Palynostratigraphy in Relation to

Sequence Stratigraphy, Straight Cliffs Formation

(Upper Cretaceous), Kaiparowits Plateau, Utah

U.S. GEOLOGICAL SURVEY BULLETIN 2115-B
AVAILABILITY OF BOOKS AND MAPS OF THE U.S. GEOLOGICAL SURVEY

Instructions on ordering publications of the U.S. Geological Survey, along with prices of the last offerings, are given in the current-year 

issues of the monthly catalog "New Publications of the U.S. Geological Survey." Prices of available U.S. Geological Survey publications released prior to the current year are listed in the most recent annual "Price and Availability List." Publications that may be listed in various U.S. 

Geological Survey catalogs (see back inside cover) but not listed in the most recent annual "Price and Availability List" may no longer be 

available.

Reports released through the NTIS may be obtained by writing to the National Technical Information Service, U.S. Department of 

Commerce, Springfield, VA 22161; please include NTIS report number with inquiry.

Order U.S. Geological Survey publications by mail or over the counter from the offices listed below.

BY MAIL

Books

Professional Papers, Bulletins, Water-Supply Papers, Techniques of Water-Resources Investigations, Circulars, publications of 

general interest (such as leaflets, pamphlets, booklets), single copies 

of Earthquakes & Volcanoes, Preliminary Determination of Epicenters, and some miscellaneous reports, including some of the foregoing series that have gone out of print at the Superintendent of 

Documents, are obtainable by mail from

U.S. Geological Survey, Information Services

Box 25286, Federal Center

Denver, CO 80225

Subscriptions to periodicals (Earthquakes & Volcanoes and 

Preliminary Determination of Epicenters) can be obtained ONLY 

from the

Superintendent of Documents

Government Printing Office

Washington, DC 20402

(Check or money order must be payable to Superintendent of 

Documents.)

Maps

For maps, address mail orders to

U.S. Geological Survey, Information Services

Box 25286, Federal Center

Denver, CO 80225

Residents of Alaska may order maps from

U.S. Geological Survey, Earth Science Information Center

101 Twelfth Ave., Box 12

Fairbanks, AK 99701

OVER THE COUNTER

Books and Maps

Books and maps of the U.S. Geological Survey are available 

over the counter at the following U.S. Geological Survey offices, all 

of which are authorized agents of the Superintendent of Documents

 ANCHORAGE, Alaska-Rm. 101, 4230 University Dr.

 LAKEWOOD, Colorado-Federal Center, Bldg. 810

 MENLO PARK, California-Bldg. 3, Rm. 3128,

345 Middlefield Rd.

 RESTON, Virginia-USGS National Center, Rm. 1C402, 

12201 Sunrise Valley Dr.

 SALT LAKE CITY, Utah-Federal Bldg., Rm. 8105, 

125 South State St.

 SPOKANE, Washington-U.S. Post Office Bldg., Rm. 135, 

West 904 Riverside Ave.

 WASHINGTON, D.C-Main Interior Bldg., Rm. 2650, 

18th and CSts.,NW.

Maps Only

Maps may be purchased over the counter at the following 

U.S. Geological Survey offices:

 FAIRBANKS, Alaska-New Federal Bldg, 101 Twelfth Ave.

 ROLLA, Missouri-1400 Independence Rd.

 STENNIS SPACE CENTER, Mississippi-Bldg. 3101
Palynostratigraphy in Relation to

Sequence Stratigraphy, Straight Cliffs Formation

(Upper Cretaceous), Kaiparowits Plateau, Utah

By Douglas J. Nichols

SEDIMENTOLOGIC AND STRATIGRAPHIC INVESTIGATIONS OF 

COAL-BEARING STRATA IN THE UPPER CRETACEOUS 

STRAIGHT CLIFFS FORMATION, KAIPAROWITS PLATEAU, UTAH

U.S. GEOLOGICAL SURVEY BULLETIN 2115-B

An analysis of the distribution of fossil spores, pollen, and 

dinoflagellate cysts in samples from cores drilled in 

coal-bearing strata independently interpreted according 

to sequence-stratigraphic principles

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1995
U.S. DEPARTMENT OF THE INTERIOR 

BRUCE BABBITT, Secretary

U.S. GEOLOGICAL SURVEY 

Gordon P. Eaton, Director

For sale by U.S. Geological Survey, Information Services

Box 25286, Federal Center

Denver, CO 80225

Any use of trade, product, or firm names in this publication is for descriptive purposes only and 

does not imply endorsement by the U.S. Government

Library of Congress Cataloging-in-Publication Data

Nichols, Douglas J.

Palynostratigraphy in relation to sequence stratigraphy, Straight Cliffs Formation (Upper 

Cretaceous), Kaiparowits Plateau, Utah / by Douglas J. Nichols.

p. cm. (Sedimentologic and stratigraphic investigations of coal-bearing strata in 

the Upper Cretaceous Straight Cliffs Formation, Kaiparowits Plateau, Utah ; B) (U.S. 

Geological Survey bulletin ; 2115)

Includes bibliographical references (p. ).

Supt. of Docs, no.: I 19.3:2115B

1. Palynology Utah Kaiparowits Plateau. 2. Paleobotany Cretaceous. 

3. Geology, Stratigraphic Cretaceous. 4. Straight Cliffs Formation (Utah) 

I. Tide. II. Series. III. Series: U.S. Geological Survey bulletin ; 2115. 

QE75.B9 no. 2115-B 

[QE993]

557.3 s dc20 95-16541 

[551.7'7'0979251] CIP
CONTENTS

Abstract........................................................................................................................... Bl

Introduction..................................................................................................................... 1

Study Area and Materials................................................................................................ 1

Conventional Lithostratigraphy...................................................................................... 5

Tibbet Canyon Member.......................................................................................... 5

Smoky Hollow Member.......................................................................................... 5

John Henry Member................................................................................................ 5

Drip Tank Member.................................................................................................. 6

Sequence Stratigraphy..................................................................................................... 6

Palynostratigraphy.......................................................................................................... 8

Previous Studies...................................................................................................... 8

Analyses of Cores SMP-1-91 and CT-1-91............................................................ 9

Straight Cliffs Palynoflora...................................................................................... 9

Characteristic Species............................................................................................. 10

Palynostratigraphic Zonation.................................................................................. 11

Paleoenvironments.......................................................................................................... 12

Conclusions..................................................................................................................... 16

Taxonomic Notes............................................................................................................ 17

References Cited............................................................................................................. 20

PLATE

[Plate follows references cited]

1. Spores and pollen from the Straight Cliffs Formation.

FIGURES

1. Map of study area, Kaiparowits Plateau, Utah............................................................................................................ B2

2 Lithostratigraphic classification diagram of Turonian through lower Campanian rocks, Kaiparowits Plateau ......... 5

3 Diagram classifying Straight Cliffs Formation by sequence stratigraphy................................................................... 7

4. Diagram of cores SMP-1-91 and CT-1-91.................................................................................................................. 10

5. Chart showing stratigraphic occurrences of palynomorphs in core SMP-1-91........................................................... 13

6. Chart showing stratigraphic occurrences of palynomorphs in core CT-1-91.............................................................. 14

TABLES

1. Palynological samples from core SMP-1-91............................................................................................................... B3

2. Palynological samples from core CT-1-91.................................................................................................................. 4

3. Alphabetical and numerical lists of palynomorph taxa recorded in samples from core SMP-1 -91............................ 15

4. Alphabetical and numerical lists of palynomorph taxa recorded in samples from core CT-1 -91............................... 16

III

Palynostratigraphy in Relation to

Sequence Stratigraphy, Straight Cliffs Formation

(Upper Cretaceous), Kaiparowits Plateau, Utah

By Douglas J. Nichols

ABSTRACT

Selected samples from two cores in the Straight Cliffs 

Formation (middle Turonian-lower Campanian?) in the 

Kaiparowits Plateau, south-central Utah, yielded abundant 

nonmarine and rare marine palynomorphs. The lithostratigraphy of the sampled interval has recently been interpreted 

in accordance with sequence-stratigraphic concepts. The 

palynostratigraphy provides support for some of the new 

interpretations.

Palynomorph assemblages analyzed are primarily from 

the coal-bearing John Henry Member of the Straight Cliffs 

Formation. Most are numerically dominated by spores of 

ferns and other cryptogams and pollen of gymnosperms. Pollen of angiosperms, although less abundant, is common and 

is biostratigraphically useful. The Nyssapollenites albertensis Zone (upper Cenomanian through mid-Coniacian) is 

present in the lower part of the sampled interval, and the Proteacidites retusus Zone (mid-Coniacian through upper Santonian) is present in the upper part. The base of the P. retusus 

Zone coincides with the interpreted position within the cores 

of the A- sequence boundary, in the lower part of the John 

Henry Member. Rare marine dinocysts are present in about 

50 percent of samples interpreted by sedimentological 

criteria as deposited under tidal influence. These palynostratigraphic and paleoecologic data corroborate sedimentologic interpretations of facies within the sequencestratigraphic framework.

The flora of the coal-forming mires of the John Henry 

Member consisted largely of ferns and mosses, with certain 

angiosperms (which possibly were trees) also as major components. Common spores and pollen of the Straight Cliffs 

palynoflora are illustrated, and a new species, Foveotricolporites johnhenryensis, is described.

INTRODUCTION

This report summarizes palynostratigraphic analyses 

of samples collected from two 300-m (meter) cores

drilled in the Straight Cliffs Formation in the Kaiparowits 

Plateau, south-central Utah. The Straight Cliffs Formation 

contains major coal deposits of Late Cretaceous (Coniacian-Santonian) age. Palynostratigraphic analyses serve to 

test some of the sequence-stratigraphic interpretations of 

Shanley (1991), Shanley and McCabe (1991), Shanley 

and others (1992), and Hettinger (1993, 1995) by providing a temporal framework for age-determination and correlation of sequences, by confirming the position of a 

sequence-bounding unconformity as interpreted in the 

cored intervals, and by supporting sedimentological interpretations of depositional environments. Palynological 

analyses of the coal beds also can provide data on floristic composition of coal-forming mires. Finally, these data 

contribute to knowledge of Upper Cretaceous palynology 

of the southern part of the Western Interior.

This report presents initial observations and interpretations of distribution of palynomorphs of marine and nonmarine origin in selected samples from USGS cores SMP-1-91 

and CT-1-91 (Hettinger, 1993, 1995). Results are initial 

because taxonomic study of the palynoflora is preliminary 

and interpretations of occurrence and distribution of palynomorphs rely primarily on presence/absence data. Paleoecologic data presented here are restricted to observations of 

possible marine-tidal influence in some facies within the 

cored intervals and of the floristic composition of mires in 

coastal plain settings.

STUDY AREA AND MATERIALS

The Kaiparowits Plateau covers an area of about 3,600 

km2 in south-central Utah (fig. 1) and incorporates an interval of Upper Cretaceous rocks more than 2 km thick 

(Eaton, 1991; Shanley and McCabe, 1991). The Straight 

Cliffs Formation, of middle Turonian to early Campanian 

age, includes 295-493 m of sandstone-dominated, coalbearing strata of marginal marine, estuarine, and nonmarine 

(fluvial) origin (Peterson, 1969; Eaton, 1991). The formation thickens northward from the Tibbet Canyon area in the

Bl
B2 COAL-BEARING STRATA, KAIPAROWITS PLATEAU, UTAH

112°00' 11 TOO1

37°30'

Figure 1. Map of study area showing Kaiparowits Plateau (shaded), outcrop areas of Straight Cliffs 

Formation (horizontal line pattern), underlying and overlying rocks (no horizontal pattern), and locations of drill sites for cores CT-1-91 and SMP-1-91 (modified from Hettinger, 1995).

southern part of the plateau to the vicinity of Henrieville, 

Utah, in the northwest (Eaton, 1991). The formation is well 

exposed for about 80 km along strike in the northwesttrending Straight Cliffs escarpment, from the vicinity of 

Lake Powell to Escalante, Utah. The marine facies are 

developed predominantly along this east edge of the plateau 

and grade westward to fluvial-dominated facies (Shanley 

and McCabe, 1991). Thick deposits of coal, which are in 

the John Henry Member of the Straight Cliffs Formation 

(Peterson, 1969), are present in the east-central part of the 

plateau, between cliff-forming, stacked, shoreface-sandstone units and alluvial plain deposits to the west (McCabe 

and Shanley, 1992).

The two cores on which the present palynostratigraphic study is based are from U.S. Geological Survey 

drill holes SMP-1-91 and CT-1-91 (Hettinger, 1993, 1995). 

The drill holes are located in the interior part of the Kaiparowits Plateau, respectively in the Ship Mountain Point 

(SMP) and Collet Top (CT) 7.5 minute quadrangles. Both 

holes were spudded near the top of the Straight Cliffs Formation. SMP-1-91 has a total depth (TD) of 293.4 m and 

core was recovered from the interval from 60 to 962.7 ft

(18.3 to 293.4 m). CT-1-91 has a TD of 322.3 m and core 

was recovered from the interval from 141.1 to 1,057.4 ft 

(43.0 to 322.3 m). Units within the Straight Cliffs Formation sampled by these cores (in both conventional and 

sequence-stratigraphic terms) are noted in the following 

sections of this report. Most samples are from the John 

Henry Member of the Straight Cliffs Formation.

Samples discussed in this report are listed in tables 1 

and 2. They were collected at selected intervals from rock 

types having high potential for recovery of palynomorphs. 

These include, for example, carbonaceous shale and gray 

mudrock but exclude sandstone. Coal samples also have 

high potential for recovery of palynomorphs. Except for 

beds measuring only a few centimeters in thickness, all 

coal present in the cores had been removed for other analyses prior to collection of samples listed in table 1. Analyses of selected splits of samples from two of the coal 

beds that were removed are discussed. These samples 

include the floor and roof of each bed and clastic partings 

within the beds in addition to coal. In all, 90 samples were 

analyzed palynologically, 49 from core SMP-1-91 and 41 

from core CT-1-91.
PALYNOSTRATIGRAPHY AND SEQUENCE STRATIGRAPHY, STRAIGHT CLIFFS FORMATION B3

Table 1. Palynological samples from core SMP-1-91.

[USGS Paleobotany Locality Number D7941, including detailed samples of two thick coal beds respectively designated D8020 and D8068. Depths in the core 

are averaged for the detailed samples from the thick coal beds. Depths given in feet are original measurements marked on cores. Depositional environments 

indicated are based on interpretations of Hettinger (1993, 1995). Asterisks denote samples containing marine dinoflagellate cysts]

Sample No.

D7941-EE

D7941-DD

D7941-CC

D7941-BB

D7941-AA

D7941-Z

D7941-Y

D7941-X

D7941-W

D7941-V

D7941-U

D7941-T

D7941-S

D7941-R

D7941-Q

D8020-M

D8020-L

D8020-K

D8020-J

D8020-I

D8020-H

D8020-G

D8020-F

D8020-E

D8020-D

D8020-C

D8020-B

D8020-A

D7941-P

D7941-O

D7941-N

D7941-M

D7941-L

D8068-EE

D8068-Z

D8068-O

D8068-D

D8068-A

D7941-K

D7941-J

D7941-I

D7941-H

D7941-G

D7941-F

D7941-E

D7941-D

D7941-C

D7941-B

D7941-A

Depth in core

75.9ft (23.1m)

165.0ft (50.3m)

187.2ft (57.0m)

205.5 ft (62.6 m)

233.4ft (71.1m)

247.2ft (75.3m)

306.5 ft (93.4 m)

321.0ft (97.8m)

344. 1ft (104.9m)

351.8 ft (107.2m)

378.2 ft (1 15.3 m)

396.9 ft (121.0m)

474.3 ft (144.6 m)

547.8 ft (167.0 m)

580.5 ft (176.9 m)

177.1 m

177.2 m

177.9 m

180.4m

181.1m

181.2m

181.7m

182.3 m

182.8 m

183.3m

183.6m

183.7 m

183.8m

615.6 ft (187.6m)

636.2 ft (193.9 m)

655.0 ft (199.6m)

680.3 ft (207.4 m)

732. 1ft (223. 1m)

231.3m

234.0 m

236.8 m

237.5 m

238.1 m

786.8 ft (239.8 m)

796.2 ft (242.7 m)

803.0 ft (244.8 m)

832.5 ft (253.7 m)

835.9 ft (254.8 m)

868. 1ft (264.6m)

871.9 ft (265.8 m)

876.5 ft (267.2 m)

902.7 ft (275. 1m)

927.9 ft (282.8 m)

947.5 ft (288.8 m)

Rock type

mudrock

carbonaceous mudrock

mudrock

mudrock

carbonaceous mudrock

carbonaceous mudrock

carbonaceous shale

carbonaceous shale

mudrock

mudrock

carbonaceous shale

coal

shale

carbonaceous shale

mudrock

carbonaceous shale

coal

coal

coal

coal

coal

coal

coal

coal

coal

coal

coal

mudrock

mudrock

carbonaceous shale

carbonaceous shale

mudrock

mudrock

shale

coal

shale (parting)

coal

shale (parting)

carbonaceous shale

mudrock

mudrock

carbonaceous shale

carbonaceous shale

carbonaceous shale

carbonaceous shale

carbonaceous shale

coal

siltstone

shale

Dep. environment

fluvial channel

floodplain

floodplain

floodplain

floodplain

floodplain

floodplain

floodplain *

tidal

floodplain

floodplain

mire

tidal

floodplain

floodplain

floodplain

mire

mire

mire

mire

mire

mire

mire

mire

mire

mire

mire

floodplain

tidal *

floodplain

floodplain

tidal

tidal

floodplain

mire

floodplain

mire

floodplain

floodplain

tidal

floodplain

tidal *

floodplain

floodplain *

tidal *

floodplain

mire

floodplain

floodplain
B4 COAL-BEARING STRATA, KAIPAROWITS PLATEAU, UTAH

Table 2. Palynological samples from core CT-1-91.

[USGS Paleobotany Locality Number D7993. Depositional environments indicated are based on interpretations of Hettinger (1993,1995). Asterisks denote samples containing marine dinoflagellate cysts. Sample D7993-B was barren of palynomorphs]

Sample No.

D7993-PP

D7993-OO

D7993-NN

D7993-MM

D7993-LL

D7993-KK

D7993-JJ

D7993-II

D7993-HH

D7993-GG

D7993-FF

D7993-EE

D7993-DD

D7993-CC

D7993-BB

D7993-AA

D7993-Z

D7993-Y

D7993-X

D7993-W

D7993-V

D7993-U

D7993-T

D7993-S

D7993-R

D7993-Q

D7993-P

D7993-0

D7993-N

D7993-M

D7993-L

D7993-K

D7993-J

D7993-I

D7993-H

D7993-G

D7993-F

D7993-E

D7993-D

D7993-C

D7993-B

D7993-A

Depth in core

153.4ft (46.8m)

207.5 ft (63.2 m)

214.6 ft (65.4 m)

244.1ft (74.4m)

263.5 ft (80.3 m)

298.3 ft (90.9 m)

327.7 ft (99.9 m)

348.2 ft (106. 1m)

377.0 ft (114.9m)

386.2 ft (117.7m)

397.8 ft (121. 3m)

438.9 ft (133.8m)

450.3 ft (137.3m)

464.7 ft (141. 6m)

466.9 ft (142.3 m)

482.2 ft (147.0 m)

490.4 ft (149.5 m)

518.5 ft (158.0m)

524.1 ft (159.8 m)

538.5 ft (164.1 m)

567.9 ft (173. 1m)

602.2 ft (183.6m)

630.0 ft (192.0m)

647.3 ft (197.3 m)

653.4 ft (199.2 m)

654.8 ft (199.6 m)

662.5 ft (201.9 m)

677.4 ft (206.5 m)

730.5 ft (222.7 m)

732.5 ft (223.3 m)

782.2 ft (238.4 m)

824.2 ft (25 1.2m)

853.0 ft (260.0 m)

855.6 ft (260.8 m)

861.3 ft (262.5 m)

886.2 ft (270. 1m)

988. 1ft (301.2m)

989.5 ft (301. 6m)

990.5 ft (301. 9m)

1,015.1 ft (309.4m)

1,043.0 ft (317.9m)

1,046.5 ft (3 19.0m)

Rock type

mudrock

mudrock

carbonaceous mudrock

mudrock

mudrock

mudrock

mudrock

mudrock

carbonaceous mudrock

mudrock

mudrock

carbonaceous shale

mudrock

carbonaceous mudrock

mudrock

mudrock

mudrock

mudrock

carbonaceous mudrock

mudrock

mudrock

mudrock

carbonaceous mudrock

mudrock

mudrock

mudrock

carbonaceous shale

mudrock

mudrock

mudrock

mudrock

mudrock

shale

coal

coal

shale

coal

carbonaceous shale

carbonaceous shale

mudrock

mudrock

mudrock

Dep. environment

fluvial channel

floodplain

floodplain

floodplain

floodplain

floodplain

tidal

tidal

tidal

tidal *

tidal

floodplain *

floodplain

floodplain

floodplain

tidal *

floodplain

tidal *

tidal*

tidal*

tidal

tidal*

floodplain

tidal

floodplain

floodplain *

floodplain

floodplain

tidal

tidal *

shoreface *

floodplain

tidal *

mire

mire

tidal *

mire

floodplain

floodplain

floodplain

floodplain

floodplain
PALYNOSTRATIGRAPHY AND SEQUENCE STRATIGRAPHY, STRAIGHT CLIFFS FORMATION B5

CONVENTIONAL 

LITHOSTRATIGRAPHY

The Straight Cliffs Sandstone was named by Gregory and Moore (1931). Peterson and Waldrop (1965) 

later applied the name Straight Cliffs Formation to the 

succession of marine and nonmarine strata that includes 

fine-grained clastic rocks and coal as well as sandstone. 

The Straight Cliffs Formation overlies the Tropic Shale 

(upper Cenomanian to middle Turonian) and underlies the 

Wahweap Formation (Campanian). Peterson (1969) 

named four members within the Straight Cliffs Formation, from oldest to youngest the Tibbet Canyon, Smoky 

Hollow, John Henry, and Drip Tank Members (fig. 2). 

All of these members have their type localities near the 

south edge of the plateau. As described by Peterson, the 

Straight Cliffs Formation ranges in age from middle Turonian to approximately early Campanian. Peterson also 

described a major unconformity within the Straight Cliffs 

Formation that apparently represents a significant amount 

of geologic time. Based on various interpretations of the 

ages of molluscan fossils from the Tibbet Canyon Member 

and lower part of the John Henry Member, the missing 

time includes the late Turonian through middle Coniacian 

(Peterson, 1969), late Turonian through late Coniacian 

(Peterson and Kirk, 1977), or the late Turonian (Eaton, 

1991).

Upper Cretaceous (part)

Stage

Campanian 

(part)

Santonian

Coniacian

Turonian

Formation

Wahweap 

Formation

Straight 

Cliffs 

Pormatl,p,m

,

s

=

«

H

Tropic 

Shale 

(part)

Member

Drip Tank 

Member

John Henry 

Member

Smoky Hollow 

Member

Tibbet Canyon 

Member

Figure 2. Conventional lithostratigraphic classification of Turonian through lower Campanian rocks in the Kaiparowits Plateau 

(modified from Eaton, 1991).

TIBBET CANYON MEMBER

At its type locality the Tibbet Canyon Member is about 

32 m thick and consists largely of sandstone (Peterson, 

1969). Its lower contact with the marine Tropic Shale is gradational, but its upper contact with the Smoky Hollow Member is sharp. Peterson interpreted that the Tibbet Canyon 

Member was deposited in shallow marine and beach environments because it contains cephalopods, inoceramid pelecypods, shark teeth, and trace fossils.

An age of middle Turonian for the Tibbet Canyon 

Member is based on the presence of a species of Inoceramus 

indicative of the Prionocyclus hyatti ammonite zone (Peterson, 1969; Eaton, 1991). The Tibbet Canyon Member is progradational, and it evidently ranges in age from early middle 

Turonian (Collignoniceras woollgari woollgari zone) in the 

southwestern part of the plateau to late middle Turonian (P. 

hyatti zone) in the central and eastern parts (Shanley, 1991).

SMOKY HOLLOW MEMBER

At its type locality the Smoky Hollow Member consists 

of about 35 m of interbedded sandstone, mudrock, carbonaceous shale, and coal; it increases in thickness to about 101 

m near Escalante, Utah (Peterson, 1969). Peterson interpreted the Smoky Hollow to have been deposited in nonmarine fluvial, lagoonal, and paludal environments. It includes 

three informal units: a basal coal zone, a middle barren zone, 

and an upper unit called the Calico bed. The Calico bed is a 

distinctive light-gray to white sandstone containing quartz 

and chert pebbles and lenses of conglomerate. The previously mentioned major unconformity within the Straight 

Cliffs Formation was interpreted by Peterson (1969) as being 

at the top of the Calico bed.

The barren zone has yielded vertebrate fossils including 

rare mammals of probable Turonian age (Eaton, 1991). The 

Turonian age is determined on the basis of stratigraphic position, because the Smoky Hollow Member is not well dated 

directly.

JOHN HENRY MEMBER

The John Henry Member consists of interbedded sandstone, mudrock, carbonaceous shale, and coal. At its type 

locality it is about 226 m thick, but it thickens to about 329 

m in the northeastern part of the plateau (Peterson, 1969). 

Most of the coal in the Straight Cliffs Formation is in the 

lower part of the John Henry Member. In the central and 

southwestern parts of the plateau, the member comprises a 

lower coal zone, lower barren zone, the Christensen coal 

zone, a middle barren zone, the Rees coal zone, and an upper 

barren zone (Peterson, 1969). In the southwestern and central parts of the plateau, the member is largely of nonmarine
B6 COAL-BEARING STRATA, KAIPAROWITS PLATEAU, UTAH

(fluvial, floodplain, paludal, and lagoonal) origin (Peterson, 

1969) but includes beds deposited under tidal influence, as in 

tidal creeks and estuaries (Shanley and McCabe, 1991). In 

the northeastern part of the plateau, the John Henry comprises a lower marine mudrock tongue, four prominent 

marine sandstone units respectively designated A- through 

D-, an upper marine mudrock tongue, the marine G- sandstone, and the Alvey coal zone (Peterson, 1969). In this area 

the member is interpreted to be predominantly marine in origin and to include beach, shallow water, and offshore 

deposits (Peterson, 1969). The sandstone units form the 

Straight Cliffs escarpment. Among these units, the A- sandstone has proved to be the most important in recent reinterpretations of the stratigraphic framework of the John Henry 

Member.

The age of the John Henry Member probably ranges 

from Coniacian through Santonian and possibly includes the 

early Campanian, based on marine mollusks; however, interpretations of the age of these fossils vary. Collections 

reported by Peterson (1969) come from the lower marine 

mudrock tongue, the A- sandstone, the upper marine 

mudrock tongue, and the G- sandstone. Peterson (1969) cited 

an age of middle or late Coniacian for mollusks from the 

basal part of the member, but later (Peterson and Kirk, 1977) 

revised that age determination to early Santonian. Eaton 

(1991) contended that these fossils are more likely early 

Coniacian in age. He cited the occurrence of the inoceramid 

Volviceramus involutus and quoted E.G. Kauffman (University of Colorado) as stating that this species is early Coniacian, but this age designation appears to be incorrect. The 

zone of this species is equivalent to that of the ammonite 

Scaphites ventricosus, which is middle to upper Coniacian. 

(See also Shanley, 1991.) Peterson (1969) cited an age of 

Santonian for the middle part of the John Henry. For the 

upper part of the member he cited an age of early Campanian, but Eaton (1991) concluded that the member is no 

younger than late Santonian (Desmoscaphites bassleri 

zone). Shanley (1991) reported that the fossils from the same 

collection belong to the Scaphites hippocrepis zone, which is 

early Campanian in age. Palynostratigraphic evidence from 

the present study on the age of the John Henry Member is 

discussed later.

DRIP TANK MEMBER

The Drip Tank Member is a cliff-forming sandstone 

unit at the top of the Straight Cliffs Formation, the informally designated upper sandstone member of Peterson and 

Waldrop (1965). At its type locality it is about 43 m thick, 

but it may be as much as 159 m thick to the northwest (Peterson, 1969). The Drip Tank is interpreted to be of fluvial origin (Peterson, 1969).

The Drip Tank Member contains no age-diagnostic fossils. Its age was inferred to be early Campanian by Peterson 

(1969), based on the age of the underlying John Henry

Member, which he took to be early Campanian in its uppermost part. Eaton (1991) suggested that the age of the Drip 

Tank Member is constrained by his interpreted late Santonian age of the uppermost John Henry Member and a presumed early Campanian age for the overlying Wahweap 

Formation.

SEQUENCE STRATIGRAPHY

Shanley (1991) and Shanley and McCabe (1991) reinterpreted the stratigraphy of the Straight Cliffs Formation in 

the Kaiparowits Plateau according to the concepts and principles of sequence stratigraphy. The concepts hold that sedimentary sequences are deposited in response to creation of 

accommodation space that, in nearshore and coastal plain 

strata, is controlled by changes in relative sea level. The 

changes in sea level are produced by the interaction of basin 

subsidence and eustasy. Because much of the Straight Cliffs 

Formation is of nonmarine origin, Shanley (1991) and Shanley and McCabe (1991) related their sequence-stratigraphic 

interpretations to changes in base level, although ultimately 

these changes also are governed by relative sea level. Their 

reinterpretation provides a new view of the depositional 

architecture of the Straight Cliffs Formation. Shanley and 

McCabe found that the existing, conventional lithostratigraphic classification and nomenclature are not useful in 

their reinterpretation, and they developed an alternative subdivision of the interval to describe their results. This section 

outlines only the broadest aspects of their new interpretations as they pertain to palynostratigraphy; readers are 

referred to Shanley and McCabe (1991) and Hettinger 

(1995) for more complete discussions.

Sequence-stratigraphic classification of the upper part 

of the Tropic Shale and the overlying Straight Cliffs Formation suggests that this interval is formed of five depositional 

sequences, each of which contains highstand and transgressive systems tracts (fig. 3). The sequences are separated by 

four sequence-bounding unconformities. These sequence 

boundaries are recognized by abrupt basinward shifts in 

facies across erosional surfaces, which developed in 

response to lowering of base level. Two of the unconformities are major and two are minor (none should be confused 

with the unconformity interpreted to be at the base of the 

John Henry Member by Peterson, 1969).

The lower of the two major unconformities is the Calico 

sequence boundary. It is at the base of the Calico bed, and it 

separates pebbly sandstone and conglomerate (braided-river 

deposits) of the Calico bed from underlying sandstone, siltstone, and carbonaceous shale (coastal plain deposits). The 

juxtaposition of these different facies across an erosion surface having as much as 40 m of relief is evidence for the 

existence of a regional unconformity and a corresponding 

basinward shift in facies. Shanley and McCabe (1989) interpreted the Ferron Sandstone Member of the Mancos Shale, 

which lies northeast of the Kaiparowits Plateau, as the
PALYNOSTRATIGRAPHY AND SEQUENCE STRATIGRAPHY, STRAIGHT CLIFFS FORMATION B7

50 m

 * *** v&

HST

Drip Tank

Member

John Henry

Member

Smoky Hollow

Member

Tibbet Canyon

Member

c

o

CO

E

o

LL

i

o

O) "co

CO

Tropic Shale (part)

d.^-

co .0.

c

CO

"co

CO

CO

CO "o

CO 'c

8

CO "c

o

H

Figure 3. Sequence-stratigraphic classification of the Straight Cliffs Formation (conventional classification shown 

at right for comparison). Outcrop section at left is in southwestern part of Kaiparowits Plateau; section at right is in 

central part of Straight Cliffs escarpment on east edge of the plateau; they are about 60 km apart. HST, highstand 

systems tract; TST, transgressive systems tract; s.b., sequence boundary. Dashed lines indicate correlations of condensed sections and their alluvial equivalents; gaps in outcrop section at right are positions of covered nonmarine 

intervals, including coal-bearing strata; varying positions of sequence boundaries between outcrop sections are based 

on data from partial outcrop sections not shown. Diagram modified from Shanley and McCabe (1991) with their 

interpretations of depositional environments omitted.

basinward deposits equivalent to the hiatus at the Calico 

sequence boundary. The second major unconformity is near 

the top of the Straight Cliffs Formation. It is the Drip Tank 

sequence boundary, and it lies near the base of the Drip Tank 

Member. It separates coarse-grained braided-river deposits 

from underlying fine-grained fluvial, coastal plain, and 

shoreface deposits.

The two comparatively minor but still significant 

unconformities are the Tibbet sequence boundary and the 

A- sequence boundary. The Tibbet sequence boundary is 

an extensive erosion surface within the Tibbet Canyon 

Member of conventional lithostratigraphy, and it separates estuarine valley-fill deposits from underlying shoreface sandstone. The A- sequence boundary is within the 

John Henry Member. It is an extensive erosional surface 

that separates coarse-grained estuarine valley-fill deposits 

from underlying fine-grained coastal plain deposits and

shoreface sandstone. At the east edge of the plateau this 

unconformity is located within the A- sandstone of Peterson (1969).

The sequence boundaries separate deposition al 

sequences that include transgressive and highstand systems 

tracts. (Apparently it is conventional that sequences are 

named after the lowest stratigraphic unit within them. Therefore, the terminology applied to these sequences mimics, but 

is only partially equivalent to, the conventional lithostratigraphic names. The application of a different set of terms 

would have been less of a potential source of confusion.) No 

special name is given to the interval below the Tibbet 

sequence boundary, a highstand systems tract that includes 

the upper part of the Tropic Shale and the lower part of the 

Tibbet Canyon Member (Figure 3 illustrates these systems 

tract relationships.) The interval between the Tibbet and Calico sequence boundaries is the Tibbet sequence. It consists of
B8 COAL-BEARING STRATA, KAIPAROWITS PLATEAU, UTAH

estuarine valley-fill deposits overlain by coastal plain strata. 

The valley-fill deposits are interpreted as a transgressive systems tract, and the coastal plain deposits as a highstand systems tract. The interval above the Calico sequence boundary 

is the Calico sequence. It consists of braided-river deposits 

(the Calico bed) that grade upward into tidally influenced 

fluvial strata capped by shoreface deposits; this part of the 

interval is interpreted as a transgressive systems tract. Overlying the transgressive systems tract of the Calico sequence 

is a highstand systems tract consisting of stacked shoreface 

parasequences that grade westward into coastal plain and 

alluvial deposits. The interval above the A- sequence boundary is the A- sequence. The basal part of this interval consists 

of tidally influenced fluvial and estuarine deposits (transgressive systems tract), and the thick, upper part of this interval consists of stacked shoreface parasequences that grade 

westward into coastal plain and alluvial strata (highstand 

systems tract). These deposits constitute most of the John 

Henry Member of conventional lithostratigraphy and 

include most of the thick coal beds of the Straight Cliffs Formation. The interval above the Drip Tank sequence boundary is the Drip Tank sequence.

An important aspect of the sequence stratigraphy study 

in the Kaiparowits Plateau is the recognition of marine tidal 

deposits and tidally influenced fluvial deposits in nonmarine 

settings. As mentioned, in the eastern part of the plateau the 

transgressive systems tract above the Calico sequence 

boundary consists of braided-river deposits that grade 

upward into estuarine deposits. These beds have sedimentary 

structures characteristic of tidal influence (Shanley and others, 1992). Transgression continued from east to west. In the 

western part of the plateau, the chronostratigraphically correlative intervals above the Calico sequence boundary are 

braided-river deposits overlain by fluvial-plain deposits that 

are in turn overlain by tidally influenced alluvial deposits. 

These tidally influenced beds, which are 60 km or more from 

the shoreline, represent maximum flooding and are equivalent to the condensed marine section to the east. Estuarine or 

tidally influenced deposits are recognized also in the lower 

part of the Tibbet sequence and in the lower part of the Asequence. The transgressive systems tract in the A- sequence 

includes tidally influenced channel deposits overlain by 

marine sandstone in the eastern part of the plateau and a succession of alluvial channel deposits overlain by tidally influenced alluvial deposits in the western part. In addition to 

sedimentary structures indicative or suggestive of tidal influence, Shanley (1991), Shanley and McCabe (1991), and 

Shanley and others (1992) used brackish-water trace fossils 

to identify tidal deposits. Hettinger (1993, 1995) similarly 

used sedimentary structures observable in cores SMP-1-91 

and CT-1-91 to identify such deposits. Palynological analysis of such deposits also can help in their recognition because 

marine dinoflagellate cysts may be preserved. These palynomorphs represent motile algae that inhabited marine and

brackish water. They can be present in estuaries, tidal channels, and rivers whose flow is periodically reversed by tides.

PALYNOSTRATIGRAPHY

PREVIOUS STUDIES

Pertinent previous studies of Cretaceous palynology of 

the region are limited in number. The most directly relevant 

study is that of Orlansky (1971). Orlansky described and 

illustrated 124 palynomorph species from 20 samples of the 

Straight Cliffs Formation in outcrop near Henrieville, Utah 

(fig. 1). His study included discussions of seven species of 

marine dinoflagellates in addition to spores and pollen of terrestrial plants. Although an important contribution when 

published, subsequent changes in taxonomic concepts and 

the nomenclature of fossil spores and pollen have rendered 

much of Orlansky's taxonomy and nomenclature unreliable. 

May (1972) illustrated but did not describe palynomorphs 

from coal-bearing strata in Utah, including the Straight 

Cliffs Formation as exposed in a coal field in the northeastern part of the Kaiparowits Plateau. A photographic plate 

published by May (1972, pi. 13) is of some value in identification of the palynomorph species he recovered, but his biostratigraphic and paleoecologic conclusions are misleading 

because they are inadequately documented within his text or 

by comparative studies.

Some previous palynologic studies in adjacent areas 

pertain to the present investigation. A study of a correlative 

Upper Cretaceous interval in the San Juan Basin of northwestern New Mexico was conducted by Tschudy (1976). No 

illustrations of palynomorphs are included in this report, but 

the taxonomy is sufficiently detailed for it to be used to 

establish a palynostratigraphic framework. Tschudy's 

(1980) survey of records of Normapolles pollen in the Western United States, which includes photomicrographs, is useful and effective for verifying identifications of some of the 

taxa discussed in his earlier report.

The most recent and most thorough taxonomic study in 

the southern Western Interior region is that of Jameossanaie 

(1987). Jameossanaie described and illustrated 172 species 

of spores and pollen from Upper Cretaceous coal-bearing 

deposits in northwestern New Mexico. His taxonomy and 

nomenclature are current, and his specimens are well illustrated in 12 photographic plates. However, the interval discussed by Jameossanaie evidently is younger than the 

Straight Cliffs Formation in Utah.

The palynostratigraphic zonation of the Upper Cretaceous that has application in the study area is that of Nichols 

and others (1982). They defined biozones using both marine 

and nonmarine palynomorphs that are of potential utility in 

the study area, although these biozones are based on stratotype sections in Wyoming and Montana and their utility in 

southern Utah was previously untested. The study by
PALYNOSTRATIGRAPHY AND SEQUENCE STRATIGRAPHY, STRAIGHT CLIFFS FORMATION B9

Nichols and others (1982) was updated recently (Nichols, 

1994). Results from the study of the Kaiparowits cores show 

that two of these biozones in fact are present in southern 

Utah.

ANALYSES OF CORES SMP-1-91 AND CT-1-91

Ninety-one samples were collected and processed for 

this study, 49 from core SMP-1-91 (14 coal; 35 non-coal) 

and 42 from core CT-1-91 (3 coal; 39 non-coal, one of which 

was barren). Because more samples were available from that 

core, detailed analyses concentrated on SMP-1-91, which 

served as a standard for biostratigraphic (palynostratigraphic) interpretations, and CT-1-91 was used to verify 

results. Samples from SMP-1-91 include two series from 

thick coal beds here designated D8020 and D8068, respectively (fig. 4). Both are within the John Henry Member, but 

their importance especially concerns the sequencestratigraphic interpretation of the Straight Cliffs Formation. 

Coal bed D8020 is 6.5 m thick and is near the middle of the 

A- sequence; coal bed D8068 is 4.3 m thick and is at the base 

of the A- sequence (just above the A- sequence boundary). 

D8020 serves as a representative of the thick coal beds in the 

A- sequence, and D8068 provides close biostratigraphic 

control useful for confirmation of the position of the Asequence boundary.

Distribution of 56 palynomorph taxa in the cores was 

recorded in this study. Among these taxa are several at the 

genus level that include more than one species; thus the 

occurrences and distribution of 70 or more palynomorph 

species are considered. Pteridophyte spores and gymnosperm pollen are common but have little biostratigraphic 

importance. Species of angiosperm pollen known or thought 

to have biostratigraphic importance received special attention in this study, as did dinoflagellate cysts (recorded as a 

single category) that are indicative of tidal influence in the 

depositional environment. Percentage relative abundance of 

palynomorph taxa was determined for coal samples, to determine the composition of mire floras; semiquantitative evaluations of relative abundance were recorded for most other 

samples.

STRAIGHT CLIFFS PALYNOFLORA

A survey of the samples from cores SMP-1-91 and 

CT-1-91 shows that the palynoflora of the Straight Cliffs 

Formation is numerically dominated by spores of ferns 

and other cryptogams and pollen of gymnosperms, 

although angiosperm pollen, primarily small tricolpate 

forms, is numerically abundant in most samples as well. 

The commonly occurring species are well known in 

Upper Cretaceous rocks of the Western Interior of North 

America. However, some of the less common species

(especially angiosperm pollen) serve to distinguish the 

Straight Cliffs palynoflora from others of the same age. A 

brief overview of the entire palynoflora follows.

The most commonly occurring spores are: species of 

the fern spore genera Gleicheniidites and Laevigatosporites (both of which are present in 65-85 percent 

of samples in each core and numerically dominant in 

some), species of the bryophyte spore genus Stereisporites (sphagnum moss; present in 50-70 percent of 

samples and abundant in several, notably in coal), and 

species of the fern spore genera Cyathidites and Reticuloidosporites (present in 45-60 percent of samples and common in many). Gleicheniidites spp. and Stereisporites 

spp. are especially common in coal samples, although 

they are also common in non-coal samples.

The most commonly occurring species of gymnosperm pollen in the Straight Cliffs Formation belong to the 

genera Corollina, Araucariacites, Pityosporites, and Taxodiaceaepollenites. These are present in 45-65 percent of 

the samples, but they tend not to be numerically abundant. Corollina, occurring usually as monads but also as 

tetrads, is present throughout the sampled interval, in all 

members of the formation, and is notably abundant in a 

few samples. Specimens assignable to species of the other 

three genera are extremely rare or absent in the coal samples analyzed in this study. This pattern of distribution in 

the Kaiparowits samples is especially significant for pollen 

of Taxodiaceaepollenites because this pollen is produced 

in great quantities by trees that are the principal component of swamp-forest vegetation in many Paleocene coaldepositional environments in the Western United States. 

Evidently these arboreal gymnosperms were not significant components of mire floras in the Kaiparowits area in 

Late Cretaceous time.

Angiosperm pollen is present throughout the Straight 

Cliffs Formation. Nondescript tricolpate pollen referable to 

the genera Cupuliferoidaepollenites, Tricolpites, and (or) 

Retitricolpites is present in almost every sample. This pollen, which probably has fagaceous or platanaceous affinity, is numerically abundant in many samples and 

dominant in some. Evidently it represents a major component of the flora. However, because pollen of this morphology is widespread both geographically and 

stratigraphically, and is of somewhat uncertain botanical 

affinity, it has little paleoecologic and no biostratigraphic 

value. Other angiosperm pollen of more distinctive morphology present at least in low numbers in many samples 

of the Straight Cliffs Formation belongs to species of the 

tricolporate genera Nyssapollenites and Foveotricolporites 

and the triporate genera Triporopollenites, Plicapollis, 

Pseudoplicapollis, and Proteacidites. Some of these species are useful in characterizing the formation palynologically and in interpreting it palynostratigraphically.
BIO COAL-BEARING STRATA, KAIPAROWITS PLATEAU, UTAH

SMP-1-91

to 

a.

c

0

CD

E 

o

LL

Straight (

5 <a o

Q. vJ

O ^

John Henry Member

O 1^7

1 a

fl

CO

25m50 

75-

100- 

125 

150 

175-

200-

250-

275-

'..:' ;. ;". V.i'. 

'. j ;i ;."'.f ;.;, ;::/ -.

. . ; : ,'.

^:'*&J}ii

E_^_^^^

:^^:^^

?i=J^i^^

b-^^r^-^

^ ^ ^^^ ^ H

J^J^-^^i^^

_-_-_-_-_-_-

 ".' '. :.-;:""'

.~~..~ ~.~-~

. ' '.' ' - " . ' :

^SSS?^:

^

 

-_^-_-_^-^

^;^-z-z^^

^^_-^_-^_-^_-^_-

- D7941-EE

50 m 

Drip Tank sequence

boundary

-D7941-DD 

-D7941-CC 

-D7941-BB 75 "*"

-D7941-AA 

-D7941-Z

100 -

-D7941-Y 

-D7941-X

-D7941-W

-D7941-V 125

-D7941-U

-D7941-T

150- 

-D7941-S

175- 

-D7941-R

-D7941-Q 

-D8020-A to -M

200- 

-D7941-P 

-D7941-0

-D7941-N

-D7941-M

225 -

-D7941-L 

"D8068-Ato-EE

-D7941-K^ , 

 D7941-I J "^ ^"^So

-D7941-G, H nclQry - ^

275 - 

- D7941-D, E, F

-D7941-C

-D7941-B

300 -

-D7941-A

 :,:'y-:;-;<;^:.'

^T^r^:C"C^

 

. :" . ' . . -." '. :;" :;.-; /

=.^^^-^-

 ^S""333"

'ii£j£&

^^^^B

: ". .' . -: '- ' '-.

-^^^^^^

D7993-PP 

D7993-NN, 00

-D7993-MM 

D7993-LL

- D7993-KK

D7993-JJ 

D7993-II

D7993-GG, HH 

D7993-FF

D7993-EE 

D7993-DD 

D7993-BB, CC

D7BB3-Z, AA

D7993-X,Y 

D7993-W

D7993-V 

hD7993-U

D7993-T 

D7993-S 

D7993-Q, R 

D7993-P 

D7993-0

D7993-M, N

D7993-L 

D7993-K

D7993-H, I, 

D7993-G

D7993-D, E, F

- D7993-C

- D7993-A, B

EXPLANATION

Sandstone, conglomeratic

Sandstone, crossbedded

Sandstone, swaley bedded 

or massive

Interbedded sandstone 

and mudrock

Mudrock and shale

Coal

Figure 4. Generalized lithostratigraphy of cores SMP-1-91 and CT-1-91, approximate positions of palynological samples, and inferred 

correlations between the cores (modified from Hettinger, 1993). Datum is the Drip Tank sequence boundary, which is coincident with the 

contact between the John Henry and Drip Tank Members in the cores. Scale in meters (m) is depth in core.

CHARACTERISTIC SPECIES

Foveotricolporitesjohnhenryensis n. sp. is perhaps the 

single most characteristic species in the Straight Cliffs 

palynoflora (pi. 1, figs. 17-20). It is distinctive in appearance

and relatively common in occurrence, being present in about 

one-third of all samples of the John Henry Member (it was 

not recorded in the few Smoky Hollow and Drip Tank Member samples examined). It was not reported in previous studies of the Straight Cliffs Formation by either Orlansky
PALYNOSTRATIGRAPHY AND SEQUENCE STRATIGRAPHY, STRAIGHT CLIFFS FORMATION Bll

(1971) or May (1972). A formal description of this tricolporate pollen species is given later in "Taxonomic Notes."

A second tricolporate species occurring in the Straight 

Cliffs Formation is less typical of the formation but is 

palynostratigraphically significant; that species is Nyssapollenites albertensis (pi. 1, fig. 16). It is present in the Smoky 

Hollow Member and throughout the John Henry Member 

(Tibbet and Calico sequences and above); it was not 

observed in the Drip Tank Member (Drip Tank sequence). It 

is significant because it (along with some other species) 

defines a major palynostratigraphic zone, which is discussed 

later.

Other characteristic species in the Straight Cliffs 

palynoflora are triporate angiosperm pollen. They are species of the Normapolles genera Plicapollis and Pseudoplicapollis, and species of Proteacidites. Plicapollis rusticus (pi. 

1, fig. 15) was originally described from the upper Campanian of Tennessee by Tschudy (1975). Later he reported it 

from the Crevasse Canyon Formation (Coniacian and Santonian) and the basal part of the Menefee Formation (Santonian) in northwestern New Mexico (Tschudy, 1976, 1980). 

This species was not reported previously from the Straight 

Cliffs Formation by either Orlansky (1971) or May (1972). 

Plicapollis rusticus is present in the middle part of the John 

Henry Member, however, both below and above the Asequence boundary. Species of Pseudoplicapollis in the 

Straight Cliffs are P. cuneata and P. triradiata. P. cuneata 

(pi. 1, fig. 13) was first described from Santonian of the 

Atlantic Coastal Plain (Christopher, 1979) and later reported 

from the lower Campanian of New Mexico by Jameossanaie 

(1987), who also described P. triradiata from the same 

deposits. Orlansky (1971, pi. 10, fig. 37) illustrated a specimen that appears to be P. triradiata (although he identified 

it as a species of Cupanieidites). In the Straight Cliffs Formation these species are present above the A- sequence 

boundary; P. triradiata is present also above the Drip Tank 

sequence boundary.

The occurrences of Proteacidites deserve special mention. Species of this triporate pollen genus characterize the 

Upper Cretaceous of the Western Interior of North America. 

Nichols and Jacobson (1982) reviewed all available records 

of its occurrence and determined that its stratigraphic range 

in the region is Coniacian through Maastrichtian. The genus 

has been reported previously in the Straight Cliffs Formation 

by Orlansky (1971) and May (1972). Species are difficult 

to distinguish, and in this study they are grouped under the 

name Proteacidites spp. (pi. 1, figs. 11-12). Proteacidites 

spp. is present in the John Henry Member in about half of all 

samples above the interpreted position of the A- sequence 

boundary and in the Drip Tank Member, that is, within the 

A- and Drip Tank sequences.

In addition to Proteacidites spp., other species of triporate pollen are present in the Straight Cliffs palynoflora, 

occurring in 50 percent or more of samples of the John Henry 

Member. In this study they were recorded as species of the

form genus Triporopollenites, but some may belong to genera of the Normapolles complex other than Plicapollis and 

Pseudoplicapollis. Tschudy (1980) recognized Vacuopollis 

among specimens illustrated by Orlansky (1971, pi. 10, figs. 

34-35). Orlansky (1971, pi. 10, figs. 31-32) illustrated two 

other specimens that he identified as Sporopollis sp. They do 

not belong to that genus, but appear to closely resemble 

specimens identified by Jameossanaie (1987, fig. 16, specimens 41-44 only) from Campanian rocks in New Mexico as 

Complexiopollis abditus. Similar specimens were observed 

in the present study, but their identification was not verified 

because they are very rare and consequently of less importance palynostratigraphically than the species of Foveotricolporites, Plicapollis, Pseudoplicapollis, and Proteacidites 

discussed previously.

Finally, the presence ofArecipites spp. (pi. 1, figs. 7-8) 

in the Straight Cliffs Formation is noteworthy. This occurrence may be the stratigraphically oldest record in North 

America of the genus, which has affinity with the Arecaceae 

(palm family). Palms have long been considered to be an 

important component of Cretaceous floras, but their preMaastrichtian pollen record is not well documented. In the 

Straight Cliffs Formation, pollen of Arecipites is present 

sporadically throughout the Coniacian-Santonian John 

Henry Member.

PALYNOSTRATIGRAPHIC ZONATION

On the basis of occurrences of key palynomorph taxa, 

two of the Upper Cretaceous palynostratigraphic zones of 

the Western Interior region are recognizable in the Straight 

Cliffs Formation. These are the Nyssapollenites albertensis 

Interval Zone and the Proteacidites retusus Interval Zone. 

The Nyssapollenites albertensis Zone is late Cenomanian 

through mid-Coniacian in age (Nichols, 1994). The presence 

of the N. albertensis Zone in the lower part of the Straight 

Cliffs Formation (Tibbet and Calico sequences) is consistent 

with the previously discussed late Turanian and early Coniacian age determinations of this interval based on molluscan 

fossils. Nyssapollenites albertensis is present also in the 

post-Coniacian part of the Straight Cliffs Formation, but 

there it is present along with species indicative of the overlying palynostratigraphic zone.

The lowest stratigraphic occurrence of the pollen species Proteacidites retusus defines the base of the mid-Coniacian through upper Santonian P. retusus Zone. The 

presence of the P. retusus Zone in the John Henry Member 

verifies the Coniacian-Santonian age of that unit. More 

important with regard to the sequence stratigraphy of the 

Straight Cliffs Formation, the occurrence of Proteacidites 

pollen coincides with the interpreted position within the 

John Henry Member of the A- sequence (Hettinger, 1993, 

1995). The morphologically distinctive and biostratigraphically important pollen of Proteacidites has its lowest
B12 COAL-BEARING STRATA, KAIPAROWITS PLATEAU, UTAH

stratigraphic occurrence just above the interpreted position 

of the A- sequence boundary in both cores, at 759 ft (231.3 

m) in SMP-1-91 and at 890 ft (271.3 m) in CT-1-91. Pollen 

of Proteacidites is consistent in occurrence in samples 

above these levels in both cores. That the actual first occurrence datum of the P. retusus Zone in both cores just happens to coincide with the interpreted position of the Asequence boundary is highly unlikely. On the contrary, it is 

highly likely that the apparent base of the zone coincides 

with a minor unconformity (the A- sequence boundary), the 

presence of which enhances the abrupt appearance of 

palynomorphs that characterize the palynostratigraphic 

zone. Thus palynostratigraphy supports the interpretation of 

the A- sequence boundary as a significant stratigraphic 

horizon, which in turn supports the sequence-stratigraphic 

interpretation of the Straight Cliffs Formation.

The positions of two other sequence boundaries are 

interpreted by Hettinger (1993, 1995) within cores SMP-1- 

91 and CT-1-91. He identified the Calico sequence boundary 

at the 944.1 ft (287.8 m) level in SMP-1-91 and at the 

1,041.1 ft (317.3 m) level in CT-1-91. Palynostratigraphic 

data are limited at these depths in the cores because only one 

productive sample was recovered in each core from strata 

below the interpreted position of the Calico sequence boundary. Although the data are limited, palynostratigraphy provides some support for the presence of an unconformity. In 

core SMP-1-91, sample D7941-A, which is below the interpreted position of the Calico sequence boundary, yielded a 

palynomorph assemblage of seven taxa, all of which are 

present also in overlying strata (fig. 5). The assemblage in 

sample D7941-B, 6 m above, has 12 additional taxa, all of 

which are present also in overlying strata. This strong change 

in the palynoflora, which is much stronger than that between 

any other two successive samples in the core, is indicative of 

the presence of an unconformity between the sampled horizons. The palynofloral change across the interpreted position 

of the Calico sequence boundary is less striking in core CT1-91 (fig. 6), but still possibly significant. More data are 

needed to verify these results.

Hettinger (1993, 1995) interpreted the position of the 

Drip Tank sequence boundary to be at the 143.1 ft (43.6 m) 

level in core SMP-1-91 and at the 206 ft (62.8 m) level in 

core CT-1-91. Here again palynologic data are extremely 

limited, because only one palynologically productive sample 

could be obtained above those horizons in each core. No significant changes are noted between assemblages bracketing 

the boundary in either core. In both cores the assemblages 

both below and above the interpreted position of the boundary are within the Proteacidites retusus Zone. Notably 

absent from all assemblages from the cores are specimens of 

the pollen species Pseudoplicapollis newmanii (although 

two other species of the genus are present). This biostratigraphically important lower Campanian species defines a 

palynostratigraphic zone of earliest Campanian age in the 

Rocky Mountain region (Nichols and others, 1982; Nichols,

1994). Although more data clearly are needed, the evidence 

at hand is that the basal part of the Drip Tank sequence (and 

the basal part of the Drip Tank Member) are no younger than 

late Santonian.

PALEOENVIRONMENTS

Little can be said of the paleoenvironmental setting of 

the Straight Cliffs Formation, based on palynology, that is 

not already evident from consideration of stratigraphy, sedimentology, and lithology. As mentioned, the most common 

species of pollen and spores in the formation are similarly 

common in contemporaneous rocks throughout the Western 

Interior region. In this study these species were recovered 

from a variety of depositional environments ranging from 

tidal estuaries through coastal plain, fluvial floodplain, and 

coal-forming mire. A few observations are worth summarizing, however.

About 50 percent of samples collected from intervals 

interpreted as tidal or tidally influenced deposits (tables 1 

and 2) contain rare marine dinoflagellate cysts (dinocysts). 

Their presence substantiates the sedimentological evidence 

of tidal influence for these samples. The relative abundance 

of dinocysts is less than 1 percent in those samples, and additional scans of slides prepared from the other samples interpreted as deposited under tidal influence may reveal 

dinocysts in some of them, as well. Dinocysts were recorded 

also in two samples from core SMP-1-91 (table 1) and two 

from CT-1-91 (table 2) that have been interpreted as being 

from floodplain deposits. The paleoenvironment of these 

deposits may bear reevaluation, but their stratigraphic position is in close proximity to beds deposited under tidal influence (Hettinger, 1993, 1995). It is noteworthy that the 

presence of dinocysts in rocks deposited so far from a marine 

environment would have been difficult to interpret, had not 

the stratigraphic and sedimentologic analyses indicated the 

presence of tidally influenced deposits. These specimens 

might have been interpreted simply as out of place, perhaps 

as reworked from underlying marine rocks.

Although data are limited, the palynoflora of coal samples analyzed suggests that the vegetation of the coalforming mires was dominated by ferns and mosses, with certain angiosperms also present as major components. Interpretations are based on analyses of selected samples from 

two thick coal beds (D8020 and D8068), and from two thin 

coal beds in core SMP-1-91 and three thin coal beds in CT1-91 (see tables 1 and 2).

That these mires were raised bogs, as suggested by 

McCabe and Shanley (1992), is reasonable. Sphagnum moss 

(represented by several species of the spore genus Stereisporites} is common in several samples of coal analyzed. 

In some modern peat-forming environments, sphagnum 

moss forms raised bogs. However, sphagnum moss clearly 

was only one component of mire vegetation, and it did not
1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49 50 51 52 53 54 55

D7941-EE

D7941-DD D7941-CC 

D7941-BB 

D7941-AA 

D7941-Z D7941-Y D7941-X D7941-W 4 

D7941-V D7941-U D7941-T 

D7941-S D7941-R D7941-Q D8020-M 

D8020-B to -L 

D8020-A D7941-P 

D7941-O 

D7941-N 

D7941-M D7941-L 

D8068-EE

D8068-Z D8068-O D8068-D D8068-A D7941-K D7941-J D7941-ID7941-H 4 D7941-G D7941-F 4D7941-E 4 D7941-D D7941-C D7941-B

4

k

4 

4

»

D7941-A 4

Figure 5. Strat a single thick co

k 4 

4

4

I 

4

1> 4> 4

igr 

alt

4

kk

<

» 4

k 4 > 4

4 4 4

44

4

r 4

4

>

4( 

k 4

4

k 4k 4

k k ki 4

»

f " 

V » 4

-4

4 4

4 

1 4 

I 4 

4

> 4

i i

4 4 4

4

1

4 4

I 4

4

4444 

> 4> 4

4

I 4> ,;<

n' tin

. 4

aphic oc 

)ed. Nun

k 1 k k 

k k

k 4k 1 

4

» ( 

4

r 

» 4r 4»i; :» .» i. > '-

b <

)» 1

4

k 

k k

k

k

»

j ,

i '

4 4

k 

4

44

1

4

»

> 4 1 4 

4

k

4

I1> ~.

4 4

k 4 ) 4 k 4 

4

4

4

>

4

 4 

: <

4

> »

4 

1

k 

k 4

k 

k

k I

4 

1

k 4 

4

4

» 4»1 4>

4 

» 4 » 4

k

k 4

 i 4 k 

1 4

k 

» 4 

4

» 4

4

> 4

44 

» 4

44

» i» 4 » 4

4 4

k 4 

k

4 

k

4 

k k

»»»>1 :» 4>> 1 4 » »

> 

kk

k "

k > 

4

4

44

4 

4 44

<4 4

i4 

44 

* 4

k

4

> 

» 41 4 » 4 »I1 4I» » 4»» 4> 4

4I

4 4 

k

4 4 

k 4

4 

» 4 1 4 

4

»

4 

4 

4 

» 

4

>> 4

»

k 4

1 4

k 

k 4> 4 1 

»

» » »» 4» »

1 !i

4 

1 4

; 4

*

*

k 

4

» *

41 

>

» 4

* 

** 

4

»> > »

>

4»

> >

4

4 1 

4

4 4 4

4 4

4

4

4

4

4 

4

| -,.___.,=. ,.,; ................. li (

currences of palynomorph taxa by sample in core SMP ibers are keyed to the list of taxonomic names in table

» 4

4

) 4) 4

) 4 

4

) 4 

1 

» 4> » 4 

4 

> 4> 4

4 

> 4 

4

I» ( >

»»

»I 4

i» i

4

>

» » >»» I »

4

>

» 

> 41 

4

4

»

4

44 4

4 4 

4 4

1 

4 4

I

44

4

>

>

> )

» »> 

») »»

4

4 4

4

4 

( 

4

»

4

I 

I 

)

i

4

4 4

4i

4

4

> 4

11 4 4

)»>

44

N

4 

44

> 4

-1-91. Dots indicate presence 

3. Taxa are divided into majc

t ) 4

» 4 » 4 

4

t

t 

k

)I 

1

4

»» 4

4

I ., > 4 » 4»: s 

4

»

.R 

ffg

4

»

» 4

» » 

4

»

i ' 

k» » 4

I 4

4

> 4

I 

4 

4

44 444 

1 4

> 4

k

>

((

» 4

4 

I 

4

» 41 » 4 

4 

4 4

> 4» 4>

k

» (

k ( 

4

I 4 

< 

k 4

» 4

4

» 4

44

> 4 » 1 4 >»

k 1k 

k

k 4

i 1 

k 

4

k> 

4

»

4

» 4 

4

> 4

i 4 

»

4 

4

>

( 

k

1 I 4

4 

» 4»>k> .: >k 4

4

4 

> k

4

k

(

I » »

4

> 4» 4 k

kk

ki -4

4 44

> 4 >

41

4

41

»» 4 >

4

*

k *

41

< 

k 

41 

* 441 4

<§ «

* 4 

>

4

> 

4

I 1

k

>

» 1 4

) 4

k

4

4 4 

4 

k

k 4

4 4

i 4 

k 1

4 4

» > 4 >

k

k 

4

»

k » 

»

) 

»

4

>

k 4

4k

4k

I

4 

1

» ! - 

i 4k 

1

w

ecords for D8020-B to -L are composited from all sa roups: 1, marine dinocysts, undifferentiated; 2-24, bry

Drip Tank 

Mbr. (pt.)

PALYNOSTRATIGRAPHY AND SEQUENCE STRATIGRAP

j=r^

O 0) 5;

-> I^

HY, STRAIGHT CLIFFS F

m

U

Smoky Jj 

Hollow Q 

Mbr. Z 

(Pt.)

»mples from 

i , 00 ophyte and ^-

pteridophyte spores (shaded); 25-34, gymnosperm pollen; 35-54, angiosperm pollen (shaded); 55, freshwater algal cysts, undifferentiated.
B14 COAL-BEARING STRATA, KAIPAROWITS PLATEAU, UTAH

12345678 910111213141516171819202122232425262728293031323334353637383940

D7993-PP 

Drip Tank s. b. - D7993-OO

D7993-NN

D7993-MM

D7993-LL

D7993-KK

D7993-JJ 

D7993-II 

D7993-HH

D7993-GG 4

D7993-FF 

D7993-EE 4 

D7993-DD 

D7993-CC 

D7993-BB

D7993-AA 4

D7993-Z

D7993-Y 4 

D7993-X 4 

D7993-W 4

D7993-V

D7993-U 4 

D7993-T 

D7993-S 

D7993-R

D7993-Q 4

D7993-P

D7993-O

D7993-N 

D7993-M 4 

D7993-L 4 

D7993-K 

D7993-J 4 

D7993-I 

D7993-H

D7993-G 4 

A- s. b.- 

D7993-F

D7993-E 

D7993-D

D7993-C 

Calico s. b. - 

D7993-A

4

4

4

4

» 4

4

4

» 4

» 4 

» 4 

I

4

» 4

4

)

4

» 4 

1

} 

4 

4

> 4 

4

4

4

4

<

> 4

1

t

>

1

)

1

> ,

| :

i ;

i

I

»

»

i

» '-, 

}

\ 

\

\ ^

» < 

i i

I 4

» 4

4

4

4

4

4

4

4

4 

4

(

»

> 4

l

>

)

1

I

t

 4

>

1

1 4

,

1 

»

t

> 4

4

4

4

<

<

4

4

4

t

> 4 

4

4

4

4

4

1 4

4

4

4 

4

<

<

4

4

I

1 4

»

»

»

t 4

1 i

t

1 

( 

t

4

1

>

»

»

I 4

1 i

1 

) < 

t

> 1

l

4

» 4

»

4

4

> 4

4

4 

4 

4

t

4

>

4

4 

> 4 

4

) <

4

1

i

4

4

4

I 4

1

4

1 4

1 4

» 

I 4

1 4

4

4

4

) <

1 4 

I 4 

t

l

I

1

1

1

t

>

1 

t 4

1 4

) 4 

4

»

>

1

I 4

1

4

4

>

» 4

I 4 

>

t

>

>

4

>

I

4

4

»

4

4

4

)

4

4

4 

1 4

> 4

»

 4

1

i

t

> 4 

» 4

>

4

1 

t

>

t

»

>

>

4

4

\

4

1 4

1 4

4 

4 

4

< 

< 

< 

(

(

(

<

< 

4

4

<

<

(

( 

1 

1

1

> <

1

1 

1 

) 

» 

>

»

>

(

»

> 

I

1

I

 

> 

)

>

» 4

4

4

4

» 4

4

4

4

4

4

4

4 

4

4

4

4

t

4

<

>

>

1 1

i

1

i

i

l

i 

4

) 

>

»

(

 4

4

)

4

>

1

4

4

4

4

4

4 

» 4

4

4

4

4

4

4

4 

» 4 

4

<

» 4

4

»

» 4

 4

4 

» 4

4

I 4 

» 4

>

> 4

I

)

>

>

>

> 

>

> (

» 4

t 4

i

»

» 

(

l 

>

>

1

»

>

4

4

4

4

»

4

4

> 

4

4

4

1 1

^

^

>

) 4

4

>

t

, 4 

t

1 4

> :

>

t 

>

1

»

» 1

> 4

»

4

4 

4 

1

4

; < »

4

4

>

t 4

i

» 

i

4

t

i

»

>

1 '

4 

4

4

4

4

1

, 1

J 1

1

1 

1

l

1

I

1 l

4

4

4 

4 

4

4

4 

4

4

4

4 

,4

4 

4

1

4

1

1

»

I 

1 

|

»

1

1

»

»

»

»

> 

1

1

4

t

4

) 1

4

4 

4 

4

4

4

4

' 1

»

4

1

 

1

» 4 

) 

1

» 4

4 

1

A

I ,

,

!'. i

: 4 

> 4

4

t 4

4

k

I 

)

1

: 

: ,

>

> :

)

i: 4

;

4

* 4

'.; ;

4 

,4

4

4

4 

4

4 

<

i

» 

::

l ,

» :

; ;

); ;

i

» ;

 <

t 

»

1

1 

) 4

1

1

( 

4

4 

4

(

4

4

4 

»

1

f = 

1

1 <

1

Drip Tank 

Mbr. (pt.)

1

i

l

>

= IS

1

 John 

> "" Henry 

1 Mbr.

t

»

>

1

I

1

>

ii^i

 Smoky 

> Hollow

Mbr. 

(pt.)

>

Figure 6. Stratigraphic occurrences of palynomorph taxa by sample in core CT-1-91. Dots indicate presence. Numbers are keyed to the 

list of taxonomic names in table 4; fewer individual taxa listed than in figure 5 because some are combined and others omitted. Taxa are 

divided into major groups: 1, marine dinocysts, undifferentiated; 2-17, bryophyte and pteridophyte spores (shaded); 18-26, gymnosperm 

pollen; 27-40, angiosperm pollen (shaded).

dominate these paleoenvironments to the exclusion of other 

plant species, as it does in some modern environments. Ferns 

producing spores assignable to three species of Gleicheniidites evidently were the most common plants in mires, and 

angiosperm pollen of one kind is abundant.

The botanical affinity of the most common angiosperm 

pollen in coal samples (Cupuliferoidaepollenites spp.) is 

somewhat uncertain, although the pollen morphology is suggestive of the modern family Fagaceae. It is possible,

although not demonstrable, that the plants producing this 

pollen were trees (many modern species of the Fagaceae are 

arboreal in habit). Forests that grow on raised bogs in the 

tropics at present have low species diversity (Teichmiiller 

and Teichmiiller in Stach and others, 1975). Presumably 

Late Cretaceous climates of the Kaiparowits area were subtropical or tropical (as indicated, for example, by the presence of palm pollen in the Straight Cliffs palynoflora). Thus, 

pollen of Cupuliferoidaepollenites may represent trees that
PALYNOSTRATIGRAPHY AND SEQUENCE STRATIGRAPHY, STRAIGHT CLIFFS FORMATION B15

Table 3. Alphabetical and numerical lists of palynomorph taxa recorded in samples from core SMP-1-91.

[Numbers are keyed to the distribution chart (fig. 5)]

Alphabetical list Numerical list

Aequitriradites spinulosus (Cookson & Dettmann) Cookson &

Dettmann (24) 

Appendicisporites spp. (2) 

Araucariacites australis Cookson ex Couper (26) 

Arecipites sp. 1 (43) 

Arecipites sp. 2 (50) 

Biretisporites sp. (22)

Callialasporites dampieri (Balme) Dev emend. Norris (27) 

Camarozonosporites ambigens (Fradkina) Playford (3) 

Cicatricosisporites spp. (4) 

Corollina torosa (Reissinger) Klaus emend. Cornet &

Traverse (28)

Cupuliferoidaepollenites spp. (39) 

Cupuliferoipollenites sp. (51) 

Cyathidites sp. cf. C. diaphana (Wilson & Webster) Nichols &

Brown (11)

Deltoidospora minor (Couper) Pocock (20) 

Deltoidospora sp. "T" (5)

Echinatisporis varispinosus (Pocock) Srivastava (7) 

Ephedripites sp. "D" (34) 

Eucommiidites minor Groot & Penny (29) 

Foraminisporis wonthaggiensis (Cookson & Dettmann)

Dettmann (19) 

Foveosporites sp. (15)

Foveotricolporites johnhenryensis n. sp. (40) 

Gleicheniidites senonicus Ross emend. Skarby, var. 1 (16) 

Gleicheniidites senonicus Ross emend. Skarby, var. 2(12) 

Gleicheniidites senonicus Ross emend. Skarby, var. 3 (17) 

Laevigatosporites haardtii (Potonie & Venitz)

Thomson & Pflug (6) 

Liliacidites sp. (46) 

Matonisporites sp. (8) 

Microreticulatisporites sp. (14) 

Nyssapollenites albertensis Singh (36) 

Nyssapollenites sp. (37)

Ornamentifera echinata (Bolkhovitina) Bolkhovitina (23) 

"Palaeoisoetes" sp. (21) 

Pityosporites spp. (25) 

Plicapollis rusticus Tschudy (44) 

Pristinuspollenites sp. (33) 

Proteacidites spp. (48) 

Pseudoplicapollis cuneata Christopher (49) 

Pseudoplicapollis triradiata Jameossanaie (52) 

Quadripollis krempii Drugg (32) 

Reticuloidosporites pseudomurii Elsik (18) 

Rhoipites spp. (45) 

Rugubivesiculites sp. (31)

Sparganiaceaepollenites hospahensis Jameossanaie (53) 

Stereisporites spp. (13)

Taxodiaceaepollenites hiatus (Potonie) Kremp (30) 

Triatriopollenites granulatus (Simpson) Leffingwell (54) 

Tricolpites minutus Sah & Kar (35) 

Tricolpites spp. (41)

Triporoletes novomexicanus (Anderson) Srivastava (9) 

Triporopollenites sp. 1 (47) 

Triporopollenites sp. 2 (42) 

Algal cysts, undifferentiated (55) 

Dinocysts, undifferentiated (1) 

Other pollen (38) 

Other spores (10

1 Dinocysts, undifferentiated

2 Appendicisporites spp.

3 Camarozonosporites ambigens (Fradkina) Playford

4 Cicatricosisporites spp.

5 Deltoidospora sp. "T"

6 Laevigatosporites haardtii (Potonie & Venitz) Thomson & Pflug

7 Echinatisporis varispinosus (Pocock) Srivastava

8 Matonisporites sp.

9 Triporoletes novomexicanus (Anderson) Srivastava

10 Other spores

11 Cyathidites sp. cf. C. diaphana (Wilson & Webster) 

Nichols & Brown

12 Gleicheniidites senonicus Ross emend. Skarby, var. 2

13 Stereisporites spp.

14 Microreticulatisporites sp.

15 Foveosporites sp.

16 Gleicheniidites senonicus Ross emend. Skarby, var. 1

17 Gleicheniidites senonicus Ross emend. Skarby, var. 3

18 Reticuloidosporites pseudomurii Elsik

19 Foraminisporis wonthaggiensis (Cookson & Dettmann) 

Dettmann

20 Deltoidospora minor (Couper) Pocock

21 "Palaeoisoetes" sp.

22 Biretisporites sp.

23 Ornamentifera echinata (Bolkhovitina) Bolkhovitina

24 Aequitriradites spinulosus (Cookson & Dettmann) 

Cookson & Dettmann

25 Pityosporites spp.

26 Araucariacites australis Cookson ex Couper

27 Callialasporites dampieri (Balme) Dev emend. Norris

28 Corollina torosa (Reissinger) Klaus emend. Cornet & Traverse

29 Eucommiidites minor Groot & Penny

30 Taxodiaceaepollenites hiatus (Potonie) Kremp

31 Rugubivesiculites sp.

32 Quadripollis krempii Drugg

33 Pristinuspollenites sp.

34 Ephedripites sp. "D"

35 Tricolpites minutus Sah & Kar

36 Nyssapollenites albertensis Singh

37 Nyssapollenites sp.

38 Other pollen

39 Cupuliferoidaepollenites spp.

40 Foveotricolporites johnhenryensis n. sp.

41 Tricolpites spp.

42 Triporopollenites sp. 2

43 Arecipites sp. 1

44 Plicapollis rusticus Tschudy

45 Rhoipites spp.

46 Liliacidites sp.

47 Triporopollenites sp. 1

48 Proteacidites spp.

49 Pseudoplicapollis cuneata Christopher

50 Arecipites sp. 2

51 Cupuliferoipollenites sp.

52 Pseudoplicapollis triradiata Jameossanaie

53 Sparganiaceaepollenites hospahensis Jameossanaie

54 Triatriopollenites granulatus (Simpson) Leffingwell

55 Algal cysts, undifferentiated
B16 COAL-BEARING STRATA, KAIPAROWITS PLATEAU, UTAH

Table 4. Alphabetical and numerical lists of palynomorph taxa recorded in samples from core CT-1-91.

[Numbers are keyed to the distribution chart (fig. 6)]

Alphabetical list Numerical list

Appendicisporites spp. (15)

Araucariacites australis Cookson ex Couper (23)

Arecipites spp. (38)

Callialasporites dampieri (Balme) Dev emend. Norris (22)

Camarozonosporites ambigens (Fradkina) Playford (10)

Cicatricosisporites spp. (7)

Corollina torosa (18)

Cupuliferoidaepollenites spp. (27)

Cupuliferoipollenites sp. (36)

Cyathidites sp. cf. C. diaphana (Wilson & Webster) Nichols &

Brown (17)

Deltoidospora minor (Couper) Pocock (4) 

Deltoidospora sp. "T" (13) 

Echinatisporis varispinosus (11) 

Ephedripites sp. "D" (19) 

Foraminisporis wonthaggiensis (Cookson & Dettmann) Dettmann

(5)

Foveotricolporites johnhenryensis n. sp. (34) 

Gleicheniidites spp. (6) 

Laevigatosporites haardtii (Potonie & Venitz) Thomson & Pflug

(2)

Microreticulatisporites sp. (12) 

Nyssapollenites albertensis (35) 

Nyssapollenites sp. (28)

Ornamentifera echinata (Bolkhovitina) Bolkhovitina (16) 

Pityosporites spp. (24) 

Plicapollis rusticus Tschudy (39) 

Pristinuspollenites sp. (26) 

Proteacidites spp (32) 

Pseudoplicapollis spp. (40) 

Quadripollis krempii Drugg (25) 

Reticuloidosporites pseudomurii Elsik (8) 

Rhoipites spp. (31) 

Rugubivesiculites sp. (20) 

Stereisporites spp. (9)

Taxodiaceaepollenites hiatus (Potonie) Kremp (21) 

Tricolpites minutus Sah & Kar (30) 

Tricolpites spp. (29)

Triporoletes novomexicanum (Anderson) Srivastava (14) 

Triporopollenites spp. (37) 

Dinocysts, undifferentiated (1) 

Other pollen (33) 

Other spores(3)

1 Dinocysts, undifferentiated

2 Laevigatosporites haardtii (Potonie & Venitz) Thomson & Pflug

3 Other spores

4 Deltoidospora minor (Couper) Pocock

5 Foraminisporis wonthaggiensis (Cookson & Dettmann) 

Dettmann

6 Gleicheniidites spp.

7 Cicatricosisporites spp.

8 Reticuloidosporites pseudomurii Elsik

9 Stereisporites spp.

10 Camarozonosporites ambigens (Fradkina) Playford

11 Echinatisporis varispinosus

12 Microreticulatisporites sp.

13 Deltoidospora sp. "T"

14 Triporoletes novomexicanum (Anderson) Srivastava

15 Appendicisporites spp.

16 Ornamentifera echinata (Bolkhovitina) Bolkhovitina

17 Cyathidites sp. cf. C. diaphana (Wilson & Webster) 

Nichols & Brown

18 Corollina torosa

19 Ephedripites sp. "D"

20 Rugubivesiculites sp.

21 Taxodiaceaepollenites hiatus (Potonie) Kremp

22 Callialasporites dampieri (Balme) Dev emend. Norris

23 Araucariacites australis Cookson ex Couper

24 Pityosporites spp.

25 Quadripollis krempii Drugg

26 Pristinuspollenites sp.

27 Cupuliferoidaepollenites spp.

28 Nyssapollenites sp.

29 Tricolpites spp.

30 Tricolpites minutus Sah & Kar

31 Rhoipites spp.

32 Proteacidites spp.

33 Other pollen

34 Foveotricolporites johnhenryensis n. sp.

35 Nyssapollenites albertensis

36 Cupuliferoipollenites sp.

37 Triporopollenites spp.

38 Arecipites spp.

39 Plicapollis rusticus Tschudy

40 Pseudoplicapollis spp.

inhabited raised bogs in the area, and that contributed to the 

accumulation of coal-forming peat.

As mentioned, pollen of taxodiaceous conifers such 

as that which dominates palynological assemblages from 

most thick Tertiary coal beds in the region is very rare. 

Thus no palynological evidence is available that coniferous trees were major contributors to Straight Cliffs coal. 

Further detailed analyses of Straight Cliffs coal-depositional environments represented by thick coal beds are 

warranted, especially in conjunction with coal-petrographic analyses.

CONCLUSIONS

Palynologic analyses demonstrate the presence of two 

regional palynostratigraphic zones in upper Turanian 

through upper Santonian strata of the Straight Cliffs Formation in the Kaiparowits Plateau. This stratigraphic interval 

includes the upper part of the Smoky Hollow Member, the 

John Henry Member, and lower part of the Drip Tank Member of conventional lithostratigraphy, and corresponding, 

recently defined sequence-stratigraphic units, namely the 

upper part of the Tibbet sequence, the Calico and
PALYNOSTRATIGRAPHY AND SEQUENCE STRATIGRAPHY, STRAIGHT CLIFFS FORMATION B17

A- sequences, and the lower part of the Drip Tank sequence. 

The Nyssapollenites albertensis Zone (upper Cenomanian 

through mid-Coniacian) is present in the upper part of the 

Smoky Hollow Member and lower part of the John Henry 

Member (=uppermost part of the Tibbet sequence and the 

Calico sequence), and the Proteacidites retusus Zone (midConiacian through upper Santonian) is present in the middle 

and upper parts of the John Henry Member and lowermost 

part of the Drip Tank Member (=the A- sequence and lowermost part of the Drip Tank sequence). No palynomorphs 

indicative of Campanian age were found in the Drip Tank 

Member, but very few samples from the Drip Tank were 

available for analysis.

The boundary between the two palynostratigraphic 

zones coincides with the position of the A- sequence boundary as interpreted in the cores by Hettinger (1993, 1995). 

Limited palynostratigraphic data also tend to confirm the 

interpreted position of the Calico sequence boundary. The 

interpreted position of the Drip Tank sequence boundary has 

not been confirmed, but too few samples were available to 

resolve this question with certainty on the basis of palynostratigraphy.

Tidally influenced deposits in transgressive and highstand systems tracts are indicated by the presence of rare 

marine dinocysts in predominantly nonmarine strata. They 

confirm Hettinger's (1993, 1995) interpretation of depositional environment of these beds. These dinocysts are found 

at considerable distance from the ancient shoreline and 

would be otherwise difficult to account for in predominantly 

fluvial deposits.

Unusually thick coal beds are present in the John Henry 

Member, in highstand systems tracts landward of stacked 

shoreface parasequences that form the Straight Cliffs escarpment. Palynological analyses of coal samples indicate that 

the vegetation of the coal-forming mires consisted largely of 

ferns and sphagnum moss together with certain species of 

angiosperms. The mire floras may have included arboreal 

angiosperms.

Some species of angiosperm pollen in the Straight 

Cliffs palynoflora are biostratigraphically important forms, 

especially pollen of the Normapolles complex and certain 

other triporates. Records of occurrence of some pollen and 

spore species in the study area are contributions to knowledge of Upper Cretaceous palynostratigraphy. One species 

of angiosperm pollen is new.

Additional palynostratigraphic studies of the Straight 

Cliffs Formation, especially the unsampled basal and uppermost parts, should provide further tests of sequence-stratigraphic interpretations of these largely nonmarine strata. 

Further detailed palynologic studies of the thick coal beds 

should provide a more complete overview of the nature of 

the coal-forming mires, especially if conducted in close collaboration with coal-petrographic analyses.

TAXONOMIC NOTES

The following comments provide some detail about 

selected pollen and spore species present in the Straight 

Cliffs palynoflora. They may serve in further investigations 

of the palynology of the Kaiparowits area. Formal description of a new species is given. After this description, several 

previously described taxa are discussed in alphabetical 

order.

FOVEOTRICOLPORITESJOHNHENRYENSIS n. sp.

Plate 1, figures 17-20.

Holotype: Slide D7993-I (1), England Finder coordinates 27L/1; plate 1, figure 17.

Type Repository: U.S. Geological Survey, Denver laboratory, Palynological Type Collection.

Description: Tricolporate pollen, spheroidal to oblate, 

amb triangular to slightly rounded triangular with blunt corners; colpi bordered by prominent margines of thickened 

ektexine 1-1.5 |im wide, extending about one-half of radius 

toward poles on each hemisphere; pori circular, unbordered, 

=1.5 Jim in diameter, obscure in polar view; sculpture foveolate to foveo-reticulate, lumina 0.5-1.0 |im, muri 0.5-1.0 

|im, sculpture tending to become finer toward colpi; exine 

=1.5 Jim thick; diameter of grains 20-27 |im, most less than 

25 |im (19 specimens measured).

Comparison: The genus Foveotricolporites was proposed by Pierce (1961) for foveolate, tricolporate pollen; the 

type species is F. rhombohedmlis Pierce. Foveotricolporites 

johnhenryensis n. sp. differs from F. rhombohedralis from 

the Cenomanian of Minnesota in having prominent margines 

and in its oblate rather than prolate form. It differs from F. 

callosus Singh from the Cenomanian of Alberta in its oblate 

rather than prolate form, and from Tricolporopollenites sp. 2 

of May (1972) from the Turonian of Utah, with which Singh 

(1983) compared his species, in form and in smaller size. No 

other species of Foveotricolporites have been described 

from the Cretaceous. Foveotricolporites johnhenryensis n. 

sp. differs from Margocolporites varireticulatus Jameossanaie from the Campanian of New Mexico, to which it bears 

resemblance, in having oblate rather than prolate form, in 

tending to have a rounded triangular amb rather than straight 

to concave sides, and in having shorter colpi. It differs from 

species of Nyssapollenites in the Straight Cliffs palynoflora 

and elsewhere in having foveolate sculpture, and from 

Straight Cliffs species and others belonging in the genus 

Rhoipites in being oblate rather than prolate, and in having 

unbordered pores.

Occurrence: John Henry Member of the Straight Cliffs 

Formation (Coniacian-Santonian), Kaiparowits Plateau, 

Utah. This species is present in about one third of the samples analyzed.
B18 COAL-BEARING STRATA, KAIPAROWITS PLATEAU, UTAH

ARECIPITES spp.

Plate 1, figures 7-8.

Pollen assigned to this genus is monosulcate and acuminate-oval in polar view. Specimens from the Straight Cliffs 

Formation are 15-20x30-35 Jim in size. The exine is thin, 

two-layered, and foveolate to finely reticulate. Two species 

are informally recognized in this study, one having slightly 

coarser sculpture than the other. Too few specimens were 

recorded to provide a basis for formal description of new 

species.

Pollen of this morphology is characteristic of the palm 

family, Arecaceae (also called Palmae). Similar pollen is 

common in younger Cretaceous rocks in western North 

America, but the Kaiparowits specimens may be the stratigraphically oldest, well-documented specimens of palm pollen so far recorded. Similar specimens are present in the 

Straight Cliffs Formation in the Markagunt Plateau area of 

southwestern Utah (D.J. Nichols, unpub. data, 1994).

COROLLINA TOROSA (Reissinger) Klaus emend. Cornet & Traverse

Plate 1, figure 6.

Pollen of the species Corollina torosa is present in 

almost all samples of the Straight Cliffs Formation, including those from coal, although it is relatively rare in samples 

from the thick coal here designated bed D8020. It tends to 

dominate assemblages from below and within the Calico 

bed, from some levels sampled within the John Henry Member, and from the Drip Tank Member.

This species was produced by gymnosperms of the 

extinct family Hirmerelliaceae, cheirolepidiaceous conifers 

(Traverse, 1988), and it can be considered as characteristic 

of the Straight Cliffs palynoflora. The plants that produced 

this pollen must have been prominent members of the plant 

communities of the Kaiparowits area in mid-Cretaceous (late 

Turonian through Santonian) time. They apparently were 

warmth-loving shrubs that grew in thickets in low-lying 

environments marginal to water (Traverse, 1988).

CUPULIFEROIDAEPOLLENITES spp.

Plate 1, figure 9.

Small, psilate tricolpate pollen from the Straight Cliffs 

Formation was assigned to Cupuliferoidaepollenites spp. 

Most of these specimens belong to the species C. minutus 

(Brenner) Singh, which is illustrated in plate 1. This pollen 

is present at least in low numbers in almost all samples and 

is abundant in some. The specimens recovered have negligible biostratigraphic or paleoecologic significance but are 

noteworthy as components of the Straight Cliffs palynoflora. 

They probably represent species of the family Fagaceae.

CYATHIDITES sp. cf. C. DIAPHANA (Wilson & Webster) 

Nichols & Brown

Plate 1, figure 2.

This species is trilete, rounded-triangular in outline 

with strongly concave sides, and psilate. The laesurae extend 

little more than halfway from the proximal pole to the margin. Specimens closely resemble Cyathidites diaphana, an 

upper Maastrichtian and lower Paleocene species. The Kaiparowits species is common throughout the Straight Cliffs 

Formation. These spores were produced by ferns that were 

present in several Straight Cliffs depositional environments 

and were not restricted to the coal-forming mires of the John 

Henry Member, where other species of fern were common. 

Although the genus name suggests affinity with the modern 

tree-fern genus Cyathea, there is no evidence that these 

spores represent tree ferns.

ECHINATISPORIS VARISPINOSUS (Pocock) Srivastava

Plate 1, figure 3.

This species is trilete (although the laesurae are 

obscured on most specimens), circular in outline, and distinctively echinate. It presumably was produced by some 

kind of fern, although its precise botanical affinity is unclear. 

These spores are common throughout the Straight Cliffs Formation, are present in most samples analyzed, and are abundant in some. The species has a long range in the Cretaceous 

of western North America and is notable in the Straight 

Cliffs palynoflora only because it is so common.

GLEICHENIIDITES spp.

Plate 1, figure 4.

Spores assigned to Gleicheniidites spp. in this study are 

trilete, triangular, and psilate, and are distinctive in having 

the prominent interradial crassitudes characteristic of the 

genus. All specimens recorded or observed can be assigned 

to the rather broadly defined species Gleicheniidites senonicus Ross emend. Skarby. Among Straight Cliffs specimens, 

as many as three species might be distinguished on the basis 

of details of morphology such as diameter and extent of 

development of interradial crassitudes, but only cursory 

effort was made to make such distinctions because the morphologic variants do not differ in stratigraphic occurrence.

These spores, which were produced by gleicheniaceous 

ferns, are present in almost all samples of the John Henry 

Member. They are especially common in coal samples and 

probably represent one or more species of fern that inhabited 

coal-forming mires in the Kaiparowits area in Late Cretaceous time.

NYSSAPOLLENITES ALBERTENSIS Singh

Plate 1, figure 16.

Nyssapollenites albertensis is tricolporate and psilate, 

and small in size. The species is present throughout the
PALYNOSTRATIGRAPHY AND SEQUENCE STRATIGRAPHY, STRAIGHT CLIFFS FORMATION B19

Straight Cliffs Formation. Although it is not especially common, it is important because it signifies the presence of the 

upper Cenomanian to middle Coniacian Nyssapollenites 

albertensis Interval Zone (Nichols, 1994). This zone is 

present in the lower part of sections sampled in each core, 

below the position of the A- sequence boundary. Above that 

horizon, this species occurs with Proteacidites retusus in the 

Proteacidites retusus Interval Zone (middle Coniacian-upper Santonian).

PLICAPOLLIS RUSTICUS Tschudy

Plate 1, figure 15.

Plicapollis rusticus is a morphologically distinctive 

species of the Normapolles complex of pollen originally 

described from the upper Campanian of Tennessee by 

Tschudy (1975). Specimens are triporate and the apertures 

are complexly structured, as is characteristic of Normapolles 

pollen, and this species is characterized by a prominent triradiate plication or thickening of the exine centered at the pole 

and extending to the apertures. The specimens recorded in 

this study are from 25 to 29 |im in diameter (nine specimens 

measured).

As mentioned, similar specimens, probably of the same 

species, were illustrated by Tschudy (1980) from the Crevasse Canyon (Coniacian-Santonian) and Menefee Formations (Santonian) in New Mexico. In the Kaiparowits 

Plateau, this species is present within the John Henry Member of the Straight Cliffs Formation.

PROTEACIDITES spp.

Plate 1, figures 11-12.

Proteacidites spp. includes one or more species of distinctive triporate, reticulate pollen as illustrated in plate 1. 

Two species, P. retusus Anderson and P. thalmannii Anderson, were described from New Mexico by Anderson (1960), 

but many more species may exist in the Senonian rocks of 

the region. Straight Cliffs Formation specimens resemble 

these, but no attempt has been made to resolve their taxonomy and nomenclature at the species level.

Species of Proteacidites are among the most biostratigraphically important kinds of pollen in western North 

America, because they are present throughout the Upper 

Cretaceous, from the Coniacian through the Maastrichtian. 

As noted in the discussion of palynostratigraphy, the stratigraphic range of the genus is of special importance in this 

study. It defines the presence of the middle Coniacian-upper 

Santonian Proteacidites retusus Interval Zone in the John 

Henry Member of the Straight Cliffs Formation specifically 

within the A- sequence as determined in the cores by Hettinger (1993, 1995). Presence of this biozone reconfirms the 

age of the formation, which was previously determined (with 

some uncertainty) on the basis of its molluscan fauna. It also 

demonstrates that the palynostratigraphic zone, which has its

stratotype in western Wyoming, extends as far south as the 

Kaiparowits area of southern Utah.

PSEUDOPLICAPOLLIS CUNEATA Christopher

Plate 1, figure 13.

Pseudoplicapollis cuneata is another member of the 

Normapolles complex of pollen. The triporate apertures are 

distinctive in internal structure. This species is distinguished from others of the genus by the absence of triradiate plications at the poles. As mentioned, this species was 

first described from the Santonian of the Atlantic Coastal 

Plain by Christopher (1979) and also has been reported 

from the lower Campanian of New Mexico by Jameossanaie (1987). In the Kaiparowits Plateau, it is present in the 

John Henry Member of the Straight Cliffs Formation above 

the position of the A- sequence boundary as determined in 

cores SMP-1-91 and CT-1-91 by Hettinger (1993,1995).

RETICULOIDOSPORITES PSEUDOMURII Elsik

Plate 1, figure 5.

This monolete spore is characterized by rough and 

irregular sculpture that vaguely resembles reticulation. This 

species differs from the other species of monolete spore in 

the Straight Cliffs palynoflora, Laevigatosporites haardtii 

(not illustrated), in its distinctive sculpture.

Reticuloidosporites pseudomurii is biostratigraphically 

important because it serves to verify the presence of the Proteacidites retusus Interval Zone in the Straight Cliffs Formation. It is present only above the A- sequence boundary in 

core CT-1-91, but it occurs in two samples below this stratigraphic level, still within the John Henry Member, in core 

SMP-1-91.

STEREISPORITES spp.

Plate 1, figure 1.

Stereisporites spp. includes species that are assigned by 

some authors to one or more of the genera Cingutriletes, Distanocorisporis, Distverrusporis, and Sphagnumsporites. 

Several distinguishable species are present in the Straight 

Cliffs palynoflora, although only one is illustrated in plate 1.

These spores were produced by Cretaceous species 

related to the modern genus Sphagnum, sphagnum moss. 

They have no biostratigraphic value because they are known 

throughout the Upper Cretaceous (as well as older and 

younger strata), but they are ecologically important because 

they indicate the presence of sphagnum bogs in the Kaiparowits area during the Coniacian and Santonian. These 

spores are present throughout the coal-bearing John Henry 

Member of the Straight Cliffs Formation and are notably 

abundant in some samples, especially of coal. As mentioned, 

the coal-forming mires (or bogs) of the John Henry Member 

also contained abundant ferns (some fern spores are illustrated in pi. 1, figs. 2-5) and some angiosperms.
B20 COAL-BEARING STRATA, KAIPAROWITS PLATEAU, UTAH

TRICOLPITES spp.

Plate 1, figure 10.

Small, reticulate, tricolpate pollen is common in the 

Straight Cliffs palynoflora, occurring in most samples and 

all members of the formation. Two species were distinguished on the basis of coarseness of sculpture, only one of 

which is illustrated in plate 1. These species have no biostratigraphic value because they or others virtually indistinguishable from them are common throughout the Cretaceous 

and Tertiary of western North America. They have little ecologic value, either, because they could represent a wide variety of angiosperms having a variety of ecologic preferences. 

Botanical affinity probably is with the Platanaceae.

TRIPOROPOLLENITES spp.

Plate 1, figure 14.

Several species of triporate pollen, other than species of 

the Normapolles complex mentioned previously, are present 

in the samples analyzed in this study. Only one is illustrated 

in plate 1. These species differ from Normapolles triporates 

in having simple aperture structure. They represent several 

species of angiosperms present in the Kaiparowits area during Coniacian and Santonian time, none of which was especially abundant. However, their presence serves to 

characterize the Straight Cliffs palynoflora.

REFERENCES CITED

Anderson, R.Y., 1960, Cretaceous-Tertiary palynology, eastern 

side of the San Juan Basin, New Mexico: New Mexico Bureau 

of Mines and Mineral Resources Memoir 6, 59 p., pis. 1-11.

Christopher, R.A., 1979, Normapolles and triporate pollen assemblages from the Raritan and Magothy Formations (Upper Cretaceous) of New Jersey: Palynology, v. 3, p. 73-121, pis. 1-9.

Eaton, J. G., 1991, Biostratigraphic framework for the Upper Cretaceous rocks of the Kaiparowits Plateau, southern Utah, in 

Nations, J.D., and Eaton, J.G., eds., Stratigraphy, depositional 

environments, and sedimentary tectonics of the western margin, Cretaceous Western Interior Seaway: Geological Society 

of America Special Paper 260, p. 47-63.

Gregory, H.E., and Moore, R.C., 1931, The Kaiparowits region, a 

geographic and geologic reconnaissance of parts of Utah and 

Arizona: U.S. Geological Survey Professional Paper 164, 

161 p.

Hettinger, R.D., 1993, Sedimentological descriptions and geophysical logs of two 300-m cores collected from the Straight Cliffs 

Formation of the Kaiparowits Plateau, Kane County, Utah: 

U.S. Geological Survey Open-File Report 93-270, 50 p.

 1995, Sedimentological descriptions and depositional interpretations, in sequence stratigraphic context, of two 300-meter 

cores from the Upper Cretaceous Straight Cliffs Formation, 

Kaiparowits Plateau, Kane County, Utah: U.S. Geological Survey Bulletin 2115-A, 34 p.

Jameossanaie, Abolfazl, 1987, Palynology and age of South 

Hospah coal-bearing deposits, McKinley County, New Mexico: New Mexico Bureau of Mines and Mineral Resources Bulletin 112, 65 p.

May, F.E., 1972, A survey of palynomorphs from several coal-bearing horizons of Utah, in Doelling, H.H., ed., Central Utah coal 

fields; Sevier-Sanpete, Wasatch Plateau, Book Cliffs and 

Emery: Utah Geological and Mineralogical Survey Monograph 

3, p. 497-542, pis. 1-29.

McCabe, P.J., and Shanley, K.W., 1992, An organic control on 

shoreface stacking patterns Bogged down in the mire: Geology, v. 20, p. 741-744.

Nichols, D.J., 1994, A revised palynostratigraphic zonation of the 

nonmarine Upper Cretaceous, Rocky Mountain region, United 

States, in Caputo, M.V., Peterson, J.A., and Franczyk, K.J., 

eds., Mesozoic systems of the Rocky Mountain region, U.S.A.: 

Denver, Colorado, Rocky Mountain Section SEPM, 

p. 503-521.

Nichols, D.J., and Jacobson, S.R., 1982, Palynostratigraphic framework for the Cretaceous (Albian-Maestrichtian) of the overthrust belt of Utah and Wyoming: Palynology, v. 6, p. 119-147.

Nichols, D.J., Jacobson, S.R., and Tschudy, R.H., 1982 [1983], Cretaceous palynomorph biozones for the central and northern 

Rocky Mountain region of the United States, in Powers, R.B., 

ed., Geologic studies of the Cordilleran thrust belt: Denver, 

Colo., Rocky Mountain Association of Geologists, v. 2, p. 

721-733, pi. 1.

Orlansky, Ralph, 1971, Palynology of the Upper Cretaceous 

Straight Cliffs Sandstone, Garfield County, Utah: Utah Geological and Mineralogical Survey Bulletin 89, 57 p., 11 pis.

Peterson, Fred, 1969, Four new members of the Upper Cretaceous 

Straight Cliffs Formation in the southeastern Kaiparowits 

region, Kane County, Utah: U.S. Geological Survey Bulletin 

1274-J, 28 p.

Peterson, Fred, and Kirk, A.R., 1977, Correlation of the Cretaceous 

rocks in the San Juan, Black Mesa, Kaiparowits and Henry 

Basins, southern Colorado Plateau: New Mexico Geological 

Society Guidebook, 28th Field Conference, San Juan Basin III, 

p. 167-178.

Peterson, Fred, and Waldrop, H.A., 1965, Jurassic and Cretaceous 

stratigraphy of south-central Kaiparowits Plateau, Utah: Utah 

Geological Society and Intermountain Association of Petroleum Geologists, Guidebook to the Geology of Utah 19, 

p. 47-69.

Pierce, R.L., 1961, Lower Upper Cretaceous plant microfossils 

from Minnesota: Minnesota Geological Survey Bulletin 42, 86 

p., 3 pis.

Shanley, K.W., 1991, Sequence stratigraphic relationships and 

facies architecture of Turonian-Campanian strata, Kaiparowits 

Plateau, south-central Utah: Golden, Colo., Colorado School of 

Mines Ph. D. dissertation, 390 p.

Shanley, K.W., and McCabe, P.J., 1989, Sequence stratigraphic 

relationships and facies architecture of Turonian-Campanian 

strata, Kaiparowits Plateau, south-central Utah [abs.]: American Association of Petroleum Geologists Bulletin, v. 73, 

p. 410-411.

 1991, Predicting facies architecture through sequence 

stratigraphy An example from the Kaiparowits Plateau, Utah: 

Geology, v. 19, p. 742-745.
PALYNOSTRATIGRAPHY AND SEQUENCE STRATIGRAPHY, STRAIGHT CLIFFS FORMATION B21

Shanley, K.W., McCabe, P.J., and Hettinger, R.D., 1992, Tidal 

influence in Cretaceous fluvial strata from Utah, U.S.A. A 

key to sequence stratigraphic interpretations: Sedimentology, 

v. 39, p. 905-930.

Singh, Chaitanya, 1983, Cenomanian microfloras of the Peace River area, northwestern Alberta: Alberta Research Council Bulletin 44, 322 p., 62 pis.

Stach, E., Mackowsky, M.-Th., Teichmuller, M., Taylor, G.H., 

Chandra, D., and Teichmuller, R., 1975, Stach's textbook of 

coal petrology: Berlin, Gebriider Borntraeger, 428 p.

Traverse, Alfred, 1988, Paleopalynology: Boston, Unwin Hyman, 

600 p.

Tschudy, R.H., 1975, Normapolles pollen from the Mississippi 

embayment: U.S. Geological Survey Professional Paper 865, 

42 p., 20 pis.

 1976, Palynology of Crevasse Canyon and Menefee Formations of San Juan Basin, New Mexico, in Beaumont, E.G., Shomaker, J.W., and Stone, W.J., eds., Guidebook to coal geology 

of northwest New Mexico: New Mexico Bureau of Mines and 

Mineral Resources Circular 154, p. 48-55.

 1980, Normapolles pollen from Aquilapollenites province, 

western United States: New Mexico Bureau of Mines and Mineral Resources Circular 170, 14 p.

Published in the Central Region, Denver, Colorado 

Manuscript approved for publication March 21,1995 

Edited by Lorna Carter 

Graphics prepared by Norma J. Macs 

Photocomposition by Shelly Fields

.S. GOVERNMENT PRINTING OETICE: 1995-673-046/86127

PLATE 1

Contact photographs of the plate in this report are available, at cost, from 

U.S. Geological Survey Library, Denver Federal Center, Denver, CO 80225
	PLATE 1

	[All specimens x 1,000]

Figure 1. Stereisporites sp.

2. Cyathidites sp. cf. C. diaphana (Wilson & Webster) Nichols & Brown.

3. Echinatisporis varispinosus (Pocock) Srivastava.

4. Gleicheniidites sp. cf. G. senonicus Ross emend. Skarby.

5. Reticuloidosporites pseudomurii Elsik.

6. Corollina torosa (Reissinger) Klaus emend. Cornet & Traverse.

7, 8. Arecipites spp.

9. Cupuliferoidaepollenites minutus (Brenner) Singh.

10. Tricolpites sp.

11,12. Proteacidites spp.

13. Pseudoplicapollis cuneata Christopher.

14. Triporopollenites sp.

15. Plicapollis rusticus Tschudy.

16. Nyssapollenites albertensis Singh.

17. Foveotricolporites johnhenryensis n. sp., holotype.

18-20. Foveotricolporites johnhenryensis n. sp., paratypes.
U.S. GEOLOGICAL SURVEY BULLETIN 2115-B PLATE 1

13

10 11

15

17 18 ^^^^^^ F' 19 

SPORES AND POLLEN FROM THE STRAIGHT CLIFFS FORMATION

v

16



SELECTED SERIES OF U.S. GEOLOGICAL SURVEY PUBLICATIONS

Periodicals

Earthquakes & Volcanoes (issued bimonthly). 

Preliminary Determination of Epicenters (issued monthly).

technical Books and Reports

Professional Papers are mainly comprehensive scientific reports 

)f wide and lasting interest and importance to professional scientists and 

ingineers. Included are reports on the results of resource studies and of 

opographic, hydrologic, and geologic investigations. They also include 

:ollections of related papers addressing different aspects of a single scientific topic.

Bulletins contain significant data and interpretations that are of 

asting scientific interest but are generally more limited in scope or geographic coverage than Professional Papers. They include the results of relource studies and of geologic and topographic investigations; as well as 

collections of short papers related to a specific topic.

Water-Supply Papers are comprehensive reports that present siglificant interpretive results of hydrologic investigations of wide interest 

o professional geologists, hydrologists, and engineers. The series covers 

nvestigations in all phases of hydrology, including hydrology, availabilty of water, quality of water, and use of water.

Circulars present administrative information or important scientifc information of wide popular interest in a format designed for distribuion at no cost to the public. Information is usually of short-term interest.

Water-Resources Investigations Reports are papers of an interactive nature made available to the public outside the formal USGS pubications series. Copies are reproduced on request unlike formal USGS 

mblications, and they are also available for public inspection at deposiories indicated in USGS catalogs.

Open-File Reports include unpublished manuscript reports, maps, 

md other material that are made available for public consultation at de- 

>ositories. They are a nonpermanent form of publication that may be cit- 

:d in other publications as sources of information.

i/laps

Geologic Quadrangle Maps are multicolor geologic maps on to- 

>ographic bases in 7 1/2- or 15-minute quadrangle formats (scales mainy 1:24,000 or 1:62,500) showing bedrock, surficial, or engineering 

;eology. Maps generally include brief texts; some maps include structure 

md columnar sections only.

Geophysical Investigations Maps are on topographic or planimetic bases at various scales, they show results of surveys using geophysical 

echniques, such as gravity, magnetic, sejsmic, or radioactivity, which relect subsurface structures that are of economic or geologic significance, 

tfany maps include correlations with the geology.

Miscellaneous Investigations Series Maps are on planimetric or 

opographic bases of regular and irregular areas at various scales; they 

wesent a wide variety of format and subject matter. The series also inludes 7 1/2-minute quadrangle photogeologic maps on planimetric 

tases which show geology as interpreted from aerial photographs. The 

cries also includes maps of Mars and the Moon.

Coal Investigations Maps are geologic maps on topographic or 

planimetric bases at various scales showing bedrock or surficial geology, 

stratigraphy, and structural relations in certain coal-resource areas.

Oil and Gas Investigations Charts show stratigraphic information for certain oil and gas fields and other areas having petroleum potential.

Miscellaneous Field Studies Maps are multicolor or black-andwhite maps on topographic or planimetric bases on quadrangle or irregular areas at various scales. Pre-1971 maps show bedrock geology in relation to specific mining or mineral-deposit problems; post-1971 maps 

are primarily black-and-white maps on various subjects such as environmental studies or wilderness mineral investigations.

Hydrologic Investigations Atlases are multicolored or black-andwhite maps on topographic or planimetric bases presenting a wide range 

of geohydrologic data of both regular and irregular areas; the principal 

scale is 1:24,000, and regional studies are at 1:250,000 scale or smaller.

Catalogs

Permanent catalogs, as well as some others, giving comprehensive 

listings of U.S. Geological Survey publications are available under the 

conditions indicated below from USGS Map Distribution, Box 25286, 

Building 810, Denver Federal Center, Denver, CO 80225. (See latest 

Price and Availability List.)

"Publications of the Geological Survey, 1879-1961" may be purchased by mail and over the counter in paperback book form and as a set 

microfiche.

"Publications of the Geological Survey, 1962-1970" may be purchased by mail and over the counter in paperback book form and as a set 

of microfiche.

"Publications of the U.S. Geological Survey, 1971-1981" may be 

purchased by mail and over the counter in paperback book form (two volumes, publications listing and index) and as a set of microfiche.

Supplements for 1982, 1983, 1984, 1985, 1986, and for subsequent years since the last permanent catalog may be purchased by mail 

and over the counter in paperback book form.

State catalogs, "List of U.S. Geological Survey Geologic and Water-Supply Reports and Maps For (State)," may be purchased by mail and 

over the counter in paperback booklet form only.

"Price and Availability List of U.S. Geological Survey Publications," issued annually, is available free of charge in paperback booklet 

form only.

Selected copies of a monthly catalog "New Publications of the 

U.S. Geological Survey" is available free of charge by mail or may be obtained over the counter in paperback booklet form only. Those wishing a 

free subscription to the monthly catalog "New Publications of the U.S. 

Geological Survey" should write to the U.S. Geological Survey, 582 National Center, Reston, VA 22092.

Note.-Prices of Government publications listed in older catalogs, 

announcements, and publications may be incorrect. Therefore, the prices 

charged may differ from the prices in catalogs, announcements, and publications.
*» T