Depositional Environments 

of the White Rim 

Sandstone Member of the 

Permian Cutler Formation, 

Canyonlands National 

Park, Utah 

By Brenda A. Steele 

Interpretation of depositional environments and distributions of dune, interdune, and sabkha deposits in the 

White Rim Sandstone Member, concentrating on the area between the 

Green and Colorado Rivers. 

U.S. GEOLOGICAL SURVEY BULLETIN 1592 
DEPARTMENT OF THE INTERIOR 

DONAlD PAUl HODEl, Secretary 

U.S. GEOlOGICAl SURVEY 

Dallas l. Peck, Director 

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON: 1987 

For sale by the 

Books and Open-File Reports Section 

U.S. Geological Survey 

Federal Center 

Box 25425 

Denver, CO 80225 

library of Congress Cataloging in Publication Data 

Steele, Brenda A. 

Depositional environments of the White Rim sandstone member of the Permian Cutler formation, Canyonlands National Park, Utah. 

(U.S. Geological Survey bulletin; 1592) 

"Interpretation of depositional environments and distributions of dune, interdune, and sabkha deposits 

in the White Rim sandstone member, concentrating on the area between the Green and Colorado Rivers." 

Bibliography: p. 

Supt. of Docs no.: I 19.3:1592 

1. Sandstone-Utah-Canyonlands National Park. 2. Geology, Stratigraphic-Permian. I. Title. II. 

Series. 

GE75.B9 no. 1592 

[QE471.15.S25] 

557.3 s 

[551.7'56'0979259] 

85-600195 
CONTENTS 

Abstract 1 

Introduction 1 

Geologic setting 3 

Methods of study 3 

Permian Stratigraphy 3 

White Rim Sandstone Member 4 

Stratigraphic relationships 5 

Interpretation of depositional environments 6 

Dune deposits 7 

Interdune deposits 9 

Sabkha deposits 12 

Relationship of dune and interdune deposits 13 

Depositional setting 13 

Economic geology 17 

Conclusions 17 

References cited 18 

FIGURES 

1. Index map of Canyonlands National Park and surrounding area 1 

2. White Rim Sandstone Member, view of type locality 2 

3. Detailed map of study area showing locations of measured sections 3 

4. Generalized stratigraphic chart of Canyonlands National Park 4 

5. Generalized east-west stratigraphic section 4 

6. Isopach map of White Rim Sandstone Member 4 

7. White Rim Sandstone Member eastern pinchout 5 

8. Tabular planar crossbed sets with tangential bases, dune deposit 6 

9. Sand flow toes, dune deposit 7 

I 0. Inversely graded ripple strata, dune deposit 8 

11. Equal-area rose diagram of crossbedding dip direction measurements 8 

12. High-index ripples, dune deposit 8 

13. Ripple strata forming pin-striped bedding, dune deposit 8 

14. Bimodal erosional lag, dry deflationary interdune 9 

15. Textural inversion, dry deflationary interdune 10 

16. Wavy, horizontally laminated bedding, depositional interdune 10 

17. Plan view of adhesion ripples, depositional interdune 10 

18. Plan view of desiccation polygons, depositional interdune 11 

19. Bioturbation, bedding plane surface, depositional interdune 12 

20. Dolomite rhombohedrons, depositional interdune 13 

21. Schematic fence diagram White Rim Sandstone Member dune, interdune and 

sabkha deposits 14 

22. Interbedded dune and depositional interdune deposits 15 

23. Schematic diagram of White Rim Sandstone Member depositional setting 15 

24. Paleogeographic map of Canyonlands National Park and surrounding area 16 

25. Glauconite pellet, dune deposit 17 

Contents Ill 

Depositional Environments of the 

White Rim Sandstone Member of the 

Permian Cutler Formation, , 

Canyonlands National Park, Utah 

By Brenda A. Steele 

Abstract INTRODUCTION 

The White Rim Sandstone Member of the Permian 

Cutler Formation in Canyonlands National Park, southeastern Utah, was deposited in a coastal eolian environment. The White Rim consists of three types of eolian 

deposits: dune, interdune, and sabkha. Characteristics 

of the dune deposits are large-to medium-scale, unidirectional, tabular planar crossbed sets; high-index ripples oriented parallel to the dip direction of the foresets; 

inverse graded laminations formed by ripple migration; 

sand-flow toes; and raindrop impressions. Interdune deposits are of two types, erosional and depositional, 

formed under varying degrees of wetness. Erosional interdune deposits are characterized by thin, coarse sand 

to granule size, bimodal lags at the base of crossbed 

sets. Depositional interdune deposits are characterized 

by discontinuous, wavy horizontal laminations, color 

banding, adhesion ripples, relict salt-ridge structures, 

and bioturbation. Generally, both types of interdune deposits are thin and lenticular. In the eastern part of the 

study area the entire lower half of the White Rim is flatbedded sandstone that has most of the characteristics 

of depositional interdune deposits. A detrital-dominant, 

inland sabkha, which formed downwind of the main 

White Rim dune field, may be represented by this flatbedded sandstone. Location of the sabkha was topographically controlled by early movement of the Monument upwarp and grew as the result of a stable and 

slowly rising water table. 

Canyonlands National Park in southeastern Utah 

(fig. 1) has some of the most spectacular and colorful 

The Lower Permian White Rim Sandstone Member 

was deposited during a period of marine transgression 

when the area of Canyonlands National Park was exposed to alternating marine and nonmarine conditions. 

Permian paleogeography and stratigraphic relationships, 

sand body geometry, dune form, and petrologic features 

such as glauconite pellets, a crinoid fragment, and heavy 

mineral concentrations all indicate the White Rim Sandstone Member was deposited in a coastal setting. 

111 ° 

39o [iSALTi¢KE 

Moab 

~'v 

«~ Area of «;-.~ «"-

figure 1 'X"'~ ~v ~ -.) 

o Hanksville 

38° 

110° 109° 

(/. 

'ttco /i 'f?,o I 

,o..q ~It, I Junction 

-?..qD 0 -?~ 0-1- 5J U,o( # I/,~:-)' 

~0 S..qs I 

cP 11\t I 0 Moab 

DEADHORSE ~OINT 

STATE PARK 

CANYONLANDS I 

NATIONAL PARK 

I lg 

~IC2 Monticello 0 5 

1 

g 

18 

oBlanding I 

ARIZONA NEW 

MEXICO 

40 MILES 

I I I I I 

50 KILOMETERS 

Figure 1. Index map of Canyonlands National Park and 

surrounding area. 

Introduction 1 
Figure 2. White Rim Sandstone (WR) and underlying Organ Rock (OR) Members of Permian Cutler Formation, type 

locality, looking south toward confluence of the Green and Colorado Rivers. Thickness of White Rim is approximately 

14m. 

canyon scenery in the country. One of the most recognizable units exposed along the canyon wall in the park is 

the White Rim Sandstone Member of the Permian Cutler 

Formation, which forms a conspicuous white ledge surrounded by dominantly reddish-brown sandstone and shale 

(fig. 2). The abundant, large-to medium-scale, unidirectional, tabular planar crossbedding in the White Rim 

prompted early workers in the region to conclude that, 

for the most part, it represents ancient dunes deposited 

in an eolian environment (Baker and Reeside, 1929; 

McKnight, 1940; Baker, 1946; Kunkel, 1958; Heylmun, 

1958; and Hallgarth, 1967a). 

The first detailed study of the White Rim Sandstone 

Member was done by Baars and Seager (1970) and was 

concentrated in the Elaterite Basin area (fig. 1). They concluded the White Rim is almost entirely shallow marine 

and only the easternmost part, near the base of Shafer 

Trail (fig. 3), is eolian. This interpretation was based on 

a detailed analysis of sedimentary structures and on the 

presence of a problematic (alga?) fossil found in Eiaterite 

2 White Rim Sandstone Member, Cutler Formation, Utah 

Basin. The large-scale, unidirectional cross stratification 

in the White Rim was interpreted to represent numerous, 

elongate, offshore bar deposits formed by longshore currents moving from the northwest. Also, according to 

Baars and Seager (1970), these bar deposits invariably 

overlie horizontally bedded material in the area between 

the Green and Colorado Rivers. They interpreted the horizontal bedding to represent a regressive sequence, and the 

offshore bars a transgressive sequence. 

In order to resolve this difference in interpretation, 

a detailed study of the White Rim was conducted in the 

area between the Green and Colorado Rivers in Canyonlands National Park (fig. 3). Stratigraphic relationships, 

sedimentary structures, and petrographic characteristics of 

the White Rim were examined. Results from this study 

indicate the White Rim was deposited in an eolian system 

and contains dune, interdune, and sabkha deposits. Also, 

the White Rim has a close marine association and represents a coastal dune field (Steele-Mallory, 1981a). 
110 o DO ' 

5 MILES 

I 11 11 I I 

5 KILOMETERS 

EXPlANATION 

Gravel road 

Jeep trail 

• Measured section location 

Canyonlands National Park boundary 

Figure 3. Detailed map of study area showing locations 

of measured sections. 

Geologic Setting 

Canyonlands National Park is located in the northcentral portion of the Colorado Plateau and is part of the 

Canyonlands section of the Plateau (Fenneman, 1928). 

The Canyonlands section is essentially a large plateau surface that has been epeirogenically upwarped and broadly 

folded (Hunt, 1956). Entrenchment of the Green and Colorado Rivers and their tributaries on this surface in the 

last 5 million years (Trumble, 1980) has formed a series 

of deep canyons. The present study was done in the Island 

in the Sky district of the park, which includes the 60-kmwide erosional basin of the Green and Colorado Rivers 

(fig. 3). 

Almost continuous sedimentary deposition in the 

Canyonlands region throughout much of the Paleozoic, 

Mesozoic and Cenozoic Eras resulted in a thick accumulation of sediments, which exhibit diverse compositions. 

Late Tertiary to Holocene erosion has completely removed 

the entire Cenozoic and part of the Mesozoic record. Presently, relatively undeformed rocks of Pennsylvanian to Jurassic age are exposed in the park (fig. 4). Baars and 

Molenaar (1971), Lohman (197 4), and Fassett and 

Wengerd (1975) have discussed the geologic history of 

Canyonlands. 

Methods of study 

The White Rim Sandstone Member is excellently 

exposed in canyon walls of the Green and Colorado Rivers (fig. 2). The White Rim trail, a primitive four-wheel 

drive road (fig. 3), gives limited access to outcrops. 

Twelve complete and three partial stratigraphic sections 

were measured, described, and sampled. Stratigraphic sections were spaced in order to attain maximum coverage 

of the White Rim throughout the study area (fig. 3), but 

working access to full sections of the White Rim is limited 

because it forms steep, unscalable cliffs. Complete descriptions of the measured sections are given in SteeleMallory ( 1981 b and 1982). 

In the course of measuring and describing stratigraphic sections, emphasis was placed on the examination 

and description of primary sedimentary structures, including their size, orientation, and morphology . Mean crossbed dip directions were calculated for each measured section by the vector summation method first used by Reiche 

( 1938). Equal-area rose diagrams of all crossbed dip directions were made. These were used to classify dune 

types and to help reconstruct the depositional history of 

the White Rim. Local and regional geologic relationships 

of the White Rim to adjacent stratigraphic sequences also 

were examined to help reconstruct the White Rim's depositional history. 

At each measured section, the White Rim and the 

overlying and underlying units were sampled for thin sections. A detailed petrographic examination was made of 

107 thin sections to identify textures, mineralogy, and 

diagenetic features. Complete descriptions of the thin sections are given in Steele-Mallory (1981 b and 1982). 

PERMIAN STRATIGRAPHY 

During Permian-Pennsylvanian time, southeastern 

Utah underwent a period of orogenic activity. Major structural features formed were the northwest-southeast trending Uncompahgre uplift and the adjacent, parallel-trending 

Paradox basin (fig. 1). Both features greatly influenced 

Permian depositional patterns in the region. Figure 5 is 

a generalized stratigraphic section for Canyonlands and 

the surrounding area. Throughout much of the Early Permian, the Uncompahgre uplift (fig. 1) contributed large 

amounts of detrital material to the area, resulting in a 

900- to 2,400 m-thick accumulation of continental clastic 

material adjacent to the uplift, the undifferentiated Cutler 

Formation (Williams, 1964; Campbell, 1980). At the 

same time, marine conditions prevailed to the west, in 

south-central Utah and northern Arizona (Hallgarth, 

1967 a). Sediments deposited in both marine and continental environments interfinger in Canyonlands (Baars and 

Molenaar, 1971). The Rico Formation (Elephant Canyon 

Formation of Baars, 1962) and the Organ Rock, Cedar 

Permian Stratigraphy 3 
AGE NAME THICKNESS 

(METERS) 

Moab Member 

u Entrada Slick Rock 

Vi 122-152 en Sandstone Member ~ 

a: Dewey Bridge ~ Member ..., 

Navajo 99-168 Sandstone 

Glen Kayenta Canyon 49-91 

Group Formation 

Wingate 

Sandstone 64-104 

u 

Vi Unnamed en Chinle upper member 63-226 ~ 

a: 

1- Formation Moss Back 

Member 0-24 

Unnamed 

Moenkopi upper member 76-287 

Formation Hoskinnini 

Member 0-37 

White Rim 

Sandstone Member 

z Cutler Organ Rock ~ Formation Member 244-305 

~ a: 

w Cedar Mesa a.. 

Sandstone Member 

Rico Formation 

(Elephant Canyon Formation1) 76-178 

z 

~ 

z 

<( Honaker Trail > Formation, 274-549 ...J 

>- Hermosa CJ) 

Group 1 z 

z 

w Paradox ? a.. Formation1 

1of Baars, 1962 

Figure 4. Generalized stratigraphic chart of Canyonlands national Park (modified from Lohman, 1974). 

Mesa Sandstone, and White Rim Sandstone Members of 

the Cutler Formation were all deposited in this complex 

depositional setting. 

White Rim Sandstone Member 

Baker and Reeside ( 1929) named the White Rim 

Sandstone Member for exposures of a light-colored, cliffforming sandstone, forming a prominent bench between 

the Green and Colorado Rivers. It is the upper of two 

light-colored sandstone units of the Permian Cutler Formation in Canyonlands. The determination of the age of the 

White Rim depends on regional correlations because direct 

dating is not possible. The White Rim overlies the 

Wolfcampian Rico Formation, (also called the Elephant 

Canyon Formation of Baars, 1962), and was most likely 

deposited during late Leonardian to early Guadalupian 

time (Baars, 1962; Hallgarth, 1967a). 

4 White Rim Sandstone Member, Cutler Formation, Utah 

WEST 

San Rafael 

Uplift 

Canyonlands 

National Park 

Moab 

Utah 

EAST 

Kaibab Moenkopi Formation TRIASSIC 

1 of Baars, 1 962 

2Lohman, 1974 

Hermosa Group1 

PERMIAN 

(thickness 

320- 483 m) 2 

PENNSYLVANIAN 

Figure 5. Generalized east-west stratigraphic section, 

Canyonlands National Park and surrounding area (modified from Baars and Seager, 1970). 

Regionally, the White Rim forms an elongate, 

northeast-southwest-trending sandstone body (fig. 6) that 

abruptly pinches out eastward into the Organ Rock Member (fig. 7) and an overlying unnamed unit that may be 

Permian or Triassic in age, and dips gradually to the 

N 

1 

SAN JUAN COUNTY 

10 2 0 MILES 

10 2 0 KILOMETERS 

EXPlANATION 

Monocline showing direction of plunge axis 

Figure 6. Isopach map of White Rim Sandstone Member 

(modified from Baars and Seager, 1970). 
northwest where it thickens to an estimated 220 m (Baars 

and Seager, 1970). Part of the eastern pinchout closely 

parallels the western flank and northern plunge of the 

Monument upwarp, indicating this structure was active 

during Permian time (Baars, 1979). 

Stratigraphic Relationships 

The study area is close to the eastern pinchout of 

the White Rim. Throughout most of this area the White 

Rim conformably overlies the reddish-brown sandstones 

and silty shales of the Organ Rock Member. Depositional 

environments of the Organ Rock are interpreted as fluvial 

channel and related flood plain (Baars and Molenaar, 

1971, Campbell, 1980). In the southern part of the study 

area the White Rim may conformably overlie the Cedar 

Mesa Sandstone Member (Steele-Mallory, 1981 b; 1982). 

Early workers in the region, McKnight (1940) and Baker 

( 1946), considered the Cedar Mesa to be eolian. Baars 

(1962, 1979), Blakey (1979), and Mack (1979) all considered the Cedar Mesa to be largely shallow marine, but 

recent studies by Loope (1984) also interpreted this unit 

as eolian. In addition, Campbell and Stanesco (1983) and 

Loope (1984) recognized fluvial deposits in the Cedar 

Mesa. 

The White Rim in the study area is overlain by 

a reddish-brown mottled, massively bedded, poorly sorted 

arkosic sandstone that may be bioturbated (Steele-Mallory, 1981 b, 1982). Little has been written on this unnamed unit, and its relationship to the White Rim is not 

clearly understood. McKnight (1940), Kunkel (1958), and 

Baars and Seager ( 1970) considered this unit to be an 

unnamed sandstone in the Cutler Formation. Baker (1946) 

and Hallgarth (1967a) considered the unit to be part of 

the Triassic Moenkopi Formation and placed the PermianTriassic boundary at the top of the White Rim. This unit 

is not laterally persistent. Southwest of the study area, 

near Elaterite Basin (fig. 1), the Triassic Moenkopi contains a basal conglomerate and unconformably overlies the 

White Rim (Baars and Seager, 1970). 

The contact between the White Rim and the underlying units is sharp, planar, and distinct, and no scouring 

Figure 7. Eastern pinchout of White Rim Sandstone Member (WR) into Organ Rock Member (OR) and overlying 

unnamed unit, looking south into Canyonlands National Park from Deadhorse Point State Park. 

Permian Stratigraphy 5 
Figure 8. Tabular planar crossbed sets in dune deposit, showing concave upward laminations forming tangential 

bases and a nearly horizontal bounding surface between sets, top of Beaver Bottom section. 

by the White Rim is evident. The top of the Organ Rock 

and Cedar Mesa Sandstone Members is commonly 

bleached and intensely altered with most feldspar grains 

destroyed, mica grains bleached and expanded, and abundant authigenic kaolinite (Steele-Mallory, 1981b, 1982). 

The upper contact of the White Rim is also typically sharp 

and distinct but irregular, undulating a meter or more. 

This irregularity most likely represents a paleotopographic 

surface and may be related to the eolian nature of the 

White Rim. 

The most widely accepted lateral equivalents of the 

White Rim are the upper part of the Leonardian Toroweap 

Formation and the Leonardian gamma member of the 

Kaibab Limestone found in south-central Utah and northem Arizona (Kunkel, 1958; Heylmun, 1958; Hallgarth, 

1967a; Baars and Seager, 1970; Irwin, 1971). The Toroweap consists of sandstone, carbonate, and evaporite deposited in restricted marine and related coastal eolian and 

sabkha environments (Hallgarth, 1967a; Rawson and 

Turner-Peterson, 1979). The gamma member of the 

Kaibab consists of carbonate, evaporite, and siltstone de6 White Rim Sandstone Member, Cutler Formation, Utah 

posited in restricted marine and related coastal sabkha environments (McKee, 1954; Cheevers and Rawson, 1979). 

INTERPRETATION OF DEPOSITIONAL 

ENVIRONMENTS 

The White Rim Sandstone Member in Canyonlands 

National Park was deposited in an eolian system. Unlike 

many other depositional environments, no single facies 

model exists for eolian systems, resulting in no preferred 

vertical sequences nor any consistent lateral changes 

(Walker, 1979). Ancient eolian deposits may best be recognized by the presence of features that are characteristic 

of, or at least compatible with, a modem eolian environment (McKee and Bigarella, 1979a). Glennie (1970), 

Bigarella (1972), McKee and Bigarclla (1979a, b), Hunter 

( 1977), Kocurek and Dott ( 1981), and Ahlbrandt and 

Fryberger (1982) gave good general discussions of different features of eolian deposits. Some of the more important characteristic features are: 
Figure 9. Tongue-shaped sand flow toes (arrows) near base of crossbed set, dune deposit, base of Shafer Trail. 

1 . Sets of medium- to large-scale tabular planar or 

wedge planar crossbeds that dip down wind. 

2. Bounding surfaces between cross bed sets that are 

either horizontal or inclined at low angles. 

3. High-index ripples, R.I.> 15, oriented parallel or subparallel to the dip direction of the foresets. 

4. Inverse graded laminations within crossbed sets. 

5. Sand flow toes. 

6. Coarse-grained lags between crossbed sets that are 

often bimodal. 

7. Signs of exposure to subaerial conditions such as 

raindrop impressions, root structures, or animal tracks 

and trails. 

Detailed examination of the White Rim reveals the 

presence of many of these features. Dune, interdune, and 

sabkha deposits are recognized. Each of these deposits 

has distinctive sedimentary structures and petrologic features. 

Dune Deposits 

The most prominent feature of the dune deposits 

is the conspicuoustabular planar crossbedding. Thicknesses range from less than 0.5 m to 6 m, averaging 1.5 

m. Laminations near the base of each set are commonly 

concave upward, forming long, sweeping tangential bases 

that become nearly horizontal (fig. 8). Small-scale stratification features observed within the dune sets are tongueshaped sand flow toes near the base of cross bed sets, related to avalanching of noncohesive sand on the dune slip 

faces (fig. 9); normally graded strata related to grainfall 

processes; and inversely graded strata related to ripple 

migration (fig. 1 0). All of these features are consistent 

with eolian depositional processes (Hunter, 1977; 

Ahlbrandt and Fryberger, 1982). 

Crossbedding dip directions are strongly unidirectional (fig. 11), having a vector mean dip direction of 

S. 4 7 E. , and an average dip angle of 22°. This strongly 

unidirectional, northwest to southeast trend of the crossbeds suggests the dune form was most likely either barchanoid or transverse ridges (McKee, 1979a). These dune 

types are commonly oriented at approximately right angles 

to the dominant effective wind direction and are the result 

of moderate winds and fairly abundant sand supply 

(McKee, 1979b). 

Interpretation of Depositional Environments 7 
Figure 10. Inversely graded laminations produced by 

ripple migration, dune deposit, base of Shafer Trail. 

High-index ripples, R.I.> 15, oriented parallel to 

the dip direction of the foresets, are commonly observed 

on exposed slip faces (fig. 12). High-index ripples on slip 

faces are formed either by deflection of wind over the 

dune surface or by a temporary change in wind direction 

(Bigarella, 1972). Strata produced by migrating wind ripples are distinctly laminated and inversely graded 

(Fryberger and Schenk, 1981), and are characterized by 

a "pin-striped" appearance (fig. 13). 

Rare raindrop impressions with raised rims and depressed centers are found preserved on exposed slip face 

surfaces. Raindrop impressions, although not definitive 

N 

s 

Average mean dip direction = S 4 7 E 

Total number of measurements = 707 

Figure 11. Equal-area rose diagram of crossbedding 

dip direction measurements. 

8 White Rim Sandstone Member, Cutler Formation, Utah 

Figure 12. High-index ripples, dune deposit, base of 

Queen Anne Bottom section. Ripple wavelength is approximately 13 em and ripple height is approximately 3 

mm. 

proof of eolian deposition, do indicate subaerial exposure. 

Colors of the White Rim dune deposits are commonly 

white, very light gray, or yellowish gray. These dune 

sands are generally well to moderately well sorted, generally fine grained but ranging from fine to coarse grained, 

and subrounded to rounded. The dominant mineral constituent is monocrystalline quartz, and most of the sands 

would be classified as quartz arenites (Folk, 1974). Many 

of the coarser quartz grains are frosted. Other major mineral constituents are microcline, polycrystalline quartz of 

unknown origin, and chert. Trace amounts of zircon, tourmaline, apatite, glauconite, mica, altered iron-titanium 

oxides, and garnet are also present. Little or no clay was 

observed in the samples examined. These sandstones are 

commonly calcite cemented. Silica cement, in the form 

of quartz overgrowths, is also present and has altered the 

original roundness of some quartz grains. 

Figure 13. Pin-striped bedding formed by ripple migration, dune deposit, base of Shafer Trail. 
Interdune Deposits 

An interdune is defined as an area either enclosed 

or partially enclosed by dunes. Interdune deposits are sediments that occur in the interdune areas and may record 

either deflationary or depositional processes. Recent work 

by Ahlbrandt and Fryberger ( 1981 , 1982) and Kocurek 

(1981) on modem and ancient eolian systems has recognized the relationship of water content to the types of 

sedimentary structures formed in interdunes. They have 

informally subdivided depositional and deflationary interdunes into dry, damp, wet, and evaporite on this basis. 

Fryberger and others (1983) and Kocurek (1981) listed 

the sedimentary structures common to each type of interdune setting. Also, like all depositional environments, interdune environments are not static, and any single interdune deposit may reflect a variety of conditions. Deflationary and depositional interdunes that formed under varying degrees of wetness are recognized in the White Rim. 

Generally, White Rim interdune deposits are thin 

and lenticular, a geometry that may be related to the unimodal wind regime in which the White Rim sand was 

deposited. According to Ahlbrandt and Fryberger (1981), 

interdune geometries appear to be closely related to wind 

regime, and interdunes from unimodal wind regimes are 

thought to be thin and lenticular. 

Dry deflationary interdune deposits are common in 

the White Rim and occur as thin erosional lags between 

crossbed sets (fig. 14). Their average thickness is less 

than 0. 5 m; they are lenticular and appear to be roughly 

horizontally stratified. The basic mineralogy of these deposits is similar to the dune deposits, but in general they 

are darker colored, coarser grained, and more poorly 

sorted than the surrounding dune sands. Samples taken 

from these lag deposits commonly have a bimodal grain 

size distribution and show textural inversion (fig. 15). 

Folk ( 1968) described textural inversion as the occurrence 

of large, well-rounded quartz grains "floating" within 

finer, more angular quartz grains, and considered the 

phenomenon to be a product of deflationary processes. 

Other White Rim interdune deposits appear to be 

closely related to water table fluctuations and are most 

likely the result of a combination of damp or evaporitic 

depositional processes. These interdune deposits commonly have wavy, discontinuous, horizontal laminations 

Figure 14. Bimodal erosional lag, dry deflationary interdune deposit, Unknown Bottom. 

Interpretation of Depositional Environments 9 
Figure 15. Textural inversion, dry deflationary interdune deposit, Beaver Bottom section. (Field of view approximately 

5.5 mm, polars crossed) 

that have been disrupted by either biological acttvtty or 

diagenetic changes (fig. 16). Primary sedimentary structures in the interdune deposits are commonly discernible 

only on bedding surfaces. Two distinctive interdune sediFigure 16. Wavy, horizontally laminated bedding, 

depositional interdune, base of Shafer Trail. 

10 White Rim Sandstone Member, Cutler Formation, Utah 

mentary structures recognized in the White Rim are adhesion ripples and desiccation polygons. Adhesion ripples 

form when sand is blown across a damp surface, commonly grow into the wind, and are strongly asymmetrical 

Figure 17. Plan view of adhesion ripples, depositional 

interdune, near Washer Woman section. 
(Reineck and Singh, 1975). Even minor shifts in wind 

direction affect these ripples, creating an irregular, bumpy 

bedding surface (fig. 17). Generally, sets of adhesion ripple strata are less than 0 .5 m thick in the White Rim, 

but can reach thicknesses of over 1 m. According to 

Ahlbrandt and Fryberger (1981 ), a rising water table may 

account for the thicker accumulations of adhesion ripple 

strata. 

Some White Rim interdune surfaces are covered 

with 5-sided polygons (fig. 18) that have widths of up 

to 0. 7 m and occur in almost totally sand-sized material. 

These polygons may represent relict sait-ridge structures 

and indicate occasional evaporitic conditions in the interdune areas. Initially, capillary evaporation of saline 

groundwater creates a salt crust, and the polygons later 

form as the result of alternating periods of desiccation 

and deposition (Glennie, 1970; Ericksen and Stoertz, 

1978). The sand that forms these polygons often is stained 

reddish brown. This staining may be a result of the exposure of salt-encrusted sand to the sun during salt-ridge 

formation (Fryberger and others, 1983). 

In many ancient and modern interdune areas, both 

plant and animal burrows are common (Fryberger and 

others, 1983). No distinct burrows of any kind were observed in the White Rim interdunes. Bioturbation is occasionally present (fig. 19), which gives the sediment a 

characteristic mottled, homogeneous appearance (Friedman and Sanders, 1978). 

The basic mineralogy and texture of these interdune 

deposits are similar to the dune deposits, but there are 

some differences. Their color is normally darker than the 

dune sands, ranging from yellowish orange to brownish 

orange , and they commonly have a banded appearance 

(fig. 16). Concentrations of heavy mineral grains in the 

laminations are common. Dolomite is present in the interdune sands and occurs as individual , euhedral to subhedral 

rhombohedrons that are heavily iron stained. The rhombohedrons commonly form distinct layers, often appear 

abraded (fig. 20), and are probably of secondary origin 

(Scholle , I 978). 

Few biological constituents were observed in the 

White Rim. A crinoid ossicle was identified from a 

Figure 18. Plan view of desiccation polygons, depositional interdune (1), overlain by dune deposit (D), Musselman 

Arch. 

Interpretation of Depositional Environments 11 
Figure 19. Bioturbation, bedding plane surface, depositional interdune deposit, base of Shafer Trail. 

coarse-grained zone near the base of the White Rim in 

the White Crack section (fig. 3). The ossicle is well preserved, showing single-crystal extinction, which is typical 

of echinoderm grains. Fecal pellets were also observed 

in a number of interdune samples and are commonly encased in dolomite rhombohedrons. 

Sabkha Deposits 

In the eastern part of the study area, the entire basal 

White Rim consists of flat-bedded sandstone that has most 

of the characteristics of depositional interdune deposits. 

This may represent an ancient sabkha deposit. Sabkhas, 

although similar to interdunes, are more aerially extensive 

than interdunes and are related to a stable and continued 

rise in the water table (Fryberger and others, 1983). 

Johnson and others (1978) defined inland sabkhas as 

evaporitic, commonly salt-encrusted, saline flats underlain 

by clay, silt, and sand. The development and distribution 

of inland sabkhas are controlled by topography and fluctuations in the local water table. Also, sabkhas can be either 

detrital dominant or evaporite dominant. The White Rim 

12 White Rim Sandstone Member, Cutler Formation, Utah 

sabkha consists largely of clastic material, and no evidence of extensive evaporite minerals is present; thus the 

sabkha would be classified as detrital dominant (Fryberger 

and others, 1983). One feature observed in the White Rim 

that has been described in modem detrital-dominant sabkhas (Fryberger and others, 1983) is bedding with a 

banded appearance (fig. 16). This light-dark color banding 

may result from the intercalation of light-colored sand of 

ripple-produced strata and reddish-brown stained sand of 

salt-ridge structures. 

Several factors contributed to the location and development of this sabkha. The sabkha location coincides 

with the White Rim's eastern pinchout, which Baars 

( 1979) considered to be related to early movement of the 

Monument upwarp. Thus, the Monument upwarp created 

a topographic barrier to the east. The sabkha was also 

protected to the west by the main White Rim dune complex. In some modem eolian systems, sabkhas commonly 

occur down wind of the major dune complex (Fryberger 

and others, 1983). Growth of the sabkha most likely resulted from a slow but steadily rising water table and continued accumulation of sediment. 
Figure 20. Dolomite rhombohedrons (D) of secondary origin, depositional interdune, Buck Canyon section. (Field 

of view approximately 0.7 mm, polars crossed) 

Relationship of Dune and Interdune Deposits 

Figure 21 is a schematic fence diagram compiled 

from the measured sections, showing the regional stratigraphic relationships and distribution of dune, interdune, 

and sabkha deposits. In the eastern part of the study area, 

the entire basal White Rim may be a sabkha deposit, 

reaching a thickness of almost 6 m. Depositional interdunes occur as distinct, thin, lenticular units within the 

dune deposits (fig. 22). To the northwest, in sections 

QAB and BB (fig. 3), no depositional interdunes were 

observed. Sabkha and depositional interdune deposits both 

require damp or wet conditions during their formation. 

Distribution of these deposits in the White Rim was probably closely related to the water table variations. The location of the sabkha deposit and the prevalence of the depositional interdunes in the eastern part of the study area 

suggest the water table was shallower in this area. Dry 

deflationary interdune deposits, on the other hand, occur 

throughout the study area, but are more common in the 

western part. These deposits were most likely independent 

of the water table fluctuations and were related to dune 

migration during White Rim depos·ition. 

DEPOSITIONAL SETTING 

Figure 23 is a schematic diagram of the depositional 

setting of the White Rim Sandstone Member. Dune fields 

can be broadly grouped as either coastal or inland (McKee 

and B igarella, 1979b). Several different lines of evidence 

suggest the White Rim Sandstone Member was deposited 

in a coastal setting. These are (1) Permian paleogeography, (2) stratigraphic relationships, (3) geometry of the 

White Rim sand body, (4) dune form, and (5) certain 

petrologic features. 

The White Rim Sandstone Member was deposited 

during late Leonardian to early Guadalupian time according to Baars and Seager, ( 1970). Figure 24 shows the 

proposed Early Permian paleogeography of Canyonlands 

and surrounding areas. West of Canyonlands was a broad, 

stable shelf, and to the east, the positive Uncompahgre 

highlands and Monument upwarp . The shoreline was to 

the west, running approximately north-south, and CanyonDepositional Setting 13 
OAB 

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EXPlANATION 

Sabkha deposit 

Dune deposit 

Depositional interdune deposit 

Erosional interdune deposit 

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METERS FEET 

225 

150 

75 

Figure 21. Schematic fence diagram White Rim Sandstone Member dune, interdune, and sabkha deposits. 

SD1 

0 

lands was situated in an active coastal plain area exposed 

to both marine and nonmarine processes. The proposed 

paleomagnetic equator during the Permian was to the 

north. Canyonlands was at approximately 5° S. latitude, 

and much of North America was in the Southeast Trade 

Winds Belt (Opdyke and Runcom, 1960; Dott and Batten, 

1976). Northwest to southeast winds deposited the White 

Rim sand even though the area was in the Southeast Trade 

Wind Belt. This northwest to southeast wind pattern may 

represent onshore winds, resulting from differential cool14 White Rim Sandstone Member, Cutler Formation, Utah 
Figure 22. Interbedded dune (D) and depositional interdune (I) deposits, Lathrop Canyon 2 section. 

ing and warming between land and sea. According to 

Goldsmith (1978), an onshore wind pattern commonly is 

dominant regardless of the general wind circulation pattern. Also, this southerly wind pattern was common in 

the Permian and is evident in other proposed eolian units 

in the region, including the DeChelly Sandstone Member 

of the Cutler Formation and the Coconino Sandstone 

(Poole, 1962). 

Stratigraphic relationships of the White Rim imply 

a coastal setting. It abruptly pinches out eastward into 

the nonmarine Organ Rock Member. Westward it apparently grades into the largely marine upper member of the 

Toroweap Formation and the gamma member of the 

Kaibab Limestone. Unfortunately, much of the westernmost White Rim occurs in the subsurface, and little 

information is available. The transition between marine 

and eolian environments may begin just west of Canyonlands, in the Elaterite Basin area (fig. 1), where the uppermost portion of the White Rim contains a thin, veneer-like 

unit with well-developed but localized oscillation ripples 

(Baars and Seager, 1970; Chan and Huntoon, 1984). Chan 

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LIMIT OF WHITE RIM 

SANDSTONE 

MEMBER DEPOSITION 

Figure 23. Schematic diagram of White Rim Sandstone 

Member depositional setting. 

Depositional Setting 15 
10 20 MILES 

10 20 KILOMETERS 

Figure 24. Paleogeographic map of Canyonlands National Park and surrounding area: late Wolfcampian-early 

Leonardian time. (Modified from Hallgarth, 1967b) 

and Huntoon (1984) observed coarse-grained sandstones 

with chert pebbles and abundant fluid escape structures 

in this uppermost unit and considered it to represent a 

reworked zone, formed during a marine transgression. 

Also, northwest of the study area near the San Rafael 

uplift (fig. 1), the top of a unit identified as White Rim 

is bioturbated and contains identifiable marine fossils (Orgill, 1971). 

The geometry of dune sands is probably closely related to their depositional setting (McKee and Bigarella, 

1979b). An inland dune field tends to form an extensive, 

tabular or wedge-shaped sand sheet. A coastal dune field 

can form a more narrow, elongate sand sheet. The White 

Rim, an elongate, narrow, northwest-southeast sand body, 

is more characteristic of a coastal dune field. Unimodal 

crossbedding measurements indicate the White Rim dune 

form was most likely barchanoid or transverse ridges (fig. 

8), which are common coastal dune forms in unvegetated 

areas (Goldsmith, 1978). 

Coastal dune sands are essentially beach sediments 

that have been reworked and piled up by the wind. Sev16 White Rim Sandstone Member, Cutler Formation, Utah 

eral petrologic features of the White Rim suggest the 

proximity of a beach, the most important of which is the 

presence of glauconite. Trace amounts of well-rounded, 

unaltered glauconite pellets (fig. 25) were observed in thin 

sections of samples collected from all the measured sections, and occur in both dune and interdune deposits. 

Glauconite is the name given to a variety of dull-green, 

earthy, iron-rich clay minerals of the mica group that 

commonly form under local reducing conditions in shallow-marine water (Weaver and Pollard, 1973). The presence of glauconite in a sediment usually indicates a 

marine depositional environment, for it rarely survives 

erosion and redeposition in nonmarine environments 

(Triplehorn, 1966). The occurrence of glauconite throughout the White Rim suggests proximity to a marine environment. Along with the glauconite, the crinoid fragment 

and the relative enrichment of heavy minerals in the interdune deposits may also indicate a nearby beach. According to Potter (1967), skeletal debris, heavy mineral concentrates, and small amounts of glauconite are common 

constituents of many beach sediments. 
Figure 25. Glauconite pellet (G), dune deposit, Beaver Bottom section. (Field of view approximately 0.7 mm, polars 

crossed) 

ECONOMIC GEOLOGY 

The White Rim Sandstone Member has major petroleum reserves and contains the largest tar-sand deposit in 

the United States (Ritzma, 1980). Campbell and Ritzma 

( 1979) have estimated the tar sands may contain up to 

16 billion barrels of oil in place. These deposits are found 

west of the study area in the Elaterite Basin region (fig. 

1), and are mostly either part of national parkland or proposed wilderness areas. The oil is trapped by the updip 

pinchout of the White Rim on the northwest plunge of 

the Monument upwarp (Campbell and Ritzma, 1979). According to Baars and Seager ( 1970), the most likely 

source for petroleum was the Permian Kaibab Limestone 

because of its stratigraphic position adjacent to the White 

Rim. 

There is some evidence suggesting that petroleum 

migrated through the White Rim in the study area. The 

normally reddish-brown sandstone unit overlying the 

White Rim is bleached at sections BB and BC (fig. 3), 

indicating reduction by migrating petroleum. Also, a 

number of White Rim samples contain possible accumulations of dead oil (Steele-Mallory, 1981 b, 1982). 

CONCLUSIONS 

1. The White Rim Sandstone Member of the Permian 

Cutler Formation in Canyonlands National Park, 

Utah, was deposited in an eolian system. 

2. The White Rim contains three types of eolian deposits--dune, interdune, and sabkha-which can be 

differentiated on the basis of sedimentary structures 

and petrologic features. 

3. Distinctive sedimentary structures of the dune deposits are large-scale, unidirectional, tabular planar 

crossbed sets; high-index ripples oriented parallel to 

dip direction of the foresets; and raindrop impressions. A strongly unidirectional, northwest to southeast orientation of the crossbedding suggests the dune 

forms were barchanoid or transverse ridges. The dune 

deposits are basically light-colored, fine-grained, 

Conclusions 1 7 
well- to moderately well sorted quartz arenites with 

little clay material. 

4. Interdune deposits resulting from both deflationary 

and depositional processes and formed under varying 

degrees of wetness are present. Most of the interdune 

deposits occur as thin, discontinuous units intercalated with the dune deposits. Dry deflationary deposits occur as darker colored, thin, lenticular, 

bimodal, coarse-grained lags between crossbed sets. 

Other interdune deposits appear to have formed by 

a combination of damp and evaporitic depositional 

processes. Characteristic sedimentary structures of 

these interdunes are wavy, discontinuous, horizontally 

laminated bedding with dark- and light-color banding; 

adhesion ripples; bioturbation; and desiccation polygons, which may represent relict salt ridge structures. 

Their basic texture and mineralogy are similar to the 

dune deposits, but the depositional interdunes contain 

abundant euhedral to subhedral dolomite rhombohedrons, fecal pellets, a fossil fragment, and concentrations of heavy mineral grains in laminations. 

5. A detrital-dominant, inland sabkha formed downwind 

of the main White Rim dune field. This can be seen 

in the eastern part of the study area, where the entire 

lower portion of the White Rim is flat-bedded sandstone and has most of the characteristics of depositional interdune deposits. Location of this sabkha was 

topographically controlled by early movement of the 

Monument upwarp, and grew as the result of a stable 

and slowly rising water table. 

6. The White Rim dune field was deposited in a coastal 

setting by northwest-to-southeast onshore winds during a period of marine transgression. Evidence for 

a coastal setting includes Permian paleogeography, 

stratigraphic relationships, geometry of the sand body 

and dune form, and certain petrologic features such 

as glauconite pellets, a crinoid fragment, and heavy 

mineral concentrations. 

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tr U.S. GOVERNMENT PRINTING OFFICE: 1987-773-047/46,053 REGION NO.8 • 

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