–1814
T–4027, 3180 & 2923
T–3151 & 3714
D
SW
Titd
This unit is inferred to represent limited aggradation close to the mountain-front in the early Holocene. It disconformably or conformably overlies
Qai. The best age control for this limited aggradation comes from a radiocarbon date at the mouth of Mule Canyon fan, which returned an age
of 8.75 ± 0.07 ka (Koning, 1999; Koning et al., 2002b). Clastic sediment, alluvial sediment, mostly coarse-grained. Societal uses: agriculture
and residential development; limited potential for aggregate.
Qay2r
Bull, W.B., 1972, Recognition of alluvial-fan deposits in the stratigraphic record, in Rigby, J.K., and Hamblin, W.K., eds., Recognition of ancient
sedimentary environments: Society of Economic Paleontologists and Mineralogists Special Publication 16, p. 63–83.
0
Qay1
Bauer, P.W. and Lozinsky, R.P., 1991, The Bent dome - part of a major Paleozoic uplift in southern New Mexico: New Mexico Geological Society
Guidebook 42, p. 175–182.
W
E
7000
6500
6000
5500
5000
4500
4000
3500
3000
2500
2000
1500
1000
500
0
Rhyodac e O gocene —L gh g ay NE s k ng d ke w h phenoc ys s o qua z and b o e ha cu s a megac ys c s
3687045E y e ded a da e o 2727 ± 0 17 Ma 2–3 m w de
Timp
Most of this unit aggraded between 6–3 ka (Koning, 2009). This aggradation was followed by widespread erosion punctuated by brief, localized
back-filling events (Koning, 2009). Post-3 ka, localized deposits are difficult to distinguish from the sediment associated with the 6–3 ka aggradation; thus, these deposits are generally grouped together in the middle and southern parts of the compilation map. This unit correlates to the Organ
alluvium in the Desert Project, which has been assigned an age of 7–1 ka (Gile et al., 1981). Sediment, alluvial sediment, mostly fine-grained.
Societal uses: agriculture and residential development.
B'
B
7,000
feet ASL
6,000
Tir
Sheetflood deposits, reworking eolian sand, overlying older alluvium—Only differentiated where Qse is inferred to be >30 cm thick. See
descriptions for units Qse (above) and Qao (below). Near Three Rivers, the Qse unit consists of light brown (7.5YR 6/4), clean, very fine- to medium-grained sand, with very minor to minor coarse-very coarse and pebbles. Surface may also have minor coppice dunes in the Three Rivers
area. Qse is less than 2 m thick. Clastic sediment, alluvial sediment, mostly fine-grained. Societal uses: low potential for aggregate because of
thin nature of Qse. Possible residential development.
The surface of this unit is commonly eroded, resulting in weakly developed topsoils and an erosional lag of unvarnished to weakly varnished
pebbles overlying finer-grained deposits. Bar and swale relief is non-existent to very subdued (less than 30 cm relief and likely occurring on late
Holocene deposits). Desert pavements do not tend to have well-developed Av peds, and surface clasts exhibit no to slight varnish. Topsoil development is characterized by ped development together with minor gypsum ± calcium carbonate precipitation. Gypsum and calcium carbonate are
present as filaments (1–15% of surface area) or disseminated; clasts are commonly totally covered by a "dusting" of calcium carbonate or have
thicker (0.1–0.2 mm-thick), partial calcium carbonate coats—comparable to a Stage I calcium carbonate morphology (Gile et al., 1966). Generally, no reddening is observed. In the Three Rivers area, a thin, quartz-rich, very fine- to fine-grained sand, surficial layer is found on non- or weakly
eroded surfaces—probably brought in by eolian processes and then fluvially reworked by sheetflooding. Qay2 unconformably overlies Qao and
Qai, and seems to be inset into Qay1. Moderately to well consolidated and 1–6(?) m thick.
IPb
TD: 9360 ft depth
Sheetflood and slopewash deposits, reworking eolian sand (middle Holocene to present)—Very fine- to medium-grained sand and clayey-silty
fine sand (generally less than 25% fines, but locally as much as 50%). Scattered within this sand may be trace–20% coarse- to very coarse-grained
sand and trace–15% pebbles (probably via bioturbation). Unit commonly covers high-level surfaces and mantles slopes at the headwaters of small
drainages, where the deposit commonly grades laterally into younger alluvium (Qay). Unit exhibits a wide range of colors: mostly pale brown
(10YR 6/3), light brown to brown (7.5YR 5–6/3-4), or pink to very pale brown (7.5–10YR 7/3–4). The sediment is commonly internally massive
and bioturbated, with local weak, cumulic soil development characterized by ped development and minor gyspusm + calcium carbonate accumulation, generally as filaments (comparable to a Stage I carbonate morphology). In places, the sediment is highly gypsiferous and may even form
a petrogypsic crust on the surface. Locally there are minor coarse channel-fills (generally in very thin to thin lenticular beds) consisting of pebbly
sand to sandy pebbles. Sand is subrounded to subangular, moderately- to well-sorted, and composed of quartz, minor feldspar, and 5–15% lithic
and mafic grains. Composition varies with local source area. Coppice dunes cover <10% of the surface and are 20–100 cm tall. Surface is sandy,
commonly has a sparse erosional lag gravel, and exhibits weak to no desert pavement development. Development of the top soil is relatively weak,
with no reddening, no to very minor clay illuviation, and only minor gypsum accumulation (equivalent to a Stage I morphology in a calcic soil).
Loose to moderately consolidated. Interpreted to have formed by sheetfloods reworking previously deposited surficial eolian sediment. 0.2–5 m
thick. Clastic sediment, alluvial sediment, mostly fine-grained. Societal uses: agriculture, residential development, and moderate potential for
aggregate.
In the proximal alluvial fans and mountain drainages, gravelly beds are up to 50 cm thick and lenticular to tabular. Gravel is commonly clast-supported and imbricated, and composed of pebbles, cobbles, and minor (1–15%) boulders. Sandy beds are laminated to very thin to medium and
horizontal-planar to lenticular. Sand is grayish-brown to light brownish-gray (10YR 5-6/2), very fine- to very coarse-grained, subrounded to subangular, and generally poorly sorted.
Pa
Pa
Pb
XYu
20,000
Kmd
Kth
Kml
Kd
TRm
Pag
Kmd
Kmd
IPh
IPb
IPg
TD: 9487 ft depth
10,000
Well picks below Abo Fm are from
King and Harder (1985, fig. 21)
IPh
IPb
Py
Psf
Psr
Kg
Kmd
Kth
Kg
Py
Pa
Pa
Pb
Pb
?
?
0
Pa
Pa
Kc
Py + intrusions (probably sills)
Kml
Py
Psf
Psr
Pa
? ?
? ?
?
?
Ps
Kclt
Kth
?
Kg
Kmd
Kml
Psf
Py
Pa
?
Kt
Kml
Kd
TRm
Pag
Psr
Py
sill
Kclt
Ts
Kc
Kml
Kg
Kth Kg
Tita
Tita Tita
Tim Tim Tita
Tim
Psf
Py
Kc
Tlw1a
Kth
Kd
TRm
Pag
Psr
Kth Tita Ti
Kth
Tita
Qao1
Kg
Qao2
Kmd Kmd
Kmd
Kml
Kml
Kd
Kd
TRm
TRm
Pag
Pag
Coppice dunes (upper Holocene to present)—Mounds of sand accumulated under and in the immediate vicinity of mesquite bushes (and cresosote bushes, to a lesser extent). Mounds range from 20 to 200 cm in height. These dunes also are present on eolian sand ramps adjacent to
topographic highs, where the sediment may be several meters thick. Inter-dune surfaces commonly show signs of erosion and may exhibit a lag of
pebbles. Color of dune sand ranges from light brown to pale brown to brown (7.5–10YR 5–6/3–4; 7.5YR 5–6/4) or yellowish-brown to light
yellowish-brown (10YR 5–6/4). Sand is very fine- to medium-grained, rounded to subangular (mostly subrounded), well- to moderately-sorted, and
composed of quartz, with 10–25% estimated lithic + mafic grains and 10–20% estimated potassium feldspar. Within this sand are 1–5%,
scattered, coarse to very coarse sand grains. Coppice dunes overlie a bioturbated eolian sand sheet or sheetflood deposits; this underlying
deposit is grouped with Qec. The coppice dunes are likely upper Holocene in age, but underlying deposit may possibly be as old as
middle Holocene. Dunes cover 10–35% of the surface. Loose. Deposit under the dunes is up to ~ 2 m thick. Clastic sediment, eolian sediment.
Societal uses: low to moderate potential for aggregate.
D kes and s s und v ded mapped rom a r pho os
Psr
Ts
0
Tita
Tid
Psf
Py
Kml
Kd
TRm
Pag
Psf
Py
TRm
Pag
Kclt
Psr
Tlw1a
Tlw1b
Km
Psf
Ps
Tlw1b
Tlw2a
Kt
Kml
Kd
TRm
Pag
QTbf
QTbf
Tlw2b
Pag
Kcc
Alamogordo fault
–5,000
East
intersection with N-S section
O der bas n
o he Tu arosa Bas n und v ded M ocene o owe P ocene? —Exposed eas o Th ee R ve s h s un cons s s o c ayey s y
ve y ne o med um g a ned sand oca y w h m no sca e ed med um o ve y coa se g a ned sand and 1–10% pebb es Co o s ange om ve y
pa e b own o gh ye ow sh b own 10YR 7/3–6/4 o gh b own 75YR 6/4 o p nk 75YR 7/3 Th n o h ck mos y h n o med um abu a
beds ha a e n e na y mass ve Sand s sub ounded o subangu a mode a e y so ed and composed o qua z and p ag oc ase w h ~10%
es ma ed po ass um e dspa and 10% es ma ed h c g a ns Pa eoso s a e oca y common hese a e cha ac e zed by ca c c ho zons S age
mo pho ogy n m ed exposu es unde a n by gyps c ho zons oca y he ca c c ho zons a e ove a n by h n ye ow sh ed 5YR 5/6 uv a ed
c ay a g c? ho zons O he ho og c ypes nc ude m no g ave y beds e he as 1 oca ve y h n o med um enses o sandy pebb es and
sands one oca y mode a e y cemen ed by ca c um ca bona e w h n he a o emen oned e a ve y ne g a ned sed men o 2 h n o h ck beds
o c as suppo ed sandy pebb es and cobb es m no bou de s g ave a e sub ounded o ounded mb ca ed nd ca ng a wes wa d pa eo ow
d ec on and composed o Te a y n us ve c as s andes e and subo d na e Mesozo c sands one ma x s ne o ve y coa se g a ned sand
ha s sub ounded and poo y so ed G ave s common y s ong y mp egna ed by ca c um ca bona e Uncon o mab y unde es g ave y Qao1
depos s Tb d e s om Qao1 by s sma e g ave s ze and be e cemen a on and conso da on Un s n e ed o ex end we n o he subsu
ace and ke y s pa eo va eys o pa eo embaymen s on he oo wa o he A amogo do au nea Th ee R ve s G ea es exposed h ckness s
2 m bu un s 120 m h ck a he Lewe ng #1 we see c oss sec on On he mmed a e au hang ng wa bas n
s up o ~700 m h ck see
c oss sec on
Ti
Qc
Py
105°50'00"W
Preliminary Geologic Map of the Tularosa and Bent Region,
northeastern Tularosa Basin, Otero County, New Mexico
ANGUS
0
Qc
QTg
7
105°57'30"W
0.75
Qc
Qao2
13
21
16
Qao3
QTg
Pb
17
1.5
Pa
Qao
3
Titd
QTg
12
11
Pb
Qar
QTg
1:50,000
Qao3
Qc
Qao
18
afe
Ps
Qc
Pa
4
10
8
Qao3
Qay
QTg
Qao
3
10
5
Py
Py
Qao
13
Qar
Qao2
Qao
12
• • ••• •
•
••
••
OSCURA
12
16
Qar
Qao
02'30"
QUADRANGLE LOCATION
THREE
RIVERS NW
Qac
Qc
QTg
QTg
4
Pb
••
••
05'00"
NOGAL
PEAK
•
••
33°00'00"N
106°07'30"W
Qgy
Qay2
Qgy
••
Qay2
12
22
Qar
Qay2u
18
Titd
Pb
afe
Qgy
Qgy
Qay
Qao
Qgy
Qse/Qgy
Qc
Qao2
25
Qse/Qgy
Qse/Qgy
Qac
Pa
Qar
Tu–266
Magnetic Declination
May 2004
8º 35' East
At Map Center
QTg
QTg
16
Qar
Qaof
afe
Qao2
Qac
23
Qay2u
Qarof
Qaof
02'30"
Qay
Qao
QTg
Ps
Ps
6
Titd
afe
Ps
Qao
Qac
Titd
afe
Qgy
Qaof
Qay
Qac
••
Qay2u
Qse/Qgy
Qgy
Qar
Qac
Qar
Tu–181
Qay
Qao
Pa
Qac
Titd
Qao
Qaof
Ps
Qsp
QTg
6
*h
Eolian deposits, undivided (middle to upper Holocene)—Unit encompasses undifferentiated dunes (other than coppice dunes [Qec], which are
mapped separately), and other eolian deposits. It includes eolian sand ramps adjacent to topographic highs (up to several meters thick), NE–SW
orientated longitudinal dunes (found near the northern quadrangle boundary east of Highway 54), and eolian sand in mound-like deposits that
extend horizontally over several meters. 1–6(?) m thick. Clastic sediment, eolian sediment. Societal uses: low to moderate potential for aggregate.
PRECIPITATE DEPOSITS
Ps
Py
QTg
•
Qac
Pa
Qtr
Qac
QTg
9
9
Pa
05'00"
Qgyfy2
Py
QTg
Grave on Coyo e R dge P ocene? —Lag g ave composed o ounded sands one and mes one c as s s ng n a sadd e on Coyo e R dge < 1
m h ck
The ages o he d kes and h n s s n he a ea a e ke y 37 o 42 Ma based on 40A /39A age de e m na ons o d kes and s s n he Th ee R ve s
a ea o he no h and n he Sac amen o Moun a ns o he sou heas McManus and McM an 2002 The age o emp acemen o he B ack
Moun a n s ock us no heas o he quad ang e s m dd e Eocene based on a b o e 40A /39A age o 378 Ma an 40A /39A p ag oc ase age o
34 6 Ma and a ho nb ende 40A /39A age o 373 Ma A en and Foo d 1991 M ne a za on s gene a y absen a ong he d kes and s s
Occas ona y hema e mon e ba e ca c e coppe and manganese m ne a s occu n he v c n y o n us ons D kes gene a y
ac u es and
a e 1 o 2 m w de Mo e a e y d kes
au s bu he d kes a e no de o med by subsequen eac va on o he au s S s a e o en cu by d kes
and s s can be cu by au s Seve a new 40A /39A da es a e p esen ed be ow
Landslide deposits (middle to upper Pleistocene?)—Translated, cohesive (but locally internally sheared and brecciated) blocks of rock composed
of the Yeso or San Andres formations. Locally, the deposit is rotated. Rock blocks slid down-slope (probably relatively quickly) under the influence
of gravity. East of Crosby Spring in the northern map area, deposit consists of bouldery, unstratified debris of Dakota Sandstone. 2–50 m thick.
Hillslope sediment, generally coarse grained. Societal uses: very limited.
ALLUVIAL DEPOSITS
9
3
Qar
Qay2u
Qse/Qgy
Pa
O der a uv um w h subord na e younger a uv um m dd e o uppe P e s ocene and Ho ocene —See desc p ons o Qao and Qay above
NEOGENE NTRUS VE ROCKS
Psh
Pb
Ti
Qay2u
Qse
Qarof
Qar
Pag
Psf
Qao
QTg
8
Qgy
Ps
Qac
Qac
9
•
••
••
••
••
••
•
afe
Qay2u
QTg
9
••
Qse/Qgy
QTg
QTg
Qac
Qay2u
Qgy
Pa
Qao
Qao
Pa
Qay
17
Psr
Py
QTg
QTg
11
Qar
Qarof
Qaof
Qay
Tist
7
Kd
7
19
Qsec/Qao2
Qao
Qtr
••
••••
•••
afe
Km
Qao
Qao
Pb
22
28
Qaof
Qarof
•••
•••
••••
•••
•••
•••
••••
•••
•••
•••
•••
•••
•••
•••
•••
••
•••
•
•••
•••
•••
•••
•••
•••
•••
••
••
14
Qse/Qgy
Qgy
12
Qac
10
Qaof
afe
•
15
Qac
Qao
afe
Qar
•• •
• •
••
•
••
•
•
•
16
Qay2u
Qaof
Qar
•••
•
• •••
•
•
••
••
• •
•
••
••
Qao
07'30"
20
Ps
••
•
•
•
••
••
•
Titd
3
˛h
Pa
Qac
11
5
Py
Pa
15
17
10
3
Pa
25
Qsec/Qao
4
5
Pa
QTg
QTg
14
12
5
8
24
Qac
QTg
Pb
5
Qay1
Qay
Pa
Qac
Qao
Qay2
QTg
Qao
3
5
7
7
QTg
Qao
Qac
4
Qar
Qse/Qgy
8
••
Qgy
QTg
14
•
••
••
•
•
Qac
Qay2u
•
•
•
• •
• •
••
••
•
•
••
••
••
••
••
••
••
••
•••
••
•• • •
• • • ••
••
•••
••
•
••
• • •• • • • •
••
••
••
• •••
••
Qar
4
6
16
Qse/Qgy
•
• ••
• ••
••
•
•
•
•
•
••
Qac
Qay1
Qgy
•
••
•
••
•
•••
•
••
•••
•••
• ••
•• • • • • • •
••••••
•
•••••• •••
•
Qao
Qar
Qaof
Qaof
••
•
•
•
••
•• •
•
•
• ••
•
•
• ••
••
•
•
•
••••••••••••••
•
•
•
•
• ••• •••
••• •••
••
•• •••
••• ••
• • • • ••
•• • •••••
••
•
Qar
3
Qsec/Qay
8
Qac
Py
Qac
QTg
QTg
Qsec
Qao
Qay
Pa
Qao
•
•
•••
•••
•••
•••
•
•
•
•••
•••
•••
•••
•
•
•
•••
•••
•••
•••
•
•
•••
•••
•••
•••
•
•
•
•••
•••
•••
•••
•
•
•
•••
•••
•••
•••
•
•
•••••
•••••••••
••••••••••••••••
••••••••
•
•
•
•
•
••••••
•••••••
••••••
••••••
•
•
•
•
•
•
•
•
•••••••••••••••••••
• •
••
••
••••
•
•
••
••
••
•
••
••
••
••
•
••
••
••
••
•
•
••
••
••
•
••
••
••
••
•
•
•• •• • •
8
Pa
Qac
Qac
Qac
Qao
•
•
Qay1
Pa
QTg
Qac
Ti
5
10
Qao
QTg
Qac
••
02'30"
•
11
Titp
Tim
7
Qac
Qao
QTg
Qao
QTg
45
18
3
Titd
Qay
Pa
Pb
QTg
•
Pa
QTg
•
Qar
•
36
4
Tid
ˇm
Qac
Qao
12
15
Tiag
7
Pa
7
Qse
Qaof
•
4
•
•
QTg
Qay2u
afe
Qarof
Qse/Qgy
7
Tita
4
Qac
QTg
QTg
Qay2
Qse/Qgy
Qar
afe
Qar
Qay2u
••
•
••
• •
Qar
•
••
••
••
• •
••
••
••
• •
••
• ••
• •
••
•••
••
••
Qay2u
Qac Pa
Qse/Qgy
Tis
9
4
QTg
Qac
Pa
Pa
Py
QTg
Qac
Titb
Qao2
2
QTg
Qac
Tbf
^d
Qac
Pa
Pb
Pa
^d
_Ob
14 16
Qac
Qao
Qar
••
••
••
••
Qgy
afe
afe
Qaof
Qaof
Qaof
Qay2u
Pa
High-level gravelly deposits capping ridges (Pliocene to lower Pleistocene)—Gravel, sand, and silty sand deposited on high-level erosional
surfaces that are 15–70 m above modern stream grade north of the Rio Tularosa and east of the Alamogordo fault. Extensively mapped on the
piedmont south of the Rio Tularosa, but underlying erosional surfaces there are much closer to modern stream grade. Gravel is typically clast-supported, imbricated, subrounded to subangular, poorly to very poorly sorted, and consists of pebbles and cobbles (1–5% boulders) composed of
sedimentary (mostly limestone) and igneous clasts. Deposit is well consolidated, and the basal few meters of the unit, where exposed, are
commonly cemented by calcite. This calcite cementation is inferred to be related to precipitation of calcium carbonate from ground wa e Road
cu s evea S age o g ea e pedogen c ca bona e deve opmen n e ed owe P ocene o owe P e s ocene age s based on compa son o
he coa se na u e o h s depos o he coa se na u e o depos s o ha age n he A buque que and Españo a Bas ns o he no h— nc ud ng he
Tue o Fo ma on S ea ns 1953 Ancha Fo ma on Kon ng e a 2002a and Puye Fo ma on Wa esback 1986 Wa esback and Tu bev e
1990 Up o 25 m h ck C as c sed men a uv a sed men mos y coarse gra ned Soc e a uses aggrega e
85
9
14
Qse/Qaof
Qao3
8
12
8
15
Qse/Qao2
10'00"
17
QTg
Qay
afe
Qac
Qay2u
Qse/Qgy
••
••
••
Qarof
•••
• •
••
•••
••
••
Qay2u
•
••
••
Qaof
afe
Qac
7
QTg
Qay2
Pa
18
23
QTg
•
Qgy
Qar
afe
Qay2u
Qse/Qgy
Qaof
Qao
Tim
7
Qac
afe
17
Tid
17
7
Qao
QTg
Pb
Qaoy
• • • • • • • • ••
••
Qgyay2
Pa
••
Qse/Qgy
Tu–117
••
••
Tu–255–257
•
••
afe
Qse/Qgy
Qarof
Qay2u
•
•
••
•••
Qay2u
QTg
80
Pa
QTg
QTg
Qac
7
Qay
Qac
Pa
Qay
Pa
afe
Qac
8
40
QTg
Qao
Qac
Qac
•
• •
••
•• • • • ••
••
••
•• •
• • •
••
•••
Qaof
Qao
2
Tls
Py
20
Qtr
Tim
8
QTg
Qay
QTg
Qac
Qao
Pa
QTg
Qao
••
••
••
••
••
• ••
••••
••• ••
•
••
•
•••
afe
Qaof
Qaof
QTg
Qaoy
Qar
Qaoy
QTg
14
19
23
16
Qao1
Qao3
Tid
9
QTg
QTg
Tg
afe
Pa
10
27
Qse/Qao
Py
20
7
5
14
6
Qay2
13
Pa
afe
Ti
Qao
QTg
afe
•
•••
••
••
• •
•
•
05'00"
afe
Qar
Qarof
Qar
Qar
Qaoy
QTg
QTg
QTg
Pa
5
21
14
Py
9
4
18
25
8
Tid
9
Pa
Pa
Qac
Qaoy
QTg
••
••• ••
•••••
•••
••••
Qarof
Qar
Qac
Pb
QTg
Qao2
Qac
Qay
••
••
••
••
••••
Qaof
Qac
QTg
Qar
Qao2
• •
•••••
Qse
Qar
Qgyay2
••
•••
Qse/Qgy
• • • • • • • •
Qgy
afe
•
Qarof
Qar
Qay2u
Qgy
• ••
••••
••••
Tu–116
••
••
••
••
••
• • • • • • • • •
••••••
Tu–130
Qse
•
Qgy
Qaof
2
4
Qao
Qar
Qay2u
• •
Qgy
Pa
Pa
21
10
25
13
28
7
15
32 14 18
Tid
10
Qao1
^d
Tid
Qao3
33
2
afe
QTg
Qay1
Qar
Qse
QTg
5
4
8
62 47 12
50
60
17
31
29
Qay
Ti
5
32
12
Tid 27
•
18
Qao3
Qao3
QTg
Qao2
5
7
17
Qao3
Qay
Qac
Qaoy
Qc
Qao3
Qao3
14
Tid
Qao2
23
Pa
Pa
QTg
5
•
Qar
12
35
22
Qai
Qay
Ti
Qac
12
afe
Py
Qao2
14
17
Qai
Tid
Tis
6
Tid
Qao2
Pa
QTg
Qar
5
QTg
Tid
Titb
Tid
Tid
Titd
5
Qay
4
Qar
afe
• ••••••
Qay2u
•
•• • • • • • •
•••
Qay2
•
••
••
••
Qay2
Qse/Qgy
••
•
Qaof
afe
•
•••
Qgy
Qgyay2
•
Qse
Qe
Qse
•• • • •
Qse/Qgy
••
• • • • •
• • • • • • • • • •
• • • • • • • • •
• • • • • • • • •
• • • • • • • •
• • • • • • • •
• • • • ••• • • •• •• •
• • ••
••
•• ••
•
•
•• ••
••
•
•
Qgy
Qse
Ti
5
Ti
Qao2
Qao2
Pa
9
Qai
Pa
Qao2
Tid
Qar
9
8
2
5
Pa
6
Qay2r
13
Qtr
11
7
3
Qao2
6
Qay2
Qao3
Qao3
Py
•
•
•
•
•
•
•
•
•
•
•
•
•
•
•
• • • •• •• • • •
• • • •••
••
•••
•
••
••
••
Qgyay2
Qe
Qao
6
5
8
Qc
3
Qao
Ti
Tid
•• • •
• •• • • • • • • •
•
•
• • • • •
• • • • •
•••
Qaof
Qse
Qgyay2
Qaof
Qao
Pa
Qao3
Py
QTg
Py
7
15
6
17
Qao
3
3
6
9
Qao
afe
Qay2r 3
••
••
•••
Qaof
Ti
3
Qac
Tu–154
Qar
Qaof
afe
2
Pa
Tita
33
Qao
Qaof
3
37
Py
12 Qay1
Qao2
Tid
Qao3
afe
Qao2
10
Tim
15
Tid
30
6
5
14
10
• •
afe
Qse
Qgy
Qar
10
5
4
6
Qay1
Ti
3
Ti
2
7
10
Tid
4
QTg
5
•
Qgy
Qse/Qgy
Qay2
Qay2r
Qao
QTg
7
Ti
19
Qao2
55
38
41
6
•••
Qay2
Qay2r
Qse/Qgy
Qse
Qgy
Qay2
Tu–209
10
Qao
afe
Qay2u
afe
Qaof
Qary3
Qay1
Qaof
Qgy
Qaof
Qao
17
6
5
2
8
6
Tid
Qar
7
4
7
45
Pa
10
Qao3
5
QTg
Tita
Tim?
18
18
16
7
Qao3
••
Qse
Qse/Qgy afe
Qgy
Qay2
Qar
4
4
Tid
3
Qao1
Py
Qay2
4
Qls
10
2
25
••
• • • ••
••••••
•
• • • •• • • • • • • • • •• • • •
• •
• • • • •
Qse
Qao
Qao
Qse/Qgy
Qgy
Qar
10
10
Ti
Ti
Qao3
Tita
QTg
Qao1
•
Qay2r
Qao
Qay2r
•••
•
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
••
07'30"
afe
Qay2u
Qao
Qaof
Qaof
Qao afe
Tid
9
Ti
Qay2r
Tid
7
Tita
12
5
5
••
••••
Qay2u
Qay2u
6
•
Qao afe
Qse
5
Tid
Qp
Qay2
Tid
12
12
30
Qay1
afe
Tita
8
5
Ti
6
3
10
8
26
Qao1
Qao2
Qar
Tid
13
Tita
Tim
•
Qay2u
Qao
Tid
4
Tim
35
•
T–1900
Ti
Pa
5
Ti
Ti
5
Tid
8
Py
•••
• • •
23
Qao
Qao
Tita 7
QTg
11
Qar
Qay2u
Qao
10
10
9
QTg
12
Tita
19
7
4
5
3
Tita
Tita
Tita
Py
Pa
Py
12
Qao1
Pa
12
32
Tim
9
17
Qao2
QTg
Qao2
9
9
14
12
17
11
9
Qls
9
10
Py 7
9
10
7
Qp
7
12
17
18
Py
7
16
7
10
7
Qc
••• • • • • • •
28
3
8
Ti
Tid
Tid
Ti
Py
Qao2
Ti
• •
Qao
Pa
7
Pb
9
9
22
QTg
8
7
4
QTg
Ti
Pa
Tid
37
Py
Qao1
12
10
5
4
10
2
37
10
7
19
••
22
afe
Qao
Qao
7
12
4
7
7
10
Tita
Qay2r
Tim
15
13
35
11
2
5
7
3
5
14
19
4
17
4
••
T–71
Qao
Qay2u
12
Qar
8
6
Ti
Qao2
Ti
Ti
Qay2r
Ti
30
Tim
Tita
Tid
Tita
9
Tim
7
Tid
20
3
Tita
Tid
4
Tid
Tim
5
22
Qar
17
4
2
5
12
5
17
6
Tid
15
Tita
10
12
13
Py
Ti
Titb
Pa
Qay2
9
Tid
7
11
Tim
8
Qay2r
12
7
Pa
8
Tid
Tim
•
afe
Qao
Qay2
10
Qao2
Pa
10
Tim
4
23
18
18
19
Tim
2
20
12
•
•
••
• •
• •
afe
afe
15
7
11
70
Tid
11
Ti
18
30
Tid
Tid
Tita
8
9
Tim
Qay2r Py
•
Qay1
Qay2
14
QTg
7
Ti
15
Tita
Py
••
••
•
Qay2u
Tid
Tid
4
16
14
7
Tita
7
7
19
10
Qls
Tim
6
10
• •
•
Qar
Ti
10
36
Tid
••
7
12
Tid
25
15
Tid
7
4
4
Tita
Qse
12'30"
4
7
10
4
Qc
10
Ps
10
25
4
3
8
10
Qc
25
16
3
Qaovf
Qaoy
Qayo
Qai
3
6
5
7
6
15 9
7
5
12
14
3
3
10
6
Tim
Psf
7
13
8
10
6
Py
Tid
10
3
5
7
6
Tid
••
T–1797
7
Ti
Py
Tid
6
5
Qao2
7
••••
7
4
10
Tita
Psr
24
4
9
8
14
19
10
Qc
10
Tita
Tid
10
12
Qay2r 12
7
3
53
Tid
22
Ti
8
65
Qc
60
Ti
11
12
10
Qao3
22
14
2
Tim
Ti
36
Tita
32
••
•
4
afe
Qao
Ti
Ti
Ti
7
64
62
8
Ti
17
Py
•
45
7
11
18
Tid
26
Tid
54
5
55
•• • • •
Py Qar
21
5
15
85
•
Qao
Ti
34
27
13
Psr
Tid
37
•
••
Py
Py
Tim
36
15
10
Py
57
50
30
Qay2
Qao3
7
•
••••
17
•••
5
• • • Py
•
•
•
••••
•••
••
20
Qay2
80
50
7
27
35
10
15
55
50
6
Ti
45
13
Qao2
12
Ps
9
30
49 45
Ti
Ti
4
3
105°50'00"W
Py
9
35
Psf
38
33
33
Qec
Qay1
8
15
10
4
Qao2
11
10
Qay2
17
Qay
Qse/Qao
Qse/Qaof
Qse/Qgy
10
Ps
Qay2
13
Tid
Ti
Tid
Tim
Titb
Pa
3
25
12
Qse
Pag
••
14
14
Qao2
Tita
28
13
Tim
Psr
••
• •
• •
20
16
Ti
2
•
Qao
Pa
Qayo
Tid
Qls
Titd
28
11
Ti
24
•
Qay2u
Qay2r
Qay1
7
20
Qao2
Qao
afe
Qay2u
10
7
•
T–1797–S7
18 17
20
3
•
Qao
Tid
••
Qay2u
Qar
afe
11
14
Kd
Qao3
Qse
Psf
Tid
Psr
10
Tid Qls
Psh
7
•
Qar
Py
12
••
Qec
27
^m
Qse
Tim
8
23
Py
Qtr
17
Ti
Psr
16
44
53
28
19
Tim
14
Py
16
Ti
14
Qao2 25
^m
12
Qay2u
Qay2r
Qary2
Qay2
Qgy
Qgyfy2
8
Ti
Py
47
Tid
3
45
18
22
Ti
Py
12
11
Pag
15
14
Qe
afe
Qe
Qse
Pag
13
Qao2
Ti
29
6
28
18
Qar
Kd
25
20
24
Ti
30
6
10
7
9
24
21
Tid
20
Ti
Ti
8
7
14
Ti 8
Qao1
Qls
20
Km
23
Qao2
Ti
3
18
10
Ti
6
9
Pag
26
Ti
Psr
Psr
Qao3
9
17
Qao2
Tid
Qao2
18
12
14
14
31
25
20
36
Ti
5
Ti
Qay
Qar
12
••
T–1797
S–7
10
Tid
•
Qay2
Qay2u
Qaof
10
Qay2r
2 Qc
Py
Qay1
Qao
Qao
10
Qao2
4
Ti
8
20
Tim
Qao2
37
Py
•
• ••
• • • • Tid
••
4
•
•
9
16
18
Qay2r
Tid
6
9
4
4
Tid
Qao
Qay2r
••
••••••
••
••••••
••
••••••
••
••••••
••
••••••
••
••••••
••
•
•
••
•
• ••
••••••
••••••
••••••
••••••
•••••
••••
••••
•••
•••
•••
•••
•••
••••
•••
•••
•••
•••
•••
•••
•••
•••
•••
••
••
•••
•••
•••
•••
•••
•••
•••
•••
•••
••••
••••
••••
••••
••••
••••
••••
••••
••••
• ••
••
•• • ••••
•• •
• • ••• •
•••••• • ••• ••
10'00"
Py
15
8
10
1
•
Qay2
•• •••••
afe
Qay2u
Qaof
Qao2
Qay2u
Qay1
••
Qay2
Qaof
6
Qar
Qay2
4
5
Py
••
Qayo
7
17
••
Qao
••
Tid
Tid
Tist
35
Tita
25
Ti
Titd
Qar
14
27
18
16
15
17
Ti
7 17
8
15
27 35
Ti
Qay2r
9
Asterisk (*) denotes units shown in cross section only
Qao2
Kd
^m
10
20
16
Ti
7
Qao2
36
12
7
21
Terrace gravel (Pleistocene)—Gravelly terrace deposits found alongside, and paralleling, modern drainages, including the Three Rivers drainage.
The bases of the terrace deposits (straths) are greater than 2 m above these drainages. The terrace deposit is generally poorly exposed.
Gravel are subrounded to subangular, poorly sorted, and consists of pebbles with subordinate cobbles and 1–10% boulders. Spallation of
exposed clasts results in abundant subangular-angular gravel on the surface. The gravel is clast- to matrix-supported and composed predominately
of intermediate-mafic igneous rocks, with subordinate Paleozoic–Mesozoic sedimentary clasts (mostly sandstone and limestone). The gravel is
interbedded with varying proportions of sand. Sand is very fine- to very coarse-grained, pale brown to very pale brown (10YR 6–8/3; 10YR 7/4),
subangular to subrounded, and moderately to poorly sorted. In at least some deposits, a significant proportion of the sand is composed of gypsum
grains. Deposit also includes fine-grained sediment that is internally massive, brownish–yellow (10YR 6/6), locally clayey-silty, and dominated by
very fine- to fine-grained sand (much of which is gypsum grains); the fine sediment locally contains gypsum-cemented rhizoliths. Surfaces are flat,
variably eroded, and commonly exhibit strong gypsum accumulations that obscure the underlying terrace deposit. The gypsum mantle and poor
exposure creates local uncertainty about whether a given terrace has a significant deposit or is simply an erosion surface. Some higher surfaces
exhibit well-developed desert pavements and well-varnished surface gravel. Weakly to moderately consolidated. Mostly 1–5 m thick, with local
paleovalley fills up to 15 m thick.
PL O–M OCENE SED MENTARY UN TS
Colluvium (middle to upper Pleistocene and Holocene)—Angular to subangular pebbles, cobbles, and boulders in a matrix of clayey-silty sand.
Massive or in steeply inclined, tabular beds. Gravel composed of a variety of lithologic types, but limestone dominates. Common on north-facing
slopes. Generally mapped in mountainous areas where it is >2 m thick and obscures underlying geologic formations and geologic structures (such
as faults or folds). Also locally mapped adjacent to the Alamogordo fault scarp south-southeast of Three Rivers, where it consists of gypsiferous
sand (mostly very fine- to medium-grained) and variable amounts of gravel. Hillslope sediment, generally coarse grained. Societal uses: possibility for aggregate in limited areas.
EOLIAN AND SHEETFLOOD–SLOPEWASH DEPOSITS
Correlation of Map Units
• •
Ps
25
15 Ti
30
Qao3
29
3
22
9
14
15
6
Qc
Py
16
20
A' Geologic cross section
16
30
30
Qaoy
Pediment gravel, undivided (upper Pleistocene)—Thin sandy gravel, generally gypsiferous, that overlies pediment surfaces in the lower part of the
Sacramento Mountains. Surfaces are relatively smooth and exhibit well-varnished desert pavements. Underlying soil generally marked by gypsum
accumulation comparable to a Stage II to III calcium carbonate morphology. Less than 1 m thick. Clastic sediment, alluvial sediment, mostly
coarse-grained. Societal uses: aggregate.
Pag
21
22
35
13
5
7
5
Tid
13
26
7
15
Ti
Tist
5
Ti
19
Tist
^m
8
Pag 5
5
Py
Ti
30
11
•••
• • •• • •••• •
10
8
Py
11
Qao2
••
•
•
Tid
afe
afe
••
20
Qao
Ti
Ti
Py
Qar
8
Qao3
43
8
10
Timp
16
15
8
Ti
Qc
15'00"
10
Psf
Ti
12
Qc
Py
Ti
12
Psf
•
•
••
Qao2
Qay2u
Py
Tita
43
30
7
9
10
Ti
13
13
Py
Qar
10
42
Ti
Kd
12
10
5
6
25
Ti
7
Tist
11 40
16
Titd
Ti
7
Kd
45
Ti
Tid
Tist
18
Ti
Ti
Py
Psr
Tita
13
Ps
10
Tim
Qay2r
10
Py
9
Tist
30
18
Ti
13
Qao3
Psr
Qao2
15
31
55
14
Ti
24
6
Qar
•
Psh
3
11
33 Tita
30
22
17
•
•
Qar
Qay Qp
12
Tita
Ti
Tim
Tid
Ti
Tim
Km
Tita
18
8
Tid
••
Psh
7
8
8
Qay
Qaof
Tim
A
18
10
12 8
Psr
Qay
5
Desal Test
Well #8
9
13
HILLSLOPE AND MASS-WASTING DEPOSITS
Spring
Tim
Ti
6
43
22
22
Tita
Tita
8
Py
Foliation lineation
10Qary
4
4
11 Ti
8
Tita
7
Tita
Tita
4
Tim
8
30
20
15
Tita
15
20
•
66
10
6
Ti
4
Psr
36
25
S4 inclined foliation
Artificial fill or excavations (modern)—Compacted silt, clay, and very fine to very coarse sand (with minor pebbles) under highways and
railroads. Very coarse pebbles and cobbles drape compacted fill under railroad tracks. Also found in berms surrounding excavations, which
include pits, quarries, or reservoirs. The base of these excavations has generally been filled by >10 cm thick deposits of clay, silt, sand, and
gravel transported by arroyo runoff, mass-wasting, or slopewash processes. Human-engineered land.
afe
S3 inclined foliation
Psr
9
Py
12
3
8
• •
8
Py
2
afe
3
Psr
21
20
Py
Qay2
8
••
•
8
••
•
•
4 17
10 13
Qay1
Qao
Qar
•
•
afe
7
22
23
23
36
•• •
7
Psr
13
18
29
20
8
Kml
16
13
Psr
QTg
ARTIFICIAL FILL AND EXCAVATIONS
S2 vertical foliation
7
10
25
10
Psf
15
Qtg
QUATERNARY–PLIOCENE SEDIMENTARY UNITS
Qls
20
7
16
5
20
23
2
Qao2
Qar
4
14
3
4
4
13
Tita
26
Tim
3
7
Ti
Psr
10
Qay2
Tita
Tid
Qay1
afe
8
Qao2
Psr
Ti
4
24
S2 inclined foliation
34
24
19
11
50
Tita
10
18
15
22
Tist
Psf
28
9
Ti
Tid
6
Ti
28
15
Psr
• •
Qaof
Py
39
12
4
10
Psf
Qao
•
Qao
•
Qao2
17
Ti
Psr
3
6
6
15
S1 inclined foliation
Kmd
20
18
27
23
25
Qary
10
Tim
6
6
Ti
7
11
Ti
28
25
19
12
21
9
31
Psf
Qar
Desal
Test
Well #5
7
11
Psr
34
Ti
Qao
Tita
11
27
13
21
64
85
23
Igneous rocks can have phaneritic, aphanitic, and/or porphyritic textures. In phanertic rocks the individual interlocking crystals are large enough
to see with the naked eye or at 10x magnification. In apahanitic rocks, the crystals are too small to see with the naked eye or with 10x magnification. Aphyric is another term used to describe volcanic rocks that have few and/or small crystals. Porphyritic rocks have larger crystals set in an
aphanitic matrix. Rocks with crystals smaller than 1 mm are considered fine-grained, 1–5 mm are medium-grained, 0.5–3 cm are coarse-grained,
and greater than 3 cm are very coarse-grained.
10
22
15
23
Qao1
30
19
6
Tita
6
4
Qao
• •
• • • • •
Qao
••••••
Qao
•
15
7
5
5
8
12
3
10
14
Ti
Qay2r
6
Tid
Ti
Tid
Psr
•
• •
•••
•
Qao
•
•
Ti
Pag
25
17
Ti
Tita
7
•
Qse
•
••
Ti
Tist
4
•
••
Qao
Qayo
Qao
• •
Qao
•
••
•
•••
•••
•••
Qar
Qao
•
•
•
••
Kd
•
••
••••
31
25
9
12
•30
Qc
17'30"
10
Kt
Qao1
15
14
Qary
17
Strike and dip of overturned bedding
13
20
10
38
Qay
10
17
20
13
30
20
59
Strike and dip of vertical joint
Kg
17
23
Qao3
Qay
5
10
35
Qse
•
Desal Test
Well #4
Qse
•
••
••
••
•••
••
24
•
••
• • 22
6
10
4
Psf
11
Psf
Qao2
•
••
5
•
Pag
5
Psf
10
29
Strike and dip of inclined bedding
Kc
10
17
18
16
40
Tist
9
19
Qay
50
Py
Qse/
Qao
•
• • •• • • •
•
••••••••••••••• • •
•
••
•
••
••
• •
•
•
• • • • • ••
• •
•••
••
•
••
•
••
••
•
••••••
Qao2
Qay2
Tid
Qary
25
Qp
Textures in Igneous Rocks
22
18
10
11
9
27
8
9
42
• • •
• • • • • •
Cross bedding — Truncated foresets represent top
14
14
9
17 10
^m 17
6 19
27
Kd
10
19
Qao2
14
18
7
13
13
5
24
16
25
•
Qar
17
12
9
7
Kmd
2
16
16
12
Shear zone
Ti
Kc
7
5
7
12
6 4
7
14 10 15
8
Qary
25
7
6
8
Titd
10
9
Qao1
Qary
Qp
Qay2u
afe
Qse
Qay2
Qao3
QTg
27
Qao1
••
Qse/Qaof
Qao
Qse/Qao
Desal Test
Well #1
• •
Qao
Psf
Pag
Qay
Psf
Qao2
4
12
••
• 85
24
14
Minor S-fold
30
10
QTg 23
Kclt
QTg
Kc
5
20
4
11
10
15
Kml
7
•••••
Tid • • •
Pag
Qse
Qar
•
••
12'30"
45 10
Qp
••
Qay2
•
•
Qaof
•
afe
Qay2u
••
Qaof
•••••
QTg
18
Qao1
Qay
Kt 2
QTg
2
Grain sizes follow the Udden–Wentworth scale for clastic sediments (Udden, 1914; Wentworth, 1922) and are based on field estimates. Pebbles
are subdivided as shown in Compton (1985). The term “clast(s)” refers to the grain size fraction greater than 2 mm in diameter. Descriptions of
bedding thickness follow Ingram (1954). Colors of sediment are based on visual comparison of dry samples to the Munsell Soil Color Charts
(Munsell Color, 1994). Soil horizon designations and descriptive terms follow those of the Soil Survey Staff (1992), Birkeland et al. (1991), and
Birkeland (1999). Stages of pedogenic calcium carbonate morphology follow those of Gile et al. (1966) and Birkeland (1999). Unless otherwise
noted below, sand in Quaternary deposits is subrounded to subangular. Medium to very coarse sand has a composition consistent with a litharenite, whereas very fine- to fine-grained sand is more arkosic (as inferred using a hand lens).
Qay
Tid
Tid
Tim
•
4
10 6
Overturned syncline — Showing direction of plunge; dashed where approximately located; dotted where concealed
Qay
33
34
7
37
12
18
Qao2
Kc
12
12
Tita
Tita 6
18
9
Kc
QTg
Qao2
7
Surface characteristics aid in mapping both lithostratigraphic and allostratigraphic units. Older deposits generally have older surfaces, so surface
processes dependent on age—such as desert pavement development, clast varnishing, gypsum and calcium carbonate accumulation, and eradication of original bar-and-swale topography—can be used to differentiate the alluvial fan deposits. Locally, erosion may create a young surface on
top of an older deposit, so care must be exercised in using surface characteristics to map Quaternary deposits.
10
Qao1
Qay
9
Overturned anticline — Showing direction of plunge; dashed where approximately located; dotted where concealed
Minor M-fold
Tim
37
Syncline — Showing direction of plunge; dashed where approximately located;
dotted where concealed
Kc
Qao2
Qay
9
TERRACE AND PEDIMENT DEPOSITS
For sedimentary units, a brief discussion is warranted on the difference between lithostratigraphic and allostratigraphic units. Most map units
presented below are lithostratigraphic: recognized by their geomorphic position or the inferred geomorphic process responsible for deposition.
Lithostratigraphic units can be differentiated by lithologic properties (such as texture, color, and composition). Some lithostratigraphic units are
subdivided into allostratigraphic units, which are separated by interpreted unconformable contacts or by inset relations (both representing inferred
time gaps). Allostratigraphic units have numbers at the end of their map labels. For example, lithostratigraphic unit Qao is subdivided into allostratigraphic units Qao3, Qao2, Qao1; lithostratigraphic unit Qay is subdivided into allostratigraphic units Qay3, Qay2, and Qay1 (listed youngest to
oldest). These allostratigraphic units possess different ages, although the sediment looks relatively similar within the overall lithostratigraphic unit
(Qao or Qay).
Anticline — Showing direction of plunge; dashed where approximately located;
dotted where concealed
Kc
Tim
15
11
7
10
Kc
Tim
Kml
QTg
Tim
Titb
10
10
7
14
QTg
Tim
Tim
Qar
8
10 23
Qao3
23
16
• •
••
10
10
••
•
13
•
•
•
•
7
••
13
7
Py
Qls
Psr
2
Psf
18
Qc
Laramide reverse fault —Showing dip; barb on upthrown side; dashed where
approximately located; dotted where concealed
8
Kc
Qao1
• •
•
5
10
23
30
Qc
•
•• 8
••
•
Qao2
4
Pag
Qao3
16
16
20
5
••••••
59
15
Tim
19
14 Tid
3
Kc
Kmd
Tita
12
Kd 7
Qao
Qao
Kml
5
10
7
Tita
21
^m
13
Tid
Ti
• 21 12
Qao1
28
23
5
47
30
Qay2u
Qp
Pag
Qar
Ti
•
Qaof
••
Qp
Psf
Qao2
Tita
26
24
3
Kt
11
23
^m
• • •
4Qao1
85 20 Titb
5
• • • • • • • • • •
•
Qay
Qls
Qay1
18
• •
• •
Qay2u
Qay2
26
7
Kc
Kg
Titb
Km
16
D
•
Tita
Pag
12
17
12
Qc
Titd
10
8
Tita
Titb
3
10
13
3
12
Qay
5
11
Qar
•
Kc
11
Kml
13
▲
20'00"
Tim
Qao1
Qao
Qar
Tim
Kd
Kd
50
10
Tim
28
Kt
Qao2
•••
Qay
4
Tim
42
Kml
Qao2
25
Titd
Ti
^m
Qse
Kd 6
Psf
••••
Qay2
Qar
U
QTg
5
Km
Titb
• 16
• • •4 • •
3
1
Qse
D
17
afe
Qao
Qse/Qaof
Qaof
Qao2
Qay2u
Qao
••
•••
•••
• •••
••
Qaof
7
U
Qse/Qao
Qaof
• ••••••• • •
Qay
Qay
Qao1
Qayo
Qao3
Tim
53 15
•
Qay2
•
Qar
Qao3
Qao
afe
Qao
Qao2
Pag
Qay2
Qao
•11• • • • • • • • • • • •
15
Qay2
Qay
25
4
Tid
^m
30
Titd
••
Qar
Qaof
11
QTg
Qayo
25
14
•
•• •• •
Qaof
Qay
Psf 7
Qao
•
Qay2
23
Qay
•
5 ••
Qary3 Tita
Qay
Qay2u
13
11
19
Km
23
Qary
Kc
Tc
Tc
Kd
28
18
^m
Qc
10
12
Tita
•••••
•••••
7
Qao1
Qay2u
Qsec/Qay
Tid
••• •••••
••
••••• 4
•••••
Qar
afe
Qay
• • •
••
••
•
•
••
• • • •
••• •
Qay3r
Qaof
18
Qay2u
Qec
••
Qaof
^m
Qao
••
Qay
14
Psf
Qaof
Qec
Kd
Qao2
Qay
Qse
5
Qary
Tid
Kd
Km
Qao3
Kml
10
20
24
Qse
8
Qao3
Qar
Tim
••
15'00"
Qao3
15
••••
Qay3
6
8
Qc
Qay2u
Qc
23
Kg
17 7
•
Qar
15
•••
•••
Qay
Qse
11
••
Qay
Qsec/Qay
Qay
Qar
Qsec/Qao2
Qar
Qay2u
13
Qay2u
Qay2r
Qay2
afe
Qay2u
Tid
Qao1
Kc
5
Qao2
27
Titd
32
Tita
4
Qao2
QTg
Kc
Qao2
afe
Qay2
•
Qary3
• ••••••• • • •••• •
• •
Qec
Qao
•
Qsec/Qay
Qar
25
•
Qay2
Qary3
Qar
Qay2u
22
32
5
Qay
Tc
22
Qao2
Qc
•
•••
• •
Qay2u
Qay
Qao1
Qse/Qao2
Kc
• 30
Kc
Qao1
Qse/Qao2
•
•
Qao
Qay2u
Qay3
70
Tc
••
Ti
30
Qar
Qao
Qay3
Tim
afe
Qao2
••
Qay3r
Qay3r
25
50
21
27 9
Qao1
•• • • • • • •
•• • • •
• ••
Qay2u
Tita
•
• ••
••
••
••
•••
Qay3
Qay2
Qec
41
24
32
27
afe
Qay3
10
39
32
Kg
28 24
40
30
▲
55
Qao2
Qary
Qao2
Qao
••
• •• •
••
Qay2u
Qar
Qay
Qay2u
•• •
•
••
Qse/Qao2
Qar
31
10
25
Kc
46
29
Qtg
Km
Qao2
Qay3
17'30"
23
5
Qay
Qayr
Qao1
Qay2
Qay2u
Qar
27
Qao2
•
Qse
21
16
••
Qary
Miocene normal fault — Bar and ball on downthrown side; dashed where
approximately located; dotted where concealed
Qay
Qay
Qay
Tc
35
Kg
Kd
Pag
Qary3
Qay
Tbf
^m
32Tc
Qao2
Tbf
Qsec/Qao2
12
22
30
Qao1
Qay
Qao2
Qao
Qar
21 13
Qse
Qao1
Qtg
15
••
•
••
••
••
• •
• ••
••
• •
Pag
Qec Pag
Qay2
Qay2u
Qtg
Qar
Qao2
••
•
Qec
Tc
••
•
••
Qao2
27
Qay3r
Qar
13
Tc
• • •
Qse
Qao2
••
••
8
Qay
37
Qay
Qai Qse Qary 24
22
Kc
20
••
••
27
Tc
Qse
Kc
40
18
Qse
••
••
•••••
Qar
16
Qe
Qay2
afe
Qary3
Qay3
Qtg
Qao
Qse
Qse
Qay
27
Qe
Qay2u
Qay2u
Titd
••
••
Contact — Dashed where approximately located; dotted where concealed
• • • •
Qao2
• • •
••
• • ••
Qay
Qao1
Qec
Kd
25
•
••
Qay2u
Qtg
Tc
Qse
38
Qec
Qao3
Qse
9
10
Qtg
Qay
Twh
Qay
••
•
••
••
Qay2u
16
Kc
Qec
••
••
Qec
Qay2u
Qao
Qsec
Kc
Qse/Qao2
28
••
•
••
Qse/Qao
afe
• • • • • • • •• •• • • •
•• •
••
Qay2u
25
afe
••
••
•
•
Map Symbols
Qay
Qao2
Qao2
34
Qse
••
•
Qsec/Qay
Qe
Qao2
afe
Qec
The Quaternary units in this map area are grouped into the following categories: artificial fill or excavations, hillslope and mass-wasting deposits,
eolian and sheetflood–slopewash deposits, precipitate deposits, alluvial deposits (found on piedmont slopes and alluvial fans), and pediment and
terrace deposits. Alluvial fan deposits are generally found west of the mountain-front fault zone, and piedmont slope deposits east of the mountain-front fault zone (the Alamogordo fault). The latter two categories warrant further discussion. Alluvial fans are geomorphic features characterized by depositional lobes that are fan-shaped in plan-view. On topographic maps, alluvial fans are readily noted by the outward curving or
bulging of contour lines around the mouths of incised, mountain-front drainages. A good example of this bulging of contour lines is seen west of the
mouth of Temporal Creek. Some useful studies that emphasize alluvial fan processes and depositional environments include Hooke (1967), Bull
(1972 and 1977), Blair and McPherson (1994a and 1994b), Blair (1999), and Ritter et al. (1993). East of the Alamogordo fault, distinct alluvial
fan morphology is lacking for extensive Quaternary deposits under westward-sloping, high-level surfaces. We assign the Quaternary deposits east
of the Alamogordo fault as piedmont deposits, which have also been called alluvial slope deposits. Alluvial slope deposits are further discussed
in Hawley and Wilson (1965), Smith (2000), and Kuhle and Smith (2001).
6
Qary
Qay
Qao1
••
••••
••••
••••
•
•
•
Qao
•• • •
Qtg
•• •
• ••
Qay
•• • •
•
Qar
•
•
•• • •
Qay3
Qao1
Qao1
••
•
Qar
Tc
Qar
Qao1
Qao2
Twh
••
•
•
Tim
Qay
Qao2
Qec
Qse
Qay
Qe
Qay2u
Qay2u
Qao2
Qc
Twh
Qay3
afe
•
Qsec/Qao2
Qao
Qec
•
Kc
27
Qay
Qao3
Quaternary–Pliocene Units
Qar
•
Qay
Qay2u
Qe
20'00"
••
Qao2
Qay2
45
Kc
Qay
• • • • •
Qay2 Qay3
•
Ts
Description of Map Units
33°23'30"N
• • • • •
•
Qai
Qar
Qay2
40
55'00"
• • • • •
Qec
Qar
Qsec
Qao2
Qec
Qao2
Qse/
Qao2
Qay3r
afe
••
••
Qay2r
Qay
Qec
••
Qec
Qec
Qe
Qse
Qse
Qay
Qsec/Kc
Qao3
Qar
Twh
Qayr
Tim
Kg
Qay
Qay3
Timp
Qai
Qao2
Qay2
••
••
••
•
• ••
••
••
•
•
••
••
••
Qec
Qsec
18
17
Tim
Qay
Qao2
Qar
Qai
• • • • •
Qe
Qc
Tglta
••••••
•
•
•
•••
•••
••
Qao2
Qec
•
Qec
Qec
28
Qary
Qao2
21
Tgjb
Qay
Qar
Qao1
Kclt
Qsec/
Qao2
Qe
afe
Qay
Qar
Qsec
••
•
Qec
Qar
Qec
Qar
13
••
Qay
•
Qay2
Km
Tgl
Qay2
Qao2
••
9
Tgjpt
Qao2
Qao2
Qar
Twtr
Tgjpt
Qay
Qao1
Kc
Tita
Qao2
Qsec
Qao2
Qay
Kml
Qe
Qao1
Tgjvs
Tgjta
••
•
Qec
Tim
afe
Qao
Qe
••
Qar
•
Qec
Tgjb
Qsec/Qao2
Qec
6
Tim
••
Qse
Qe
Qao
Qay
Qay3
Qe
Qec
28
Tglta
••
•
24
Qao2
Qay2r
25
Qar
Qay1 Qar
105°57'30"W
Tgjpt
••
Qao2
•
Qsec/Qao2
Qe
Qay
Kc
Qao1
••
Kml
Tim
afe
••
• •
Qsec/Qay
Km
Qao2
••
•
Qec
Psf
Qe
Qe
Kd
Qec
Qao
Qao1
••
Qay2
^m
Qay
106°00'00"W
Qar
••
••
•
••
••
•
•
••
••
••
•
••
••
•
•
••
••
•
••
••
•
•
••
••
•
•
••
••
•
•
••
••
••
•
•
•
•
•
•
••
••
••
••
•
••
•
••
•
•
•
••
• •• •
••
••
••
••
••
•
•
••
••
••
••
••
•
•
•
•
••
••
••
••
••
••
•
•
••
••
••
••
•
•
••
••
•
Qe
Qay
••
•
Qec
Psr
Qec
Qse
••
Qsec/Qao2 Qec
02'30"
afe
•••
•
•
••••
•••
•••
••• •
•
•• •• •• •• • • •
• • • • • • •••• • • •
••••
•••
••••
••
••
•• ••
••
•••
••
••
•
•
•
•
••
•• • • • • • •
••
• •••
••
• •• •
••
•
•
•
•• • •
••
••
•• • •
••
••••
••
• •
••
•
•
•
• • • • ••• •
••
• • • • •
• •
• ••••
••
•
•• •• • • •
•• ••
•• •••
•
•
•• •••
••
•
••
•
••
••
•
•
Qao2
Qay
••
05'00"
Qsec
Qay2
••
106°07'30"W
33°23'30"N
NEW MEXICO INSTITUTE OF MINING & TECHNOLOGY
A DIVISION OF
••
•
NEW MEXICO BUREAU OF GEOLOGY & MINERAL RESOURCES
Older allostratigraphic subunit of older alluvium (lower to middle Pleistocene)—Generally a sandy gravel with subordinate to subequal
interbeds of clayey-silty, gypsiferous, very fine- to fine-grained sand containing minor medium to very coarse sand. Finer-grained sediment increases
progressively south of the Three Rivers drainage. Gravel contains pebbles with variable cobbles, locally with minor boulders. Gravel are subrounded to subangular, poorly to moderately sorted, and composed of limestone, intermediate to mafic intrusive rocks, and subordinate sandstone (limestone clasts dominate to the south and igneous clasts dominate to the north). Color of sand ranges from pale brown to very pale brown (10YR
Opensubrounded
File Report
564
6–8/3), pink (5–7.5YR 7/3), or light yellowish-brown to light brown (10–7.5YR 6/4). Sand is very fine NMBGMR
to very coarse-grained,
to
subangular, and moderately to poorly sorted. Very fine- to medium-grained sand is composed mostly of subangular
to
angular
gypsum
grains,
Last Modified 30 June 2014
whereas coarser sand is composed of lithic grains. Base of deposit generally lies several meters above the base of unit Qao2. Surface of unit
typically lies >3 m above the Qao2 surface. Prevalent petrogypsic horizon developed on its surface and very strongly varnished surface
clasts. Moderately consolidated, highly gypsiferous, and variably cemented. Unit is locally strongly cemented near Salinas Draw. 5–25 m-thick.
Clastic sediment, alluvial sediment, mostly coarse-grained. Societal uses: residential development, aggregate potential, low agricultural potential because of gypsic top soil and gravelly texture.
*h
*b
*g
M
D
S–O
_Ob
Fourm e Draw Member—The Fou m e D aw Membe s composed o n e bedded gh g ay do om e da k g ay mes one and am na
ed gypsum The ca bona es con a n oss s bu oss s a e no as common as hey a e n he R o Bon o Membe The e a ve a o o gypsum
o ca bona e nc eases upsec on h ough he membe The h ckness o h s un s unce a n because he op s no exposed h s un s
qu e de ormed The con ac be ween he Fourm e Draw and R o Bon o membe s s ve y g ada ona and s he e de ned o be a he
base o a d s nc ve mes one bed p esen ac oss he map a ea The ma ke mes one s da k g ay oss e ous and has a gypsum bed
ha s abou 6 m h ck be ow The ca bona es above he ma ke mes one become p og ess ve y mo e do om c up sec on The ma ke
mes one s gene a y he h ckes success on o mes one above c s o he R o Bon o Membe bu he ma ke does va y n h ckness
6–24 m average s 12 m The ma ke mes one o ms an eas y aceab e un on poo y exposed gypsum man ed h s The 6 m h ck
gypsum bed s con nuous ac oss he a ea bu h n d scon nuous gypsum and n e ca a ed mes one beds o en occu n he uppe mos R o
Bon o Membe as much as 25 m be ow he mappab e ma ke mes one S m a y h n sequences o da k g ay oss e ous mes one ha
g ade up n o do om e and h ck beds o gypsum a e p esen above he ma ke mes one Es ma ed h ckness s approx ma e y 300 m
Hondo Sands one—The Hondo Sands one s a go d b own o an we so ed med um o ne g a ned qua z a en e w h we ounded
sand g a ns Bedd ng s common y abu a c oss bedd ng s a e The sands one s d scon nuous and anges om 0–10 m h ck The sand
s one whe e p esen s on y 0 7 m h ck on Ca Moun a n UTM 415916E 3670526N NAD27 and s 5–10 m h ck on he wes end o
Coyo e R dge The un cons s s o a s ng e sands one bed ha s 0 5–4 m h ck n he h s us no h o Tempo a C eek An ou c op o Hondo
Sands one a UTM 406593E 3675665N NAD27 ha s n p ox m y o a au con a ns nodu es o ba e nea he op o he exposu e
The sands one un h ckens o 10 m h ck owa d he no hwes us sou h o Sa nas D aw whe e wo sands one beds a e sepa a ed by a
med a do om e ha s 1 m h ck He e he owe sands one s mass ve and he uppe sands one has abu a bedd ng The Hondo Sand
sone s abou 2 m h ck no h o he Sa nas D aw au
R o Bon o Member—Da k g ay h n o h ck bedded oss e ous mes one w h h n o med um bedded gypsum nea he op o he un
Foss s nc ude p oduc d b ach opods c no ds ech node m sp nes and b yozoa agmen s The con ac w h he unde y ng Yeso G oup
s gene a y qu e sha p howeve h n <0 5 m gypsum beds can pe s s a ew me e s above he con ac The R o Bon o Membe s 60–75
m h ck
Yeso Forma on Pe m an —Red and ye ow s s one h n beds o gray mes one and am na ed o h n bedded gypsum dom na e he
basa par o he sec on A 30 m h ck med um bedded mes one o ms a p om nen bed n he m dd e po on o he un The uppe pa o he
Yeso Fo ma on on Ca Moun a n s gypsum w h ye ow and ed s s one and h n bedded mes one Red s s one o en occu s nea he op o he
un n con as he uppe Yeso Fo ma on o he no h o Ca Moun a n s p ma y gypsum and mes one The mes ones a e spa se y oss e ous
con a n ng b ach opods A so a y nau o d 15 cm ac oss was ound n mes one nea he base o he un Sea s a oss s a e a he Yeso/San
And es con ac n he no heas e n pa o he map a ea Onco es a e p ese ved n he mes one a UTM 416913E 3670824N NAD 27 The
Yeso Fo ma on has a g ada ona con ac w h he unde y ng Abo Fo ma on ha s pa cu a y we exposed sou h and sou hwes o Ca Moun
a n The ed a kos c sands one and ed and g een muds one o he Abo Fo ma on g ade upwa d n o h n beds o b ack and g een sha e
ne g a ned g een and ye ow sands one and h n beds o gypsum and mes one The uppe con ac s g ada ona w h he San And es Fo ma on
Ke ey 1971 measu ed a comp e e sec on o Yeso Fo ma on on he Ca Moun a n quad ang e n he v c n y o Coyo e Peak n T13S R10E Sec
21 and 22 Max mum h ckness s 372 m
Abo Forma on Pe m an —B ck ed sands one muds one s s one and cong ome a e The Abo Foma on s dom na ed by muds one 50% and
a kos c sands one and cong ome a e 40% Foss e ous mes one and pedogen c ca bona e wh ch a e p ma y ound n he basa 150 m make
up he es o he un O e 1959 Sands ones a e c oss bedded o abu a coa se o med um g a ned and poo y o mode a e y so ed Angu a
o sub ound qua z o hoc ase e dspa and muscov e a e common sand g a ns Cong ome a es con a n we ounded c as s o P o e ozo c qua z
e P o e ozo c hyo e po phy y che o unce a n age and sands one Th n oss e ous mes one beds ha a e 0 2–0 7 m h ck occur oca y
nea he ans ona base o he un Th n 4–20 cm che beds are ound us above he con ac w h he Bu sum Fo ma on and above a h n 0 2
m mes one bed a UTM 408507E 3666281N NAD 27 Pe ed wood s p ese ved n he Abo Fo ma on a UTM 408658E 3664679N
NAD27 Ma ach e and hema e m ne a za on s assoc a ed w h he Abo Fo ma on 427–550 m h ck O e 1959 Spee 1983 Th ckness
o Abo s 530–630 m a he no h
Bursum Forma on La e Pennsy van an o Ea y Pe m an —F uv a sands one and muds one n e bedded w h oss e ous ma ne mes one and
b ack sha e F ne g a ned uv a depos s n he Bu sum Fo ma on cons s o edd sh g ay and da k edd sh g ay muds one and sandy c ays one
whe e he m no sand s ve y ne o coa se g a ned and a kos c Sands one and pebb y sands one occupy med um o h ck en cu a o abu a
channe s n e na bedd ng s mass ve o p ana am na ed o n ve y h n o med um p ana o en cu a beds Channe
sed men s
p nk sh gray o redd sh gray o p nk sh gray Sand s ne o ve y coa se g a ned mos y med um o ve y coa se g a ned angu ar o mos y
subangu ar o subrounded mode a e y so ed and s a kos c o h c a kos c L mes one s composed o med um o h ck mos y h ck abu a
m c c o b oc as c beds ha a e g ay o gh g ay Ma ne sha es a e g ay and p ana o s gh y wavy am na ed S a a a e yp ca y s ong y
cemen ed a hough he sha es a e ab e n add on he Bu sum Fo ma on con a ns beds o poo y so ed cong ome a e up o seve a me e s
h ck w h pebb e o cobb e s zed ounded o sub ounded qua z e and angu a o sub ounded hyo c po phy y c as s as we as cong ome a c
beds dom na ed by mes one c as s The un ep esen s he ans on om p edom nan y ma ne cond ons ha ex s ed du ng depos on o he
unde y ng Pennsy van an Ho de Fo ma on o a e es a env onmen du ng depos on o he ove y ng Pe m an Abo Fo ma on A ga b ohe ms
w h abundan c no d s ems p ese ved a he op ha a e oca ed us no heas o Tu a osa have been s ud ed n some de a e g Scho e e a
2007 B yozoans and b ach pods a e o he common oss s on he mounds Th s un s equ va en o he Lab oc a Fo ma on o O e 1959 Lucas
and K a ne 2004 based on eg ona s udy o hese ans on beds have conc uded ha he depos s be ong n he Bu sum Fo ma on he name
"Labo c a" may be e a ned as a membe o he Bu sum Fo ma on n he no he n Sac amen o Moun a ns The age ass gnmen o he Bu sum
Fo ma on s a so unde go ng con nued d scuss on S G Lucas pe sona commun ca on 2009 Based on No h Ame can usu n d b os a g a
phy he bu k o he Bursum Forma on n he Sacramen o Moun a ns s Wo camp an ad ona y cons de ed o be Lowe Pe m an Recen
b os a g aph c s ud es based on conodon s howeve sugges ha owe mos Wo camp an s a a n No h Ame ca may u ma e y be cons de ed
Uppe Ca bon e ous n he g oba scheme A any a e he hos a g aph c base o he o ma on n he map a ea s g ada ona w h he unde y
ng Ho de Fo ma on and s chosen a he op o a a e a y con nuous compa a ve y h ck bed o ma ne mes one ass gned o he op o he
Pennsy van an Ho de Fo ma on he basa Bu sum depos s cons s ng o a success on o edd sh and g een sh s s one and sands one w h
n e beds o mes one and oca y a bed o mes one cong ome a e nea he base o he o ma on We o owed O e 1959 by us ng a con nu
ous mes one bed O e s bed 55 o ma k he g ada ona op con ac be ween he Bu sum and he Abo o ma ons Es ma ed h ckness eas o
Tu a osa s 170–300 m h cken ng om sou h o no h ac oss he map a ea O e 1959 K ng and Ha de 1985 n e p e he Bu sum Fo ma on
o be 280–328 m h ck n Hous on Fed A 1 and Hodges Hous on 1 espec ve y
Ho der Forma on Uppe Pennsy van an — n e bedded da k co o ed ma ne sha e and oss e ous mes one con a n ng beds o sands one
edd sh o ma oon muds one and occas ona beds o mes one cong ome a e nea he op and ma ne ca bona e da k co o ed sha e and a ga
b ohe ms n he owe po on o he o ma on The base o he o ma on s no exposed n he map a ea As d scussed above he op o he Ho der
Forma on s grada ona w h he ove y ng Bu sum Fo ma on n he map a ea Es ma ed o be abou 275 m h ck us sou h o he map a ea
O e 1959 and n erpre ed o be 121 m n Hous on O and M ne a s 1 S a e
Beeman Forma on Pennsy van an subsu ace on y —Th n beds o a g aceous mes one n e bedded w h ca ca eous sha e w h do om e and
d scon nuous a kos c sands one nea he base Kon ng e a 2007 Es ma ed o be 110–150 m h ck and n erpre ed o be 265 m h ck n Hous
on O and M ne a s 1 S a e
Gobb er Forma on Pennsy van an subsu ace on y —Sha e and qua z sands one o m he op o he un he unde y ng med a Bug Scu e
L mes one g ades upwa d n o he uppe un The owe Gobb e Fo ma on s composed o sha e and che y mes one w h m no coa se g a ned
sands one ne pebb y sands one and sandy che cobb e cong ome a e Kon ng e a 2007 ~400 500 m h ck
Lake Va ey Forma on M ss ss pp an subsu ace on y —The Lake Va ey Fo ma on nc udes ca ca eous sha e muds ones h n bedded
mes one and m no qua zose s s one C no d bea ng b ohe m mounds a e common n he m dd e o he o ma on Th ckness va es om a max
mum o nea y 80 m o a mo e usua 50 m n a eas nea mounds The o ma on s cons de ab y h nne 15–20 m away om he b ohe m mounds
Kon ng e a 2007 n e p e ed o be 146 m h ck n Hous on O and M ne a s 1 S a e
Oña e S y Gap and Percha Sha e Forma ons Devon an subsu ace on y —Da k g ay o b own sh g ay s y do om e do om c s s ones and
ve y ne g a ned qua z sands ones L gh g ay ca ca eous sha es a e common oward he base and b ack non ca ca eous sha es a e common
a he op o he sec on Pebb y sands ones occurr ng oca y a ong he base are n ayers no very res s an o eros on Un s poor y
exposed and common y covered by co uv um The uppe con ac s a d scon o m y Kon ng e a 2007 15–30 me e s h ck mos y ~30 m
h ck
Fusse man Forma on S u an Va mon Do om e Mon oya Forma on E Paso Forma on O dov c an subsu ace on y —Lowe Pa eozo c
do om e and che w h m no sha e Sandy do om e and h n o med um beds o qua z sands one a e p esen nea he base o h s comb ned
un Kon ng e a 2007 225–288 m h ck
B ss Sands one Camb o–O dov c an —Exposed on he Ben dome F ne o coa se g a ned we so ed qua z sands one Sand g a ns a e
we ounded o sub ounded qua z che and ace e dspa ha a e n p aces cemen ed by ca bona e and n o he s by qua z ove g ow hs
Baue and Loz nsky 1991 Bedd ng s abu a o c oss bedded and pp e ma ks a e p esen The sands one s gene a y an n co o bu con a ns
g aucon e ha oca y causes he sands one o be g een nea he base Baue and Loz nsky 1991 27–34 me e s h ck
p_d
D or e P o e ozo c? —Exposed on he Ben dome G ay po phy c p u on c ock w h a med um g a ned ma x o a ka e dspa p ag oc ase
and a e ed ho nb ende py oxene and b o e Baue and Loz nsky 1991
p_g
Gran e P o e ozo c? —Exposed on he Ben dome Red coa se g a ned p u on c ock w h a ka
opaque m ne a s Baue and Loz nsky 1991
e dspa p ag oc ase qua z b o e and
Comments to Map Users
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
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