I 

Pollen Zonation and Correlation of 

Maastrichtian Marine Beds and Associated , 

Strata, Ocean Point Dinosaur Locality, North 

Slope, Alaska 

U.S. GEOLOGICAL SURVEY BULLETIN 1990-E 
AVAILABILITY OF BOOKS AND MAPS OF THE U.S. GEOLOGICAL SURVEY 

Instructions on ordering publications of the U.S. Geological Survey, along with 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 are 

listed in various U.S. Geological Survey catalogs (see back inside cover) but not listed in the most recent annual "Price and Availability 

List" are no longer available. 

Prices of reports released to the open files are given in.the listing "U.S. Geological Survey Open-File Reports," updated monthly, 

which is for sale in microfiche from the U.S. Geological Survey Books and Open-File Reports Section, Federal Center, Box 25425, 

Denver, CO 80225. 

Order U.S. Geological Survey publications by mail or over the counter from the offices given 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 periodicals (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, Books and Open-File Reports Section 

Federal Center, Bo:x 25425 

Denver, CO 80225 

Subscriptions to periodicals (Earthquakes & Volcanoes 

and Preliminary Determination of Epicenters) can be obtained 

ONLY from 

Superintendent of Documents 

U.S. 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, Map Distribution 

Federal Center, Box 25286 

Denver, CO 80225 

R Residents of Alaska may order maps from 

U.S. Geological Survey, Map Distribution 

_ New Federal Building - Box 12 

101 Twelfth Ave., Fairbanks, AK 99701 

OVER THE COUNTER 

Books 

Books 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--4230 University Dr., Rm. 101 

ANCHORAGE, Alaska--605 West 4th Ave., Rm G-84 

DENVER, Colorado--Federal Bldg., Rm. 169, 1961 Stout 

St. 

LAKEWOOD, Colorado-- Federal Center, Bldg. 810 

LOS ANGELES, California--Federal Bldg., Rm. 7638, 

300 North Los Angeles St. 

MENLO PARK, California--Bldg. 3, Rm. 3128, 345 Middlefield Rd. 

RESTON, Virginia--National Center, Rm. 1C402, 12201 

Sunrise Valley Dr. 

SALT LAKE CITY, Utah--Federal Bldg., Rm. 8105, 125 

South State St. 

SAN FRANCISCO, California--Customhouse, Rm. 504, 

555 Battery St. 

SPOKANE, Washington--U.S. Courthouse, Rm. 678, 

West 920 Riverside Ave. 

WASHINGTON, D.C.--U.S. Department of the Interior 

Bldg., Rm.265_Q, 1849 C St., NW. 

Maps 

Maps may be purchased over the counter at the U.S. 

Geological Survey offices where books are sold (all addresses 

in above list) and at the following Geological Survey offices: 

ROLLA, Missouri---1400 Indepenc,lence Rd. 

FAIRBANKS, Alaska--New Federal Building, 101 

Twelfth Ave. 
Chapter E 

Pollen Zonation and Correlation of 

Maastrichtian Marine Beds and Associated 

Strata, Ocean Point Dinosaur Locality, North 

Slope, Alaska 

By NORMAN 0. FREDERIKSEN 

A multidisciplinary approach to research studies of sedimentary rocks 

and their constituents and the evolution of sedimentary basins, both 

ancient and modern 

U.S. GEOLOGICAL SURVEY BULLETIN 1990 

EVOLUTION OF SEDIMENTARY BASINS-NORTH SLOPE BASIN 
U.S. DEPARTMENT OF THE INTERIOR 

MANUEL LUJAN, jR., Secretary 

U.S. GEOLOGICAL SURVEY 

Dallas L. Peck, Director 

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 

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1991 

For sale by the 

Books and Open-File Reports Section 

U.S. Geological Survey 

Federal Center, Box 25425 

Denver, CO 80225 

Library of Congress Cataloging-in-Publication Data 

Frederiksen, Norman 0. 

Pollen zonation and correlation of Maastrichtian marine beds and 

associated strata, Ocean Point dinosaur locality, North Slope, Alaska I by 

Norman 0. Frederiksen. 

p. em. - (Evolution of sedimentary basins-North Slope Basin ; 

ch. E) (U.S. Geological Survey bulletin; 1990-E) 

Includes bibliographical references. 

Supt. of Docs. no.: I 19.3:1990-E 

1. Palynology-Alaska-Ocean Point Region. 2. Paleobotany-Cretaceous. 

3. Paleobotany-Alaska-Ocean Point Region. 4. Stratigraphic correlation. 

I. Title. II. Series. Ill. Series: U.S. Geological Survey bulletin; 1990-E. 

QE75.B9 no. 1990-E 

(QE993] 

557.3 s-dc20 91-4305 

[561'.13'097987] CIP 
CONTENTS 

Abstract El 

Introduction El 

Palynological methods El 

Acknowledgments E3 

Stratigraphy E3 

Composite palynostratigraphic section E3 

Seismic lines 16-81 and 31-81 E3 

Composite section 16-81 + 31-81 and seismic line 41-81 ES 

Relative ages of ARCO shothole samples ES 

Relative age of sample R3328 ES 

Summary of composite palynostratigraphic section E7 

Zonation of composite palynostratigraphic section E9 

Correlation and age of composite section Ell 

Previous palynological work in Colville River region and northwestern 

Canada Ell 

Pollen zonation of the Western Interior El3 

Previous conclusions about age of sampled section El3 

Correlation of sections in Colville River region and northwestern 

Canada ElS 

Conclusions El7 

Taxonomy El8 

Rousea compta El8 

Siberiapollis constrictus El8 

Azonia hirsuta El8 

Azonia strictiparva El8 

Wodehouseia wigginsii E19 

Aquilapollenites alaskensis El9 

Aquilapollenites unicus El9 

Aquilapollenites sp. cf. A. augustus E20 

Aquilapollenites sp. A E20 

Fibulapollis inaequalis E20 

Manicorpus pseudosenonicus E21 

Sample locality register E21 

References cited E22 

PLATES 

[Plates follow References Cited] 

1. Porate, colpate, and colporate pollen 

2. Porate, colpate, and colporate pollen 

3. Colpate pollen 

4. Colpate pollen 

5. Colpate pollen 

6. Colpate pollen 

7. Col pate pollen 

FIGURES 

1. Palynologic sample locations in the lower Colville River area, Alaska E2 

2. Occurrence and range chart of angiosperm pollen taxa, composite section for 

zone A and the Wodehouseia spinata Assemblage Zone of the lower Colville 

River area, North Slope of Alaska E6 

3. Graphic correlation of shothole samples from seismic lines 16-81 and 31-81 E8 

Contents Ill 
IV Contents 

4. Graphic correlation of shothole samples from seismic line 41-81 with composite 

section 16-81+31-81 E9 

5. Ranges of some stratigraphically important pollen taxa in samples from the 

composite palynostratigraphic section constructed by graphic correlation of 

shothole samples from seismic lines 16-81, 31-81, and 41-81 ElO 

6. Ranges of pollen taxa used for zonation and subzonation of the composite 

palynostratigraphic section for the "middle" and upper Maastrichtian, lower 

Colville River area El2 

7. Map of northern North America showing localities from which Maastrichtian 

pollen has been described El4 

8. Graphic correlation of the North Slope composite section with coeval rocks of 

the Brackett basin, Northwest Territories, Canada El6 

TABLES 

1. "Middle" to late Maastrichtian pollen taxa of the North Slope, Alaska E4 

2. Definitions of "middle" and upper Maastrichtian pollen zones and tentative 

subzones, Colville River region, North Slope, Alaska Ell 
Pollen Zonation and Correlation of Maastrichtian 

Marine Beds and Associated Strata, Ocean Point 

Dinosaur Locality, North Slope, Alaska 

By Norman 0. Frederiksen 

Abstract 

A detailed composite palynostratigraphic section is 

herein constructed for the Maastrichtian rocks overlying the 

Ocean Point dinosaur locality using outcrop and seismic 

shothole samples along and near the lower Colville River, 

North Slope of Alaska. This composite section includes two 

Maastrichtian pollen zones-in ascending order, zone A (a 

new, tentative zone) and the Wodehouseia spinata Assemblage Zone of Nichols and others (1982). In the study area, 

the Wodehouseia spinata Zone is divisible into five tentative subzones. Six new pollen species are described from 

the two zones: Rousea compta, Azonia strictiparva, 

Wodehouseia wigginsii, Aquilapollenites alaskensis, Fibu-

/apollis inaequalis, and Manicorpus pseudosenonicus. 

A pollen correlation exists between reliably dated Upper 

Cretaceous sections of the Western Interior and the Brackett 

basin in the Northwest Territories of Canada. In ihis paper, 

a pollen correlation is made between the lower Colville 

River section and the Brackett basin section. This correlation shows that the study section on the North Slope is 

"middle" to latest Maastrichtian in age. The Ocean Point 

marine beds near the Colville River are within the 

Wodehouseia spinata Assemblage Zone and are "middle" 

Maastrichtian on the basis of pollen correlations. 

INTRODUCTION 

Few reliable data have been available on ages of uppermost Cretaceous strata on the North Slope of Alaska because 

these strata generally lack marine fossils. Furthermore, the 

marine fossils that are present, with the exception of benthic foraminifers, ( 1) have long geologic ranges, (2) have 

geologic ranges that seem to be different on the North Slope 

than in other regions, or (3) are endemics whose geologic 

ages are very uncertain (Marincovich and others, 1983, 1985, 

1986; Brouwers, 1988). 

The purposes of this paper are (1) to compile a composite palynostratigraphic section for the lower Colville River 

Manuscript approved for publication, May 13, 1991. 

region, from west of Ocean Point eastward and northward 

(upsection) to the top of the Cretaceous sequence in the 

region, (2) to describe and name new pollen species present 

in the composite section, and (3) to compare the stratigraphic 

ranges of important pollen taxa in the composite section 

with ranges of the taxa in the Western Interior of North 

America to determine ages of the North Slope samples. 

This study is based on occurrences of 64 angiosperm 

pollen taxa (table 1; fig. 2). These taxa were recovered from 

32 seismic-line shothole samples from west and east of the 

Colville River and from 18 outcrop samples taken along the 

Colville River, mainly west of Ocean Point (fig. 1; see "Sample Locality Register"). I previously examined approximately 

65 pollen-bearing Campanian and Maastrichtian samples 

downsection from the Ocean Point area (Frederiksen and 

others, 1988; Frederiksen, 1989); thus, the range bases of 

pollen taxa mentioned in this paper are well defined, at least 

compared to most pollen taxa previously studied in northwestern North America. 

Palynological Methods 

Palynological samples were prepared using standard 

acid maceration. All samples were separated by heavy liquid (ZnC12

), were sieved on 10-J.Un nylon screens, and were 

mounted in glycerine jelly. Preservation of pollen in nearly 

all samples was excellent. 

Slide designations show the sample number with the 

slide number in parentheses. The coordinates listed in the 

holotype descriptions and in table 3 locate the specimens on 

microscope 871956 at the U.S. Geological Survey, Reston, 

Va. On this microscope, the coordinates for the center point 

of a standard 25.4x76.2 mm slide are 38.8x102.5 (horizontal x vertical axes); the horizontal coordinates increase toward 

the right edge of the stage, and the vertical coordinates 

increase toward the front of the stage. Slides having R prefixes are stored at the U.S. Geological Survey, Reston, Va.; 

slides haying D prefixes are stored at the U.S. Geological 

Survey, Denver, Colo. Slides having ARCO labels and no 

preftx (for example, 16410) are stored at Chevron U.S.A., 

Pollen Zonation and Correlation of Maastrichtian Marine Beds, North Slope, Alaska El 
Inc., San Ramon, Calif., except slide 20738(2), which belongs to D.W. Edelman of Edelman, Percival, and Associates, Red Oak, Tex. 

A composite palynostratigraphic section is herein constructed for the "middle" and upper Maastrichtian along the 

lower Colville River. Most upper Maastrichtian samples were 

collected from shotholes along three seismic lines (fig. 1), 

and graphic correlation was used (see figs. 3, 4) to position 

the shothole samples relative to one another in the composite section (fig. 2). The principles and practice of graphic 

correlation have been described in detail in previous papers 

(Shaw, 1964; Miller, 1977; Edwards, 1984) and are not 

discussed here. The concept of graphic boxes to better defme likely true positions of range tops and bases (biostratigraphic events) was introduced by Edwards (1984). Each 

taxon is given an odd-numbered designation (see table 1); 

• ARCO 98 

• ARCO 97 

HARRISON BAY ( A-3) QUADRANGLE 

(Part) 

HARRISON BAY ( A-2) QUADRANGLE 

(Part) 

70°~~------------~~------------------------------------------~------------------------------------------------~ 

0 5 KILOMETERS t-1 ___.~, -''---..Li .,..., --'----r'l I

0 3 MILES 

AREA OF MAP 

UMIAT (D-2) QUADRANGLE 

(Part> 

ARCO 266 • 

F!gure 1. Palynologic sample locations in lower Colville River area, Alaska. Only sampled parts of U.S. Geological 

Survey seismic lines are shown. Numbered localities along the Colville River upriver from Ocean Point are sections of 

Phillips (1988). Strike and dip of the Colville Group shown in the A-2 quadrangle . 

. E2 Evolution of Sedimentary Basins-North Slope Basin 
in the graphic correlation charts (figs. 3, 4), range bases are 

identified by the taxon number and range tops are identified 

by the next higher integer than the taxon number. For example, Orbiculapollis globosa is taxon 49; the range base 

of this taxon in any particular section is event 49, and the 

range top of the taxon is event 50. A range base data point 

is marked lby the symbol "o," a range top data point by"+." 

Photographs of many Campanian and Maastrichtian 

pollen spr,cies of the Colville River region have previously been published (Tschudy, 1969; Wiggins, 1976; 

Frederiksen and others, 1988). Therefore, pollen photographs herein (pis. 1-7) show only species for which 

photographs of specimens from the study area have not 

previously been published. 

With few exceptions, the year given as part of each 

taxonomic name refers to the date when the name was published, not to a particular paper. Therefore, the "References 

Cited" do not include authors and dates that appear only as 

parts of taxonomic names. 

Acknowledgments 

I thank the following people for generously providing sampJes from Campanian and Maastrichtian rocks of 

the Colville River area: V.D. Wiggins, Chevron U.S.A., 

Inc.; H.S. Sonneman and J.B. Stough, Exxon Company, 

U.S.A.; D.W. Edelman, Edelman, Percival and Associates; 

R.A. Spicer, Oxford University; J.T. Parrish, University of 

Arizona; and T.A. Ager, K.J. Bird, E.M. Brouwers, and 

B.D. Tschudy, U.S. Geological Survey. 

STRATIGRAPHY 

Rocks sampled for this study belong to the Upper 

Cretaceous Colville Group, which consists of the Seabee, 

Schrader Bluff, and Prince Creek Formations (Brosge and 

Whittington, 1966); the Colville Group is about 1,150 m 

thick in the study area according to seismic-reflection data 

(Tetra Tech, Inc., 1982). 

The Seabee Formation is at least partly of Turonian 

age; it is not exposed in the study area. The mainly marine 

Schrader Bluff Formation and the mainly nonmarine Prince 

Creek Formation (fig. 2) overlie the Seabee. The Schrader 

Bluff and! Prince Creek Formations consist of shale, sandstone, and bentonitic and tuffaceous strata; the Prince Creek 

also includes coal beds. The two formations interfmger regionally, but in the section studied, the only rocks assigned 

to the Schrader Bluff are in the tongue composed of the 

Ocean Point marine beds (Macbeth and Schmidt, 1973; 

Wiggins, 1976; Frederiksen and others, 1988), which include the marine strata equivalent to those observed in 

sections 20-25 of Phillips (1988). These rocks apparently 

belong to the Sentinel Hill Member of the Schrader Bluff 

Formation. Prince Creek rocks in the region are tentatively 

assigned to the Kogosukruk Tongue of the formation (Brosge 

and Whittington, 1966). Overlying the Schrader Bluff and 

Prince Creek Formations are sandy, gravelly, lignitic strata 

that Carter and Galloway (1985) referred to as the Tertiary 

Sagavanirktok Formation. Few exposures of Cretaceous and 

early Tertiary strata are present in the region, except along 

streams, because these strata are blanketed by the Pliocene 

and Pleistocene Gubik Formation (Carter and Galloway, 

1985). 

In the region, the strike of the Colville Group is generally northwest (Tetra Tech, Inc., 1982; T.A. Ager, written 

common., 1988). The dip of the uppermost Cretaceous and 

lowermost Tertiary strata is approximately 1° ENE. This 

determination is based in part on correlation of strata in 

seismic shotholes in the study area (T.A. Ager, written common., 1988), in part on the dip of an Upper Cretaceous 

seismic reflector in the region (KJ. Bird, oral common., 

1989), and in part on the structure-contour maps of Werner 

(1987) for the uppermost Cretaceous and lowermost Tertiary strata in the Kuparuk River Unit (KRU) northeast of the 

study area. Werner's maps show dips of aboutl.5° ENE in 

the eastern part of the KRU, which is about 70 km northeast 

of Ocean Point, and about 1° ENE in the western part of the 

KRU, which is about 40 km northeast of Ocean Point 

COMPOSITE PALYNOSTRATIGRAPHIC SECTION 

This study is based on examination of (1) 29 seismicline shothole samples from west of the Colville River, (2) 3 

shothole samples from east of the river for which some data 

had previously been published by Wiggins (1976) but which 

have been reexamined during this study, (3) 8 outcrop samples, mainly from the Ocean Point marine beds, that had 

previously been studied (Frederiksen and others, 1988), and 

(4) 10 new outcrop samples from nonmarine strata within 

and below the sequence of Ocean Point marine beds (fig. 

1). Thus, the composite palynostratigraphic section (fig. 2) 

includes 50 samples (see "Sample Locality Register") and 

apparently represents about 239 m of section (see fig. 6). 

Samples from U.S. Geological Survey (USGS) seismic 

shothole lines (from west of the Colville River) were extremely useful for this study because very few upper 

Maastrichtian exposures are known from the lower Colville 

River area (Frederiksen and others, 1988). The USGS 

shothole samples were, according to the drillers' notes, taken 

from depths of75-90 ft (23-27 m) below the surface. 

Seismic Lines 16-81 and 31-81 

The process of compiling a composite palynostratigraphic section for the "middle" to upper Maastrichtian 

Pollen Zonation and Correlation of Maastrichtian Marine Beds, North Slope, Alaska E3 
Table 1. "Middle" to late Maastrichtian pollen taxa of the North Slope, Alaska 

[A few additional species represented by very rare specimens are shown on the plates but not listed here or shown on the range chart (fig. 2)] 

Taxon 

number 

1 

3 

5 

7 

9 

11 

13 

15 

17 

21 

23 

25 

27 

29 

31 

33 

35 

37 

39 

41 

43 

45 

47 

49 

51 

53 

55 

57 

59 

61 

Taxon 

Porate pollen 

Alnus spp. 

Anacolosidites sp. 

Betulaepollenites spp. 

Erdtmanipollis spp. 

Jarzenipollis trina (Stanley 1965) Kedves 1980 

Paraalnipollenites confusus (Zaklinskaya 1963) Hills 

& Wallace 1969, type H of Frederiksen and others 

(1988) 

Paraalnipollenites confusus type Z of Frederiksen and 

others (1988) 

Proteacidites thalmannii Anderson 1960 complex 

Triatriopollenites spp. 

Triporopollenites megagranifer (Potonie 1934) 

Thomson & Pflug 1953 type of Frederiksen and others (1988) 

Triporopollenites mullensis (Simpson 1961) Rouse & 

Srivastava 1972 

Trivestibulopollenites spp. 

Ulmipollenites krempii (Anderson 1960) Frederiksen 

1979 

Ulmipollenites tricostatus (Anderson 1960) Frederiksen 

1980 

Trlcolpate and trlcolporate pollen 

C allistopollenites radiatostriatus (Mchedlishvili in 

Samoilovich & Mchedlishvili 1961) Srivastava 1969 

Callistopollenites tumidoporus Srivastava 1969 

Callistopollenites sp. of Frederiksen and others (1988) 

Cercidiphyllites sp. of Frederiksen and others (1988) 

Cranwellia + Striatellipollis 

Kurtzipites annulatus Norton in Norton & Hall 1969 

Kurtzipites circularis (Norton in Norton & Hall 1969) 

Srivastava 1981 

Kurtzipites trispissatus Anderson 1960 

Myrtipites scabratus Norton in Norton & Hall1969 

Orbiculapollis globosa (Chlonova 1957) Chlonova 

1961 

Porosipollis porosus (Mchedlishvili in Samoilovich & 

Mchedlishvili 1961) Krutzsch 1969 

Rousea compta n. sp. 

Senipites drumhellerensis Srivastava 1969 

Siberiapollis constrictus (Samoilovich in Samoilovich 

& Mchedlishvili 1961) n. comb. 

Siberiapollis sp. aff. S. occulatus (Samoilovich in 

Samoilovich & Mchedlishvili 1961) Tschudy 1971 

= Proteacidites sp. of Frederiksen and others 

(1988, pl. 1, fig. 17) 

Siberiapollis sp. aff. Proteacidites sp. 1 of Mcintyre 

(1974) = Proteacidites sp. 1 of Mcintyre (1974) of 

Frederiksen and others (1988, pl. 1, fig. 18) 

E4 Evolution of Sedimentary Basins-North Slope Basin 

Taxon 

number 

65 

67 

69 

71 

73 

75 

77 

79 

81 

83 

85 

87 

89 

91 

93 

95 

97 

99 

101 

105 

107 

109 

111 

113 

115 

117 

119 

121 

123 

125 

127 

129 

131 

133 

Taxon 

Tricolpate and trlcolporate pollen-Continued 

Tricolpites sp. aff. T. matauraensis Couper 1953 

Trudopollis spp. 

Oculata pollen 

Azonia cribrata Wiggins 1976 

Azonia fabacea Samoilovich in Samoilovich & 

Mchedlishvili 1961 

Azonia hirsuta (Samoilovich 1965) Wiggins 1976 

Azonia sp. cf. A. hirsuta. 

Azonia pulchella Felix & Burbridge 1973 

Azonia strictiparva n. sp. 

Wodehouseia bella Wiggins 1976 

Wodehouseia edmontonicola Wiggins 1976 

Wodehouseia elegans (Samoilovich in Samoilovich & 

Mchedlishvili 1961) Wiggins 1976 

Wodehouseia gracile (Samoilovich in Samoilovich & 

Mchedlishvili 1961) Pokrovskaya 1966 

Wodehouseia octospina Wiggins 1976 

Wodehouseia quadrispina Wiggins 1976 

Wodehouseia spinata Stanley 1961 (includes Wodehouseia stanleyi Srivastava 1966) 

Wodehouseia vestivirgata Wiggins 1976 

Wodehouseia wigginsii n. sp. 

Trlprojectate pollen 

Aquilapollenites sp. aff. A. abscisus Chlonova 1961 

Aquilapollenites alaskensis n. sp. 

Aquilapollenites sp. cf. A. augustus Srivastava 1969 

Aquilapollenites conatus Norton 1965 

Aquilapollenites fusiformis Tschudy 1969 

Aquilapollenites immiser Sweet 1986 

Aquilapollenites quadrilobus Rouse 1957 

Aquilapollenites reticulatus (Mchedlishvili in 

Samoilovich & Mchedlishvili 1961) Tschudy & 

Leopold 1971 

Aquilapollenites unicus (Chlonova 1957) Chlonova 

1961 

Aquilapollenites sp. A 

Bratzevaea amurensis (Bratzeva 1965) Takahashi in 

Takahashi & Shimono 1982 

Fibulapollis inaequalis n. sp. 

Fibulapollis scabratus Tschudy 1969 

Manicorpus delicatus (Stanley 1961) Bondarenko 

1968 

Manicorpus notabile Mchedlishvili in Samoilovich & 

Mchedlishvili 1961 

Manicorpus pseudosenonicus n. sp. 

Manicorpus rostratus Srivastava 1968 
of the lower Colville River area (fig. 2) began with seismic 

lines 16-81 and 31-81 (fig. 1). A complication in arranging 

samples from line 16-81 into stratigraphic order is that some 

of the shotholes were spudded on the coastal plain at about 

100 ft (30.5 m) elevation, and some were .spudded in the 

Colville River valley floor below, at elevations of 25-i5 ft 

(7.6-13.7 m). Considering the geographic locations of the 

shotholes in this line, the topography, and the dip of the 

strata, the samples from this line were ordered stratigraphically as shown on the vertical axis of figure 3, the graphiccorrelation diagram for seismic lines 16-81 and 31-81. 

The line of correlation in figure 3 can be placed with 

considerable accuracy because ( 1) the two seismic lines cross 

(dot enclosed by a diamond in fig. 3), and (2) the slope of 

the line of correlation is known to be about 45° because the 

vertical and horizontal axes of the diagram have the same 

thickness scale and because rates of late Maastrichtian deposition in the areas of the two seismic lines are likely to have 

been very similar. Placement of the line of correlation also 

agrees with positions of the error boxes for the palynostratigraphic events in figure 3; these events (range bases 

and tops) are based on tabulated occurrences of taxa in the 

two sections. 

Composite Section 16-81 +31-81 and Seismic 

Line 41·-81 

A composite section was drawn for lines 16-81 and 

31-81 using the line of correlation in figure 3. The upper 

pmt of this composite section appears as the vertical axis in 

figure 4, a graphic-correlation diagram for composite section 16-81 + 31-81 and line 41-81. The line of correlation 

(fig. 4) can be accurately placed because a fmn tie-point 

exists between the two sections (dot enclosed by a diamond 

in fig. 4) and because the slope of the line is known. However, few palynostratigraphic events are recorded in the thin 

stratigraphic intervals shown in figure 4, and the error boxes 

for the events are large because few samples were available, particularly from seismic line 41-81. Therefore, it is 

fortunate that the line of correlation could be based on the 

locations of the seismic lines and on the inferred rates of 

sedimentation. Using the line of correlation in figure 4, samples from line 41-81 could be integrated with those of composite section 16-81+31-81 (vertical axis of fig. 5). 

Relative Ages of ARCO Shothole Samples 

As noted previously, I reexamined three ARCO 

shothole samples from east of the Colville River (fig. 1) for 

which some pollen data had been published by Wiggins 

(1976). Because the dip in the study area appears to be 

about 1° ENE, the stratigraphic sequence of the samples, in 

descending order, should be: line 1, shotpoint 98; line 1, 

shotpoint 97; line 2, shotpoint 266 (abbreviated here as 

ARCO samples 98, 97, and 266). ARCO samples 98 and 97 

can be fitted into the composite palynostratigraphic section 

because Myrtipites scabratus, Wodehouseia octospina, 

Porosipollis porosus, and Wodehouseia quadrispina are present in these samples; the first two of these species have 

defining range bases, and the last two species have defining 

range tops (fig. 5). Furthermore, ARCO 98 also contains 

the stratigraphically useful species Aquilapollenites 

alaskensis and A. conatus. Both samples lack M ani corpus 

delicatus and Wodehouseia gracile and therefore appear to 

be younger than the range tops of these two species. ARCO 

97 contains Senipites drumhellerensis; this species has the 

same observed range top as M. delicatus and W. gracile, but 

it occurs in fewer samples within the upper part of its range 

and therefore has a less distinct last occurrence than the 

other two species. Thus, these two ARCO samples must be 

in the uppermost part of the sampled Maastrichtian section 

of the area, and I consider them to lie biostratigraphically 

between samples R3819 and R3820 of seismic line 31-81. 

ARCO sample 266 contains the stratigraphically 

important species Manicorpus delicatus, Senipites drumhellerensis, and Wodehouseia gracile, which have defining 

range tops (fig. 5). Aquilapollenites conatus, Ulmipollenites 

krempii, and Wodehouseia wigginsii were not found in sample 266; therefore, the sample presumably is older than the 

range bases of A. conatus and U. krempii but younger than 

the range top of W. wigginsii. ARCO sample 266 also contains Wodehouseia vestivirgata, found west of the Colville 

River only in sample R3828 from sei~mic line 31-81 (fig. 

5). In short, several lines of evidence lead to the conclusion 

that ARCO sample 266 is slightly older than sample R3828. 

Relative Age of Sample R3328 

·Sample R3328 is the youngest Cretaceous outcrop 

sample of Frederiksen and others (1988). On the map (fig. 

1) this sample is close to seismic line 16-81, shotpoint 315; 

the sample from shotpoint 315 (not examined in this study) 

was collected from a depth of between 75 and 90ft (23-27 

m) below the top of the cliff. Sample R3328 was collected 

in the cliff face at approximately the same depth as shotpoint sample 315. Sample R3328 contains Manicorpus 

delicatus, Senipites drumhellerensis, Ulmipollenites krempii, 

and Wodehouseia quadrispina; therefore, the sample should 

lie below the range tops of M. delicatus and S. drumhellerensis and above the range bases of U. krempii and W. 

quadrispina. The stratigraphically important species 

Aquilapollenites conatus was not seen in sample R3328; 

thus, the sample may lie below the range base of this species. Accordingly, pollen data do not conflict with the approximate correlation of outcrop sample R3328 with sample R3889 (shotpoint sample 317, seismic line 16-~1). 

Pollen Zonation and Correlation of Maastrichtian Marine Beds, North Slope, Alaska ES 
UNIT 

PRINCE 

CREEK KogoFORMA- sukruk(?) 

Tongue 

TION 

SCHRADER Ocean 

BLUFF Point 

FORMA- marine 

beds 

TION 

PRINCE Kogo- CREEK sukruk FORMA- Tongue TION 

SAMPLE 

R3768 

R3924 

R3818 

R3819 

ARC098 

ARC097 

R3820 

R3821 

R3769 

R3770 

R3786 

R3787 

R3823 

R3772 

R3824 

R3825 

R3328 

R3889 

R3789 

R3826 

R3827 

R3828 

ARCO 266 

R3885 

R3890 

R3834 

R3792 

R3835 

R3837 

R3838 

R3791 

R3891 

R3892 

R3152C 

R3152B 

R3152A 

R4140A 

R4140B 

R4140C 

R4140D 

R4140F 

R4140G 

R3413Q 

R34130 

R4295H 

R3413G 

R3413E 

R4295G 

R4295F 

R4295E 

X 

X 

X 

M 

X 

M 

M 

X 

X 

X 

X 

X 

I 

X 

I 

X 

R 

X 

I 

X 

X 

l 

X 

M 

X 

X 

M 

X 

I 

X 

X 

X 

j 

X 

X 

X 

X R 

X 

I 

X 

X 

X 

I 

f 

X 

X 

M 

X 

M 

X 

X 

R 

R 

X R X M 

X 

I 

A 

I 

X 

X 

X 

X 

l 

M 

X R 

I R X 

I 

M 

X 

M 

M 

x 

I 

X 

X 

X 

X 

I 

M X 

X 

X 

I X 

X 

~ i X I M X I X 

X X 

M 

M 

X 

X 

M 

M 

M 

X 

I 

X 

I 

X 

t 

X 

R 

X 

M X 

X X X 

X 

I 

? 

X 

X 

I 

X 

X 

X X 

X 

X 

I 

X 

X 

I 

X 

X 

I 

X 

X 

X 

X X 

X 

l 

.. 

X 

X 

X 

X 

X 

X 

X 

X 

I 

X 

X 

X 

I 

X 

X 

X X 

X X 

X 

X X 

I 

X 

X 

X 

X 

I 

X X 

~ I 

X 

X 

j 

X 

X 

X 

Figure 2. Occurrence and range chart of angiosperm pollen taxa, composite section for zone A and Wodehouseia 

spinata Assemblage Zone of lower Colville River area, North Slope, Alaska. X, present; P, probably present; ?, possibly 

present; R, interpreted as reworked. Symbol "A" (meaning "affinis") indicates specimens similar to and perhaps conspecific with that species are present. Symbol "M" (meaning "many") indicates that species is most abundant of its group in 

a sample, provided at least five specimens of species were seen in sample. Groups are: Triprojectate group (Aquilapollenites 

+ Bratzevaea + Fibulapollis + Manicorpus) and Oculata group (Azonia + Wodehouseia). Stratigraphic nomenclature 

modified from Brosge and Whittington (1966) and Frederiksen and others (1988). Prince Creek rocks above Ocean Point 

marine beds were tentatively assigned to Kogosukruk Tongue of formation by Brosge and Whittington (1966). Spacing 

of samples not to scale. Obliquely ruled parts of Subzone column denote transitional boundaries. Arrows denote 

species is present above and (or) below section. 

E6 Evolution of Sedimentary Basins-North Slope Basin 
X 

X 

x 

I 

X 

X 

X 

X X 

I X 

X X 

X I 

~ i 

M 

I 

X 

I X X X 

X 

M 

X 

X X 

I 

X 

X 

X I X 

X 

X 

I 

i 

X 

X 

I 

X 

I 

X 

X 

X X 

X X 

X X X M 

X 

X 

M 

X 

X 

I X 

X X 

• • 

xx~t I X X 

X I 

X X 

X X 

I I 

X X 

X 

X 

X 

X 

I 

X 

X 

r~ ~ i I X 

i 

i 

X 

X 

X 

X 

X 

l 

Figure 2.---Continued 

X 

i 

X 

X 

I 

X 

X X 

X X 

L 

X 

X 

X 

X 

X X 

x 

I 

X 

X 

X 

• 

X 

• X 

? • X X • 

I 

X 

X 

I 

X 

X 

X I I X 

X X 

X 

X 

X X 

I 

X 

I 

X 

I 

X 

X 

X 

I X 

I 

X 

I 

X 

X 

X 

X 

X 

X X X 

X 

I 

X 

r r 

X X X 

X ~ I X 

X X X 

f l 

X I 

L~ 

Summary of Composite Palynostratigraphic 

Section 

X 

~t X X 

X X 

I I 

X X 

X X 

X X 

I 

X 

X 

X 

I 

i 

X 

X 

Shothole samples from USGS seismic lines were placed 

in stratigraphic order using graphic correlation. The three 

ARCO shothole samples and outcrop sample R3328 were 

X 

X 

X 

X 

• 

X 

X 

X 

I 

X 

X 

I 

X 

M 

I 

i 

X 

1 

X 

X 

I 

X 

X 

X 

I 

X 

I 

¥ 

X 

I 

M 

X 

X 

M 

X 

I 

l 

X M 

X X 

M X X 

X X X 

X X X 

X X X 

X X 

X X 

M X 

I M M X 

M X 

X X 

I X X M 

I I 

X X 

I 

L 

M X 

X I 

i 

r 

X 

X 

I 

X 

X 

I 

M 

I 

X 

X 

M 

X 

X 

X 

X 

X 

I 

X 

I 

X 

SAMPLE 

R3768 

R3924 

R3818 

R3819 

ARC098 

ARC097 

R3820 

R3821 

R3769 

R3770 

R3786 

R3787 

R3823 

R3772 

R3824 

R3825 

R3328 

R3889 

R3789 

R3826 

R3827 

R3828 

ARCO 266 

R3885 

R3890 

R3834 

R3792 

R3835 

R3837 

R3838 

R3791 

R3891 

R3892 

R3152C 

R31528 

R3152A 

R4140A 

R41408 

R4140C 

R4140D 

R4140F 

R4140G 

R34130 

R34130 

R4295H 

R3413G 

R3413E 

R4295G 

R4295F 

R4295E 

SUBZONE 

5 

4 

3 

1 

ZONE 

Wodehouseia 

spinata 

Assemblage 

Zone 

Zone A 

added to the composite palynostratigraphic section for the 

sake of completeness, but they add little to the knowledge of 

species ranges except to place in the sequence the occurrences of Wodehouseia bella and W. elegans. Stratigraphically 

below the USGS shothole samples are 17 outcrop samples 

whose positions are well known (Phillips, 1988); 

Pollen Zonation and Correlation of Maastrichtian Marine Beds, North Slope, Alaska E7 
The result of sample compositing is the fmal composite range chart for 64 pollen taxa in 50 samples (fig. 2) 

representing the "middle" and upper Maastrichtian in the 

lower Colville River area. As noted in the following section 

of the paper, the top of the section in figure 2 is probably 

within 7 to 21m of the Cretaceous-Tertiary boundary in the 

THICK- SHOT- PAL YNESS, POINT NOLOGICAL 

M SAMPLE 

282 R3786 

287 R3787 

100 

317 R3889 

305 R3789 

,.... 75 CX) 

cb 

w 310 R3885 z 

::J 

() 345 R3890 ~ 

(/) 

w 50 350 R3792 (/) 

0 / 

337 R3791 097 25 

369 R3891 

0 375 R3892 

CX) ""' LO "<t CX) 

C") C") C") C") C\J PALYNOLOGICAL CX) CX) CX) CX) CX) 

C") C") C") C") C") SAMPLE a: a: a: a: a: 

CX) (!) "<t C\J C\J 

SHOTPOINT ~ ~ ~ ~ C") 

THICKNESS, M 0 25 

area. The base of the study section is taken as the lowest 

occurrence of Aquilapollenites unicus, which is in section 

15 of Phillips (1988, sample 86EB93). The base of the study 

section is about 14 to 17 m above the highest tephra bed 

and the highest strata containing vertebrate fossils shown in 

Phillips' ( 1988) sections. 

""' (!) LO "<t C") (\j OOlCX> C\J C\J C\J C\J C\J (\J.-.- CX) CX) CX) CX) CX) CX) CX)CX)CX) 

C") C") C") C") C") C") C")C")C") 

a: a: a: a: a: a: a: a: a: 

0 CX) (!) 0 ~ "<t C\J.-0 

C") 

~ ~ ~ ~ 000 ,.... 

50 75 100 

SEISMIC LINE 31-81 

Figure 3. Graphic correlation of stratigraphic sections based on shothole samples from seismic lines 16-81 and 31-81 

(see fig. 1 for location of seismic lines). Dot enclosed by diamond is where two seismic lines cross. Data points are 

events (o, range base; +, range top) accompanied by event numbers. 

E8 Evolution of Sedimentary Basins-North Slope Basin 
ZONATION OF COMPOSITE 

PALYNOSTRATIGRAPHIC SECTION 

The composite palynostratigraphic section for the 

"middle" and upper Maastrichtian of the lower Colville 

River area has been divided into two pollen zones (table 

2; figs. 2, 6). These are zone A and the overlying 

Wodehouseia spinata Assemblage Zone of Nichols and 

others (1982) and Nichols and Sweet (in press). Correlation of these zones with other regions is discussed in the 

T""' 

co I 

<.0 

,.... 

z 

0 

1--

0 

w 

(j) 

w 

1--

C/) 

0 

a.. 

:2 

0 

(.) 

~ 

CJ) 

CJ) 

w 

z 

~ 

(.) 

J: 

1-

-50 

25 

0 

(.) 

~wa; CJ)Z• 

iJj:::::i~ 

~ 

CJ) 

_J 

<: 

(.) 

1- a 

z 0 

0 _J 

ow 

a. z..J 

1- >-a. 0 _J~ 

J: <:<: CJ) O.CJ) 

282 R3786 

287 R3787 

(.) 

~wa; CJ)Z• 

jjj:::::ic;) 

~ 

CJ) 

_J 

<: 

(.) 

1- a 

z 0 

0 _J 

ow 

a. z..J 

1- >-a. 0 _J~ 

J: <:<: CJ) Q.CJ) 

100 R3818 

101 R3819 

102 R3820 

104 R3821 

117 R3823 

120 R3824 

PALYNOLOGICAL N 

I'--

I'--

0 

I'--

I'--

SAMPLE C') C') 

a: a: 

..-- ~ 

SHOTPOINT N 

N C\i 

THICKNESS, M 0 

section "Correlation of Sections in Colville River Region 

and Northwestern Canada." 

The base of zone A is the range base of Aquilapollenites unicus. As mentioned previously, in the 

lower Colville River area this palynostratigraphic event 

occurs in section 15 of Phillips (1988, sample 86EB93; 

sample R4295E of fig. 2). In the study area, the range 

base of A. unicus is somewhat more distinct than the 

range base of Wodehouseia spinata because A. unicus is 

nearly ubiquitous and is usually the most abundant 

/ 

+1_o_o __________ ---i 

88 

(J) 

<.0 

I'--

C') 

a: 

0 

C\i 

25 

SEISMIC LINE 41-81 

50 

~ 

N 

(J) 

C') 

a: 

118 

89 

LO 

co 

75 

figure 4. Graphic correlation of a stratigraphic section based on shothole samples from seismic line 41-81 with the composite 

s~ction ba.sed on sho~hol~ s~mples from seismic lines 16-81 and 3.1-81 (see fig. 1 for location of seismic lines). Dot enclosed by 

d1amond 1s where se1sm1c l1nes 41-81 and 16-81 cross. Data po1nts are events (o, range base; +, range top) accompanied by 

event numbers. · 

Pollen Zonation and Correlation of Maastrichtian Marine Beds, North Slope, Alaska E9 
THICKNESS, 

M 

125 

100 

50 

25 

0 

SAMPLES BY 

SEISMIC LINE 

41-81 

R3768 

R3924 

R3769 

R3772 

16-81 31-81 

R3818 

R3819 

R3820 

R3821 

R3823 

-

-

-

-

-

R3824 .-

R3889 R3825 

R3789 R3826 

,-

,-

R3885 

R3890 

R3792 

R3827 -

R3828 ;-

R3834 .-

~ -~ ~ Cl) 

:::::: ~ c: 

Cl) 

.s ·s Cl) ~ ~ Q) 0) :0::::: ::::::: .g, Cl) ~ Q) 

s: ~ ~ ..c:: 

~ E -~ -~ Q) Q) 2 Cl) Cl) Cl) ::J "tj 

::J :::J e- Cl) 

0 0 

..c:: ..c:: 0 ~ 

~ ~ -~ :§.. c: c: 

~ ~ ~ Q) 

CJ) 

• 

~ w ' 

~ -~ 

.s Cl) 

c: Cl) ~ 

~ ~ 

Q) ~ .s :::::: ~ 

~ ~ Cl) ~ ~ Cl) 

.£!;! c: Cl) 

u ::J 0 ~ .e ~ Cl) ~ ~ u ~ e ::J ~ u 

0) o- Cl) Cl) 0 ~ 

0 ~ -~ ..Q 

-~ -~ ~ -~ Cl) 0.. 

Q) _CI) Q) ·c: c: Cl) Q) ~ Cl) :::::: Cl) Q) Q) Cl) ·c: 

::J ::J ::::::: ::::::: Cl) ::J Q) 0 0 0 0 0 -~ 0 ::::::: ..c:: .s ..c:: 0.. 0.. ..c:: 0 

~ Cl) 

~ ~ ~ .s ~ .s e ::J ::J ~ 

~ d: ~ 3 o- o- ~ ~ ~ ~ 1~ 

,, ' 

Figure 5. Ranges of some stratigraphically important pollen taxa in samples from composite 

palynostratigraphic section constructed by graphic correlation of shothole samples from seismic lines 

16-81,31-81, and 41-81. See figures 3 and 4 for graphic correlation and figure 1 for location of 

seismic lines. Dot indicates species was found in only one sample. Arrows denote species is present 

above and (or) below section. 

E1 0 Evolution of Sedimentary Basins-North Slope Basin 
Table 2. Definitions of Nmiddle" and upper Maastrichtian 

pollen zones and tentative subzones, Colville River region, 

North Slope, Alaska 

[Numbers following species names are event numbers, most of which 

are in figure 8. Ranges of defining species are shown in figure 6] 

Zone 

Wodehouseia 

spinata 

Assemblage 

Zone 

Zone A 

Subzone Datum(s) defining base of zone or 

subzone 

5 Range bases of Wodehouseia 

4 

3 

2 

1 

octospina (89) and Myrtipiles 

scabraJus ( 4 7); range tops of 

Wodehouseia gracile (88), 

Aquilapollenites sp. aff. A. 

abscisus (100), and Manicorpus 

delicaJus (128); occurrence of 

Aquilapollenites alaskensis (101) 

Range base of Aquilapollenites 

conaJus (107) 

Range bases of Ulmipollenites 

krempii (27), Orbiculapollis 

globosa (49), and Wodehouseia 

quadrispina (91); range top of 

Wodehouseia wigginsii (98) 

Range base of Wodehouseia 

wigginsii (97) 

Range base of Wodehouseia spinata 

(93 ); approximate markers are the 

range tops of Wodehouseia 

edmontonicola (84 ), 

Aquilapollenites sp. cf. A. 

augustus (106), and Fibulapollis 

scabraJus (126) 

Range base of Aquilapollenites 

unicus (117) 

species of the triprojectate group throughout the lower 

part of its range (fig. 2). In the study area, the boundary 

between zone A and the Wodehouseia spinata Assemblage Zone is primarily defined by the lowest occurrence 

of Wodehouseia spinata, but the zone boundary is also 

marked approximately by the range tops of Aquilapollenites sp. cf. A. augustus and Fibulapollis scabratus and particularly by the stratigraphically important 

range top of Wodehouseia edmontonicola. In this area, 

zone A is about 36 m thick (fig. 6). 

The Wodehouseia spinata Assemblage Zone has 

been intensively studied in North America, as discussed in 

the section "Pollen Zonation of the Western Interior." In 

the lower Colville River area, the pollen assemblage in 

sample R34130 marks the base of this zone (fig. 2), at a 

level that is near the top of section 22 of Phillips (1988). 

W. spinata has been observed in most but not all samples 

within the lower part of its range; in these samples, it is 

sparse to moderately abundant. W. spinata is more consistently present in the upper part of the upper Maaslrichtian 

in this area. In the study area, the W. spinata Assemblage 

Zone is slightly more than 200 m thick (fig. 6) and has 

been divided into five tentative subzones, as shown in 

table 2. The boundaries of several of these subzones are 

somewhat transitional (fig. 6) because the range tops and 

bases defining each subzone boundary are not always at 

the same horizon. Several species additional to those listed 

in table 2 might have been used to define subzone boundaries, but these species, for example Aquilapollenites 

reticulatus and Azonia cribrata, are so common within 

their stratigraphic ranges that they are found as reworked 

specimens higher in the section; thus, the true range tops 

of these species are not very well known. 

The tentative subzones of table 2 and figure 6 are 

relatively thin-typically about 40 m-and will be difficult 

to recognize in other places except where detailed sampling 

is possible. Nevertheless, the subzonation scheme emphasizes that, in the lower Colville River area and presumably 

throughout the North Slope of Alaska, the Wodehouseia 

spinata Assemblage Zone-representing roughly the latter 

half of Maaslrichtian time-can be subdivided using range 

tops and bases of important pollen species. 

CORRELATION AND AGE OF COMPOSITE 

SECTION 

This part of the paper is (1) a review of previous 

Maastrichtian pollen work that has been done in the 

Colville River region and in northwestern Canada, (2) a 

summary of the late Maastrichtian pollen zonation of the 

Western Interior of North America, where this zonation 

has been tied to occurrences of marine fossils and dinosaurs, (3) a summary of previous paleontological conclusions about the age of the section sampled for this paper, 

and ( 4) a discussion of pollen correlations from the 

Colville River study area to the northern Western Interior that aid in determining the age of the strata in the 

study area. 

Previous Palynological Work in Colville River 

Region and Northwestern Canada 

A relatively small number of papers and abstracts 

have been published on the Campanian and Maastrichtian palynology of the Colville River region, mainly in 

the past several years (Tschudy, 1969; Wiggins, 1976, 

1981, 1982; Frederiksen and others, 1985, 1986, 1988; 

Frederiksen, 1986, 1989; Brouwers and others, 1987; 

Frederiksen and Schindler, 1987). What has been lacking 

for the North Slope of Alaska is detailed knowledge of 

Pollen Zonation and Correlation of Maastrichtian Marine Beds, North Slope, Alaska Ell 
(/) (/) 

.2 ;::, 

(/) -~ ;::, 

g> (/) 

~ .a 

0 ctl ctl -~ .S:2 ~ ctl 

~ .s (/) 

c: c: (/) ctl .E :::::: 

~ ~ (J) (/) 

ctl .2 .s ::::::: 13 (/) (/) ..!lc:: ;::, c: .m .2 .s (/) 

~ {3 (/) .S:2 (/) ctl 

0 ci. .2 ci. ~ ctl 0 c: ~ ~ (/) 

~ ~ t:n (.) c: .s .a 0 (/) .2 .E .Q) ~ ~ (/) ctl ctl ;::, (.) 

.a ;::, ~ ~ Q ~ (.) 

(J) (/) 

~ ~ t:n (/) o- (/) (/) t:n (/) .a 0 ..!lc:: 

-~ -~ -~ ~ -~ -~ -~ -~ -~ -~ -~ ~ ~ -~ (/) (/) (J) c: (J) (/) (J) c: (J) c: c: (J) :::::::: ·c: (J) ~ (/) (J) 

~ (/) ;::, (/) ~ (/) (J) 

~ (/) 0 ~ (/) (/) ·c: 

;::, ::::::: ;::, e. ;::, ;::, ::::::: ;::, 

~ (/) ;::, 

0 0 0 0 0 0 0 0 0 0 0 ~ -~ 0 

THICK- ..c:: 0.. 0.. ..c:: 0 ..c:: 0.. ..c:: 0.. g. ..c:: ;::, 0.. ..c:: 0 

~ ~ ~ ~ .S:2 ~ ~ ~ ~ :-::::: ~ .S:2 ~ .s ~ .9-

NESS, ;::, ;::, c: ;::, ;::, ;::, -e ;::, t:: .§ SUB- ~ o- ~ ~ ~ ~ o- ~ o- o- ~ oUNIT M <( <( <( <( 0 <( ~ ~ ::::> ZONE ZONE 

5 

f-200 I I 

z 

0 

i= Q) 

<( ::J 

:2 C) 

c: a: 0 

0 IWodehouseia 

1--

u. c::- ~ ?£ 1-

LU ::J 

a: 

LU ~ ::J () (/) 

spinata 150 

LU 0 

C) 

() 0 Assemblage 

z ~ 

a: 

a.. Zone 

- 100 2 

-

a: c ~u. 1-

<( u. . ~~(/) a:::J:2 ·- "'0 

I_JU. C: ..... Q) 

corn.o ()Ill ~E C/) 0 Vw~c:( " I~ Q) 0LU;2Z O::J::J ZL.Ua:O O)lo....O) 

c:a:oi= 0~ c: ~::Jo c...Ou. (/)IZone A 

Ill ' 

50 

0 

Figure 6. Ranges of pollen taxa used for zonation and subzonation (table 2) of composite palynostratigraphic section 

for the "middle" and upper Maastrichtian strata in Ocean Point area of lower Colville River (fig. 2). Obliquely ruled 

portions of Subzone column denote transitional subzone boundaries. Arrows denote species is present above and (or) 

below section. 

E12 Evolution of Sedimentary Basins-North Slope Basin 
the Upper Cretaceous pollen stratigraphy. The most detailed palynostratigraphic papers published thus far are by 

Wiggins (1976) and Frederiksen and others (1988). Wiggins 

(1976, table 1) provided Campanian and Maastrichtian 

pollen ages for several specific localities near Ocean Point 

and to the south on the Colville River. His age determinations, particularly for the Maastrichtian, were based mainly 

on pollen correlations with other regions of northern North 

America and Siberia. Building on Wiggins' work, 

Frederiksen and others (1988) studied palynomorph assemblages from 8 Cretaceous outcrop samples from the 

Ocean Point area and 11 Paleocene outcrop samples from 

localities east and northeast of Ocean Point. Their data 

helped in determining an approximate position of the 

Cretaceous-Tertiary boundary in the area. 

After completing work that was included in 

Frederiksen and others (1988), T.A. Ager (written 

commun., 1988) examined 11 pollen-bearing seismic 

shothole samples and additional outcrop samples from 

northeast of the Cretaceous samples studied for this 

paper. His determination of Paleocene ages for these 

new samples, based on palynological evidence, means 

that the stratigraphically highest sample considered in 

this paper is within 7 to 21 m of the Cretaceous-Tertiary 

boundary. 

The uppermost part of the Cretaceous sequence of the 

lower Colville River area must be very late Maastrichtian in 

age because it contains pollen species that elsewhere in the 

Western Interior are not present below. the uppermost 

Maastrichtian. These are Ulmipo/lenites krempii, Myrtipites 

scabratus, and Wodehouseia quadrispina. In western Canada 

from Alberta to the southwestern Canadian Arctic Islands, 

the uppermost parts of many Cretaceous sections consist of 

an interval, 12 em to 30m thick, in which the angiosperm 

component of the pollen flora is of very low diversity 

(Doerenkamp and others, 1976, zone CVII; Jerzykiewicz 

and Sweet, 1986; Lerbekmo and others, 1987; Sweet, 1988; 

Sweet and Braman, 1988). This uppermost Maastrichtian 

interval may be represented in the study area by the interval 

of decreased pollen diversity that forms the uppermost 30 m 

of the lower Colville River composite palynostratigraphic 

section (Frederiksen, 1989, fig. 3). However, only two 

samples were examined palynologically from this interval 

(R3768 and R3924 of figs. 2 and 6); therefore, details are 

lacking about the diversity decrease at the top of the Cretaceous section. 

Maastrichtian pollen species from northwestern 

Canada have been listed in theses and published papers 

(fig. 7). The most thorough pollen-stratigraphic work in 

this region is by Nichols and Sweet (in press) on the 

Bonnet Plume basin, Yukon Territory (fig. 7, Joe. E) and 

Brackett basin, Northwest Territories (fig. 7, Joe. F), by 

Sweet and others (1989) on the Brackett basin, and by 

Mcintyre (1974), Doerenkamp and others (1976), Sweet 

(1978), Wilson (1978), and Kalgutkaf and Sweet (1988) 

in the Mackenzie Delta region (fig. 7, loc. D). 

Pollen Zonation of the Western Interior 

Nichols and others (1982) provided a palynomorph 

zonation for the Cretaceous rocks of the central and northem Rocky Mountains region of the United States. They 

defined the Wodehouseia spinata Assemblage Zone to include rocks between the range base of the nominate species and the range tops of many latest Cretaceous species, 

range tops that were demonstrated to coincide with the 

Cretaceous-Tertiary boundary. The Wodehouseia spinal a 

Assemblage Zone is considered to be late Maastrichtian; 

because marine fossils and dinosaurs are present in the 

rocks assigned to this pollen zone in· the Rocky Mountains, 

the zone is believed "to be equivalent to the zone of the 

ammonite Hoploscaphites nicolleti and stratigraphically 

overlying biozones, including the nonmarine biozone of 

the dinosaur genus Triceratops, (Nichols and others, 1982, 

p. 729). In the Western Interior (except in Alberta), the 

base of the Wodehouseia spinata Assemblage Zone is 

thought to approximate the boundary between the lower 

and upper Maastrichtian (Nichols and Sweet, in press). 

This boundary is estimated to have an age between 71 and 

70 Ma, and the age of the Cretaceous-Tertiary boundary is 

about 66.5 Ma (Haq and others, 1987). Thus, the W. 

spinata Assemblage Zone probably represents approximately 4 m.y. of time (Nichols and others, 1982). It must 

be pointed out that the Wodehouseia spinata Assemblage 

Zone of Nichols and others (1982) (and Nichols and 

Sweet, in press) differs from the Wodehouseia spinata 

Zone of Srivastava (1970), which includes lowermost 

Paleocene strata (Lerbekmo and others, 1987). 

Nichols and Sweet (in press) conducted an extensive 

review of geologic and geographic ranges of pollen species in the Upper Cretaceous rocks from New Mexico to 

northwestern mainland Canada. They showed that Wodehouseia spinata appears to have an approximately isochronous range base nearly throughout the Western Interior; 

the only area where the range base of the species is known 

to be a different age is in Alberta, where the first appearance of W. spinata is younger than elsewhere. 

Regional pollen zonations for parts of northwestern 

Canada have also been proposed, and these will be discussed herein. 

Previous Conclusions About Age of Sampled 

Section 

Most of the strata studied for this paper lack marine 

fossils; thus, at present, pollen grains are the most important 

Pollen Zonation and Correlation of Maastrichtian Marine Beds, North Slope, Alaska E13 
_.). 

oo 

ALASKA 

X 

0 

0 

~ 

0 

0 

t") 

+ 

ARCTIC OCEAN 

en f D \ D 

,_ I.UI J - ~ II(' \ 

en:~ .~, 

~ / ~ e s\. 

,_;o ' 

NORTHWEST TERRITORIES 

• F 

~~ YUKON \ 

,:, 1 TERRITORY \ 

. \~ -( L \-1-- ----- ' ~--------- T \ . ' I'~ \ \ ~ \ \ 

0 

&0 

------~~--~------------~L\~~--------~---------~ ~ oo 0 

0 

II) 

0 

0 

200 400 600 

200 400 

c.l 

00 

800 1000 KILOMETERS 

600 800 1000 MILES 

Figure 7. Map of northern North America showing localities from which Maastrichtian pollen has been described. Locality A 

is Colville River study area; other localities are from the following papers and theses: B-Choi (1983); C-Doerenkamp and 

others (1976); D (Mackenzie Delta region)-Mclntyre (1974), Doerenkamp and others (1976), Sweet (1978), Wilson (1978), 

Kalgutkar and Sweet (1988); E (Bonnet Plume basin)-Rouse and Srivastava (1972), Kalgutkar and Sweet (1988), Nichols and 

Sweet (in press); F (Brackett basin)-Bihl (1973), Wilson (1978), Sweet and others (1989), Nichols and Sweet (in press). 

E14 Evolution of Sedimentary Basins-North Slope Basin 
fossils for dating the bulk of the sequence. A variety of 

marine fossils (mainly mollusks, ostracodes, benthic foraminifers, and dinoflagellate cysts) have been studied from the 

Ocean Point marine beds (fig. 6), but the interpretation of 

some of these marine fossils is controversial. 

Using mollusk and ostracode evidence, Marincovich 

and others (1985, 1986) and Brouwers (1988) suggested 

that the Ocean Point marine beds are early Tertiary in age. 

However, most species of mollusks and ostracodes in these 

beds are endemic to the North Slope; thus, the ages of these 

fossils are uncertain. On the basis of benthic foraminifers, 

the Ocean Point marine beds were originally thought to be 

late Campanian in age (Macbeth and Schmidt, 1973) but 

are now considered to be early Maastrichtian (McDougall, 

1987) or late Maastrichtian (W.V. Sliter, oral common., 

1989). Dinoflagellate cyst evidence suggests that the Ocean 

Point marine beds are late Campanian or Maastrichtian in 

age (Frederiksen and others, 1988). 

On the basis of pollen data that were explained 

only in part, Wiggins (1976, fig. 2 and table 1) showed 

the Ocean Point marine beds as approximately midMaastrichtian, and he dated several samples from seismic shotholes lying southeast of Ocean Point as late 

Maastrichtian in age. Also on the basis of pollen evidence, but without making detailed correlations with 

other regions, Frederiksen and others (1988) considered 

the Ocean Point marine beds to be mid-Maastrichtian in 

age and placed the Cretaceous-Tertiary boundary about 

7.5 km northeast (upsection) of Ocean Point. 

Marincovich and others (1985, 1986) suggested that 

the Cretaceous palynomorphs in the Ocean Point beds may 

be redeposited specimens. However, the occurrence of late 

Maastrichtian pollen taxa (for example, Wodehouseia 

quadrispina, W. octospina, Aquilapollenites conatus) 

above but not in or below the Ocean Point beds (fig. 2) 

indicates that the Ocean Point marine beds underlie upper 

Maastrichtian strata and therefore are Late Cretaceous in 

age. Furthermore, the order in which particular pollen 

events (range bases and tops) occur is the same in all three 

seismic-line sections west of the Colville (figs. 3, 4); this 

similarity of event ordering in different parts of the area 

strongly suggests that the observed sequence of range 

bases and tops reflects evolution, extinction, immigration, 

and emigration and is not due to reworking. 

Correlation of Sections in Colville River Region 

and Northwestern Canada 

Three zonations based at least partly on pollen have 

been proposed for Upper Cretaceous stratigraphic sequences in northwestern Canada. Doerenkamp and others (1976) 

established a pollen and dinoflagellate zonation for the 

Mackenzie Delta region (fig. 7, loc. D) and the southwestem region of the Canadian Arctic Islands (fig. 7, loc. C). 

Their zones CVIc and CVll are equivalent to the W odehouseia spinata Assemblage Zone of the Western Interior. 

However, Doerenkamp and others (1976) did not provide 

detailed range data for Maastrichtian pollen species in their 

study region. Sweet and others (1989) proposed a tentative 

pollen zonation for the Brackett basin, Northwest Territories (fig. 7, loc. F); this zonation used pollen species names 

as zone identifiers (fig. 8). Finally, Sweet (in Nichols and 

Sweet, in press) created an-additional tentative zonation that 

applied to a composite palynostratigraphic section for the 

Brackett basin, Northwest Territories, and Bonnet Plume 

basin, Yukon Territory (fig. 7, loc. E); this zonation used 

numerals as identifiers, and the zones were termed assemblages (fig. 8). Independent age assignments are generally 

lacking for the Maastrichtian sequences in the Bonnet Plume 

and Brackett basins; thus, ages of the zones and assemblages were mainly determined by correlating them with pollen assemblages in Alberta, Montana, and Wyoming that 

were independently dated on the basis of marine and vertebrate fossils. Nichols and Sweet considered their assemblage 9 to be "early late Maastrichtian" and assemblage 10 

to be "latest Maastrichtian" on the basis of these correlations; ages assigned to the zones of Sweet and others (1989) 

are shown in figure 8. 

A graphic-correlation diagram (fig. 8) was constructed 

by comparing pollen range bases and tops on the North 

Slope of Alaska (fig. 2) with those in coeval rocks of the 

Brackett basin in northwestern Canada (Nichols and Sweet, 

in press, table 1 and fig. 5; Sweet and others, 1989; Sweet, 

written common., 1989). In Maastrichtian time, the North 

Slope (fig. 7, loc. A) was at a latitude of approximately 79°, 

and the Brackett and Bonnet Plume basins (fig. 7, locs. F, 

E) were at a latitude of approximately 71° (calculated on 

the basis of maps 19 and 23 of Smith and others, 1981). 

It is easy to make generalized pollen correlations 

of "middle" to late Maastrichtian rocks between the 

North Slope of Alaska and northwestern Canada, but it 

is difficult to make very detailed correlations between 

the two regions, for several reasons. First, some stratigraphically important species found in northwestern 

Canada were not observed in the North Slope samples, 

for example Aquilapo/lenites attenuatus Funkhouser 

1961, A. reductus Norton 1965, A. parallelus Tschudy 

1969, A. delicatus Stanley 1961 var. collaris Tschudy & 

Leopold 1971, and Manicorpus gibbus Srivastava 1968; 

all of these species except Aquilapollenites parallelus 

occur as far south as the Wyoming-Montana-Alberta region, but the ranges of the producing plants may not 

have extended as far north as the North Slope. Conversely, some species found on the North Slope have not 

been recorded from northwestern Canada, apparently because their ranges did not extend that far south; 

examples are Aquilapollenites alaskensis, Fibulapollis 

Pollen Zonation and Correlation of Maastrichtian Marine Beds, North Slope, Alaska E15 
inaequalis, F. scabratus, Wodehouseia vestivirgata, and· 

W. wigginsii. A second difficulty in. using pollen for detailed correlations between sections in the North Slope 

and northwestern Canada is that some species common 

<( 

~ 

(j) 

<( 

.....J 

<( 

ui 

a.. 

0 

.....J 

(j) 

I 

1-

0: 

0 

z 

z 

0 

i= 

<( 

~ 

(( 

0 

u.. 

PRINCE 

CREEK 

FORMATION 

SCHRADER 

BLUFF 

FORMATION 

PRINCE 

CREEK 

FORMATION 

w 

z 

0 

N 

Q) 

c: 

0 

N 

Q) 

Ol 

ro 

::0 

E 

Q) 

(/) 

(/) 

<( 

~ 

cu 

.s: 

~ 

.~ 

Q) 

(/) 

:::J 

0 

..c:: 

~ 

~ 

<( 

Q) 

c: 

0 

N 

w 

z 

0 

N 

m 

::J 

(/') 

5 

1---f4 

~ 

3 

-

1-

2 

I--

1 

~ 

u) 

(/') 

w 

z 

~ 

() 

:C 

t200 

100 

0 

93 

0 

0 

88 

+ 

133 

0 

Wodehouseia 

gracile! 

Aquilapollenites 

parallelus 

Zone 

"MID(?) 

MAASTRICHTIAN" 

89 

0 

100 

I 

Manicorpus gibbus! 

Scollardia trapaformis 

Zone 

9 

"MID-MAASTRICHTIAN" 

Porosipollis 

porosus 

Zone 

"MID OR 

LATE MAASTRICHTIAN" 

SUMMIT CREEK FORMATION 

BRACKETT BASIN, 

NORTHWEST TERRITORIES 

47 

134 

EB 

27 

200 

I 

Myrtipites 

scabratus 

A~uila- polenites 

delicatus 

var. collaris 

Zone 

10 

"LATEST 

MAASTRICHTIAN" 

I 

THICKNESS, M 

ZONE 

ASSEMBLAGE 

AGE 

FORMATION 

Figure 8. Graphic correlation of North Slope composite section (fig. 7, loc. A) with coeval rocks of Brackett basin, Northwest 

Territories (fig. 7, loc. F). Data points are events (o, range base; +, range top) accompanied by event numbers. Range top event 

labeled K-T is Cretaceous-Tertiary boundary defined by range tops of several Maastrichtian pollen species (see text). On 

horizontal axis, the thickness, zone, age, and formation columns are from Brackett basin (Sweet and others, 1989, p. 89-98); 

assemblages pertain to both Brackett and Bonnet Plume basins and are from Nichols and Sweet (in press). Base of section 

shown for Brackett basin is base of assemblage 9 and base of the Wodehouseia gracile/Aquilapollenites paralle/us Zone. 

E16 Evolution of Sedimentary Basins-North Slope Basin 
to the two regions appear to have diachronous range tops 

and (or) range bases within northern North America, as 

shown by the distance of these event points from the line 

of correlation in figure 8. Examples of apparently 

diachronous events are 88 (range top of Wodehouseia 

gracile), 89 (range base of W. octospina), 27 (range base 

of Ulmipollenites krempii), and 11 (range base of 

Paraalnipollenites confusus type H). 

The upper end of the line of correlation in figure 8 

is at the Cretaceous-Tertiary boundary on the North 

Slope and in the Brackett basin. Not shown on the diagram are individual range tops of many species that are 

at or slightly below the Cretaceous-Tertiary boundary in 

both regions (for example, range tops of Aquilapollenites 

conatus, Wodehouseia spinata, W. octospina, and 

Myrtipites scabratus); these range tops in the North 

Slope section are shown in figures 2 and 6. 

Nichols and Sweet (in press) concluded that the 

range base of Wodehouseia spinata (event 93) in the 

Brackett and Bonnet Plume basins of northwestern Canada 

was approximately isochronous with the same event in the 

Western Interior of the United States. However, Sweet 

(written commun., 1989) believes that the range base of 

the species may be slightly older in northwestern Canada 

than in the Wyoming-Montana-Alberta region. In any 

case, it seems reasonable to assume that the range base of 

W. spinata is approximately the same age on the North 

Slope of Alaska as in northwestern Canada, and for this 

reason event 93 is used to anchor the lower end of the line 

of correlation in figure 8. The range base of W. spinata is 

by definition the base of the Wodehouseia spinata Assemblage Zone of Nichols and others (1982) and Nichols and 

Sweet (in press), the base of the Wodehouseia gracile/ 

Aquilapollenites parallelus Zone of Sweet and others 

(1989), and the base of Assemblage 9 of Nichols and 

Sweet (in press). 

In contrast to the probably isochronous range base 

of Wodehouseia spinata, the range base of Aquilapollenites unicus (not shown in fig. 8) is apparently 

highly diachronous in northwestern North America. On 

the North Slope, the latter event marks the base of zone 

A but is stratigraphically only about 36 m below the 

range base of Wodehouseia spinata (event 93). In the 

Bonnet Plume basin, the range base of A. · unicus is 

within assemblage 8, in rocks thought to be "middle" 

Maastrichtian in age (Nichols and Sweet, in press), but 

apparently it is stratigraphically well below the range 

base of W. spinata in that basin. In the Brackett basin, 

the range base of A. unicus may be late Campanian according to Sweet and others (1989) and therefore much 

older than the same event on the North Slope or in the 

Bonnet Plume basin. 

As noted previously, the range base of Paraalnipollenites confusus type H (event 11) is well below the 

line of correlation; its position suggests this event is much 

older on the North Slope of Alaska than in the Brackett 

basin. However, specimens of P. confusus type Hare rare 

in the Maastrichtian of the Bonnet Plwne and Brackett basins 

(A.R. Sweet, written commun., 1988), and only scattered 

occurrences of the species are noted in the Maastrichtian of 

the North Slope (fig. 2); thus, the true range bases of P. 

confusus type H are probably not very well known in different regions of northern North America. Events 133 and 134 

are the range base and range top, respectively, of Manicorpus 

rostratus; this species has a much longer stratigraphic range 

in the Brackett basin than on the North Slope. 

On the North Slope of Alaska, the range base of consistently occurring Wodehouseia quadrispina (event 91) is 

stratigraphically below the range base of W. octospina (event 

89), but in the Brackett basin the reverse is true (Sweet, 

written commun., 1989). However, in both regions the 

presence of these two species is a useful marker for approximately the upper fourth of the Maastrichtian Stage (assuming that in these regions the range base of Wodehouseia 

spinata is mid-Maastrichtian or late early Maastrichtian in 

age). The range bases of Aquilapollenites conatus (event 

107) and Myrtipites scabratus (event 47) and the range top 

of Porosipollis porosus (event 52) seem to be approximately isochronous in the Brackett basin and on the North Slope. 

Nichols and Sweet (in press) noted that in the Bonnet 

Plume and Brackett basins, the ranges of Wodehouseia gracile and W. spinata only slightly overlap; this is shown in 

figure 8 by the range top of Wodehouseia gracile (event 88) 

lying stratigraphically above the range base of W. spinata 

(event 93), but both events are in the lower part of assemblage 9. Conversely, Nichols and Sweet noted that farther 

north, in the Mackenzie Delta region (fig. 7, loc. D), there 

is a greater overlap of ranges for Wodehouseia gracile and 

W. spinata. An even greater interval of overlap of the two 

species exists on the North Slope of Alaska, where event 88 

is stratigraphically far above event 93. In short, W. gracile 

apparently died out earlier in the south than in the north. 

The stratigraphically high occurrences of W. gracile on the 

North Slope are not likely to consist of reworked specimens, because W. gracile is found in many samples throughout its stratigraphic range, and it is the most abundant species 

of the Oculata group (Azonia + Wodehouseia) in some samples as high as subzone 3 of the Wodehouseia spinata Assemblage Zone (fig. 2). 

CONCLUSIONS 

1. The first detailed palynostratigraphic section is 

published for rocks on the North Slope of Alaska; it shows 

ranges of 64 angiosperm pollen taxa in 50 outcrop and 

seismic shothole samples from the "middle" and upper 

Maastrichtian. Six of the species are new. 

Pollen Zonation and Correlation of Maastrichtian Marine Beds, North Slope, Alaska E17 
2. The composite study section consists of two pollen zones. These are, in ascending order, zone A (a new, 

tentative zone) and the Wodehouseia spinata Assemblage 

Zone of Nichols and others (1982). In the study area, the 

Wodehouseia spinata Zone is divisible into five tentative 

subzones that will make detailed correlations in the region 

more reliable than was previously possible. 

3. The study section for the lower Colville River is 

correlated on the basis of pollen with "middle" to upper 

Maastrichtian strata of the Brackett basin, Northwest 

Territories of Canada. The Brackett basin had previously 

been correlated, also on the basis of pollen, with Upper 

Cretaceous sequences of the Western Interior that were 

reliably dated with ammonites, dinosaurs, and the iridium 

anomaly marking the Cretaceous-Tertiary boundary. Pollen correlation shows that the top of the Cretaceous section along the lower Colville River is latest Maastrichtian 

in age. 

4. The Ocean Point marine beds on the Colville 

River are within the Wodehouseia spinata Assemblage 

Zone. These marine beds are "middle" Maastrichtian, as 

determined by pollen correlations. 

TAXONOMY 

The following six new species are herein formally 

named, illustrated, and described: 

Rousea compta 

Azonia strictiparva 

Wodehouseia wigginsii 

Aquilapollenites alaskensis 

Fibulapollis inaequalis 

Manicorpus pseudosenonicus 

Two additional new species, Aquilapollenites sp. cf. 

A. augustus and Aquilapollenites sp. A, are also illustrated and described. In addition, two new combinations 

(Siberiapollis constrictus and Aquilapollenites magnus) are 

proposed, the morphology of Azonia hirsuta is discussed, 

and evidence as to the range top of Aquilapollenites unicus 

is reviewed. Details on sample locations are given in the 

"Sample Locality Register." 

Rousea compta n. sp. (taxon 53) 

Plate 1, figures 21-26; plate 2, figures 1-3 

Holotype.-Slide 16408-4(B), coordinates 

38.1x109.0; pl. 1, figs. 21-23; west bank of Colville 

River, Umiat D-3 quadrangle, lower Maastrichtian. 

Description.-Prolate to subprolate tricolpate pollen grains. Polar axis 25-39 J.l.lll; equatorial axis 17-29 

J.Lm (10 measured specimens); holotype 30x19 J.Lm. Poles 

moderately to rather broadly rounded. Colpi extend %-4Js 

length of polar axis; margins of colpi not thickened. 

Exine 1-2 J.U11 thick; ektosexine, endosexine, and nexine 

E18 Evolution of Sedimentary Basins-North Slope Basin 

about the same thickness. Most of exine is rather 

coarsely reticulate, maximum diameter of brochi in different specimens is 1-2 J.l.lll. However, the brochi are 

much smaller at the poles, mainly <0.5 J.l.lll. 

Remarks.-This species is characterized by the distinct difference in size of brochi between the poles and 

most of the remainder of the grain (compta, Latin for 

"ornamented"). 

Distribution.-Lower Maastrichtian to upper 

Maastrichtian (to subzone 3 of the Wodehouseia spinata 

Assemblage Zone) of the Colville River area. 

Siberiapollis constrictus (Samoilovich in Samoilovich & 

Mchedlishvili 1961) n. comb. (taxon 57) 

Plate 2, figures 4, 5 

Basionym.-Proteacidites constrictus Samoilovich 

in Samoilovich and Mchedlishvili, 1961, p. 182, pl. 57, 

figs. 3-4. 

Remarks.-Proteacidites is triporate, but this species 

is distinctly brevitricolporate. 

Azonia hirsuta (Samoilovich 1965) Wiggins 1976 (taxon 73) 

Plate 2, figures 8, 9, 12 

}acutiana hirsuta Samoilovich, 1965, p. 131-132, fig. 11 a, b; pl. 

4, figs. 1 a-g, 2a-g. 

Ocellipollis munitus Chlonova, 1966, p. 66-67, pl. 1, figs. 1-4. 

Azonia hirsuta (Samoilovich) Wiggins, 1976, p. 61. 

Remarks.-The two specimens of Jacutiana hirsuta illustrated by Samoilovich (1965) do not have obvious apertures, but the outlines of the specimens have 

weakly expressed indentations where apertures would be 

if the grains lay in equatorial view. The holotype of 

Ocellipollis munitus is almost identical to the holotype 

of Jacutiana hirsuta except that the holotype of 0. 

munitus has distinct slit-like apertures; therefore, 

Wiggins (1976) was justified in considering the two species to be conspecific. The other specimens of 0. 

munitus illustrated by Chlonova (1966) have considerably thicker exines than the holotype and may represent 

a different species. 

Azonia strictiparva n. sp. (taxon 79) 

Plate 2, figures 13-15 

Azonia cf. A parva Wiggins 1976. Frederiksen and others, 1988, 

pl. 1, figs. 24-25. 

Holotype.-Slide R4140A(3), coordinates 54.1x99.9; 

pl. 2, fig. 13; nonmarine beds within the sequence of Ocean 

Point marine beds near Ocean Point, "middle" Maastrichtian. 

Description.-Isopolar pollen grains with bilateral 

symmetry. Short axis of grain 16-21 J.l.lll; long axis 20-

25 J.Lm (8 measured specimens). Dimensions of holotype 

19x22 J.Lm. Apertures 2-geminicolpate, colpi 6--10 J.Lm 

long, slitlike or slightly open, with rough margins. Exine 

1-1.5 J.Lm thick at sides of grain and 0.8-1 J.Lm thick at 
the ends. Sexine tectate; columellae distinct; endosexine 

generally thicker than nexine or ektosexine. Design of 

sexine finely reticulate to granulate. 

Remarks.-Grains in this species are symmetrical 

(stricti-, Latin for "straight"), whereas grains in Azonia 

parva Wiggins 1976 are fabiform. Grains of A. strictiparva 

are also considerably smaller than those of A. parva. 

Distribution.-Lower Maastrichtian to "middle" 

Maastrichtian (to subzone 1 of the Wodehouseia spinata 

Assemblage Zone) of the Colville River area. 

Wodehouseia wigginsii n. sp. (taxon 97) 

Plate 3, figures 1-4 

Holotype.-Slide R3837(2), coordinates 25.4x101.4; 

pl. 3, figs. 1, 2; from U.S. Geological Survey seismic line 

31-81, shotpoint 146, upper Maastrichtian. 

Description.-Isopolar pollen grains with bilateral 

symmetry. Overall dimensions of grain 29-37x32-51 J.1ffi 

(9 measured specimens); holotype 35x48 J.lffi. Apertures 2-

geminicolpate, colpi oval to boat shaped, 4-5 J.1ffi long, 

with smooth margins; centers of colpi 8-11 J.1ffi apart. 

Nexine of body and sexine of carinate flange each about 1 

Jlm thick. Width of flange, 5-6 J.l.m along sides of grain 

and 0.8-1.5 J.1ffi at ends of grain. Sexine of body tectate; 

design of sexine over body finely reticulate. The only 

spines on the body are scattered short spines at ends of 

grain; flange has radiating long spines, some of which 

project beyond edge of flange. 

Remarks.-This species is characterized by lacking 

spines on the body except at the ends of the grain. The 

species is named after Virgil D. Wiggins of Chevron 

U.S.A., Inc. 

Distribution.-Upper Maastrichtian (subzone 2 of 

the Wodehouseia spinata Assemblage Zone) of the 

Colville River area. 

Aquilapollenites a/askensis n. sp. (taxon 1 01) 

Plate 3, figures S-9 

Holotype.-Slide ARCO 98(B), coordinates 

48.6x105.8; pl. 3, figs. 7, 8; sample from ARCO seismic 

line 1, shotpoint 98, east of Colville River, upper 

Maastrichtian. 

Description.-Tricolpate, isopolar pollen grains with 

three equatorial projections. Polar axis 41-57 J.lffi; equatorial axis including projections 48-65 Jlm (13 measured 

specimens). Width of body (between bases of projections) 

14-21 J..Lffi; width of equatorial projections at their midpoint 

9-11 J.lffi. Dimensions of holotype: polar axis 55 J.lffi; equatorial axis approximately 62 J.lffi. Poles of body and tips of 

equatorial projections broadly rounded; attachment areas of 

equatorial projections to body sharply concave. The body 

tends to decrease in width in the equatorial area ("waspwaisted"). Colpi rather obscure, apparently extending only 

from the tips to the bases of the equatorial projections. Exine 

about 1 J.1ffi thick in most areas, 0.5 J.1ffi thick at tips of 

projections. Nexinal costae 1.5-2 J.1ffi thick, extending about 

two-thirds the length of the equatorial projections but barely 

extending onto body of grain. Sexine tectate; columellae 

indistinct at high power. Sexine punctate and finely conate; 

coni closer together on equatorial projections than on body. 

Remarks.-This species is distinguished by its 

straight-sided to "wasp-waisted" body and finely conate 

sexine. The body has a greater length to width ratio than 

in Aquilapollenites unicus (Chlonova 1957) Chlonova 

1961 and A. magnus (Mchedlishvili in Samoilovich & 

Mchedlishvili 1961) n. comb.; furthermore, in A. 

alaskensis, the lengths of the nexinal costae on the equatorial projections and the body are different than in A. 

unicus and A. magnus. A. alaskensis has longer equatorial projections and more distinct nexinal costae than in 

Projectoporites spinulosus Mchedlishvili in Samoilovich 

& Mchedlishvili 1961. 

Distribution.-Found only in the upper part of the 

upper Maastrichtian (subzone 5 of the Wodehouseia 

spinata Assemblage Zone) of the Colville River area. 

Aquilapollenites unicus (Chlonova 1957) Chlonova 1961 (taxon 

117) 

Plate 7, figure 4 

Discussion.-Aquilapollenites unicus is very similar 

to Aquilapollenites magnus (Mchedlishvili) n. comb. 

(basionym: Projectoporites magnus Mchedlishvili in 

Samoilovich & Mchedlishvili, 1961, p. 227, pl. 74, figs. 

1a-e). The two species are somewhat difficult to compare 

because the original description of A. unicus by Chlonova 

(1957) was based on a partial misunderstanding of its morphology and because only two specimens of A. magnus 

were found by Mchedlishvili. However, the main differences between the two species seem to be that A. unicus has 

a thicker exine and has endexinal costae that extend far out 

onto the equatorial projections, whereas A. magnus has a 

thinner exine and shorter endexinal costae. 

The A. unicus-A. magnus complex has been found 

in Maastrichtian rocks in east-central and coastal Yukon 

Territory (Rouse and Srivastava, 1972; Kalgutkar and 

Sweet, 1988; Nichols and Sweet, in press), in various 

parts of the Northwest Territories (Mcintyre, 1974; 

Doerenkamp and others, 1976; Wilson, 1978; Sweet and 

others, 1989; Nichols and Sweet, in press), and on the 

North Slope of Alaska (Frederiksen and others, 1988, pl. 

2, fig. 10; this paper, fig. 2). This pollen complex was 

also found in Paleocene rocks in west-central Northwest 

Territories (Wilson, 1978) and on the North Slope of 

Alaska (Frederiksen and others, 1988), and a similar species, Aquilapollenites sp. of Staplin and others (1976, pl. 

2, fig. 25), was found in the lower Tertiary of the 

Mackenzie Delta region and the Canadian Arctic Islands 

(Staplin· and others, 1976; Head, 1986). In Siberia, A. 

Pollen Zonation and Correlation of Maastrichtian Marine Beds, North Slope, Alaska E19 
unicus ranges to the top of the Cretaceous and, as rare 

specimens, into the Danian (Chlonova, 1980, fig. 8). 

Frederiksen and others (1988, fig. 4) considered Paleocene specimens of the A. unicus-A. mag nus complex to be 

reworked, but the true range top of this species complex 

may be in the Paleocene because this complex may be 

ancestral to the genus Novemprojectus in the PaleoceneEocene boundary interval of northern Alaska (Ager and 

others, 1986) and in the Eocene of the Canadian Arctic 

(Choi, 1984). Therefore, the true range top of the A. unicusA. magnus complex is somewhat uncertain. 

Aquilap~llenites sp. cf. A. augustus Srivastava 1969 (taxon 1 OS) 

Plate 7, figures 5-10 

Description.-Tricolpate, isopolar to subisopolar 

pollen grains with three equatorial projections; polar areas of body much larger than equatorial projections. 

Polar axis 38-56 JJ.m; equatorial axis including projections 38-68 JJ.m (10 measured specimens). Width of 

body (between bases of projections) 16-48 JJ.m; width of 

equatorial projections at their midpoint 10-17 JJ.m. In 

subisopolar specimens, one pole is longer, broader, and 

(or) more broadly rounded than the other. Poles of body 

and tips of equatorial projections broadly rounded; attachment areas of equatorial projections to body distinctly concave. Colpi obscure; in specimens lying in oblique view, no colpi are seen on the body. Thus, the 

colpi apparently are confined to the equatorial projections. Exine about 1-1.5 J.U1l thick in most areas, 0.5 Jlm . 

thick at tips of projections. Nexinal costae as thick as 

3.5 Jlm, extending about YrX the length of the equatorial projections and extending a moderate distance onto 

body of grain. Sexine tectate; columellae distinct. Sexine 

distinctly punctate, with somewhat scattered small 

spines. The spines cover most or all of the body as well 

as the tips of the equatorial projections. 

Remarks.-This species is composed of a somewhat 

heterogeneous group of specimens that are intermediate 

between Aquilapollenites augustus Srivastava 1969 and A. 

unicus (Chlonova 1957) Chlonova 1961. The body is 

broadly rounded at the poles as in A. augustus and not as 

rectangular as in A. unicus. The equatorial projections are 

broader than in A. unicus, and they are smaller than in A. 

augustus. The equatorial axis including projections is usually slightly greater than the polar axis. 

Distribution.-Lower Maastrichtian of the Colville 

River area. 

Aquilapollenites sp. A (taxon 119) 

Plate 4, figures 2-5 

Description.-Tricolpate, isopolar pollen grains with 

three rudimentary equatorial projections. Polar axis 30-35 

J.Ull; equatorial axis including projections 21-24 J.U1l (7 

measured specimens). In equatorial view, poles moderately 

E20 Evolution of Sedimentary Basins-North Slope Basin 

to broadly rounded; equatorial projections conical in 

shape; attachment areas of equatorial projections to body 

gently concave. Colpi extend nearly full length of grain. 

Exine about 1 J.U1l thick in most areas, thinning in some 

specimens to 0.5 J.U1l at tips of projections. Nexinal costae 

only on body, thickest in attachment area (3-5 J.U1l thick) 

and about 10 m long, thinning toward poles. Sexine 

tectate; columellae distinct at high power. Design of sexine 

distinctly punctate. 

Remarks.-This species is characterized by its very 

small equatorial projections. 

Distribution.-Found only in sample R3824, U.S. 

Geological Survey seismic line 31-81, shotpoint 120, 

upper Maastrichtian (subzone 4 of the Wodehouseia 

spinata Assemblage Zone). 

Fibulapollis inaequalis n. sp. (taxon 123) 

Plate 4, figures 7-12; plate 5, figures 1-3 

Holotype.-Slide R4140G(2), coordinates 65.5x110.6; 

pl. 4, figs. 7, 8; nonmarine beds within the interval of the 

Ocean Point marine beds near Ocean Point, "middle" 

Maastrichtian. 

Description.-Tricolpate, heteropolar pollen grains 

with three equatorial projections. Polar axis 19-32 J.Ull; 

equatorial axis including projections 21-42 JJ.m (14 

measured specimens). Dimensions of holotype: polar 

axis 32 JJ.m; equatorial axis 35 J.Ull. In equatorial view: 

One polar projection considerably larger than the other; 

equatorial projections longer but narrower than major 

polar projection. Polar projections very broadly rounded; 

tips of equatorial projections moderately rounded; attachment areas of equatorial projections to body generally only slightly concave. Colpi extend from tips of 

equatorial projections probably only to the bases, or not 

quite to the bases, of these projections. Exine 0.8-1 JJ.m 

thick in most areas, slightly thinner at tips of equatorial 

projections. Nexinal costae only slightly bow shaped (as 

seen in equatorial view), 1.5-3.5 Jlffi thick and 5-11 JJ.m 

long. Sexine tectate; columellae indistinct to fairly distinct at high power. Entire sexine distinctly punctate and 

rather finely conate. 

Remarks.-This species is characterized by being 

distinctly heteropolar (inaequalis, Latin for "unequal, 

different," referring to the poles). The species is similar 

to Manicorpus sp. of Kalishevich and others (1981, pl. 

29, fig. 2). Previously described species of Fibulapollis 

are isopolar to sub(?)isopolar. Fibulapollis scabratus 

Tschudy 1969 has straighter sides and more narrowly 

rounded poles. Aquilapollenites minutus Srivastava 1966 

of Bihl (1970, pl. 3, fig. 7) has slightly concave sides 

but is isopolar. Aquilapollenites aptus Srivastava 1969 is 

similar to Fibulapollis inaequalis, but A. aptus has a 

more prominently developed minor pole; Srivastava described the species as being subisopolar. 
Distribution.-Base of the Maastrichtian to "middle" 

Maastrichtian (to subzone 1 of the Wodehouseia spinata 

Assemblage Zone) of the Colville River area. 

Manicorpus pseudosenonicus n. sp. (taxon 131) 

Plate 5, figures 11-15; plate 6, figures 1-3 

Manicorpus trapeziforme Mchedlishvili in Samoilovich & 

Mchedlishvili 1~61 of Mcintyre, 1974, pl. 20, figs. S-6. 

Holotype.-Slide R3824(1), coordinates 27.7x110.1; 

pl. 5, figs. 11-12; sample from U.S. Geological Survey 

seismic line 31-81, shotpoint 120, west of Colville ~iver, 

upper Maastrichtian. 

Description.-Tricolpate, heteropolar pollen grains 

with three equatorial projections; a major pole is well developed, but a minor pole is very small or typically lacking altogether. Polar axis 18-47 JJ.m; equatorial axis 

including projections 35--64 J.1.ffi (13 measured specimens). 

Dimensions of holotype: polar axis 21 JJ.ffi; equatorial axis 

37 Jlffi. In equatorial view: pole and tips of equatorial projections broadly to somewhat narrowly rounded; attachment areas of equatorial projections to body distinctly 

concave. In polar view: shape triangular, sides gently concave, comers narrowly rounded. Colpi extend from tips of 

equatorial projections probably only to the bases of these 

projections. Exine about 1.5-2 J.1.ffi thick at the pole, consisting mostly of endosexine; sexine thickens slightly toward attachment areas, then thins to 0.5-1 J.1.ffi thick at tips 

of equatorial projections. Nexinal costae (in specimens 

where present) bow shaped (as seen in equatorial view), as 

much as 4.5 J.1.ffi thick and 15 J.1.ffi long, extending equally 

as far on the body as on the equatorial projections. Sexine 

tectate. Body distinctly and finely reticulate; however, the 

polar region is typically more finely reticulate than elsewhere and may be punctate to nearly psilate. Equatorial 

projections punctate and finely but distinctly conate. Equatorial projections may be pendent or nearly perpendicular 

to polar axis. 

Remarks.-This species has conate equatorial projections like Manicorpus delicatus (Stanley 1961) Bondarenko 

1968, but M. delicatus has a distinctly ornamented pole. 

Manicorpus pseudosenonicus has a polar area of thinner 

exine and finer reticulation like M. senonicus Mchedlishvili 

in Samoilovich & Mchedlishvili 1961 and Manicorpus 

trapeziforme Mchedlishvili in Samoilovich & Mchedlishvili 

1961, but M. senonicus and M. trapeziforme have reticulate 

rather than conate equatorial projections. Manicorpus 

trapeziforme Mchedlishvili in Samoilovich & Mchedlishvili 

i961 of Doerenkamp and others (1976, pl. 3, fig. 2) may 

also belong to Manicorpus pseudosenonicus. 

Distribution.-Lower Maastrichtian to upper 

Maastrichtian (to subzone 5 of the Wodehouseia spinata 

Assemblage Zone) of the Colville River area; also found 

in the Mackenzie Delta region of northwestern Canada (as 

Manicorpus trapeziforme: Mcintyre, 1974). 

SAMPLE LOCALITY REGISTER 

Quadrangle locations given only for samples not 

shown in figure 1. Relative positions of R3413 and 

R3152 series of samples, from sections 21/22 and 25, 

respectively, of Phillips (1988), were provided by E.M. 

Brouwers (written common., 1990). Sample designations 

followed by (P) are included in the list only because 

photomicrographs of specimens from these samples are 

included in the plates. 

Sample Locality 

16408-4(P) Sec. 25, T. 5 N., R. 2 E., Umiat (D-3) 

quadrangle 

16410-3(P) Sec. 26/27, T. 8 N., R. 2 E., Harrison 

Bay A-3 quadrangle 

20738(P) Smiley (1969) sample 52, Umiat (B-3) 

quadrangle 

ARCO 97 ARCO line 1, shotpoint 97, sec. 29, T. 8 

N., R. 5 E. (Wiggins, 1976) 

ARCO 98 ARCO line 1, shotpoint 98, sec. 20, T. 8 

N., R. 5 E. (Wiggins, 1976) 

ARCO 266 ARCO line 2, shotpoint 266, sec. 9, T. 6 

N., R. 5 E. (Wiggins, 1976) 

D3124A(P) Lat 69° 40' N., long 151° 25' W., T. 4 

N., R. 2 E., Umiat (C-3) quadrangle 

(Tschudy, 1969) 

D4036--80A(P) U.S. Geological Survey Sentinel Hill 

core test 1, depth of sample 899-909 

ft; lat 69° 36' 57" N., long 151° 27' 

11" W ., Umiat (C-3) quadrangle 

(Robinson and Collins, 1959) 

R3152A Field no. 83EB130, section 25 of Phillips 

(1988), about 7.2 m below iron-stained 

bed 

R3152B Field no. 83EB133, section 25 of Phillips 

(1988), about 3.7 m below iron-stained 

bed 

R3152C Field no. 83EB 136, section 25 of Phillips 

(1988), from the iron-stained bed 

R3317 A(P) Field no. 84-T A-AUG 5 stop 1 sample 

A, near section 4 of Phillips (1988), 

1.2 m below base of freshwater limestone bed, Harrison Bay (A-3) 

quadrangle 

R3328 Field no. 84-TA-JUL 29/4/1, C S~ N~ 

sec. 6, T. 8 N., R. 4 E. 

R3413E Field no. 84EB29, section 21/22 of 

Phillips (1988), at about the same level 

as sample 87LP 15, 20 of section 21 

R3413G Field no. 84EB31, section 21/22 of Phillips 

(1988), about 0.46 m above sample 

R3413E 

Pollen Zonation and Correlation of Maastrichtian Marine Beds, North Slope, Alaska E21 
R34130 

R3413Q 

R3694A(P) 

R3695B(P) 

R3768 

R3924 

R3769 

R3770 

R3772 

R3786 

R3787 

R3789 

R3791 

R3792 

R3818 

R3819 

R3820 

R3821 

R3823 

R3824 

R3825 

R3826 

R3827 

R3828 

R3834 

R3835 

R3837 

R3838 

R3885 

R3889 

R3890 

R3891 

R3892 

R3946P(P) 

R3946Q(P) 

R3947D(P) 

R3947J(P) 

R4140A 

Field no. 84EB39, section 21/22 of 

Phillips (1988), at a level just above 

sample 87LP 47, 48,49 of section 22 

Field no. 84EB41, section 21/22 of 

Phillips (1988), about 1.8 m above 

sample R34130 and slightly higher 

than the top of section 22 (Phillips, 

1988) 

Field no. 84SH-III-10, NE~ NE~ SW/. 

sec. 22, T. 1 N., R. 2 E., Umiat (B-3) 

quadrangle 

Field no. 84PC-I-10, C SE~ sec. 6, T. 3 

N., R. 3 E., Umiat (C-3) quadrangle 

USGS seismic line 41-81, shotpoint 185 

USGS seismic line 41-81, shotpoint 193 

USGS seismic line 41-81, shotpoint 210 

USGS seismic line 41-81, shotpoint 214 

USGS seismic line 41-81, shotpoint 221 

USGS seismic line 16-81, shotpoint 282 

USGS seismic line 16-81, shotpoint 287 

USGS seismic line 16-81, shotpoint 305 

USGS seismic line 16-81, shotpoint 337 

USGS seismic line 16-81, shotpoint 350 

USGS seismic line 31-81, shotpoint 100 

USGS seismic line 31-81, shotpoint 101 

USGS seismic line 31-81, shotpoint 102 

USGS seismic line 31-81, shotpoint 104 

USGS seismic line 31-81, shotpoint 117 

USGS seismic line 31-81, shotpoint 120 

USGS seismic line 31-81, shotpoint 126 

USGS seismic line 31-81, shotpoint 128 

USGS seismic line 31-81, shotpoint 130 

USGS seismic line 31-81, shotpoint 132 

USGS seismic line 31-81, shotpoint 142 

USGS seismic line 31-81, shotpoint 144 

USGS seismic line 31-81, shotpoint 146 

USGS seismic line 31-81, shotpoint 148 

USGS seismic line 16-81, shotpoint 310 

USGS seismic line 16-81, shotpoint 317 

USGS seismic line 16-81, shotpoint 345 

USGS seismic line 16-81, shotpoint 369 

USGS seismic line 16-81, shotpoint 375 

Field no. 86EB 16, section 7 of Phillips 

(1988), Harrison Bay (A-3) quadrangle 

Same locality as above, field no. 86EB 17 

Field no. 86EB 167, section 1 of 

Phillips (1988), Harrison Bay (A-3) 

quadrangle 

Field no. 86EB 173, same locality as 

R3947D 

Field no. 86EB 73, section 24 of Phillips 

(1988), nonmarine strata within the sequence of the Ocean Point marine 

beds 

E22 Evolution of Sedimentary Basins-North Slope Basin 

R4140B 

R4140C 

R4140D 

R4140F 

R4140G 

R4295B(P) 

R4295E 

R4295F 

R4295G 

R4295H 

Field no. 86EB121, same locality as 

R4140A 

Field no. 86EB 72, same locality as 

R4140A 

Field no. 86EB 122, same locality as 

R4140A 

Field no. 86EB 124, same locality as 

R4140A 

Field no. 86EB 125, same locality as 

R4140A 

Field no. 86EB65, section 10 of Phillips 

(1988), Harrison Bay (A-3) quadnmgle 

Field no. 86EB93, section 15 of Phillips 

(1988) 

Field no. 86EB 103, section 17 of Phillips 

(1988) 

Field no. 86EB99, section 17 of Phillips 

(1988) 

Field no. 86EB114, section 20 of Phillips 

(1988) 

REFERENCES CITED 

Ager, T.A., Edwards, L.E., and Oftedahl, 0., 1986, Eocene palynomorphs from the Franklin Bluffs, Arctic Slope, northeast 

Alaska [abs.]: Palynology, v. 10, p. 243. 

Bihl, G., 1970, New evidence on the age of the Sheerness badlands, east-central Alberta: Bulletin of Canadian Petroleum 

Geology, v. 18, p. 216-226. 

---1973, Palynostratigraphic investigation of upper 

Maastrichtian and Paleocene strata near Tate Lake, N.W.T.: 

Vancouver, B.C., University of British Columbia, unpub. 

Ph.D. dissertation, 51 p. 

Brosge, W.P., and Whittington, C.L., 1966, Geology of the 

Umiat-Maybe Creek region, Alaska: U.S. Geological Survey Professional Paper 303-H, p. 501-638. 

Brouwers, E.M., 1988, Late Maastrichtian and Danian faunas 

from northern Alaska: Reconstructions of environment and 

biogeography [abs.]: Geological Society of America Abstracts with Programs, v. 20, p. A371. 

Brouwers, E.M., Clemens, W.A., Spicer, R.A., Ager, T.A., 

Carter, L.D., and Sliter, W.V., 1987, Dinosaurs on the 

North Slope, Alaska: High latitude, latest Cretaceous environments: Science, v. 237, p. 1608-1610. 

Carter, L.D., and Galloway, J.P., 1985, Engineering-geologic 

maps of northern Alaska, Harrison Bay quadrangle: U.S. 

Geological Survey Open-File Report 85-256, 47 p. 

Chlonova, A.F., 1957, 0 vydelenii rukovodiashchikh vidov pri 

opredelenii vozrasta otlozhenii po sporovo-pyl'tsevomy 

analizu [On differentiation of the leading species for determination of the age of strata by spore-pollen analysis]: 

Novosibirsk, Akademiia Nauk SSSR, lzvestiia Vostochnykh 

Filialov Akademii Nauk SSSR, no. 2, p. 43-46. 

--1966, Novye vidy pyl 'tsy morfologicheskogo tipa 

"o·culata" [New species of the morphological type 

"oculata"], in Palinologiia Sibiri, k II Mezhdunarodnoi 
Palinologicheskoi Konferentsii (Utrekht, Niderlandy, 

1966) [Palynology of Siberia, for the 2nd International 

Conference on Palynology (Utrecht, Netherlands, 1966)]: 

Akademiia Nauk SSSR, Sibirskoe Otdelenie, p. 66-69. 

---1980, Floristicheskie provintsii Mela SSSR i 

prilegaiushchikh raionov vostochnoi Azii po palinologicheskim dannym [Cretaceous floristic provinces of the 

USSR and adjacent regions of eastern Asia according to 

palynological data], in Paleopalinologiia Sibiri: Stat'i 

sovetskikh palinologov k V Mezhdunarodnoi palinologicheskoi konferentsii (Kembridzh, Angliia, 1980) 

[Paleopalynology of Siberia: Articles of Soviet palynologists for the 5th International Palynological Conference 

(Cambridge, England, 1980)]: Moscow, Izdatel'stvo 

"N auka," p. 39--64. 

Choi, D.K., 1983, Paleopalynology of the Upper CretaceousPaleogene Eureka Sound Formation of Ellesmere and Axel 

Heiberg Islands, Canadian Arctic Archipelago: University 

Park:, Pa., Pennsylvania State University, unpub. Ph.D. dissertation, 580 p. 

---1984, A new Eocene triprojectate pollen genus from the 

Canadian Arctic, Novemprojeclus: Review of Palaeobotany 

and Palynology, v. 43, p. 337-341. 

Doerenkamp, A., Jardine, S., and Moreau, P., 1976, Cretaceous 

and Tertiary palynomorph assemblages from Banks Island 

and adjacent areas (N.W.T.): Bulletin of Canadian Petroleum Geology, v. 24, p. 372-417. 

Edwards, L.E., 1984, Insights on why graphic correlation 

(Shaw's method) works: Journal of Geology, v. 92, no. 5, 

p. 583-597. 

Frederiksen, N.O., 1986, Reconnaissance biostratigraphy of the 

Expressipollis and Oculata pollen groups in Campanian and 

Maastrichtian rocks of the North Slope, Alaska [abs.]: Palynology, v. 11, p. 227-228. 

---1989, Changes in floral diversities, floral turnover rates, 

and climates in Campanian and Maastrichtian time, North 

Slope of Alaska: Cretaceous Research, v. 10, p. 249-266. 

Frederiksen, N.O., Ager, T.A., and Edwards, L.E., 1986, Comment on "Early Tertiary marine fossils from northern 

Alaska: Implications for Arctic Ocean paleogeography and 

faunal evolution": Geology, v. 14, p. 802-803. 

---1988, Palynology of Maastrichtian and Paleocene rocks, 

lower Colville River region, North Slope of Alaska: Canadian Journal of Earth Sciences, v. 25, p. 512-527. 

Frederiksen, N.O., Ager, T.A., Oftedahl, O.G., and Edwards, 

L.E., 1985, Palynological samples near the Cretaceous{fertiary boundary, North Slope of Alaska [abs.]: Society of 

Economic Paleontologists and Mineralogists, Annual Midyear Meeting, Abstracts, v. 2, p. 31. 

Frederiksen, N.O., and Schindler, K.S., 1987, Campanian to 

Maastrichtian pollen biostratigraphy and floral turnover 

rates, Colville River region, North Slope, Alaska [abs.]: 

American Association of Petroleum Geologists Bulletin, 

v. 71, p. 558. 

Haq, B.U., Hardenbol, J., and Vail, P.R., 1987, Chronology of 

fluctuating sea levels since the Triassic: Science, v. 235, 

p. 1156-1167. 

Head, M.J., 1986, Latest Cretaceous-Paleogene palynology of 

Ellesmere and Axel Heiberg Islands, East Canadian Arctic 

[abs.]: Geological Association of Canada, Mineralogical 

Association of Canada, and Canadian Geophysical Union, 

Joint Annual Meeting, Program with Abstracts, v. 11, 

p. 79. 

Jerzykiewicz, T., and Sweet, A.R., 1986, The CretaceousTertiary bolDl.dary in the central Alberta Foothills. I: Stratigraphy: Canadian Journal of Earth Sciences, v. 23, 

p. 1356-1374. 

Kalgutkar, R.M., and Sweet, A.R., 1988, Morphology, taxonomy 

and phylogeny of the fossil fungal genus Pesavis from 

northwestern Canada: Geological Survey of Canada, Bulletin 379, p. 117-133. 

Kalishevich, T.G., Zaklinskaya, E.D., and Serova, M.la., 1981, 

Razvitie organicheskogo mira tikxookeanskogo poyasa na 

rubejhe mezozoia i kainozoia [Development of the organic 

world of the Pacific Ring at the Mesozoic-Cenozoic boundary]: Moscow, lzdatel' stvo "N auka", 149 p. 

Lerbekmo, J.F., Sweet, A.R., and St. Louis, R.M., 1987, The 

relationship between the iridium anomaly and palynological 

floral events at three Cretaceous-Tertiary boundary localities in western Canada: Geological Society of America Bulletin, v. 99, p. 325-330. 

Macbeth, J.l., and Schmidt, R.A.M., 1973, Upper Cretaceous 

foraminifera from Ocean Point, northern Alaska: Journal of 

Paleontology, v. 47, p. 1047-1061. 

Marincovich, L., Jr., Brouwers, E.M., and Carter, L.D., 1985, 

Early Tertiary marine fossils from northern Alaska: lmpli-· 

cations for Arctic Ocean paleogeography and faunal evolution: Geology, v. 13, p. 770-773. 

---1986, Reply lo the comment by Frederiksen, Ager, and 

Edwards on "Early Tertiary marine fossils from northern 

Alaska: Implications for Arctic Ocean paleogeography and 

faunal evolution": Geology, v. 14, p. 803-804. 

Marincovich, L., Jr., Brouwers, E.M., and Hopkins, D.M., 1983, 

Paleogeographic affinities and endemism of Cretaceous and 

Paleocene marine faunas in the Arctic [abs.], in U.S. Geological Survey Polar Research Symposium-Abstracts with 

Program: U.S. Geological Survey Circular 911, p. 45-46. 

McDougall, K., 1987, Maestrichtian benthic foraminifers from 

Ocean Point, Alaska: Journal of Foraminiferal Research, 

v. 17, p. 344-366. 

Mcintyre, D.J., 1974, Palynology of an Upper Cretaceous section, Horton River, District of Mackenzie, N.W.T.: Geological Survey of Canada Paper 74-14, 57 p. 

Miller, F.X., 1977, The graphic correlation method in biostratigraphy, in Kauffman, E.G., and Hazel, J.E., eds., Concepts 

and methods of biostratigraphy: Stroudsburg, Pa., Dowden, 

Hutchinson and Ross, p. 165-186. 

Nichols, D.J., Jacobson, S.R., and Tschudy, R.H., 1982, 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, Rocky Mountain Association of Geologists, v. 2, 

p. 721-733. 

Nichols, D.J., and Sweet, A.R., in press, Biostratigraphy of 

Upper Cretaceous nonmarine palynofloras in a north-south 

transect of the Western Interior Basin, in Evolution of the 

Western Interior Basin: Geological Association of Canada 

Special Paper. 

Pollen Zonation and Correlation of Maastrichtian Marine Beds, North Slope, Alaska E23 
Phillips, R.L., 1988, Measured sections, paleoenvironments, and 

sample locations near Ocean Point, Alaska: U.S. Geological 

Survey Open-File Report 88-40, 1 sheet. 

Robinson, F.M., and Collins, F.R., 1959, Core test, Sentinel Hill 

area and test well, Fish Creek area, Alaska: U.S. Geological 

Survey Professional Paper 305-1, p. 485-521. 

Rouse, G.E., and Srivastava, S.K., 1972, Palynological zonation 

of Cretaceous and Early Tertiary rocks of the Bonnet Plume 

Formation, northeastern Yukon, Canada: Canadian Journal 

of Earth Sciences, v. 9, p. 1163-1179. 

Samoilovich, S.R., 1965, Pyl'tsa novykh vidov verkhnemelovykh 

pokrytosemennykh rastenii lakytii [Pollen of new species of 

Upper Cretaceous angiosperm plants of Yakutia], in 

Paleofitologicheskii Sbomik [Paleophytological Collection]: 

Vsesoiuznyi Heftianoi Nauchno-Issledovatel'skii Geologorazvedochnyi Institut (VNIGRI), Trudy, v. 239, p. 121-

141. 

Samoiloyich, S.R., and Mchedlishvili, N.D., eds., 1961, Pyl'tsa i 

spory zapadnoi Sibiri, Iura-Paleotsen [Pollen and spores of 

western Siberia, Jurassic-Paleocene]: Vsesoiuznyi Heftianoi 

Nauchno-lssledovatel' skii Geologorazvedochnyi Institut 

(VNIGRI), Trudy, v. 177, 657 p. 

Shaw, A.B., 1964, Time in stratigraphy: New York, McGrawHill, 365 p. 

Smiley, C.J., 1969, Cretaceous floras of the Chandler-Colville 

region, Alaska-stratigraphy and preliminary floristics: 

American Association of Petroleum Geologists Bulletin, 

v. 53, p. 482-502. 

Smith, A.G., Hurley, A.M., and Briden, J.C., 1981, Phanerozoic 

paleocontinental world maps: Cambridge, Cambridge University Press, 102 p. 

Srivastava, S.K., 1970, Pollen biostratigraphy and paleoecology 

of the Edmonton Formation (Maastrichtian), Alberta, 

Canada: Palaeogeography, Palaeoclimatology, Palaeoecology, v. 7, p. 221-276. 

Staplin, F.L., ed., 1976, Tertiary biostratigraphy, Mackenzie 

Delta region, Canada: Bulletin of Canadian Petroleum Geology, v. 24, p. 117-136. 

Sweet, A.R., 1978, Palynology of the lower part, type section, 

Tent Island Formation, Yukon Territory, in Current Research, Part B: Geological Survey of Canada Paper 78-1B, 

p. 31-37. 

E24 Evolution of Sedimentary Basins-North Slope Basin 

---1988, A regional perspective on the palynoflora} response to K-T boundary event(s) with emphasis on variations imposed by the effects of sedimentary facies and 

latitude [abs.), in Global catastrophes in Earth history: An 

interdisciplinary conference on impacts, volcanism, and 

mass mortality, Snowbird, Utah, October 20-23, 1988, 

Abstracts: Houston, Lunar and Planetary Institute Contribution 673, p. 190-191. 

Sweet, A.R., and Braman, D.R., 1988, Floral changes within 

the interval containing the Cretaceous-Tertiary boundary 

in western Canada: A stratigraphic, palaeogeographic and 

palaeoenvironmental perspective [abs.]: 7th International 

Palynological Congress, Brisbane, Australia, Abstracts, 

p. 161. 

Sweet, A.R., Ricketts, B.D., Cameron, A.R., and Norris, O.K., 

1989, An integrated analysis of the Brackett coal basin, 

Northwest Territories, in Current Research, Part G: Geological Survey of Canada Paper 89-1G, p. 85-99. 

Tetra Tech, Inc., 1982, Petroleum exploration of NPRA, 1974-

1981, final report: Houston, Tetra Tech, Inc., I, II, ill, Report 8200, 183 p. 

Tschudy, B.D., 1969, Species of Aquilapollenites and Fibulapollis from two Upper Cretaceous localities in Alaska: 

U.S. Geological Survey Professional Paper 643-A, p. AlA17. 

Werner, M.R., 1987, Tertiary and Upper Cretaceous heavy-oil 

sands, Kuparuk River Unit area, Alaskan North Slope, in 

Meyer, R.F., ed., Exploration for heavy crude oil and 

natural bitumen: American Association of Petroleum Geologists Studies in Geology, no. 23, p. 537-547. 

Wiggins, V.D., 1976, Fossil oculata pollen from Alaska: Geoscience and Man, v. 15, p. 51-76. 

---1981, Noctuipollis, a new Upper Cretaceous (Campanian) pollen genus from Arctic Alaska: Grana, v. 20, p. 37-

41. 

---1982, Expressipollis striatus n. sp. to Anacolosidites 

striatus n. sp. An Upper Cretaceous example of suggested 

pollen aperture evolution: Grana, v. 21, p. 39-49. 

Wilson, M.A., 1978, Palynology of three sections across the 

uppermost Cretaceous/Paleocene boundary in the Yukon 

Territory and District of Mackenzie, Canada: Palaeontographica, Abt. B, v. 166, p. 99-183. 
j 

PLATES 1-7 

[Contact photographs of the plates in this report are available from the U.S. Geological Survey Library, Federal Center, 

Denver, Colorado 80225] 
PLATE 1 

Porate, colpate, and colporate pollen 

[Magnification x 1,000. All specimens Maastrichtian in age. Specimens photographed with bright field illumination, 

unless otherwise noted] 

FIGURES 1, 2. Triporopollenites megagranifer (Potonie 1934) Thomson & Pflug 

1953 type. 

3, 4. Anacolosidites sp.; interference contrast 

5. Kurtzipites annulatus Norton in Norton & Hall 1969. 

6-8. Orbiculapollis globosa (Chlonova 1957) Chlonova 1961. 7, interference 

contrast. 

9-11. Kurtzipites trispissatus Anderson 1960. 10, interference contrast, 

overmacerated specimen from which nexine is missing. 

12, 13. Myrtipites scabratus Norton in Norton & Hall 1969. 

14. Betulaepollenites(?) sp. 

15. Bombacacipites sp. aff. B. sp. of Nichols and Sweet (in press, pl. 3, fig. 

13). 

16-20. Tricolpites sp. aff. T. mLJtauraensis Couper 1953. 18-20, interference 

contrast 

21-26. Rousea compta n. sp. 21-23, holotype. 22-25, interference contrast. 
U.S. GEOLOGICAL SURVEY BULLETIN 1990-E PLATE 1 

6 

21 

2 3 4 5 

7 8 9 10 

11 12 13 14 15 

16 17 18 19 20 

22 23 24 25 26 

TRIPOROPOLLENITES, ANACOLOSIDITES, KURTZIPITES, ORBICULAPOLLIS, MYRTIPITES, 

BETULAEPOLLENITES, BOMBACACIPITES, TRICOLPITES, ROUSEA 
PLATE 2 

Porate, colpate, and colporate pollen 

[Magnification x 1,000. All specimens Maastrichtian in age except those in figures 8, 9, and 12. Specimens photographed 

with bright field illumination, unless otherwise noted] 

FIGURES 1-3. Rousea compta n. sp.; interference contrast 

4, 5. Siberiapollis constrictus (Samoilovich in Samoilovich & Mchedlishvili 

1961) n. comb. 

6, 7. Proteacidites sp. 

8, 9, 12. Azonia hirsuta (Samoilovich 1965) Wiggins 1976; all three specimens 

are Campanian in age. 

10, 11. Azonia sp. cf. A. hirsuta. 

13-15. Azonia strictiparva n. sp. 13, holotype. 14, 15, interference contrast. 
U.S. GEOLOGICAL SURVEY BULLEilN 1990-E PLATE 2 

2 3 

6 

. -

4 5 

7 

8 9 

10 11 

12 13 14 15 

ROUSEA, SIBERIAPOLLIS, PROTEACIDITES, AZONIA 
PLATE 3 

Colpate pollen 

[Magnification x 1,000. All specimens Maastrichtian in age. Specimens photographed with bright field illumination, 

unless otherwise noted] 

FIGURES 1-4. Wodehouseia wigginsii n. sp. 1, 2, holotype. 2-4, interference contrast 

5-9. Aquilapollenites alaskensis n. sp. 7, 8, holotype. 8, interference contrast. 

10. Aquilapollenites conatus Norton 1965. 
U.S. GEOLOGICAL SURVEY BULLETIN 1990-E PLATE 3 

3 

2 

4 

5 6 

9 

7 8 

10 

WODEHOUSEIA, AQUILAPOLLENITES 
PLATE4 

Colpate pollen 

[Magnification x 1,000. All specimens Maastrichtian in age. Specimens photographed with bright field illumination, 

unless otherwise note] 

FIGURES 1. Aquilapollenites conatus Norton 1965. 

2-5. Aquilapollenites sp. A. 

6. Aquilapollenites quadrilobus Rouse 1957; interference contrast. 

7-12. Fibulapollis inaequalis n. sp. 7, 8, holotype. 

13-14. Bratzevaea amurensis (Bratzeva 1965) Takahashi in Takahashi & 

Shimono 1982; interference contrast. 
U.S. GEOLOGICAL SURVEY BULLETIN 1990-E PLATE 4 

2 3 4 

6 5 

7 

9 

13 

8 10 

11 12 14 

AQUILAPOLLENITES, FIBULAPOLLIS, BRATZEVAEA 
PLATE 5 

Colpate pollen 

[Magnification x 1 ,000. All specimens Maastrichtian in age. Specimens photographed with bright field illumination, 

unless otherwise noted] 

FIGURES 1-3. Fibulapollis inaequalis n. sp. 

4. Fibulapollis sp. aff. F. inaequalis. 

5, 6. Fibulapollis sp. Poles finely reticulate and conate; bOdy and equatorial 

projections punctate and conate. 6, interference contrast 

7, 8. Manicorpus notabile Mchedlishvili in Samoilovich & Mchedlishvili 

1961; interference contrast 

9, 10. Manicorpus rostratus Srivastava 1968. 

11-15. Manicorpus pseudosenonicus n. sp. 11, 12, holotype. 14, 15, interference contrast. 
U.S. GEOLOGICAL SURVEY BULLETIN 1990-E PLATE 5 

2 3 4 

,• 

5 

9 

7 8 

10 

11 12 

13 14 15 

FIBULAPOLLIS, MANICORPUS 
PLATE 6 

Colpate pollen 

[Magnification x 1,000. All specimens Maastrichtian in age. Specimens photographed with bright field illumination, 

unless otherwise noted) 

FIGURES 1-3. Manicorpus pseudosenonicus n. sp. 2, 3, interference contrast. 

4, 5. Manicorpus sp. cf. M. pseudosenonicus n. sp. 

6. Manicorpus rostratus Srivastava 1968. 

7-8. Manicorpus sp. 
U.S. GEOLOGICAL SURVEY BULLETIN 1990-E PLATE 6 

2 3 

4 5 

7 8 

6 

MANICORPUS 
PLATE 7 

Colpate pollen 

[Magnification x 1,000. All specimens Maastrichtian in age. Specimens photographed with bright field illumination, 

unless otherwise noted] 

FIGURES 1-3. Aquilapollenites immiser Sweet 1986. 

4. Aquilapollenites unicus (Chlonova 1957) Chlonova 1961. 

5-10. Aquilapollenites sp. cf. A. augustus Srivastava 1969. 6, interference 

contrast; note that in this specimen, the left equatorial projection is 

folded over the body. 
U.S. GEOLOGICAL SURVEY BULLETIN 1990-E PLATE 7 

4 

2 5 

3 6 

9 

10 

AQUILAPOLLENITES 

*U.S. GOVERNMENT PRINTING OFFICE: 1991-685-417 

l?'$1i'~@~~~~~~ 

EBlrrillu«:jjun!lll%~§ & VoltcBJI!llM§ (issued bimonthly). 

Prr~nn.mnnuB~rry !Dl~~~rrllllllftl!llm~~!onu oq EJ?lcenu~ern (issued monthly). 

r~~ll'ilrr1l~~~n~ IBl©©~~ ~rr1l@l ~®f9>©rFU~ 

IPrroq~~nonuBlll IPmJ?~rn are mainly comprehensive scientific reports of 

wide and lasting interest snd importance to professional scientists and engineers. Included me reports on the results of resource studies and of 

topographic, hydrologic, snd geologic investigations. They also include 

collections of related papers addressing different aspects of a single scientific topic. 

JBunnlle~furns contain significant data and interpretations that are of lasting scientific interest but sre generally more limited in scope or 

geographic coverage than lProfessional Papers. They include the results 

of resource studies and of geologic and topographic investigations; as well 

as collections of short papers related to a specific topic. 

W!ll~~rr-SunJ?!JllllS' IPBIJ?~rn are comprehensive reports that present significant interpretive results of hydrologic investigations of wide interest 

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

investigations in all phases of hydrology, including hydrogeology, 

avuilability of water, quality of water, and use of water. 

Cftrrcunllmrn present administrative information or important scientific 

information of wide populsr interest in a format designed for distribution 

at no cost to the public. Information is usually of short-term interest. 

WB~~err-nt~ounrrc~ linuv~rul~m~fionu§ ~~]?Orr~ are papers of an interpretive nature made available to the public outside the formal USGS publications series. Copies are reproduced on request unlike formal USGS 

publications, and they are also available for public inspection at 

depositories indicated in USGS catalogs. 

OJ?enu-IFllle ~eJ?Oil'~ include unpublished manuscript reports, maps, 

and other material that are made available for public consultation at 

depositories. They are a nonpermanent form of publication that may be 

cited in otht!r publications as sources of information. 

~S[p)~ 

Geollo~ftc QunBJd!l'Blllll~lle ~!!I]?§ are multicolor geologic maps on 

topographic bases in 7 1/2- or 15-minute quadrangle formats (scales mainly 1:24,000 or 1 :62.500) showing bedrock. surficial, or engineering geology. Maps generally include brief tex.ts; some maps include structure 

and columnar sections only. 

GeoJ?IlDS'l~ftcBlll linuve§~ftgmttfiom lWB!J?§ are on topographic or planimetric 

bases at various scales; they show results of surveys using geophysical 

techniques, such as gravity, magnetic, seismic, or radioactivity, which 

reflect subsurface structures that are of economic or geologic significance. 

Many maps include correlations with the geology. 

Mlft~enll!llnueom linuvesttfigB~ttfionus §erftes MBIJPS are on planimetric or 

topographic bases of regular and irregular areas at various s~ales; ~ey 

present a wide variety of format and subject matter. The senes also mcludes 7 1/2-minute quadrangle photogeologic maps on planimetric bases 

which show geology as interpreted from aerial photographs. Series also 

includes maps of Mars and the Moon. 

Co!lllt liilllves~ftg!ll~!onu§ lWB~J?S 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. 

onn !lll!lld G!ll§ 1Inuves~ftg!li~!OI!ll§ Cllnu~ show stratigraphic information 

for certain oil and gas fields and other areas having petroleum potential. 

M!~ennueom lFftelld §~und!~ lW!ll]?§ 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. 

IHiydroll~k liilllns~ftg!llttfiOI!ll§ A~!!IS~ are multicolored or black-andwhite maps on topographic or planirnetri"' bases presenting a wide range 

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

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

Ca~a1~rog~ 

Permanent catalogs, as well as some others, giving comprehensive listings of U.S. Geological Survey publications are available under 

the conditions indicated below from the U.S. Geological Survey, Books 

and Open-File Reports Section, Federal Center, Box 25425, Denver, 

CO 80225. (See latest Price and Availability List) 00

IPun\blllfictAl~OI!ll§ oU!lne GeollogficBJit §un!l'vey, n37~- n~6n 00 may be purchased by mail and over the counter in paperback book form and as a 

set of microfiche. 00

lPM\blllftc!ll~!mns ofr ilie GeollogkB~R Sunrrvey, ll~62- ~7000 may be purchased by mail and over the counter in paperback book form and as a 

set of microfiche. 00 IPunbll!c!lla!onus oHille lU.§. Geollogic!llll §urrvey, ~7n- n~3n" 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. 

§un)?pllellllllel!ll~ 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. 

§~!!I~~ C!lltt!llltog§, "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. 

"IP!l'!ce !lll!lld Avm~fillm\blilley ILls~ oq UJ.S. Geollogftc!lllt §llA!l'ny IPu10Hftcattfionu§,00 issued annually, is available free of charge in paperback booklet form only. 

§elt~c~~ COJ?ftes ofr !!I IlllllOilll~llnlly c!lltt!llltog 00 New Publications of the U.S. 

Geological Survey" 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. 
Frederiksen-POLLEN ZONATION AND CORRELATION OF MAASTR1Ct4TIAN MARINE BEDS, NORTH SLOPE, ALASKA-U.S. 

....