NEW MEXICO BUREAU OF MINES AND MINERAL RESOURCES
PA
RK
)
(S
AN
DI
A
l
ll
ll
l l ll
l
Xq
llll
l l l ll l
ll
lll l
ll
ll
l l ll
l
l lllll
llll
llll
l l ll
l ll l
l
ll
l l ll
l
ll
llll
llll
llll
llll
llll
llll
l
lll
7000 FEET
NEW MEXICO
0
1 KILOMETER
QUADRANGLE LOCATION
Armstrong, A. K. and Mamet, B. L., 1974, Biostratigraphy of the Arroyo Peñasco Group, Lower Carboniferous (Mississippian),
North-Central New Mexico, in: New Mexico Geological Society, 25th Field Conference Guidebook, p. 145-158.
Brookins, D. G., 1982, Radiometric ages of Precambrian rocks from central New Mexico: New Mexico Geological Society
Guidebook 33, p. 187-189.
by Karl E. Karlstrom 1 , Sean D. Connell 2, Charles A. Ferguson 3 , Adam S. Read 4 ,
Glenn R. Osburn 5 , Eric Kirby 1 , John Abbott 6 , Christopher Hitchcock 7 ,
Keith Kelson 7 , Jay Noller 7 , Thomas Sawyer 7 , Steven Ralser 6 ,
David W. Love 4 , Matthew Nyman 1 , and Paul W. Bauer 4
Madera Formation, undivided — Two informal members, an arkosic limestone and a gray limestone, are
recognized but not differentiated. The upper and lower members are respectively generally correlative to the
Wild Cow Formation and Los Moyos Limestone (Formation) of the Madera Group of Myers and McKay (1976).
These informal member names are used because the units were lithostratigraphically defined on the Sedillo
(Read et al., 1999) and Tijeras (Karlstrom et al., 1994) 7.5-minute quadrangles rather than biostratigraphically
defined and may therefore not strictly correlate with the units defined by Myers and McKay (1976). The Madera
Group nomenclature was abandoned because of the gradational contacts between members and the difficulty
of distinguishing these contacts in the field. Total thickness is approximately 1,320 ft (402 m) near Cedro Peak
to the southeast (Myers and McKay, 1976) and 1,260 ft (385 m) on the Crest of Montezuma (Picha, 1982)
to the north (consistent with thickness estimates based on map relationships in the study area).
.
˛m
Morrison Formation, undivided — Three members are commonly recognized in northern New Mexico but
are not differentiated in this map area. In descending stratigraphic order, the members are: the Jackpile
Sandstone, the Brushy Basin Shale, and the Salt Wash Sandstone (the Westwater Canyon Sandstone of former
usage, Lucas et al., 1995). The Recapture Shale member has been redefined by Lucas et al. (1995) as the
Summerville Formation of the upper San Raphael Group (Lucas and Anderson, 1997). Due to poor exposure
in the study area, these units are not differentiated. Medium- to thick-bedded, light-colored, generally poorlysorted, feldspathic sandstones, with green and red shaley interbeds. Sandstones contain abundant quartz
granules and greenish mud-chip clasts, and the feldspar grains are typically strongly altered to white clay
minerals. The upper part of this unit, in some areas, is a moderately to well-sorted, moderately bioturbated
feldspathic sandstone which may be equivalent to the Jackpile Member. Abundant dark grayish-green shaley
intervals with thin dark-colored micritic limestones are present in some areas near the base of the map unit.
Total thickness is approximately 500 ft (150 m).
˛m u
Entrada and Todilto Formations, undivided — Cross section only. Estimated total thickness is up to 100 ft
(30 m).
Todilto Formation (chiefly Luciano Mesa Member) — In most areas the only part of this unit that is exposed
is the Luciano Mesa Member, a laminated, fetid, dark-gray, micritic limestone. Laminations in the limestone
appear to be algal in origin and consistently lack of macrofossils. Rarely, the overlying Tonque Arroyo Member,
a thin-bedded to laminated gypsum unit is preserved.
Entrada Formation — A poorly exposed, light green-colored, massive (bioturbated?) sandstone unit that rarely
displays high-angle cross-stratification.
Je
˛m l
Upper Triassic
Chinle Group, undivided (probably Petrified Forest Formation) — Mudstone with lenticular beds of
lavender-gray sandstone; mudstones are reddish-brown to orange-tan in the upper part, and purple to reddishbrown in the lower part. Green reduction spots are common, as are local limestone-pebble conglomerate
lenses, particularly near the base of the unit. Total Chinle Group thickness is about 1,300 ft (400 m).
.
ˇc
ˇz
Chinle Group, Agua Zarca Formation — The only distinct sub-unit of the Chinle Group recognized
during this study (differentiated where possible). It is a tan- to light-grayish pink, resistant, thin- to mediumbedded quartz arenite and feldspathic arenite. The lower contact with the underlying Moenkopi Formation
(ˇm) is disconformable. The unit is about 350 ft (105 m) thick.
ˇm
PALEOZOIC ROCKS
Upper Permian
Ps
Pg
San Andres and Glorieta Formations, undivided — The upper two lithostratigraphic units of the Permian
are complexly interleaved. The lithotypes, which may not strictly correlate with formations of the same names,
are gray limestone (San Andres, Ps) and white quartz arenite (Glorieta, Pg). These were differentiated where
possible.
San Andres Formation — Light gray and less commonly tan colored, medium- to thick-bedded limestone.
The limestones are mostly micrites or skeletal wackstones, commonly with some component of quartz sand.
The San Andres Formation is interbedded with the Glorieta Formation (Pg) with a total upper Permian (Ps and
Pg) thickness of approximately 400 ft (120 m).
Pegmatite dikes — Pegmatite dikes, pods, and lenses ranging from <1 in to >50 ft (<30 cm to >15 m) in
thickness and up to about 3,000 ft (915 m) in length; interpreted to be coeval with the Sandia granite (Ys).
Yps
Sandia granite porphyry — Fine- to med- grained phase of the Sandia granite (Ys) with scattered K-feldspar
phenocrysts (up to several cm). Interpreted to be coeval with the intrusion of the Sandia granite.
.
Glorieta Formation — White and pink (along the contact with the underlying Yeso Formation), massive or
plane-bedded to low-angle planar cross-stratified quartz arenite. Locally, the sandstones are extensively
bioturbated by Macaronichnus, and near the contact with Yeso Formation they are feldspathic. The sandstones
are typically well sorted, but a thin, feldspathic quartz-pebble conglomerate occurs just below the base of the
lowermost San Andres Formation limestone in the Arroyo Armijo area along the boundary between Sandia
Park and Sandia Crest quadrangles. These sandstones and the limestones of the San Andres Formation are
interbedded with each sandstone bed generally less than 30 ft (10 m) thick.
Abo and Yeso Formations, undivided — The lower two lithostratigraphic units of the Permian represent a
red-colored feldspathic to quartzose siliciclastic sequence that, because of generally poor exposure, was
mapped as a single unit throughout the study area. The Yeso Formation is a reddish to pink or tan-colored,
medium- to thin-bedded, feldspathic sandstone, shale and silty shale with interbedded massive or laminated
micritic gray or tan limestone (Pyc) near the top. The sandstones are typically cross-stratified and/or crosslaminated and virtually identical to those within the underlying Abo formation except that, rarely, salt hopper
casts and molds are present. The Abo Formation is a red and locally tan-colored (particularly near the base),
medium- and thin-bedded arkose and feldspathic sandstone interbedded with red, micaceous siltstone and
shale, commonly with green reduction spots. The lowermost arkoses are typically lighter-colored and coarsergrained than the younger feldspathic sandstones, and at least one of them is strongly bioturbated (Macaronichnus).
B
B'
Yss
40
68
86
Lucas, S.G. and Anderson, O.J., 1997, The Jurassic San Rafael Group, Four Corners region, in: New Mexico Geological Society,
48th Field Conference Guidebook, p. 115-132.
Myers, D. A., and McKay, E. J., 1976, Geologic map of the north end of the Manzano Mountains, Tijeras and Sedillo quadrangles,
Bernalillo County, New Mexico: U.S. Geological Survey Miscellaneous Investigations Series, I-968, scale 1:24,000.
GILMAN
late
Qpm2
SAN
YSIDRO
OF-DM–18
LOMA
CRESTON
JEMEZ
PUEBLO
OF-DM–25
SANTO
DOMINGO
PUEBLO
SANTA
ANA
PUEBLO
HORCADO
RANCH
WHITE
ROCK
GM–73
CERRO BERNALILLO
CONEJO
NW
SAN
FELIPE
PUEBLO NE
OF-DM–19
OF-DM–37
PLACITAS
OF-DM–2
BENAVIDEZ
RANCH
VOLCANO
RANCH
LA MESITA
NEGRA
DALIES
NW
RIO
PUERCO
ALAMEDA
285
OF-DM–32
25
DALIES
PICTURE
ROCK
MADRID
OF-DM–40
BELEN
ROSILLA
PEAK
PECOS
BULL
CANYON
GALISTEO
OF-DM–1
OF-DM–4
HUBBELL
SPRING
35°15'
105° 30'
OF-DM–29
OF-DM–13
OF-DM–5
OF-DM–8
LOS
LUNAS
SE
BOSQUE
PEAK
1:12,000
EDGEWOOD MORIARTY
OF-DM–35
NORTH
CHILILI
1:12,000 and 1:24,000
35°00'
1:12,000
MORIARTY
SOUTH
1:12,000
1:12,000
TAJIQUE
MILBOURN
RANCH
ESTANCIA
TORREON
EWING
MOUNTAINAIR
NE
TOME
CAPILLA
PEAK
TOME NE
VEGUITA
TURN
BELEN
SW
LA JOYA
NW
1:12,000
TOME SE
MANZANO PUNTA DE
MOUNTAINAIR
PEAK
AGUA
WILLARD
B ELEN 1:100,000
S OCORRO 1:100,000
ABEYTAS
LADRON
BLACK
BUTTE
34°30'
106°00'
BECKER
1:12,000 1:12,000
SCHOLLE
34° 22' 30"
LA JOYA
SILVER
CREEK
SAN
ACACIA
BECKER
SW
CERRO RAYO HILLS
MONTOSO
107°
109°
1:12,000
LEMITAR
MESA
DEL
YESO
Taos
SIERRA
DE LA
CRUZ
WATER
CANYON
SOCORRO
35°
Karlstrom (pÇ mapping of entire
quad)
SANTA FE
Grants
OF-DM–38
LOMA
DE LAS
CANAS
Albuquerque
BUSTOS
WELL
Connell & Love (Q mapping of
entire quad)
Socorro
Read, A. S., Karlstrom, K. E., Ilg, B., 1999, Mississippian Del Padre Sandstone or Proterozoic Quartzite?: New Mexico Geological
Society, 50th Field Conference Guidebook, p. 41-45.
Richey, S. F., 1991, Construction, lithologic, and geophysical data from monitoring wells in Albuquerque, Bernalillo County, New
Mexico: U.S. Geological Survey, Open-File Report 90-578, 83 p.
.
Ferguson & Osburn
33°
Deming
Las
Cruces
Nyman & Bauer
Location Map
Stearns, C. E., 1953, Tertiary geology of the Galisteo-Tonque area, New Mexico: Geological Society of America Bulletin, v. 64,
p. 459-508.
Overturned syncline —Trace of axial plane showing direction of plunge; dashed where approximately located,
dotted where concealed, queried where inferred
Steiger, R. H., and Wasserburg, G. J., 1966, Systematics in the Pb208 -Th207-U235, and Pb206 -U238 systems: Journal of Geophysical
Research, v. 71, p 6065-6090.
Szabo, E., 1953, Stratigraphy and paleontology of the Carboniferous rocks of the Cedro Canyon area, Manzanita Mountains,
Bernalillo County, New Mexico: [M.S. thesis], University of New Mexico, 137 p.
Tilton, G. R., and Grunenfelder, M. H., 1968, Uranium-lead ages, Science, v. 159, p. 1458-1461.
Horizontal bedding; overturned bedding
.
Qpo
Qpx 1
QTp
QTpx
? ?
QTsp
Tmi
Kv
Kvs
Km
Kms
Kvt
Kvm
Kd
Abbott
Nyman
Brown
Ralser
Kirby
Read
Jm
Jt
Je-t
Je
ˇc
ˇz
ˇm
556
SANDIA
MOUNTAINS
Cedar
Crest
14
Tijeras
Thomas, E., Van Hart, D., McKitrick, S., Gillentine, J., Hitchcock, C., Kelson, K., Noller, J., and Sawyer, T., 1995, Conceptual
geologic model of the Sandia National Laboratories and Kirtland Airforce Base: Technical Report, Site-Wide Hydrogeologic
Characterization Project Organization 7584, Environmental Restoration Program. Prepared by GRAM, Incorporated,
Albuquerque, New Mexico; and William Lettis and Associates, Oakland, California, Section 2 and Appendix D.
.
.
QTt
106° 30'
35°07' 30"
Smith, L. N., Bullard, T. F., and Wells, S. G., 1982, Quaternary geology and geomorphology of Tijeras Canyon, New Mexico:
New Mexico Geological Society, 33rd Field Conference Guidebook, p. 5-8.
Overturned anticline—Trace of axial plane showing direction of plunge; dashed where approximately located,
dotted where concealed, queried where inferred
? ?
OF-DM–34
107°00'
Read, A. S., Allen, B. D., Osburn, G. R., Ferguson, C. A., and Chamberlain, R., 1998, The Geology of the Sedillo quadrangle,
Bernallio County, New Mexico: New Mexico Bureau of Mines and Mineral Resources, Open-file Digital Geologic Map OFDGM 20, scale 1:24,000.
Thrust fault —Tic showing dip; solid where exposed, dashed where approximately located, dotted where
concealed; triangular teeth on upthrown side of thrust
Qpx 2
Paleogene
35°00'
106°22'30"
103°
105°
106°30'
SAN
LORENZO
SPRING
Qvm 1
OF-DM–24
OF-DM–27
COMANCHE
RANCH
Qvm t1
THIS STUDY
OF-DM–20
MOUNT
ESCABOSA
WASHINGTON
Qpm1
Qvm t
LAGUNA
ORTIZ
106°30'
35°07'30"
A LBUQUERQUE 1:100,000
ISLETA
Cavin (1985)
Thomas, et al. (1995)
OF-DM–39
OF-DM–6
Connolly (1981)
35°30'
NORTH
ROWE SAN YSIDRO
OJO
WILDHORSE
RENCONA
HEDIONDA
MESA
KING
DRAW
Myers & McKay (1976) (so. of I-40)
LOWER
COLONIAS
285
CAPTAIN
DAVIS
MOUNTAIN
OF-DM–48
Kelley & Northrop (1975) (entire quad)
OF-DM–11
GOLDEN
SAN
PEDRO
SEDILLO
35°00'
106°22'30"
HONEY
BOY
RANCH
S ANTA F E 1:100,000
OF-DM–30
HAGAN
40
1:12,000
OF-DM–31
OF-DM–7
OF-DM–49
OF-DM–36
OF-DM–3
OF-DM–21
BELEN
NW
PECOS
FALLS
ELK
MOUNTAIN
McCLURE
RESERVOIR
OF-DM–23
SANDIA
PARK
OF-DM–17
LOS
LUNAS
36°00'
GLORIETA
OF-DM–41
OF-DM–50
TIJERAS
LA MESITA
ALBUQUERQUE
NEGRA SE ALBUQUERQUE
EAST
WEST
WIND
MESA
JICARITA
PEAK
V ILLANUEVA 1:100,000
OF-DM–10
1:24,000
1:7,200 and
1:24,000
? ?
? ?
COWLES
SANTA FE
AGUA
FRIA
SANDIA
CREST
OF-DM–16
LOS
GRIEGOS
TRUCHAS
PEAK
ASPEN
BASIN
TETILLA
PEAK TURQUOISE SETON
HILL
VILLAGE
BERNALILLO
OF-DM–9
SIERRA
MOSCA
CUNDIYO
Qvm 2
1:8,000
OF-DM–47
MONTOSO
PEAK
OF-DM–15
SAN
FELIPE
PUEBLO
EL VALLE
TESUQUE
L OS A LAMOS 1:100,000
OF-DM–14
TRES
RITOS
T AOS 1:100,000
Santa Fe
SANTO
DOMINGO
PUEBLO SW
PEÑASCO
Qvm t2
SHADY
BROOK
84
GM–45
ARROYO
LOMA
SAN
DE LAS
MACHETE
FELIPE
CALABACILLAS
MESA (SKY VILLAGE SE)
(SKY VILLAGE)
COCHITI
DAM
OF-DM–33
Qsct
Arroyo
eras
Tij
40
Ca
Tijeras
337
Physiography of the Tijeras area
based upon 10-m USGS DEM data.
Ps
Psg
Pg
Pay
˛m
Pyc
˛m u
˛m l
˛s
Ma
METASEDIMENTARY
METAVOLCANIC
PLUTONIC
Ys
Ye
Strike and dip of joint or fracture; vertical joint or fracture
80
75
Strike and dip of S2 foliation
56
Magmatic foliation in granite defined by alignment of mafic enclaves
22
Magmatic foliation in granite defined by alignment of feldspar megacrysts
23
Strike and dip of pegmatite or aplite dikes and veins
A, S, K
Biotite granite — Biotite-rich, medium-grained, massive to foliated granite; occurs as mixed zones in the
Manzanita granite.
Metamorphic mineral occurrences and assemblages: K = kyanite; A = andalusite; A,S = andalusite + sillimanite;
A,S,K = andalusite+sillimanite+K-spar; A,St,Cd = andalusite+staurolite+chloritoid; A,S,Cd =
andalusite+sillimanite+chloritoid; S,K = sillimanite+K-spar
ll
5
4H
Quarry
Geochronologic sample location (U-Pb, 14C, etc.; see table and unit descriptions)
M A N ZANITA
MOUNTAINS
Table of Geochronologic Samples
Locality
Date
Formation
1
2
3
1,790 ±90 BP
1,423±2 Ma
1,455±12 Ma
1,437±47 Ma
1,446±26 Ma
1,422±3 Ma
1,423±2 Ma
1,632±45 Ma
1,659±13 Ma
Qayt
Xcm(sz)
Ys
Ys
Ys
Ys
Xq
Xcm
Xcm
Prospect
l
Yp
Xmg
ALBUQUERQUE
Strike and dip of S1 foliation, arrow indicates trend and plunge of lineation defined by elongate minerals and
stretched grains
45
lll
CAÑADA
OF-DM–42
OF-DM–12
Qvm 3
36°30'
Picha, M. G., 1982, Structure and stratigraphy of the Montezuma salient-Hagan basin area, Sandoval County, New Mexico: [M.S.
thesis]: Albuquerque, University of New Mexico.
Reverse fault —Tic showing dip; solid where exposed, dashed where approximately located, dotted where
concealed; square teeth on upthrown side
Strike and dip of bedding
BEAR
PONDEROSA SPRINGS
PEAK
ESPAÑOLA
GUAJE
MOUNTAIN
TAOS SW
RANCHOS
DE TAOS
Qvm t3
Qpx 3
PUEBLO
PEAK
Parchman, M. A., 1981, Precambrian geology of the Hell Canyon area, Manzano Mountains, New Mexico: [M.S. thesis], University
of New Mexico, Albuquerque, NM, 108 p.
Minor fold axis, trend and plunge, with map view sketch of fold
55
BLAND
TRUCHAS
PUYE
Los
Alamos
FRIJOLES
REDONDO
PEAK
CHIMAYO
Mieras, B. L., Sageman, B. B., Kauffman, E. G., Caldwell, W. G. E., Kauffman, E. G., 1993, Trace fossil distribution patterns in
Cretaceous facies of the Western Interior Basin, North America, in: Evolution of the Western Interior Basin, Special Paper Geological Association of Canada, v. 39, p. 585-620.
.
Location of geologic cross section
Slickensides on fault or minor fault
54
OF-DM–43
Qpm3
1:48,000
37°
Breccia or gouge zones
30
WHEELER
PEAK
GM–71
a
Lucas, S. G., Anderson, O. J., and Pigman, C., 1995, Jurassic Stratigraphy in the Hagan Basin, North-Central New Mexico, in:
New Mexico Geological Society Guidebook, 46th Field Conference Guidebook, p. 247-255.
.
Shear zone —Tic showing dip
65
Leucocratic granite and aplitic granite — Light-colored biotite-poor granite in dikes and pods within the
Manzanita granite.
Xbg
Lucas, S. G., Williamson, T. E., and Sobus, J., 1993, Plio-Pleistocene stratigraphy, paleoecology, and mammalian biochronology,
Tijeras Arroyo, Albuquerque area, New Mexico: New Mexico Geology, v. 15, n. 1, p. 1-8.
Syncline— Trace of axial plane showing direction of plunge; dashed where approximately located, dotted
where concealed, queried where inferred
Paleoproterozoic rocks
Xmg
HOLY
GHOST
SPRING
JEMEZ
SPRINGS
VALLE
TOLEDO
OF-DM–28
Anticline — Trace of axial plane showing direction of plunge; dashed where approximately located, dotted
where concealed, queried where inferred
Mafic enclaves — Cross section only. A high density of ellipsoidal enclaves of microdiorite. These mafic
enclaves often define magmatic foliation within the Sandia granite.
Manzanita granite — Strongly foliated very coarse-grained biotite monzogranite (biotite is chloritized). UPb zircon date of 1,645 ±16 Ma (Brown et al., 1999) from the Mt. Washington 7.5-minute quadrangle
(Karlstrom et al., 1997a).
Lambert, P. W., 1968, Quaternary stratigraphy of the Albuquerque area, New Mexico: [Ph.D. dissertation]: Albuquerque, University
of New Mexico, 329p.
Normal fault —Tic showing dip, arrow showing trend and plunge of slickensides where measurable; solid where
exposed, dashed where approximately located, dotted where concealed, queried where inferred; ball and
bar on downthrown side, upthrown (U) and downthrown (D) sides indicated where concealed and/or interpreted
50
Ye
Xlg
GM–34
SEVEN
SPRINGS
OF-DM–45
(SKY VILLAGE NE)
Kirby, E., Karlstrom, K. E., and Andronicus, C. L., 1995, Tectonic setting of the Sandia pluton: An orogenic 1.4 Ga granite in New
Mexico: Tectonics, v. 14, p. 185-201.
Geologic contact —solid where exposed, dashed where approximately located; dotted where concealed
.
Geologic contact based upon interpretation of aerial photography
85
Sheared Sandia granite — Plastically deformed megacrystic monzogranite to granodiorite, enriched
in biotite due to depletion of quartz-feldspar from the matrix.
GM–28
(SKY VILLAGE NW)
Kelley, S. A., Chapin, C. E., and Corrigan, J., 1992, Late Mesozoic to Cenozoic cooling histories of the flanks of the northern
and central Rio Grande rift, Colorado and New Mexico: New Mexico Bureau of Mines and Mineral Resources Bulletin 145,
39 p.
E XPLANATION OF M AP S YMBOLS
Sandia granite — Mainly megacrystic biotite monzogranite to granodiorite. K-feldspar megacrysts, up to
several cm long, are commonly aligned in a magmatic foliation; contains numerous ellipsoidal enclaves of
microdiorite, fine-grained granite, and gabbro (interpreted to be mingled mafic magmas, Ye), and xenoliths
of quartzite, mica schist, and mafic metavolcanic rock. Pegmatites (Yp), aplites (Ya), and quartz veins are
ubiquitous. Various dates are available from geochronologic sample Locality 3: U-Pb zircon plus sphene
1,455±12 Ma (Tilton and Grunenfelder, 1968, recalculated by S. Getty, unpublished); U-Pb zircon of 1,437±47
Ma (Steiger and Wasserburg, 1966, recalculated in Kirby et al., 1995); U-Pb zircon of 1,446±26 Ma (D.
Unruh, unpublished data); Locality 3 also has 40Ar/39Ar analyses from hornblende of 1,422±3 Ma (Kirby
et al., 1995); Locality 2 has an 40Ar/39Ar date of 1,423 ±2 Ma (Karlstrom et al., 1997b).
.
Ys
SAN
MIGUEL
MOUNTAIN
VALLE
SAN
ANTONIO
OF-DM–26
Kelley, V. C., and Northrop, S. A., 1975, Geology of the Sandia Mountains and vicinity: New Mexico Bureau of Mines and
Mineral Resources Memoir 29, 136p.
Machette, M. N., 1978, Geologic map of the San Acacia Quadrangle, Socorro County, New Mexico: U.S. Geological Survey,
Geologic Quadrangle Map GQ-1415, scale 1:24,000.
Aplite dikes — Light colored, fine- to medium-grained, and often sugary-textured aplite dikes consist of quartz,
orthoclase, accessory muscovite, and in places are garnet-bearing (Kelley and Northrop, 1975). These dikes
are generally thin planar dikes but may also be pods and stringers (up to approximately 500 ft, or 150 m, in
diameter); interpreted to be coeval with the Sandia granite (Ys).
Yp
Lower Permian
Pay
Xr
VELARDE TRAMPAS
TRAMWAY BLVD.
Psg
Madera Formation, lower gray limestone — A sequence of often fossiliferous and massively bedded
cliff-forming wavy laminated and cherty micritic limestone interbedded with shales. Shale is particularly
abundant near the base of this member where it grades into the Sandia Formation. Generally correlative
with the Los Moyos Limestone of Myers and McKay (1976).
PROTEROZOIC ROCKS
Mesoproterozoic igneous rocks
Ya
LA
VENTANA
COLLIER
DRAW
Kelley, V. C., 1977, Geology of the Albuquerque basin, New Mexico: New Mexico Bureau of Mines and Mineral Resources
Memoir 33, 60p.
Metarhyolite and to felsic metavolcanic rock — Coarse-grained, buff to reddish-orange felsic metavolcanic
rock, commonly banded, locally contains quartz and feldspar phenocrysts. Includes Tijeras felsic metavolcanics
of Connolly, (1981).
30
Moenkopi Formation — A recessive-weathering, dark red-colored micaceous shale, silty shale and thinbedded feldspathic sandstone. Approximately 200 ft (60 m) thick.
GM–27
OJITO
SPRING
Karlstrom, K. E., Dallmeyer, R. D., Grambling, J. A., 1997b, 40Ar/39Ar evidence for 1.4 Ga regional metamorphism in New
Mexico: Implications for thermal evolution of lithosphere in the southwestern USA: Journal of Geology, v. 105, p. 205-223.
Mafic metavolcanic rocks — Heterogeneous unit consisting of massive to schistose metabasalt and metaandesite with subordinate chlorite phyllite and schist of volcaniclastic origin. Coarse dioritic units may locally
intrude the volcanic rocks. Includes the Tijeras greenstone of Connolly (1981), Coyote greenstone of Cavin
(1985), and Isleta metavolcanics of Parchman (1981).
Xmv
Arroyo Peñasco Group, Espiritu Santo Formation(?) — A poorly exposed outcrop of sandstone and
limestone along a splay of the Tijeras fault. Several measured sections of thin remnants of the Arroyo Peñasco
Group were described by Szabo (1953) and Armstrong (1967) but remain undifferentiated on this map (see
the Sandia Formation description above).
Middle and Lower Triassic
GM–26
GM–33
Karlstrom, K. E., Chamberlain, R. M., Connell, S. D., Brown, C., Nyman, M., Calvin, W. J., Parchman, M. A., Cook, C., Sterling,
J., 1997a, Geology of the Mount Washington 7.5-minute quadrangle, Bernalillo and Valencia Counties, New Mexico: New
Mexico Bureau of Mines and Mineral Resources, Open-file Digital Geologic Map OF-DM 8, scale 1:24,000.
.
Metamorphosed dacitic tuff — Gray to light green metavolcanic and volcaniclastic schist and phyllite with
local fragments of phyllite, chlorite phyllite, greenstone, and jasper.
Xdt
Mississippian
Ma
SAN
PABLO
RANCHO
DEL
CHAPARRAL
OF-DM–22
68
SAN
JUAN
PUEBLO
A BIQUIU 1:100,000
Karlstrom, K. E., 1999, Southern margin of the Sandia pluton and the “Cibola problem:” minipaper in: New Mexico Geological
Society, 50th Field Conference Guidebook, p. 30.
Coarse-grained Cibola monzogranite — Two-mica monzogranite, contains scattered cm-size phenocrysts.
LOS
CORDOVAS
30 km
285
Ferguson, C. A., Timmons, J. M., Pazzaglia, F. J., Karlstrom, K. E., Osburn, G. R., Bauer, P. W., 1996, Geology of the Sandia Park
7.5-minute quadrangle, Bernalillo and Sandoval Counties, New Mexico: New Mexico Bureau of Mines and Mineral Resources,
Open-file Digital Geologic Map OF-DM 1, scale 1:24,000.
Metamorphosed lithic arenite — Quartz schist, quartz-chlorite schist, and quartzite (Xq), interlayered with
volcaniclastic schists (Xp); quartzite locally contains alumino-silicates. Includes the Tijeras quartzite of Connolly
(1981) and the Isleta metasediments of Parchman (1981).
Xla
20
84
Connolly, J. R., 1981, Geology of the Precambrian rocks of Tijeras Canyon, Bernalillo County, New Mexico: [M.S. thesis], University
of New Mexico, Albuquerque, NM, 147 p.
Chlorite-amphibole phyllite and schist — Metasedimentary and volcaniclastic rocks that grade from mafic
metavolcanics to lithic arenites. Includes metasedimentary rocks of the Tijeras greenstone of Connolly (1981)
and part of the Coyote phyllite of Cavin (1985).
Xp
Madera Formation, upper arkosic limestone — A gray, greenish-gray, olive-gray, tan and buff-brown
fossiliferous limestone (comprises slightly more than half of member) interbedded with intervals of subarkosic sandstone and mudstone. The limestone is thinly to thickly bedded and massive, with sparsely
disseminated chert. Sandstones and mudstones vary from reddish-brown to maroon to greenish-gray
and gray. Sandstones and arkosic sandstones, while sometimes lenticular and laterally discontinuous,
can be often traced over distances of several kilometers (see Read et al., 1998). These arkosic sandstones
are typically coarse- to medium-grained and often contain granules and pebbles. The base of this member
is defined as the first occurrence of a thick and relatively continuous arkosic sandstone bed. Petrified
wood is seen locally throughout this member.
Sandia Formation — Consists of a variety of lithologies including, in descending stratigraphic order: interbedded
brown claystone and gray limestone, massive gray limestone, and a lower olive-brown to gray, subarkosic,
fine- to coarse-grained sandstone. The contact with overlying Madera Formation (˛m) is chosen at the base
of the lowest thick, ledge-forming limestone. The lower contact is unconformable with the Arroyo Peñasco
Group or Proterozoic crystalline rocks. Isolated thin outcrops in Tijeras Canyon of sandstone and limestone
from the Espiritu Santo Member of the Arroyo Peñasco Group (see Szabo, 1953; Armstrong, 1967; Armstrong
and Mamet, 1974, Kelley and Northrop, 1975) generally remain undifferentiated from the Sandia Formation.
Limestone in the Sandia Formation is distinct from limestone in the overlying Madera Formation as they are
typically thinner-bedded, clast-supported, greenish, and contain abundant siliciclastic material. Approximately
170 ft (50 m) thick.
˛s
10
LYDEN
Connell, S. D., 1996, Quaternary geology and geomorphology of the Sandia Mountains piedmont, Bernalillo and Sandoval
Counties, central New Mexico: New Mexico Bureau of Mines and Mineral Resources Open-File Report 425, 414 p., 3 plates
(open-file release of Connell, 1995).
Quartzite — Thick-bedded to massive and gray to milky-white quartz arenite with crossbedding and bedding
defined by bands of iron oxides. Pelitic partings and interbeds contain aluminum silicates. Includes Cerro Pelon
and Coyote quartzites of Cavin (1985) and Cibola quartzite of Connolly (1981). Locality 4 has an 40Ar/39Ar
date of 1,423±2 Ma (Kirby et al., 1995).
Xq
l ll
Jet
0
Connell, S. D., 1995, Quaternary geology and geomorphology of the Sandia Mountains piedmont, Bernalillo and Sandoval
Counties, central New Mexico: [M.S. Thesis] Riverside, University of California, 390 p., 3 plates.
.
Medium-grained Cibola monzogranite — Equigranular, medium-grained, two-mica monzogranite;
average grain size is 1-3 mm.
TRES
OREJAS
ARROYO
SECO
3
CARSON
TAOS
JUNCTION
20 mi
CHILI
Mica schist, quartz-muscovite schist, and phyllite — Commonly rust red from hematitic staining, strongly
crenulated and commonly crowded with boudinaged and folded stringers and lenses of vein quartz. Includes
Coyote schist and Coyote phyllite of Cavin (1985).
Xms
Upper and Middle Pennsylvanian
Upper Jurassic
Jm
Xcc
lll l
Kd
Xcm
Yeso Formation, upper limestone unit — Intervals of massive or algal/cryptalgal-laminated limestone
within the upper part of the Yeso Formation. The limestones are typically micritic, fenestral fabrics are
commonly preserved, and they contain abundant quartz sand. Differentiated where possible east of the
Village of Cañoncito. Generally less than 16 feet (5 m) thick.
ARROYO
HONDO
Qvm
Taos
Cavin, W. J., 1985, Precambrian geology of the northern Manzanita Mountains, Bernalillo County, New Mexico: [M.S. thesis],
University of New Mexico, Albuquerque, NM, 144 p.
Fine-grained Cibola granite — Leucocratic two-mica granite.
CERRO
DE LOS
TAOSES
TAOS
Tijeras
10
OF-DM–46
llll
Dakota Formation — Medium-bedded, pervasively silica-cemented, plane-bedded to tabular cross-stratified,
quartz arenite, typically with abundant vertical, lined burrows, many of which are Diplocraterion traces.
Approximately 300 ft (90 m) thick.
Pyc
Xcf
NMBMMR STATEMAP
Quadrangles
Brown, C. L., Karlstrom, K. E., Heizler, M., and Unruh, D., 1999, Paleoproterozoic deformation, metamorphism, and 40Ar/39Ar
thermal history of the 1.65-Ga Manzanita pluton: New Mexico Geological Society, 50th Field Conference Guidebook, p. 255268.
Cibola granite, undivided — Biotite-muscovite monzogranite with U-Pb dates of 1,632 ±45 Ma (geochronologic
sample Locality 5), from north of the Tijeras fault and 1,659±13 Ma (Locality 6) from south of the Tijeras fault
(D. Unruh, 1998 unpublished data).
Xc
Qayt
? ?
I NDEX M AP OF NMBMMR’ S
STATEMAP
7.5-M INUTE G EOLOGIC Q UADRANGLES
2/00
0
6 Department of Earth and Environmental Science, New Mexico Institute of Mining and Technology, Socorro, NM 87801
7 William Lettis & Associates, Inc., 1777 Botelho Dr., Suite 26 2, Walnut Creek, CA 945 96
The sandstones are cross-stratified (typically trough and wedge-planar geometries) and the finer grained rocks
are commonly ripple cross-laminated. In addition, mud-chip clasts and plant debris are common. The upper
contact with the Yeso Formation (Py) is conformable but difficult to distinguish in the field. The lower contact
with the Madera Formation (˛ m) is gradational with interbedded limestone and reddish-brown mudstone. The
top of the lowermost laterally continuous and relatively thick limestone bed is chosen as the Madera Formation
contact. Total thickness for the Abo and Yeso formations combined is approximately 1,300 ft (400 m).
Qpy
106°30'
35°07'30"
Armstrong, A. K., 1967, Biostratigraphy and carbonate facies of the Mississippian Arroyo Peñasco Formation, north-central New
Mexico: New Mexico Bureau of Mines & Mineral Resources Memoir 20, 81 p.
June 1, 1994
28 February 2000 Revision
Mapping of this quadrangle was funded by a matching-funds grant from the 1994 STATEMAP
program of the National Geologic Mapping Act coordinated by the U.S. Geological Survey
and the New Mexico Bureau of Mines and Mineral Resources (Dr. Charles E. Chapin, Director
and State Geologist; Dr. Paul W. Bauer, Geologic Mapping Program Manager).
Mancos Shale, sandstone unit — A discontinuous, <5 meter-thick interval of medium-bedded, resistant,
non-argillaceous sandstone with abundant vertical burrows. In the northerly adjacent Sandia Park
quadrangle, this sandstone unit overlies a fossiliferous shale containing late Turonian guide fossils. The
sandstone may correlate with the Tocito sandstone, and it appears to pinch-out to the south were its
approximate stratigraphic position is occupied by a massive, non-calcareous sandstone body interpreted
as the northern pinch-out of the Gallup Sandstone.
Interstate 40
REFERENCES
Qay
middle
Geology of Tijeras quadrangle,
Bernalillo County, New Mexico
Qca
early
6000
Ced
ar
Syn Crest
clin
e
INDEX TO GEOLOGIC MAPPING
PREVIOUS WORK
35° 00'
106° 22' 30"
Pleistocene
74000m E.
af
QHao
QHa
Pliocene
3
IGNEOUS
Miocene
73
Neogene (Tertiary & Quaternary)
3
72
U NITS
SEDIMENTARY
Holocene
74000m N.
Cret aceous
5000
Epoch
38
10
3
71
1 MILE
4000
0' MSL
Jurassic
3
25'
OF
Pay
Triassic
Ys
70
C ORRELATION
Permian
Xmg ˛s
ˇz
ˇm
Ps
Pg
˛ml
Qay
˛ml ˛s
˛ml
1,000'
Xmv?
Pay
˛mu
˛ml
˛mu
5
˛s
Xq
Ps
Penn.
Xcm
Qay
Qpy
54
2,000'
Miss.
43 42
71
52
lt
ˇc
Pg
˛m
fau
Mesoproterozoic
Xmg
40
ˇm
ust
4
5
6
Method
14C
40Ar/39Ar
(whole rock)
U-Pb zircon + sphene
U-Pb zircon
U-Pb zircon
40Ar/39Ar (hornblende)
40Ar/39Ar (muscovite)
U-Pb zircon
U-Pb
Reference
Sample No. Beta-104958 (this study)
Karlstrom et al. (1997 b)
Tilton and Grunenfelder (1968 ), recalculated by S. Getty (unpubl.)
Stieger and Wasserburg (1966 ), recalculated in Kirby et al. (1995 )
D. Unruh, (unpublished); Karlstrom (1999)
Kirby et al. (1995 )
Kirby et al. (1995 )
D. Unruh, (unpublished); Karlstrom (1999)
D. Unruh, (unpublished); Karlstrom (1999)
on
ny
Four
Hills
35°00'
106°22'30"
Xc
Paleoproterozoic
Xla
3,000'
hr
QHa
45
44
Qay
MSL 0'
Xq
CENOZOIC
af
Qay
Xmv?
Jet
M
oo
re
t
Jm
˛ml
˛ml
nt
ˇc
ˇz
Xcm
4 New Mexico Bureau of Mines and Mineral Resources, Socorro, NM 87801
Kms
˛m
˛s
Km
Special thanks to Mr. Joe Rogers, Mr. Larry Rainosek, Mr. Richard Nieto (Carnuel Land Grant Association), Mr. Ray McDaniels (Acequia Madre
de Carnuel Community Ditch Association) and Mr. Chris Jinzo and Mr. Gary Hefkin of the Acequia Madre de San Antonio Community Ditch
Association for logistical assistance and access to their lands during this study.
4,000'
MESOZOIC
Xla
60
5
Kd
ce
PALEOZOIC
59
Qay
af
5,000'
PROTEROZOIC
˛s
ve
Se
Km
Jet
˛s
a
he Yss
s
s
ng
pri
1,000'
Xla
The map has not been reviewed according to New Mexico Bureau of Mines and Mineral Resources standards. Revision of the map is likely
because of the on-going nature of work in the region. The contents of the report and map should not be considered final and complete until
reviewed and published by the New Mexico Bureau of Mines and Mineral Resources. The views and conclusions contained in this document are
those of the authors and should not be interpreted as necessarily representing the official policies, either expressed or implied, of the State of New
Mexico and the U.S. Government.
on
Xmg
45
Cross sections are constructed based upon the interpretations of the authors made from geologic mapping, and available geophysical and
subsurface (drillhole) data. Cross sections should be used as an aid to understanding the general geologic framework of the map area, and not
be the sole source of information for use in locating or designing wells, buildings, roads, or other man-made structures.
ny
˛s
Xmv
Xms
Ca
Qvm2
45 Xmv
64
˛m
Made
ra
60
47
Qvm2
55
2,000'
nS
Xq
Ys
59
Xla
QHa
Qay
Xmg
75
Qay
Xcm Xcm
48
Pay
e
on
z
r
12
65
44
7,000'
6,000'
˛s
Kvt
Are
Xcm
45
Jm
38
15
Pay
Qayt
Pay
Kvs
Kd
˛mu
Xmv
Pg
˛m
Qca
˛s
Qca
Pay
Kvs
Pg
8,000'
˛m
Kvs
Kvt
Kvs
Xcm
5,000'
˛s
50
ˇm
Ps
Qpy
Km
76
NATIONAL GEODETIC VERTICAL DATUM OF 1929
Mancos Shale, undivided — Dark gray shale, slightly calcareous shale, and septarian nodule-bearing shale,
with rare, thin, black micrite beds and at least two ~10 ft-thick (3-4 m), medium-bedded calcareous sandstone
intervals. The micrites and sandstones are typically fossiliferous yielding abundant molluscan shell fragments
indicating a late Turonian age for the youngest part of the sequence. Total thickness is approximately 1,300
ft (400 m).
Kvs
ue
Xmg
Xcm
67
CONTOUR INTERVAL 40 FEET
UTM GRID AND 1972 MAGNETIC NORTH
DECLINATION AT CENTER OF SHEET
QHa
ˇc
ault
r
Xmg
˛s
Xcm
85
Qay
ˇc
A geologic map displays information on the distribution, nature, orientation and age relationships of rock and deposits and the occurrence of
structural features. Geologic and fault contacts are irregular surfaces that form boundaries between different types or ages of units. Data depicted
on this geologic quadrangle map are based on reconnaissance field geologic mapping, compilation of published and unpublished work, and
photogeologic interpretation. Locations of contacts are not surveyed, but are plotted by interpretation of the position of a given contact onto a
topographic base map; therefore, the accuracy of contact locations depends on the scale of mapping and the interpretation of the geologist(s).
Any enlargement of this map could cause misunderstanding in the detail of mapping and may result in erroneous interpretations. Site-specific
conditions should be verified by detailed surface mapping or subsurface exploration. Topographic and cultural changes associated with recent
development may not be shown.
Pay
rq
0.5
Qayt
COMMENTS TO MAP USERS
9,000'
ˇm
ˇz
Psg
Qca
ue
1
ˇz
˛mu
22
Manzanita
Shear Zone
SAN ANTONITO (NM 44) 4.7 MI.
MADRID 29 MI.
38
15
48
10,000
feet ASL
Kvs
ˇm
˛m
Ys
44
53
SE
ˇc
ˇm
A lbu q
Xcm
46
Xcm
Xmg
TIJERAS 7.5-MINUTE QUADRANGLE
SEDILLO 7.5-MINUTE QUADRANGLE
l l ll
l
lll
lll
l
ll
llll
6,000'
80
Xmg
Interstate 40
l
l
l l ll
ll
ll
ll
llll
lll l
lll l
l ll
ll
ll
ll
ll
ll
lll l
llll
llll
l llll
l l ll
l
ll
20
ras f
us
thr
l llll
l l l l l l
l l
l l l l
231 MILS
ˇc
Pay
Tije
t
ul
fa
V
l
ne
zo
l l l l
l
l l l
l l
l l
l l
l l l
l l
l l l
ras
t zon
e – Four
H ills s t r a nd
faul
dia
San
)
NG
RI
SP
LL
Tij
e
INTERSTATE 25 8 MI.
(ALBUQUERQUE EAST)
l l
BE
ll l
l l l l l l l l l l l l l l l l l
l l
0° 50'
Km
C'
)
UB
Qay
3,000'
l
Kvm
˛ml
?
13°
15 MILS
Kvs
ˇz
ˇm
Ps
Pg
˛m
˛m
Kvt
Jm
Psg
˛ml
28
32
mixed zone
˛s
71
44
2,000'
0 MSL
Kd
Jet
7,000'
13
Qca
Xla
fau
Xmv?
lt
SA
(H
llll
ll l
lll
˛s
55
3000
˛s
8,000'
4
QHa
34
55 31 50 Xp
˛m 15
Xcm
60
6
Xla
52
0
2000
Kd
ˇc
Pay
Qay
ll
Mesaverde Group, marine shale unit — Shale and mudstone with thin-bedded, commonly limonitic
siltstone interbeds. Characterized by a lack of coal seams and abundant woody debris, and by the
presence of molluscan fossils and shell fragments. These rocks correlate partially with the marine
sandstone and shale unit (Kvm) of the northerly adjacent Sandia Park quadrangle.
.
ll
z
˛s
Xmg
Qvm2
(MOUNT WASHINGTON)
1000
Ps
6
5
Xmv
Xmv?
3,000'
ust
Xmv?
Km
Pay
O
0
Pg
˛ml
Qay
GN
1000
Jm
ˇc
9,000'
Xmv
3
0.5
7
AB
1
MN
l
Xcm
Xlg
A'
lll l
t a af
af
Xcm
5
6
˛ml
10
Xla
t hr
Xcm
Guitierrez
fault
ˇz
SC
Mesaverde Group, terrestrial shale unit — Shale and mudstone with thin-bedded siltstone interbeds.
Characterized by the absence of marine fossils, abundant woody debris and common association with
coal seams. These rocks correlate partially with the terrestrial sandstone and shale unit (Kvt) of the
Sandia Park quadrangle to the north-east (Ferguson et al. 1996).
25
81
28
5
ˇm
5 Department of Earth and Planetary Sciences, Washington University, St. Louis, MO 63130
Tertiary Intrusives
Mesaverde Group, sandstone unit — Feldspathic arenite to quartz arenite, locally with abundant
dark-colored chert grains. Four types of sandstones are included in this unit: 1) resistant, medium- to
thick bedded, trough and wedge-planar cross-stratified, light-colored sandstones, 2) recessive, massive
or flaggy-weathering, argillaceous, greenish-brown colored sandstones and siltstones with abundant
woody debris and mud chip clasts, 3) resistant, clean (non-argillaceous), well-sorted, light-colored, planarbedded to low-angle cross-stratified sandstone, and 4) recessive weathering, thin- to medium-bedded,
dark brown to greenish colored, argillaceous and variably calcareous sandstone containing abundant
molluscan shell fragments (chiefly bivalves). The first two lithotypes were mapped as terrestrial sandstones
(Kvt) in the northerly adjacent Sandia Park quadrangle (Ferguson et al. 1996), and interpreted as alluvial,
or distributary channel sandstones. The third type, which is also characterized by the upper shoreface
environment restrictive trace fossil Macaronichnus (c.f. Mieras et al., 1993), is interpreted as a shoreface
or beach sandstone which were mapped as Kvs in the Sandia Park quadrangle to the northeast. The
fourth type is a marine sandstone that was mapped as part of a marine sandstone and shale unit (Kvm)
in the Sandia Park quadrangle.
68
13
10,000
feet ASL
3 Arizona Geological Survey, 416 W. Congress, #100, Tucson, AZ 85701
Oldest pediment surface — Deeply dissected and commonly grussified, formerly extensive south-sloping
surface of erosion cut mostly upon Sandia granite (Ys). Surface projects about 120-200 ft (35-60 m) above
Tijeras Creek. Probably correlative to the basal contact of old eastern-slope alluvium (QTp).
.
Mesaverde Group, undivided — A complex unit of marine, marginal marine, and fluvial sandstones, shales,
and siltstones with several intervals of coal-bearing strata. The sequence is divided into three interbedded map
units: sandstone (Kvs), marine shale (Kvm) and terrestrial shale (Kvt). Note that these subdivisions are defined
differently from the three subdivisions of the Mesaverde Group as recognized in the northerly adjacent Sandia
Park quadrangle; marine sandstone and shale (Kvm), terrestrial sandstone and shale (Kvt), and shoreface
sandstone (Kvs). The exposed thickness of the incomplete Mesaverde Group section is approximately 1,400
ft (430 m).
Xcm
3
R. 5 E.
27
4
1 Department of Earth and Planetary Sciences, University of New Mexico, Albuquerque, NM 87131
2 New Mexico Bureau of Mines and Mineral Resources, Albuquerque, NM 87106
Older subunit (middle Pleistocene) — Poorly to moderately consolidated deposits of light- to strongbrown (7.5YR) and very pale-brown to light-gray (7.5-10YR), poorly to moderately stratified and sorted,
sand clayey sand and gravel. Deposit surface (top) is dissected and commonly exhibits erosional ridgeand-ravine topography. Moderately well developed soils with Stage III+ carbonate morphology and
many moderately thick clay films. Probably correlative to stream alluvium of Tijeras Canyon (Qpmt1),
and generally correlative to units P3-P4 of Thomas et al. (1995).
MESOZOIC ROCKS
Cretaceous
52
R. 4.5 E.
8
5
2
Qca
SCALE 1:24,000
K. E. Karlstrom: mapping and compiliation of Proterozoic rocks, cross sections; S. D.
Connell and D. W. Love: Quaternary mapping and unit descriptions (Connell); C. A.
Ferguson and G. R. Osburn: Phanerozoic mapping and stratigraphy, (northeastern
area of quad), unit descriptions, correlations, and regional structural interpretation; A.
S. Read: differentiation of the Madera formation (southeastern area of quad), final map
and cross section compilation; and P. W. Bauer: intellectual contributions.
D. J. McCraw, M. M. Mansell, and G. E. Jones: digital cartographic production
Xq
35
27' 30"
3
2
(E
Base from U.S. Geological Survey 1954, photorevised 1961
Polyconic projection, 1927 North American datum, 10,000-foot grid based on New
Mexico coordinate system, cental zone
1000-meter Universal Transverse Mercator grid ticks, zone 13, shown in blue
Xq
R. 4 E.
ll
66
ll
Qca
3
65
ll
Qpm2
3
68
Xmv
65
54
ll
430 000 FEET
an
i
an
78
Xmv
l
64
53 Xms
Xp
M
Xcm
ll l l ll
3
Xms
16
Xp
l ll
QHa
Qay
Xq Xcm
74
l
Qay
Xcm
76
Qvm2
Xq af
l l l ll
Qay
Qay
Qpx3
Xq
lll
50
ll
S,K
Xla
Qvm1
QHa
af
Qay
Xmg
Qay
75
Qay
ll
Xcm
34
Qay
71
Xmv
sh
46
48
50
QHa
45
ea
re
Ys
50
Qvm2
˛mu
6
6
Qay
63
Qay
55
60
7
Xmv
Qvm2
44
40
Qay
Xms
Xq
Xq
7
4,000'
QHa
Xms
55
Xq
52
13
NW
Qay
2
˛s
Xms
Xq
Xms
40
Xq
Xq
49
64
40
18
36
Qvm3
43
54
Qpy
20
QHa
50
60
35
48
3 6
Flat Irons
fault
C
Qay
7
6
2
˛ml
4,000'
Xq
n
af
Xcm
Xq
˛m
80
Xmv
13
3
7
Qay
6
8
?
˛s
Mo
o
Xp
Vi
Xmv
Ys
Xq
I I I I I I I I I I I I I I I I I I I I I I I
66
˛m
16
Xms
Qca
Xq
I I I I I I I I I I I I I I I I I I I
56
82
68
30
˛m
Qpx3
˛m
24
29
ll
75
6
Xq
Xmv
Xq
31
o
zQvm
58
76
Qca
74
15
83
5
63
Xq
1,000'
Tijeras
fault zone
16
7
6
Qca
e nt
Xq
78
Qay
5
32
56
ne
47
55 76
Xq
49
56
75
Xms
?
5
5,000'
nc
co
ot
24
27
42
45
Xq
80
48
Xmv
Xms
Xq
Xdt
-1,000'
3
7
18
59
30
32
52
Qay
˛ml
8
6,000'
˛ml
7
31
˛s
Xms
Xms
71
65
Xcm
76
30
Qay
64
71
70
l lll
Xcm
Xcm
40
Xq
Xcm
Xmv
54
35° 00'
106° 30'
36
Qvm Xmv
47
˛s
75
45
2 46
20
Xmv
Qpy
74
Xcm Xq
Xmv
lll
40 45
38
Qpx3
˛m
Qay
58
75
˛m
Xcm
Xcm
Xcm
l
Qca
QHa
˛m
48
ll
Xmv
QHa
82
74
ll
Ys
Qpm3
66
61
Xmv
58
50
˛mu
6
45
˛ml
Xq
75
63
Qca
8
7
7
Xms
Xms
Xcm
ˇz
67
43
?
˛s
Xq
43
Xq
80
75
40
50
Xcm
4
5
38
˛s
n
ton
u
l
P
˛s
-1,000'
7
Qvm2
64
76
75
45
43
70 70
Ys
50
40
Xmv
68
70
77
57
35
45
25
l
1 460 000
FEET Qpy
55
51
Qay
50 51
63
38
ll
l Tmi
l
Qvm3
T. 9 N.
˛s
8
81
10
?
02' 30"
˛ml
?
Ps
72
43
ll
l
Qpx3
˛m
Xms
l
l
67
60
ll
l
Xq
66
62
55
57
Xmv
QHa
60
84
58
51
36
Xcm
22
l
54
58
80
75
72
66
67
62
l ll
42
Xmv
Xq
Qvm
l l
l l
l l
l
Tmi l l
58
55
ll
Qpm3
46
56
59
Xms
T. 10 N.
6
9
62
Qay
Qay
20
˛mu
Vi
ea
sh
s
g ?
ed
ai n
rin
r
t
p
S
ns
ia
and
S
f
eo
Bas
?
MSL 0'
25
7
5
60 45 32
43
Xq
18
50
60
ll
Qay
Xms
5
ven
Se ?
Ys
24
Xmv?
7,000'
˛ml
˛mu
Yss
1,000'
5m
˛mu
Xla
˛mu
˛mu
˛ml
Xq
79
17
5
8,000'
Pay
Ys
Ys
17
Xq
Xms
42
af
Xp
Xcc
ne ?
o
rz
8
85
12
Tmi
˛ml
˛s
Xcc
Km1
24
82
46
38
Xms
˛s
Qvm2
72
55
63
32
Xla
Xla
15
30
63
73
68
37
42
68
39
Xmv
56
Qay
53
U
D
Qpx3
Ys
49
52 64
51
Xms
Xmv
78
62
86
61
84
Qvm2
˛s
44
46
57
Ys
55
49
K
9
38
˛s?
24
30
6
Qvm2
60
QHa
Xms
Qay
43
41
80
QHa
l l
l l
l l
l l Tmi
l l
l l
l
Qpy
lll
Ys
in
t
47
˛ml
10
?
2,000'
17
5m
25
15
32
Yp
Xq
Xcm
Kmf
Khd
62
16
5
Qay
Qay
Xms
Qvm2
71
51
llll
QHa
cen
Qay
37
Xq
llll
76
30
54
44
e
or
Mo
llll
Qpy
?
QHa
llll
Ys
?
68
Xms
65
Xms
71
Xmv
Ys
l
Qpm3
Ys
Ys
50
35
l l
l l
l l
l l
l l
l l
l l
l
l l
35
l
l l
l
l
l l
l
l l Tmi
l
l l l l
l
l l l ll l l
35
l
20
l
l
l
l
l
20
l
l
l
l
l
l Tmi
l
l
l
l
l
l
l
l
l
l
l l
l l
l l
39
?
Qay
32
8 3
9
Tmi
Yp
Km2
Xla
24
22
35
8
24
25
36
Xcm
Schematic aligned enclaves
38
11
33
23
63
35
Yp
31
˛s
78
Yp
3,000'
˛ml
27
Pay
Pay
Xcc
˛s
38
27
29
4,000'
43
22
12
79
Yp
Schematic
aligned
megacrysts
Ys
50
42
28
5,000'
B'
80
37
D
U
15
˛s
Xms
60
38
K
llll
20
l l
l
Xcm
50
Younger subunit (upper to middle Pleistocene) — Poorly to moderately consolidated and poorly to
moderately sorted deposits of very pale-brown to strong yellowish-brown (7.5-10YR), poorly to moderately
stratified and sorted, silty clay and loamy sand and gravel. Soils are moderately developed and possess
Stage II to III carbonate morphology and few to common, thin to moderately thick clay films. Probably
correlative to stream alluvium of Tijeras Canyon (Qpmt1), and generally correlative to units P5-P6 of
Thomas et al. (1995).
Mafic to intermediate dikes (Oligocene?) — Generally deeply weathered mafic to intermediate, steeply
dipping, north trending dikes. Dikes are probably correlative to an Oligocene mafic to intermediate dike
exposed on the northern flank of the Sandia Mountains (cf., Connell et al., 1995).
.
Xr
ll
74
ll
63
l l ll
68
llll
73
15
23
20
78
30
15
16
86
10 25
l
ll l l
18
8
˛s
˛s
Xms
36
ll
˛ml
10
ll
63
17 14
11
Yp
Ys
30
38
13
10
˛s
38
15
25
11
17
˛s
14
14
5
˛ml
QTsp
12
12
17
˛mu
16
˛ml
QHa
Yss
Xcc
Yp
22
20
QHa
80
6,000'
Pay
The top of the Mesozoic section
beneath QTsp is unconstrained
and lower Tertiary sediments
may be preserved on the
hanging wall of the Sandia
Fault.
20
4
5
20
˛s
l
10
6
15
Xms
Xms
˛ml
10
l l ll
9
5
24
˛ml
ult
t
ll
Ys
54
74
ll l l
65
64
69
Xcm
49
Xmv
l ll l l l l
ll
81
Xcm
ll ll
Ys
59
Xcm
73
Xla
72
fa
60
Xmv
llll
81
Xcm
70
˛ml
12
10
9
37
20
6
7,000'
17
80
˛ml
˛s
65
lllll
Yss
60
2
7
11
20
Xms
˛mu
16
8
8
13
Xq
81
l
l l l l
l l l ll l ll l l l l l l l l l
50
l
ll
3
20
27
10
15
88
5
5
Qay
5
5
55
74
Xmv
l ll
l
ll
5
10
77
Xcc
81
15
80
70
4
81
Ps
Pg
Pg
11
6
10
88
8,000'
38
14
ˇm
Ps
Ys
Pg
9,000'
ˇz
ˇm
ˇz
Ps
21
13
ˇc
ˇz
Ys
ˇm
21
12
8
˛ml
˛s
10,000'
ˇc
9,000'
QHa
13
4
ˇc
17
9 6
Ps
˛mu
16
6
11,000'
Apachito
Canyon
Pg
35
12
ll
llll
l
8
13
6
˛mu
˛s
38
llll
6
18
30
30
15
10
17
5
5
10
9
8
80
85
l ll l l
78
27
Pay
50
18
4
7
40
5
Qay
11
11
14
62
7
6
7
50
85
70
Qpy
Youngest subunit (upper Pleistocene) — Poorly consolidated and poorly to moderately sorted graybrown to reddish-brown, subangular to subrounded, pebble to cobble gravel with silty sand interbeds.
Inset against middle subunit Qvm2. Soils are moderately developed and exhibit Stage II carbonate
morphology. A radiocarbon date of more than 21,000 years BP reported by Thomas et al. (1995, p.
2-36, unit Pf5) indicates a late Pleistocene age. Probably correlative to stream alluvium of Tijeras Canyon
(Qpmt1), and generally correlative to units P5-P6 of Thomas et al. (1995).
l
78
Ys
Qpy
Ys
15
85
l
ll
˛mu
9
18
83
llll
Qpx3
Ys
Ys
17
l l ll
10
10
6
26
33
25
ˇz
ˇm
Pay
˛mu
Qvmt 24
3
Sandia
fault
10,000'
38
7
12,000'
11,000'
55
11
40
13,000
feet ASL
Tijeras
fault zone
Qay
25 11
˛mu
l
Sandia Crest
(projected)
82
19
4
4
l
ll
l
˛mu
9
14
10
75
QHa
88
ll
10
7
l lll
8
6
85
12
13
53
50
6
11
40
˛ml
40
5
6
4
21
33
Xmv
43
8
lll
˛mu
20
30
70
64
85
ll
53
Qpm3
15
lll
Ys
56
38
46
Xla
llll
Ys
40
72
llll
64
73
l
QHa
35
Older subunit (middle Pleistocene) — Poorly to moderately consolidated deposits of light- to strongbrown (7.5YR) and very pale-brown to light-gray (7.5-10YR), poorly to moderately stratified and sorted,
sand clayey sand and gravel. Deposit surface (top) is dissected and commonly exhibits erosional ridgeand-ravine topography. Moderately well developed soils with Stage III+ carbonate morphology and
many moderately thick clay films. Correlative to the geomorphic surface Q6 of Connell (1995, 1996)
and to stream alluvium of Tijeras Canyon (Qpmt1). Generally correlative to units P3-P4 of Thomas et al.
(1995).
64
A,S,K
l
19
16
66
34
Yss
Ys
39
38
58
56
5
12
af
Tmi
10
14
˛s
70
8
65
40
11
11
23
10
Xla
8
18
8
48
65
Xp
59
lll
Qay
54
77
77
68
65
60
75
86
15
2
6
B'
SE
38
8
6
14
25
55
79
66
62
14
l l
l
l
17
5
l
Xla
70
70
Xp
Xcc
64
22
18
85
78
Xla
Xcm
25
Xmv
4
ll
2
62
65
30
68
64
25
45
Xp
lll
Ys
65
28
70
21
Qpx3
Ys
Ys
Xcm
˛ml
62
Xcm
25
17
l l ll
28
TmiYss
15
3
8
˛mu
l ll l
l
62
7
10
80
15
25
80
Xla
12
B
˛mu
af
24
8
20
0' MSL
ˇc
10
Pay
20
18
2
4
8
Pay
65
78
20
4
50
45
7
6
25
Xcm
70
Tmi
20
18
15
18
˛s
65
13
22
12
18
66
70
80
10
35
55
65
Qay
24
25
55
88
l l ll
8
9
10
15
25
Qpx2
Xp
74
Xcm
62
QHa
76
31
45
70
QHa
Qpx2
Xcm
23
60
65
70
QHao
47
70
70
70
8
˛mu
89
1m
6
25
87
1,000'
Xmv
Xmv
Pay
20
7
ll
Xcm
12,000'
25
7
5
7
28
78
Xp
36
61
Qpy
Qpy
QHao
47
36
53
70
87
75
70
82
Qpx3
Ys
Xcm
Ys
Xla
Xq
l
2,000'
NW
13,000
feet ASL
10
31
8
18
6
4
Qay
85
Xmv
65
4
Xmv
16
12
12
12
8
19
7
85
53
53
Qay
Ys
l
l
l
17
70
53
ll
l l
15
25
28
63
49
10
11
36
21
4
Xmv?
Depth to base of Sandia Pluton not constrained
MSL 0'
12
˛ml
10
3,000'
05'
42
20
12
lt
Xcm
Yss
1,000'
14
Qay 19
18
10
16
ll
ll
l
l
75
58
l
6
˛ml
62
Xp
A
10
22
17
ll l
C'
10
7
34
50
Xcm
lll
15
43
70
50 33
˛s
5
60
52
64
Xcc
58
A
ll
ll
l
23
34
Qpx2
Xp
Xd
Qpx2
Xp
Xp
Qayt
48
Xq
l
l
Qpm3
17
Qpm3
Ys
68
64
Xcc
l
78
Qay
Ys
63
Xla
61
ll
42
75
70
l ll
˛mu
28
29
50
A,St,Cd
Xla
65
57
Qpx2
Ys
38
48
35
Yss 58
78
Qpx2
Ys
A
Qca
57 33
67
Qpx2
Ys
68
65
Qpx2
Xmv
65
65
Qpm3
54
71
QHao
Yss
22
20
l l l l l l
l
l
l
l
l
,
l l l
l l
l l
l l
38
28
Tmi
12
Qvm
Qvmt1
Tmi
l l l l
l l
l
l
l l
l l l
l l l
l l l
T. 9 N.
Qpx2
Ys
l l l l
l
l
l
l
l
l
l
l l l
l l
l l
02' 30"
Ys
Qca
14
l l l l l l l
l
T. 10 N.
Tmi
Ys
33
l l
l l l
Qay
Qay
51
Xq
87
Qvmt2 Xp
af
Xcm
60
47
Xcm
43
Tmi
19
QHa
QHa
QTpx
Ys
Ys
22
70
l l l
l
79
63
62
30
Ys
Qpx2
Ys
38
66
62
14
23
QTpx
Ys
18
Qvmt
19
81
14
9
Ys
Xla
44
16
ll
ll
fa u
Xp
Xq
ing
S
4,000'
us t
10
12
52
8
af
Yss
Ys
QHa
15 18
17
l
46 24
84
19
Ys
70
60
Qvmt1c
Qay
36
79
33
QTpx
Ys
Qay
ll
24
88
80
Xp
Qvmt2
ll
65
Xmv
65
Qvmt2
Qay Xcc
Yss
58
65
Qayt
Qayt
38
Ys
D U
Qayt
Xcm
Qay
16
56
QHao
22
52
l
ll l
QHao
Ys
QTsp
Qpx3
Ys
Xq
Qca
Qayt
Ys
Qayt
55
75
QHa
Qayt
QHa
l
10
5,000'
Mo
ore
pr
n
ve
e
S
2,000'
Pay
15
Pay
l
l
Ys
af
af
QHao
12
af
49
Qayt
Qayt
78
Qay
Ys
Ys
66
Qay
QHa
QHao
36 44
54 55
32
21
49
58
Qvmt2
Qpx2
Xmv
65
Ys
Ys
8
˛ml
l
ll
Xcm
t hr
ea
3,000'
Pay
20
18
32
11
9
12
lll
Qpx2
Ys
50
33
75
80
78
17
Qca
Qayt
12
Qpo
50
14
12
12
21
25
44
7
Xla
85
70
Xmv
52
34 39
51
35
36
38
63
af
Ys
Qpx2
Ys
Ys
Ys
Qay
QHa
Ys
Qay
Yss
Qpx3
Ys
3
76
Qpx2
Ys
QHa
Qayt
Ys
Qvmt2
72
Xcm
Xcm
Qvmt2
38
44
Xcc
Qpm3
Qayt
13
15
˛ml
18
QHa
12
18
14
52
23
Xmv
80
79
41
26
33
54
40
Qpx1
Ys
27
55
30
76
50
44
46 41
Qpx2
Ys
Qpx3
Ys
Xcc
32
Xcm 36
A,S,Cd
47
˛s
Pay
12
14
14
54
42
10
af
7
Pay
12
60
Qca
Xq
t
Xp
Xla?
e
on
z
r
h
ss
Ys
6,000'
12
Qayt
Qay
65
af
12
8
12
Ys
Xq
Kvs
Qpo
Qpo
17
Xmv
Train of
Enclaves
4,000'
84
QHa
Psg
Pay
11
22
Yp
Yp
Xla
38
30
18
33
32
QHa
ll l l
Qayt
1
Ys
Ys
15
33
18
12
12
Qay
Qayt
af
60
Qay
12
15
15
28
Pay
31
Xms
Xq
Kvs
Kvm 30
Kvs
Pay
Qvmt
20
Pay
30
llll
Ys
Qay
Xcc
45
41
32
31
43
53
Qpx1
Ys
A,S
QTp
30
Xms
Xq
Xq
Yp
Yp
7
13
˛mu
50
˛ml
50
Qvmt2
Xmv
56
72
50
30
af
42
?
42
35
Pay
12
7,000'
˛s
Xms
Yp
9
13
18
20
lll
Qay
Yss
Qpx3
Ys
Ys
Ys
85
Qca
75
10 4 Tmi
33
8
65
6
Pay
23
Qayt
45
25
QHa
60
Xq
Qayt
Xcm
46
46
Xcm
Ya
Qvm
23
ll
Ys
Qayt
Ys
80
Qpm3
QHa
Qpx3
Ys
Qay
Yss
50
Xmv
Qvm?
6 15
41
58
7
Qvmt
29
8
7
7
15
43
Pay
34 26
lll
af
26
Pay45
Kvs
af
QHa
˛m
Qca
Xcf
55
43
46
Qvmt1
Xcm
85
42
41 31
53
5
Ys
54
55
55
82
Xcm
Xcf
39 31
50
29
44
28
75
65
Tmi
55
3523
Kvm Kvs
72
17
Xq
Xmv
Yp
60
Kvs
85
Xcm
Kvm
QTp
6
29
30
76
˛s
Yss
5,000'
66
68
58
55
47
69
63
72
Qay
Kvs
12
15
Kvt
77
QTp
75
40 71
55
72
˛m
80
35
lll
Ys
Ys
24
Ys
18
Qay
4
10
18
Ys
20
af
Qpx2
Ys
Xcm
53
86
80
A,S 14
35
26 23
20
Ys
QHao
Qpx2
Ys
Qay
25
43
ˇc
49
Pay
Psg
55
78
Qay
Xcm
53
29
56
56
Ys
Qca
60
75
25
52
5
Xq
29
60
25
Qca
58
Qca
42
55
58
80
48 77
42 72
49
Xcm
5 4 70
80
71
Ya
32
29
Ys
16
86
25
Ys
73
Qpx3
Ys
QHa
Qvmtc
Qpx2
Ys
22
Ys
Qvmt2
Qvmt2 Qvmt1
4
5
51
49
70
Km
60
49
41
42
Ys
77
Ys
36 5
82
Qca
Kd
77
78
50
Pay 80 66
23
49 50
QTp ˛m 5461
63
27 18
30
69
Ma 65
Qvmt2
34
61
65 30 39
13 29
Pay
70
57
38 65
68
Qpm
Xcm
49 48
73
54
Qpo 58
80
10
51
26
Pay
55
˛m
52
Qca
18
22
QTp
85
˛m
58
Qpo
55
Pay
˛m
33
56
9
31
22
79
57
Xq
45
Yss
47
8
62
Xcc
58
82
QHa
Qay
Qay
QHao
25
Ys
13
86
Qpx3
Ys
Ys
82
˛m
23 63
65 67
45
40
87 57 73
70
Pay
19 22
21
45
50
58
Qtr
l
6
Xcm
81
Xq
35
80
35
lll
Yps
l l l
5
Qvmt2
Qayt
af
af
38 10
34
˛s
Qay
llll
Qvmt2
19
Qay
18
14
14
11
64
63
58
Train of
Enclaves
Ys
11
71
62
Tijeras
Canyon
˛m
Yp Yp
6,000'
QHao
65
Kvs 80
67
67
Yp
Train of Yp
Enclaves
9,000'
8,000'
˛m
80
69
78
31
Yp
Yp
53
81
75
Yp
10,000'
˛s
Yp
Yp
Kvt
67
68
85
78
Km
85
82
Ys
80
Km
Km
Qca
Km
Ys
Yp
Kvs
Qca
Km
83
88
8,000'
70
79
65
64
80
40 34
74
38
Km
Kd
Jm
QTp
QTp
30
82
Embudo
Canyon
QHao
81
77
Jm
Jm
79
69
QHao
Kd 35
Km
Jm
Qca Qtr 52 80
68
ˇc
28
llll llll
Qvmt2
10
Xcm
16 49
Qpx2
Ys
Qca
Xcm
Qca
l
Ys
9
˛s
13
17
64
Jm
Qca
Jm
50 51
88 83
28 58 80
37 7685
80
85 64
8
10
14
l ll
Ys
Yps
5
QHa
QHao
52
15
15
28
64
17
l lll
Qvmt2 Qayt QHao
Qayt
20
af
45
35 68
Ys
15
22
20
20
Pay Ps
30
llll
Qvmt2
Yps
41
73 44
26
5
25
13
22
llll
Qvmt1
15
36
3
44
30
Jt
85
Ps
Ys
7,000'
Kd
Km
Qca
˛m
˛s
Km
86
68
QHao
˛s
Yp
74
74
˛m
9,000'
Kd
Je
65
ˇc
Qvmt3
84
Km
˛m
˛s
80
ˇc
73
82
10,000'
70
84
72
79
QTp
81
l
Ys
85
9
29
45
50
75
26
QHa
12
20 51
l
af
Tmi
30
41
22
QTp
15
20
80
14
Pay
50
83 19
53
54
Kd Qpm3
53
QHao
81
Qay
61 70
Qca
67
85
ˇc
ll
l l
Qpx2
Ys
70
Yps
Ys
25
Yps
27
ˇc
ˇc
69 23
85
Qvmt3
˛m
ll l
33
Yps
Ys
5
8
QTp
l
75
25
˛s
13
20
20
74 74
34 71
ˇc
82
63
55 42
51 69 ˇm
14
40
8075
ˇz
83
56
42
70
71
Tmi
Qay 81 ˇc
2560
71
22
ˇc
73
76
35 45 10
Kd
65
55
23
73
13
Km
Jm
57
51
14
l l
lll l
?
QHao
44
12
Ys
l l l l l l l l l l
l l l l l l l l l l l l l l l l l l l l l l l
Qay
Yps
Tmi
84
l l l l l l
l l l l l l l l l l l l
Ys
?
24
Ys
af
l l l l l l l l
l l l
ll
l
38
Younger subunit (upper to middle Pleistocene) — Poorly to moderately consolidated and poorly to
moderately sorted deposits of very pale-brown to strong yellowish-brown (7.5-10YR), poorly to moderately
stratified and sorted, silty clay and loamy sand and gravel. Deposit surface (top) along the mountain
front is slightly to moderately dissected and exhibits subdued bar and swale topography on interfluves.
Soils are moderately developed and possess Stage II to III carbonate morphology and few to common,
thin to moderately thick clay films. Correlative to the geomorphic surface Q7 of Connell (1995, 1996).
Correlative to stream alluvium of Tijeras Canyon (Qpmt2), and generally correlative to unit P5 of Thomas
et al. (1995).
Older pediment surface — Broad, relatively low relief erosional surface on Sandia granite (Ys). Surface
projects to the basal contact of eastern-margin piedmont alluvium (Qpo). Surface projects between 50-100
ft (15-30 m) above Tijeras Creek.
Kvt
74
48
Ys
Middle pediment surface — Broad, relatively low relief erosional surface on the Sandia granite (Ys). Surface
is lower than the pediment surface of Qpx1 and correlated to the base of older eastern-margin piedmont
alluvium (Qpo). Surface projects between 50-100 ft (15-30 m) above Tijeras Creek.
.
Kvs
af
Ys
Ys
Qay
Younger pediment surface — Exposed erosional surface between Sandia granite (Ys) and overlying younger
stream alluvium (Qay).
Kv
Ys
89
Qvmt2
QTsp
4H
42
8
9
18
Yps
5
Tmi
76
28
Ys
Qvmt2
38
60
˛m
11
42
Ys
l
QHa
QTsp
Youngest subunit (upper Pleistocene) — Poorly consolidated and poorly to moderately sorted graybrown to reddish-brown, subangular to subrounded, pebble to cobble gravel with silty sand interbeds.
Inset against middle subunit Qpm2. Soils are moderately developed and exhibit Stage II carbonate
morphology. A radiocarbon date of more than 21,000 years BP reported by Thomas et al. (1995, p.
2-36, unit Pf5) indicates a late Pleistocene age. Correlative to stream alluvium of Tijeras Canyon (Qpmt3),
and generally correlative to units P5-P6 of Thomas et al. (1995).
Pediments, as mapped within the study area, are areally extensive, low-relief surfaces of erosion that were
probably cut by fluvial processes. Pediments grade to the former levels of major piedmont drainages and have
smooth, generally concave-up, surfaces that are commonly marked by tors and corestones. They are primarily
developed on Sandia granite (Ys), but are rarely preserved on Madera Formation, quartzite and metavolcanic
rocks. Pediments are also recognized as short benches preserved on spur ridges along the northwestern slope
of Cerro Pelon. Two generations of weathering rinds developed on corestones indicate that these surfaces
have experienced multiple periods of erosion (Smith et al., 1982), resulting in the formation of broad weatheringlimited slopes underlain by grus and Sandia granite. Up to 15 ft (4.5 m) of grussified granite, and rare
interbedded pebble lenses of weathered granite are locally preserved on pediment slopes. Locally divided
into four units on the basis of inset relationships and height above local base level.
.
l l l l l l l l
50
24
Ys
Qpm2
QTsp
Pediments
Tmi
88
Ys
af
Qpy
26
22
Tmi
36
Qpm1
Jt
QTpx
20
58
32 66
Qvmt1
Qvmt2
Older subunit (middle Pleistocene) — Moderately consolidated pebble to cobble gravel. Deposits
surface (top) is approximately 50-55 ft (15-17 m) above Tijeras Creek and represents the highest stream
gravel west of Seven Springs in Tijeras Canyon. Unit is locally overlain by about 5 ft (1.5 m) of grus
where inset against the Sandia granite (Ys). Soils locally exhibit Stage III carbonate morphology. Clasts
are dominated by granite, with local accumulations of metavolcanic, gneiss, sandstone and limestone.
Correlative to eastern-margin piedmont alluvium (Qpm1) and units Qf1a and Qa1 of Smith et al. (1982),
and generally correlative to units P3-P4 of Thomas et al. (1995).
Piedmont deposits (lower Pleistocene to Miocene) — Subhorizontally stratified to slightly east-tilted, reddishbrown to yellowish-brown and very pale-brown (7.5-10YR) conglomerate, gravelly sandstone, and sandstone
with subordinate siltstone and rare mudstone. Conglomerate clasts are predominantly composed of subangular
to subrounded granite with subordinate metamorphic rocks, and minor subrounded limestone. Unconformably
overlies Sandia granite (Ys) and is unconformably overlain by eastern-margin piedmont alluvium. A monitoring
well (4H) near the intersection of Tijeras Creek and Four Hills Road (Richey, 1991) encountered 69 ft (21 m)
of eastern-margin piedmont alluvium and Santa Fe Group piedmont deposits just west of the Sandia fault.
These deposits interfinger with and overlie early Pleistocene (Irvingtonian land mammal “age”) fluvial deposits
of the ancestral Rio Grande near the mouth of Tijeras Arroyo (see Lucas et al., 1993). May be correlative with
piedmont-slope and alluvial fan deposits of the Sierra Ladrones Formation (Machette, 1978) exposed at the
southern margin of the Albuquerque Basin. Estimated hydraulic conductivity is low. Base is not exposed, but
deposit thickens to the west across the Sandia fault zone to where it is several thousand feet thick.
Qpx3
65
Ys
Ys
Santa Fe Group
Qpx2
10
Ys
QTsp
51
34
Yps
QHa
Yps
54
Tmi
Yps
Ys
af
Qpm2
Middle subunit (upper to middle Pleistocene) — Moderately consolidated deposits of sandy to
cobbly gravel, with local accumulations of boulders. Minor light-brown to reddish-brown silty sand
interbeds. Clasts are composed of rounded to subangular limestone, granite, quartzite and sandstone.
Basal contact is irregular and sits about 50 ft (15 m) above top of the youngest stream alluvium (QHa).
Inset against stream alluvium of unit Qvmt1 and pediment surface Qpx1 and forms gravelly alluvium
within Tijeras Canyon. Two terraces are recognized near Seven Springs, but not differentiated. Soils
are moderately developed and exhibit Stage II to III carbonate morphology in gravel. Surface is typically
overlain by thin (<1 ft) layer of grus where inset against the Sandia granite (Ys). Correlative to easternmargin piedmont alluvium (Qpm2) and units Qf1a and Qa1 of Smith et al. (1982), and generally
correlative to unit P5 of Thomas et al. (1995).
Old eastern-slope alluvium (lower Pleistocene to upper Pliocene(?)) — Moderately consolidated and
poorly to moderately sorted gravel that forms the highest gravel preserved along the southeastern flank of the
Sandia Mountains. Locally contains two undivided subunits. Contains subrounded to subangular clasts of
limestone with minor (< 5%) sandstone and highly weathered, grussified granite and metamorphic rocks. The
basal contact is about 40-200 ft (12-60 m) above local base level. Deposits cover a formerly areally extensive
pediment developed along the southeastern flank of the Sandia Mountains that may be correlative to the Tuerto
gravel of Stearns (1953). Deposit surface (top) is dissected and soils are generally stripped, but locally exhibit
Stage III+ carbonate morphology. Variable thickness from 0-30 ft (0-10 m).
Qpx1
63
Ys
QHa
Older eastern-slope alluvium (middle to lower Pleistocene) — Poorly to moderately consolidated deposits
of yellowish-brown (10YR), poorly to moderately sorted and stratified, gravel and sand with thin silty-clay
interbeds. Forms alluvial fans that developed along relatively steep tributary drainages to the Arroyo de San
Antonio and Tijeras Creek. Gravel clasts are predominantly subrounded limestone with a greater proportion
of sandstone that in old eastern-slope alluvium (QTp). Overlies a formerly extensive erosional surface (pediment)
developed on the eastern dip-slope of the Sandia mountains. Deposit surface (top) is dissected and soils are
generally stripped, but locally exhibit Stage III carbonate morphology. Deposits grade to high pediment surface
QTpx in Tijeras Canyon. Variable thickness from 0-16 ft (0-5 m).
QTsp
Ys
33
62
53
D U
Eastern-slope alluvium
QTp
?
Ys
Yps
Ys
21
52
Tmi
31
Km
Qpo
84
Ys
Qpx2
Ys
Typically contains poorly to well sorted and stratified, clast- and matrix-supported sand and gravel with minor
muddy sand interbeds associated with modern and late Pleistocene entrenched arroyos and streams originating
in the northern Manzanita Mountains. Deposits unconformably overlie pre-Cenozoic rocks, and are differentiated
on the basis of inset relationships and soil-morphology. Clasts are commonly angular to subrounded limestone,
metarhyolite, gneiss, and quartzite.
Qvm1
71
?
Qpx2
Ys
Qpm2
Alluvium of Madera Canyon
Qvm2
˛m
49
50
Qpx2
Ys
Qpy
Qvm3
50 64
14
4
Middle eastern-margin piedmont alluvium, undivided (upper to middle Pleistocene) — Poorly to
moderately consolidated deposits of very pale-brown to strong-brown and light-gray (7.5-10YR) sand and siltyto clayey-sand, and gravel. Deposit surface (top) is 30-165 ft (9-50 m) above local base level. Gravel clasts
are predominantly subangular granite and schist with minor subrounded limestone derived from the western
front of the Sandia Mountains and Four Hills salient. Slightly to moderately dissected deposit surface exhibits
subdued constructional bar-and-swale topography on interfluves. Weakly developed soils exhibit Stage II to
III+ carbonate morphology and minor to moderate clay film development. Locally divided into three subunits
(Qpm1, Qpm2, and Qpm3). Variable thickness from 0-30 ft (0-9 m).
Qvm
Ys
?
Youngest subunit (upper Pleistocene) — Poorly to moderately consolidated deposits of sandy gravel
and cobble to boulder gravel. Unconformably overlies crystalline rocks with an irregular contact. Inset
against stream alluvium of units Qvmt1 and Qvmt2. Correlative to eastern-margin piedmont alluvium
(Qpm3) and units Qf1b and Qf2 of Smith et al. (1982), and generally correlative to unit P6 of Thomas
et al. (1995).
Middle stream alluvium of Madera Canyon, undivided (upper to middle Pleistocene) — Poorly to
moderately consolidated deposits of very pale-brown to strong-brown and light-gray (7.5-10YR) sand and siltyto clayey-sand, and gravel. Deposit top is 30-165 ft (9-50 m) above local base level. Gravel clasts are
predominantly subangular granite and schist with minor subrounded limestone derived from the western front
of the Sandia Mountains and Four Hills salient. Slightly to moderately dissected deposit surface exhibits subdued
constructional bar-and-swale topography on interfluves. Weakly developed soils exhibit Stage II to III+ carbonate
morphology and minor to moderate clay film development. Locally divided into three subunits (Qvm1, Qvm2,
and Qvm3). Variable thickness from 0-30 ft (0-9 m).
Qpx3
Ys
83
38
Qpm1
˛m
42
36
57
72
QHa
Ys
Ys
Younger eastern-margin piedmont alluvium (Holocene to uppermost Pleistocene) — Poorly to moderately
sorted and stratified gravel, sand with minor silt-clay mixtures inset against eastern-margin piedmont alluvium
(Qpm). Deposit surface (top) is moderately dissected and exhibits well developed to subdued bar-and-swale
topography. Soils possess Stage I to II carbonate morphology and weakly to moderately developed clay
films. Generally correlative to units H7-H9 of Thomas et al. (1995). Variable thickness from 0-30 ft (0-9 m).
Qpm2
Ys
D U
48
45
Qca
15
Yps
36
64
T. 10 N.
Qpm3
10
25
Yps
10
Qay
Yps
50
Ys
Pg
QHa
56
80
ˇm
60
68
84
47
72
52 69
65
48
55
63 54
Ps
64
45
27
52
81
47
Pyc
46 Pyc
ˇm
59
35 53
ˇz
40
67
72
80
Pyc 60 80
˛m
18
5514
39
Pay
45
45
55
Pg
Pyc
56
QTp
Yps
Qay
20
QHa
58
Jm
75
Qpm3
Jt
85
Pay
30
32
38
ˇz
26
Tijeras
fault zone
˛m
64
ˇz Jm
38
32
Ps
42
13
38
ˇm
35
13
31
6
Tmi
Qpx3
Ys
4
Typically contains poorly to moderately sorted and stratified, clast- and matrix-supported sand and gravel with
minor muddy sand interbeds associated coalescent range-front alluvial fans in the Sandia Mountains and Four
Hills salient. Deposits unconformably overlie Santa Fe Group deposits and older rocks, and are differentiated
on the basis of inset relationships and soil-morphology. Clasts are commonly angular to subangular granite
with minor subrounded limestone.
Qpm
D U
Ys
7
4
15
4
Qay
Qpm
Eastern-margin piedmont slope deposits
Qpy
36
25
46
Ys
83
Well cemented stream alluvium, undivided (middle Pleistocene) — Indurated, scattered lensoidal
accumulations of calcium-carbonate cemented, subangular to subrounded pebbly sandstone and pebble to
cobble conglomerate. Unconformably overlying pediments developed on Sandia granite (Ys). Probably
correlative to older subunit of the alluvium of Tijeras Creek (Qvmt1). Unit is less than 6 ft (2 m) thick.
Qvmtc
Ys
5
38
14
Pyc
34
28
30
48
31
8
11,000'
Km
71
80
11,000'
88 78
45
Kd75 26 Jm
49
12,000
feet ASL
Qca
Qca
ˇc
S
12,000
feet ASL
41
75
Qpo
45
QTp
10
32
34
48
2
Qpo
32
Ps Pg
42
15
Pyc
Yps
Yps
63 32
37
Ys
25 30
QTp
Qca
70 44
12
24
l l l l l l l l l l l l l l l
l
Qvm t1
34
59
38
Middle stream alluvium of Tijeras Canyon, undivided (upper to middle Pleistocene) — Moderately to
well-consolidated gravelly alluvium containing subrounded to subangular clasts of limestone with minor
sandstone, gneiss and metavolcanic rocks. Unit represents former position of the ancestral Tijeras and Madera
Creeks and is differentiated into three subunits on the basis of inset relationships. Soils are moderately to well
developed and possess Stage II to III calcic horizons in Tijeras Canyon (Smith et al., 1982). This unit commonly
contains unmapped inclusions of younger stream alluvium (Qay, Qayt, and QHa). Thickness is variable from
0-15 ft (0-5 m).
Qvm t2
34
Qpm
Younger stream alluvium of Tijeras Canyon (Holocene) — Deposits contain variable proportions of gneiss,
limestone, sandstone and minor granite within the Tijeras drainage. Locally includes undivided stream alluvium
(QHa) in narrow arroyos. A minimum age is constrained by a radiocarbon date of 1,790 ±90 years BP (Locality
1, Beta Analytic Labs No. 104958) near the top of the deposit. Correlative to unit H7 of Thomas et al. (1995)
and unit Qa2 of Smith et al. (1982), and correlative to geomorphic surfaces Q8 and Q9 of Connell (1995,
1996). Variable thickness from 0-20 ft (0-6 m).
Qvm t3
QHa
˛m
8
Ys
Tmi
Qpx3
Ys
Ys
05'
Typically contains moderately to well sorted and stratified, clast- and matrix-supported sand and gravel with
minor muddy sand interbeds associated with the Tijeras Creek drainage. Deposits are differentiated into a
trunk stream that interfingers with steeper tributary drainages to Tijeras Canyon (unit Qay). Clasts are commonly
subangular to subrounded granite, metarhyolite, limestone, yellowish-brown and reddish-brown sandstone
derived from the headwaters of the Tijeras Canyon drainage-basin. Unconformably overlie Santa Fe Group
deposits and older rocks, and are differentiated on the basis of inset relationships and soil-morphology.
Qvm t
Yps
Ys
Ys
Alluvium of Tijeras Creek
Qay t
Tmi
75
Yps
5
42 Ps
Pg
80
˛s
11
Tmi
Qpx3
Ys
Qay
Younger stream alluvium (Holocene to uppermost Pleistocene) — Poorly consolidated deposits of lightbrown to dark-gray, fine-grained silty sand with minor pebbly sand and clayey sand interbeds; pebble lenses
are common along basal contact. Unit forms broad terraces ranging from 8-30 ft (3-9 m) above Tijeras and
Madera Creeks. Two terrace levels are locally recognized, but not differentiated, within Tijeras Canyon. Clasts
are chiefly rounded limestone with minor granite, metavolcanic and gneiss within Madera Canyon. The trunk
stream of the Tijeras Canyon drainage is divided into unit Qayt. Locally includes undivided stream alluvium
(QHa) in narrow arroyos. Soils are weakly developed and exhibit Stage I and II carbonate morphology.
Deposit age is constrained by a radiocarbon of about 10,000 years BP (Thomas et al., 1995, p. 2-43).
Correlative to unit H7 of Thomas et al. (1995), and correlative to geomorphic surfaces Q8-Q9 of Connell
(1995, 1996). Variable thickness from 0-20 ft (0-6 m).
Qay
QHa
D U
65
6
Yps
Pg
QTp
30
41
QHao
14
77
18
Qca
20 24
26
20
Pg
35
Pg 31
QTp
Ys
Yps
Qpm
D U
Pay 68
75
10
Yps
l l l l l l l l l l l l l l l l l l l l l l l l l
l l l l
l l l
l
l l
l l l l l l
l l l l l l l l l l l l l l l l
QHao
?
strand
Youngest stream alluvium, undivided (Historic to upper Holocene) — Unconsolidated deposits of brown,
light gray-brown, and yellowish-brown (10YR) sand, silty to clayey sand, and gravel. Underlies modern arroyos
and inset against younger stream alluvium (Qay). Color and clast composition varies with drainage-basin
composition, but gravel typically contains limestone, gneiss, quartzite, sandstone, granite and metarhyolite.
Deposit surface exhibits no pedogenic development, and unit locally forms small alluvial fans within low-order
tributary drainages of Madera and Tijeras Canyons. Locally divided into an older terrace (QHao) on the basis
of inset relationships. Deposits locally contain asphalt fragments and construction debris. The age is constrained
by radiocarbon dates ranging between 1,000 to 3,000 years BP (Thomas et al., 1995, p. 2-37 and 2-43).
Correlative to units H8 and H9 of Thomas et al. (1995), and correlative to geomorphic surface Q9 of Connell
(1995, 1996). Variable thickness from 0-10 ft (0-3 m).
84
Yps
QHa
37
Qay
ˇc
32
ˇc
18
28 15
Pg
37
36
Qpo
28
Ps
33
QTp
Qay
Qca
30
Qca
Ps
39
20
Qca
Yps
l l l l l l
l l l l l l l
38
14
l l
l l l l
l l l l
l l
l l
l l
l l
B
25
l
Typically contains poorly to well sorted and stratified, clast- and matrix-supported sand and gravel with minor
muddy sand interbeds associated with modern and late Pleistocene entrenched arroyos and streams originating
in the Sandia and Manzanita Mountains. Deposits unconformably overlie Santa Fe Group deposits and older
rocks, and are differentiated on the basis of inset relationships and soil-morphology.
.
Qpo
55
49
Qca
36
Pg
39 32
ˇc
41
55
15
Ys
9
Qca
29
25
26
75
64
43
14
l l l l
l l l l
l l
l l
Stream-valley Alluvium
Ys
Yps
l
Qpm
47
21
5
5
32
ll
85
38
73
ˇc 53
ˇc
QTp
24
51
30
A'
N
50
n
ce
38
Pay
Ps
Qca
19
23
87
17
14
Tmi
QHao
Pg
20
60
86
67
l
QHa
75
46
ll l l
Qpy
Qpm
Qpm
21
Qay
38
Qca
7
Pg
Ps
20
Tmi
36
25
Yps
46
34
10
strand
Sandia fault zone – West Embudo
Colluvium and alluvium, undivided (Holocene to upper-middle Pleistocene) — Poorly consolidated,
poorly sorted and stratified, fine- to coarse-grained, clast- and matrix-supported deposits derived from a variety
of mass-movement hill slope processes, including debris flow, shallow slump and creep. Gravel clasts are
typically angular to subangular and composition reflects local provenance. Soils locally exhibit Stage I to III
carbonate morphology. Clasts are typically angular and composition generally reflects local provenance.
Commonly surrounds small undivided inliers of Madera Formation limestone on the eastern dip-slope of the
Sandia Mountains. Differentiated where areally extensive, thick, or where geologic contacts are obscured.
Variable thickness, up to 12 ft (4 m).
9
14
39
QHa
A
33
QTp
20
24
19
5
Pyc
˛m
4
50
Yps
38
57
55
32
ll
86
Yps
Tmi
59
˛m
Ps
Qca
31
Pay
81
ll
38
Travertine and spring deposits (upper Pleistocene to upper Pliocene?) — Light-gray nodular to massive
constructional mounds of travertine interlayered with mudstone and conglomerate derived from local upland
sources. Unit is commonly associated with springs along the eastern dip-slope of the Sandia Mountains. Variable
thickness, ranging from 3-30 ft (1-10 m).
Ys
65
QHa
Qay
ˇc
33
22
7
Qay
34
Ps 27
n
Vi
S an d i a fa u lt z o n e – Ea s t Embud o
Qpy
Artificial fill (Historic) — Dumped fill and areas affected by human disturbances. Locally mapped where
areally extensive or geologic contacts are obscured.
.
QHa
23
QHa
87000m N.
Thin surficial deposits derived from wind and mass-movement processes, or extensive areas disturbed by openpit aggregate mining or construction.
10
l l l l l l l l
38
CENOZOIC DEPOSITS
Neogene (Quaternary and Tertiary) System
Colluvial, landslide, eolian, and anthropogenic deposits
QTt
10
82 7
43
UNIT DESCRIPTIONS
Qca
41 42
QTp
Qca
25 84
36
15
G EOLOGIC C ROSS S ECTIONS
1 500 000
FEET
EDGEWOOD 13 MI.
MADRID 29 MI.
14
64
Pg
17
14
ll
17
Qpy
Qpm
af
Yps
Yps
ll
Dr. Paul W . Bauer
Geologic Mapping
Program Director
Dr. Peter A. Scholle
Director and State Geologist
5
Pay
15
Ys
ˇz
30
ˇm
10
Ps
Qay
42 25
21
llll
Yps
59
QHa
Pay
28
Ps
30
Qay
ˇm 14
Ps
23
17
Qca
25
31
106° 22' 30"
35° 07' 30"
74000m E.
(SEDILLO)
P
EMA
l
AT
l
n
nce fo r t h e 21st Ce
67
lll
Scie
QTp
32
Pay
Ys
3
Ps
43
l ll l l l l
l l
l l
l l
rth
460 000 FEET
73
42 18
38
ll
S
T
y
tur
3
˛s
Qpm
Ea
72
71
llll
Tec h
3
3
25'
ESCABOSA 11 MI.
MOUNTAINAIR 50 MI.
C
(SANDIA CREST)
llll
68
ll
3
ll
66
QHa
l
27' 30"
3
65
l lll
3
l
64000m E.
ll
3
R. 5 E.
l
lll l
106° 30'
35° 07' 30"
ll l
NE
NEW MEXICO
A
l
NM B
ur
e
TIJERAS QUADRANGLE
lll
Me x i c o
CO
Ne w
W
I
ll l llll
e
ME X
S)
TA
CI
LA
(P
i n e s & Mi n e r a
lR
ces
ur
so
a
fM
uo
NMBMMR Open File Map Series
OF–GM–4
Map last modified 28 February 2000
MEXICO INSTITUTE OF MINING & TECHNOLOGY
l ll
A DIVISION OF NEW
Xms
Xq
Xla
Xp
Xdt
Xmv
Exploratory or groundwater monitoring well, including abbreviation
Xr
Yps
Xbg
Xlg
Xcf
Ya
Xcm
Xcc
Yss