374000
Description of Map Units
106°22'30"W
375000
Quaternary
B
Tbr
Tpa
Tbr
Tpa
Tpb
Qec
Tbh
Tpv
Tpa
Tpbhd
70
Qc
Tm
Tbp
Tbi
Tbi
3956000
14
Qbo
Qc
Qbo
Tbr?
6.52
Tbr
Tphd
Tbp
Tcc
Tcct?
Qc
Tbr
60
7.06
75
Tbi
55
65
Qbt
Qc
Qbt
Tbp
6.63
Tbi
7.1
6.93
Qbt
Qbt
Tbp
Tbr
Tbi
Tbi
3953000
Tbi
Tbp
37
Qc
Qc
Tbp
Qbt
27
Tbp
Tpa
Qal
A
35°42'30"N
Qbo
87
Qbo
Qc
Tbr
Tbp
Tbr
Qal
Tbi
Tpbd
Qbo
Tbp
5
Qal
Tbi
Tpa
Tbp
Tbp
Tbp
Tpbd
27
Tbi
Qec
25
83
Tbp
8
80
15
Qc
Tbi
16
40
27
25
Qbt
Qal
Tbi
Qc
82
80
Qbt
Qal
Tbr
3950000
Qal
12
Tglp?
Qc
Qbo
Qbt
Qc
Tglp
Qbo
Qal
Qec
Tbr
Qc
3949000
QTc
Qc
Tglp
Qec
12
Qt2
Tbp
Tglp
Tglp
Tbp
Qc
QTc
3948000
35°40'0"N
Tbr
Tbr
Qc
Tglp
Qc
Tbr
Tglp
Qc
Qc
Tbr
Qc
QTc
Qbt
Tglp
Tglp?
35
70
Qec
Qal
Qbo
Qec
Qoa
Qt2
Qec
3948 000
Qec
Tbp
56
55
15
QTc
Qt3
Tglp
Qal
50
Qal
QTc
Qe
Qal
3947 000
Qt1
Qec
Qec
QTc
50
Qe
Qt1
QTc
Qbo
QTc
Qec
Qal
13
Qal
Tglp
Tglp
Qe
3946000
Qc
QTc
Qe
QTc
QTc
Qc
Qec
QTc
Qec
3946 000
QTc
Qe
Qal
Tglp
Qec
QTc
Tglp
Tglp
Qal
QTc
Tglp
QTc
QTc
QTc
Qc
QTc
Qc
Qc
Qal
QTc
Tglp
Qe
QTc
3943000
364000
365000
106°30'0"W
Qe
366000
367000
106°27'30"W
Digital cartography by S. D. Lynch, M. M. Mansell, and D. J. McCraw
BLAND
0
Cañada
371000
0
1000
2000
3000
106°25'0"W
Qal
Tbp
372000
5000
6000
COCHITI
DAM
NEW MEXICO
Magnetic Declination
May, 2006
9º 48' East
At Map Center
0.5
0
Holocene
Qal
QTslg
QTslg
373000
QTc
Qt4
374000
7000 FEET
35°37'30"N
375000
106°22'30"W
New Mexico Bureau of Geology and Mineral Resources
New Mexico Tech
801 Leroy Place
Socorro, New Mexico
87801-4796
1 KILOMETER
CONTOUR INTERVAL 20 FEET
NATIONAL GEODETIC VERTICAL DATUM OF 1929
SANTO
DOMINGO
PUEBLO SW
SANTO
DOMINGO
PUEBLO
Comments to Map Users
Tsf
May 2005
7.12
Qe
Qt4
Peralta
Canyon
Tbp
Tpbd
Tphd
Units by Area
East
QTc
Bland
Canyon
Tbi
Tbp
Tbp
Tbp
Tpb
Tpv
Tpbd
Tppa
Tpa
Tpa
Tphd
Tpoa
he
nc
n
Ca
on
ny
on
P
&
T
Valle
Grande
Qs
Qs
Qb
&
P
Qs
o
Ts
Qs
35°45'
Tb
@
Ti
T
Ts
Gr
Cañada
p_
P @
&
@
Q
³
Tb
@
QT
T
aQT
QT
QT
Q
Cochiti
Reservoir
Miles
5
0
Q - Quaternary sediments
T - Tertiary sedimentary rocks
Ti - Tertiary intrusive rocks
& - Pennsylvanian sedimentary rocks
Qb - Quaternary basaltic volcanic rocks
Tb - Tertiary basaltic volcanic rocks
@ - Triassic sedimentary rocks
p_ - Precambrian rocks undifferentiated
QT - Quaternary -Tertiary sediments
Ts - Tertiary silicic volcanic rocks
P - Permian sedimentary rocks
volcanic vents
Generalized geologic map of the Jemez Mountains depicting the location of the
Cañada quadrangle on the southern flank of the Jemez caldera.
References
Dethier, D.P., Harrington, C.D., and Aldrich, M.J., 1988, Late Cenozoic rates of erosion in the western Española basin, New Mexico: Evidence from geologic
dating of erosion surfaces: Geological Society of America Bulletin, v. 100, p. 928-937.
Dethier, D.P., 1996, Geologic map of the Cochiti Dam quadrangle: unpublished mapping for the U.S. Geological Survey, 1:24,000.
Dethier, D.P., and McCoy, W.D., 1993, Aminostratigraphic relations and age of Quaternary deposits, northern Española basin, northern New Mexico:
Quaternary Research, v. 39, p. 222-230.
Stein, H.J., 1983, Geology of the Cochiti mining district, Jemez Mountains, New Mexico [M.S. thesis]: University of New Mexico, Albuquerque, 122 p.
WoldeGabriel, G., and Goff, F., 1989, Temporal relations of volcanism and hydrothermal systems in two areas of the Jemez volcanic field, New Mexico:
Geology, v. 17, p. 986-989.
fa
r
Pe
Tbr
Tbp
Tpa
t
ul
fa
io
Qbt
Qbt
Tbr
ed
Tbp
Tpa
Tpa
D
8000
fa
M
Qbt
Qbo
Qbo
ia
Qbt
Tbp
Qbo
Tppa
Tpa
Pa
r
ja
ito
t
ul
fa
7000
Qbt
Qbo
Tppa
Qbo
6000
No vertical exaggeration
ks
B
B'
an
C
ta
ral
Pe
8800
8800
8000
8000
n
yo
>
1 - Gary Smith and Andrika Kuhle, 1997-2006
2 - Scott Lynch, 2003
3 - Scott Lynch, 2003; Stein (1983)
4 - Goff et al. (1990)
5 - Goff et al. (1990); Lavine (1995)
6 - Gary Smith, 1997
Tbr
Tbp
Tbi
a
añ
C
da
t
ul
oc
3944
Q
Q
tR
3946
7000
ta
al
Tbr
t
ul
6000
1
p_
Smith, R.L., Bailey, R.A., and Ross, C.S., 1970, Geologic map of the Jemez Mountains, New Mexico: U.S. Geological Survey, Miscellaneous Investigations
Map I-571, scale 1:125,000.
yo
an
zC
iti
ch
A' Line of cross section
ny
n
Te
A
Fault, dashed where approximate, solid
where certain, dotted where concealed
Ball on downthrown side, dip shown
where measured
3948
Valles Caldera
A'
8000
esa
87
Contact, dashed where approximate,
solid where certain, dotted where
concealed, dip shown where measured
P
A
M
60
QT
Smith, G.A., McIntosh, W.C., and Kuhle, A.J., in press, Sedimentologic and geomorphic evidence for teeter-totter subsidence of the Santo Domingo
accommodation-zone basin, Rio Grande rift, New Mexico: Geological Society of America Bulletin.
Hoodoos eroded in the Peralta Tuff member of the Bearhead Rhyolite (foreground) and gravel of the
Cochiti formation (skyline) provide the geologic framework of the Kasha Katuwe Tent Rocks
National Monument. Photo by Gary Smith.
est
W
New Mexico Institute of Mining and Technology, Socorro, NM, 87801
Department of Earth and Environmental Sciences, University of New Mexico, Albuquerque, NM, 87131
Ca
T
Qs
Qs
Smith, G.A. and Kuhle, A.J., 1998, Geology of the Santo Domingo Pueblo and Santo Domingo SW 7.5' quadrangles, Sandoval County, New Mexico, New
Mexico Bureau of Mines and Mineral Resources, Open-file Geologic Map OF-GM 15 and 26, scale 1:24,000.
Tcct
Tpv
Tphd
6
Co
on
Strike of vertical flow foliation
5
ny
1
ta
Ts
Qs
Geologic Cross Sections
Ca
ral
Q
375
nd
Pe
P
@
Smith, G.A., and Kuhle, A.J., 1998, Hydrostratigraphic implications of new geological mapping in the Santo Domingo Basin: New Mexico Geology, v. 20, p.
21-27.
Tpbd
Tcc
x
Cerro
Balitas
2
3950
&
36°00'
Smith, G.A., and Lavine, A., 1996, What is the Cochiti Formation?: in: Goff, et al., eds., New Mexico Geological Society, Guidebook 47, p. 219-224.
Tbr
3952
Strike and dip of flow foliation
Tb
Ts
Smith, G.A., 2001, Development of a pyroclastic apron adjacent to rhyolite domes in a subsiding basin: Upper Miocene Peralta Tuff, Jemez Mountains, New
Mexico, in Volcanoes of New Mexico, L. Crumpler and S.G. Lucas, editors: New Mexico Museum of Natural History and Science Bulletin 18, p. 85-96.
Sanchez
Canyon
Tbr
Sa
Bearhead
x Peak
T
T
p_
Smith, G.A., 1999, Tectonics and volcanism of the late Miocene Bearhead magmatic episode in the southeastern Jemez Mountains, New Mexico: New
Mexico Geology, v. 21, p. 37-38.
4
Bla
3954
106°15'
Tb
McIntosh, W.C., and Quade, J., 1995, 40Ar/39Ar geochronology of tephra layers in the Santa Fe Group, Española basin, New Mexico: New Mexico
Geological Society, Guidebook 46, p. 279-287.
Tsf
373
106°30'
P
Goff, F., Gardner, J.N., and Valentine, G., 1990, Geology of St. Peter’s Dome area, Jemez Mountains, New Mexico: New Mexico Bureau of Geology and
Mineral Resources Geologic Map GM-69, 2 sheets, scale 1:24,000.
3
Strike and dip of bedding
Strike of vertical joints
78
371
on
by
Scott D. Lynch 1, Gary A. Smith 2, and Andrika J. Kuhle 2
27
3956000m N.
369
ny
Horizontal bedding
367
365000m E.
106°45'
Lavine, A., Smith, G.A., and Goff, F., 1996, Volcaniclastic rocks of the Keres Group: insights into mid-Miocene volcanism and sedimentation in the
southeastern Jemez Mountains: New Mexico Geological Society 47th Field Conference Guidebook, p. 211-218.
Tm
Tpa
The rocks in the Cochiti mining district are hydrothermally altered and intensely fractured. Faults and fractures in the district are commonly filled with N-S
and NE-SW trending, gold and silver bearing epithermal quartz veins up to 1 meter wide. The rocks are variably chloritized, silicified, and argillized.
WoldeGabriel and Goff (1989) dated hydrothermal illite and determined this alteration occurred between 5.9-6.5 Ma and may thus be associated with
Bearhead Rhyolite magmatism.
Chamberlin, R.M., Pazzaglia, F.J., Wegmann, K.W., and Smith, G.A., 1999, Preliminary geologic map of the Loma Creston 7.5-min. quadrangle, Sandoval
County, New Mexico, New Mexico Bureau of Mines and Mineral Resources, Open-file Geologic Map OF-GM 25, scale 1:24,000.
Qec
Qoa
Tbr
North of Bearhead Peak there is mostly hypabyssal rocks of the Cochiti mining district. The area is in the footwall of a NE-trending fault zone, including the
major Bland fault (Stein, 1983). Uplift and erosion of these blocks has exposed the feeder system of the Keres Group volcanic rocks, a depth of exposure seen
nowhere else in the Jemez volcanic field. The rocks are primarily dikes and stocks of the Paliza Canyon formation that are intruded by Bearhead Rhyolite
dikes and stocks. The dikes commonly are near vertical and strike north to northeast, coincident with fault orientations in the area.
Lavine, A., 1995, Sedimentologic and temporal relations between volcanic and volcaniclastic rocks of the Keres Group, Jemez Mountains: Implications for the
physical and volcanic evolution of Keres Group composite volcanoes [M.S. thesis]: Albuquerque, University of New Mexico.
Colle
Canyon
Tbi
The Bearhead basin accommodates the 500 m thick, west-tilted section of Peralta Tuff between Peralta and Medio Dia Canyons (Smith, 1999). The fault zone
of Peralta Canyon forms the western stepped margin of the basin, with the Peralta fault forming its far western edge. The Peralta Tuff thins against the western
margin, and is abruptly truncated by the Peralta fault. The down to the west Medio Dia fault zone forms the eastern margin of the Bearhead basin. The
southeastern margin of the basin is partly uplifted in the footwall of the Pajarito fault. This uplift, along with possibly greater displacement along the Peralta
fault zone than the Medio Dia fault zone, accounts for the westward tilt of the Bearhead basin. The basin is about 8 km wide near its southern end. It tapers to
the north between northeast trending faults and the northwest trending Medio Dia fault. It is about 2.5 km wide near the northern quadrangle boundary, where
northeast trending, down to the southeast faults form its northern margin. The thick section of Peralta Tuff Member and overlying Cochiti Formation is absent
east and west of the Bearhead basin, indicating deposition during basin subsidence (Smith, 1999).
Justet, L., 1999, The geochronology and geochemistry of the Bearhead Rhyolite, Jemez volcanic field, New Mexico [M.S. thesis]: University of Nevada, Las
Vegas, 152 p.
Qbo
QTslg
Many of the Keres Group magmas intruded and erupted along faults in the southern Jemez volcanic field (Gardner et al. 1986). In the Canada quadrangle,
several Bearhead Rhyolite stocks and domes are found at the intersection between N-S trending and NE-SW trending faults. In the northwest corner of the
quadrangle, Bearhead Rhyolite vents are aligned along N-S trending faults, which are intruded by rhyolite dikes. The intermediate and rhyolitic dikes in the
Cochiti mining district very commonly trend N-S and NE-SW.
Sandstone (Miocene) - White, silicified and metamorphosed fine-grained, well-sorted, sandstone.
Consists of ~90% quartz with minor feldspar and lithic fragments. Mostly massive but locally
includes faint horizontal and cross bedding. Based on grain size, composition, and lack of associated
mudstone, the sandstone is tentatively correlated to middle Miocene eolian sandstones, such as the Zia
sandstone, in the Albuquerque basin, and the Ojo Caliente sandstone Member of the Tesuque
formation, in the Espanola basin. Stein (1983) and Smith (2001) interpret as roof pendants within
stocks of unit Tm. Maximum thickness is 100 m.
Qbt
Tglp
The Pajarito fault zone is a major north to northeast trending structure in the Jemez Mountains. In the Canada quadrangle it has a record of movement in the
middle Pleistocene. Between Bland and Cochiti Canyons it displaces the Bandelier Tuff by 80 meters. In Bland Canyon it also cuts middle Pleistocene terrace
gravel (Qt3), which is in fault contact with Peralta Tuff. Goff et al. (1990) estimate a maximum displacement of 300 m in the Keres Group rocks along the
Pajarito fault between Bland and Cochiti Canyons.
Bailey, R.L., Smith, R.L., and Ross, C.S., 1969, Stratigraphic nomenclature of volcanic rocks in the Jemez Mountains: U.S. Geological Survey Bulletin 1274P, 19 p.
Qt1
West
The Jemez volcanic field is at the intersection of the north-trending Rio Grande Rift and the northeast-trending Jemez lineament. High-angle normal faults
trending north, north-northwest and northeast are numerous in the Canada quadrangle. Most of these faults dip between 65°-80° to the east or southeast. A
notable exception is the major Medio Dia fault, which is down to the west. They are well exposed in the Keres Group volcanics, commonly with fault gouge,
breccias, slicks, alteration zones, and in some places quartz veins. The displacement in Keres Group rocks is greater than 170 meters where the Peralta fault
enters Peralta Canyon and juxtaposes Peralta Tuff against Paliza Canyon andesite ( Tpa). The Bland fault juxtaposes hypabyssal Keres Group rocks in the
footwall against Peralta Tuff in the hanging wall. Several faults also offset upper Pliocene pediment gravels (Tglp) in the southern part of the quadrangle by as
much as 70 m, and a few displace the 1.22 Ma Bandelier tuff (Qbt) in the northern part by typically less than 30 m.
Santa Fe Group
Qt2
Units by Area
The Cochiti Formation (QTc) gradationally overlies the Peralta Tuff Member in the southern part of Canada quadrangle and is interbedded with the Sierra
Ladrones Formation (QTslg) near the southeastern corner. Bandelier Tuff ( Qbo) is present within the uppermost Cochiti Formation east of Tent Rocks.
Gardner, J.N., and Goff, F., 1984, Potassium-argon dates from the Jemez volcanic field: implications for tectonic activity in the north-central Rio Grande rift,
New Mexico Geological Society, Guidebook 35, p. 75-81.
Index to Geologic Mapping
Age (Ma)
Volcanic vent
New Mexico Bureau of Geology and Mineral Resources
Open-file Geologic Map 85
Qc
Bearhead Rhyolite is stratigraphically above Paliza Canyon Formation in the Canada quadrangle. The Peralta tuff member (Tbp) is typically overlain and
intruded by Bearhead Rhyolite domes, flows, and intrusions (Tbr/Tbi), but in Peralta Canyon they are intercalated or the Peralta Tuff buries the lava. Bandelier
Tuff (Qbo/Qbt) overlies Bearhead Rhyolite and Keres Group.
Gardner, J.N., Goff, F., Garcia, S., and Hagan, R.C., 1986, Stratigraphic relations and lithologic variations in the Jemez volcanic field: Journal of Geophysical
Research, v.91, p. 1763-1778.
http://geoinfo.nmt.edu
Explanation of Map Symbols
2
Tcct
Tcc
Ca
The map has not been reviewed according to New Mexico Bureau of Geology and Mineral Resources
standards. The contents of the report and map should not be considered final and complete until
reviewed and published by the New Mexico Bureau of Geology 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.
Qls
In the western part of the quadrangle, Paliza Canyon Formation andesite flows (Tpa) and intrusive rocks (Tm) are the oldest volcanic units exposed. Paliza
Canyon Formation biotite dacite flows (Tpbd) overlie andesite flows (Tpa) along the western quadrangle margin. A Paliza Canyon Formation hornblende
dacite flow (Tphd) is present beneath Peralta Tuff ( Tbp) and apparently above andesite flows (Tpa). It is a single exposure in the northwest corner of the
quadrangle and its stratigraphic relationship with the biotite dacite (Tpbd) is unknown.
Canovas Canyon rhyolite (Miocene) - tuff. White to pink ash-fall and ash-flow tuffs. Consists of at
least four mappable units. Lowermost unit consists of pink lithic-rich ash-fall tuff containing
abundant lithic fragments of pink flow-banded rhyolite. Other units consist of thin beds of white,
fine-grained ash and pumice. Maximum observed thickness about 20 m.
Tcct
lle
Cross sections are constructed based upon the interpretations of the author 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.
Geologic map of the Cañada
quadrangle, Sandoval County, New Mexico
STATEMAP quadrangles are available
for free downloads at:
Co
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 may be based on any of the following: 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.
Tcc
Qt3
Tbr
[505] 835-5490
LOMA
CRESTON
Qal
QTc
Mapping of this quadrangle was funded by a matching-funds grant from the STATEMAP program
of the National Cooperative Geologic Mapping Act, administered by the U. S. Geological Survey,
and by the New Mexico Bureau of Geology and Mineral Resources, (Dr. Peter A. Scholle,
Director and State Geologist, Dr. J. Michael Timmons, Geologic Mapping Program Manager ).
1 MILE
4000
Qt4
Tbp
FRIJOLES
1
BEAR
SPRINGS
PEAK
Tbp
A 12.4 Ma Canovas Canyon Rhyolite flow (Tcc) and an underlying tuff (Tcct) are exposed in Sanchez Canyon and are the oldest volcanic units in the Canada
quadrangle. The flow is overlain by intercalated Paliza Canyon Formation andesite and dacite flows, domes, and volcaniclastic deposits. The lower part of
this sequence is intercalated with Canovas Canyon rhyolite domes, flows, and tuffs as young as 9.2 Ma (Gardner and Goff, 1984). There is no compositional
progression in this sequence of rocks (Goff et al., 1990). The sequence is overlain by Peralta Tuff, which is overlain by a Bearhead Rhyolite dome.
Canovas Canyon rhyolite (Miocene) - Domes, flows, and intrusions. White to gray to pink, flowbanded devitrified rhyolite and rhyodacite. Contains phenocrysts of quartz, plagioclase, biotite,
±sanidine, ±hornblende. May contain flow breccia, perlite, and rare obsidian at margins of intrusions.
Tcc underlies or intrudes intermediate-composition rocks of lower Keres Group. K-Ar ages of four
domes and flows range from 9.24 ±1.50 Ma to 12.4 ±2.0 Ma (Goff et al., 1990). Maximum observed
thickness about 110 m.
Correlation of Map Units
QTslg
QTc
370000
0.5
1000
REDONDO
PEAK
14
Qt4
1:24,000
1
QTc
Qt4
QTslg
369000
3944 000
Qt4
The northern 2/3 of the Canada quadrangle is Keres Group rocks and Bandelier Tuff, and the southern 1/3 is primarily volcaniclastic basin-fill sediments and
pediment gravels of the Santa Fe Group. The Keres Group rocks form prominent highlands along the northwestern and northeastern sides of the quadrangle,
with Bandelier Tuff capping the mesas in between. Keres Group rocks are also present in the deeply incised canyons between the mesas of Bandelier Tuff.
Paliza Canyon formation (Miocene) - Olivine basalt. Contains sparse phenocrysts of plagioclase,
augite, and olivine. Exposed in Colle Canyon at northern quadrangle margin. Intruded by Tm.
Tpb
QTc
Tglp
368000
Base map from U.S. Geological Survey 2002, from photographs taken 1996, edited in 2002.
1927 North American datum, UTM projection -- zone 13N
1000-meter Universal Transverse Mercator grid, zone 13, shown in blue
QTc
Qbo
QTc
Qe
B'
6.81
Tbp
Tglp
QTc
QTc
12
QTslg
Qal
Qc
QTc
Qbo
Qbo
Tbp
Qt1
Qt4
Qbo
Tglp
QTc
Tglp
Qt4
Tglp
Tbp
Tglp
QTc
Qbo
Tbp
QTc
QTc
35°37'30"N
Tglp
Qbo
Tbp
Qal
3944000
Qc
Qc
Qal
Qbo
Tbp
Qc
Qec
Qe
15
Qc
QTc
QTc
Qt1
Pliocene
Tglp
Qal
Qe
Tglp
3945 000
Tglp
Tglp
Qe
Tglp
QTc
Qbo
Qe
Tglp
QTc
QTc
Qt1
Qbo
Qc
Qc
QTc
Qc
QTc
QTc
Qt1
Qbo
26
QTc
TERTIARY
Miocene
3945000
Qc
In the southern Jemez volcanic field, the Bandelier tuff erupted over a rugged terrain of volcanic rocks known as the Keres Group (Bailey et al., 1969). The
group was refined by Gardner et al. (1986) and consists of Canovas Canyon rhyolite, Paliza Canyon formation, and Bearhead rhyolite. Paliza Canyon
Formation dominates Keres Group, and consists of voluminous andesitic to dacitic, with some basaltic, lavas and associated volcanic breccias (Gardner et al.,
1986). Canovas Canyon rhyolite flows and tuffs typically underlie Paliza Canyon andesites and dacites, but are intercalated locally. Most of the Canovas
Canyon and Paliza Canyon volcanic rocks were erupted 8-10 Ma (Gardner et al., 1986; Goff et al., 1990; Lavine et al., 1996; Chamberlin et al., 1999).
Overlying the Paliza Canyon formation is the Bearhead Rhyolite, which consists of rhyolite intrusions, lava flows and domes, and the associated pyroclastic
and sedimentary strata of the Peralta Tuff Member. Bearhead rhyolite erupted between 6-7 Ma (Gardner et al., 1986).
Paliza Canyon formation (Miocene) - Monzonite dikes and stocks. Characterized in detail by Stein
(1983). Contains phenocrysts and locally glomerocrysts of plagioclase and augite set in a fine-grained
phaneritic to aphanitic groundmass of plagioclase, orthoclase, quartz, and augite. Fine-grained or
aphanitic locally. Light to very dark gray to dark green to black, pervasively hydrothermally altered.
Present along Colle Canyon in footwall of major NE-striking fault. Intruded by Tbi. Dikes range
between 1 cm to 30 m wide, trend northerly, and are vertical.
Tm
Cochiti Formation (Upper Miocene to Lower Pleistocene) - Volcanic sand and gravel in poorly
sorted, tabular beds. Clasts consist of Keres Group volcanic rocks with a distinct upward increase in
the abundance of devitrified and altered rhyolite at the expense of vitric rhyolite. Gradationally
overlies the upper Miocene Peralta Tuff Member of the Bearhead Rhyolite (Smith and Lavine, 1996;
Smith, 2000). The basal contact at Tent Rocks is located about 10 m above a 6.79 ±0.05 Ma
pyroclastic deposit (McIntosh and Quade, 1995). A 6.16 ±0.07 Ma (W. McIntosh, personal
communication, Oct. 1997) rhyolitic tephra is present in lower beds of the formation at Tent Rocks.
East of Tent Rocks, the lower Pleistocene Bandelier Tuff (Qbo) is present within the uppermost
Cochiti Formation. In the Cochiti Dam quadrangle, the upper Cochiti Formation contains primary and
reworked tephra-fall beds dated at 1.87 ±0.01 Ma and 1.84 ±0.02 Ma by 40Ar/39Ar (W. McIntosh,
personal communication, Feb. 1997 ) and correlated, by visual comparison, to the San Diego Canyon
A and B ignimbrites. The Cochiti Formation is interbedded with unit QTslg near the southeastern
corner of the quadrangle.
QUATERNARY
Pleistocene
Tglp
Qe
Tpv
Sierra Ladrones Formation (Upper Miocene to Lower Pleistocene) - Gravel deposited by axial
river (ancestral Rio Grande). Restricted to outcrops in the southeastern corner of the quadrangle, but
also found as clasts in Peralta Tuff at Tent Rocks, and in fault gouge along Pajarito fault on west side
of Bland Canyon. Contains about 35-40% quartzite, 20% granitic and metamorphic rocks and the
remainder mostly volcanic rocks. Clasts of Oligocene Pedernal Chert comprise 1 to 5% of most
outcrops. In the adjacent Santo Domingo Pueblo SW quadrangle, axial gravel is interbedded with
beds of Peralta Tuff Member of the Bearhead Rhyolite (Smith and Kuhle, 1997b) that yield
40Ar/39Ar ages of 6.81 ±0.02, 6.81 ±0.01, and 6.88 ±0.01 Ma (W. McIntosh, personal
communication, Feb. 1997 ). At Tent Rocks, rhyolitic hydromagmatic deposits dated at 6.90 ±0.06 Ma
(McIntosh and Quade, 1995; Smith, 2000), and clearly from a lower stratigraphic position than the
samples providing the three ages above, contain accessory clasts derived from axial gravel deposits.
Tephra, apparently reworked from the lower Bandelier Tuff, and dated at 1.62 ±0.01 Ma (W.
McIntosh, personal communication, Feb. 1997 ) is present approximately 20 m below the top of the
Sierra Ladrones Formation in the Santa Fe River valley immediately upstream of Cochiti Dam in the
Santo Domingo Pueblo quadrangle (Smith and Kuhle, 1997a). These dates limit the age of the Sierra
Ladrones Formation outcrops in the Santo Domingo from late Miocene to early Pleistocene, although
outcrops on this quadrangle are all of late Miocene age.
QTslg
Qal
Qbo
QTc
6.19
Qal
Qec
Qec
QTc
Qec
The Canada quadrangle is located at the boundary between the southern Jemez volcanic field and northern Santo Domingo Basin, and on the western edge of
the Rio Grande rift. The Santo Domingo Basin is an accommodation zone within the rift that is filled primarily with Santa Fe Group sediments (Smith and
Kuhle, 1998). The Jemez volcanic field is at the intersection between the rift and the northeast-trending Jemez lineament. These structures are
characteristically expressed in the Jemez Mountains as northerly and northeasterly trending normal faults. Miocene to Pleistocene lavas and pyroclastics
ranging in composition from basalt to rhyolite make up the volcanic field, and its development culminated with the formation of the Valles caldera and
associated 1.22 Ma eruption of the Bandelier tuff. The southeastern margin of the Valles caldera is about 10-15 km northwest of the Canada quadrangle.
Paliza Canyon formation (Miocene) - Volcaniclastic deposits. Coarse-grained volcaniclastic
breccia, conglomerate, and sandstone interbedded with thin Paliza Canyon formation lava flows and
flow breccias of basalt and basaltic andesite composition. Primarily debris-flow and fluvial deposits
consisting of reworked flow-breccia blocks and tephra. Locally includes primary and slightly
reworked gray, andesitic tephra and white rhyodacitic and dacitic tephra. Outcrops in Cochiti and
Sanchez Canyons include monolithologic breccias with sparse radially-jointed blocks that may be
block-and-ash-flow deposits. Stratigraphy, volcanology, and sedimentology of these deposits
described by Lavine (1995)
Quaternary and Tertiary
35°40'0"N
Tglp
Qe
Qbo
QTc
Tglp
Tglp
Qe
QTc
Qoa
Qt4
QTc
Qe
Qe
Qt1?
45
Tglp
Tglp
QTc
QTc
18
7
QTc
Tglp
Qt1
70
Paliza Canyon formation (Miocene) - Olivine andesite. Domes and flows of black to gray andesite
and minor red cinder deposits. Contains plagioclase, clinopyroxene, hypersthene and iddingsitized
olivine in itersertal to glassy groundmass. May contain sparse plagioclase-pyroxene clots. May
contain apatite microphenocrysts. Flows massive with vesicular flow tops. Flows rarely sheeted.
Tpoa
Bandelier Tuff, Otowi Member and Guaje Pumice Bed (Lower Pleistocene) - White to tan nonwelded rhyolite ash-flow tuff containing abundant (~10-15%) phenocrysts of euhedral quartz (3 mm)
and sanidine, with more quartz than sanidine, and trace mafic phenocrysts. Commonly contains
abundant (3-10%) mafic lithic clasts. Basal pumice-fall deposit (Guaje Pumice Bed) occurs locally
(less than 2 m thick). Typically forms slopes, and tent rock formation is also common. Erupted ~1.61
Ma during the Toledo caldera formation. Maximum thickness ~100 m.
Qbo
Qec
Qbo
Qc
Tbp
Qec
Tglp
6.91
Qec
Tbr
Qe
QTc
Qal
Qec
Qe
Qe
Qbo
Qec
75
7
QTc
3949 000
50
Qal
Tglp
Tglp
3947000
35
Qbo
Qal
Qec
Qe
QTc
Qt4
Qec
Tbr
24
QTc
QTc
Tglp
Tbp
Qc
Tbp
Tglp
Tglp
Qt1
Paliza Canyon formation (Miocene) - Flows, domes, and minor intrusives of gray to dark pink to
black porphyritic andesite. Also includes associated volcanic breccias, which are especially thick in
upper Cochiti Canyon (Lavine, 1995). Contains 1-5% phenocrysts of plagioclase, clinopyroxene, and
lesser amounts of hypersthene. Maximum observed thickness about 140 m. Commonly flow banded.
Tpa
Bandelier Tuff, Tshierge Member and Tsankawi Pumice Bed (Lower Pleistocene) - White to tan to
orange, non-welded to welded, rhyolite ash-flow tuff containing abundant (~15%) phenocrysts of
quartz and sanidine, with quartz more abundant than sanidine, and trace clinopyroxene. Quartz
phenocrysts are large (up to 3 mm) and euhedral. Sanidine is clear and commonly displays a blue
iridescence. Locally contains abundant lithic clasts but typically lithic-poor (less than 2%).
Compound cooling unit consisting of at least three flow units. Typically non-welded to slightly
welded, but is densely welded locally. Basal pumice-fall deposit (Tsankawi Pumice Bed) occurs
locally (less than 2 m thick). Forms conspicuous orange cliffs. Erupted ~1.22 Ma during Valles
caldera formation. Maximum thickness ~150m.
Qbt
QTc
Qt1?
Qt1
QTc
Qe
Qt4
Qt3
60
46.4, 46.7
Tglp
Tbp
Qt1
QTc
3950 000
Qe
Qt3
Qbt
Qal
QTc
Qal
Qt3
Tpv
Qt3
Tbp
QTc
Qal
Tbp
10
QTc
Paliza Canyon formation (Miocene) - Porphyritic andesite. Domes and flows of coarse, gray to
black porphyritic andesite having large phenocrysts of plagioclase and abundant phenocrysts of
clinopyroxene and hypersthene in a glassy almost intersertal groundmass of plagioclase,
clinopyroxene, hypersthene, and opaque minerals. Plagioclase may be complexly zoned, and may
contain clots up to 20 cm in diameter. Flows may be sheeted or contain flow breccia. K-Ar age west
of Rancho Canada 9.33 ±0.19 Ma (Goff et al., 1990). Maximum observed thickness about 150 m.
Tppa
Older alluvium (Lower Pleistocene?) - Alluvial gravel and sand locally underlying Bandelier Tuff
north of Peralta Canyon. Delineates paleodrainages incised into the Peralta Tuff Member of the
Bearhead Rhyolite, Cochiti Formation, and gravel of Lookout Park, and later filled by the
BandelierTuff. Thickness is typically 1-3 m.
Qoa
Qec
Qt1
Qt3
Qal
Tbp
Qbo
Tpv
Qbo
Tglp
QTc
Qt3
Qt3
Qt4
Qt2?
15
Qt4
Qt3
Qal
16
Tbp
72
Qc
54 Qbo
Qt1
Qal
Qt3
Qbo
6.97
Tbp
Qc
3951 000
Qt4
Paliza Canyon formation (Miocene) - Hornblende dacite. Domes, flows, and minor intrusives of
gray to pink porphyritic dacite containing ~1-5% phenocrysts of plagioclase, hornblende, minor
clinopyroxene, ±biotite. May contain clots of plagioclase and mafic minerals. Flows massive to
banded, may contain flow breccia. Outcrop in NW corner of quadrangle is coarsely porphyritic with
plagioclase and hornblende phenocrysts up to 1 cm. Maximum observed thickness about 60 m.
Tphd
El Cajete Member Pumice (Valles Rhyolite, Upper Pleistocene) - Discontinuous sheetwash and
fluvially reworked rhyolite pumice-fall deposit, typically less than 5 m thick. Also includes poorly to
moderately sorted primary deposits that occur along the Pajarito fault zone and in Bland Canyon.
Pumice clasts are white to tan, vesicular, and typically less than 7 cm in diameter. They contain less
than 2% phenocrysts of quartz, sanidine, biotite, and rare clinopyroxene and hornblende. Erupted
approximately 60 ka from the El Cajete crater in southern moat of Valles caldera. Quarried in many
locations. Maximum thickness about 10 m.
Qec
Qt4
Tpv
10
Tbr
Tbp
Qbo
Qbt
80
15
Qbt
18
Qec
Qc
Qbo
Qec
Tbr
Qc
Qt4
Qbo
Tbp
Qbt
Qt1
Qt1
Tbr
Tbr
6.99
Qc
Tbp
Qc
Qbo
Qbo
3952 000
Paliza Canyon formation (Miocene) - Biotite dacite. Domes, flows, and minor intrusives of gray to
pink porphyritic dacite containing ~1-5% phenocrysts of plagioclase, biotite, ±clinopyroxene,
±hornblende, ±quartz. Typically massive but is flow banded or flow brecciated locally. Maximum
observed thickness is about 150 m.
Tpbd
Terrace gravel (Middle Pleistocene) - Fill-terrace gravel, generally 3-5 m thick, but locally as
much as 20 m thick, marking former courses of Peralta and Cochiti Canyons. This gravel deposit
commonly forms inverted ridges rather than being inset along modern drainages and, therefore, is
technically not a terrace deposit, but is mapped as a terrace deposit to be consistent with
designation of presumed correlative gravel. Terrace gravel in a similar landscape position on the
Santo Domingo Pueblo Southwest quadrangle contains the 620 ka Lava Creek B ash (Smith and
Kuhle, 1997b).
Qt1
Qt4
Qec
Qec
Tpv
Tbp
A'
QTc
Tpv
30
Qc
Qbo
50
Qt4
Qec
Qt4
35°42'30"N
Tpa
9
Tpv
Qbo
Qal
67
Qbt
Qec
Qbt
Qc Qal
Tbp
32
Tbi
Qbo
Qbo
6.96
Qbt
81
Qc
6.86
Qc
Tpv
10
15
7.06
Qbo
38
Tbp
Tbp Qc
Tpa
Qc
17
77
18
Qbt
60
6
Qbo
Qbt
9.33
71
10
Tbp
Tbp
Tbi
Qbo
7
Qc
3951000
Qbt
Qec
Qal
30
77
Tbr
Qbt
25
Qbo
Tbp
85
Qbo
Qbo
Qal
27
Tbi
Qec
Tppa
7
3952000
Tpv 30
60
Qec
Qbt
9.25
Tppa
10
Tbr
Terrace gravel (Middle Pleistocene) - Fill-terrace gravel, 5-10 m thick, located approximately
50-70 m above grade. The correlative terraces along the Rio Grande on the Santo Domingo
Pueblo quadrangle are less than 550 ka (Smith and Kuhle, 1998) and are tentatively correlated to
Española Basin terraces for which Dethier and McCoy (1993) estimate an age of 310 ±70 ka. Qt2
is probably correlative with the Cañada terrace of Aby (1997).
Qt2
23
Tpv
30
Tbp
Tpv
Qal
Qbt
Qc
Tbi
Tpbd
Qbt
18
3953 000
Qbt
Tbi
24
25
47
Qec
Qbt
Tpbd
Bearhead rhyolite, Peralta tuff member (Upper Miocene) - White to tan to pale pink, pyroclasticfall, flow, and surge deposits interbedded with gray to tan sandy gravel. Pyroclastic deposits consist
of pumice and ash of crystal-poor rhyolite containing less than 3% phenocrysts of quartz, sanidine,
biotite, and plagioclase. Typically contains abundant (10%) lithic clasts of dominantly andesite and
rhyolite lava with lesser amounts of dacite and basalt lava. Sedimentary layers contain exclusively
volcanic clasts, which are predominantly glassy and devitrified rhyolite, with variable amounts of
intermediate-composition rocks from the older Paliza Canyon formation. Sedimentary strata are
thickest near the base of the unit in Bland Canyon, and are restricted to the Bearhead basin (Smith,
2001) between Peralta and Bland Canyons. The stratigraphy of the Peralta Tuff is described by Smith
(2001). Forms tent rocks locally. Erupted between about 6.2-7.0 Ma (Smith, 2001). Thickness in the
map area is about 500 m.
Tbp
Terrace gravel (Middle Pleistocene) - Fill-terrace gravel 5-10 m thick, with an upper surface
approximately 30-35 m above grade. Terraces probably correlate to similarly numbered terrace
deposits along the Rio Grande in the Santo Domingo Pueblo quadrangle (Smith and Kuhle, 1998).
The Rio Grande terraces likely correlate to those for which Dethier and McCoy (1993) estimate
an age of 170 ±40 ka.
Qt3
Tppa
Qls
Tcc?
Tcc
Qec
12
Tbi
Tcc
10.5
Tpv
Tpv
Tbp
Tbr
Tpa
3954 000
Tpv
Tpoa
Tppa
Qal
Qls
Tcct
Tppa
Tpa
10
Tcc
Qbt
Tpa
Tpv
Bearhead rhyolite (Upper Miocene) - White to light gray rhyolite dikes, plugs and stocks. Contain
1-3% phenocrysts of quartz, sanidine, biotite, ±minor plagioclase. Commonly displays intense,
vertically oriented platy cleavage. Vitrophyre typical near margins. Present along and at the
intersection of N-S and NE-SE striking faults.
Tbi
Terrace gravel (Upper Pleistocene) - Fill-terrace gravel with an upper surface approximately 1820 m above grade along Peralta and Cochiti Canyons. Gravel is typically no more than 3 m. On
the Santo Domingo Pueblo quadrangle, Qt4 grades to a terrace along the Rio Grande that is
overlain by ca. 60 ka El Cajete pumice (Smith and Kuhle, 1997a). Dethier and McCoy (1993)
estimate an age of 95 ±15 ka for fill terraces at a similar elevation above grade in the Española
Basin.
Qt4
12.4
Tpv
80
Tbr
Qbo
Tbp
Tpv
Tphd
Qbo
Tphd
Tbp
Tpa
Tbr
Qc
Tbp
9.18
Tpa
Qec
Tcct?
Tbr
Tcct?
65
Terrace gravel (Pleistocene) - Fill and strath piedmont-stream terraces formed along tributaries to the
Rio Grande, primarily associated with Peralta, Bland, and Cochiti Canyons. Gravel is composed of
variably altered andesitic and rhyolitic clasts and, in Peralta Canyon, Bandelier Tuff fragments.
40
Tpbd
Tcct?
Qbt
Tpbd
Tbi
Tcc
Tppa
Tpa
3954000
Tcct
15
Tbi?
35
50
50
Tbr
Qbt
Tbp
65
3955 000
Qbt
Qls
Tbp
Tcct
Bearhead rhyolite (Upper Miocene) - Lava domes and flows of white to pale pink to light gray
rhyolite and volcanic breccias. Contains 1-3% phenocrysts of quartz, sanidine, biotite, ±minor
plagioclase. Commonly strongly flow banded with vitrophyre near margins. Domes distributed along
N-S and NE-SW striking faults. Erupted between 6.52-7.06 Ma (Justet, 1999). Maximum thickness
is ~370 meters observed near the type locality of Bearhead Peak.
Tbr
Eolian sand and silt (Upper Pleistocene to Holocene) - Massive fine sand and coarse silt forming a
0.5-3 m thick deposit, primarily on top of the ancient geomorphic surface that is underlain by the
gravel of Lookout Park.
Qe
Tpa
Keres Group
Landslides (Upper Pleistocene to Holocene) - Poorly sorted debris that has moved down steep
slopes chaotically or as a series of blocks.
Qls
Tbp
Qbt
Tpv
Tcct?
85
Tbr
Tpv
Qc
Qbo
7.12
Tbr
Tpv
Tpa
Tbi
9.24
Tbi
Tpa
Qbt
Tbr
Tpa
Tm
Tpa
Tpa
Qbt
Tcct?
Tbp
Qbt
Qc
3955000
Tpoa
Tpbd
Tbi
Qbo
Tpv
3956 000
Tcc
Gravel of Lookout Park (Upper Pliocene) - Cobble to boulder gravel resting on a broad pediment
surface cut primarily on Cochiti Formation in the southwestern part of the quadrangle. The gravel is
composed mostly of Keres Group andesite and rhyolite clasts, and is 5-15 m thick. Gravel is inset
below basalt of Santa Ana Mesa dated at 2.41 ±0.03 Ma, on the Santo Domingo Pueblo Southwest
quadrangle (Smith and Kuhle, 1997b), and underlies lower Bandelier Tuff (1.61 Ma), indicating
deposition during a short period of the late Pliocene. Remnants of a stage IV calcic soil horizon are
present at the surface in some places. This older soil was stripped and then the gravel was largely
buried in eolian sand and silt (Qe) in which a new soil has formed with a stage II-stage III calcic
horizon evident in various places.
Tglp
Colluvium (Upper Pleistocene to Holocene) - Hillslope and talus deposits from local sources. In
the southern half of the quadrangle, colluvium is loose gravel primarily eroded from the gravel of
Lookout Park. Most hillslopes contain a few centimeters to a meter thickness of colluvium, but unit
Qc is mapped only where the thickness and distribution of colluvium prohibits confident mapping of
other units. As thick as 20 m locally.
Qc
30
Qbo
8
Tbi
Tbi
Tpbd
Tpv
Tpoa
9.11
Tbi
Tbr
Qbo
Tbi
Tbi
Tpbd
9.32
75
20
Tbi
Tpoa
Qbt
Tpbd
Qbt
Tpa
Alluvium deposited by active streams (Upper Pleistocene? to Holocene) - Poorly sorted gravelly
sand and sandy gravel deposited in channels and minor floodplain areas of ephemeral streams and
arroyos. Beds of eolian fine sand up to 0.5 m thick are locally present, and colluvium is present near
valley margins. Total thickness is unknown but may be as much as 10-30 m.
Qal
35°45'0"N
Tpv
Tpv
Qbt
Tpv 10
Tpa
Tm
Tpa
Qbt
Tpbd
Tcc
Tpa
Qbt
Qec
Qls
Tpa
Qbo
Qls
Tm
Qc
Tpv
Qec
Tpbd
Tpy
Tbi
Tm
Qbt
Tpa
Tm
Tpa
3957 000
Tpbd
Qls
Tbp
Tbi
Tm
Tpbd
Qec
Qbo
Tpa
Tbi
Qc
Qbt
Qbo
Tsf
Tm
Tm
Tm
ul
t
Tpbhd
3957000
Geologic Overview
Tertiary
>
fa
35°45'0"N
Last Modified 28 June 2007
7000
Tm
Tbi
Tbr
Tm
Qbt
Qbo
Tglp
Tglp
Tbi
?
No vertical exaggeration
Qbt
Tbp
Tpa
6000
Qbt
Tbr
Tbp
Tbp
Tpa
Tpa
Tglp
7000
Tbp
Tpa
QTc
6000
Elevation (feet)
373000
nd
e
372000
Elevation (feet)
106°25'0"W
371000
Ri
370000
lta
369000
ra
368000
Pe
106°27'30"W
367000
NMBGMR Open-file Map Series OFGM 85
?
366000
>
365000
>
106°30'0"W
Elevation (feet)
364000
A DIVISION OF NEW MEXICO INSTITUTE OF MINING AND TECHNOLOGY
Elevation (feet)
NEW MEXICO BUREAU OF GEOLOGY AND MINERAL RESOURCES