NMBMMR Open File Map Series
OF–GM–6
Map last modified 22 February 2000
AN
)
O
(H
AG
˛m
16
12
13
?
•
•
••
•
?
••
•
••
••••
?
?
?
?
?
?
?
40
3
70
25'
3
3
71
7000 FEET
ˇc
22
18
Qca
Ps
N.
T. 11 N.
5,000
ˇc
Pg
Ps
Qca
3
74000m E.
Ys
ˇz
35° 07' 30"
106° 22' 30"
Ys
4,000
3,000
3,000
Tmi
2,000
2,000
22 February 2000 Revision
E XPLANATION OF M AP S YMBOLS
by Adam S. Read 1 , Karl E. Karlstrom 2 , Sean Connell 1 ,
Eric Kirby 2 , Charles A. Ferguson 3 , Bradley Ilg 2 , Glenn R. Osburn 4 ,
Dirk Van Hart 5 , and Frank J. Pazzaglia 2
A
Location of geologic cross section
A'
1 New Mexico Bureau of Mines and Mineral Resources, Socorro, NM 87801
Anticline — Trace of axial plane showing direction of plunge; dashed where approximately located, dotted where concealed,
queried where inferred
Syncline— Trace of axial plane showing direction of plunge; dashed where approximately located, dotted where concealed,
queried where inferred
••
Scree, talus, and colluvium, undivided (Holocene to upper-middle Pleistocene) — Coarse-grained,
angular, clast-supported talus found primarily in first-order hollows on steep, west-facing slopes of the Sandia
Mountains.
Travertine (Pleistocene) — Constructional mounds of travertine ranging from 1 to 10 m thick, typically found
around active springs. Variable thickness, between 3-30 ft (1-10 m) thick.
Alluvium
Divided into stream-valley alluvium, eastern basin-margin piedmont alluvium, and eastern-slope alluvium. Streamvalley alluvium typically contain moderately to well sorted, poorly to well stratified, clast- and matrix-supported
deposits associated with modern and late Pleistocene entrenched arroyos across the map area. Eastern basinmargin piedmont alluvium contains generally poorly sorted, poorly stratified, clast- and matrix-supported
deposits having angular to subangular clasts of granitic, metamorphic, and minor limestone derived from the
western and northern slopes of the Sandia Mountains on the footwall of the Sandia fault (eastern margin of
the Albuquerque Basin). Eastern-slope alluvium typically contain very poorly to moderately sorted, clast- and
matrix-supported deposits associated with drainages developed on the eastern dip-slope of the Sandia
Mountains and headwater region of the Tijeras Canyon drainage.
Qay
Youngest stream alluvium, undivided (Historic to Holocene) — Unconsolidated deposits of brown, light
gray-brown, and yellowish-brown (10YR) sand, silty to clayey sand, and gravel. Underlies arroyos and is inset
against younger stream alluvium (Qay). Very weakly developed soils exhibit no pedogenic carbonate at the
surface and weak Stage I carbonate morphology at depth. Correlative to geomorphic surface Q8 and Q9
of Connell (1995, 1996). Variable thickness, from 0-20 ft (0-6 m).
Younger stream alluvium, undivided (Holocene to uppermost Pleistocene) — Poorly consolidated
deposits of pale-brown to light-brown (7.5-10YR) sand to sandy clay loam and gravel. Inset against middle
piedmont and western-margin alluvium (Qpm). Surface is slightly dissected and possesses weakly developed
soils with Stage II carbonate morphology. Remnants of the lower pediment surface (Qpx3) is preserved in Juan
Tabo Canyon and probably corresponds to the basal contact of this unit. Correlative to geomorphic surface
Q8 of Connell (1995, 1996). Variable thickness, from 0-25 ft (0-8 m).
Paleogene-Cretaceous Systems
TKu
Tmi
Pay
MESOZOIC ERATHEM
Upper Cretaceous
Pyc
Menefee Formation, undivided — Cross section only. Gray, tan to orange-tan, cross-bedded, and laminated
to thick-bedded siltstone and sandstone; dark-gray to olive-gray and black shale; dull, dark-brown to shiny
black lignitic coal; and maroon to dark-brown iron concretions. The lower contact between the Menefee
Formation and the Point Lookout Sandstone (Kpl) is interfingering and gradational. Total unit thickness varies
regionally from 680 ft to 1,200 ft (205 m to 365 m) due in part to post-depositional erosion.
.
Kmf
Point Lookout Sandstone — Cross section only. Gray-tan to light-tan and drab-yellow, very fine- to finegrained, massive, quartz sandstone with limonitic sandstone lenses and interbedded thin gray shale. Unit
thickness ranges from about 240 ft (73 m) near Placitas, to 315 ft (96 m) in the Hagan embayment.
Kpl
Strike and dip of magmatic foliation in granite defined by alignment of megacrysts
Strike and dip of pegmatite dikes and veins
Trend and plunge of lineation —defined by elongate minerals or stretched grains
Kd
˛ms
˛s
Middle Jurassic
San Raphael Group — Locally includes the Summerville (Js), Todilto (Jt), and Entrada (Je) Formations as
recently defined by Lucas et al. (1995) and Lucas and Anderson (1997). Exposed only within a highly fractured
fault-bounded block of Mesozoic rocks located just south of the Jaral fault and Rincon Ridge (see Van Hart,
in press). Total estimated San Raphael Group thickness in this fault block is 128 ft (39 m).
.
Js
Je
San Raphael Group, Todilto Formation (Luciano Mesa Member) — A thinly laminated, petroliferous,
dark-gray, micritic limestone. Fossils are not recognized, but laminations are probably algal in origin.
The overlying Tonque Arroyo Member appears to be absent in this area (Van Hart, in press). A very
small outcrop of this important stratigraphic marker is overlain by the Summerville Formation, underlain
by the Entrada Formation, and is approximately 3 ft (1 m) thick.
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; also locally contains limestone-pebble conglomerate lenses. Exposures confined to
limited outcrop just south of the Jaral Fault and near the Village of Cañoncito (on the southeastern corner of
the map). Total Chinle Group thickness is about 1300 ft (400 m).
ˇc
ˇz
Chinle Group, Agua Zarca Formation — The only distinct sub-unit of the Chinle Group recognized
during this study (differentiated near the Village of Cañoncito). It is a tan- to light-grayish pink, resistant,
thin- to medium-bedded quartz arenite and feldspathic arenite. The lower contact with the underlying
Moenkopi Formation (ˇ m) is disconformable. The unit is about 350 ft (105 m) thick.
.
Mississippian
Ma
Arroyo Peñasco Group, Espiritu Santo Formation — The locally thin and discontinuous Espiritu Santo
Formation unconformably overlies Proterozoic basement. Generally only the basal Del Padre Sandstone
Member is present, but the limestones, dolomites, and limey mudstones of the unnamed upper member are
preserved in places north of Sandia Peak. Microfossils from these carbonate rocks near Placitas and other
areas indicate an Osagean age (Armstrong and Mamet, 1974). No other formations within the Arroyo Peñasco
Group have been recognized in the map area. The thickest section and best exposure of the Arroyo Peñasco
Group in the region of the Sandia Mountains is on the west slope of the Crest of Montezuma east of Placitas
(Armstrong and Mamet, 1974; Connell et al., 1995). The Del Padre Sandstone is a distinctive sedimentary
quartzite and quartz-pebble conglomerate that is generally very white and extremely well lithified. The silicified
finer-grained varieties of quartzite from the Del Padre Sandstone are easily mistaken for metamorphic rocks
but have no apparent foliation and have visible rounded grains on weathered or broken surfaces. Additionally,
these quartzites and associated quartz pebble conglomerates are only seen along the Great unconformity
between Proterozoic basement and the Pennsylvanian Sandia Formation. Mineralized faults and fractures
containing barite-flourite-galena and quartz are often seen in these rocks. Some of these structures apparently
do not extend above the Sandia Formation and are therefore interpreted as the result of pre-Madera Formation
deformation. The age of the mineralization is unknown. These rocks were previously considered Proterozoic
metasediments (see Kelley and Northrop, 1975) and some clearly are metamorphic based on recent thin
section study (Read et al., 1999). However, based on stratigraphic position, the lack of foliation, and on study
of several thin sections, the bulk of the rocks mapped as Arroyo Peñasco Group are sedimentary rocks that
did not experience the high-grade metamorphism typical of Proterozoic supracrustal rocks in this area. Generally
less than 50 ft (15 m) thick where preserved.
PROTEROZOIC ERATHEM
Mesoproterozoic igneous rocks
Pegmatite and aplite dikes — Dikes, pods, and lenses ranging from <1 in to >50 ft (<30 cm to >15 m) in
thickness and perhaps up to 2,600 ft (800 m) in length; interpreted to be coeval with the Sandia granite (Ys).
? ?
? ?
A BIQUIU 1:100,000
13
17
Qfo
Qpo
19
R EFERENCES
Middle pediment surface — Broad, relatively low relief erosional surface on the Sandia granite (Ys). Surface is topographically
lower than pediment surface of unit Qpx1 and correlated to the base of older eastern-margin piedmont alluvium (Qpo). Provisionally
correlated to geomorphic surfaces Q4-Q5 of Connell (1995, 1996).
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.
GM–26
GM–27
LA
VENTANA
SAN
MIGUEL
MOUNTAIN
GM–28
VALLE
SAN
ANTONIO
SEVEN
SPRINGS
JEMEZ
SPRINGS
GILMAN
GM–33
GM–45
SAN
YSIDRO
OF-DM–18
106°30'
35°15'
VALLE
TOLEDO
WHEELER
PEAK
36°30'
OF-DM–43
PUEBLO
PEAK
BLAND
BEAR
PONDEROSA SPRINGS
PEAK
LOMA
CRESTON
JEMEZ
PUEBLO
OF-DM–25
CAÑADA
COLLIER
DRAW
(SKY VILLAGE NW)
QTug
OF-DM–42
COCHITI
DAM
SANTO
DOMINGO
PUEBLO
OF-DM–15
L OS A LAMOS 1:100,000
OF-DM–14
SANTA
ANA
PUEBLO
CERRO BERNALILLO
CONEJO
NW
OF-DM–45
(SKY VILLAGE NE)
SAN
FELIPE
PUEBLO
SAN
FELIPE
PUEBLO NE
OF-DM–19
OF-DM–37
PLACITAS
OF-DM–2
BENAVIDEZ
RANCH
QTsp
VOLCANO
RANCH
LOS
GRIEGOS
LA MESITA
NEGRA
DALIES
NW
RIO
PUERCO
DALIES
ALAMEDA
OF-DM–10
BELEN
NW
BELEN
SANDIA
PARK
OF-DM–6
OF-DM–1
TIJERAS
40
SEDILLO
OF-DM–4
GM–73
PEÑASCO
TRES
RITOS
ISLETA
HUBBELL
SPRING
OF-DM–13
OF-DM–5
OF-DM–8
LOS
LUNAS
SE
BOSQUE
PEAK
SHADY
BROOK
TRUCHAS
JICARITA
PEAK
EL VALLE
T AOS 1:100,000
SIERRA
MOSCA
CUNDIYO
36°00'
TRUCHAS
PEAK
PECOS
FALLS
COWLES
ASPEN
BASIN
285
MONTOSO
PEAK
SANTA FE
OF-DM–32
McCLURE
RESERVOIR
OF-DM–7
TETILLA
PEAK TURQUOISE SETON
HILL
VILLAGE
25
ELK
MOUNTAIN
OF-DM–47
AGUA
FRIA
PICTURE
ROCK
OF-DM–40
OF-DM–31
PECOS
LOWER
COLONIAS
OF-DM–11
S ANTA F E 1:100,000
OF-DM–41
MADRID
HONEY
BOY
RANCH
ROSILLA
PEAK
GLORIETA
OF-DM–23
BULL
CANYON
GALISTEO
OF-DM–49
35°30'
NORTH
ROWE SAN YSIDRO
285
OF-DM–30
GOLDEN
CAPTAIN
DAVIS
MOUNTAIN
OJO
WILDHORSE
RENCONA
HEDIONDA
MESA
OF-DM–36
OF-DM–48
OF-DM–39
SAN
PEDRO
LAGUNA
ORTIZ
35°15'
105° 30'
KING
DRAW
OF-DM–29
EDGEWOOD MORIARTY
OF-DM–35
NORTH
OF-DM–20
A LBUQUERQUE 1:100,000
OF-DM–3
OF-DM–21
Base not exposed
SANDIA
CREST
OF-DM–17
LOS
LUNAS
OF-DM–33
V ILLANUEVA 1:100,000
LA MESITA
ALBUQUERQUE
NEGRA SE ALBUQUERQUE
EAST
WEST
WIND
MESA
OF-DM–12
TESUQUE
HORCADO
RANCH
WHITE
ROCK
HAGAN
OF-DM–50
OF-DM–16
RANCHOS
DE TAOS
84
BERNALILLO
OF-DM–9
CHIMAYO
Santa Fe
SANTO
DOMINGO
PUEBLO SW
OF-DM–26
OF-DM–46
ESPAÑOLA
GUAJE
MOUNTAIN
TAOS SW
GM–71
PUYE
Los
Alamos
FRIJOLES
REDONDO
PEAK
GM–34
HOLY
GHOST
SPRING
OJITO
SPRING
5.3
Connell, S. D., 1998, Geology of the Bernalillo 7.5-minute quadrangle, Sandoval County, New Mexico, New
Mexico Bureau of Mines and Mineral Resources, Open-File Digital Map 16, scale 1:24,000.
RANCHO
DEL
CHAPARRAL
? ?
21
Upper pediment surface — Broad, relatively low relief erosional surface on Sandia granite (Ys). Surface projects to the basal
contact of eastern-margin piedmont alluvium (Qpo) and is provisionally correlated to geomorphic surfaces Q2-Q3 of Connell
(1995, 1996).
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 OpenFile Report 425, 414 p., 3 plates (open-file release of Connell, 1995).
Connell, S. D., 1997, Geology of the Alameda 7.5-minute quadrangle, Bernalillo and Sandoval Counties, New
Mexico: New Mexico Bureau of Mines and Mineral Resources, Open-File Digital Map 10, scale 1:24,000.
SAN
PABLO
VELARDE TRAMPAS
68
SAN
JUAN
PUEBLO
CHILI
(SKY VILLAGE)
Lower pediment surface — Exposed erosional surface between Sandia granite (Ys) and overlying younger stream alluvium
(Qay). Probably correlative to geomorphic surface Q8 of Connell (1995, 1996).
MOUNT
ESCABOSA
WASHINGTON
35°00'
CHILILI
MORIARTY
SOUTH
TAJIQUE
MILBOURN
RANCH
ESTANCIA
TORREON
EWING
MOUNTAINAIR
NE
OF-DM–24
TOME
CAPILLA
PEAK
TOME NE
OF-DM–27
23.7
Connell, S. D., Allen, B. D., and Hawley, J. W., 1998, Subsurface stratigraphy of the Santa Fe Group using
borehole geophysics, Albuquerque area, central New Mexico: New Mexico Geology, v. 20, n. 1, p. 27.
VEGUITA
Tmi
Paleogene
COMANCHE
RANCH
KTu
TURN
BELEN
SW
TOME SE
MANZANO PUNTA DE
MOUNTAINAIR
PEAK
AGUA
Connell, S. D., Cather, S. M., Karlstrom, K. E., Read, A. S., Ilg, B., Menne, B., Andronicus, C., Bauer, P. W.,
and Johnson, P. S., 1995, Geology of the Placitas 7.5-minute quadrangle, Sandoval County, New Mexico:
New Mexico Bureau of Mines and Mineral Resources, Open-file Digital Geologic Map OF-DM 2, scale
1:24,000.
Kmf
Juan
Tabo
Cabin
+
Ferguson, C. A., Timmons, M., Pazzaglia, F., Karlstrom, K. E., 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-DGM 1, scale 1:24,000.
.
Sandia
+
Crest
Geohydrology Associates, Inc., 1993, Geohydrologic studies at High Desert, Bernalillo County, New Mexico:
Albuquerque, New Mexico, 87107, 13p.
556
Karlstrom, K. E., Connnell, S. D., Ferguson, C. A., Read, A. S., Osburn, G. R., Kirby, E., Abbott, J., Hitchcock,
C., Kelson, K., Noller, J., Sawyer, T., Ralser, S., Love, D. W., Nyman, M., Bauer, P. W., 1999, Geology of
the Tijeras 7.5 minute quadrangle, Bernallillo County, New Mexico: New Mexico Bureau of Mines and
Mineral Resources, Open-file Digital Geologic Map OF-DGM 4, scale 1:24,000.
.
n
anyo
C
Pino
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, 136 p.
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.
Kirby, E., Karlstrom, K. E., and Andronicus, C., 1995, Tectonic setting of the Sandia pluton: An orogenic 1.4
Ga granite in New Mexico, Tectonics, v. 14, p. 185-201.
Lozinsky, R. P., 1994, Cenozoic stratigraphy, sandstone petrology, and depositional history of the Albuquerque
basin, central New Mexico, in Keller, G.R., and Cather, S.M., eds., Basins of the Rio Grande rift: Structure,
Stratigraphy, and Tectonic setting: Geological Society of America, Special Paper 291, p. 73-82.
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.
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.
a
fM
uo
Ne w
Read, A. S., Allen, B. D., Osburn, G. R., Ferguson, C. A., and Chamberlin, R., 1998, The Geology of the Sedillo
quadrangle, Bernallio County, New Mexico, New Mexico Bureau of Mines and Mineral Resources, Openfile Digital Geologic Map OF-DGM 20, scale 1:24,000.
Read, A. S., Karlstrom, K. E., Ilg, B., in press, Mississippian Del Padre Sandstone or Proterozoic Quartzite?,
minipaper in: New Mexico Geological Society, 50th Field Conference Guidebook.
.
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.
Stearns, C. E., 1953, Tertiary geology of the Galisteo-Tonque area, New Mexico: Geological Society of
America Bulletin, v. 64, p. 459-508.
Tilton, G. R., and Grunenfelder, M.H., 1968, Uranium-lead ages, Science, v. 159, p. 1458-1461.
Ea
i n e s & Mi n er
al
Re
Me x i c o
rth
Scie
nc e for t he 21st C
Dr. Peter A. Scholle
Director and State Geologist
.
Van Hart, D.,1999, in press, Geology of Mesozoic sedimentary rocks in the Juan Tabó area, northwestern
Sandia Mountains, Bernalillo County, New Mexico: New Mexico Geology, v. 21, n. 4.
.
W
MEX
AT
I
EMA
Dr. Paul W . Bauer
Geologic Mapping
Program Director
NEW MEXICO BUREAU OF MINES AND MINERAL RESOURCES
A DIVISION OF NEW
BLACK
BUTTE
LA JOYA
SILVER
CREEK
SAN
ACACIA
BECKER
SW
Khd
109°
107°
34°
22'
30"
LEMITAR
MESA
DEL
YESO
CERRO RAYO HILLS
MONTOSO
SIERRA
DE LA
CRUZ
Grants
35°
WATER
CANYON
SOCORRO
Albuquerque
BUSTOS
WELL
Las
Cruces
Location Map
OF-DM–34
Jm
Socorro
Deming
LOMA
DE LAS
CANAS
SANTA FE
33°
OF-DM–38
Kd
103°
Taos
106°30'
SAN
LORENZO
SPRING
105°
37°
SCHOLLE
Kpl
Kmu
BECKER
107°00'
Js
Jt
ˇc
ˇz
ˇm
T
y
ABEYTAS
34°30'
106°00'
Je
Tec h
ur
ent
S OCORRO 1:100,000
LADRON
Kml
Physiography of the Sandia Crest
quadrangle based upon 10-m USGS
DEM data.
35°07' 30"
106°22' 30"
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. 247255.
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.
LA JOYA
NW
WILLARD
B ELEN 1:100,000
OF-DM–28
S
San Raphael Group, Entrada Formation — Variably colored, very fine to fine-grained, weakly
cemented, crossbedded, eolian, quartz sandstone with coarser grained components. These rocks are
very poorly exposed south of the Jaral fault. The lower contact with the Chinle Group (ˇ c) is disconformable.
Estimated local thickness of 75 ft (23 m).
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 (Ma) or Proterozoic crystalline rocks. 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.
Qca
15
Exploratory or groundwater monitoring well, including abbreviation. HD-1 and HD-2 data from Geohydrology Associates (1993);
SHO3 and SHOCH and data from G. Hall (unpubl. data, 1998).
SHO3
CO
Jt
San Raphael Group, Summerville Formation — Purple-gray, red-brown, and green-gray mudstone
interbedded with tan, gray, and greenish-gray, very fine grained sandstone. These rocks are assigned
to the Summerville Formation based on stratigraphic position (previously called the Recapture Shale
Member of the Morrison Formation--see Lucas et al., 1995; and Lucas and Anderson, 1997). Estimated
exposed thickness is 50 ft (15 m).
Madera Formation, massive limestone beds — Prominent ledge forming limestone beds, mapped
as marker units where possible. Up to approximately 40 ft (12 m) thick.
84
ARROYO
LOMA
SAN
DE LAS
MACHETE
FELIPE
CALABACILLAS
MESA (SKY VILLAGE SE)
TAINS
Morrison Formation, Salt Wash Member — Light tan to yellowish white, massive, friable sandstone exposed
only in a highly fractured fault-bounded block of Mesozoic rocks just south of the Jaral fault and Rincon Ridge.
Exposed thickness is approximately 85 ft (26 m) compared to an estimated thickness of 216 ft (66 m) for the
Salt Wash Member exposed near Placitas (see Van Hart, in press). Total Morrison Formation thickness varies
regionally, ranging from about 850 ft (260 m) near Placitas, to 780 ft (240 m) in the Hagan embayment.
Jm
˛mc
Qpm1
11
LOS
CORDOVAS
OF-DM–22
30 km
285
Water-supply well, including number assigned by the New Mexico Office of the State Engineer
RG31974
UN
Upper Jurassic
Madera Formation, sandstone and arkose beds — Sandstones and arkosic sandstones, mapped
as marker units where possible. Up to approximately 60 ft (18 m) thick.
1.8 Ma
MO
Dakota Formation — Cross section only. Medium-bedded, pervasively silica-cemented, medium-grained,
yellowish-gray to orange-yellow quartz arenite. Unit thickness ranges from 75 ft (23 m) west of Placitas, to less
than 25 ft (8 m) in the Hagan embayment.
Prospect, mine
IA
Mancos Shale, lower member — Cross section only. Lithology is similar to the upper Mancos Shale (Kmu)
with subequal proportions of olive-brown to gray to black shale and laminated to interbedded, olive-brown
to gray, very fine grained sandstone, siltstone, and shale. Unit thickness is highly variable regionally and across
the study area, ranging from 850 ft (260 m) west of Placitas to 1850 ft (565 m) in the Hagan embayment.
Kml
Gravel of Lomos Altos (upper Pliocene) — Thin gravel lag consisting of subrounded limestone pebbles and
cobbles derived from eastern dip-slope of the northern Sandia Mountains. Probably correlative to the Gravel
of Lomos Altos on the northern flank of the Sandia Mountains (Connell et al., 1995). May also be equivalent
to the Tuerto gravel of Stearns (1953). Approximately 3-30 ft (1-10 m) thick.
Madera Formation, undivided — Two informal members, an arkosic limestone and a gray limestone, are
recognized but not differentiated. The upper arkosic limestone is a gray, greenish-gray, olive-gray, tan and buffbrown 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, are commonly
lenticular, and often laterally discontinuous. Arkosic sandstones are typically coarse- to medium-grained and
often contain granules and pebbles. The lower gray limestone is a gray, ledge-forming, cherty limestone
separated by thinner and less resistant intervals of light-brown, pale greenish-brown, tan, greenish-gray, and
gray, argillaceous limestone. 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., 1998) and Tijeras (Karlstrom et al., 1999) 7.5-minute quadrangles rather than biostratigraphically
defined and may therefore not strictly correllate 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 ft) 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
Hosta-Dalton Sandstone — Cross section only. Drab, yellow-gray to yellow-tan, very fine- to medium-grained,
weakly cemented sandstone with olive-brown sandstone lenses. Unit thickness ranges from 210 ft (64 m) near
Placitas to 370 ft (112 m) in the Hagan embayment.
Khd
Yeso limestone — 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.
Upper and Middle Pennsylvanian
Mancos Shale, upper member — Cross section only. Medium- to dark-gray to olive-gray shale, and silty
shale, with less abundant very fine to fine-grained, locally gypsiferous sandstone. This unit is an upper tongue
of the lower member of the Mancos Shale (Kml). Thickness is variable, but ranges from about 240 ft (73 m)
west of Placitas, to 360 ft (110 m) in the Hagan embayment.
Kmu
Old eastern-margin piedmont alluvium, undivided (lower Pleistocene to upper Pliocene(?)) — Moderately
consolidated, poorly to moderately sorted and stratified gravel and sand with minor, thin silty-clay interbeds.
Gravel clasts are granite with rare limestone. Granite clasts are commonly grussified and deeply pitted. Remnants
of upper and lower pediment surfaces (Qpx1 and Qpx2) are locally preserved on Sandia granite (Ys) and
probably correspond to the stripped base of unit QTp. Correlative to geomorphic surfaces QT1-Q3 of Connell
(1995, 1996), older eastern-margin piedmont alluvium (Qpo) or the Suela alluvium (Qss) exposed on the
Placitas and Bernalillo quadrangles (Connell, 1998, and Connell et al., 1995, respectively). Variable thickness,
from 0-45 ft (0-14 m).
Eastern-slope pediment-alluvial fan complex (middle Pleistocene) — Alluvial fan deposits that overlie
broad, northeast-sloping pediment surfaces cut on older sedimentary rocks. Correlative to piedmont-alluvial
fan complexes (unit Qpf) on the adjacent Sandia Park quadrangle (Ferguson et al., 1996). Variable thickness,
ranging from 10-20 ft (3-20 m).
72
D
Qpf
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).
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).
Mafic or intermediate dike (upper Oligocene?) — Generally deeply weathered mafic to intermediate,
steeply dipping, north trending dikes. These are probably correlative to an Oligocene mafic to intermediate
dike exposed on the northern flank of the Sandia Mountains (Connell et al., 1995).
.
l l l l l l l l l
Middle eastern-margin piedmont alluvium, older subunit (middle Pleistocene) — Moderately
consolidated deposits of light- to strong-brown (7.5YR) and very pale-brown to light-gray (7.5-10YR),
poorly to moderately stratified and sorted, sand clayey sand and gravel. Dissected deposit surface
exhibits erosional ridge-and-ravine topography. Subdued bar-and-swale constructional topography is
locally preserved on broad weakly dissected interfluves. Much of the deposit surface is dissected by
arroyos and exhibits erosional ridge and ravine topography. Moderately well developed soils with Stage
III+ carbonate morphology and many moderately thick clay films. Geomorphic surface Q6 of Connell
(1995, 1996).
Eastern-slope alluvial-fan deposits (middle Pleistocene) — Poorly sorted and stratified, gravel and sand
with minor, thin silty-clay interbeds. Gravel clasts are predominantly limestone with subordinate sandstone.
Deposit surfaces are approximately 100 ft (30 m) above local base level and exhibit modified bar and swale
topography. Soils posses Stage II+ to III+ carbonate morphology. Variable thickness and thickens to the east
to over 60 ft (18 m) thick. Correlative to alluvial fan deposits inset below the Tuerto gravel (unit Qfo) on the
adjacent Sandia Park quadrangle (Ferguson et al., 1996). Probably correlative to eastern-margin piedmont
alluvium (Qpm or Qpo) along western front of Sandia Mountains.
Strike and dip of magmatic foliation in granite defined by alignment of mafic enclaves
Lower Permian
Tertiary Igneous Units
Eastern-slope alluvium
Qfo
56
780
ces
ur
so
Tsla
Banded granitic gneiss — Isolated screens (and xenoliths) of banded biotite-rich granitic gneiss intruded by
the Sandia Granite in Madera Canyon as well as larger outcrops in Barrow Canyon beneath the PaleozoicProterozoic unconformity. May be correlative with pelitic gneiss or the Cibola granite exposed on the Sandia
Park Quadrangle (Ferguson et al., 1996).
Strike and dip of S2 foliation
75
N
QTpa
Calc-silicate and calc-pelite — Lensoidal calc-silicate bodies interlayered with quartz-rich pelites (Xqs).
Strike and dip of S1 foliation
TRAMWAY BLVD.
Qpm1
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) gravel, sand,
and silty to clayey sand. Inset against older eastern-margin piedmont alluvium (Qpo) and inset by younger
stream alluvium (Qay). Gravel clasts are predominantly subangular granite and schist with subrounded limestone,
and angular white quartz (aplite dikes) derived from the western front of the Sandia Mountains. Slightly to
moderately dissected deposit surface possesses 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 an older subunit. Correlative to geomorphic surfaces Q6-Q7 of Connell
(1995, 1996). Variable thickness, estimated from 0-140 ft (0-43 m).
45
A
Qpm
Younger eastern-margin piedmont alluvium (Holocene to uppermost Pleistocene) — Unconsolidated
deposits of brown, light gray-brown, and yellowish-brown (10YR) gravel, sand, and sandy clay loam. Gravel
clasts are predominantly cobbles to boulders of angular to subangular, granite with minor subrounded limestone.
Soils possess Stage I to II+ carbonate morphology and few thin clay films. Geomorphic surface Q9 of Connell
(1995, 1996) Variable thickness, from 0-40 ft (0-12 m).
Xgn
Strike and dip of joint or fracture
80
S
Qpy
Piedmont and stream alluvium, undivided (Historic to middle Pleistocene) — Cross section only. Undivided
deposits of stream-valley (QHa and Qay) and eastern-margin piedmont alluvium (Qpm).
.
Xcs
Quartz-rich pelitic schist — Quartz-muscovite schist and quartz-chlorite schist locally interlayered with
amphibolites, mafic metavolcanics, and calc-silicates; commonly contains aluminosilicates.
.
34
Lower Tertiary and Cretaceous sedimentary rocks, undivided (Paleogene-Cretaceous) — Cross section
only. Undivided lower Tertiary and Cretaceous deposits that may include the Unit of Isleta No. 2 (Lozinsky,
1994), Galisteo Formation, and Menefee Formation.
Eastern-margin piedmont alluvium
Qp
Pg
Horizontal bedding
60
Stream-valley Alluvium
QHa
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. Interbedded with the San Andres Formation with each sandstone bed
generally less than 30 ft (10 m) thick.
Xqs
20
a
QTsp
Strike and dip of bedding, ball indicates that younging is known
Paleoproterozoic metamorphic rocks
10
Are
Eastern basin-margin piedmont deposits, undivided (lower Pleistocene to Miocene) — Cross section
only. Poorly to moderately stratified to slightly east-tiled, reddish-brown to yellowish-brown and very pale-brown
(7.5-10YR) conglomerate, gravelly sandstone, and sandstone with subordinate siltstone and rare mudstone.
Buried by eastern-margin piedmont alluvium (Qpm). Conglomerate clasts are predominantly composed of
subangular granite with minor subrounded limestone schist, and angular white quartz (derived from aplite dikes
exposed in the Sandia Mountains). 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.
Thickens to the east and interfingers with fluvial deposits of the ancestral Rio Grande to the west (Connell,
1998). Thickness is variable and thickens to the west. Estimated thickness, ranges from 2,000-7,000 ft (6102,135 m) to the west.
40
30
TAOS
JUNCTION
20 mi
LYDEN
9
ARROYO
SECO
3
Taos
7
Slickensides on fault
30
TRES
OREJAS
Sandia Crest
10
0
Strike and dip of minor fault
ARROYO
HONDO
TAOS
Qpm
Breccia or gouge zones
85
CERRO
DE LOS
TAOSES
CARSON
0
Qpf
Monocline with anticlinal bend—Trace of axial plane; short arrow on steeper bend; dashed where approximately located, dotted
where concealed, queried where inferred
••
QTt
Qpm2
128
NMBMMR STATEMAP
Quadrangles
Qp
ue
Qtr
Ps
Upper Santa Fe Group
5
rq
Qsct
Colluvium and alluvium, undivided (Holocene to upper-middle Pleistocene) — Poorly consolidated,
poorly sorted and stratified, fine- to coarse-grained, clast- and matrix-supported gravel derived from a variety
of mass-movement hillslope processes, including debris flow, shallow slump and creep. May locally include
shallow landslide debris. Gravel clasts are typically subangular to subrounded limestone derived from the
eastern dip-slope of the Sandia Mountains. Commonly surrounds small unmapped bedrock inliers. Supports
distinct vegetative community and associated drainage density, both of which are represented by a distinct
tonal pattern on aerial photographs. Differentiated where areally extensive, thick, or obscures geologic contacts.
Variable thickness, up to 16 ft (5 m).
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).
3
ue
Qca
Disturbed land and artificial fill, undivided (Historic) — Dumped fill and areas affected by open-pit
aggregate mining or construction. Locally mapped where disturbance is areally extensive or geologic contacts
are obscured.
PALEOZOIC ERATHEM
Upper Permian
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), and xenoliths of
quartzite and mafic metavolcanic rock. Pegmatites, aplites, and quartz veins are ubiquitous. Various dates are
available: U-Pb zircon plus sphene 1,455 ±12 Ma (Tilton and Grunenfelder, 1968, recalculated by Steve
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 (Unruh, unpublished data); 40Ar/39Ar from hornblende is 1,422±3
Ma and from muscovite is 1,423±2 Ma (Kirby et al., 1995); apatite fission track dates range from 14±4 Ma
at low elevation to 30± 5 Ma at high elevation (Kelley et al., 1992).
NM B
ur
e
af
Moenkopi Formation — A recessive-weathering, dark red, micaceous shale, silty shale and thin-bedded
feldspathic sandstone. The unit is about 200 ft (60 m) thick.
Upland gravel (middle Pleistocene to upper Pliocene(?)) — Well rounded, poorly stratified gravel lag
deposits that mantle a low-relief upland erosion surface (pediment) approximately 330 ft (100 m) above local
base level. May be correlative to the Tuerto gravel of Stearns (1953), or to the gravel of Lomos Altos along
the northern flank of the Sandia Mountains (Connell et al., 1995). Correlative to unit QTug on the adjacent
Sandia Park quadrangle (Ferguson et al., 1996). Thickness is generally less than 3 ft (1 m).
.
QTug
Ys
I NDEX M AP OF NMBMMR’ S
STATEMAP
7.5-M INUTE G EOLOGIC Q UADRANGLES
9/ 99
A l buq
•••
•••
••
Thin surficial deposits derived from wind and mass-movement processes, or extensive areas disturbed by openpit aggregate mining or construction.
Qsct
not shown
• • • • •••
••
UNIT DESCRIPTIONS
ˇm
daf
QHa
1
Qay
late
••
••
Middle and Lower Triassic
U NITS
10
Fault—Showing dip with arrow showing trend and plunge of slickenlines where measurable; solid where exposed; dashed where
approximately located; dotted where concealed; ball-and-bar on downthrown side of normal fault, teeth on upthrown side of
reverse fault (combination of reverse fault teeth and bar-and-ball indicates interpretation of normal reactivation of a reverse fault);
upthrown (U) and downthrown (D) used where fault dip is unknown
50
4 Department of Earth and Planetary Sciences, Washington University, St. Louis, MO 63130
5 GRAM, Inc., Albuquerque, NM
Old eastern-slope alluvium, Tijeras Canyon unit (lower Pleistocene to upper Pliocene(?)) — Moderately
consolidated, poorly to moderately sorted and stratified gravel and sand. Poorly exposed. Gravel locally
overlies reddish-brown silty sand. Inset against upland gravel (QTug) and recognized at southwestern corner
of map area, within the San Antonio Arroyo drainage (major tributary to Tijeras Arroyo). Probably correlative
to old eastern margin piedmont alluvium (QTp). Approximately 3-10 ft (1-10 m) thick.
.
Holocene
Geologic contact—solid where exposed, dashed where approximately located, dotted where concealed, queried where inferred
2 Department of Earth and Planetary Sciences, University of New Mexico, Albuquerque, NM 87131
3 Arizona Geological Survey, 416 W. Congress, #100, Tucson, AZ 85701
R. J. Titus and D. J. McCraw: digital cartographic production
OF
Marine Oxygen
Isotope Stage
0 ka
middle
Mapping of this quadrangle was funded by a matching-funds grant from the 1997 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).
C ORRELATION
early
QUADRANGLE LOCATION
NATIONAL GEODETIC VERTICAL DATUM OF 1929
QTp
4,000
Ys
February 1999
CONTOUR INTERVAL 20 FEET
CENOZOIC ERATHEM
Neogene (Quaternary and Tertiary) System
Colluvial, landslide, eolian, and anthropogenic deposits
5,000
Tmi
T. 10 N.
20
Geology of Sandia Crest quadrangle,
Bernalillo and Sandoval Counties,
New Mexico
1 KILOMETER
88
000m
ˇm
22
20
6,000
Ys
Tmi
38
late
0
27
6,000
35
early
0.5
ˇz
ˇm
29
7,000
Pleistocene
••
1
22 34
Qfo
Pg
7,000
Pliocene
••
•••
•••
NEW MEXICO
10.6°
Pg
22
8,000
Pino
Canyon
Miocene
6000
Ps
QHa
8,000
Qfo
25
18
27
ˇc
Qca
Neogene (Tertiary & Quaternary)
5000
9,000
Ys
)
4000
Ys
Ys
89
LO
3000
˛s
Ys
IL
2000
˛s
ED
1000
1 MILE
30
Pay
73
The Shield
10,000
Ys
Ys
QHa
23
31
Pay
3
72
21
Qca
26
QHa
Qca
The
Needle
(S
0
0
QTpt
Ys
ˇz
Qca
•••
1000
27
22
16
21
9,000
13
˛s
˛m
˛s
27
40
18
Pay
18
Ma
26
32
Ys
11,000
˛m
Cretaceous
Ja
?
35
˛s
˛m
21
Py
˛m
˛s
˛s
20
˛m
˛s
Jurassic
•
•••
•••
••
Barrow fault
? ?
?
•
(TIJERAS)
0.5
Ps
La Cueva
fault zone
˛m
Sandia
Peak
Triassic
••
•••
••
•••
••
˛s
l
1
1999 MAGNETIC NORTH
DECLINATION AT CENTER OF SHEET
••
••
••
•••
••
QHa
••
SCALE 1:24,000
MN
••
•
••••
••••
?
••
••••
••
•
•
•••
••••
••
•
••
•••
••
•••
•
?
••
••
•
••
••
••••
fa u l t
•
••
••
•••
Cañoncito
••
••
••
•
fa
ul
••
l
••
•••
•
••
••
•
••
•
••
•••
•• •
••
•• • • • • •
••
••
••
••
•
••
t
•••
•••
••
•
••••
••
••
•
••
10,000
10
QHa
10
••
l l l l l
68
33
Sandia Crest
˛m
˛m
38
20
••
l l l l l
Qsct
••
••
••
••
C'
Base from U.S. Geological Survey 1961, photorevised 1967 and 1972
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
••
Tmi
Pay
ˇm
19
Pyc
12,000
Pa
11,000
QHa
•
27
Py
Py
Pa
•
QHa
Qay
•••••
Tmi
l l
3
16
Qfo
26
˛s
27' 30'
Pg
Pay
QHa
Tmi
R. 5 E.
19
13,000
Py
Ps
Pa
Ps
27
••
QHa
••
12,000
90
27
21
•••
38
22
Pyc
20
Qay
˛s
R. 4 E.
18
QTug
41
27
Py
QHa
13
33
34
26
~7,000 ft (2,100 m) of Mesozoic
strata removed post ~20 Ma
(AFT data -- Kelley, et al., 1992)
ˇm
Pg
ˇm
Pg
20
28
••
Ys
Tmi
66
45
50
21
42
43
Pyc
17
•
32
Qsct
l l
l l l
49
7
18
74
27
35
l
l l
l l
50
3
••
••
••
••
•••
••
••
••••
••
•••
••
•
••
•••
••
••
•••
••
•
••
ra
•••
••••
?
•••
•••
••
50
Qca
l
l l
l l
20
Pg
Pg
18
10
17
Contributing authors and map areas:
Read, A.: Las Huertas, Barro, Madera, Tejano, and Canoncito canyons and vicinity, as
well as along the Paleozoic-Proterozoic Unconformity north of Sandia Crest (1:12k);
Karlstrom, K. & Kirby, E.: The Sandia pluton and parts of Rincon ridge (1:12k/1:24k);
Connell, S.: Quaternary/Tertiary geology of the western edge of the Sandia Mountains.
(1:24k); Ferguson, C. & Osburn, G.: The SE corner of the map south of Cienega picnic
ground (1:12k); Ilg, B.: Parts of Rincon ridge and along the Paleozoic-Proterozoic
Unconformity north of Sandia Crest (1:12k); Van Hart, D.: Mesozoic Rocks south of the
Jaral fault (1:100k); Pazzaglia, F.: Quaternary deposits along the eastern edge of the
map (1:12k); this map also builds on the work of Kelley and Northrop (1975) and their
students.
?
?
•
••
•
••
Pay
•
•••
Ys
62
44
16
14,000
ˇs
ˇs
13,000
21
19
15,000
Pino Canyon
fault zone
ˇc
ˇc
Ps
24
60
45
16
31
31
72
Cross section
B–B'
ˇc
14,000
Ps
25
45
QHa
Cross section
A–A'
15,000
B'
Ps
QTug
15
42
10
16,000
feet ASL
20
••
18
S
16,000
feet ASL
18
19
28
Ps
QHa
•••
22
C'
N
13
24
31
20
51
40
••••
••
Qca
C
19
Pyc
Pay
10
20
16
430 000 FEET
Ps
28
20
17
20
36
QHa
Pg
••••
Qca
• • • Qsct
•••
–5,000
Pg
31
29
15
35
•••••
••
•••
••
••• ••
Qca
16
37
•
••
•
18
Tmi
QHa
Pyc
27
8
••
Pay
Qca 3891
QTug
Qca
••
54
77
˛s
Ys
–5,000
21
Qca
QTug
Pg
QHa
Pay
Pyc
14
69
41
–4,000
–4,000
92
20
24
Qca
•••
77
85
˛m
Ps Pg
Qca
˛m
9
24
40
•
70
••
–3,000
–3,000
Pg
32
•
Qca
• ••
••
˛s
Pay
Pyc
Pay
••
••••
••
•
•••••••••••
40
••
30
12
••••
83
–2,000
17
?
10
Qca
l
28
• • • • • • • • • • • • • • • • • • • • ••••••• • •
••
• •
Qca
Pg
QHa
Pay
31
˛ms
Tmi
Qpm
Qpm
23 12
ˇm
–1,000
–2,000
QTug
Pyc
12
•
Tmi
•• •
•••
70
31
•
••
••
• • Qsct
80
l l l l l
l l
••
Qca
•••
•••
•••
••
Tmi
l
l l l l
Qpo • • • • • • • • •
•
•
•
••
••
˛s
Ps
30
•
?
•
••
• • •••
••
••
••
Qca
ˇs
38
••
stratigraphic
separation is
poorly constrained
?
–1,000
10'
37
Qsct
l
Ys
•••
17
Qca
81
80
Qpo
Pay
87
23
Ys
••
l
64
fault
D o c Long
••
Ys
85
Ys
•
Qca
˛s
?
30
31
˛m
0 SL
ˇc
˛mc
˛m
˛ms
18
••
10
19
Jt
Je
0 SL
Ys
1,000
Jm
29
32
8
20
1,000
˛s
˛ms 20
˛mc
13
18
19
86
Ys
••
•
74
Pay
2,000
Kml
Kd
QHa
••
Khd
94
˛mc
22
Qca
Km u
14
17 74
spring
26
3,000
3,000
2,000
˛s
QHa
28
8
79
QHa
Cross sections are constructed based upon the interpretations of
the authors made from geologic mapping, and available 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.
Ys
26
18
38
5,000
4,000
Pay
40
9
Ys
FP 62
˛m
˛s
24
33
Pay
74
••
l l l l l
•
39
••
•
SL 61
6,000
Kmf
31
Ys
Qtr
61
l l l l l
•
l l l l l
3
QHa
52
13
64
•
Ys
9
l l l l l
Tmi
59
43
28
••
•
••
••
••
•
••
l l
l l l
?•
•
••
•
••
••
•
••
•
••
•
••
QHa
Ys
57
36
••
Qpm
••
•
QHa • • • •
•
• •?
•
••
20
Ys
••
•
Qca
•
• •••
• • ••
Qpo
Ys
˛s
34
Pay
60
Pay
˛m
4,000
˛ms
12
20
˛m
13
87
••
Qay
••
65
?
Qpy
Qpm
QTsp
5,000
˛mc
Tmi
15
••••
••
Ys
Ys
•
••
no •••
Pi ••••
?•
••
• • Qca
Qpm
7,000
Pg
?
˛s
˛s
QHa
12
35
daf
QHa
70
l
?
8,000
ˇm
95
32
83
20
30
˛ms
23
daf
31
80
74
l l l l l
20
••
Qsct
39
15
25
•••
˛m
˛m
?
14
Ys
70
?
••
20
12
QHa
Qpm
?
Tmi
l l l l l
••••
l l l l l
QHa
••••
•••
••••
• ˛s
13
•••
15
73
87
Qpm
2
11
18
38
˛s
~5 m
•••
••
••
•
••
••
•••
•••••
••
(ALAMEDA)
••
Ys
20
18
l l l l l
)
••
QHa
Pg
Pg
6,000
˛m
Ys
˛s
•••
ST
••
82
Ys
Ys
35
Qca
Ys
••••
EA
˛s
6
••
Qpo
•••
••••
Ys
• •• •
RQ
UE
•
˛m
68
• •• •
Ps
Pay
˛s
Pyc
7,000
Xgn
?
14
˛m
••
•
LB
UQ
UE
•
SL •
23 36
˛m
top of
Rincon
Ridge
8,000
Ys
••
16
••
••
Qpo
Qpm
Ys
•••
43
24
˛m
Ys
13
•FP
9,000
Ys
25
15
Ys
10,000
˛s
˛s
42
˛m
?
?
?
11,000
˛s
˛s
9,000
96
• •
••
••
••
••
77
Qpm
Ys
•••
•••
˛s
••
25
˛s
˛m
Qca
20
•••
••
•
QHa
Ys
•
•
•
• • •• •
• •• •• • •
•
••
••
˛m
˛s
unconformity
projected from
Sandia Crest
˛s
Barro
fault
Cañoncito
fault
˛m
˛m
˛s
18
˛ms
˛m
˛m
˛m
Pay
10,000
Qca
QHa
••
••
•
74
88
12,000
feet ASL
11,000
38
88
E
12,000
feet ASL
?
˛m
15
84
••••
•••••
(A
•
••
Ys
•
B'
Cross section
C–C'
?
85
••
1,000
Qca
13
Qpm
?
•
••
•
•
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68
•
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lt
2,000
W
Qca
• ?
•• •
?
••
•
•••
l
l l
l l
fau
Qpu
72
• QHa
Ys
•
•••
•
•
•
•
•••
Ma
3,000
Ys
B
?
39
••
• • ••• • ••••••
•
••
66
Ys
Qfo
•
QHa
15
50
Ys
••
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•••••
•••
••• ••••
••
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4,000
Ys
Ma
˛s
18
•
••
•••
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•
•
••
9
e
58
Ys
QHa
12' 30" A'
17
Ma
17
Ma
Qca
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Pg
1,000
97
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n
zo
Ys
••••
••
?
••
•
••
•••
17
5,000
Ys
Ys
38
Ys
53
Xgn
•
l
l l
l l l
l l l
88
Qpm
l l l l l
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•
84
U
••
?
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l l l l l
l l l l l
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•
l
l l l l
D
17
78
85
Ys
66
?
22
30
••
6,000
˛s
Qacuc
˛s
83
˛s
˛m
˛s
7,000
2,000
T. 11 N.
Qca
Ma
47
T. 12 N.
Ma
QHa
QHa
Ys
23
•
˛s
11
Ma
Ys
8,000
˛m
98
QHa
Ys
˛s
Tmi
Ys
61
•
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w
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••••••
• • • • • • •S• a• n d ia fa u lt
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60
•••
••••
35° 07' 30"
106° 30'
Qsct
••
Ys
Xgn
Ma
Ys
38
Qca
Ys
65
Ys
20
70
••••
••••••••••
••
•••
Qpm
Ys
Ys
˛m
Ma
Tmi
3,000
Qfo
36
Ys
QHa
•••
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•••
88
•
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•
••
•••
•••
38
••
˛s
Ma
˛s
Ys
Ys
28
Ma
Ys
Qca
Tmi
•
Ma
Ma
Pa
TKu
12
cc veins
72
Ys
Qpm1
•
••
?
? Ma
˛s
16
67
Qpm1
•
••
Ys
Ys
Ma
19
31
8
Qpm
TD 42'
bottoms in Ys
•••
•••
D
l l l l l
l
l l l
••••••
••
T. 11 N.
T. 10 N.
•
•••
••• d
• • •s t r a n
•••
• • • do
• • • bu
• • • Em
• • • East
•••
••• e • • • zon
• • • lt
• • • fau
•
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89
•
••
63
••••
••••••
•••
38
••
•
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QHa
Ys
Tmi
Ys
˛s
Ys
QHa
˛s
?
Qsct
?
HD 2
˛s
Ys
˛m
75
74
13
?
˛s
••••
••••••
•••
Qpm
••
l l
ll l
l l
l l ll 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
Qpy
Qpm
QHa
•
••
•
••
?
QHa
˛s
Ys
8
Qca
˛s
Ys
4,000
?
••
Ma
20
QTpa
Ys
•••••••
•••
U
˛s
Ys
••••••••
•••
Qpm
•
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QTpa
•••••••
•••
QHa
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7
QHa
?
?
Ma
22
Ma ˛s
Qsct
••
15
˛s
33
Ys
Ys
•
•
••••
••
••••
••••
••
••••••
1 510 000
FEET
D
Tmi
Qpx2
Ys
Ys
•••••
Qpm
25
Ma
23
••
˛m
˛s
Ma
ˇm
Py
˛s
Qca
20
•
••
˛s
Ys
˛s
ˇs
15
21
15
••
30
8
˛ms
16
˛s
21
16
˛s
9,000
˛m
top of
Rincon
Ridge
Ys
Ys
˛s
?
Ys
QTsp
Ps
˛ms
23
20
24
Qsct
•
••
• • ••
•
••
•••••
HD 1
TD 500'
bottoms in
basin fill
Ys
84
˛s
19
Ys
15
••
••
45
aplite
20
˛s
••
•••••
91
˛s
Tmi
QHa
QHa
38
23
••
•••••••
QHa
20
26
• ••
Tmi
11
14
FP 82
Ys
Ma
• • ••
l
l l l l
l
l l
••••••
SHO 3
TD 495'
bottoms in
basin fill
14
l l l l l
l l l l
l
l l l l
l
l
l l l l
l l l l
l
l l l l l
•••••
10'
12
Qca
˛m
˛s
Jt
˛ms
14
17
˛m
˛m
QHa
QHa
QHa
Qsct
••
12
13
22
Ys
l
••••
Qpm1
92
l l
l l l
••••
38
38
Tmi
QHa
TD 520'
bottoms in
basin fill
93
••
••••
B
Qpx2
Ys
•
•••
•••
•••
•••
•• •
•••
••
•••
••
•••
••
•••
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•••
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•
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•
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••
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••
••
••
••
••
•• ••••
•
••
••••
RG 31974
Qpx1
Ys
•••• •
•
•••
•••
•• ••••••
••
• •• • • • •
• •••• •
•••
Qay
Tmi
••••••
•••
••
94
l
l l l l
•••••
•••
•• •
• • • • ••••
• • •• •• ••••
•
••
••
••
D U
38
Tmi
•
6,000
˛m
16
˛ms
85
Ma
˛s
15
daf
Ys
Js
99
12
˛m
27
Ys
10,000
˛m
Tmi
17
••
•
••
TD 500'
bottoms in
basin fill
85
Qpo
D U
18
14
•••
•••
•••
••
SHOCH
18
•••
l l l l l
QTpa
Qpm
ne
•
•••
•••••••
••
Qay
78
˛m QHa
••
• • • • • • •• • • • • • • • • • • •
•••
••••••••
••
95
85
l l l l l
•••
•••
Qpo
Ys
zo
••
••
•••• • • •
•••
•••••••
••
38
Qay
QHa
QHa
88
12
lt
•••••••••••
••
••••••
••
Qay
fau
•
l
l l l l
••
Ys
Qpo
•••
89
Qpo
D U
Qca
75
QTp
•••
6
13
˛s
?
˛s
Kd
7
˛m
FP 89
?
27
˛m
˛m
Ys
Ys
Ys
Jm
15
Ma
˛m
68
˛s
˛m
Khd
20
11
˛s
˛s
˛s
11,000
˛s
˛s
˛m
Tramway
Blvd. strand
7,000
˛m
87
85
89
84
Qpo
•• • •
96
eva
•••
••
••
•
38
65
85
Ys
Qpx2
Ys
••••••••••
• ••••••
•••
•
••
Qay
•
A
84
75
Cu
15
88
60
Qpm
••
•
28
88
64
Ys
Js
ˇc Je Jt
La
•
Qpo
Qpo
10
79
60
54
•
••
Ys
Qca
˛s
Pa
˛s
5,000
15
Ys
QHa
˛s
Sandia
fault zone
Kml
15
68 35
11
15
˛s
82
˛s
10
13
˛m
20
Xqs
Qpm
Ma
8
82
••
46
23
Ma
QTpa
88
32
60
•••••
••
••
79
˛s
14
?
••• • • • Qpo
•• ••
•• ••
••
•
Ys
42
86
˛m
˛m
MEXICO INSTITUTE OF MINING & TECHNOLOGY
Permian
ni
K
••
•
42
50
•••
63
Qpo
Ys
••••••
65
•
42
5
85
˛m
86
QTpa
Qpx1
Ys
Pa
ˇc
˛s
˛m
˛m
8,000
38
16
FP 82 ˛s
5
conjugates SL 81
20
FP 40
6
SL 40
12
25
••
40
32
Jm
••
••
••••
•
83
22
48
Ys
15
85
Qpy
Xqs
46
78
•
12,000
Qca
Qm
19
20
Qca
Ys
Qpf
bend in section
Sandia
Crest
˛m
Km u
1 540 000
FEET
48
Ys
˛s
˛s
••
˛s
10
Qca
23
••••
••
Xqs QHa
Ys
•
•
Qpx1
Ys
58
52
Qca
QHa
60
40
T. 12 N.
?
QHa
Ys
72
80
••
28
80
Qpx3
Ys
˛s
••
••
Ys
77
59
••
•
••••
•
61
••
•
•••
81
˛s
˛s
17
Qpx1
Ys
••••
•••••
•
32
42
20
5 to 10 m
72
Qpx2
Ys
71
72
˛m
˛s
•
17
00
13,000
feet ASL
poorly constrained
9,000
15
67
58
Qpx1
Ys
•
Qpx1
Ys
Qpx3
Ys
Qpx3
Ys
90
Ys
39
˛s
12
13
˛s
73
•
Qpx1
Ys
89
45
QHa
•
36
49
97
38
15
20
38
Qay
˛s ?
••
Qpx3
Ys
Xqs
Ys
Qay
10
QHa
Ys
Qca
23
72
•• •
QHa
77
28
Qca
20
Qpx1
Ys
65
•
74
12
25
88
12' 30'
•
12
16
˛s
80
Xqs
10,000
•
26
?
32
38
Ma
˛s
34
ˇc
?
Ys
32
T. 11 N.
?
56
51
60
77
20
Ys
••
00
83
•
39
20
16
76
40
38
14
˛s
˛m
˛s
80
11,000
t
˛s
˛m
72
˛s
12,000
Qca
ul
Qca
17
33
˛m
•• ••
67
•••
84
Qca
•••
•
83
61
Ys
˛s
˛s
QHa Ys
01
15
fa
••
••
fe
40
e
••
g
Ed
Ma
16
73
39
10
14
E
Cross section
C–C'
Ps
COMMENTS TO MAP USERS
Pg
Pay
Penn.
lt
48
8
Ma
80
13,000
feet ASL
89
˛s
W
˛m
io
80
84
Xqs
Qca
••••••••••• • ••
•••
85
?
73
?
• ••• • •
78
70
fau
80
Ys
54
?
on
Xcs
Ma
lt
01000m N.
15
5
A'
A
A nt
82
39
Tsla?
QHa
56
o fau
˛m
Tsla?
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. Several different scales of mapping
were incorporated into this map; therefore, the user should be aware of significant variations in map detail.
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.
Pyc
˛m
˛s
Miss.
75
58
?
?
˛m
106° 22' 30"
35° 15'
460 000 FEET
73
Ma
Meso.
15
Ys
8
3
Ys
Paleo.
••
76
46
18
˛s
travertine
(Qtr)
57
PLACITAS 5.2 MI.
QHa
•• • • • •••••••••
Qca
Suela
fault
n ?
Sa
25
Xqs
28
CENOZOIC
˛s
slicks &
pseudo tachylite
25'
71
P o m e cer r
57
3
70
17
˛s
78
3
••••
Ma
80
82
69
••••
Ma
(PLACITAS)
3
68
MESOZOIC
3
PALEOZOIC
Ys
R. 5 E.
PROTEROZOIC
66
P
27° 30'
3
NE
R. 4 E.
66
(SANDIA PARK)
3
SANDIA PARK 0.9 MI.
1.8 TO N. MEX. 10
65
•
3
••
64000m. E.
•
3
?
)
106° 30'
35° 15'
A LAMEDA 7.5' QUADRANGLE
S ANDIA CREST 7.5' QUADRANGLE
LL
NEW MEXICO
C'
RG31974
LI
NA
ER
(B
SANDIA CREST QUADRANGLE
Xgn
Yp
Xqs
Xcs
Mapping of this quadrangle was funded by a matching-funds grant from the STATEMAP program of the U.S.
Geological Survey, National Cooperative Geologic Mapping Program, to the New Mexico Bureau of Mines
and Mineral Resources (Dr. Charles E. Chapin, Director; Dr. Paul W. Bauer, P.I. and Geologic Mapping
Program Manager). 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, or the U.S. Government.