U.S. DEPARTMENT OF THE INTERIOR

                 U. S. GEOLOGICAL SURVEY










Preliminary Geologic Map of the STORM KING MOUNTAIN

        Quadrangle, Garfield County, Colorado(1)

                                         By


GEORGE M. FAIRER, MORRIS W. GREEN, AND RALPH R. SHROBA(2)



                       Open-File Report 93-320

This report is preliminary and has not been reviewed for
conformity with U.S. Geological Survey editorial standards
or with the North American Stratigraphic Code.  Any use of
trade, product, or firm names is for descriptive purposes
only and does not imply endorsement by the U.S.  Government.
Although these data have been used by the U.S. Geological
Survey and have been successfully imported into data base
programs, no warranty, expressed or implied, is made by the
USGS as to how successfully or accurately the data can be
imported into any specific application software running on
any specific hardware platform.  The fact of distribution
shall not constitute any such warranty, and no
responsibility is assumed by the USGS in connection
therewith.

                                       1993

(1)  This database of the Storm King Mountain 7.5 minute
quadrangle, originally released as U.S Geological Survey
Open-File Report 93-320, has been updated to include a
digitized database.  The digitized version is also identifed
as OFR 93-320.  The Digital database is in ARC/INFO Format.
Although this database has been subjected to rigorous review
and is substantially complete, the USGS reserves the right
to revise the data pursuant to further analysis and review.
Furthermore, it is released on condition that neither the
USGS nor the United States Government may be held liable for
any damages resulting from its authorized or unauthorized
use.
     This digital geologic map does not include a digital
(DRG) topographic data file as it is currently unavailable.
When the DRG database becomes available it can be combined
with the geologic database.
     The geologic database can be downloaded via 'anonymous
ftp' from a USGS system named greenwood.cr.usgs.gov
(136.177.48.5).  The files are located in a directory named
/pub/open-file-reports/ofr-93-320.

The database manager is: Ralph R. Shroba
                         (303) 236-1293
                         U.S. Geological Survey
                         Box 25046, Mail Stop 913
                         Denver, CO 80225

     This geologic map was prepared as part of a study of
digital methods and techniques as applied to complex
geologic maps.  The geologic map was digitized from the
original greenline sheets used to prepare the published
Open-File map of the Storm King Mountain quadrangle (Fairer
and others, 1993).  Consequently, the digital version is at
1:24,000 scale using the Polyconic map projection parameters
of the topographic base map.  Stable base contact prints of
the greenline sheets were digitized on a Calcomp 9500 using
GSMAP (Selner and Taylor, 1993) software running on a ACMA
486 Personal Computer.  The files were converted to ARC/INFO
format using GSMGIS software.  These files were transferred
to a Sun SPARCstation 20 computer where they were then
loaded into ARC/INFO.  Each vector and polygon was given
attributes derived from the original 1993 geologic map using
ALACARTE (Wentworth and Fitzgibbon, 1991) software.
     This database was developed on a SPARCstation 20
computer system using ARC/INFO 7.0.2 software.  The lineset
and shadeset files are coded for a HP DesignJet 650C plotter
using HPGL2 software.

List of files:
     alcgeol.e00(a)     symbol set
     alcwrg.e00(a)   line set
     ctr269.e00(b)   shade set
     fnt003.e00(c)   font set
     loadsk.aml      load program
     loess.e00       shade set
     mapbar.aml(b)   mapbar program
     sk.box          index box program
     sk.text         index text
     sk5.e00         line and polygon data set
     skex.eml        map assembly program
     skl.e00         loess polygon data set
     sklb.box        loess index box program
     skst1.e00       structure data set
     skstr.e00       structure data set
     wyo.e00(c)      text set
     sk.doc          text (this file)
     README.SK       readme text
     seals.e00(c)    logo polygon set

     (a) T.T. Fitzgibbon
     (b) W.R. Beaman
     (c) G.R. Green

     The authors acknowledge the assistance of G.N. Green in
preparation of the digitized version of this geologic map.

Line Types and Attributes

     Line Types             ALCWRG
     Contact, certain         25
     Contact, concealed       29
     Normal fault, certain    1
     Normal fault, inferred   3
     Normal fault, concealed  5
     Anticline                31
     Syncline                 31
     Monocline                31
     Water boundary           25
Polygon Types and Attributes

     P-types                ALCWRG
     af                       24
     Qfp                      8
     Qfy                      1
     Qty                      38
     Qto                      34
     Qtt                      40
     Qfo                      217
     Qp                       218
     Qti                      220
     Qac                      3
     Qc                       2
     Qsw                      5
     Qls                      4
     Qta                      36
     Qlo                      37
     Tcc                      11
     Tb                       57
     Tw                       62
     Kmv                      78
     Km                       80
     Kd                       82
     Jm                       223
     Je                       224
     Trc                      235
     PIPsb                    236
     PIPm                     228
     IPe                      234
     IPb                      240
     Ml                       248
     DOCu                     110
     Cs                       119
     XY                       249

(2) Denver, Colorado

Preliminary Geologic Map of the Storm King Mountain
Quadrangle, Garfield County, Colorado
By George M. Fairer, Morris W. Green, and Ralph R. Shroba

CORRELATION OF MAP UNITS

Refer to non-digitized version of this open-file report for
a diagram showing correlation of map units

DESCRIPTION OF MAP UNITS

[Surficial deposits shown on the map are estimated to be at
least 3 ft thick.  Fractional map symbols (for example,
Qlo/Qto) are used where loess mantles older surficial
deposits and the underlying deposits have been identified.
Thin, discontinuous colluvial deposits, residual material on
bedrock, and some of the artificial fills were not mapped.
Also not mapped are four elongate areas above mined coal
beds on the north side of the Grand Hogback, near Coal Ridge
and Horse Mountain, where the ground surface is highly
oxidized, fractured, and prone to subsidence (Stover and
Soule, 1985).  Divisions of Pleistocene time correspond to
those of Richmond and Fullerton (1986).  Age assignments for
surficial deposits are based chiefly on the degree of
modification of original surface morphology, height above
stream level, and degree of soil development.  Soil-horizon
designations are those of the Soil Survey Staff (1975) and
Guthrie and Whitney (1982).  Most of the surficial deposits
are calcareous and contain different amounts of primary and
secondary calcium carbonate; stages of secondary calcium
carbonate morphology are those of Gile and others (1966).
Grain sizes given for surficial deposits are based on visual
estimates and follow the modified Wentworth grade scale
(American Geological Institute, 1982).  In descriptions of
surficial map units, the term clasts refers to the fraction
greater than 0.08 in. (2 mm) in diameter, whereas the term
matrix refers to the finer material.  Dry matrix colors of
the surficial deposits were determined by comparison with
Munsell Soil Color Charts (Munsell Color, 1973).  The colors
of the surficial deposits correspond to those of the
sediments and(or) bedrock from which they were derived.
Surficial deposits derived from non-red sediments and
bedrock are commonly light brownish gray (2.5Y 6/2), pale
yellow (2.5Y 7/4), light gray (10YR 7/2), very pale brown
(10YR 7/3, 8/3, 7/4, and 8/4), pale brown (10YR 6/3), light
yellowish brown (10YR 6/4), light brown (7.5YR 6/4), and
pink (7.5YR 7/4).  Those derived from red sediments and
bedrock are commonly light reddish brown (5YR 6/4 and 2.5YR
6/4), reddish brown (5YR 5/4 and 2.5YR 5/4), reddish yellow
(5YR 6/6), light red (2.5YR 6/6), and red (2.5YR 5/6).]
manmade deposits-Earth and rock fragments placed in the
former channel of the Colorado River

af    Artificial fill (latest Holocene)--Compacted fill
material composed mostly of silt, sand, and rock fragments.
Mapped only in the former channel of the Colorado River
beneath segments of Interstate 70 and beneath the nearby
tracks of the Denver and Rio Grande Western Railroad.  The
unit locally includes small areas of flood plain and stream-
channel deposits (Qfp), young fan alluvium (Qfy), young
terrace alluvium (Qty), and colluvium (Qc).  Thickness
generally less than 30 ft

alluvial deposits-Silt, sand, and gravel in flood plains,
stream channels, and terraces along the Colorado River and
its major tributaries, in alluvial fans on flood plains and
terraces, and in pediment deposits on gently sloping
surfaces cut on bedrock

Qfp   Flood-plain and stream-channel deposits (Holocene and
late Pleistocene)--Chiefly clast-supported, slightly
bouldery, pebble- and cobble-gravel in a sand matrix that is
locally overlain by gravelly sand to sandy silt.  Poorly to
moderately well sorted and poorly to well bedded.  Clasts
are commonly subangular to rounded; their lithologies
reflect those of the bedrock in the upstream areas.  The
unit occurs along the Colorado River and along Canyon Creek
upstream of the terminal moraines (unit Qti).  Low-lying
areas are prone to periodic flooding.  Deposits along Canyon
Creek may contain more sand and silt than those along the
Colorado River.  The unit locally includes small alluvial-
fan deposits (Qfy), low terrace deposits that are commonly
less than 15 ft above modern stream level, and sheetwash
deposits (Qsw), and locally may include some organic-rich
deposits.  The upper part of the unit may be a complex of
cut-and-fill deposits of Holocene and late Pleistocene(?)
age.  The lower part of the unit is probably equivalent, at
least in part, to  the younger terrace alluvium (Qty).  The
unit is tentatively correlated with deposits in terrace T8
of Piety (1981) along the Roaring Fork River between
Glenwood Springs and Carbondale, Colo.  Thickness along the
Colorado River greater than 45 ft near the western
quadrangle boundary (Colorado Highway Department,
unpublished data); maximum thickness along the Colorado
River may be about 60 ft; maximum thickness along Canyon
Creek may be 80 ft or more

Qfy   Younger fan alluvium (Holocene and latest
Pleistocene)--Mostly poorly sorted, clast- and matrix-
supported, slightly bouldery, pebble- and cobble-gravel in a
silty sand matrix, and locally pebbly and cobbly silty sand
that contains thin (5-20 in.) lenses of sand, pebble gravel,
and cobbly pebble gravel.  Deposits derived from the Mancos
Shale (Km) have a clayey silt matrix that is sticky when it
is wet and has prominent shrinkage cracks when dry.  Some of
these deposits may contain expansive clays and have high
shrink-swell potential.  The unit locally contains boulders
as long as 6 ft; some of the larger boulders were probably
deposited by debris flows.  Nonbedded to poorly bedded; beds
are commonly less than 3 ft thick.  Clasts are commonly
angular to subangular sandstone north of the Colorado River
and angular to subangular sandstone, angular to subrounded
basalt, and locally angular to subangular shale and
siltstone south of the Colorado River.  The unit is
undissected and was deposited chiefly by small intermittent
streams graded to the flood plains of modern streams (Qfp)
and to the tops of terraces that are underlain by younger
terrace alluvium (Qty).  Locally includes valley-fill
deposits of intermittent streams, debris-flow deposits,
sheetwash deposits (Qsw), and colluvium (Qc).  Exposed
thickness 10-60 ft; maximum thickness probably about 80 ft

Qty   Younger terrace alluvium (late Pleistocene)--Stream
alluvium that underlies terrace remnants that are about
40 ft above the Colorado River.  The unit consists mostly of
a poorly sorted, clast-supported, slightly bouldery, pebble-
and cobble-gravel in a sand matrix.  Where deposited by
minor tributary streams, the upper part of the unit commonly
consists of poorly sorted, clast-supported, bouldery,
pebble- and cobble-gravel in a sand matrix that is overlain
by about 3 ft of pebbly sand.  Clasts in the lower part of
the unit are commonly subrounded to rounded and are derived
from a variety of sedimentary, igneous, and metamorphic
rocks in the upstream areas.  Near the mouth of South Canyon
Creek, clasts in the upper part of the unit are mostly
sandstone and a minor amount of siltstone and basalt.  The
unit is commonly overlain by about 3-10 ft of loess (Qlo)
and by younger fan alluvium (Qfy).  Unit Qty is probably
equivalent in part to outwash of the Pinedale glaciation,
which is about 12-35 ka (Richmond, 1986, chart 1A).  Much of
the glacial outwash along Canyon Creek and East Canyon Creek
is buried by younger fan alluvium (Qfy) and is probably of
Pinedale age.  Unit Qty is tentatively correlated with
deposits in terraces T7 and T6 of Piety (1981) along the
Roaring Fork River between Glenwood Springs and Carbondale,
Colo., and with deposits in terraces A and B of Bryant
(1979) farther upstream between Woody Creek and Aspen, Colo.
Exposed thickness 40 ft; maximum thickness possibly about
130 ft

Qto   Older terrace alluvium (middle Pleistocene)--Stream
alluvium that underlies terrace remnants about 130 ft above
the Colorado River.  The unit mostly is a poorly to
moderately well-sorted, clast-supported, bouldery, pebble-
and cobble-gravel and cobbly pebble gravel in a sand matrix
that is overlain by about 15-30 ft of sand and pebbly sand.
Locally thin beds of sandy pebble gravel near the base of
the unit are cemented by fine-grained calcium carbonate.
Clasts are chiefly subrounded to rounded sandstone, gneiss,
quartzite, basalt, granodiorite(?), limestone, and dolomite
deposited by the Colorado River and by Canyon Creek near its
confluence with the Colorado.  Alluvium along the Colorado
upstream of the confluence of Canyon Creek contains abundant
basalt boulders, some of which are as long as 6 ft  The unit
is locally mantled by 8-12 ft of loess (Qlo) and by older
fan alluvium (Qfo).  The morphologic development of the soil
that is formed in the top of the unit and locally in the
lower of two loess sheets that locally mantle the unit in
the adjacent New Castle 7-minute quadrangle (Green and
others, 1993) suggests that unit Qto is of Bull Lake age
(Shroba, 1989) and may be about 140-150 ka (Pierce and
others, 1976; Pierce, 1979) or about 130-300 ka (late middle
Pleistocene; Richmond, 1986, chart 1A).  The unit is
tentatively correlated with deposits in terraces T5 and T4
of Piety (1981) along the Roaring Fork River between
Glenwood Springs and Carbondale and with deposits in terrace
C of Bryant (1979) farther upstream between Woody Creek and
Aspen.  Exposed thickness 60 ft, maximum thickness possibly
about 130 ft

Qtt   Oldest terrace alluvium (middle Pleistocene)--Stream
alluvium that underlies small terrace remnants that are
about 220 and 300 ft above the Colorado River downstream of
its confluence with Canyon Creek.  The unit is mostly a
poorly sorted, clast-supported, slightly bouldery, pebble-
and cobble-gravel in a sand matrix.  It locally consists of
thin (5-15 in.) lenses and beds of sandy silt, silty sand,
and sandy pebble gravel.  The unit locally grades upward
into about 20 in. of moderately well-sorted, clast-
supported, pebble gravel in a sand matrix that is overlain
by about 20-40 in. of slightly pebbly sand.  Clasts are
mostly subrounded to rounded and are derived from a variety
of sedimentary, igneous, and metamorphic rocks in the
upstream areas.  Many pebbles and cobbles of biotite-bearing
rocks in the upper part of the unit are weathered to gruss.
A stage III K soil horizon is locally present in the top of
the unit.  The unit is mantled by 6-13 ft of loess (Qlo) and
locally by about 15-30 ft of sandstone-rich older fan
alluvium (Qfo), which is overlain by loess.  The loess
mantle locally consists of two or more sheets.  The unit may
be correlative in part with other terrace deposits within
30 mi of the quadrangle that contain or are overlain by the
620 ka Lava Creek B volcanic ash.  The ash is about 300 ft
above the Colorado River near the east end of Glenwood
Canyon (Izett and Wilcox, 1983), about 290 ft above the
Crystal River near Carbondale, (Piety, 1981) and about
260-280 ft above the White River near Meeker, Colo. (J.W.
Whitney, U.S. Geological Survey oral commun., 1992; Whitney
and others, 1983).  The unit is tentatively correlated with
deposits in terraces T3 and T2 of Piety (1981) along the
Roaring Fork River between Glenwood Springs and Carbondale,
and with deposits in terrace D of Bryant (1979) farther
upstream between Woody Creek and Aspen.  Exposed thickness
20-30 ft; maximum thickness possibly about 80 ft

Qfo   Older fan alluvium (late and middle Pleistocene)--
Mostly poorly sorted, clast- and matrix-supported, slightly
bouldery, pebble- and cobble-gravel in a silty sand matrix,
sandy pebble gravel, and pebbly sand.  Clasts are chiefly
angular to subangular sandstone and locally shale and
siltstone.  Poorly bedded; commonly contains discontinuous
beds and lenses.  Unit underlies slightly dissected surfaces
along the Colorado River that are mantled by about 3-10 ft
of loess (Qlo).  Deposited by Baldy Creek and small
intermittent streams graded to the tops of terrace remnants
composed of old terrace alluvium (Qto and Qtt).  Locally
includes valley-fill deposits of intermittent streams,
debris-flow deposits, sheetwash deposits (Qsw), and
colluvium (Qc).  Exposed thickness 3-25 ft; maximum
thickness possibly about 80 ft

Qp    Pediment deposits (middle Pleistocene)--Gravelly
alluvium and debris-flow deposits at two levels that overlie
gently sloping surfaces cut on Mancos Shale (Km) north of
the Colorado River, near the western quadrangle boundary.
Mostly poorly sorted, clast-supported, bouldery, pebble- and
cobble-gravel in a sandy silt matrix and poorly sorted,
cobbly sandy pebble gravel to pebbly silty sand.  Clasts are
chiefly angular to subrounded sandstone.  The unit probably
consists of alluvium, debris-flow deposits, sheetwash
deposits (Qsw), and colluvium (Qc).  Nonsorted, bouldery,
debris-flow(?) deposits are common in the upper part of the
unit.  Some of the sandstone boulders in the unit are as
long as 6 ft.  A stage III K soil horizon is locally formed
in the top of the unit.  The bedrock beneath the unit is
locally slightly oxidized to a depth of 10 ft or more.  The
unit is dissected and is mantled by about 6-13 ft of loess
(Qlo), which locally consists of two or more sheets.  A
reddish-yellow (5YR 6/6) argillic B horizon is locally
present in the top of the basal loess sheet.  The lower
limits of the pediment deposits are about 280 and 360 ft
above the Colorado River.  The lower pediment deposit
appears to be graded to a terrace remnant of the oldest
terrace alluvium (Qtt) in the adjacent New Castle 7-minute
quadrangle.  Exposed thickness commonly 6-10 ft; maximum
thickness possibly about 50 ft

Glacial deposits--Ice-deposited silt, sand, and gravel in
moraines near the junction of Canyon Creek and East Canyon
Creek

Qti   Till (late and middle Pleistocene)--Gravelly deposits
that typically form steep-sided, bouldery, hummocky lateral
and end moraines and ground moraine near the junction of
Canyon Creek and East Canyon Creek.  The unit is mostly an
unstratified, unsorted, matrix- and locally clast-supported,
slightly bouldery, pebble- and cobble-gravel in a matrix of
slightly silty, poorly sorted sand.  Clasts are mostly
angular to rounded and include gneiss, schist, fine-grained
metasedimentary rocks (greenstone (?) of Bass and Northrop,
1963), dolomite, limestone, quartzite, sandstone, and
basalt.  A few dolomite clasts are soled and striated.
Boulders of Precambrian rocks on the moraines are as long as
24 ft.  Closed depressions surrounded by low ridges are
common on the terminal moraines.  The closed depressions are
probably partly filled by unmapped loess (Qlo) or loess-
derived sheetwash deposits (Qsw).  The map unit is locally
overlain by young fan alluvium (Qfy), loess (Qlo), sheetwash
deposits (Qsw), landslide deposits (Qls), and talus deposits
(Qta); and it may locally include deposits of stratified
drift.  Terminal moraines in the valley of Canyon Creek are
well preserved and are narrowly breached by stream erosion,
whereas those in the valley of East Canyon Creek were
modified or were removed by stream erosion and landsliding.
The lower limit of glaciation is at an altitude of about
5900 ft along Canyon Creek.  Much of the unit is probably of
Pinedale age (about 12-35 ka, Richmond, 1986, chart 1A);
although some of the outermost glacial deposits near the
junctions of Canyon and Bearwallow Creeks and East Canyon
and Possum Creeks, are probably of Bull Lake age (about 140-
150 ka; Pierce and others, 1976 and Pierce, 1979 or about
130-300 ka; Richmond, 1986, chart 1A)and some of them may be
of pre-Bull Lake age.  Exposed thickness 3-30 ft, maximum
thickness possibly about 500 ft in the large lateral moraine
on the west side of Canyon Creek

Alluvial and colluvial deposits-Sand and gravel in flood
plains and small alluvial fans along minor tributary
streams, and sheets of pebbly sand that locally overlie
alluvial deposits in valley bottoms and mantle the adjacent
valley sides and hill slopes

Qac   Undivided alluvium and colluvium (Holocene and late
Pleistocene)--Chiefly undifferentiated flood plain and
stream-channel deposits (Qfp), young fan alluvium (Qfy), and
colluvial debris-flow (Qc) and sheetwash  (Qsw) deposits.
The alluvium typically consists of interbedded sand, pebbly
sand, and pebble gravel and ranges from thin-bedded
(0.2-6 in.) clayey, silty sand to thick-bedded (>3 ft),
poorly sorted, clast- and matrix-supported, slightly
bouldery, pebble- and cobble-gravel in a sand matrix.

Sheetwash deposits are typically pebbly silty sand.
Deposits derived from Mancos Shale (Km) commonly contain
more silt and clay than those derived from the other bedrock
units.  Some of the deposits derived from the Mancos may
contain expansive clays and have high shrink-swell
potential.  Alluvial deposits form flood plains, low
terraces, and small alluvial fans along small perennial
streams and some of the larger intermittent streams that are
tributary to the Colorado River.  Sheetwash deposits locally
mantle the valley bottoms and the adjacent valley sides and
hill slopes.  Exposed thickness of the alluvium 3-30 ft;
maximum thickness probably about 40 ft.  Exposed thickness
of the colluvium 3-6 ft; maximum thickness probably about
15 ft.  The post-glacial sediments, which accumulated above
the lateral moraine that dams the south end of the valley of
Bearwallow Creek, may be as much as about 300 ft thick and
may include some lacustrine deposits

Colluvial deposits-Silt, sand, and gravel on valley sides
and hill slopes that were mobilized, transported, and
deposited by gravity and sheet erosion

Qc    Colluvium, undivided (Holocene and late Pleistocene)--
Mostly clast-supported, pebble-, cobble-, and boulder-gravel
in a silty sand matrix, and gravelly, silty sand, sandy
silt, and clayey silt.  Deposits derived from the Mancos
Shale (Km) commonly contain more silt and clay than those
derived from the other bedrock units.  Some of the deposits
derived from the Mancos Shale and shale in the Morrison
Formation (Jm) and Mesaverde Group (Kmv) may contain
expansive clays and have high shrink-swell potential.
Typically unsorted to poorly sorted and unstratified to
poorly stratified.  Clasts are typically angular to
subrounded; their lithologic composition reflects that of
the bedrock and(or) the surficial deposits from which the
colluvium was derived.  The unit locally includes sheetwash
(Qsw) creep, debris-flow, and landslide (Qls) deposits that
are too small to map separately or that lack distinctive
surface morphology and could not be distinguished in the
field or on aerial photographs.  The map unit also locally
includes thin loess (Qlo) mantles on older gently sloping
colluvial deposits, small deposits of alluvium and colluvium
(Qac) in and along minor drainageways, and probably small
pediment deposits (Qp) on the north side of the Grand
Hogback.  Exposed thickness 6-13 ft; maximum thickness
probably about 15 ft

Qsw   Sheetwash deposits (Holocene and late Pleistocene)--
Mostly pebbly, silty sand and sandy silt that are derived
chiefly from weathered bedrock and loess (Qlo) by sheet
erosion.  Common on gentle to moderate slopes in areas
underlain by the Wasatch Formation (Tw).  The unit locally
includes small deposits of loess (Qlo) and undivided
alluvium and colluvium (Qac) in and along minor
drainageways; may locally include creep (colluvium, Qc) and
alluvial-fan (Qfy) deposits.  Exposed thickness 6-15 ft;
maximum thickness probably about 30 ft

Qls   Landslide deposits (Holocene and late Pleistocene)--
Chiefly unsorted and unstratified rock debris characterized
by hummocky topography.  Many of the landslides were complex
(Varnes, 1978) and commonly formed on unstable slopes that
are underlain by the Eagle Valley Evaporite (IPe), Maroon
Formation (PIPm), Mancos Shale (Km), and Wasatch Formation
(Tw).  The younger deposits are commonly bounded upslope by
crescentic headwall scarps and downslope by lobate toes.
The unit includes debris-slide, rock-slide, debris-slump,
slump-earth-flow, earth-flow, and debris-flow deposits
(Varnes, 1978).  The sizes and lithologies of the clasts and
the grain-size distributions of the matrices of these
deposits reflect those of the bedrock units and surficial
deposits that were displaced by sliding.  Deposits derived
from the Mancos may contain expansive clays and have high
shrink-swell potential.  Deposits derived from the Eagle
Valley Evaporite are prone to hydrocompaction and subsidence
owing to the dissolution of gypsum, anhydrite, and halite.
The unit locally includes sheetwash (Qsw), creep, and
debris-flow (colluvium, Qc) deposits.  Exposed thickness
6-15 ft; maximum thickness possibly 150 ft

Qta   Talus deposits (Holocene and late Pleistocene)--
Chiefly unsorted, crudely stratified, angular, cobbly and
bouldery rubble on steep slopes below bedrock outcrops in
the northern part of the quadrangle.  The matrix is mostly
sand and silt; some of the matrix in the older deposits may
be of eolian origin.  The upper part of the unit locally
lacks matrix.  The unit probably includes minor deposits of
colluvium (Qc).  Small talus deposits in the valleys of
Canyon, East Canyon, and Possum Creeks were not mapped.
Maximum thickness probably about 50 ft
Eolian deposits-Wind-deposited sand, silt, and clay that
mantles level to gently sloping surfaces

Qlo   Loess (late and middle ? Pleistocene)--Wind-deposited,
nonstratified, friable, slightly plastic to plastic,
slightly clayey, sandy silt and silty sand.  The unit may
locally include minor deposits of clayey silt.  The grain-
size distribution of slightly weathered loess in and near
the quadrangle is about 23 percent sand, 55 percent silt,
and 17 percent clay (Harmon and Murray, 1985, tables 13 and
14).  Most of the sand-size particles are very fine and
fine.  The unit is prone to sheet erosion, gullying, and
compaction when wet.  Locally includes some loess-derived
sheetwash (Qsw) and creep (colluvium, Qc) deposits.
Deposited during two or more episodes of eolian activity.
Deposition may have continued into Holocene time.  Probably
derived chiefly from flood plain sediments of the Colorado
River and its major tributaries and possibly in part from
(1) outcrops of Tertiary siltstone and mudstone in the
Piceance Basin west of the quadrangle (Tweto, 1979) and
(2) large areas of exposed sandstone in the Canyonlands
region in southeastern Utah (Whitney and Andrews, 1983).
The mapped distribution of loess is approximate, because it
lacks distinct topographic expression.  The unit commonly
mantles level to gently sloping surficial deposits that are
older than the younger fan alluvium (Qfy).  Younger terrace
alluvium (Qty) is mantled by one loess sheet, older terrace
alluvium (Qto) is locally mantled by two loess sheets, and
pediment deposits (Qp) and the oldest terrace alluvium (Qtt)
are locally mantled by two or more loess sheets.  The soil
that is formed in the upper loess sheet on the older terrace
alluvium commonly consists of the following sequence of
horizons:  A/Bw/Bt/Bk.  The soil that is formed in the lower
loess sheet on the older terrace alluvium contains more clay
and calcium carbonate than the soil in the upper loess sheet
and commonly consists of the following sequence of horizons:
Bw/Btk/K/Bk.  Where the upper loess sheet is composed of
silty sand, the soils have weakly developed, non-prismatic
argillic B horizons.  Exposed thickness 6-13 ft

Tcc   Conglomerate on Canyon Creek (Miocene ?)--Mostly
poorly sorted, clast- and locally matrix-supported, cobbly
pebble gravel in a sand matrix that is locally cemented by
fine-grained calcium carbonate.  Contains subangular to
subrounded clasts derived from the Maroon Formation (PIPm)
and older bedrock units.  Lithologies include red sandstone,
quartzite, limestone, and chert as well as red siltstone and
igneous and metamorphic rocks reported by Bass and Northrop
(1963).  Much of the unit may be fan alluvium deposited by
former streams flowing from the south flank of the White
River Plateau.  The conglomerate on the north flank of Storm
King Mountain is slightly better sorted and contains fewer
cobbles than the conglomerate near Canyon Creek.  Because
the conglomerate on Storm King Mountain lacks clasts younger
than the Maroon Formation, it is mapped with the
conglomerate on Canyon Creek rather than as a high-level
deposit of the ancestral Colorado River.  Near Canyon Creek,
the unit is steeply folded in a west-northwest-trending
syncline that may have formed as a result of the dissolution
and subsidence of the underlying Eagle Valley Evaporites
(IPe) (Bass and Northrop, 1963) or possibly late Cenozoic
(post 10 Ma) differential movement associated with the
renewed uplift of the White River Plateau (Larson and
others, 1975).  The western limit of the unit may extend as
much as 3 mi beyond the western limit shown on the map.  The
unit was named by Bass and Northrop (1963) for outcrops
along Canyon Creek in the Storm King Mountain quadrangle and
was subsequently mapped as Browns Park Formation (Miocene)
by Tweto and others (1978).  Estimated thickness about
200 ft (Bass and Northrop, 1963)

Tb   Basalt (Miocene)--Multiple(?) flows of alkali basalt
and basaltic andesite (Larson and others, 1975).  Unit may
locally include interbedded siltstone and sandstone of the
Browns Park Formation(?) (Larson and others, 1975).  Cut by
northwest-trending faults in the southeastern part of the
quadrangle and caps Horse Mountain in the south-central part
of the quadrangle.  The top of the unit is as much as
2,900 ft about the Colorado River, and 2,700 ft above the
Roaring Fork River in the adjacent Glenwood Springs
7.5-minute quadrangle.  Mapped as unit Tv2 by Larson and
others (1975), who report whole-rock K-Ar ages of 9-14 Ma
for the unit.  The uppermost flow of a three(?)-flow
sequence of unit Tv2 on Lookout Mountain, about 6 mi east of
the eastern quadrangle boundary, yielded a whole-rock K-Ar
age of 10.10.5 Ma (Larson and others, 1975).  Unit thickens
southward toward its possible source near Sunlight Peak
(Bass and Northrop, 1963; Larson and others, 1975, fig. 6),
about 5 mi south of the southern quadrangle boundary.
Estimated maximum thickness in the Storm King Mountain
quadrangle about 160 ft

Tw    Wasatch Formation (Eocene to Paleocene)--Interbedded,
variegated reddish-brown, reddish-purple, yellowish-brown,
tan, and white conglomerate, conglomeratic sandstone,
sandstone, siltstone, mudstone, and claystone unconformably
overlying Mesaverde Group rocks. Sediment is first cycle,
poorly sorted, and contains an abundance of metamorphic and
granitic rock fragments; locally includes a basal cobble
conglomerate as much as about 50 ft thick, designated the
Ohio Creek Conglomerate by Bass and Northrop (1963, p.J58).
Coarse clastic beds are trough crossbedded and vary in
thickness, whereas fine-grained clastic beds are commonly
thin.  All beds are laterally discontinuous and, in general,
are lenticular; overall, the sequence fines upward.  About
5000 ft thick
                Deposition of sediments occurred in a high-
energy stream-dominated fluvio-lacustrine depositional
setting during the initial phase of sedimentary infill of
the Piceance basin as it formed during the Laramide orogeny.
Sediments were derived form multiple source areas within the
present Rocky Mountains as they were uplifted during the
orogeny.  Braided-stream and flood plain deposition
dominated as the primary means of sediment transport and
deposition.  Differentiation of sediment into more discrete
lithofacies within alluvial complexes was hindered by the
relatively short distances from sediment source to
depocenters in the basin and the apparent large volume of
sediment.

Kmv   Mesaverde Group rocks undivided (Upper Cretaceous)--
Thin and thick beds of yellowish-brown and olive-gray
carbonaceous mudstone interbedded with fine- to medium-
grained silty sandstone, siltstone, and claystone; contains
thin beds and pockets of silty and sandy pebble- and cobble-
conglomerate; beds are generally massive.  Locally
interbedded with thin beds (seams) and laminations of coal;
clinker is common.  Contains several beds of white, well-
sorted, short forset-crossbedded, quartzose sandstone in the
lower part which contrasts strongly in appearance and
physical character with surrounding silty carbonaceous beds.
Except for white sandstone beds, in clastic sediments are
generally poorly sorted, subangular, quartzose, and occur
with an appreciable quantity of particulated coaly
carbonaceous material; some beds are silica cemented; beds
form prominent ridges and cliffs.  About 5000 ft thick
                Deposition occurred during the first major
Cretaceous regressive marine cycle in the Rocky Mountain
seaway following the Dakota transgressive cycle.  Mesaverde
deposition occurred dominantly in backshore areas and on
deltas of the lower coastal plain where sediment-laden
streams meandered between coal swamps, marshes, and mudflats
behind a seaward-migrating shoreline.  White sandstone beds
preserved in the lower part of the sequence are the product
of shoreline processes at the beach where surf- and wave-
zone fluvial activity winnowed, sorted, and otherwise
concentrated sand-sized particles.
                Mineable coal beds (not mapped) in the
Mesaverde occur in three zones in the map area; the lower
zone consists of the Wheeler, D, and Allen coal beds located
approximately at 900, 985, and 1500 ft, respectively, above
the base of the unit.  The middle zone consists of the C, B,
and A coal beds located approximately at 2200, 2245, and
2330 ft, respectively, above the base of the unit.  The
upper zone consists of a single bed, the Keystone coal bed,
located at about 3900 ft above the base of the unit (Gale,
1910; Bass and Northrop, 1963, p.J57).

Km    Mancos Shale (Upper Cretaceous)--Dominantly light- to
dark-gray carbonaceous shale locally containing thin
lenticular beds of dark-gray and black fossiliferous (mainly
fragmented) limestone and thin-bedded, very fine grained
silicious silty sandstone; sediments of the Mancos Shale are
generally limy.  The formation contains white to yellowish-
brown bentonite horizons (altered volcanic ash) a few inches
thick.  The upper and lower formation contacts of the Mancos
are conformable. Unit about 5,500 ft thick.  Generally
underlies floors of valleys where it commonly is poorly
exposed beneath Quaternary surficial deposits.
                Deposition occurred primarily on the
continental slope in transgressive (lower part of the
sequence) and regressive (upper part of the sequence)
submarine environments. Clastic deposition occurred by
sediment settling and turbidity flow, whereas limestone
formed by chemical precipitation.  The dark-gray and black
color of the rocks is attributed largely to the content of
black coaly detrital organic matter apparently derived from
the destruction of pre-Dakota coaly carbonaceous swamp
deposits on the lower coastal plain by high-energy
transgressive shoreline processes.

Kd    Dakota Sandstone (Lower Cretaceous)--Yellowish-brown,
medium- to coarse-grained, massive to crossbedded, quartzose
sandstone containing pockets and lenses of gray chert-pebble
and chert-cobble  conglomerate; interbedded with dark-gray
to black carbonaceous sandy siltstone and mudstone.
Sandstone is commonly well sorted, angular, and well
cemented with silica; forms prominent cliffs.  Contact with
underlying Morrison Formation is unconformable; contact with
overlying Mancos Formation is conformable and locally
intertongueing.  About 175 ft thick
                Deposition occurred on a lower coastal
plain, at or near the shoreline, and in shallow marine
embayments in a transgressive coastal setting.  Sandstone
and conglomerate were deposited in broad, distributary
fluvial channels in which fluvial currents and, locally,
offshore currents, influenced the structure and distribution
of sand bodies.  Intervening carbonaceous siltstone was
deposited in mudflats, bays, and estuaries adjacent to the
shoreline and in interfluvial areas adjacent to distributary
channels in backshore areas.  Much silt and carbonaceous
material deposited in shallow water embayments and estuarie
environments as well as farther seaward, may have been
derived from the destruction of backshore swamp and marsh
deposits as the high-energy shoreline environment migrated
landward during the Dakota transgressive cycle.

Jm    Morrison Formation (Upper Jurassic)--Medium- to light-
green and maroon shale and mudstone and thin beds of silty
sandstone (mainly in lower part) and dark-gray limestone.
Sand fraction is mainly clear, gray, and white quartz
grains; but, green, gray, and brown chert grains are common.
Beds are thin and lenticular.  About 500 ft thick
                Deposition occurred in a lacustrine-
dominated fluvio-lacustrine depositional setting.  In the
map area, the formation is a single lithofacies of a large
fluvio-lacustrine system present throughout much of the
Colorado Plateau and western interior of the United States.

Je    Entrada Sandstone (Upper Jurassic)--Light-orange,
medium- to very fine grained, well-sorted, crossbedded
sandstone; sand grains are subrounded to well rounded and
consist mainly of quartz.  Contact with overlying Morrison
Formation is sharp and conformable; contact with underlying
Chinle Formation is unconformable.  About 90 ft thick
                Crossbed sets are large scale and apparently
were formed by eolian activity in large, laterally
extensive, dune fields.  The basal few inches of the
formation commonly consists of a layer of coarse-grained
sand- and pebble-sized clasts of variegated chert and
quartz.  This layer apparently formed as a lag concentrate
by wind deflation on the erosion surface developed on top of
the underlying Chinle Formation.  The formation is present
throughout much of the Colorado Plateau and western interior
of the United States.

TRc   Chinle Formation (Upper Triassic)--Thinly and even-
bedded red beds composed of shale and siltstone and thin
beds of limestone and limestone-pebble conglomerate.  Shale
and siltstone are dark reddish brown to reddish orange;
limestone and limestone-pebble conglomerate are light
purplish red and gray.  Shale and siltstone locally exhibit
ripple marks and mudcracks.  Contact with the State Bridge
Formation below is gradational; contact with the Entrada
Sandstone above is unconformable.  About 300 ft thick
                Grain-size of clastic units, primary
sedimentary structures, and the presence of limestone-pebble
conglomerate, suggest that deposition occurred in relatively
shallow, seasonally dry, lacustrine depositional settings
within large interfluvial areas (flood plains) or in broad
shallow lakes which occupied the central part of the
sediment-filled Eagle basin.  The lack of coarse-grained,
bed-load clastic sediment in association with the formation
is characteristic.  The formation is present throughout the
southwestern United States and is represented in the map
area by only a part of the distal, fine-grained lithofacies
of the formation.

TRPsb  State Bridge Formation--(Lower Triassic? and Permiam)
Thin uniform beds of brick-red, reddish-brown, light-gray,
and green and greenish-gray micaceous siltstone and shale
interbedded locally with medium- to fine-grained crossbedded
sandstone and thin beds of gypsum/anhydrite. Unit grades
vertically into underlying and overlying formations.  About
150-200 ft thick
                The unit represents a seasonally active
lacustrine-dominated fluvio-lacustrine sequence, deposited
in the latter stage of Eagle basin sedimentary infill, at a
time when lakes and ponds were numerous and streams feeding
them were shallow, sluggish, and near base level within the
basin.

PIPm  Maroon Formation (Permian and Pennsylvanian)--
Principally red beds of conglomerate, conglomeratic
sandstone, arkosic sandstone, siltstone, mudstone,
claystone, and shale and  minor thin beds of limestone.
Conglomerate contains pebble- and cobble-sized material in a
matrix of poorly sorted, fine- to medium- and very coarse
grained angular sand.  Sediments are first cycle; they
contain appreciable mica; colors are dominantly bright
reddish orange and reddish brown; limestone beds are dark
gray.  Beds are generally trough crossbedded and uniform in
thickness; they range from a few inches to several tens of
feet in thickness and rarely exhibit scoured bases.  Fine-
grained beds locally exhibit current and oscillation ripple
marks and mudcracks.  About 3,000 ft thick
                Deposition occurred dominantly in braided
streams and adjacent flood plains in the mid-fan area of a
large coalescing, arid to semi-arid, alluvial-fan complex
present in marginal areas of the Paleozoic Eagle basin.
                The upper part of the formation in the map
area includes possible stratigraphic equivalents of the
Weber Sandstone of northeast Utah and northwest Colorado
(Bass and Northrop, 1963, p.J47).  Overlying the Weber,
ranging from about 50 to 100 ft below the top of the
formation is a 6 foot interval of fossiliferous dolomite and
dolomitic limestone differentiated by past workers and named
the South Canyon Creek Member of the Maroon Formation (Bass
and Northrop, 1963, p J48).

IPe   Eagle Valley Evaporite (Middle Pennsylvanian)--
Principally gypsum and anhydrite and lesser amounts of
halite; contains traces of potash salts.  Evaporites contain
interbeds of conglomerate, sandstone, siltstone, shale, and
limestone.  Beds range from a few feet to about 150 ft in
thickness.  Colors are grayish white, yellowish gray, black,
dark gray; beds are intensely folded, faulted, and ductilely
deformed by load metamorphism, diapiric upwelling, and
flowage and hydration of anhydrite (Mallory, 1971).
Intertongues with Belden Formation below and the Maroon
Formation above; intertongues laterally with the Minturn
Formation east of the map area.  Formation incompletely
exposed in the map area.  Estimated total thickness 1000-
1500 ft
                Evaporites are the products of sea water
evaporation in a restricted seaway that was present in the
central part of the landlocked Paleozoic Eagle basin which
formed between the Uncompaghre and Front Range uplifts
(Mallory, 1971).  The formation is a distal lithofacies of a
large fluvio-lacustrine and marine depositional system
present in the basin from early Pennsylvanian through early
Triassic time.  Associated fluvial and lacustrine clastic
sediments in the Eagle Valley Evaporite sequence are
products of transgressive and regressive fluvial and
lacustrine deposition under arid to semi-arid climatic
conditions adjacent to the seaway.

IPb   Belden Formation (Lower Pennsylvanian)--Dark-gray to
black and dark-brown micaceous and locally coaly shale;
contains beds and lenses of dark-gray to black argillaceous
limestone, claystone, mudstone, sandstone, conglomerate, and
thin coal seams and partings; abundantly carbonaceous and
fossiliferous; Bass and Northrop (1963, p.J36-J39) identify
258 fossil species, including algae, foraminifera,
anthozoans, bryozoans, brachiopods, pelecypods, gastropods,
scaphopods, cephalopods, annelids, trilobites, ostracods,
blastoids, crinoids, echinoderms, and vertebrate remains.
About 900 ft thick
                The oldest in series of superimposed and
formations deposited in the Eagle sedimentary basin which
formed in the northwestern part of the Central Colorado
Trough which lay between the Uncompaghre and Front Range
elements of the Ancestral Rocky Mountains.
                Deposition was dominantly in littoral and
sublittoral marine and lower deltaic environments under
moderately humid climatic conditions.  Subenvironments
included interfluvial, poorly and well-drained fresh- and
salt-water swamps, marshes, lakes, ponds, bays, estuaries,
and shallow distributary fluvial channels and channel
complexes.
                Based on the dominance of fine-grained
sediment and apparent low depositional energies, sediment
apparently accumulated near base level in the subsiding
central part of the Eagle basin a relatively long distance
from the basin margins and sediment source areas.  East of
the map area, in close proximity to the former basin margin,
the Belden grades laterally into coarse-grained fluvial
rocks of the Minturn and Maroon Formations; it conformably
grades upward into evaporite sequence of the overlying Eagle
Valley Evaporite (Mallory, 1971) called the Paradox
Formation by Bass and Northrop,(1963)

Ml    Leadville Limestone (Mississippian)--Light- to medium-
gray, massive, fossiliferous, oolitic limestone, containing
thin beds of sandy and crystalline dolomite in the lower
part; limestone contains stringers of dark-gray chert.
Locally, the upper part of the formation consists of as much
as about 50 ft of red to reddish-purple claystone containing
nodules of weathered limestone that was designated the Molas
Formation by Bass and Northrop (1963).  The limestone forms
prominent cliffs and lies unconformably below the Belden
Formation.  About 250 ft thick
                Limestone and dolomite beds apparently
formed by chemical precipitation and limestone diagenesis in
a deep marine depositional environment, whereas the
claystone in the upper part of the formation probably formed
as a weathered mantle on a karst surface under moderately
humid terrestrial conditions subsequent to lithification and
uplift of the marine sequence in either late Mississippian
or early Pennsylvanian time.

DOCu  Devonian, Ordovician, and Cambrian rocks undivided --
Rocks containing abundant invertebrate marine fossils whose
ages and stratigraphic occurrence allow recognition of the
formations and members described below (see Bass and
Northrop, 1963); sequence mapped as single unit.  Includes,
in descending order, the Chaffee Formation (Upper Devonian),
Manitou Formation (Lower Ordovician), and Dotsero Formation
(Upper Cambrian).  Total thickness about 450 ft
              Chaffee Formation (Upper Devonian) consists of
the Dyer and Parting Members.  Total thickness about 250 ft
Dyer Member: Alternating limestone and dolomite locally
containing stringers of chert; some beds are sandy.  Grades
upward into the Leadville Limestone.  Lower part of member
consists mostly of gray nodular limestone.  140-180 ft
thick.  Parting Member: Interbedded light-green and black
shale, tan quartzite, and sandy dolomite; shale is
micaceous; quartzite is medium to coarse grained and locally
conglomeratic.  Unconformably overlies the Manitou
Formation.  60-95 ft thick
              Manitou Formation (Lower Ordovician) consists
of the Tie Gulch Dolomite and Dead Horse Conglomerate
Members. Total thickness 120-150 ft  Tie Gulch Dolomite
Member: Cliff-forming unit consisting of light- to medium-
brown, fine- to medium-grained, dolomite in thin, even beds;
locally contains yellow chert stringers and thin beds of
flat-pebble conglomerate.  About 50 ft thick  Dead Horse
Conglomerate Member: Dominantly thin beds of gray flat-
pebble limestone conglomerate similar to pebble-
conglomerate beds in the underlying Glenwood Canyon Member
of the Dotsero Formation; conglomerate beds alternate
locally with thin beds and laminae of shale.  Glauconite
present in the lower part of the sequence but almost absent
in the upper part.  About 90 ft thick
                Dotsero Formation (Upper Cambrian) consists
of the Clinetop Algal Limestone and Glenwood Canyon Members.
Total thickness about 100 ft  Clinetop Algal Limestone
Member: Light-gray to lavender-white, flat-pebble limestone
conglomerate and crystalline to dense algal limestone.
Forms 3-5 ft thick caprock on the Dotsero Formation.
Glenwood Canyon Member: Light-gray to tan glauconite-bearing
dolomite, greenish-gray limy shale, and thin beds of
limestone and dolomite `0at-pebble conglomerate.  About 80-
90 ft thick
                Sediment composition and primary sedimentary
structures indicate deposition of the sequence in shallow
marine water through chemical precipitation of limestone,
dolomite, and subaqueous clastic deposition of sand and
silt.  The abundance of limestone and dolomite flat-pebble
conglomerate suggests periodic subaerial exposure of
mudflats on which desiccation polygons formed that were,
during later aqueous inundation, modified by oscillation to
rounded pebble- and cobble-sized mudballs.  Some units in
the sequence also contain beds and laminations marked by
oscillation ripples and hummocky crossbeds formed by
agitation of relatively shallow water.

Cs    Sawatch Formation (Upper Cambrian) Buff-white, light-
brown, and pink, fine- to very course grained quartzite,
sandstone (locally arkosic and conglomeratic), and dolomite;
commonly in uniform beds 2-4 ft thick; contains thin beds
and laminae of gray, green, and purple micaceous shale.
Quartzite and sandstone are locally crossbedded and
laterally continuous.  Quartzite forms conspicuous cliffs.
Dolomite in upper part of the formation locally contains
glauconite.  Upper and lower contacts covered or obscured by
faulting.  About 500 ft thick
                 Sediment apparently deposited under
current-dominated shallow-marine conditions in the littoral
and sublittoral zones.

YX    Precambrian rocks (Middle to Early Proterozoic)--Dark-
greenish-gray, reddish-black, and black quartz-biotite
schist intruded locally by granite and pegmatite dikes.
Contact with overlying rocks unconformable and poorly
exposed.
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Alluvial history in the White River basin, northwest
Colorado [abs]:  Geological Society of America Abstracts
with Programs, v. 15, n. 5, p. 328.
CONVERSION FACTORS
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     Multiply             By            To obtain
     -------------------------------------------------
     inches (in.)         2.540         centimeters(cm)
     feet (ft)            0.3048        meters (m)
     miles (mi)           1.609         kilometers (km)
     -------------------------------------------------

Refer to non-digitized version of this open-file report for
 a description of map symbols.