NEW MEXICO BUREAU OF GEOLOGY AND MINERAL RESOURCES
105°37'30"W
444000
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A DIVISION OF NEW MEXICO INSTITUTE OF MINING AND TECHNOLOGY
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PENASCO
RANCHOS
RANCHOS DE TAOS
DE TAOS
TRES RITOS
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PUEBLO PEAK
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Magnetic Declination
March, 2006
9º 30' East
At Map Center
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454000
36°15'0"N
7000 FEET
455000
NATIONAL GEODETIC VERTICAL DATUM OF 1929
Tch
May 2000
1 KILOMETER
CONTOUR INTERVAL 40 FEET
(Ranchos de Taos and Taos): Servilleta Formation, basalt (Pliocene) - In cross section only. Dark-gray, diktytaxitic olivine
tholeiite, which forms thin, fluid, widespread pahoehoe basalt flows of the Taos Plateau volcanic field. These flows commonly
form columnar-jointed cliffs in the Rio Grande Gorge. Tabular plagioclase and sparse olivine are the only phenocrysts. Individual
flows, which are up to 12 m thick, are grouped into packages of from one to ten flows. These packages are separated by 0.3-4.5
m thick sedimentary intervals (Leininger, 1982). Five central volcanic vents to the north are sources for the Servilleta Formation
(Lipman and Mehnert, 1979). 40Ar/39Ar ages from basalts exposed in the Rio Grande gorge range in age from 4.81 ± 0.03 Ma for
the lowest basalt near the Gorge Bridge, to 3.12 ± 0.13 Ma for the highest basalt flow at the Gorge Bridge (Appelt, 1998).
105°30'0"W
Geologic map of the Ranchos de Taos
quadrangle, Taos County, New Mexico.
SHADY BROOK
CERRO VISTA
4012000
&ash2
by
Paul Bauer , Keith Kelson , J. Lyman3, M. Heynecamp1, and Dave McCraw1
1
(Carson, Taos SW, and Ranchos de Taos): Ojo Caliente Sandstone of Tesuque Fm of Santa Fe Group (Miocene) - Buff to
white, well-sorted eolian sandstone. Dominant grain size is fine sand. Abundant 1.3-5.0 cm thick brown CaCO3 concretions. QFL
proportions average 62% quartz, 28% feldspar, and 10% lithics. LvLsLm ratio averages 82% Lv, 8% Ls, and 10% Lm. Thin
reddish-brown, finely laminated siltstone horizons are found locally. Tabular crossbeds are common, with sets over 4 m in height.
Transport was from southwest to northeast. Deposited at 13-12 Ma (Steinpress, 1980). Best exposures are in roadcuts along
NM-68, northeast of Pilar. About 250 m thick.
Tce
Chama-El Rito Member of Tesuque Fm of Santa Fe Group (Middle Miocene) - Volcanic-rich, non-fossiliferous sandstone
(50%) and conglomerate (42%), with minor mudrock interbeds (8%). Conglomerates are generally purplish to gray due to
predominance of pebble-size Tertiary volcanic clasts. Sandstones are pinkish-gray to buff, poorly to moderately sorted, with highly
variable grain size. Sandstones are transitional between arkoses and volcanic arenites. Siltstone and clayey siltstone beds are
reddish-brown and generally less than 1 m thick. Sandstone QFL percentages average 39% quartz, 31% feldspar, and 30%
lithics. LvLsLm percentage averages 80% volcanic lithics. White beds of calcareous, pyroclastic volcanic ash, less than 2 m thick,
are found locally. Fluvial and alluvial sedimentary structures are common. Represents braided stream deposits on a distal alluvial
fan derived from a volcanic terrain to the northeast. Lower part contains 10-m-thick weakly consolidate, coarse, cobble to boulder
conglomerate composed of rounded, white to gray quartzite clasts (up to 2 m) and subordinate granite clasts. Age is about 18-14
Ma (Steinpress, 1980). Pinches out to the southeast. Thickness up to 480 m.
1
QUADRANGLE LOCATION
This draft geologic map is preliminary and will undergo revision. It was produced
from either scans of hand-drafted originals or from digitally drafted original maps
and figures using a wide variety of software, and is currently in cartographic production.
It is being distributed in this draft form as part of the bureau's Open-file map series
(OFGM), due to high demand for current geologic map data in these areas where
STATEMAP quadrangles are located, and it is the bureau's policy to disseminate
geologic data to the public as soon as possible.
After this map has undergone scientific peer review, editing, and final cartographic
production adhering to bureau map standards, it will be released in our Geologic Map
(GM) series. This final version will receive a new GM number and will supercede
this preliminary open-file geologic map.
DRAFT
New Mexico Bureau of Geology and Mineral Resources
Open-file Map Series
2
OFGM 33
COMMENTS TO MAP USERS
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).
New Mexico Bureau of Geology and Mineral Resources
New Mexico Tech
801 Leroy Place
Socorro, New Mexico
87801-4796
[505] 835-5490
http://geoinfo.nmt.edu
This and other STATEMAP quadrangles are (or soon will be) available
for free download in both PDF and ArcGIS formats at:
http://geoinfo.nmt.edu/publications/maps/geologic/ofgm/home.html
A 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.
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.
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.
Chamita Formation of Santa Fe Group (Miocene and Pliocene) - Composition ranges vertically. Lower section consists of buffcolored, moderate to poorly sorted sands with clasts of intermediate volcanic rock, quartzite, and other metamorphic rocks.
Middle section contains fewer volcanic clasts and more metamorphic clasts. Upper section is devoid of volcanic clasts. Overall,
unit coarsens upwards, and dips decrease from 30o NW at base to horizontal at top. Exposure just north of Pilar contains an
internal angular unconformity of about 15o near top of exposure. Interfingering basal contact with Ojo Caliente Sandstone.
Thickness about 230 m.
To
2
NMBGMR, 801 Leroy Pl., Socorro, NM, 87801
William Lettis and Assoc., 1777 Botelho, Walnut Creek, CA 94596
3
Department of Earth and Environmental Sciences, New Mexico Tech, Socorro, NM, 87801
Nodular/brecciated limestone of the Alamitos(?) Formation - Bluish-gray, packestone with cross-cutting calcite veins.
Contains fossils of fusilinids, crinoids, brachiopods, bryozoans, Rugose corals, and algae. Generally round-weathering
outcrops. Fusilinids are Desmoinesian in age (B. Allen, 2000, personal communication). Interpreted as cyclic deposits in
shallow, fully marine environment within the photic zone.
IPcq Distinctive conglomerate - Poorly sorted, clast-supported, thin, isolated beds of conglomerate containing 99% round quartzite
pebbles (2-20 cm in diameter) with a fine-grained matrix. Ledge former. Discontinuous along strike due to channel- and lensshapes. Occurs as isolated beds that range from 2-10 m in thickness.
Mdp
Tp
Picuris Formation, undivided (Oligocene) - Light gray to pinkish gray, immature, pumice-rich conglomeratic sandstone.
Tpu
(Ranchos de Taos and Taos SW): Picuris Formation, upper member (Oligocene) - Light gray to pinkish gray, immature,
pumice-rich, ashy, polylithologic, conglomeratic sandstone. Consists mainly of sandstones with gravel-sized clasts of pumice
and silicic volcanic rocks (mostly 26 Ma Amalia Tuff), and minor Precambrian quartzite and intermediate composition volcanic
rocks (including the Latir Peak quartz latite). Most of gravel-sized fraction is pumice, with some clasts up to 25 cm in diameter.
Most clasts are rounded to well rounded. Imbrication of clasts is common, although bedding features are indistinct due to the
homogeneous nature of lithology and grain size, and the weak induration. Mostly, unit is matrix cemented, with local minor
silica cement. Poorly to well lithified. Contains layers and lenses of resistant, well cememted, cobble conglomerates
interlayered with easily eroded, weakly cemented pebble conglomerates. Generally gray weathering. Paleoflow
measurements indicate source to the north (Rehder, 1986). Total thickness of upper member is 200-250 m. Interpreted as an
alluvial fan deposit derived from the Latir volcanic field at around 26 Ma (Rehder, 1986).
(Taos SW): Del Padre member of Espiritu Santo Formation of Arroyo Penasco Group (Mississippian) - Quartz
sandstone, local quartzite conglomerate, siltstone, and shale. Interfingers with Espititu Santo Formation carbonates.
Proterozoic Rocks
dd
(Carson): Dacite dike (age unknown, but probably Middle Proterozoic) - Dark green-gray quartz diorite dikes intruded into
Proterozoic rocks only. Dikes are vertical, with strikes clustered around an azimuth of 150 o. Composed of pale green
clinopyroxene (Cr-diopside?), zoned plagioclase (labradorite?), and minor quartz, magnetite, and ilmenite. Commonly altered to
chlorite and clay. Pyroxene and feldspar show normal plutonic textures. Locally, dikes are laced with carbonate veins. Dikes are
generally less than 1 m wide. Contacts between diorite and country rock are sharp and commonly contain zones of brecciation
and faulting. Faults are sub-vertical with dip slip fault striations. Dikes are parallel to the Pilar-Vadito fault and other southeaststriking faults.
xxx
Pegmatite - Simple pegmatites of quartz-K-feldspar-plagioclase-muscovite. Pegmatite bodies typically are dikes or lenses, locally
aligned parallel to country rock foliation and fold hinges. Thicknesses range from a few centimeters to several meters.
Xmg
Miranda granite (informal name) - East of the Picuris-Pecos fault. Generally consists of pink to white, medium-grained, mica-rich
granitic rock with euhedral megacrysts of feldspar. These granitic rocks are everywhere weathered looking, fairly equigranular,
and commonly crumbly. Appears to intrude the Rio Pueblo schist along southern contact. Pegmatites are locally voluminous.
Contains at least one tectonic foliation. Three closely-spaced, orthogonal joint sets cause this rock to weather into small, angular
blocks. Age unknown, but similar in occurrence and texture to the 1.6 Ga Tres Piedras Granite of east-central Tusas Mountains.
Xu
Undifferentiated Proterozoic - Supracrustal metamorphic rocks and plutonic and metaplutonic rocks of the Taos Range.
Xhpl
(Carson and Taos SW): Piedra Lumbre Formation, Hondo Group - Exposed only in two small areas northeast of the PilarVadito fault. Includes quartz-muscovite-biotite-garnet-staurolite phyllitic schist with characteristic sheen on crenulated cleavage
surfaces, and finely laminated, light gray, phyllitic quartz-muscovite-biotite-garnet schist and darker bluish gray fine-grained biotite
quartzite to metasiltstone. Euhedral garnets are 1 mm, biotite books are 2 mm, and scattered anhedral staurolites are up to 5 mm
in diameter. Calc-silicate layers exist locally. Original sedimentary structures such as graded bedding are locally preserved.
Contact with underlying Pilar Formation is gradational. Apparent thickness is 200-400 m.
Xhplq (Carson and Taos SW): Piedra Lumbre Formation quartzite, Hondo Group - Massive to layered, light-colored, crossbedded
micaceous quartzite. Locally garnet-bearing. Approximate thickness of 25 m.
Xhplp (Carson): Piedra Lumbre Formation phyllite, Hondo Group - Dark gray to black, fine-grained, garnet-bearing phyllite. Crops
out only in the core of the Hondo syncline east of the Pilar-Vadito fault.
Xhp
(Carson and Taos SW): Pilar Formation, Hondo Group - Exposed northeast of the Pilar-Vadito fault. Dark gray to black,
carbonaceous phyllitic slate. Extremely fine-grained homogeneous rock except for rare 1- to 2-cm thick light colored bands of
quartz and muscovite that may represent original sedimentary bedding. In thin section, fine-grained matrix consists of quartz (5070%), muscovite (15-30%), and prominent streaky areas of graphitic material. Lenticular porphyroblasts (0.1 to 0.5 mm) are
altered to yellow-brown limonite. Pervasive slaty cleavage is locally crenulated. Small isoclinal folds locally. Basal 1.5 m-thick,
black to blue-black, medium-grained, garnet quartzite is distinctive. Garnets are anhedral, oxidized, and red-weathered.
Gradational with Hpl. Thickness unknown due to extreme ductile deformation.
Xhr6
(Carson and Taos SW): Rinconada Formation, R6 schist member, Hondo Group - Tan, gray, silver quartz-muscovite-biotitestaurolite-garnet schistose phyllite interlayered with fine-grained garnetiferous muscovite quartzite. Euhedral staurolites (<5 cm)
abundant in some layers. Small euhedral garnets (<2 mm) throughout. Strong parting along well-developed foliation. Sharp
contact with Hp. Thickness is approximately 90 m.
Xhr5
(Carson and Taos SW): Rinconada Formation, R5 quartzite member, Hondo Group - Variety of white to blue medium-grained
quartzites interlayered with fine-grained schistose quartzites and quartzose schists. Measured section by Hall (1988) from an area
just to the south, from top to bottom: 1) tan to white, friable, thinly layered, crossbedded micaceous quartzite; 2) blue, mediumgrained, thickly layered, resistant saccharoidal quartzite; locally crossbedded; 3) white to tan, friable schistose quartzite layered
with blue, medium-grained saccharoidal quartzite; thin layers of fine-grained quartz-muscovite-biotite schist; basal 1.5 m massive
blue medium-grained quartzite; 4) tan, thinly layered, micaceous quartzite layered with quartz-rich muscovite schist; abundant
crossbedding; 5) blue and white streaked, thickly bedded, medium-grained quartzite with abundant crossbedding; and 6) tan,
thinly layered, micaceous quartzite interlayered with quartz-rich quartz-muscovite schist; abundant crossbedding. Gradational
contact with Hr6. Thickness is approximately 75 m.
Xhr4
(Carson and Taos SW): Rinconada Formation, R4 schist member, Hondo Group - Medium- to coarse-grained, silvery gray,
quartz-muscovite-biotite-staurolite-garnet schist containing one or more distinctive, 0.5-2.0 m thick, layers of glassy blue quartzite,
rusty red weathering garnetiferous white quartzite, massive, extremely hard, red weathering, olive-brown biotite-staurolite-garnetorthoamphibole rock, white, glassy, hornblende quartzite, gray biotite-hornblende calc-schist, mylonitic blue to pink and blue,
glassy quartzite, and white to gray calcite marble. In this area, Hr4 is a transitional sequence of interlayered schist and quartzite,
making the contacts with Hr3 and Hr5 indistinct. Thicknesses range from 50-175 m.
Xhr3
(Carson and Taos SW): Rinconada Formation, R3 schist member, Hondo Group - White, gray, bluish-green and blue,
medium-grained, thinly to thickly bedded, resistant quartzite with abundant crossbeds (Hr3q). Locally includes two mappable
layers of pelitic schist (Hr3s) that resemble Hr4 and upper Hr1/2. Distinctive marker layer near center of unit is 25 m-thick, white,
thinly bedded, ridge-forming quartzite. Sharp contact with Hr4. Thickness is approximately 75 m.
(Los Cordovas): Basalt (Pliocene) - Primarily Servilleta Basalt of Peterson (1984). Along western edge of quadrangle, may
include other Tertiary basaltic rocks derived from Tres Orejas, west of the Los Cordovas quadrangle. In addition to source vents
to the north identified by previous workers (Lipman et al., 1979; Peterson 1984; Dungan et al., 1984), newly postulated source
vents are located near Taos Municipal Airport (N4034125, E0439650), within Taos Pueblo Tract A (N4033850, E0437550), and in
the northeastern part of the Tres Orejas quadrangle (N4036350, E0432475). 40Ar/39Ar ages from basalts exposed in the Rio
Grande gorge range in age from 4.81 ± 0.03 Ma for the lowest basalt near the Gorge Bridge, to 3.12 ± 0.13 Ma for the highest
basalt flow at the Gorge Bridge (Appelt, 1998).
10
24
NEW MEXICO
TAOS SW
&ash4
21
1:24,000
TAOS
&ass4
&asl1
&ass1
Base map from U.S. Geological Survey1964, from photographs taken 1961, field checked in 1964.
1927 North American datum, UTM projection -- zone 13N
1000-meter Universal Transverse Mercator grid, zone 13, shown in red
LOS CORDOVAS
&ash3
&ashu
22
(Carson and Taos SW): Servilleta Formation, basalt (Pliocene) - Dark-gray, diktytaxitic olivine tholeiite which forms thin, fluid,
widespread pahoehoe basalt flows of the Taos Plateau volcanic field. These flows commonly form columnar-jointed cliffs in the
Rio Grande Gorge. Tabular plagioclase and sparse olivine are the only phenocrysts. Individual flows, which are up to 12 m thick,
are grouped into packages of from one to ten flows. These packages are separated by 0.3-4.5 m thick sedimentary intervals
(Leininger, 1982). The mesa east of Pilar displays four basalt flows north of the Embudo fault and only one flow south of the fault.
Five central volcanic vents to the north are sources for the Servilleta Formation (Lipman and Mehnert, 1979). 40Ar/39Ar ages from
basalts exposed in the Rio Grande gorge range in age from 4.81 ± 0.03 Ma for the lowest basalt near the Gorge Bridge, to 3.12 ±
0.13 Ma for the highest basalt flow at the Gorge Bridge (Appelt, 1998).
4013000
&ash1
20
33
85
Qfy
446000
10
20
Tp
36°15'0"N
105°37'30"W
18
Tb
&als2
&ass3
Qtu
Tp
&amu
4012000
Tp
60 20
Rhyodacite cone of Tres Orejas (Pliocene) - Dark, phenocryst-poor, locally flow layered rhyodacite that crops out in northern
Carson Quadrangle. Phenocrysts of augite and hypersthene are sparse and small; SiO2 is 62-64% (Lipman and Mehnert, 1979).
Uppermost Tb flows locally overlap the flanks of Tres Orejas. Older Tb flows lie below rhyodacite volcanoes elsewhere on the
Taos Plateau, so rhyodacite and olivine basalt (Tb) eruptions overlapped in time. 40Ar/39Ar ages from pyroxene dacites of Tres
Orejas are 4.84 ± 0.02 Ma (Appelt, 1998).
Tpcongl
55
45
&ass2
5
&ass2
15
20
QTg
Qtu
5
&asl2
&ass2
Qfy
Qtu?
Mes
Tr
&als2
Qc
Qtu?
(Carson): Older alluvium (Pliocene and early Pleistocene) - Poorly sorted sand and gravel deposits, preserved as remnant
gravel on ridge tops and hill tops, commonly composed of large, rounded to subrounded quartzite boulders up to several meters
in diameter; in Carson quadrangle, present on high erosional surfaces, and along the Pilar-Vadito fault; maximum thickness
unknown but at least 10 m.
Tertiary Rocks
&ash2
8
Qtu
Blueberry Hill deposit (late Tertiary? to middle Pleistocene) - Poorly sorted silt, sand and pebbles; commonly cross-bedded,
and stained with black manganese oxide and yellowish-orange iron oxide coatings; oxidized; clasts are weathered or grussified;
contains distinct discontinuous sandy interbeds; clasts are granitic rock types, quartzite, metamorphic rock types, volcanic rock
types and rare sandstone; commonly crudely imbricated; imbrication suggests southwesterly flow direction in areas south and
east of Taos Municipal Airport; westerly flow direction in area north of Taos Municipal Airport; northwesterly flow direction in area
southeast of Rio Pueblo de Taos; based on exposures at southwestern end of Blueberry Hill, unit thickness exceeds 25 m and
may be considerably more; deposit may interfinger with unit Qt1rg in northwestern part of Los Cordovas quadrangle (relationship
unknown); deposit overlies or is inset into unit Tb in southern part of quadrangle. Unit also referred to as "Basin Fill deposit" by
Kelson (1986).
60
Qfu
89
Qfy
Xg
&als4
4014000
Xg?
Qfy
&ass4
&als1
&
Qc
Qc
Qtu
Qtu
63
Xg
70
Mt
Qtu
4013000
13
Qty
Mt
Qty
20
13
13
&
Mt
Mes
22
Qfy
Qfy
4015000
Qfu
Tp
Mt
&ass5/&a
5
Qfy
Qtu
Mt
4014000
&als1
Qtu
Qtu
Tp?
Fluvial gravel deposited by ancestral Rio Grande (early to middle? Pleistocene) - Poorly sorted sand, pebbles, and cobbles;
clasts of basalt, quartzite, slate, schist, other metamorphic rock types, other volcanic rock types, and (rarely) sandstone and
limestone; overlies Tb north of Pilar Mesa, but is inset into Tb on Pilar Mesa in Carson quadrangle; locally may contain clasts of
Tertiary Amalia Tuff; where preserved, associated relict soils have stage III to IV calcium carbonate development, thick argillic Bt
soil horizons, and 7.5YR to 10YR hues in soil Bt horizons; upper soil horizons commonly affected by surface erosion; may be
mantled locally by unit Qe.
QTbh
4015000
Tp
Qt1rg
10
35
26
Undifferentiated stream terrace deposits (middle to late Pleistocene) - Probably correlative with units Qt1 through Qt4, poorly
sorted silt, sand, pebbles and boulders; mapped in Taos quad only locally at mouth of Rio Pueblo de Taos near Taos Pueblo, and
at the mouth of the Rio Fernando.
&am3
15
Qtu
Mt
Xg
Qtu
15
75
65
Undifferentiated alluvial fan deposits (middle to late Pleistocene) - Probably correlative with units Qf1 through Qf4, poorly
sorted silt, sand, pebbles, and cobbles; mapped along majority of Sangre de Cristo range front, but nor correlated to other fan
units because of lack of well-defined age control or distinct lithologic characteristics.
4016000
&ass3
30
Alluvial-fan deposits (middle Pleistocene) - Poorly sorted silt, sand, pebbles, and boulders; stage III to IV calcium carbonate
development, although soil horizons are commonly affected by surface erosion; clasts primarily of quartzite, slate, and schist;
granitic clasts also present east of Arroyo del Alamo; finer grained to the north, away from the Picuris Mountains range front; in
Taos SW quadrangle, ash probably within Qf1 deposits at locality near Stakeout Road dated at 1.27 ± 0.02 Ma (40Ar/39Ar method,
W. McIntosh, personal communication, 1996); in Los Cordovas quadrangle, clasts primarily of granitic, intermediate volcanic,
basalt, and metamorphic rock types; in Los Cordovas quad, Qf1 is correlative with Unit Q1p of Kelson (1986); Qf1 surface on the
Los Cordovas quadrangle is dissected by numerous southwesterly-trending arroyos; deposit is more than 12 m thick in
northeastern part of quadrangle, and is thinner from northeast to southwest; directly southwest of Taos Municipal Airport, Qf1
deposit is less than about 1 m thick and unconformably overlies unit Tb. Elsewhere, Qf1 appears to overlie unit QTbh or unit Tb;
in Taos quadrangle, clasts primarily of granitic and metamorphic rock types; slope of Qf1 surface on the Taos quad is
southwesterly, and is dissected by numerous southwesterly-trending arroyos; deposit is more than 12 m thick in northwestern part
of quad, and is thinner from northeast to southwest; on Blueberry Hill, Qf1 deposit is about 3 m thick at Highway 64, but is thinner
(about 2 m) to the southwest, where it unconformably overlies unit Qtbh; Qf1 is differentiated from QTbh by larger clast size
(Kelson, 1986), less oxidation, poor sorting, absence of abundant manganese oxide staining, and clasts that are less weathered.
Qfu
20
20
Qty
50
10
&als3
25
Qtu
Qtu
4017000
12
Tp
36
30
IPlst
Alluvial-fan and stream terrace deposits flanking Rio Pueblo de Taos and tributaries (middle Pleistocene) - Poorly
sorted silt, sand, pebbles, and boulders; clasts primarily of granitic, metamorphic, volcanic, and sedimentary rocks; associated
soils have stage III to IV calcium carbonate development, thick argillic Bt soil horizons, and 7.5YR to 10YR hues in soil Bt
horizons; upper soil horizons may be affected by surface erosion; modified from Kelson (1986).
Older alluvial-fan deposits (early? to middle Pleistocene) - Poorly sorted silt, sand, pebbles, and boulders; clasts primarily of
quartzite, slate, and schist; fan surface is highly dissected and eroded, soil characteristics unknown; on Pilar Mesa in Carson
quadrangle, deposit is dominated by slate pebbles and cobbles.
80
Qfy
Qtu
Qfy
Alluvial - fan and stream terrace deposits (middle to Late Pleistocene) - Poorly sorted silt, sand, pebbles, and
boulders; stage II to III calcium carbonate development; clasts primarily of quartzite, slate, and schist; granitic clasts also present
east of Arroyo del Alamo; possible Qt3 remnant inset into terrace Qt2 on western side of Taos may be artificial terrace related to
residential development; modified from Kelson (1986).
Qfo
10
&ashu
4016000
Qfy
&asu
13
(Taos): Undivided Pennsylvanian sedimentary rocks of the Alamitos Formation (late Desmoinesian) and Flechado
Formation (Morrowan-Atokan-Desmoinesian) - Consists chiefly of poorly exposed, olive, brown, red, and dark gray shale and
siltstone plus fine- to coarse-grained sandstone with lesser amounts of conglomerate and limestone. Limestone (IPlst) is less
than 1% of the formation. Distinctive, rounded quartz cobble conglomerate (IPcon) is less than 1% of the formation. Alamitos
Formation is equivalent to the "upper arkosic limestone member" of the Madera Formation to the south. Flechado Formation is
equivalent to La Posada Formation to the south, which is equivalent to the Sandia Formation and the "lower gray limestone
member" of the Madera Formation. Fusilinids collected from the exposures southeast of Taos Pueblo are Desmoinesian in age (B.
Allen, 2000, personal communication). In general, the volume of limestone decreases northward within the map area. Crossbeds
examined in the Taos quad in coarse-grained sandstones all show a generally westward paleoflow. Thickness unknown, but a
minimum of approximately 2000 m.
(Ranchos de Taos): Espiritu Santo Formation of Arroyo Penasco Group (Mississippian, Osagean) - Consists of basal Del
Padre Sandstone member of thin basal conglomerate, quartz sandstone, and minor limestone beds at top. Grades into overlying
Tererro Formation. Upper, carbonate-rich part of Espiritu Santo Formation is mostly absent from the Ponce de Leon springs area.
15
13
Qfu
&assu
&assu
Tpu
IP
Mes
Tp?
Tplq
Tplq
70
Qfy
32
55
89
Qfy
Tp
&asu
85
&amu
28
Paleozoic Rocks
(Ranchos de Taos): Tererro Formation of Arroyo Penasco Group (Mississippian, Meramecian and Chesterian) - Near
Ponce de Leon springs, consists of 1-2 m of basal stromatilitic limy sandstone overlain by about 7 m of dolomitic limestone,
overlain by about 12 m of calcitic dolomite with stromatilites and bedded and nodular chert (Armstrong and Mamet, 1990).
Thickness is approximately 20 m.
4018000
15
&asu
30
&ass5
35
Tp
35
Tp
Mt
75
30
20
Tp
54
15
&asu &asu
&asu &asu
28
58
Xg
Landslide deposit (late Pleistocene to Holocene) - Poorly sorted sand to boulders, includes large rotational slide blocks within
the Rio Grande and Rio Pueblo de Taos gorges, which involve large, rotated and detached beds of Servilleta Basalt (Tb).
Mt
&alsu
60
5
32
(Carson and Taos SW): Picuris Formation, quartzite-boulder conglomerate (Oligocene) - Weakly consolidate, coarse,
cobble to boulder conglomerate composed of rounded, white to gray quartzite clasts (up to 2 m) and subordinate granite
clasts. Poorly sorted and unstratified. Sand matrix.40Ar/39Ar age of 34.5±1.2 Ma for a white ash adjacent to a conglomerate
layer is a good estimate of the depositional age of the unit. Probably equivalent to a Picuris Formation quartzite conglomerate
that is near a 34.6 Ma white ash in the Ranchos de Taos quadrangle. Equivalent to the Bradley Conglomerate of Leininger
(1982). Estimated thickness is 450m (Leininger, 1982).
Flechado Formation (Pennsylvanian, Morrowan-Atokan-Desmoinesian) - Thick sequence of olive, brown, and dark gray
shales and siltstones, with low-feldspar sandstones and conglomerates. Limestone is only 5-10% of the formation. Equivalent to
La Posada Formation to the south, which is equivalent to the Sandia Formation and the "lower gray limestone member" of the
Madera Formation. Approximately 760 m thick.
60
80
40
89
Tpc
IPf
13
19
30
Picuris Formation, andesite (Oligocene) - Andesite porphyry exposed in small outcrop south of Llano Quemado in the
Ranchos de Taos quadrangle.
Qf1
&alsu
20
20
Tpa
Alamitos Formation (Pennsylvanian, late Desmoinesian) - Consists chiefly of coarse-grained arkosic sandstone with lesser
amounts of conglomerate, limestone, and gray and red shales. Grades upward from clastic-rich to limestone-rich. Equivalent to
the "upper arkosic limestone member" of the Madera Formation to the south. Approximately 1200 m thick.
15
&am1
25 85
(Ranchos de Taos): Picuris Formation, lower member (Oligocene) - Boulder and cobble conglomerates and conglomeratic
sandstones interbedded with thinly bedded sandstones. Boulder unit is distinctive, composed of well rounded, poorly sorted,
mostly clast supported, Proterozoic quartzite clasts, with minor altered, intermediate Tertiary volcanics (Latir volcanics) and
Paleozoic sedimentary rocks. The boulder unit grades (fines) upward to less indurated pebble conglomerate and
conglomeratic sandstone, and variegated green, red, and white siltstone and claystone. Bedding is locally discontinuous, with
multiple minor erosional unconformities. Carbonate cement is pervasive. Local layers of primary air fall ash that are well
sorted, contain biotite crystals, and are yellow-gray to light olive brown, to gray-white.20-50 m thick. New 40Ar/39Ar ages of
ashes from near Pete Tafoya's house and 1 km southwest of Ponce de Leon springs are 34.64 ± 0.16 Ma and 27.93 ± 0.08
Ma. Interpreted as a sequence of debris flow and alluvial fan deposits derived from Sangre de Cristo Mountains and Latir
volcanic field to north and northeast (Rehder, 1986).
IPa
&ashu
Qfy
32
15
&am1
Tpl
Qt2rg Stream terrace deposits flanking Rio Grande (middle Pleistocene) - Poorly sorted silt, sand, pebbles, and boulders; clasts
primarily of granitic, metamorphic, intermediate volcanic, basalt, and sedimentary rocks; locally may contain clasts of Tertiary
Amalia Tuff; associated soils have stage III to IV calcium carbonate development, thick argillic Bt soil horizons, and 7.5YR to
10YR hues in soil Bt horizons; upper soil horizons may be affected by surface erosion; may be mantled locally by unit Qe;
modified from Kelson (1986).
10
&am1
20
&alsu
&alsu 32
&1st
4019000
&amu
20
65
Qfy
75
&cg
&ash3
&amu
89
70
36°17'30"N
12
35
35
26
4017000
&ashu
18
31
&1st
&ass5
&ashu
Qc
46
67
40
Qfu
Qf2
Qt2
25 12
79 41
Qal
&ash4
15
20
35 8
Qc
32
89
12
68
77
Qc
4020000
&am1
89
Qc
16
13
Qc
20 25
68
&am3
&als4
50
25
85
&ash4
62
&assu
24
(Ranchos de Taos): Picuris Formation, Llano Quemado breccia member (Oligocene) - Light gray to red, monolithologic
volcanic breccia of distinctive extremely angular, poorly sorted, light-gray, recrystallized rhyolite clasts in a generally redddish
matrix. Rhyolite clasts contain phenocrysts of biotite, sanidine, and quartz. Highly lithified, due to partial welding of the matrix
rather than silica or carbonate cement. Ridge-former. Unit shows both clast and matrix support. Beds are generally 1-8 m
thick. Clasts are up to 15 cm in diameter, and overall clast size decreases southward. Less than 1% of clasts are Proterozoic
slate and weathered Tertiary volcanic rocks. 5-45 m thick. Described by Rehder (1986). New 40Ar/39Ar date on sanidine from
a rhyolite clast from exposure 1 km southwest of Ponce de Leon spring is 28.35 ± 0.11 Ma. The breccia is interpreted as a
series of flows from a now-buried, nearly rhyolite vent (Rehder, 1986).
Qf4 Alluvial-fan and stream terrace deposits (late Pleistocene) - Poorly sorted silt, sand, pebbles, and boulders; associated
Qt4 soils have stage III calcium carbonate development, argillic Bt soil horizons and 10YR to 7.5YR hues in Bt horizons; clasts
primarily of granitic and metamorphic rocks north of Rio Pueblo de Taos, and granitic, metamorphic, and sedimentary rock types
south of Rio Pueblo de Taos; clasts also include basaltic rock types along Arroyo Seco and along Rio Pueblo de Taos
downstream of Los Cordovas; modified from Kelson (1986).
12
8
58
60
55
70
Qls
18
&ass5
&ss
16 Qty
59
75
Eolian deposits (late Pleistocene to Holocene) - Poorly to well-sorted sand and silt occurring primarily as a mantle or blanket;
locally contains pebbles of basalt and intermediate volcanic rock types; predominant wind direction from southwest; where unit
Qe mantles units Tb, Qt1rg, and Qt2rg, shown as units Qe/Tb, Qe/Qt1rg, and Qe/Qt2rg, respectively.
Qf3
Qt3
&ash4
70
88
45
Tpu
36°20'0"N
&assu
Qty
&
Mes
4018000
&ash4
10
24
Qc
Qfy
&ash2
&ass5
15
80
75
&am1
&ass5
15
45
41
Mes
Qe
Qfy Young alluvial-fan and stream terrace deposits (late Pleistocene to Holocene) - Poorly sorted silt, sand, pebbles, and
Qty
boulders; stage I to II calcium carbonate development; clasts primarily of quartzite, slate, schist, granite, and volcanic rock types;
includes unit Qt6 of Kelson (1986).
15
10
15
Qfy
70
&am2
10
15
57
65
Qfy
&assu 77
&ss
Qls
Playa deposits (Holocene and latest Pliestocene) - Small playa deposits located on Quaternary landslide deposits along the
northern canyon of the Rio Grande generally downstream of the village of Pilar.
&
Qc
Qfy
24
4022000
12
&am1
&ass5
20
15
Tplq
Tp
&assu
55
55
32
25
20
&ss
50
Qp
Tplq
Qtr Travertine deposits (late Pleistocene to Holocene) - Small travertine deposits that are located along faults. Travertine probably
formed along now-extinct springs.
&ash3
&ass5
&s
24 30
80
18
75
60
Qf2
&als3
25
&ss
&amu
Qty
Qfy
20
75
&ash4
30
10
85
80 75
Qty
Qfy
Qfy
Tpu
Qty
Tplq Qty
Tplq
Tpu Qf4
Qty
Qf3
Qfy
Tplq
Qf3
Tplq
85
Qfy
Tpu
Qf4
Qf2
Qf2
Qf2
Tpu
Qty
72
Tpu
45
Qf2
Tplq?
Tpl
Qfy Tpl
Qc/Tp
Qty
Qf3
Qf2
92 Tpl
30
Tplq
83
Tpl
Qf2
26
Qc
Tpu Qf1
Tpl
Tpl
Qf3
Qf3
Qf3
70
55
50
77
45
Qal
30
13
Qty Qfy Mdp Mdp
80
Qc
57 70
Qf1
Qc 55 55
87
Tpl
Tpl
Tpu
Mes
Qfo?
Qc
67
Qfu?
Qty
30
57
Tpu
45
52
Qf3
62 Qty
Qty
73
30
64
Qf2 40
43
75 75
65
Tpu
Qfy
67
Qf2
Tpu
79
Tp
Tp
70
Qty Qc/Tp
Qty
Qfo
25
15
66
65
70
Tpu
75
Qty
25
Qfy
Tpu
Tpu
75
Qc/Tpu 80
70
17 Q/Tpu
41
Tpu 80
88
Qfy
Tpu Tplq
Qc
78
30 26
58
Qfy
36
4020000
11
Qc
Qf1
36°20'0"N
24
&1st
11
21
&
Qfu
Marsh deposits (Holocene) - Silt, sand and clay in low relief, saturated flatlands; probable high organic content; primarily
between Highway 64 and Taos Pueblo, bordering Rio Lucero.
&ass5
50
18
15
Qfy
Qm
20
30
9
Qfu?
Qfy
Qf2
2
39
20
Qc
&als4
21
80
&acgu
Qfu?
Qfy
4023000
&als4
12
Qfu
af
(Taos): Colluvial mantle on slopes, undifferentiated (middle Pleistocene to Holocene) - Poorly-sorted sand, pebbles and
boulders; prevalent along bases of mountain-front facets; north of Rio Pueblo de Taos dominated by granitic lithologies and
quartzite; south of Rio Pueblo de Taos dominated by sandstone and pebble conglomerate with minor limestone clasts; not shown
in Rio Pueblo de Taos gorge in Carson and Taos SW quadrangles.
71
Qc
Qty
Qf2
30
8
Qal
Qc
10
65
13
&amu
Qfu
Stream channel and valley-floor alluvium, and active floodplains (Holocene) - Poorly to well-sorted, poorly sorted sand,
pebbles, and boulders; clasts primarily of quartzite and slate in the Carson and Taos SW quadrangles, clasts of granitic,
metamorphic, volcanic, and sandstone rock types in the Taos, Ranchos de Taos, and Los Cordovas quadrangles; with clasts
along Rio Lucero dominated by granitic lithologies and quartzite; clasts along Rio Pueblo de Taos dominated by granitic, quartzite,
and sandstone lithologies; clasts south and east of Rio Pueblo de Taos dominated by sandstone and other sedimentary rock
types.
6
19
73
27
&1st
25
44
70
Qal
4024000
33
Qfu
17
4021000
18
&ass5
83 Qt
Qfu
&
Artificial fill and disturbed ground (Recent) - Poorly sorted sand, silt and pebbles, primarily associated with drainage control
and storage facilities along piedmont east of Taos.
70
89
30
&
Qfu Qfy
Af
10
&
47
Qfu
Qf2
&als3
82
Qfu?
38
Qc/Qfy
Qfu
Cenozoic Deposits
78
20
4024000
Qt1
36°22'30"N
&
Qfu
Qfy
&am2
20
Qfy
Qfy
&am2
4025000
68 &ss
4023000
&am2
&ash2
8 Qfu?
20
Qfu
&ss
10
Qal Qfu
Qt4
&am2
20
20 &alsu 27
67
Qal
Qfy
Qty
Paul W. Bauer and Keith I. Kelson
July 2003
50
65
Qfu
455000
&amu
Qfu
Qt2
105°30'0"W
454000
26
Qal
Qty
453000
15
QfuQfy
Qal
Qal
4022000
452000
17
Qal
Qfy
Qty
105°32'30"W
451000
NMBGMR Open-file Map Series
OFGM 33
Last Modified 14 March 2006
Unit Descriptions for Taos Area Geologic Quadrangle Maps
(Carson, Taos SW, Ranchos de Taos, Taos, Los Cordovas Quads)
Xhr12 (Carson and Taos SW): Rinconada Formation, R1-R2 schist member, Hondo Group - Lower unit of fine- to medium-grained,
tan to silver, quartz-muscovite-biotite schist with small euhedral garnets (<2mm) and scattered euhedral staurolite twins (<1.5cm).
Near base are black biotite books (<2cm). Locally contains andalusite porphyroblasts up to 8 cm across. Upper unit of gray to tan,
red weathering, coarse-grained quartz-muscovite-biotite-staurolite-albite-garnet schist containing interlayers of 1-10 cm, red, gray,
or tan weathering, fine-grained muscovite-garnet quartzite. Abundant staurolites are twinned, euhedral, up to 3 cm; abundant
garnets are euhedral and small (<2mm). Strong parting along foliation plane. Sharp to gradational contact with Hr3. Lower and
upper units have previously been subdivided into R1 and R2, respectively, based on mineralogy (Nielsen, 1972). Thickness is
approximately 265 m.
Xhr
(Carson): Rinconada Formation, undivided, Hondo Group - Undivided schists and quartzites near the Pilar-Vadito fault that are
extensively fractured and faulted.
Xho
(Carson and Taos SW): Ortega Formation, Hondo Group - Gray to grayish-white, medium- to coarse-grained quartzite.
Generally massive and highly resistant to weathering. Locally well-crossbedded, with kyanite- or sillimanite-concentrated in thin,
schistose, muscovite-rich horizons. Crossbeds are defined by concentrations of black iron-oxide minerals. Common accessory
minerals are ilmenite, hematite, tourmaline, epidote, muscovite, and zircon. Gradational contact with Rinconada Formation.
Thickness is approximately 800-1200 m.
(Taos SW): Xh0r, Xh0w, Xh0s.
Xvg
Glenwoody Formation, Vadito Group - Feldspathic quartz-muscovite schist and quartzose schist exposed in cliffs southwest of
Pilar and locally along the northern flank of the Picuris Range on the west side of the Picuris-Pecos fault. White, light gray, pink, or
green. Commonly contains megacrysts of feldspar and rounded and flattened quartz in a fine-grained matrix of quartz, muscovite
and feldspar. Contact with overlying Ortega Formation is a south-dipping ductile shear zone. Pervasive extension lineation in
schist plunges south. Upper 40 m of schist is pinkish, and contains anomalous manganese and rare earth elements, and unusual
minerals such as piemontite, thulite, and Mn-andalusite (viridine). L.T. Silver reported a preliminary U-Pb zircon age of ca. 1700
Ma (Bauer and Pollock, 1993). May be equivalent to the ca. 1700 Ma Burned Mountain Formation of the Tusas Mountains.
Probably equivalent to the Glenwoody Formation of the southeast Picuris Mountains. Base unexposed; minimum thickness is
about 200 m.
Xrp
(Taos SW): Rio Pueblo Schist, Vadito Group - Feldspathic quartz-muscovite schist and quartzose schist exposed in isolated
exposures in the southeast map area, on the east side of the Picuris-Pecos fault. White, light gray, pink, or green. Commonly
contains megacrysts of feldspar and rounded and flattened quartz in a fine-grained matrix of quartz, muscovite and feldspar.
Probably equivalent to the Glenwoody Formation of the northern Picuris Mountains. Thickness unknown.
Xa
(Taos SW): Amphibolite - Includes a variety of amphibolite bodies, lenses, and layers within the Miranda granite. The predominant
rock type is fine- to medium-grained, dark gray-green to black, weakly foliated amphibolite composed of blue-green to olive-green
hornblende, interstitial quartz and plagioclase, sphene, and epidote. Faint compositional layering is formed by 1-2 mm thick white
layers. Epidote veins and zones are common.