ABSTRACT

MICROFLORAL ZONATION AND CORRELATION OF SOME LOWER
TERTIARY ROCKS IN SOUTHWEST WASHINGTON AND SOME
CONCLUSIONS REGARDING THE PALEOECOLOGY OF THE FLORA

by Dennis M. Sparks

The study area is located in southwest Washington and
northwest Oregon, west of the Cascade Mountains and south
of the Olympic Mountains. It is part of a large Tertiary
geosyncline which extended from the Klamath Mountains to
'Vancouver Island. The strata included in this study
comprise a composite section 9,000 feet thick, ranging in
age from late Middle Eocene to Late Eocene or Early
Oligocene. The McIntosh and Skookumchuck Formations
represent marine and non—marine phases of the same
sedimentary cycle and are in part contemporaneous. The
Keasey Formation comprises the uppermost portion of the
composite section, representing at least part of the rock
removed by late Eocene uplift and erosion of the Skookum-
chuck Formation in part of the study area.

The two principal objectives have been to establish a
relative chronologic framework for the units described and

to elucidate the nature and distribution of the early
Tertiary flora based on the dispersed plant microfossils.

Five palynologic zones are recognized, based on the

stratigraphic range of 53 plant microfossils. Quantitative

Dennis M. Sparks
data provide additional stratigraphic subdivision of the
zones, based on relative abundance of ten selected forms.
Independence of these ten forms from control by
environmental factors is shown by the relative relationships
within the sum of the ten compared with microplankton-fungi
ratios, rock facies, and total numbers.

Correlation of the zones in an east-west cross section
shows the McIntosh Formation on-lapping the Crescent
Formation in the Willapa Hills. The Skookumchuck Formation
is shown to have been deposited during a regressive phase of
sedimentation. A north-south cross section indicates
considerable relief on the unconformity below the Lincoln
Formation in the Skookumchuck section.

One hundred twelve plant microfossils have been
identified. Included in the list of taxa with which some
of the dispersed pollen and spores may have affinities,
are some with centers of distribution in the subtropics, a
large number of temperate forms, and several cool temperate
or boreal genera. The climate was warm and humid in the
lowland, where swamp forests and wet forests were developed.
The upland was more temperate, and supported a mixed, more
mesic forest. Coniferous trees were the major constituent
of a montane element which occupied higher regions to the

east.

MICROFLORAL ZONATION AND CORRELATION
OF SOME LOWER TERTIARY ROCKS IN SOUTHWEST
WASHINGTON AND SOME CONCLUSIONS CONCERNING

THE PALEOECOLOGY OF THE FLORA

By
\

Dennis MESSparks

A THESIS

Submitted to
Michigan State University
in partial fulfillment of the requirements
for the degree of

DOCTOR OF PHILOSOPHY

Department of Geology

1967

M

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I43?

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ACKNOWLEDGMENTS

Several individuals and organizations have provided
inordinate aid and assistance to me during the various
phases of this study. Dr. Aureal T. Cross, Professor of
Geology and Botany-Plant Pathology, has served as major
professor for this dissertation. He has provided material
help in preparing the thesis, as well as providing a
stimulating atmosphere of diverse research in palynology
at Michigan State University. I am grateful to Drs. James
Trow, Jane Smith and John Cantlon for critical reading of
the manuscript. Dr. Chilton Prouty, Chairman of the
Geology Department, provided helpful critism of the thesis,
and also helped me in many other ways during my tenure at
Michigan State.

Pan American Petroleum Corporation, through their
Research Center, introduced me to the problem, and
generously supported the field work. The Geological
Society of America and the Society of the Sigma Xi provided
funds for laboratory equipment and supplies, photographic
supplies and a portion of the field work.

From September 1963 to March 1965 I was under the
tenure of a National Defense Education Act Fellowship at
Michigan State University, and I am deeply appreciative of
the opportunity to have been part of that federal program.

Finally, I wish to acknowledge the stoic patience and
spartan fortitude of my wife Shirley, whose encouragement
and material assistance has helped bring this academic

ii

effort to a successful end.
It is my sincere hope that this dissertation is worthy

of those persons who have helped in its completion.

iii

TABLE OF CONTENTS

PART PAGE
INTRODUCTION . . . . . . . . . . . . . . . . . 1
General Statement . . . . . . . . . . . . . . 1
Methods . . . . . . . . . . . . . . . . . . . 5

I. GEOLOGY . . . . . . . . . . . . . . . . . . . . 10
Introduction . . . . . . . . . . . . . . . . lO
Physiography . . . . . . . . . . . . . . . . 10
Structural Framework . . . . . . . . . . . . 12
General Features . . . . . . . . . . . . . 12
Structural History . . . . . . . . . . . . 16
Stratigraphy . . . . . . . . . . . . . . . . 19
General Statement . . . . . . . . . . . . . l9
Crescent Formation . . . . . . . . . . . . 2O

Cowlitz Formation . . . . . . . . . . . . . 22
McIntosh Formation . . . . . . . . . . . . 24
Northcraft Formation . . . . . . . . . . . 26
Skookumchuck Formation . . . . . . . . . . 26

Keasey Formation . . . . . . . . . . . . . 30

II. STRATIGRAPHIC PALYNOLOGY . . . . . . . . . . . 32
General Statement . . . . . . . . . . . . . . 32
Studied Sections . . . . . . . . . . . . . . 33
Stillwater-Olequa Creek Section . . . . . . 33

Willapa River Section . . . . . . . . . . . 34
Chehalis River Section . . . . . . . . . . 34
McIntosh Lake Section . . . . . . . . . . . 35

Rock Creek Section . . . . . . . . . . . . 35

iv

PART

III.

The Composite

Zonation

Reference Section

Qualitative Method . . . . . . . . . .

Qualitative

Results . . . . . . . . . .

Quantitative Method . . . . . . . . . .

Quantitative Results . . . . . . . . . .

Correlation
Correlation
Correlation
Correlation

Correlation

of Zones . . . . . . . . .
of McIntosh Section . .
of the Skookumchuck Section

of the Willapa River Section

of the Chehalis River Section.

Summary of Palynologic Correlations

FLORAL AND ENVIRONMENTAL SECTION

Introduction .

Composition of the Flora . . . . . . . . .

Methods . .
Flora List .

Environmental

Indicators in Flora . . . .

Tropical - Subtropical Plants . . . . .

warm Temperate Plants . . . . . . . . .

Temperate Plants . . . . . . . . . . . .

Relative Abundance Diagram . . . . . . .

Ecological Elements Within the Flora . . .

swamp Element 0 o o o o o o o o o o o 0

Wet Forest Element . . . . . . . . . . .

Mesic Forest Element . . . . . . . . . .

V

PAGE
36
38
38
40
44
49
55
59
59
60
61
62
69
69
69
69
7o
72
72
74
76
76
78
79
82

83

PART PAGE

Montane Element . . . . . . . . . . . . . 84

Areal Distribution of the Floral Elements . 85
Summary of Environmental Conditions . . . . 87

IV. SUMMARY AND CONCLUSIONS . . . . . . . . . . . 90
V. SYSTEMATIC SECTION . . . . . . . . . . . . . . 96
Nomenclature . . . . . . . . . . . . . . . 96

Location and Collection Information . . . 98

Descriptions . . . . . . . . . . . . . . . lOO

SELECTED LIST OF REFERENCES . . . . . . . . . 158

vi

LIST OF TABLES

TABLE PAGE
1. Floral List. Includes Sporophytes Inferred
From Fossil Spores or Pollen, and Plants
Identified From Leaves, wood, etc.

(From Published Sources) . . . . . . . . . . 71

vii

LIST OF FIGURES

FIGURE
1. Generalized Early Tertiary Paleogeography in
Study Area . . . . . . . . . . . . . . . . . .
2. Code Designations for Morphologic Classes and
Ornamentation Types . . . . . . . . . . . . .
3. General Geology and Structure: Southwest
Washington and Northwest Oregon . . . . . .
. Stratigraphic Correlation Chart . . . ;
Stratigraphic Range of 53 Palynomorph Species

Relative Abundance - Ten Selected Types . . .

NONU'l-Il’

Occurrence Check-list of Selected Stratigraphic
Types . . . . . . . . . . . . . . . . . . . .
8. Relative Abundance of Ten Selected Stratigraphic
Types in Correlated Sections . . . . . . . . .
9. Correlation of Zones: East-West Cross Section .
lO. Correlation of Zones: North-South Cross
Section . . . . . . . . . . . . . . . . .
11. Relative Abundance - Total Population Grouped as
Sporophyte Taxa . . . . . . . . . . . . . . .
l2. Inferred Distribution of Major Vegetational

Assemblages . . . . . . . . . . . . . . . . .

viii

PAGE

13
15
41
SO

57

58
63

66

77

86

LIST OF APPENDICES

APPENDIX PAGE

A . . . . . . . . . . . . . . . . . . . . . . . . A-l

ix

INTRODUCTION

The Tertiary rocks of western Oregon and Washington
represent a vast and little known sedimentary province. In
an area of approximately 60,000 square miles, lying west of
the Cascade Mountains and extending from the Olympic
Mountains on the north to the Klamath Mountains on the
south, about 20,000 feet of sedimentary rocks are preserved.
These rocks range in age from Middle Eocene to Pliocene.

The sequence of sediments rests conformably upon, and is
intimately related to, a series of basic volcanic rocks of
Early to Middle Eocene age, with a thickness in excess of
10,000 feet. The inferred paleogeography in Eocene time is
shown in Figure 1.

To describe the area as a basin is a misleading over—
simplification. The western limits have not been established,
and rocks extend onto the continental shelf, and even beyond
to the continental rise. To most geologists the area repre-
sents a geosyncline, but within the broad context of that
concept it is a special case, requiring, like most geosyn-
clines, a complete and unique definition. That kind of
definition and understanding has not as yet been realized,
nor is it the purpose of this paper to attempt it. Rather,
this project focuses on a very small part of the geographic
and stratigraphic extent of this Tertiary geosyncline, in
an attempt to establish a chronologic framework for the
lower Tertiary sedimentary rocks of southwest Washington

and part of northwest Oregon.

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To this end, the dispersed spores and pollen of plants
growing on the land adjacent to the area of accumulating
sediments are utilized in a biostratigraphic fashion.
Several characteristics of plant microfossils uniquely
qualify these entities for biostratigraphic application;
(1) they are nearly ubiquitous in their occurrence in most
types of sedimentary environments; (2) they are remarkably
resistant to most degradational processes in sedimentation
and diagenesis; (3) they possess characteristic morpho-
logical features which allow differentiation and recogni-
tion; and (4) they reflect time related changes in their
qualitative and quantitative distribution in the strati-
graphic column caused by evolutionary and/or environmental
conditions.

In the process of analyzing dispersed plant microfos—
sils in a stratigraphic section, two kinds of results may
be obtained. First the data show qualitative and quanti-
tative characteristics which provide time-stratigraphic
information. Second, these same data comprise a fossil
record of the plants which grew in the area, from which
compositional, distributional, and ecological information
may be obtained. These two kinds of information are
closely and genetically related, although conclusions
about one may be made without reference to the other,
sometimes, however, with less than satisfactory results.
This study approaches both aspects in the hope that a

working hypothesis regarding the ecological conditions of

Ll

4
the early Tertiary vegetation will facilitate the construc-
tion of a time-stratigraphic framework, as well as being of
significant interest in itself.

There are three principle objectives sought in the
study: first, the zonation and correlation of outcrop
sections of Middle Eocene and Upper Eocene rocks in western
Washington and northwest Oregon; second, interpretation of
the composition and general distribution of a portion of the
early Tertiary flora, and possible environmental implications;
and third, an adequate systematic treatment of the micro-
fossils to allow wider application of the information by
other workers.

The amount of published information available pertinent
to this study is not extensive. Much of the geologic work
done before 1950 in western Washington and Oregon was of a
reconnaissance nature, and the paleontologic investigations
were largely concerned with faunal assemblages described
from isolated localities. During the period from 1950 to
the present, The United States Geological Survey has been
conducting a series of studies in conjunction with the
Washington State Department of Conservation that has led to
the publication of descriptive maps and reports prepared on
a considerably more detailed scale. Frequent and repeated
reference to these publications is made in this report.

The literature of Tertiary palynology is not extensive.

Several hundred published reports are available, some of

which concern lower Tertiary rocks. Studies dealing with

5

the Tertiary section of western North America number only
about 15. A much larger number of publications is available
dealing with more conventional paleobotanical aspects
(leaves, wood, etc.) of the Tertiary section of the west
coast, and these were consulted often, although they
generally are not cited directly in the text. Current
interest in petroleum exploration in the offshore area
adjacent to the states of Washington and Oregon has led to
a rapid increase in the amount of work carried out in the
region, both stratigraphically and palynologically. The
extent of this effort and the results of it, both
economically and geologically, is, at present, competitive
information and is not available. Perhaps much of this
information will eventually be published and our under-
standing of the events of the Tertiary Period in western

North America will be greatly enhanced.

Methods

Several different methods were used in the collection
and synthesis of the data contained in this report. These
can be conviently classed as: (1) field methods; (2) lab-
oratory methods; and (3) analytical methods.

The field methods used were determined by the objec-
tives of the study. The purpose was to establish an
abstract chronologic framework for the rock column. The
sections that were selected for detailed study had, for the
most part, been previously described in detail. The samples

were collected along paced traverses, with brunton compass

6
readings of attitude to establish vertical distance between
samples. The total thickness of sections determined in this
manner agrees well with those measured more accurately and
described in the published reports. Where detailed geologic
maps were available, the samples localities were placed
directly thereon; otherwise localities were plotted on
United States Geological Survey 15’ topographic quadrangle
maps.

Laboratory preparation procedures were the same as
those used in many palynological laboratories. The
inorganic rock matrix was removed by treatment with 10%
hydrochloric acid, followed by 70% hydrofluoric acid. The
organic fraction, which was large in almost every sample,
was then treated with Schulze's solution (one part aqueous
potassium chlorate to three parts concentrated nitric acid)
for five to thirty minutes, depending on the amount of
organic detritus. This usually resulted in the oxidation
of most of the organic residue, but left the pollen and
spores, along with cuticular fragments, various lignified
plant cells, and often an assemblage of fungal and algal
cells, including dinoflagellate cysts. The oxidized organic
detritus was dissolved in a 5% potassium hydroxide solution.
The sample was then washed free of that solution, and a
stain was added (usually safranin). A glassware detergent,
Alcojet, was used to advantage on many samples to hold very
fine debris in suspension before staining, and thus

further concentrate the pollen and spores, etc. Permanent

7

slides were prepared in Clearcol with Harleco Synthetic
Resin used to cement the coverslip.

The analytical methods consisted of making a qualita-
tive collection of the dispersed spores and pollen by
morphological class, the establishment of stratigraphic
range for these classes, and a quantitative evaluation of
certain morphologic types. The classification is based
upon a scheme proposed by Tschudy (1957) in which the
morphological types are designated by descriptive formulae.
This permits the handling of large numbers of different
kinds of pollen and spores when their proper nomenclature
may not be established in the early phases of an investi-
gation. Figure 2 shows the classification used and the
formula designation for each class. Abbreviations of
certain distinctive types are occasionally used as well,
such as Al-l (Alnus-like).

The entire area of the mount under the coverslip was
scanned systematically and both the qualitative and
quantitative data were collected simultaneously. An
effort was made to control the quality of the preparations
and to obtain approximately the same number of pollen on
each slide. By extrapolation the total number of grains
per slide generally ranges from about 1000 to as high as
8500, but the average is between 2000 and 3000. The
quantitative data consists of two kinds of relative abun—
dance counts. The objective of the first was to determine

the most abundant types in the sample, some of which

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9
reflect the local environmental or ecological conditions,
and the second count was designed to provide stratigraphi-
cally significant data, independant of local conditions.
The first count was a 200 grain fixed sum count of every
pollen or spore encountered in traversing the slide until
that sum was reached. Hopefully, these data make possible
an interpretation of the distribution of plants growing in
the vicinity of the depositional site, especially as they
may be related to environments reflected in the lithologic
record, such as with the coals and lignitic siltstones.
The second kind of count was a fixed area count of ten
specific types of pollen, the sum being the total number
of the ten types present on the slide. If the assumptions
which are made regarding these ten types are valid then the
data collected by this method will yield results that are
significant to the time—stratigraphy of the area. These
quantitative methods are discussed in more detail in a
following section.

All microscopic work was carried out with Leitz
Ortholux microscope. A 35mm Leica camera mounted on the
microscope provided the photographs. Kodak Panatomic-X
and Adox KB—l4 films were used, and the prints were

enlarged to standard magnifications of 500x, lOOOx, or

1250x.

PART I: GEOLOGY
Introduction

In undertaking to establish a relative chronology
for the rocks within an area, it is imperative that the
geologic setting of the area is clearly understood by the
investigator. This is no less true in attempting to
portray the distribution and development of a flora from
the fossil record. The understanding of the geologic
setting is not necessarily intended to imply a knowledge
of the "true" geologic relationships; but rather an
awareness of the extent of objective data available and
the limitations of those data, familiarity with the various
hypotheses advanced for the historical development of the
area, and some first-hand observations of the structural
and stratigraphic relationships of the rocks in the field.
The following parapgraphs summarize the geologic setting
of the area under consideration in this study. This will
be followed in the second section by the analysis of the
time-stratigraphic distribution of the plant microfossils

within this geologic setting.
Physiography

The present day topography in western Washington and

northwest Oregon is directly related to the structure and
composition of the local bedrock. The structural highs

are the prominent topographic elevations, and the

10

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crystalline volcanic rocks exposed in the high areas hold
up sharp ridges and steep-sided canyons. The maximum
relief in the area is in the Willapa Hills which have an
elevation of about 3000 feet and the peaks stand some
1500-2000 feet above the valleys. The structurally low
areas between the prominent northwest-southeast trending
anticlinal ridges are in part occupied by the major streams
of the area, and present a low rolling topography developed
on the partly truncated folds of the lower Tertiary
sediments. The rate of chemical degradation of the largely
basic bedrock is high. Soils are frequently thick, and the
area is densely covered with vegetation. For these reasons,
the surface expression of many faults and minor folds
cannot be seen. Geomorphically, the entire area is in a
stage of early maturity, with the exception of areas where
Miocene basalts lie unconformably upon older deposits,
producing a youthfully dissected appearance. Most of the
interstream divides are sharp, and about 70 per cent of
the region is in slope. Two of the major streams of the
area, the Cowlitz River and the Chehalis River, are mature
in their lower courses, but are more youthful in their
headwater regions. The Columbia River is youthful through-
out its course, expecially where it is incised across the
structure of the Coast and Cascade Ranges. The Cowlitz
River has a wide flood plain, and shows a number of
terrace levels above the present river plain. The Chehalis

River also shows several terraces along it's lower course.

12
These probably reflect changes in base level (sea level for
these streams) during Pleistocene time, and may also
indicate the continued process of orogenic uplift in

Pleistocene and Recent time.
Structural Framework

General Features

 

The major structural features in the study area are
northwest-southeast trending uplifted areas exposing cores
of early Tertiary volcanics. Between these major high
areas and associated with them, in part, are a series of
rather poorly defined anticlines and synclines. Faults
occurring in the area are usually high angle, sometimes
reverse, and occasionally show a slip-strike component.
Bounding the area in a tectonic sense are the Cascade Ranges
to the east, the Olympic Mountains to the north, and the
east Pacific basin on the west. The major structural axes
are shown on Figure 3.

The present day Cascade Ranges are the result of
Pliocene and Pleistocene activity, although the tectonic
history of that mountain belt involves more than a single
orogenic phase. Misch (1952) describes several periods of
folding, metamorphism, and intrusion which took place in
Paleozoic, Mesozoic, and Cenozoic time. Of particular
interest to this study is the history of early Tertiary
deformation that produced an area of considerable relief

trending northwest-southeast, and located further to the

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east than the present day Cascades. The forces which
produced that uplift were probably responsible for the
structural trend seen today in the area of this study. The
presence of a highland area to the east (see Figure l), and
it's subsequent erosional history, certainly played a part
in the source and distribution of the lower Tertiary
sediments, as well as affecting the distribution of the
Eocene flora. Although the dominant source of sediments
has been a volcanic terrane, located, in part, within the
sedimentary province itself, many of the more arkosic and
quartzitic sediments were derived from the igneous and
metamorphic terrance of the early Cascade Mountains.

The Willapa Hills are developed upon a northwest-
southeast trending anticlinal high which lies near the
center of the study area (Figure 3). The axis plunges
toward the southeast, and the lower Tertiary sediments
exhibit an erosional off—lap relationship, dipping at low
angles away from the plunging crest. Crescent Formation
volcanics (see stratigraphic units, Figure 4) are exposed
in the axial portion, and have been a source of sediments
during early Tertiary time.

The Doty Uplift is an anticlinal fold trending
northwest-southeast, located about 10 miles to the north
of the Willapa Hills anticline. The lower Tertiary sedi-
ments bear a similar erosional off-lap relationship to the
Doty Uplift as they do in the Willapa Hills, although

faulting has brought Oligocene or Miocene rocks in contact

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with the Crescent volcanics in some places. The Black
Hills are located on the Doty Uplift as a topographic high.

Farther to the north, southwest of Olympia, another
unnamed anticlinal high occurs with Crescent volcanics
exposed along the axis. The sedimentary cover, if it ever
completely over-lapped the area, has been stripped off by
erosion.

The southeastward extension of these structural
features terminates where the axes plunge as the result of
the late Tertiary diastrophism in the Cascade Mountains.
Some of the major structural trends can be traced north-
west to the coast line, but their extension onto the
continental shelf is as yet unknown. Between these major
structurally-high areas, the lower Tertiary rocks are
folded in a series of smaller anticlines and synclines

almost all of which trend between N60°W and N75°W.

Structural History

 

Several periods of tectonic activity have affected
the area under consideration. The structural events prior
to Eocene time are not evident in southwestern Washington,
since the base of the Lower and Middle Eocene Crescent
volcanics is not exposed. On Vancouver Island, however,
and in the Olympic Mountains, the Crescent formation lies
unconformably upon Cretaceous and older rocks (Weaver, 1937,
1945). This relationship is not well established, however,
and all that is certain is that in Early (?) and Middle

Eocene time a great out-pouring of basic volcanics

17
occurred, covering effectively the underlying rocks from
southern Vancouver Island to the Klamath Mountains. It was
upon this basement, and associated with it in part, that
the sedimentary rocks of Middle to Late Eocene age began
to accumulate in different areas.

In early Late Eocene time, and perhaps earlier,
movements along pre-Tertiary structural trends began to
uplift portions of the crust, exposing the underlying
volcanics in northwest-southeast oriented highs. These
movements probably were continuous from Middle Eocene time,
although the first evidence of sediments derived from them
occur in early Late Eocene. The effect of these movements
was relatively minor, and usually of local extent.

Near the close of Eocene time, more significant
diastrophic events took place. Further uplift in the
Willapa Hills, Doty Uplift, and other northwest-southeast
features occurred, as well as positive movement in the
Coast Range and Olympic Mountains. Some minor folding of
the Eocene sediments also occurred near the uplifts,
allowing erosion to strip away part of the section in some
areas. Often the effects of these movements were relatively
minor. However, in some sections near the structural highs,
the marine sediments of Oligocene age lie with considerable
unconformity upon the Eocene rocks.

The major structural events that affected the area
occurred in Miocene and Pliocene time. In early Miocene,

uplift and erosion of Eocene and Oligocene rocks took place.

18
Lower and Middle Miocene marine sediments lie unconformably
upon the Eocene and Oligocene rocks. Further uplift and
extensive vulcanism in later Miocene time caused a retreat
of marine waters, and the structural pattern presently
seen was established. The Miocene deformation occurred
from compressive forces acting to fold the sedimentary rocks
into a pattern trending northwest-southeast, parallel with
the earlier trends. During Late Pliocene time, major
tectonic activity occurred in the Cascade Mountain area.
This folding and accompanying intrusion brought the Cascade
Mountain ranges to their present day configuration and
caused further movement along faults as well as more folding
within the Tertiary section of western Washington. Down-
warping occurred along the Puget-Willamette Trough, the
Grays Harbor embayment, and the lower Columbia River valley
allowing non-marine sediments to accumulate.

Tectonic activity has continued in the area through
Pleistocene time to the present as shown by movement along
several active faults, explosive volcanic activity, and
evidence of recent uplift in the Coast Range. The present
sedimentary province is displaced westward, where sediments
are accumulating on the continental shelf and slope that
are very similar to those of the Tertiary section on the
adjacent land area. The Pleistocene glaciations have
altered the pattern of structural development, certainly,
but there is no sound evidence that any of the events

initiated in early Tertiary time have yet come to an end.

l9

Stratigraphy

General Statement

 

The stratigraphic sequence of rocks considered in this
study consists of about 10,000 feet of elastic sediments
with some associated volcanics, and represents approximately
8-12 million years of time (Kulp, 1961), from Middle Eocene
to earliest Oligocene. The stratigraphic section consists

1 indicative of a wide range of

of rocks exhibiting facies
depositional environments. Sedimentary accumulations in
deep, offshore waters, shallow marine and neritic areas,
estuary and delta environments, and non-marine coastal
swamp environments are represented. The present outcrop
pattern is the result of middle and late Tertiary tectonic
events, and is shown in Figure 3. The present land surface

is densely covered with vegetation, dominated by the

coniferous forests which are so characteristic of the

 

1The term "facies" is one that has a long history of
diverse usage. Unfortunately, the many different uses,
and misuses, reduces its value in conveying the concept
for which it was originally coined. Teichert (1956)
presents an excellent review of the problem and suggests
some practical solutions. When the word "facies” is used
in this paper, it refers to the collective assemblage of
characteristics that the sedimentary rock possesses. It
includes composition, grain size, primary structures,
sorting qualities, fossil content, organic matrix, and any
other observable feature of the rock. From these facies
features the depositional environment may be interpreted.
For example, a sample of lignitic-siltstone facies is
interpreted as having been deposited in a swamp or estuarine
environment. The facies are the observable, unequivocal,
aspects of the rock; the depositional environment is the
analytical interpretation based upon them.

2O
northwest. These forests, along with the general lack of
relief in the area make it difficult to locate outcrops.
Stream beds, and railroad and highway cuts provide most of
the exposures, but these are not abundant. A description
of the rock units within the stratigraphic interval studied
follows. Figure 4 shows the relationships of the strati—

graphic units from published sources.

Crescent Formation

 

The Crescent Formation is the name given by Arnold
(1906) to the thick sequence of volcanic flows and
associated tuffaceous sediments exposed on the north side
of the Olympic Mountains at Crescent Point. Some contro-
versy regarding the nomenclature of these volcanics has
ensued, and in several reports (Weaver, 1945, and
Henrikson, 1956), the name Metchosin Formation (Clapp,
1910) has been applied to volcanic rocks occupying a
similar stratigraphic position in other areas. That some
question regarding these rocks should arise is not
surprising. The entire region, from southern Vancouver
Island to the Klamath Mountains, is underlain at the base
of the Tertiary section by a thick sequence of volcanic
rock which appears to be genetically related over the
whole region. Weaver (1944, p. 1407) describes the

distribution of the Metchosin volcanics as "one vast lava
field extending from Vancouver Island southward to the

north slope of the Klamath Mountains and eastward to the

present site of the western foothills of the Cascade

21
Mountains." He indicates that the volume of rock involved
is probably greater than that of the Miocene basalts of
the Columbia Plateau. Recent workers with the United
States Geological Survey (Brown, Gower and Snavely, 1960,
1961; Gower, 1960; Snavely, Brown, Roberts, and Rau, 1958)
use the name Crescent Formation for these rocks, and that
practice is followed in this study. The thickness of the
Crescent Formation is probably quite variable, but in the
Willapa Hills it is at least 8000 feet (Henrikson, 1956)
and near Lake Crescent, north of the Olympic Mountains, it
is in excess of 10,000 feet (Brown, Gower, and Snavely,
1960). The flows within the formation often show pillow
structure, indicating submarine extrusions, but part of
the volcanic activity was probably subaerial as well.

The Crescent Formation is exposed in numerous
localities in western Washington and Oregon. In the
Central Coast Range of Oregon, the Siletz River volcanics
were named by Snavely and Baldwin (1948) where they crop
out in many places along the crest of that anticlinal high.
These volcanics are for the most part equivalent in age
and origin to the Crescent Formation. In northwestern
Oregon, outcrops of Crescent—like volcanics were called
the Tillamook volcanic series by Warren and Norbisrath
(1946). In Washington, the Crescent Formation forms the
bedrock in most of the structurally high areas where the
sedimentary cover has been stripped away. The Willapa Hills,

the Doty Uplift, and others structurally high areas shown in

 

9:. I.

 

 

 

«\\

 

22
Figure 3, illustrate the outcrop distribution.

The age of the Crescent volcanics has been based
largely on stratigraphic position, and on a few
foraminiferal and molluscan assemblages. The fossils
indicate an Early to Middle Eocene age, at least for parts

of the Crescent Formation.

Cowlitz Formation

 

The Cowlitz Formation was named and described by
C. E. Weaver (1912). Later, Weaver (1944) designated the
type section as that exposed in the banks of Olequa Creek,
from the confluence of that stream with the Cowlitz River
north to the contact with the overlying Oligocene strata
near Winlock. Henrikson (1956), in a study of the Eocene
stratigraphy of the area, emended the type section by
including the rocks exposed in the bed of Stillwater Creek
from 3 miles west of Ryderwood to the point where they
overlap Weaver’s original section in Olequa Creek. Thus,
at the present time, the Cowlitz Formation includes about
8000 feet of rock divided into four members: (1) the
Stillwater Creek member, (2) the PeEll volcanics member,
(3) the Olequa Creek member, and (4) the Goble volcanics
member. The volcanic members are, at best, difficult to
recognize as mappable units in the field and are not
conspicuously present in the Olequa-Stillwater Creek
section. As now defined, the Cowlitz Formation is a very

thick and diverse rock unit, and not amenable to mapping

except on a very large scale. Snavely et a1., (1951)

 

23
proposed the names McIntosh, Northcraft and Skookumchuck
Formations for the sequence of rocks apparently
stratigraphically equivalent to the emended Cowlitz
Formation but 15—20 miles to the north of the Stillwater-
Olequa Creek section in the Centralia-Chehalis district.
In ascending stratigraphic order, the section consists of
marine siltstones and sandstones of the McIntosh Formation,
volcanic breccias and flows of the Northcraft Formation,
and a lignitic siltstone, sandstone and coal sequence in
the Skookumchuck Formation. With the possible exception
of the volcanic Northcraft Formation, these represent
mappable lithologic units of a scale which permit detailed
investigation and an understanding of the relationship of
depositional environments. The McIntosh Formation corres-
ponds in general to the Stillwater Creek member of
Henrikson, although it would also include marine siltstones
occurring higher in the Olequa Creek member, the non—
marine portion of which corresponds to the Skookumchuck For-
mation. The relationship of the volcanics in the two areas
is not clear, and Henrikson (1956) indicates that the
Northcraft volcanics differ petrographically from the PeEll
and Goble members of the Cowlitz Formation. There were
certainly many centers of volcanic activity in early
Tertiary time within the area considered in this study, and
lack of continuity over the area of a single, recognizable
unit is not surprising. The names McIntosh, Northcraft,

and Skookumchuck Formations are used in this study in order

 

 

 

 

find

 

.V

Pc‘g

 

 

24
to consider the marine —- non-marine phases of deposition
more easily, and to maintain consistancy with current work

of the United States Geological Survey in the area.

McIntosh Formation

 

This rock unit was named by Snavely, Rau, Hoover, and
Roberts (1951) for good exposures on the south shores of
McIntosh Lake and in cuts along State Highway 5H, 3 1/2
miles east of Tenino, Thurston County (Figure 3). A total
thickness of about 4000 feet is given for the formation in
the type area, with the base not exposed. The rocks consist
of dark gray, tuffaceous, massive to fissile, siltstone and
sandstone. The beds commonly contain calcareous concretions
and lenses. The sandstones are generally poorly sorted,
feldspathic or lithic wackes (Williams, Turner and Gilbert,
1954) with basaltic or andesitic fragments the most abundant
constituent. They appear to be immature sediments both
texturally and compositionally. Fossils of neritic
communities are not common in the type area, although
foraminiferal assemblages are abundant. East of the type
area, the sediments become generally more coarse, and
lignitic stringers are present with plant fossils preserved
in them. The rocks in the type area generally exhibit
facies that indicate deposition at a rapid rate in off-
shore, marine waters, without a great deal of high energy
sorting action. Further to the west, the lithologies

become finer grained and often exhibit fair to good

fissility. The formation occurs discontinuously throughout

 

 

.11

..L

3 .U

a-N
1. o

L.

t.

 

 

L
.4

v

 

25
the study area. In the Black Hills area, Snavely, et al.
(1958), have mapped the McIntosh Formation with extensive
interbedded basic volcanics in the lower part. Pease and
Hoover (1957) recognized two members in the McIntosh
Formation in the Doty-Minot Peak area. The lower member
in the Chehalis River valley near PeEll consists of
sandstone and siltstone, dark in color, poorly sorted, and
often showing graded bedding with interbedded basic
volcanics. These can be seen to lie directly upon or
interbedded with the Crescent Formation and are about 900
feet thick. The upper member consists of dark gray,
tuffaceous, somewhat fissile, siltstone with thin interbeds
of feldspathic sandstones. The total thickness of the
McIntosh Formation in this area is about 2500 feet.
Further to the west, in the Willapa River valley near
Raymond, less than 1000 feet of McIntosh Formation is
present (Rau 1958) and represents the upper member of Pease
and Hoover (1957). It rests directly upon Crescent
Formation volcanics without the coarse elastic and volcanic
transition beds of the lower member which are present near
PeEll.

The age of the McIntosh Formation is late Middle to
early Late Eocene. This has been established on the basis
of many well preserved foraminiferal assemblages (Snavely,
et a1., 1951 and 1958). Those authors correlate the
McIntosh foraminiferal assemblages with the upper Domengene

and lower Tejon stages of California. The McIntosh

 

ell.

\

. 1F¢

«V

26
Formation transgresses time toward the west, where the age

of these marine rocks is entirely Late Eocene.

Northcraft Formation

 

The Northcraft Formation was named by Snavely, et a1.,
(1951) from outcrops of andesitic flows and breccias
occurring in the vicinity of Northcraft Mountain, Thurston
County (Figure 3). In the type area, these volcanic rocks
are about 1000 feet thick and conformably overlie the
McIntosh Formation. The formation has not been recognized
as such west of the Chehalis River, and a source toward the
east is indicated by an increase in the thickness of the
flows in that direction. Snavely, et a1., (1958) suggest
a correlation of the Northcraft Formation with a lower part
of the Goble Series (Wilkenson, Lowry, Baldwin, 1946) in
northwestern Oregon, and it seems likely that the Goble
member of the Cowlitz Formation (Henrikson, 1956), (Goble
member of the Skookumchuck Formation of this paper),
represents the same lithologic unit.

The age of the Northcraft volcanics, as determined
largely by stratigraphic position, is early Late Eocene.
Directly overlying the Northcraft Formation, in part
unconformably, and in some cases interbedded with the
upper portion, are the non—marine rocks of the Skookumchuck

Formation.

Skookumchuck Formation

Snavely, Roberts, Hoover and Pease (1951) applied the

27
name Skookumchuck Formation to a series of non-marine
sandstones, lignitic siltstones, and coals, with some
intertongues of marine siltstone exposed along the
Skookumchuck River near Centralia, Washington. The forma-
tion has a thickness of 3500 feet in the type area, and
crops out in an irregular belt across Chehalis district,
in the lower Toutle River valley, along the Cowlitz River
and Olequa Creek, and in the PeEll-Doty area (Figure 3).
The rocks exhibit sandy, lignitic and coaly facies which
indicate deposition in a generally non—marine environment
with rapid changes between very high energy and low energy
conditions. In part the rocks probably represent a deltaic
environment, as indicated by the proximity of marine
tongues associated with cross—bedded, fairly well-sorted
channel sands and coal, indicative of swamps. Also
present are massive sandstone beds, crossbedded in part,
and lenticular in shape, which may represent channel
mouth bars, or larger offshore bars.

The sandstones, which predominate in the lower and
upper most part of the section, are bluish-gray, poor to
fairly well-sorted, feldspathic or lithic wackes, with a
fairly high percentage of volcanic rock fragments. They
are generally friable, with the grains angular to sub-
rounded, and are often carbonaceous and micaceous, which
gives the rock a well bedded appearance in some areas.
Quartz is not a dominant constituent, although it is

present in small percentages (10 - 30%). The siltstones

 

ha

 

u

1E.

V‘.

 

Y
a

.
nu

 

Nxb

u“

 
   

28
are generally feldspathic, always carbonaceous, sometimes
lignitic and they often contain brackish water molluscan
fossils. The color is dark gray to dark brown, depending
on the amount of plant detritus present. The lignitic
siltstones are often associated with coal seams which range
in thickness from one inch to several feet. The coals are
often banded, subbituminous in rank, and contain a large
amount of recognizable plant remains, including whole logs,
leaves, and roots which sometimes are seen in growth
position, penetrating the former soil layer beneath the
coal.

The non-marine phase of deposition represented by the
Skookumchuck Formation is thickest toward the east, and
thins rapidly toward the west. In the Chehalis River
valley between PeEll and Doty, the Skookumchuck Formation
is several hundred feet thick, and contains only small
amounts of coal and lignitic siltstone. Massive, bluish-
gray to greenish gray sandstone and carbonaceous, micaceous
siltstones are the most common lithologic types in that
section. Further west, in the Willapa River valley, rocks
of the Skookumchuck Formation are absent.

Where the Northcraft Formation does not separate
them, the McIntosh and Skookumchuck Formations show an
inverse relationship in thickness from east to west. In
the eastern part of the study area, deposition in the
brackish, non-marine environment of the Skookumchuck

Formation began earlier and lasted longer than in the

29
western part, the reverse is true for the McIntosh
Formation. From this it is obvious that the two formations
are in part genetically related to the same depositional
cycle, but represent different environments.

The age of the Skookumchuck Formation is given as
Late Eocene, based on limited foraminiferal and macrofaunal
evidence (Snavely, et a1., 1958). Plant fossils, which at
best have been studied only generally, indicate an Eocene,
probably Late Eocene, age (Brown, in Snavely, et a1.,
1951). The Skookumchuck Formation has been correlated with
Weaver’s original Cowlitz Formation at Olequa Creek, and in
this paper is recognized at that locality as equivalent to
part of the Olequa Creek member of Henrikson (1956).

In most of the study area, the Skookumchuck Formation
is overlain by rocks of the Lincoln Formation. The contact
is not conformable and there is some evidence that the
Skookumchuck Formation underwent a period of lithification,
slight uplift, and, in some areas, erosion before deposition
of the Lincoln Formation. In several exposed sections, a
thick breccia or conglomerate of volcanic rock fragments
and some pebbles of Skookumchuck-like lithology marks the
base of the Lincoln Formation. In other sections, the
overlying rocks are nearly conformable, but marked by a
distinct change in facies. Only in a few places where the
contact is exposed is it gradational between the
Skookumchuck Formation and the Lincoln Formation, although
the length of time involved in the observed unconformity

is open to question.

3O

Keasey Formation

 

Schenck (1927) applied the name Keasey Formation to
about 500 feet of dark gray, tuffaceous, marine sediments
exposed along Rock Creek for two miles east of Keasey,
Columbia County, Oregon. This description has since been
emended to include beds stratigraphically higher that crop
out farther down Rock Creek (Weaver, 1937; Warren and
Norbisrath, 1946). The formation consists of three members,
the lower of which represents the original type section.
The total thickness of the Keasey Formation is about 2000
feet, and it rests with apparent conformity upon rocks that
have been mapped as Cowlitz Formation (Skookumchuck of this
paper). The underlying sediments consist of bluish-gray
sandstones, lignitic siltstones and gray, micaceous silt-
stones that are very similar lithologically to the
Skookumchuck Formation, except that no coal is present.

The upper part of the Skookumchuck beds along Rock Creek
are mainly massive to slightly bedded sandstones that
appear to grade into the dark, glauconitic, tuffaceous
siltstone of the lower member of the Keasey Formation.

The Keasey Formation is exposed in numerous localities
in northwest Oregon, but an especially good section is
exposed along the Wolf Creek Highway near Sunset Tunnel
in Washington County, Oregon. The upper two members are
both well exposed in road cuts, although the lower member
is not definitely present in this section. For this study,

the lower member is of particular interest, and when the

b

nib.

~\U
'7‘

31
term Keasey Formation is used henceforth, the lower member
of the Keasey Formation will be implied. The Keasey
Formation has been recognized in Washington State (Rau,
1951; Weaver, 1937), but current workers do not use that
designation, referring instead to the Lincoln Formation,
which occupies in large part a similar stratigraphic
position, and is similar lithologically.

The age of the Keasey Formation is given as Early
Oligocene in Schenck’s original description, based on
foraminiferal and molluscan assemblages which are common
throughout the section. Moore and Vokes (1953) give a
brief but convincing argument for an earliest Oligocene
age for the Keasey Formation (rather than Eocene), although
Weaver (1944) and Warren and Norbisrath (1946) indicate the
possibility of Late Eocene age for the lower member. That
the Keasey Formation is correlative in part with the
Lincoln Formation is clear, but the exact time relationship

is not yet established.

PART II: STRATIGRAPHIC PALYNOLOGY
General Statement

The zonation of the time-rock column represented by
the rock units described in the previous section is a
primary objective of this study. For this purpose a total
of 120 samples were prepared and examined. Well—preserved
plant microfossils in large numbers were present in all but
eleven of the samples. Two of the eleven were fairly well
sorted sandstones from which the microfossils had been
winnowed in the sorting process accompanying deposition.
Eight barren samples came from one section located east of
Seattle in the foothills of the Cascades. The section
consists of the Raging River and Tiger Mountain formations,
which are probably partly correlative with the McIntosh
and Skookumchuck Formations further south. The sediments
were complexly interbedded with volcanic rocks, however,
and the lack of plant microfossils in the collected samples
is attributed to the effect of high temperatures and the
subsequent development of locally degrading conditions.
Because of the lack of microfossils, the attempt to include
that section in the correlation had to be abandoned. Only
one other sample was barren, and that also was associated
with a volcanic flow in the lower part of the Stillwater
Creek section. The samples that were used came from six
separate measured sections in western Washington and Oregon.
The location of these sections and the subsequent

32

33
correlation between them are described in the following

paragraphs.

Studied Sections

The location of the sections is shown in Figure 3, and

are described in greater detail in Appendix A.

Stillwater-Olequa Creek Section

 

This section is exposed in the banks of Stillwater
and Olequa Creeks, from three miles west of Ryderwood to
one mile south of Winlock, Lewis and Cowlitz Counties,
Washington. The total section is 8000 feet thick and
consists predominantly of marine siltstone and sandstone
of the McIntosh Formation, with increasing amounts of
interbedded non-marine siltstone, sandstone, and coal of
the Skookumchuck Formation near the top. These beds dip
8-10° east to northeast, strike from N45°W to due north,
and are off-lapping by erosion relative to the underlying
Crescent Formation. This section is located on the
northern flank of the south—eastward plunging Willapa Hills
anticline. The rocks range in age from late Middle Eocene
to Late Eocene and are overlain by the Oligocene Lincoln
Formation which appears unconformable on top of the Eocene
sediments. This section has been measured in detail by
Henrikson (1956); the upper part, only, by Weaver (1934);

and the lower part, only, by Rau (1958).

34
Willapa River Section

 

About 1250 feet of gray marine siltstone and sandstone
are exposed in the Willapa River stream bed over a distance
of three miles, about 10 miles southeast of Raymond,
Pacific County, Washington. This represents only the lower
portion of the total exposed section which is one of the
best Tertiary exposures in the area, ranging from the Upper
Eocene McIntosh Formation to the Miocene Astoria Formation.
This section is very similar lithologically to the lower
part of the Olequa-Stillwater section (McIntosh Formation)
but it is greatly shortened. Non-marine rocks of the
Skookumchuck Formation are entirely lacking. The rocks
dip 10-20° NE and strike about N30°W, and the section is
part of the north limb of the Willapa Hills anticline.

Rau (1951 and 1958) has studied the section in detail and

described the foraminifera.

Chehalis River Section

 

The Chehalis River section is a composite of several
discontinuous outcrops in the vicinity of PeEll, Lewis
County, Washington. A total thickness of about 4500 feet
is represented, consisting mostly of McIntosh Formation.
Near the top, however, beds of lignitic siltstone containing
coalified wood and massive bluish-gray sandstone are
present, which are assigned to the Skookumchuck Formation.
The rocks dip generally north at 5-25°, strike nearly east-

west, and are located on the north flank of the Willapa

Hills anticline. This section was included within the area

35
studied by Pease and Hoover (1957). The Eocene rocks appear

to be conformably overlain by the Lincoln Formation in this
section, although there is an abrupt facies change and a

coarse clastic basal unit is present.

McIntosh Lake Section

 

This section is located about 5 miles east of Tenino,
Thurston County, Washington, in a road out along State
Highway 5A on the south side of McIntosh Lake. It is part
of the composite type section of the McIntosh Formation,
and consists of about 300 feet of dark gray, fissile to
massive marine siltstone, with interbedded calcareous
horizons. The section dips uniformly 12-15o S.E., strikes
N40°W, and is located on the northeast flank of the Craw-
ford Mountain anticline which plunges to the southeast.
The McIntosh Formation at this locality has been dated as
late Middle Eocene, and has been measured in detail by
Snavely, et a1., (1958). The upper and lower contacts are
not exposed at this locality, but nearby, the volcanic
rocks of the Northcraft Formation lie directly upon the

McIntosh Formation.

Rock Creek Section

The Keasey Formation is exposed in the banks of Rock
Creek between Keasey and Vernonia, Columbia County, Oregon.
This section is discontinuously exposed and consists of
nearly 1000 feet of tuffaceous, gray, marine siltstone

with some horizons of calcareous concretions. The locality

36
is on the northeast flank of the Coast Range of Oregon
where that structural high plunges toward the north.
Several smaller folds complicate the section somewhat, but
the deformation is not extensive. The section was originally
measured and described by Schenck (1927), and Warren and
Norbisrath (1946) discuss it in detail. The age is given
as Early Oligocene. The Keasey Formation overlies sand-
stone and siltstone of the Skookumchuck Formation with an
apparently conformable contact. Only the lower member of
the Keasey Formation is represented in this section, and

the top is not exposed.
The Composite Reference Section

In order to establish a time-stratigraphic reference
for the rocks within the area, it is necessary to have a
complete rock section which represents all of the time in
question. This is the purpose of the composite reference
section. An abstract rock column is pieced together from
separate outcrops in such a way that any gaps in a given
section are filled by rocks from another section. In the
area presently being considered, there is no single section
which gives a complete record of Middle Eocene through
Early Oligocene time, although the 8000 feet of the Olequa-
Stillwater section apparently approaches that. It was
determined that part of the record was missing in the
unconformity at the top of the Skookumchuck Formation in

the Olequa-Stillwater section. From field investigations

37

it was apparent that this same break was present in several
sections, and possibly present in others where the contact
was concealed. However, in the Rock Creek section, rocks
lithologically similar to the Skookumchuck Formation grade
without any apparent break into the greenish—gray,
glauconitic, tuffaceous siltstones of the lower member of
the Keasey Formation. Paleontologic work (Warren and
Norbisrath, 1958; Moore and Vokes, 1953), indicates that
the Keasey Formation along Rock Creek is older than the
type Lincoln Formation, but younger than the Skookumchuck
Formation along Olequa Creek. This does not offer con-
clusive evidence for the placement of the Rock Creek
section on the top of the Stillwater-Olequa section in the
composite section, but it lends support. A preliminary
examination of the plant microfossils showed that the
lowermost samples from the Rock Creek section are not only
lithologically similar, but also bear a spore - pollen
assemblage that is very similar to the Skookumchuck
Formation at Olequa-Stillwater section and the Rock Creek
section to construct the composite reference section from
which the stratigraphic ranges of the plant microfossils
could be established. The time represented in this section
is from late Middle Eocene to Early Oligocene, although the

Eocene-Oligocene boundary is not well established in the

area.

38

Zonation

Qualitative Method

 

Two fundamental kinds of information are available in
the fossil record; one is qualitative, or the kinds of
fossils present; the second is quantitative, the number of
fossils present, both individuals and species. Both the
qualitative and quantitative data may contain significant
information, but it is available only if methods can be
devised to extract it. The qualitative methods of this
paper are entirely empirical. The stratigraphic ranges
within the reference section of all of the microfossil
classes comprise the data. Of the two possible kinds of
stratigraphic distribution, long ranging or limited range,
only the second is of stratigraphic value qualitatively.
Several factors may contribute singly or through inter-
actions, to limiting of the range of an organism. If the
time involved is sufficient, evolutionary processes within
a population may lead to the creation of distinct, new
forms. Through essentially the same selective processes,
established forms may become extinct. Even the most
sedentary of biologic organisms may alter their distri-
butional patterns in response to changing environmental
conditions, and new forms may occur in a stratigraphic
sequence as the result of immigration. Likewise, estab-
lished forms may emmigrate, with a resulting termination of

their fossil record in a given area. The full understanding

39
and appreciation of all of these factors may eventually
lead to establishment of continental or even inter-
continental recognition of biostratigraphic age determina—
tions, and that is the ultimate objective of biostratigraphy
in general. However, in the present study, considering the
state of the art in palynology, the simple recognition of
the effect of any of these factors is considered signifi-
cant. The most conspicuous effects recognized are the
first occurrence of new forms and the last occurrence of
established types. The latter is generally less reliable
than the first occurrence, stratigraphically. Reworking of
fossils from older into younger rocks is an occurrence often
observed by palynologists. If the time interval represented by
the total range of a species is small, that species may
become a key form for a particular zone or horizon.
Factors such as distinctive morphology, consistency or
frequency of occurrence, and extent of dispersal, etc.
may increase or decrease the value of a species as a key
fossil. By utilizing these empirical relationships, a
zonation can be achieved. Of 300 or more entities
differentiated during the course of this study, which
comprise only those types represented by a significant
number of individuals, 53 show a restricted stratigraphic
distribution. The remainder are either long ranging forms,
or they occur in such a sporadic manner that their range
is not reliably indicated. Many more palynomorphs were

observed in the samples studied, but they generally were

 

 

4O
represented by single specimens and thus lack statistical
significance. The placement of zone boundaries, based on
the qualitative aspect of the microfloral assemblages, is
largely subjective. There is no evidence of large scale
changes which are reflected in grossly different
palynological assemblages. The changes are rather subtle,
producing a gradational sequence of characteristic
assemblages with many more species in common than unique.
The boundaries were selected where the most conspicuous
differences were evident at a midpoint between distinctive

floral assemblages, or at the transition zone between them.

Qualitative Results

Five zones are established on the basis of the
stratigraphic range of 53 palynomorph species. Those ranges
are shown in Figure 5. The chart is arranged according to
the position of first occurrence of the palynomorphs in
the composite reference section. The zones are designated
by letters, starting with the lowermost as zone A. The
palynomorph types are listed by code designation. These
codes are included with the formal names applied in the
systematic section. These forms include pollen of
gymnospermous and angiospermous plants, fern spores, and
a few dinoflagellates in encysted stages and marine
organisms of unknown affinity. The ranges shown here are
not intended to indicate the absolute range of the species

in time, but the sample size considered in establishing

these ranges has been large enough that they may be

41

 

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STRATIGRAPHIC RANGE OF 53
SELECTED PALYNOMORPH SPECIES

FIGURE 5

obese
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42
utilized with some degree of confidence locally. The 53
species selected represent only a small portion of the
total palynomorph content of the rocks studied. Certainly
many of the 300 other differentiated forms, as well as
others that were not recognized as distinct, do exhibit a
distribution in time that is of stratigraphic value.
Perhaps further study will allow a more precise and far
reaching zonation.

Several characteristic features of each zone are
described in the following paragraphs, including the most
significant forms of each zone.

Zone A is characterized by the association of P3gm—1,
Alga-l, ny-8, and C3gm-l. These forms are not restricted
to this zone, but they do not appear in the younger zones
as a recognizable assemblage. The form CP3st—5 is not
found above zone A, and, although it is not a common type,
it is a useful key fossil. C3r-9, Til-6, Til—7, P3sm-4,
and Syn3g-4, have their first occurrence within zone A.

A significant feature of this zone is the lack of many
distinctive forms which are present in the younger zones.
This negative evidence is not conclusive, but it is useful.
Plate 1 illustrates the zone A palynomorphs.

In zone B, sixteen forms occur for the first time.
Alga—l and P3gm—l disappear in this zone and do not
reappear until much later in zone E. The presence of such
forms as CP3g—7, P r-3, Syn3r-1, and CP3r-7 in association

with P3gm—1 and Alga-l, and the absence of forms from

43
higher zones, characterize zone B. The most characteristic
palynomorphs are shown on plate 3.

The first common occurrence of six distinctive paly-
nomorphs, a key form, and the lack of lower and higher
forms, characterize zone C. Several appear first in the
uppermost part of zone B, but are most characteristic of
zone C. P5rug-l, Syn3g-2, Dino—1, and C3r—l are especially
significant in this zone. ny—4 has been found only in
zone C, and is common in some samples. All of these forms
are illustrated on plate 2.

Zone D is the most distinctive of the five zones.
Twelve common and distinctive forms appear for the first
time and the ranges of six forms terminate in this zone.
Also, CP3sp-l, an uncommon but consistently occurring form,
is a key fossil. Of particular interest in the recognition
of the zone is the absence of ny—8, and the first common
representation of Tsuga and Picea types. The presence of
er-l, C3r-l9, CP3st-4, CP3g—6, and Prot-5 are also signi-
ficant in this zone. Plate 4 illustrates the types of
zone D.

Zone E is a very significant time-stratigraphic unit.
The ranges of fifteen common forms terminate in this zone,
some of which have been important members of the microfloral
assemblage throughout the lower part of the section. Six
forms appear in abundance for the first time in this zone,
including A1-6 and Car—3, both of which are abundant forms

in samples from overlying Oligocene rocks that have been

 

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on

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44
examined, but not included in this study. It is probable
that this zone represents the early part of the transition
from Eocene to Oligocene microfloral assemblages, and forms
such as P3sm-4 and C3sp—4 may be reliable indexes to the
Eocene rocks of the area. The microplankton forms ny-9
and Tith—l are conspicuous in the all marine rocks of this
zone. Tytthodiscus is a very common element in the
Oligocene marine rocks higher in the section as well. Zone

E forms are illustrated on plate 5.

Quantitative Method

 

The quantitative aspects of a fossil floral assemblage
(abundance, inverse-positive associations, diversity, etc.)
may be of stratigraphic value, especially when the time and
area under consideration are fairly limited. The number of
individuals of different species (sporophytes) growing
within an area is, in a general way, in ecological equilib-
rium with the environmental forces acting upon them.
Changes in the environmental conditions are reflected in
the numbers of individuals of different species, as some
gain competitive advantage at the expense of others. These
changes are also reflected in the microfloral record, since
the amount of pollen available for incorporation in
sediments as fossils is in large part determined by the
abundance of the parent plants in the vegetation. Ideally,
the absolute number of individuals of various species of

palynomorphs originally deposited in a unit volume of

sediment, or per unit area on a depositional surface, is

45
required for stratigraphic evaluation. The absolute
abundance of a single palynomorph is not affected by the
abundance of others. If a high or low abundance of a
particular type is stratigraphically significant, this
maximum or minimum will be present in all comparable
sediments deposited at the same time, regardless of the
numbers of other individuals present. This cannot be
realized practically, however, because of the difficulties
of sampling an area of a depositional plane, and the lack
of information regarding rates of sedimentation. Therefore,
relative numbers of palynomorphs present are utilized. The
relative abundance of one kind of pollen or spore is a
function of how many individuals of other kinds are
present. Several factors may contribute to variations in
the relative abundance of individuals of different species
in a stratigraphic section. Many of these factors may have
nothing at all to do with time-related phenomena, but
rather may be the result of local variations in pollen
output, accumulation, or preservation. In this case, a
form which has a constant absolute abundance in the
sediment may show wide variation in its relative abundance,
because of the increased or decreased abundances of other
palynomorphs. Therefore, it is imperative that relative
abundance data be carefully analyzed before stratigraphic
conclusions are drawn. The data gathered are simple counts
of individuals within a population and percentages are

computed on the basis of the total count. Often a fixed

46
sum is used. The fixed sum should be sufficiently large
that the sample means are reliable estimates of the
population means. Another possibility is to count a fixed
area of a slide instead of a fixed sum. Both of these
techniques are used in this study, but for gathering
different kinds of information. A fixed sum count of 200
grains was made, including all plant microfossils arranged
into 35 classes. This provides information concerning the
most abundant forms represented, which in turn may yield
conclusions regarding the distribution of the plants and
their environments. A fixed area count was made of ten
pollen and spore species to provide stratigraphic informa-
tion.

If the hypothesis that relative abundance data has
time-stratigraphic significance is to be utilized, several
assumptions must be accepted. The first is that the plant
microfossils contained on a slide are a random sample of
the pollen-spore assemblage present at a given strati-
graphic level. Second, it is assumed that on a single time
plane, the distance between any two samples is small
relative to the distance from the source of the pollen and
spores. This means that at any given time the distribution
of the plant microfossils and their relative abundances are
constant over the area under consideration or have a
definable gradation in their areal distribution. Sorting
action or selective degradation in the sedimentary

environment creates variations in the pattern of

47
distribution, but these variables are not random and can
usually be compensated for in the final analysis. Third,
it is assumed that the ratios among spore and pollen types
in a sediment sample reflect specific, although usually
unknown, ratios among the sporophytes from which they came.
It follows from this that changes in the abundance of
pollen and spores reflect changes in the sporophyte popula-
tion. Fourth, it is assumed that any condition which leads
to a change in the abundance of individuals of different
species (sporophytes), as that change is reflected in the
related abundances of the palynomorphs selected, is
operative over a regional extent. This assumption is
necessary in order that fluctuations in the abundances of
the selected palynomorphs can be interpreted as having
correlative stratigraphic value. The conditions which
might be effective in this way include climatic shifts,
major edaphic alterations, and evolutionary trends.

The validity of these assumptions, and hence the
hypothesis, depends on the careful choice of the micro-
fossil types selected for quantitative analysis. It is
obvious that the assumptions do not hold if pollen from
indigenous swamp plants are included in the count of a
coal. Several factors determined the choice of the ten
forms counted in this phase of the study: (1) they were
long ranging forms; (2) they were common enough that they
could be expected to be found in most samples; (3) they

were distinctive enough morphologically that no confusion

48
over identification would occur, even at fairly low
magnifications of study; and (4) the source of the pollen
or spore was removed from the depositional environment.
Some control for the determination of the fourth condition
was developed by determining the relationship of various
palynomorphs to different lithologic types, and the
elimination from consideration of those which show a
significant correlation with particular lithologies. Also,
in the final counts, a continual comparison was made with
several attributes of the samples which clearly have
environmental significance, such as relative numbers of
microplankton and fungi, and the facies of the rock itself.
Consideration was also given to pollen and spore types
referable to extent genera whose known ecological require-
ments preclude the reasonable possibility of their growth
in proximity to the depositional environment in which these

palynomorphs were found. The ten types are: Osmundacites

 

(1 species); Schizeaceous spores (3 species); Podocarpidites

 

(2 species); Pinuspollenites (1 species); Sabalpollenites

 

 

(1 species); Momipites (2 species); Ilexpollenites (1

 

 

species); Pterocaryapollenites (1 species); Proteacidites

 

 

(1 species); and Ephedripites (1 species). These forms are

 

illustrated on plates 6 and 7. To provide the data on the
ten selected classes, the fixed area was the center 18 x

18 mm square of a 22 x 22 mm coverslip. Each occurrence of
the ten types within the square was recorded. The total of

all pollen and spores, exclusive of microplankton and fungi,

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49
was extrapolated from four random traverses, with all forms
counted which could be referred at least to a gross morpho-
logical class, such as tricolpate pollen or trilete spore,
etc. The relative abundance of the ten types was computed
as a percentage of the sum of those ten. The abundance of
the ten collectively, relative to all pollen and spores,

waslcomputed as a percentage of the extrapolated sum of all

Ixalynomorphs on the slide. The figures for the microplankton

arufl fungi were obtained by fixed sum counts of 200 grains
anci are relative to all other palynomorphs on the slide.

The: data obtained are discussed in the following section.

Quarltitative Results

The quantitative data are shown in Figure 6. The
diaggram is arranged into 16 columns which contain all of the
pertainent information. Column 1 is the composite geologic
referuence section, showing lithology and the distribution of
Samplxes. Column 2 is a representation of the depositional
envirwbnment as determined from the facies present in the
sectixbn. It is a very general representation and consists
0f orxly three divisions: (1) marine environment at a depth
greatxer than that where breaking waves are dominant energy
sourwlea; (2) marine environment, but including all nearshore
or Skkoal conditions, some of which may be represented by
bracliish water; and (3) non-marine environment which may
inQJJlde swamps, freshwater estuaries, parts of delta

deVelopments, etc. These interpretations are based entirely

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51

on the facies present, which include poorly sorted gray
siltstone facies; sandy, partly well sorted, carbonaceous,
fossiliferous siltstone facies; and lignitic siltstone or
coaly facies. Columns 3 through 12 show the relative
abundance profiles for the ten selected forms. The abun-
dance of the ten types relative to the sum of all spores
and.pollen is shown as a curve in column 13. Column 14
shows the abundance of microplankton relative to all
Ixalynomorphs. The same is shown for fungi in Column 15.
FfiJnally, column 16 shows the sum of the ten types counted.

Initial attention to the diagram should be focused on

the: effect, or lack of effect, of depositional environment

cui‘the abundances of the ten types selected. Three features

of tflqe diagram are indicative of the depositional environ-
ment;. If the profile of column 13 is compared with column
2: it: can be seen that the percentage total of the ten
types; is highest when the sample is from an offshore marine
Sedinuent. Likewise the numbers of the ten types are
relaizively small in nearshore or non-marine samples. This
indiczates that in the nearshore or onshore area an
indigenous plant population deposited greater numbers of
pollieri than the plants represented by the ten types
seleCited here. This lends support to the assumption that
thesfii ten types had a source area more distantly removed
fronl the depositional environment, but it is not conclusive.
It EHQpears then, that the relative abundance of the ten

takffln collectively is, in a general way, indicative of

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52
depositional environment. Also, when column 14, the micro—
plankton profile, is compared with column 2, a striking
relationship is seen. The microplankton, being totally
indigenous in the marine environment, are very reduced in

relative numbers in the samples which are close to a

vegetated shoreline. A comparison of the microplankton and

fungi curves, columns 14 and 15, shows that an inverse
rmelationship generally holds for these two groups. In

tfliis case, the fungal remains are considered indigenous
fX) the non-marine environments and the distributional
pairtern would be expected to be opposite the microplankton.
Coljamns 2, 13, 14, and 15, therefore, provide a reference

to ‘the changing depositional environments, and provide a

(nultrol to which the relative abundances of the ten

selexzted pollen and spores can be compared. When this

compnarison is made, it is apparent that the depositional

envirnonment exerts little obvious control over the abun-
dance; of the ten. At the generalized level at which the
dePositional environments are considered, the numbers of
the then selected forms relative to one another are inde—
pendfiirm;of depositional environment. There are specific
exceptions to the generalization, but these do not
invalidate the rule, the exceptions and limitations of the
gene”Falization are discussed briefly in a later paragraph.
.Another significant feature to note is the distance
beThNeen samples in the section. Although the time

jINholved is not great, the thickness of the section is.

53
Thirty two samples were analyzed from the 9,000 feet of

composite section for an average of 280 feet between samples.
The samples are not evenly distributed, however, and an
attempt to provide some control was made. The three samples
shown at the 7200 foot level of the section represent a
close interval sampling taken as ten inch channel cuts ten
feet apart in a continuous outcrop. The very similar

values for these samples indicates that the time involved

in the deposition of 30 feet of sediment was probably not
sufficient for evolutionary of climatic changes of the
magnitude necessary to be recognizable in the fossil

record. On that basis, the sample interval over the rest

of the section is assumed to be adequate for the conclu-
sions that are reached.

Relative abundance profiles may show three major
features: first, maximum and minimum values for given
species are shown; second, trends within the profile may
be indicated, either decreasing or increasing; and third,
profiles of different species may exhibit a significant
relationship to each other in particular zones or through
certain parts of the section. If these features cannot be
related to differences in the depositional environments,
then they must result largely from the distributional
patterns of the plants which produced the pollen and spores,
or from error in obtaining the data. The latter has been
minimized as much as possible by careful attention to

procedures, and it is therefore assumed that the variations

54

in the profiles result from the differences in the
composition and distribution of plant communities which
produced the pollen and spores. In a previous paragraph
it has been argued that the relationship among the members
of pollen and spores reflect a specific but unknown
relationship among the sporophytes which produced them, and
that changes in the percentage relationships of the
sporophytes will be reflected by changes in the pollen-
spore ratios. Also it is assumed that the relationship
among the numbers of spores and pollen is generally constant
between two sites on a time plane, provided the distance
between the two is small relative to the distance to the
source of the pollen and spores, and environmental
conditions are not controlling factors. This provides the
hypothetical basis by which the fluctuations in the profiles
shown in Figure 6 take on meaning in a stratigraphical
sense. The maxima and minima, the general trends, and the
positive and inverse relationships are the result of
dynamic changes within the plant communities that produced
the spores and pollen. The changes were effective over
fairly broad areas in a short time, geologically, and
recognition of the changes in the fossil record provides
useful stratigraphic information.

When the information contained in the relative abun-
dance diagram is utilized for correlation, several factors
should be considered. First, the absolute values obtained

for a specific species is not as important as it's relative

 

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55

value. That is, a maximum value in a profile is important,
but whether the absolute figure is 15% or 50% of the sum is
less significant. Likewise, a decreasing trend in the
abundance of a species is significant whether the trend is
going down from 5% to 1% of the total or from 25% to 15%.
Second, the profiles are in no way a continuous log, and
analogies drawn between the discrete samples in a section
and a continuous profile such as obtained in an electric
log are misleading. The lines connecting the bars in the
graph are simply the shortest distance between ends. They
represent an interpolation of sorts, but the possibility of
great quantitative variation in the palynomorphs abundances
in the intervals between sampled horizons must be recognized.
Third, the quantitative results do not necessarily show any
relationship to the qualitative results. The quantitative
data may be used to establish an independent part of the
zonation, but they are put to use here as correlative

points with the qualitative zones.

Correlation of Zones

 

The extent to which zones established on certain
criteria for the reference section may be recognized by
those same criteria in other areas is a measure of the
stratigraphic usefulness of the zones. In this study, four
separate sections were examined and compared with the
composite reference section to determine the extent to

which these zones could be recognized laterally. These

sections have been described previously. In order to

56

facilitate the comparison of the microfloral assemblages, a
qualitative checklist was devised (Figure 7). Some of the
palynomorphs selected for the qualitative zonation are
shown along the top of the chart, grouped under the zone in
which their first occurrence is found. Since many of the
species found first in the lower zones have a range which
extends into higher zones, the groupings of species are not
totally diagnostic assemblages for the zone under which
they appear. The zonal groupings shown provide a maximum
relative age, i.e. a comparison sample containing species
with first occurrences in zones A, B, and C is indicated as
being not older than zone C. If species which first appear
in zone D or higher are not present in the sample being
correlated, a. tentative minimum relative age is provided,
that is, not younger than zone C. The four sections being
correlated with the reference section are shown along the
Side of the chart. A check mark (X) in the sample column
Of these other sections indicates the occurrence of the
characteristic palynomorph indicated in the zonal groupings.

The quantitative data from the sections to be
Correlated is shown in Figure 8. Several points should be
mentioned regarding these diagrams. First, not all of the
profiles show correlative values at the same horizon. This
discrepancy may be due either to failure to meet all of the
necessary assumptions completely (as discussed previously),
or tO a difference in the stratigraphic positions of

Samples for which the interpolation between known values in

 

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59
the reference section is not valid. Both factors probably
interact to produce the observed anomalies. The profiles

of Ilexpollenites, Palm and to some extent, Momipites, seem

 

to be the least consistent of the ten forms. In a later
section it is suggested that these forms may have grown

close enough to the swamp environment that they are over-
represented there, and thus do not meet the conditions of

the assumption that the distance from deposition site to the

sour ce is large .

Correlation of the McIntosh Section

The two samples examined from the McIntosh Lake section
are from the dark, calcareous, carbonaceous, marine silt-
stone in the upper part of the McIntosh Formation. Sample
2 is located about 100 feet stratigraphically above Sample
1 and both contain large numbers of palynomorphs. The
presence of six types in the two samples that are commonly
fOuhd in zones A and B (see Figure 7) and the total absence
of typical zone C or higher types indicates that the rocks
in this section should be correlated with zone B. Quanti-
tatively the two samples are quite similar and are

Characterized by fairly low Podocarpidites values, signifi—

 

cant percentages of Proteacidites, and high values for the
tWO fern groups. Within zone B, these samples seem to

match samples 14 and 15 of the reference section most closely.

CO£‘glation of the Skookumchuck Section

The lowermost of the four samples examined from the

7M1
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o.‘w

 

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6O
Skookumchuck section is correlated with zone C (Figure 7).
The three higher samples all contain types indicative of
zone D. The quantitative correlations were made as follows:

Sample l—-The very high Osmundacites value, and the low

 

Podocarpidites value indicates a correlation near Sample 21

 

of the reference section.
Sample 2—-This sample also has a high percentage of

Osmundacites, but is declining relative to Sample 1, while

 

Podocarpidites is increasing. This pattern, as well as the

 

relative values of the rest of the spectrum correlates with
interpolated values between Samples 22 and 23 of the
reference.

Sample 3——This fits into the same pattern as 2.

Sample 4——This sample appears to correlate near

Samples 26 and 27. The high Osmundacites and low

 

Podocarpidites fit well into the interpolated pattern near

 

those two reference samples.

Correlation of the Willapa River Section

Palynologic assemblages in the lower part of the
Willapa River section correlate with assemblages in the
upper part of the composite reference section. Of the
seven samples analyzed, the lower four samples contain
palynomorphs indicative of zone D while the upper three
contain typical zone E palynomorphs (Figure 7). The
quantitative correlations follow:

Sample l-—The spectrum of this sample is very similar

v»

.' v V

a r. 71‘1“.

JV.-

(u

 

  

{/2

..
p
v

(«I
(H

6l
to that of Sample 25 of the reference section, and probably
correlates fairly near that position.
Sample 2-—This sample has a lower percentage of

Podocarpidites and a greatly increased value for

 

Osmundacites. Considering the rest of the spectrum as well,

 

it correlates near Sample 26 of the reference section.
Sample 3-—This sample is similar in many respects to
reference Sample 30.
Sample 4--The significant percentage of Protiacidites
in this sample, and the relative values of Podocarpidites

and Osmundacites, indicate a correlation near reference

 

Samples 30 and 33.

Sample 5--This sample is compared well near Samples
33 and 35 of the reference section. The quantity of

Egoteacedites present is significant, although not conclusive.

 

Sample 6—-The relative values and trends of this sample
Spectrum correspond quite closely to reference Sample 35.

Sample 7—-This sample possesses a characteristic
Spectrumthat cannot be compared directly with any reference

Samplra in zone E, but it is most comparable to Sample 43.

EEEEEELation of the Chehalis River Section

lirom the data of Figure 7, Samples 1 and 2 are
Correlemdye with zone D of the reference section, and
Samplrng 3 and 4 are correlative with zone E. Within these
two ZCHres, the relative abundance spectra of the four

Samples are compared with the reference section as follows:

Sample l--The low Podocarpidites value, significant

62

Proteacidites and moderate Osmundacites correlate with the

 

interpolated values between 25 and 26 of the reference
section. The forms Ilexpollenites, Pterocaryapollenites

and the Schizeaceous fern spores also show similar relative

values.

Sample 2—-This spectrum is very similar to sample 26
of the reference section, with Podocarpidites, Proteacidites

and Osmundacites present in identical percentages.

 

Sample 3-—This sample appears to correlate near Samples
35 and 39 of the reference section. The absolute values are
lower, but the whole spectrum shows a fairly good relative
fit with 35.

Sample 4-—The very low values for Podocarpidites and

Osmundacites, and an exceptionally high value for

 

Pterocaryapollenites indicate a correlation with, or near,

Eknnple 39 of the reference section.

éflgmnary of Palynologic Correlations

Figures 9 and 10 are cross sectional diagrams of the
Efiluiy area. The base of the Lincoln Formation is used as
a dalium, and thicknesses and distances are drawn to scale.
FigUJFe 9 is an east-west cross section including the
Stillwater-Olequa section, Chehalis River section, and the
williapa River section. Several features of this diagram
are significant:

1. The Skookumchuck Formation thins and finally
DimBhes out towards the west.

2. The Skookumchuck-McIntosh contact transgresses the

63

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64

time lines westward.

3. The McIntosh Formation is onlapping the Crescent
Formation to the west.

From field observations it is possible to observe the
thinning of the mostly non-marine rocks of the Skookumchuck
Formation westward. A general regressive trend of the
marine deposits toward the west is indicated, with a shore—
line stand only a few miles from the present day coastline
in Late Eocene time. It is possible that the non-marine
rocks of the Skookumchuck Formation extend even farther to
the west, but have been removed by erosion, although the
unconformity in the Willapa River section does not appear
to support that idea. The uplifting forces which caused a
westward retreat of marine conditions probably continued so
that the Eocene sediments were exposed to erosion at the
end.of Eocene time, thus producing the unconformity below
the Karine Lincoln Formation. It is also possible that the
effkects seen in this cross section are fairly local in
exixent, reflecting the presence of a volcanic high area in
the VVillapa Hills. The onlap of the McIntosh shows the
presflence of such a high area, and it was probably the source
for Inany of the sandstones in the McIntosh Formation
COmPNDsed of volcanic rock fragments. The westward displace—
ment; of marine conditions seems to have been more general,
hOWeVer. Field data and published reports (Vine, 1962 and
Virus, 1963) farther to the north indicate a similar
cotThinental overlap by the Puget Group on middle Eocene

maPine sediments (Raging River Formation).

 

65
Figure 10 shows a north-south section including the
McIntosh Lake section, the Skookumchuck section, the
Stillwater—Olequa section, and the Rock Creek section.
wa0 features are particularly noteworthy in this diagram:

1. The Skookumchuck section is considerably shortened
by" erosion relative to the Olequa—Stillwater section.

2. The Keasey Formation (lower member) represents at
lfieaist part of the time represented by the unconformity at
trlez top of the Stillwater-Olequa section.

The upper part of the Skookumchuck section collected
irl ‘this study lies very near the unconformity below the
LiJncnoln Formation, although the actual contact is not
exqpc>sed. It appears that considerably more of the
Eflaoc>kumchuck section was removed by erosion than of the
fitilewater—Olequa section. About 2,000 feet of mostly
rmni-qnarine sediments are represented by zones D and E in
the jlatter that are not present in the Skookumchuck section.
Thies represents a significant amount of relief along the
unccnnformity, although only local angular discordance can
be Eneen. This may be related to the volcanic activity
whicli produced the Northcraft Formation and the extensive
veleenlic terrane of late Eocene age to the east.

(Po the south, the unconformity seems to disappear, and
the bcnandary between the Skookumchuck and Keasey Formations
15 irKiicated by a gradual lithologic change only. This
prOViCkis a rock record for at least a part of the time

lnvolveuj in the unconformity in other sections.

66

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67

The Eocene—Oligocene time boundary is not well defined
in the region. Most authors agree that the Lincoln
Formation is Oligocene, but the lower part may be Upper
Eocene on paleontologic evidence (Rau, 1958). The
Skookumchuck Formation is well established as Upper Eocene.
The Keasey Formation (lower member) is probably Upper Eocene,
although it has been called Lower Oligocene (Moore and Vokes,
1953). No evidence of a. definable time boundary was found
in the palynological record. Many of the species of pollen
and spores found have been reported from both Eocene and
Oligocene rocks. The literature in Tertiary palynology is
not extensive enough at present to permit an accurate
evaluation of absolute age relationships of that order.
Many of the forms identified may well be index forms for
Eocene rocks, but such an assignment at this time would be
Premature. The best alternative is to depend upon age
assignments based on other fossil assemblages. Tschudy
(1964) presents a good review of these stratigraphic
prinCiples.

The value of palynological analysis is clearly
demoI’lstrated in the correlation of marine and non-marine
rooks within the cross-sections shown. With study of
additional sections, it should be possible to accurately
pOI“Cray the paleogeographic and environmental setting,
inclleing the extensive areas of non-marine deposits which
eXtehd over the eastern part of the study area and into the

Cascade Mountains. Only by the establishment of a relative

68
chronologic framework can the distribution of facies, and

their lateral changes, be fully appreciated.

A Hy

 

PART III: FLORAL AND ENVIRONMENTAL SECTION
Introduction

To obtain a better understanding of the composition,
dijstribution, and development of the fossil flora of the
earrth is a legitimate goal of the palynologist. A
coritribution to the composition and distribution of the
lommar Tertiary flora is one of the objectives of this
stucty. Data of this type contribute mainly to the purely
botarlical aspects of the plants of the Tertiary Period,
but ‘they also have stratigraphical significance. If the
goa1.<of regional biostratigraphic correlation is to be
realgizmxh full appreciation of the past phytogeographical
relatxionships is necessary, especially when dealing with
relaizixvely small time-stratigraphic units. A great deal
yet IlEEGdS to be done before any synthesis of data on the
Tertiiaxw flora, its composition and distribution, can be
acmenuplished, but progress is being made. Papers by
TWflTuxiy (1964) and Schopf (1964) are especially valuable

inproviding guidelines along which to proceed.
Composition of the Flora

Methods
\
The data for this portion of the study was obtained

at tkKe same time as the stratigraphic data, and is in part
the Same. The qualitative classification of the pollen and

S o . . .
p FEES ,present in the samples, and their subsequent naming,

69

{n

70

provides the floral data. The procedures followed in

nomenclature are discussed in the next section, but several

related aspects are pertinent now. It is assumed that

pollen or spore morphology is genetically linked with the
sporophyte. That is to say, a taxonomic group of plants
(sporophytes) can often be recognized by the morphological

characters exhibited by their dispersed spores or pollen.

The identity often extends only to family level, frequently

to generic level, but only seldom to species. It is also

assumed that it is perfectly reasonable to recognize the
presence of an extant plant taxon in the fossil record on
the basis of dispersed spores or pollen, even though the

dispersed spores or pollen may possess a different taxonomic

name. Further, it is assumed that fossil plants referable

to extant taxa. possessed ecological requirements that were,
in general, similar to those of the modern plant. On the

basis of these assumptions, the results shown in the next

para gr aphs were ob ta ined .

W

Table 1 is a generic plant list for the study area.
It is based on assumed affinities of the pollen and spores
found in this study, and on the published identifications
Of isOlated leaf floras from the Puget Group (late Middle
and La te Eocene), the McIntosh Formation, and the
SkOOkumchuck Formation. The me'gafloral data comes from

W
Olfe, et a1., (1962); Wolfe (in Vine, 1962); Warren,

N .
orblsrath, and Grivetti (1945); and Brown (in Roberts:

Table 1:

Floral List.

Leaves, Wood, etc. (From Published Sources).

Equisetum
Sphagnum
Lycopodium
Selaginella
Isotes
Anemia
Lygodium
Gleichenia
Cyathea
Hemitelia
AllantodiOPsis
Lastrea
Dicksonia
Polypodium
A8p1enium
Phyllites
Osmunda
Taxodium
Metasequoia
Glyptostrobus
Podocarpus
Pinus

Abies

Picea

Tsuga
Ephedra
Nymphoides
Quercus
Castanea
CastaneOpsis
Platanus
Cercidophyllum
Davilla
Tetracera
Cinnomonum
Persia

X X X X X X X X POLLEN-SPORES

XX

XXXXXXX

XXXXXXXXXX

X «ax X

XXXXXXXXXX

LEAVES, STEM, ETC.

X

XXX

Cryptocarya
Octea
Laurophyllum
Machilus
Lindera
Litsea
Aralia

Ilex
Euphorbiophyllum
Prunus
Rhododendron
Rhus

Cyrilla
Alangium
Nyssa

Cornus

Ulmus

Celtis
Rhamnus
Ceanothus
Gordonia
Symplocos
Tilia

Trium felta
Ficus

Betula

Alnus
Carpinus
Corylus
Juglans
Carya
Engelhardtia
Pterocarya
Platycarya
"Momipites"
Myrica

71

POLLEN-SPORES

XXXXXXXXN X

XXX

XXXXXXXXXXX

LEAVES, STEM, ETC.

XXXXXXX

XXXX

N’s,

'0

XXX

X

Bombax
Proteacidites
Maclintockia
Cupania
Liquidambar
Salix
Fuchsia
Epilobium
Bursera
Sabal
Viburnum
Stephania
Hyperbaena
Pachysandra

Includes Sporophytes Inferred From
Fossil Spores or Pollen, and Plants Identified From

POLLEN-SPORES

XX

NXXXXXXX

XXXX

LEAVES, STEM, ETC.

X

 

{A

m.

1‘

\4

 

72
1958). The occurrence as pollen-spores, as leaves, or both,
is indicated by checks adjacent to the name.

It is by no means a complete list. 100 plant taxa
(Sporophytes) were tentatively identified from dispersed
spores and pollen and appear in the table, but a total of
more than 300 entities were differentiated in the course of
the study. These 300 must certainly represent but a fraction
of the total flora extant within the study area in late
Eocene time. The area today supports about 1500 species of
higher plants, and cannot be considered as having a "rich"
flora. In modern sediments of the area, the pollen and
spores of only about 50 of these 1500 can be found with the

regularity that 200 or more are found in the late Eocene

rocks.

Environmental Indicators in Flora

Tropical - Subtropical Plants

Several of the classes of pollen encountered in the
study are inferred to represent extant genera or families
whose modern distribution sheds light on the operational
environment of the early Tertiary plants of the study area.
The most Significant of these are several plants which
indicate a tropical to subtropical element present in the

flora. These include the following:

1. Alangium - This genus is restricted to tropical

 

and subtropical parts of the Old World. It occurs

consistently in the samples studied above its first

..fl
1

Vv‘a

".
.

 

h.
:1...-

C1)

 

73

occurrence in the section although never in abundance.

2. Sapotaceae - Species of this family occur today
widely in the tropics and subtropics, extending to southern
Florida in this country. The pollen of this family is
fairly common in many samples, but is found most frequently
in the lignitic siltstone facies.

3. Symplocos — This is a tropical genus of Asia and

 

.America. It extends today into southern Mexico where it
occupies moist habitats as a tree or Shrub. The pollen is
uncommon in most of the samples studied, but occurs
consistently in the lignitic rocks.

4. Araliaceae — The 65 extant genera of this family
are primarily tropical. The Indo—Malaysian region and
tropical America are the principal centers of distribution.
Some genera are solely or almost entirely climbers; others
are trees or shrubs, often restricted to wet habitats. The
INDllen is never abundant, but occurs commonly throughout
the section.

5. Burseraceae — The genera of this family are
ir1digeneous mainly to tropical America. They are large
tr’ees or shrubs which often occupy drier habitats. Species
Oijursera are found in the Sonoran Desert. The family as
a’Whole, however, is not xerophyteic, and the pollen which
3&3 fairly common in many samples is not that of Bursera
pdorata.

6. Bombax — This genus is most abundant in the

American tropics and is indigenous to either damp or dry

t...

 

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.. -. .... . A .1. r .. w .. 2. h. 6 c .r-.. 31..
«NU. ac BC L .. a . EC :. s . «Wk 3 ... s K

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74

habitats. The pollen is not generally common, but does show
some abundance in samples of the carbonaceous, micaceous
siltstone facies.

7. Palmae - The palms are pan—tropical, subtropical
in distribution. They occur in numerous habitats, today,
but the high frequency of palm pollen in some samples of
coaly facies suggests the presence of a swamp palm in the
study area in early Tertiary time. §abal is a genus of wet
habitats of the Carolina and Florida coasts and may be

similar to the one represented by pollen in the samples.

warm Temperate Plants

Several other genera which are less tropical in
distribution, but mostly limited to warm temperate areas
are also present;

1. Taxodium - This genus is widely distributed as
a swamp tree in the southern United States, and it extends
IX) southern Illinois and Indiana. The Taxodium swamps of
IWKE Gulf Coast are well known. The pollen of this genus is
eOnnnon in most samples, but is most abundant in the lignitic
arui coaly facies.

2. Ny§§a_— The range of this genus includes the
eaEitern United States and China. It is a warm temperate
tr‘63e or shrub which occupies wet habitats and is often
associated with Taxodium. The pollen of Ny§§a_is present

in almost all samples, but its greatest abundance is in the

lignitic siltstones.

 

u...»

rl. I.

:I.

luIM

 

 
 

75

3. Liquidambar - This is a warm temperate to temperate

 

genus common in eastern United States and Asia. It is
frequently found in wet forest habitats throughout its
range. The pollen is fairly common in certain samples, and

is often associated with Symplocos and Sapotaceae pollen.

 

4. Engelhardtia — The range of this genus is mostly

 

in southeast Asia and Malaya, but two species occur in
jMexico and Costa Rica. It is a warm temperate or sub-
tropical plant of upland or mountainous habitat. Pollen of
this genus is common in nearly all samples, but it was

lumped with Momipites in the fixed sum counts. The

 

Momipites-Engelhardtia values are, however, largely composed
of the latter.

Two fern families that are thought to be represented
by spores in the samples are also worthy of mention.

1. Osmundaceae - The genera of this family are mostly
tropical, although three species of Osmunda extend into
tiemjperate America. They occur mostly in wet habitats, and
ill the temperate zone, as damp forest floor and stream side
feruas. The spores of Osmunda are very common in the samples
Stlldied, and are abundant in some carbonaceous siltstones.

2. Schizeaceae — This is an almost wholly tropical
f5imily of terrestrial ferns, with only three species
IDPesent, and these rarely, in temperate North America. The

genera Anemia and Lygodium seem to be the most commonly

 

repI‘esented members of this family, and both of these genera

grow in fairly dry habitats. Lygodium is a climbing fern.

 

..

 

A -

rlno

76
The Spores are common throughout the section, but are reduced

in relative numbers in the lignitic and coaly facies.

Temperate Plants

The remaining plant groups represented by pollen, and
those that provide the greatest abundance of pollen, are
ggenerally temperate in distribution. Most of these,
including the Betulaceae, Fagaceae, Juglandaceae, and
IJlmaceae, do, however, also have sub-tropical or tropical
:representatives of considerable importance. Species of both
iuemperate and sub—tropical distribution are probably
ruapresented in the microflora. Most of the Coniferales
(flggies, Picea, Isuga, Pings, and Podocarpus) are indicative

Of7 a truly temperate element.

Environmental Distribution of the Flora

REfilative Abundance Diagram

 

Figure 11 shows the relative abundance of 43
pefilynomorph classes which are, for the most part, generic
<1essignations. The percentages were obtained by a fixed sum
CCNJnt of 200 grains, exclusive of microplankton and fungi.
Thfie right hand column shows the sample distribution from the
CC>mposite section, and the general lithology for each
SEimple. Although the data consist of relative numbers and
arms subject to several basic limitations, discussed
DIWeviously, a careful analysis of the profiles reveals some-

thing of the nature of the plant associations which were

 

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78
extant at the time of deposition of the sampled sediment.
Comparison of particular reconstructed plant associations
with the rock facies yields some information about the
possible ecologic distribution of the flora. These

associations and their distribution are discussed in the

following paragraphs.

Ecological Elements Within the Flora

The term "ecological element" is used in this paper
to refer to broad groupings of plants growing in the same
general habitat. These elements, and their inferred
relationship to an ecological gradient (swamp, wet, mesic,
dry), are highly speculative and are not intended to
represent an ecological analysis in the modern context of
that science. Successional development and small scale
trends within the ecosystem are beyond the level of this
study.
Four separate elements are postulated from the floral
Ciata: (l) the swamp element; (2) the wet forest element;
(23) the mesic forest element; and (4) the montane forest
efilement. These groupings are based upon Significant
qLLantitative relationships within the relative abundance
IDIRofiles of Figure 11. Several Similar ecologic evaluations
CDI‘ palynologic data from Tertiary rocks have provided ideas
arici guidelines for the identification of the important
Plant associations (Neuy-Stolz, 1958; Teichmuller, 1958;

ale3 Traverse, 1955). An analysis of the modern associations

ll,

QT!

D

{.3 l

79
of plants indicative of specific habitats, can also be
useful for interpretation of the fossil record. The floral
and vegetational data from modern habitats must be viewed
with caution, however, since relatively few studies of
microfloral assemblages from specific habitats have been
carried out. Many studies of Pleistocene bogs and lakes
have been published, and these point out some of the
difficulties in reconstructing vegetation from quantitative
pollen data (Davis, 1962, 1963).

The swamp element is the only element which is likely
to be autochthonous, i.e. growing in, or indigenous, to the
depositional environment in which it is found. The other
elements are represented in mixed assemblages as part of
the allochthonous sedimentary accumulation. With increasing
distance from the depositional environment the influence of
local plant communities decreases, and the microfossil
assemblage becomes a more "average" sample of the entire
flora, rather than reflecting a dominance of certain
locally important plants. Therefore, attention is centered
on those samples of carbonaceous, micaceous, lignitic and
coaly facies which are indicative of nearshore or non-
marine environments. A good general summary of these

principals is presented by Chibrikova (1963).

Swamp Element
Pollen and spores of an indigenous swamp flora are

probably widely distributed in the depositional environments

 

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represented in the studied section. The best record of
this flora is found, however, in the lignitic and coaly
facies. Other floral elements are present in these facies
as well, but the dominance of the pollen spectra by certain
taxa probably reflects the influence of important members of
the swamp flora. A number of different swamp environments
are considered together in this analysis, ranging from open
water to densely vegetated conditions. The most diagnostic
feature from the depositional standpoint, however, is the
high concentration of plant detritus relative to the
inorganic sediments. It is within that framework that the
swamp flora is interpreted. The pollen classes thought to

represent Taxodium, Nyssa, Quercus, various triporate grains,

 

 

probably representing Betula and Myrica in part, and palm
Show positive abundance relationships at several levels in
the reference section (samples 7, 21, and 24). The pairing
of peaks in the Taxodium profile with the Ny§§a_highs, even
though Nyssa_pollen is not an abundant form, probably
indicates the presence of a swamp in which those two genera
were important plants. The high quantities of Quercus
pollen associated with Taxodium and Nyssa;especially in
Sample 39, shows that at least one Species of that genus
was an important constituent. The profile for Quercus
Shows that it was an important pollen producer at almost
all levels in the section, but several species are
represented in the counts. Those species probably were

distributed in several different habitats, thus accounting

81
for their consistent representation. The high abundance of

inferred Betula-Myrica pollen is almost certainly the result

 

of local importance of those trees in proximity to the
depositional site. At sample level 7, a high Betula-
Myrica value is correlated with an anomalously high
percentage of palm pollen. This particular sample is from
a 10 inch coal seam located in the lower part of the
section. Characteristics of the underlying siltstones
indicate that they were deposited in offshore marine
conditions. The coal, however, appears to be closely
associated with a rather thin basalt flow which thickens
abruptly slightly off the line of section. It is postulated
that this volcanic unit represents part of a volcanic
source area which may have been an island. The coal is
separated by about 4,000 feet of marine strata from the
next higher non-marine rocks of the Skookumchuck Formation.
The depositional environment was certainly non-marine
(microplankton) totally absent, and a swamp is a likely
interpretation, but Taxodium and Ny§§a_were not part of the

swamp flora. Instead, palm, Betula-Myrica, and other

 

triporate pollen producing plants, and, to some extent,
Quercus, were the important plant groups. Neuy—Stolz
(1958) describes a similar association from the lower
Tertiary brown coals of the Rhine Valley and suggest a
possible analogy in some swamps of the east coast of
Florida. Fern spores do not play an important role in the

swamp microfloral assemblages. Polypodium spores are often

 

82

common in association with Taxodium, Nyssa, and Quercus

 

assemblages, but their maximum values do not occur in the

coaly-lignitic facies.

Wet Forest Element

 

The habitat of this floral assemblage is probably not
often recorded in the sedimentary record, although it must
be very closely related to the swamp habitat. The
characteristic plants in this group are Sequoia,

Liquidambar, Carya, Rhus, and Osmunda. Also consistently

 

 

associated with these are members of the families
Araliaceae and Sapotaceae. These pollen of these inferred
associations are best seen in samples of carbonaceous,
micaceous, siltstone facies, as well as being present to
some degree in the lignitic coaly facies. Samples 22, 32,
and 41 show these relationships. This element is
comparable with the "Sequoia Wald" of the German brown
coals, (Neuy-Stolz, 1958) although none of the samples
studied in this report are thought to be from within the
forest itself, as those of the brown coals are supposed to
be. This probably results in an admixture of larger
numbers of pollen and spores from other parts of the flora,
and a less well defined "Sequoia forest" assemblage.
Spores of the family Polypodiaceae are often abundant in
Samples containing a wet forest element, and probably were
associated with these plants in life, but were not

restricted to that habitat. Sample 24 shows an assemblage

83
which contains significant amounts of pollen characteristic
of both the swamp and wet forest elements, as well as an
abundance of Pollenites constans, a pollen of unknown
affinity. The facies of Sample 24 is lignitic siltstone,
with leaves and stems common, but contains Significant

numbers of microplankton as well, and it probably represents

a depositional area with both swamp and wet forest in close

proximity.

Mesic Forest Element
This very broad grouping is comprised of a number of
generally temperate plants whose identities are based on
pollen types which frequently occur together in the
abundance profiles. The most characteristic genera are
Ilex, Tilia, Ulmus, Quercus, and Castanea. Also often

associated in the counts are members of the Polypodiaceae,

Schizeaceae, Sapotaceae, and Bombacaceae. The habitats

occupied by this group were probably removed from the
depositional sites and the unique identity of this element
is not well defined. Those samples of supposed nearshore,
environments (especially Samples 23, 25, and 47) which

received considerable quantities of allochthonous sediments,
lIrobably give the best representation of this element. The
enssociation would appear to contain several typically
teEmperate deciduous genera, although the Species may well
“of: have been restricted as summer green deciduous trees.

'A tHemperate element of the sort described here has been

demOnstrated in other lower Tertiary microfloral studies

84
(Sharp, 1951; Gray, 1960; Jones, 1962; Engelhardt, 1964).
Common forms of the element are also discussed by Neuy-
Stolz (1948) from the Rhine Valley, although that author
does not recognize the association as such within the
brown coal environment. Pollen of the genera.Pipp§_and

Podocappus are frequently associated with the mesic

 

forest element, and it is possible that these trees

occurred within the general habitat area occupied by this

element.

Montane Element

This element is postulated to account for the frequent
association of the coniferous genera Pinus, Abies, Tsuga
and Pippa, Pollen of pine and spruce are often ubiquitous
in sedimentary environments, but their most significant
percentages are in samples which represent offshore marine
depositional sites. This element is the most remote from
the depositional environment, and consequently very little
can be said regarding the nature of the plant association.

One further association must be mentioned. Pollen
thought to represent Platanus and Salix_are significant
contmdbutors to the microflora at several horizons, and are
generally abundant throughout the section. These plants
probakfly occupied streamsides and lowland habitats in
Cor“Siderable abundance. Their proximity to the streams
pPObablyaccounts for the consistent representation in all
but"Che closed swamp environments. Other plants,

partioularly the ferns, may also have been similarly

85
distributed, and their fairly high abundance may be a
reflection of the ease with which their Spores and pollen

were incorporated in the sedimentary load of the streams.
Areal Distribution of the Floral Elements

Figure 12 is an idealized diagram of the study area,
Showing the postulated floral distribution. The slope
represents an ecological gradient in which many
environmental factors were operative, but along which water
relationships and/or altitudinal effects were dominant
factors.

The swamp element probably occupied rather extensive
areas of a coastal plain. It represents an area of low
relief, near sea-level, and subject to periodic inundation
by marine waters as the result of isostatic or eustatic
fluctuations. A swamp habitat existed also within the
postulated delta complex, occupying interdistributary areas
and abandoned channels. This environment is probably
represented by some of the lignitic and coaly facies, where
channel cuts filled with sand, often containing large logs,
are associated with the coals and lignitic horizons.

The wet forest element probably occupied areas adjacent
‘to the swamps. These areas might have included floodplains,
liarge levees in the delta complexes, and more stable areas
IAIithin the swamps. The pollen of the supposed plants of
tilis element is not abundant, and it may have had a rather

Peestricted distribution in the area.

N_ ”HEDGE

 

mmomrmzmmma. ._<zo_._.<._.m_om> mo_.<_2
n_o zo:.:m_m._.m_o oucmmaz.

 

 

 

 

5.5....—
hmmmomrwzflrzo—z hmmmomr 8mm: chum—mam .53 Hmumouwrmza‘gm szEs—
i lI
fl I. 4. O _ 0 0 J O 0 M
A.
$0
O/VA /V.
aka/cow...
)AWOYO
a ..ng , .
. l... I.“ \> 3 u 00 /o
u ... a -.. ... I. & 0%
.l W N nV x. v»
._ 3‘ V at 2
fig. ...v a. at.
.VU. ..V 0 ‘0
_ ,“_‘ V ( 0 \/
MB. < 6.. 0 b
. Q.“ /.o $0k0 )V
...? \ J .V IV «0
4 . m. a
. s 0
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e
3
ac

 

masses

87

Interfingering with these elements was the mesic
forest assemblage. It is postulated that this element
occupied extensive areas of upland, grading into both the
wet forest and the montane habitats. During certain periods
of time in the geologic history of the area, this mesic
assemblage was probably widespread as either the range of
the swamp or montane flora was restricted by tectonic
activity.

The distribution of the montane element was probably
zalong the flanks of the early Tertiary counterpart of the
(Sascade Ranges. The relief in that region is not known,
lout the degree of orogenic activity described by Misch

(1952) probably created mountains of considerable magnitude.
Summary of Environmental Conditions

The composition of the early Tertiary flora within

Tikle area, based on the pollen—spore assemblages, indicates
£1 ssignificant subtropical or tropical representation in the
i73Lc>ra, as well as major contributions by temperate plants.
33flxe frequent occurrence of the subtropical-tropical pollen
types in the coaly and lignitic facies, indicates that the
1333.23nts which produced the pollen were primarily indigenous
Zi¥r1 the low-lying coastal area. The interfingering of the
ITleadrfiine and non—marine rocks in the upper part of the
I“jeeference section is evidence of a near—shore position and
Itzljfe low relief of the area. To the east, the early Tertiary

(leafsczade Ranges provided a more temperate habitat in an

88

upland or even mountainous area. It is probably most
accurate to describe the climate as sub-tropical, with the
mountainous areas showing altitudinal zonation comparable
to latitudinal belts assigned to the cool temperate or
boreal realm (Dansereau, 1957, pp. 101-106). The
mountainous regions of Central America might provide an
analgous climatic situation. Sharp (1951), Engelhardt
(1964) and Gray (1960) have compared the floral assemblages
of some Gulf Coast Eocene rocks with that of the eastern
slope of the Sierra Madre of Mexico. Many temperate genera
are present in the upland areas, coniferous trees are growing
in the mountains, and a tropical element occupies the swampy
coastline.

Several lines of evidence indicate a wet climate. The
presence of extensive swamps indicate a high water table
and ample supplies of surface water. The inferred presence
of delta complexes, and the massive quantities of
allochthonous sediments, some quite coarse, indicate an
extensive drainage development. The rivers were probably
large and their discharge high in order to accommodate
heavy sedimentary loads, perhaps due to high rainfall in the
hinterland areas. The early Tertiary Cascades may well have
operated as a moisture barrier much as the modern day
Cascades do. The pattern of onshore flow of moist air may
have been very different from today, but with marine
conditions prevailing to the west, and a mountanous region

to the east, a very wet belt could be developed.

89

The marine fauna of the McIntosh and Skookumchuck
Formations has been characterized as being sub—tropical
(Van Winkle, 1918; Effinger, 1938). Also, Brown (in
Roberts, 1958) and Wolfe (1961) indicate a tropical to
sub-tropical environment for plant megafossils collected
from rocks of the Puget Group to the north and equivalent
in age to the Skookumchuck Formation in part. These plants
have been listed previously.

The evidence thus suggests that a warm, humid, sub-
tropical climate prevailed in southwestern Washington in
early Tertiary time. No evidence for a change in that
general climate is indicated during Eocene or earliest
Oligocene time. Many minor fluctuations must have occurred,
but no trend toward the modern wet, cool temperate climate
of the area today was seen. The plants of a temperate
climate were present in the higher elevations, and with a
gradually cooling climate, the distributional range of
that element would expand, causing a conspicuous alteration
in the pollen abundance relationships. At some higher
horizon in the Tertiary section, these changes in the pollen

abundance as well as qualitative changes, should be apparent.

PART IV: SUMMARY AND CONCLUSIONS

This study was undertaken to establish a relative
chronologic framework for the lower Tertiary sedimentary
rocks of western Washington, and to evaluate the
composition, distribution, and environmental conditions
of the early Tertiary flora. Six outcrop sections were
chosen for study, providing a north—south and an east-
west cross section of the area. The cross sections
intersect at the location of the most complete rock
sequence in the area, the Stillwater—Olequa Creeks section.
Four of the sections represented type sections of the
lithologic units under consideration, and the remaining
two had been previously measured in detail.

From the field relationships, and from published data,
a composite reference section was established. The
Stillwater-Olequa section contains 8,000 feet of Middle and
Upper Eocene strata, but an unknown amount of the section is
missing at the top as evidenced by the unconformable
contact with the overlying Oligocene strata. The lower
member of the Keasey Formation provided a rock record for
at least part of this gap.

From an analysis of 50 samples in the reference section,
53 stratigraphically limited palynomorphs were found. The
Vertical distribution of these provides a five part
Zonation of the refernence section. By comparing the
Palynological assemblages in the other sections with the
r’ef'erence, a biostratigraphic correlation was achieved.

90

91
The Skookumchuck section contained 36 palynomorphs in
common with the reference section. The Chehalis River
section contained 40 of the 53 stratigraphically significant
forms. 39 correlative types occurred in the Willapa River
section, and 9 in the McIntosh Lake section.

In addition, ten long ranging palynomorphs were
recognized in the reference section whose uniform
distribution in all facies indicated that quantitative
relationships among them might be of stratigraphic value.
Relative abundance profiles for these ten forms were
established in the reference section. Individual sample
Spectra were then compared from the other sections, and
correlations made. This provides a further refinement of
the correlation within the qualitative zones. Seven of the
ten forms showed a distributional pattern that was almost
entirely independent of depositional environment. The
depositional environment is indicated by the rock facies,
the ratio of microplankton to fungal remains, and the ratio
of the sum of ten selected forms to all other spores and
pollen. The time correlations are shown to cross facies
boundaries. In the east-west cross section non—marine
rocks in the Stillwater—Olequa section are correlated with
marine rocks in the Willapa River section. Coal of the
Skookumchuck section correlates with lignitic siltstones
in the Stillwater-Olequa section, shown in the north-south
Cross section.

In all, 112 palynomorph species are identified belonging

 

92
to 60 genera in 46 families. These are selected forms and
represent only about one third of the total number
differentiated in the course of the study. Fourteen of the
identified genera or families are today subtropical or
tropical in distribution. Twenty taxa are mostly temperate,
but with subtropical representatives, and seven are wholly
temperate or boreal. A list of 58 taxa based on leaf
fossils was made from published data relating to the same
general stratigraphic and geographic locality as this study.
Almost all of the taxa represented by leaves are tropical-
subtropical plants. Twenty three taxa as interpreted by
the presence of dispersed spores and pollen presumed to
have affinities with those taxa, are present which also are
represented by leaves or wood.
The identified forms were grouped into 41 classes and
‘the relative abundances computed by a fixed sum population
Cxount of 200 grains. From the abundance profiles of these
EH?oups, significant quantitative associations are apparent.
133’ relating the associations with the depositional
e'nvironment of the samples and to the geologic setting of
‘tflee area, the distributional patterns of the plant
aSsociations was interpreted. Four major forest types were
Pee(Zognized, based on the observed quantitative relationships,
t;}1€3 sample facies, and analogous modern plant communities.
{IPIIEE four assemblages are swamp forest; wet forest; mesic
'i?c>l?est; and montane forest.

From the results of the study summarized in the foregoing

 

 

93

paragraphs, the following conclusions seem justified:

l.

The plant microfossils contained in the lower Tertiary
rocks of the study area possess qualitative and
quantitative characteristics which permit a biostrati—
graphic zonation to be established.

The zonation is laterally correlative in southwest
washington and northwest Oregon, and can probably be
extended beyond that region.

Depositional environment does not affect the identifi—
cation of the biostratigraphic zones. This fact
suggests the possibility of detailed paleogeographic
studies which include the extensive non—marine deposits
lying to the east, adjacent to, and within the Cascade
Mountains.

The McIntosh Formation shows an on-lapping relationship
with the Crescent Formation in the east-west cross-
Section. This indicates that the Willapa Hills
structural high was present during late Eocene time,
and was probably a source for some of the sediments of
the lower part of the McIntosh Formation to the north
and east.

The Skookumchuck Formation represents a regressive
phase of deposition in Late Eocene time. The
disappearance of marine conditions was general in the
area, and was culminated by uplift and erosion of the
underlying sediments. The uplift may have been fairly

localized near the volcanic highs, and deposition

94
seems to have been continuous in some areas (Rock
Creek section).
Considerable relief exists along the unconformity at
the base of the Lincoln Formation. If the correlative
time lines within the studied section were extended
and used as a datum, a clearer picture of the pre-
Lincoln surface could be obtained.
The flora occupying the land areas adjacent to the
depositional sites was very diverse. The swamps
supported forests comparable to the Taxodium Nyssa
swamps of southwestern United States, or the open
everglades-type vegetation. Wet habitats adjacent to
the swamps were occupied by a forest of Sequoia,

Quercus, Ilex, Araliaceous plants and others. The

 

drier upland held a forest perhaps in part comparable
to that of the southern Appalachian Mountains, with

Tilia, Liquidambar, Pinus, Podocarpus, Quercus,

 

Juglans and many others. The mountainous regions
postulated to the east supported a coniferous flora

in part, with Abies, Picea, and Tsuga present.

 

Many plants are represented by leaf or wood fossils
which are not represented by pollen or Spores, and the
reverse is also true. Likewise, a large part of the
flora is probably not preserved at all, especially
those plants growing outside of the depositional

environments.

The climate was tropical to subtropical in the lowland,

10.

ll.

95

more temperate in the areas of higher elevation.
Water stress was probably not a factor in the
environment, with ground and surface water, as well
as atmospheric moisture abundant.

No significant Shift in the climatic conditions is
apparent during the time represented in the composite
reference section. The beginning of such a shift may
be reflected in the uppermost part of the section,
however, where the range of the alpine forest element
Shows signs of expanding as indicated by increased
abundance of the pollen of those plants.

Further investigation into the Tertiary microfloral
record of the area would prove fruitful. The quality
and quantity of the plant microfossils, and their
demonstrated usefulness in stratigraphy and
paleoecology, indicate a high probability of success

for such studies.

PART V: SYSTEMATIC SECTION

The purpose of this section is to provide taxonomic
names and references for the pollen and spores utilized in
the preceding sections of this paper. A rigorous taxonomic
treatment is not attempted, and no new names are proposed,
although some are altered. The application of published
names and their references should provide a means for
wider application of the data contained in this paper by
other workers, even though there may be disagreement over

the validity of the name applied.

Nomenclature

 

A few comments regarding the names used in this paper
are worthy of mention, although the knotty problem of
Tertiary palynological nomenclature has been discussed at
length by Potonie (1958 and 1960), Traverse (1955, 1956,
and 1961), Krutzsch (1959) and many others. First, it is
necessary to be aware that of the 300,000 plus described
plant Species in the world today, practically none possess
a morphological description of their pollen or spores as
part of the original diagnosis, and the pollen or spores of
relatively few taxa have been studied subsequently. This
Situation is being remedied by the work of Wodehouse,
Erdman, Selling, Ikuse, Cookson and Lecompte, to mention
only a few workers in modern pollen morphology, but the
pace is not rapid. Many hundreds of species of described

plants are totally unknown as regards their pollen

96

97

morphology, not to mention the number of plants not yet
described even as sporophytes. This naturally places a
limitation on the degree of confidence with which one may
assign fossil pollen to extant taxa. This is not to say
that many plant taxa may not have pollen morphological
characters which allow them to be identified on that basis
alone, but it does mean that the uniqueness of the pollen
morphology in many taxa is not established. It follows
then, that the assignment of a new species, defined solely
on pollen morphology, to an extant genus, may lead to an
enlargement of the genus which is unwarranted. It is not
reasonable that a new species of modern plant would be
adequately described taxonomically by a complete
eleucidation of its pollen. As Potonie (1958, p. 38)
points out, if a genus is defined by a type species, based
on a sporophyte holotype, it is not reasonable to add a new
species to that genus which is based on a spore or pollen
holotype. The name is a means of referring to a specific
category, and the description and classification of that
category could well carry whatever information the data
reasonably allows as to botanical affinity. In this study,
the floral and environmental descriptions have utilized the
names of extant plant taxa, but those names have applied to
the inferred sporophytes. The Sporophytes are an analytical
interpretation based on the empirical presence of pollen
and spores which are classified by their similarity to

their Similarity to known forms. This is in no way affected

98
by the valid taxonomic names applied to the specific pollen
or spores.

In this study, the validity of the names utilized in
publications is not generally challenged, and only slight
changes have been made to maintain consistency. The names
are based largely on Potonie's work (1960), but other
references are utilized as well. Published illustrations
and descriptions were used, and no type specimens were
examined. The catalog of Fossil Spores and Pollen
published by Pennsylvania State University has been helpful
in this effort, although original references were available
for most species. The descriptions are arranged in a broad
morphological form classification following the Turma and
Subturma of Potonie. The abundance notations in the

descriptions have the following approximate values;

very abundant >~25 per 1000
abundant 10—25 per 1000
common 5-10 per 1000
uncommon 3- 5 per 1000
rare .< 2 per 1000

Lppation and Collection Information

 

Each specimen described carries a reference to a slide
and position on the slide. The coordinates are from the
stage of a Leitz Ortholux microscope. The latitude
Coordinate is given, followed by the longitude. Conversion

to other stages can be accomplished by reference to one of

three index slides marked with an "X". The coordinates of

99

the index are marked on the slide, and a conversion factor
for all readings can be obtained by taking the difference
between the corresponding readings on the index slide and
those of the new stage. The difference is then added to

the coordinates given for a specimen (one may add a negative
number in some cases). If the scale direction is opposite

on the second microscope an additional negative sign is
involved, in which case additions may change to subtractions.
Close attention to the signs avoids confusion (Traverse,
1955).

Each slide is complete with a collection and a
maceration number. The collection number refers to the
section and sample position in the field, the maceration
number refers to the laboratory preparation schedule. All
rock samples processed in the Michigan State University
Palynological Laboratory are prefixed by the letters Pb
(Paleobotanical), followed by a number. By reference to
the master file, the collection site, age, lithology and
preparation procedure for each sample can be obtained.
Vials containing the sample residues, and slides of
illustrated specimens are on file at Michigan State

University.

lOO

FERN SPORES
Genus POLYPODIISPORITES Pot., 1934
Polypodiisporites cf. faypp_Pot., 1934
(Plate 8, Figures 2 and 3)

The comparison with P. favus is close, however, the
illustrated form generally possesses slightly larger
verrucae. The botanical affinity is probably with the
family Polypodiaceae, and this species comprises a large
part of the percentages shown under that heading in
Figure 11.

Occurrence: Common throughout section, one of the
most abundant spores represented.

Location: Pb 3801 5 ; 38.0 x 119.3 (Fig. 2)

Pb 3802 7 ; 38.2 x 120.4 (Fig. 3)

Code: Mlver-4

Polypodiisporites sp. 1
(Plate 1, Figure 1; Plate 8, Figure l)

The affinity of this species with Polypodiaceae is
not certain. The exine is very thick, in some cases,
appearing to result from a fusing of distally expanded
Clavate projections in a tectate fashion.

Occurrence: Generally rare, but most frequent

occurrence in Zone A.

Location: Pb 3809 6 ; 45.9 x 124.2 (Pl. 1, Fig. l)
Pb 3805 5 ; 45.0 x 124.9 (Pl. 8, Fig. 1)

Code: Mlver-7

101

TRILETE SPORES
Genus LAEVIGATISPORITES Pot., 1931

Laevigatisporites cf. pseudomaximus Pf., in Thom. and Pf., 1953

 

 

(Plate 8, Figure 7)

This species bears a close resemblance to Cyathidites

 

australis Couper, 1960, although it is less angular in

 

outline. The botanical affinity may be with the genus
Cyathia. The comparison with L. pseudomaximus is very close.
Location: Pb 3883 6 ; 47.8 x 122.8

Code: Tlsm-ll

Genus OSMUNDACITES
Osmundacites wellmanii Couper, 1953
(Plate 6, Figure 1; Plate 8, Figure 11)

This species is one of the more common spores in the
samples studied. It almost certainly represents the genus
Osmunda, and it comprises the total percentages of that
type shown in Figure 11. Baculatisporites gemmiculavatus
Pot., 1934 is a very similar species.

Occurrence: Common to abundant, ranges throughout the
section.

Location: Pb 5622 l ; 59.0 x 119.0 (Pl. 6, Fig. 1)

Pb 3832 5 ; 35.5 x 118.2 (Pl. 8, Fig. 11)

Code: Tlgm—l

102

Genus CICATRICOSISPORITES
Cicatricosisporites cicatricosoides Krutzsch, 1959
(Plate 8, Figures 5 and 6)

The botanical affinity of this species is thought to
be with the family Schizeaceae, possibly the genus Anemia.
It comprises a small percentage of the Schizeaceae profile
in Figure 11.

Occurrence: Rare, though it occurs consistently
throughout the section.

Location: Pb 3811 l ; 39.0 x 121.9

Code: Tlclc-l

Cicatricosisporites cf. hallei Delcourt and Spurmont, 1955
(Plate 6, Figure 6)

This species probably also has affinities with the
Schizeaceae. It comprises most of the percentage of that
group in Figure 11. The comparison with C. hallei is very
close, differing only Slightly in the size of the ridges on
the distal side of the spore.

Occurrence: Generally fairly common, and very
<30nsistent throughout the section and in various facies.

Location: Pb 5621 4 ; 43.0 x 115.0

Code: Tlclc—3

 

\...-L

 

103

Genus TRILITES (Erdman; Cookson) Couper, 1953

Trilites asolidus Krutzsch, 1959

 

(Plate 6, Figures 2 and 3)
The botanical affinity of this species is probably the
family Schizeaceae, and it resembles quite closely spores of

the genus Lygodium.

 

Occurrence: Generally common and very consistent
throughout the section in various facies.
Location: Pb 3874; 30.6 x 121.6

Code: Tlfos-l

Trilites cf. paravallatus Krutzsch, 1959

 

 

(Plate 8, Figure 4)

The comparison with T. paravallatus is tentative. The

 

botanical affinity is unknown, but it is similar to some
Schizeaceae, and it was included in the counts of Figure
11 under that heading.

Occurrence: Rare in the samples studied.

Location: Pb 5617—3; 42.0 x 116.5

Code: Tlfov-l

104

Genus POLYPODIACEOISPORITES Pot., 1951
Polypodiaceoisporites sp.
(Plate 8, Figures 8 and 9)
The botanical affinity of this species is not known.
It compares well with the diagnosis of the genus
Polypodiaceoisporites, but shows no close relationship with
any described species of the genus.
Occurrence: Rare, occurs sporadically throughout
section.
Location: Pb 3843 2 ; 35.5 x 120.7

Code: Tlfos-3

Genus FOVEOTRILETES (van der Hammen) Pot., 1956

Foveotriletes crassifovearis Krutzsch, 1959

 

(Plate 8, Figure 10)

The botanical affinity of this species is unknown. It
may prove to be an excellent marker within the lower
Tertiary.

Occurrence: Rare, although it occurs consistently in
the upper part of the section.

Location: Pb 3838 6 ; 54.0 x 111.2

Code: Tlfov—2

105

Genus CONCAVISPORITES
(Thom. and Pf.) Delcourt and Spurmont, 1955

Concavisporites minimodiversus Nagy, 1963
(Plate 8, Figures 12 and 13)
The botanical affinity is unknown. It is included in
the percentages of the "other spores" class of Figure 11.
Occurrence: Generally rare, most frequent in upper
zones.
Location: Pb 3804 6 ; 43.2 x 110.3

Code: Tlsm-l6

Concavisporites minimus Krutzsch, 1952
(Plate 4, Figure l)

Gleicheniidites apilobatus Brenner is a very similar
form. The affinity of this type may be with the family
Gleicheniaceae, although it is not certain.

Occurrence: Rare, but it occurs consistently in
Zones D and E.

Location: Pb 3883 4 ; 52.2 x 121.4

Code: Tlsm-lO

Genus BACULATISPORIS Thom. and Pf., 1953

Baculatisporis cf. baculatus Krutzsch, 1959

 

(Plate 5, Figure 1)
The botanical affinity of this grain is not known, but

143 may represent the family Osmundaceae. The comparison

WithB. baculatus is only tentative.

 

Occurrence: Rare to fairly common, especially in Zone E.
Location: Pb 3839 l ; 45.7 x 127.3
Code: Tlg-l

106

GYMNOSPERMOUS POLLEN
SACCATE POLLEN
Genus ABIETINEAEPOLLENITES Pot., 1951
Abietineaepollenites microalatus (Pot.) Pot., 1951
(Plate 6, Figure 5)

This is the Pinus hapoxylon-type of Thiergart. It
appears in the percentages of Pippp, Figure 11, and was
utilized as a stratigraphic form in the abundance counts
of Figure 6.

Occurrence: Fairly common throughout the section.

Location: Pb 5618 4 ; 38.2 x 114.1

Code: V2-4

Genus ABIESPOLLENITES Thiergart, 1937
Abiespollenites cf. absolutus Thiergart, in Raatz, 1937
(Plate 9, Figures 1, 2 and 3)

The affinity of this species with Api§§_is not certain,
but it resembles pollen of that genus closely. The
comparison with A. absolutus is close, and examination of
the type would probably allow reference of the illustrated

form to that species.

Occurrence: Rare to common, generally throughout the

section.

Location: Pb 3804 6 ; 40.5 x 110.0 (Fig. 1)
Pb 5617 3 ; 49.0 x 125.0 (Fig. 2)
Pb 5618 4 ; 38.2 x 115-7 (Fig. 3)
Code: ‘V2-1

107

Genus PICEAPOLLENITES Pot., 1931
Piceapollenites sp.
(Plate 4, Figure 2)

This type is very similar to modern Pigga_pollen. It
probably represents more than a single species, but all
Specimens fall under the generic diagnosis and are
distinguished from Abiespollenites by the relatively thin
proximal cap, the fine texture of the body ornamentation,
and the characteristic attachment of the bladders.

Occurrence: Generally common, especially in and above
Zone D.

Location: Pb 3883 4 ; 40.2 x 115.0

Code: V2—5

Genus PODOCARPIDITES (Cookson) Couper, 1953
Podocarpidites sp.
(Plate 6, Figure 4; Plate 9, Figure 4)

The affinity with modern Podocarpus is almost certain

 

for this pollen, although again several species may be
represented. This form represents most of the counts shown

in the abundance graph of Figure 6 under Podocarpidites.

 

Occurrence: Rare to common, throughout the section.
Location: Pb 3838 5 ; 52.5 x 123.2 (Pl. 6, Fig. 4)

Pb 3871 1 ; 35.1 x 120.0 (Pl. 9, Fig. 4)
Code: V2-3

108
NON-SACCATE POLLEN
Genus TAXODIACEAEPOLLENITES Kremp, 1949
Taxodiaceaepollenites hiatus (Pot.) Kremp, 1949
(Plate 9, Figures 6 and 10)

The affinity of this species is thought to be Taxodium,

 

although other genera (Sequoia, Metasequoia, Cryptomeria)

 

also have similar pollen. This species comprises most of
the percentages shown for Taxodium in Figure 11, although
some Sequoia, etc. may also be included.
Occurrence: Generally common throughout section.
Location: Pb 5616 l ; 57.9 x 122.5 (Fig. 6)
Pb 3892 3 ; 32.3 x 111.6 (Fig. 10)
Code: Isc—l

Genus TSUGAEPOLLENITES Pot. and Ven, 1934

Tsugaepollenites viridifluminipites (Wodehouse)
Thom. and Pf., 1953

(Plate 4, Figure 3; Plate 9, Figure 5)

This species bears a close resemblance to pollen of
Tsuga heterophylla, although other species of the genus
have similar pollen. Only one species was recognized in
the samples studied, and this comprises the total count
shown in Figure 11.

Occurrence: Rare, but occurs consistently in and
above zone D.

Location: Pb 3896 2 ; 45.9 x 126.1 (P1. 4, Fig. 3)

Pb 3892 1 ; 39.0 x 118.0 (Pl. 9, Fig. 5)

Code: Vl-l

109

Genus SEQUOIAPOLLENITES Thiergart, 1937

Sequoiapollenites sp.

 

(Plate 9, Figure 9)
The affinity of this pollen with Seguoia is not

certain. Metasequoia has very similar pollen and is

 

represented in fossil floras of the study area by leaves
and cones. Specimens of this genus may have been referred

to Taxodiaceaepollenites if the distinctive recurved papilla

 

was not apparent.
Occurrence: Rare, occurs throughout the section, but
is most abundant in some lignitic siltstone facies.
Location: Pb 3872 3 ; 37.5 X 110.4

Code: Isc-2

llO

ANGIOSPERMOUS POLLEN

 

MONOSULCATE POLLEN
Genus SABALPOLLENITES Thiergart, 1938

Sabalpollenites cf. convexus Thiergart, 1938

 

(Plate 9, Figure 8)
This species represents the palm family, and possibly

the genus Sabal. The comparison with S. convexus is

 

tentative, the illustrated form being somewhat larger, and
with a finer reticulum.

Occurrence: Rare to common, throughout section, but
with highest frequencies occurring in some coals.

Location: Pb 3873 1 ; 45.3 x 122.8

Code: Slr—l

Genus LILIACIDITES Couper, 1953

Liliacidites intermedius Couper, 1953

 

(Plate 6, Figure 10)

This species is similar to Sabalpollenites cf.

 

convexus, but is generally larger and is more coarsely

 

reticulate. The affinity is thought to be with the family
Palmae, and may also represent the genus Sabal, This
species comprises most of the percentage under Palm in
Figure 11, and it is included as one of the ten types in

the fixed area counts shown on Figure 6.
Occurrence: Rare to common, throughout section,
especially common in some coals.

Location: Pb 3872 3 ; 49.0 x 122.0
Code: Slr-2

111

COLPATE AND COLPORATE POLLEN
Genus CUPULIFEROIPOLLENITES Pot., 1951

Cupuliferoipollenites cf. pusillus Pot., 1951

 

(Plate 10, Figure 7)

Affinity with the family Fagaceae is suggested,
particularly the genus Castanea. The pore structure is
generally well developed and serves to distinguish this
type from the similar forms referred to the genus

Castaneoidites.

 

Occurrence: Rare to common, but it occurs most
frequently in nearshore sediments.
Location: Pb 3828 5 3 39.6 x 113.8

Code: CP3sc-l

Genus QUEROIDITES Pot., Thom., and Thierg., l95O

Quercoidites henrici (Pot.) Pot., Thom., and Thier., l95O

 

(Plate 3, Figure 2; Plate 9, Figures 7 and 11)

This species is the most abundant single Species
represented in the samples. Its botanical affinity is
almost certainly Quercus and it accounts for a large part
of the percentages under that class in Figure 11. More
than one species of Quercus may be represented by this
pollen type, but at least one of the possible species grew

as a swamp tree. Large numbers of Quercus-like pollen
have been noted in several other early Tertiary microfloral

assemblages (Traverse, 1955; Nuey—Stolz, 1958).

112
Occurrence: Common to very abundant, especially in
some lignite and coal samples.
Location: Pb 3837 6 ; 38.8 x 125.7 (P1. 3, Fig. 2)
Pb 3892 l ; 30.0 x 111.5 (P1. 9, Fig. 11)

Pb 3897 4 ; 36.6 x 118.9 (P1. 9, Fig. 7)
Code: C3sc-1

Querocoidites sp. 2

 

(Plate 4, Figure 12)

This species is included in the Quercus percentages of
Figure 11, although its contribution is small. The
botanical affinity with Quercus is not definite, but the
general morphology is suggestive of that genus. In general,
the pores are weakly developed, and it may be sometimes
confused with Q. henrici.

Occurrence: Generally rare, but very consistent in
Zone D.

Location: Pb 3806 2 3 32.8 x 110.8

Code: CP3v—l

Genus PLATANOIDITES Pot., Thom., and Thierg., 1950

Platanoidites sp.

 

(Plate 9, Figures 17 and 18)
The botanical affinity of this species is not certain,

but it probably is with the genus Platanus, at least in

 

part. Leaves of Platanus are commonly found in equivalent

 

age rocks in the study area-

113

Occurrence: Common to abundant in many samples,
especially in marine sediments, both near and offshore.
The very small size of these grains probably accounts in
large part for their wide and abundant dispersal.

Location: Pb 3875 4 ; 42.8 x 121.3 (Fig. 17)

Pb 3896 2 ; 42.0 x 108.0 (Fig. 18)
Code: C3r—12

Genus ARALIACEOIPOLLENITES Pot., 1951
Araliaceoipollenites cf. edmundi (Pot.) Pot., 1951
(Plate 10, Figure 10)
The comparison with A. edmundi is very close, although

A. euphorii is also similar. This species, together with

 

Tricolporopollenites satzveyensis, comprise the Araliaceae
percentages in Figure 11. The species is common in the
lower Tertiary of central Europe. Leaves assigned to the
genus Aralia have been recorded from the Eocene rocks of
the study area, although pollen with affinities to the
family have not been commonly recorded in North America.
Stanley (1960) illustrates a form similar to this species,

and refers to it as Tricolporopollenites problematicus.

 

Occurrence: Rare to fairly common, consistently
occurring in nearshore carbonaceous siltstones.

Location: Pb 5621 4 ; 52.0 x 114.0

Code: CP3f0v-l

 

114

Genus CASTANEOIDITES Pot., Thom., and Thierg., 1950
Castaneoidites cf. exactus Pot., Thom., and Thierg, 1950
(Plate 9, Figure 12)
The comparison with C. exactus is very close, and only
a slightly larger size keeps it from being referred directly
to that Species. The botanical affinity of this type appears
to be with the family Fagaceae, and possibly the genus

Castanea. The species Castanea minutapollenites Rouse, is

 

a very similar pollen, perhaps identical.

Occurrence: Common to abundant in almost all samples
studied, but especially abundant in some samples containing
high frequencies of Quercus-like pollen.

Location: Pb 3829 5 3 34.2 x 111.0

Code: C3sm-l

Genus ILEXPOLLENITES Thiergart, 1937

Ilexpollenites iliacus (Pot.) Thierg., 1937

 

(Plate 1, Figure 6; Plate 9, Figure 14)

This species has commonly been recorded from Tertiary
deposits in North America and Europe. The botanical
affinity appears to be with the genus 11%;, and I. iliacus
contributes a large part of the percentages under gig; in
Figure 11.

Occurrence: Common to abundant in nearly all samples
studied.

Location: Pb 6320 1 ; 41.3 x 118.0 (P1. 1, Fig. 6)

Pb 5617 3 ; 50.0 x 118.0 (P1. 9, Fig. 14)

Code: C3cl-1

115

Ilexpollenites inaequaliclaviata (Traverse) Pot., 1960

 

(Plate 6, Figures 8 and 9)

This species is less common than I. iliacus, although
it is a major pollen type represented in the section. The
botanical affinity is probably with the genus Ilgx.

Occurrence: Rare to common, occurs throughout the
study section.

Location: Pb 3877 4 3 29.8 x 114.0

Pb 3883 4 3 40.7 x 115.7

Code: C3c1—2

Ilexpollenites cf. marginatus (Pot.) Raatz, 1947

 

 

(Plate 3, Figure l)
The figured specimen is a partially broken example of
the species which is significantly larger than the other
two species of this genus. It is strongly colpate, with no
tendency toward pore development as is seen in other species

of Ilexpollenites. The colpi are long, and are often seen

 

gaping Open. The clavae are generally equal in size, and
extend to the colpi margins.

Occurrence: Rare to common, but occurs only in upper
part of the section.

Location: Pb 3839 1 3 37.5 x 128.2

Code: C3cl-3

116

Ilexpollenites sp.

 

(Plate 3, Figures 12 and 13)

Some illustrations of I. iliacus show a pore structure
similar to this grain, but not generally elongated
equatorially. The illustrated species is distinctly
colporate, although the heavy ornamentation of clavate
projections may obscure the aperture structure in many
specimens. The affinity with the genus Ilex_is not certain,
although some individuals are included in the counts under
that heading.

Occurrence: Rare to common, occurs very consistently
in and above Zone B.

Location: Pb 3875 4 3 38.3 x 120.3

Code: CP3gm-l

Genus TRICOLPITES (Cookson) Couper, 1953

Tricolpites cf. striatus Couper, 1954

 

(Plate 4, Figure 4)

The Specimen illustrated shows a fairly close comparison
with T. striatus. The gross morphology of the grain suggests
a possible affinity with the family Aceraceae, although this
is not certain. This Species is a useful stratigraphic type
even though it is not abundant enough to be included in the
relative abundance counts.

Occurrence: Rare, but it occurs consistently in small
numbers in and above Zone D.

Location: Pb 3805 5 3 40.3 x 119.7

Code: C3st-1

117

Tricolpites sp. 1

 

(Plate 10, Figures 1 and 2)

This species is usually seen in the polar View, with
the colpi long and simple, without longitudinal costae.
Covering the colpus is an endexinous membrane, generally
with a granular texture. The botanical affinity is unknown.

Occurrence: Common in most samples above Zone C,
although rare in lignitic and coaly facies.

Location: Pb 3883 4 3 38.2 x 114.0

Pb 3895 4 3 32.2 x 111.9

Code: C3r-15

Tricolpites Sp° 2

 

(Plate 2, Figures 4 and 5)
The botanical affinity of this Species is not known.
It is useful as a stratigraphic form, and is easily
recognized by its conspicuously spinate exine.
Occurrence: Rare, although it occurs consistently in
Zones B, C, and D.
Location: Pb 3872 3 3 37.0 x 117.4
Pb 3874 4 3 34.9 x 128.0
Code: C3Sp—3

118

Tricolpites sp. 3

 

(Plate 9, Figure 19)

Several species of the genus Protoquercus Bolkhovitina

 

are quite similar to the illustrated form, although the
comparative material was not sufficient to allow placing
this form with that genus. The botanical affinity is not

known, but pollen of some species of modern Platanus is

 

similar. It was included in the Platanus-Salix percentage

 

counts of Figure 11, although it represents only a small
portion of that group.

Occurrence: Rare to common, the Species ranges
throughout section, but its highest frequency occurs in the
lignitic siltstone facies.

Location: Pb 3805 5 3 51.3 x 125.9

Code: C3r-l7

Tricolpites sp. 4

 

(Plate 4, Figures 5 and 6)

The botanical affinity of this species is unknown. Its
large size (ca. 35-40) and heavy, reticulate exine make it
very conspicuous. Some individuals Show a tendency toward
a porate condition, and Engelhardt (1964) figures a similar

form, referring to it as Tricolporopollenites sp. 4.

 

Occurrence: Pb 3883 4 ; 40.2 x 124.9 (Fig. 5)
Pb 5616 1 ; 58.7 x 114.8 (Fig. 6)
Code: C3r-19

119

Genus TRICOLPOPOLLENITES Thom. and Pf., 1953

Tricolpopollenites cf. retiformis Pf. and Thom., 1953

 

 

(Plate 9, Figures 15 and 16)

This Species is included in the counts of Platanus-
Salix in Figure 11. The affinity with Salix_is not certain,
but the morphology suggests that relationship. The
comparison of the illustrated form with T. retiformis is
close, although the illustrated form has a Slightly heavier
reticulum.

Occurrence: Rare to common, especially in some marine
siltstones in the middle part of the section (Zones C and
D).

Location: Pb 3838 4 3 40.0 x 114.9

Code: C3r-3

Genus RHOIPITES WODE., 1933

Rhoipites cf. bradleyensis Wode., 1933

 

 

(Plate 10, Figure 9)
The comparison with R. bradleyensis is close, although
the original illustration is slightly vague. The botanical
affinity is thought to be with the genus Eggs, family

Anacardiaceae. The morphology of Rhus typhina pollen is

 

Similar.

Occurrence: Rare, occurs sporadically throughout
Section.

Location: Pb 5621 4 3 48.9 x 115.0

Code: CP3st-4

 

120

Rhoipites pseudocingulum (Pot.) Pot., 1960
(Plate 10, Figures 14 and 16)

This species probably represents the family
Anacardiaceae, and possibly the genus Eggs, although that
is not certain. Potonie mentions Eggs as the likely
affinity in the original description of the species. The
species is frequently illustrated in studies of Tertiary
microfloral assemblages.

Occurrence: Common in most samples, but the highest
frequencies occur in nearshore marine or brackish water
environments.

Location: Pb 3802 7 3 44.5 x 120.8

Pb 3809 6 3 41.1 x 126.4

Code: CP3sc-2

Rhoipites cf. pseudocingulum forma navicula (Pot.) Pot, 1960

 

 

(Plate 10, Figures 12 and 13)

The comparison with R. pseudocingulum forma navicula is
tentative. Engelhardt (1964) illustrates a nearly identical
form and refers to it as Tricolporopollenites sp. 1. He
Compares it with Acer mullensis Simpson from the Eocene of
Great Britain. The botanical affinity is uncertain, but it
is included in the counts of Figure 11 as Eggs, and
probably represents the family Anacardiaceae, if not Ehgg,

Occurrence: Rare to common, generally throughout the
Sectixmb although it occurs most frequently in nearshore or

braclcish environments.

121
Location: Pb 3872 3 ; 47.8 x 110.1
Pb 3873 1 ; 47.2 x 119.8

Code: Cp3st—2

Rhoipites dolium (Pot.) Pot., 1960

 

(Plate 4, Figure 8)
Nuey-Stolz (1958) relates this Species to the family

Theaceae (as Tricolporopollenites dolium Thom. and Pf.).

 

Potonie (1960) indicates that R. dolium is quite similar

to R. bradleyi, and probably represents the genus Rhus.

 

The figured specimen compares closely with Potonie‘s
original illustrations, but the affinity with Eggs is not
definite. It was not included in the counts of Figure 11
under Rhus,

Occurrence: Rare to common in samples in and above
Zone D.

Location: Pb 3809 6 3 51.8 x 112.2

Code: CP3g-6

Genus CYRILLACEAEPOLLENITES (Murr. and Pf.) Pot., 1960

Cyrillaceaepollenites cf. m§_gaexactus (Pot.) Pot., 196O

 

 

(Plate 11, Figure 11)

The comparison with C. megaexactus appears to be quite

 

close, although the Specimen found in this study are
frequently Slightly larger (25-30). Pollen of Cyrilla has
been reported from other lower Tertiary localities, where

sometimes it is abundant (Brandon Lignite, Traverse, 1955).

122
Occurrence: Generally rare in samples studied, except
in some lignitic siltstones where it was common.
Location: Pb 6320 2 3 44.0 x 117.7

Code: CP3sc-12

Genus FAGUSPOLLENITES Raatz, 1937
Faguspollenites cf. versus Raatz, 1937
(Plate 11, Figure 7)

The comparison with F. versus is tentative. It compares
quite closely with modern F§g2§_pollen, and it comprises most
of the percentage count under that heading in Figure 11.

Occurrence: Rare, although it occurs consistently
throughout the section and is common in some nearshore
siltstones.

Location: Pb 3805 6 3 47.0 x 116.8

Code: CP3sc-7

FaguSpollenites Sp.
(Plate 11, Figure 3)

This species compares quite closely with some modern
Fagg§_pollen (Fagus sylvatica). It is present in many
samples, but in small numbers. It makes up a small portion
of the Fagu§_percentage of Figure 11.

Occurrence: Rare, generally throughout the section.

Location: Pb 3838 6 ; 55.5 x 115.2

Code: CP3g-5

123
Genus TRICOLPOROPOLLENITES Thom. and Pf., 1953

Tricolporopollenites cf. helmstedtensis Pf. in Thom.
and Pf., 1953

 

 

(Plate 3, Figure 9)

The comparison with T. helmstedtensis is quite close,
although the figured species often has a slightly coarser
reticulum in which the lumina are very angular. The
botanical affinity is not established. Pflug (1953)
indicates that this species is a common lower Tertiary
element in Europe.

Occurrence: Rare to common, in and above Zone B, most
frequent in Zone C and higher. Occurs consistently in
nearly all sample types.

Location: Pb 3806 2 3 93.5 x 40.5

Code: CP3r-7

Tricolporopollenites satzveyensis Pf., in Thom. and Pf., 1953
(Plate 10, Figure 11)

T. satzveyensis is regarded by Krutzsch (1957) as a
key lower Tertiary form in central Europe. It is Similar
to Araliaceoipollenites edmundi, and may represent the
family Araliaceae, although it is not certain. It was
counted under the Araliaceae heading in Figure 11, although
its contribution is small.

Occurrence: Rare to fairly common, occurs consistantly
in samples from nearshore and brackish environments.

Location: Pb 5619 l 3 57.8 x 114.0

Code: CP3fov-2

124

Tricolporopollenites cf. macrodurensis Pf. and Thom., 1953
(Plate 3, Figure 7)

The comparison with T. macrodurensis is quite close,
although not certain. The botanical affinity is unknown.
Thompson and Pflug (1953) suggest a possible relationship
with genus Parthenocissus.

Occurrence: Pb 3802 7 3 34.7 x 119.5

Code: CP3r—ll

TricolporOpollenites sp. 1
(Plate 3, Figure 5)

The affinity of this species is unknown. Its small
size and distinct reticulate exine may cause it to be
confused with Platanus-like pollen if the grain is seen in
polar view. In equatorial view, however, the small, round
pore is conspicuous.

Occurrence: Rare, although it occurs consistently in
and above Zone B, in all facies.

Location: Pb 3877 4 3 32.1 x 121.4

Code: CP3r-2

Tricolporopollenites Sp. 2
(Plate 3, Figure 6)
The botanical affinity of this type is unknown. The
coarse reticulum composed of broad lumina and thin, high

muri make this a distinctive form.

 

125
Occurence: Rare to common, especially in nearshore
siltstones in the upper part of section.
Location: Pb 3805 6 3 44.3 x 120.8
Code: CP3r-l2

Tricolporopollenites sp. 3

 

(Plate 1, Figure 14)

The affinity of this species is not known. Its
occurrence is fairly consistent in the lowermost part of
the section, but its range is not definitely established.
The very characteristic striate exine makes it readily
identifiable, even though it is quite small (18-20A).

Occurrence: Rare, a possible key form for Zone A.

Location: Pb 3828 6 3 37.5 x 119.4

Code: CP3st-5

Genus ALANGIACEOIPOLLENITES (Traverse, 1955) n. comb.

Type species: Alangiaceoipollenites (as Alangium)

 

barghoornianum (Traverse, 1955, page 65, Figure 12, photo

1023 ca. 92) n. comb.

Alangiaceoipollenites barghoornianum (Traverse) n. comb.
(Plate 11, Figure 9)

The affinity of this species with the genus Alangium is

 

almost certain. Specimens of Alangium chinense pollen in

 

the reference collection at Michigan State University are
very similar. It is the first known record of this genus

in North America outside of the Oligocene Brandon Lignite,
studied in detail by Traverse (1955). The family Alangaceae

126
is today distributed in the tropics and subtropics of the
old world.
Occurrence: Rare, although it occurs consistently in
and above Zone D, in all facies.
Location: Pb 3805 5 3 48.2 x 117.3
Code: CP3st-4

Alangiaceoipollenites sp. 1
(Plate 4, Figure 7)

This Species is very Similar to A. barghoornianum,
and additional study may Show that the two are really only
one species. The illustrated specimen shows, however, the
finer striate pattern of the exine and the more angular
outline. The botanical affinity of this species is

probably Alangium.

 

Occurrence: Rare, although fairly consistent in Zone
D and above.

Location: Pb 3880 3 3 43.7 x 124.5

Code: CP3st-5

Alangiaceoipollenites sp. 2
(Plate 3, Figure 11)

This species is very similar to Pollenites ortholaesus
Pot., and it is clearly distinct from A. barghoornianum and
.A. Sp. 1, having less well developed annular structure
around the pores, thinner exine, and distinctly foveolate
sculpture. The affinity is assumed to be with the family

Alangiaceae, although it bears a strong resemblance to pollen

127
of the closely related family, Nyssaceae.
Occurrence: Rare to common, especially in and above
Zone B.
Location: Pb 5621 4 3 40.0 x 126.9

Code: C3g-6

Genus NYSSAPOLLENITES Thierg., 1937
Nyssapollenites accessorius (Pot.) Pot., 1950
(Plate 3, Figure 103 Plate 11, Figure 4)

The botanical affinity appears to be Nygga, This
species comprises the major part of the Ny§§a_percentages
of Figure 11. It frequently occurs in association with
Taxodium-like pollen, and is assumed to indicate the

presence of Taxodium-Nyssa swamp conditions during the time

 

of deposition of some lignitic siltstones and coals.

Occurrence: Rare to common, occurs consistently in and

above Zone B.
Location: Pb 3802 7 s 39.6 x 114.1 (P1. 3, Fig. 10)
Pb 3809 6 ; 52.6 x 115.1 (P1. 11, Fig. 4)

Code: CP3g—7

Nyssapollenites cf. thompsoniana (Traverse) Pot., 1960

 

(Plate 11, Figure 5)
This comparison is only tentative. This species is

very similar to pollen of modern Nyssa, and its botanical
affinity is probably with that genus. It is included in

counts of that Species in Figure 11, although its

contribution is small.

128
Occurrence: Rare, generally throughout the section.
Location: Pb 3841 2 3 36.9 x 113.9

Code: CP3g-8

Nyssapollenites sp. 1

 

(Plate 11, Figure 8)
This species is tentatively referred to the genus

Nyssapollenites. It resembles pollen of some members of the

 

family Theaceae (Gordonia), but an affinity with that family
is not certain.

Occurrence: Rare, generally throughout the section
studied.

Location: Pb 5615 1 3 51.0 x 111.5

Code: CP3r-l3

Nyssapollenites sp. 2

 

(Plate 11, Figures 1 and 2)

This species is included in the percentages of the
Nyssa;group in Figure 11, although the affinity with that
genus is not certain.

Occurrence: Rare, occurs only occasionally in lignitic
siltstones in upper part of section.

Location: Pb 5615 l 3 50.0 x 115.0

Code: CP3g-9

129

Genus GOTHANIPOLLIS Krutzsch, 1959

Gothanipollis sp.

 

This species bears some resemblance to Specimens of
G. gothani Krutzsch, although it appears to be distinct
from that species. It appears to be a key form for lower
Tertiary rocks in North America and Europe. The botanical
affinity is unknown.

Occurrence: Rare, although it occurs conspicuously in
most samples above Zone A.

Location: Pb 3832 2 3 46.2 x 113.3

Code: Syn3g-4

Genus CUPANIEIDITES Cookson and Pike, 1954

Cupanieidites cf. orthoteichus Cookson and Pike, 1954

 

 

(Plate 3, Figure 4)
The figured species compares quite closely to C.

orthoteichus, although is somewhat larger (ca. 30) and the

 

exine is usually granular. The natural affinity may be with
the family Sapindaceae, although that is not certain in this
species.

Occurrence: Rare, although it is consistently present
in Zones C and Do

Location: Pb 3837 6 3 44.8 x 127.2

Code: Syn3g—1

130

Cupanieidites sp. 1
(Plate 3, Figure 8)

No comparative illustrations or descriptions for this
Species have been found. It appears to be an extremely
useful stratigraphic form in the samples studied. The
botanical affinity is as yet unknown, but it may well
represent the family Sapindaceae, a nearly pan—tropical
family.

Occurrence: Rare, but very consistent in Zones C and

Location: Pb 3883 6 3 44.1 x 124.2

Code: Syn3r—l

Genus SYNCOLPORITES van der Hammen, 1954

Syncolporites sp. 1

 

This species is very distinctive and easily
recognizable. The botanical affinity is unknown, and no
similar forms have been illustrated from other Tertiary
localities as far as is known. The species is characterized
by the presence of a compound colpus, united at both poles
(syncolpate) and enclosing an island at the poles. This
island extends to the equatorial area, where it is
interrupted by the pore structure. The grains are nearly
always seen in polar view, and the pore is only rarely

observed.

Occurrence: Rare, occurs very consistently, however,

in and above Zone C.

131
Location: Pb 3803 5 3 48.0 x 121.1

Code: Syn3g-2

Syncolporites sp. 2

 

(Plate 2, Figure 2)

This species appears to be closely related to
Syncolporites sp. 1, differing only in that the colpi do
not actually extend over both poles. The botanical
affinity is not known.

Occurrence: Rare, appears to be a key form for Zone C.

Location: Pb 3839 5 3 45.2 x 112.4

Code: Syn3g-2a

Genus SYMPLOCOIPOLLENITES Pot., 1951
Symplocoipollenites vestibulum (Pot.) Pot., 1951
(Plate 3, Figure 14; Plate 11, Figure 6)
This species has been frequently recorded Tertiary
deposits of Europe and North America. The botanical

affinity is thought to be with the genus Symplocos, a

 

tropical to subtropical genus of wide distribution.
Occurrence: Rare to common, occurs consistently in
Samples from Zone C and above.
Location: Pb 3840 6 3 54.0 x 117.6 (P1. 3, Fig. 14)
Pb 3836 5 ; 41.6 x 113.0 (P1. 11, Fig. 6)

Code: C3rug-1

132

Symplocoipollenites sp. 1

 

(Plate 4, Figure 10)

This Species is vaguely similar to Symplocos jacksonia

 

Traverse, described from the Oligocene Brandon Lignite.
Its botanical affinity is very likely with the family

Symplocaceae, although its generic reference to Symplocos

 

is not certain.

Occurrence: Rare, although it occurs consistently in
Zone D.

Location: Pb 5617 3 3 49.7 x 126.8

Code: Prot-5

Symplocoipollenites sp. 2

 

(Plate 2, Figures 8, 9 and 10)

The assignment of this species to Symplocoipollenites
is tentative. Krutzsch (1957) illustrates a similar type
which he calls the "gesperlte vestibuloide formen," and
indicates that the probable affinity is with the
Symplocaceae.

Occurrence: Rare, although it occurs consistently in
samples in Zone B and above.

Location: Pb 5621 4 3 37.0 x 117.9 (Fig. 8)

Pb 3876 4 ; 48.4 x 110.9 (Figs. 9 & 10)

Code: CP3sp-4

133

Genus SAPOTACEOIDAEPOLLENITES Pot., Thom., and Thier., 1950

Sapotaceoidaepollenites cf. sapatoides
(Tom. and Pf.) Pot., 1960

 

(Plate 11, Figures 11, 12 and 13)

The comparison with S. sapatoides is quite close,

 

although in some examples (Figures 11 and 12) the pores
appear more silt—like. This species is almost certainly
related to the family Sapotaceae, but the generic affinity
is not known. The Sapotaceae is a nearly pan—tropical
family today with a distribution reaching highest latitudes
in North America.
Occurrence: Rare, occurs consistently throughout the
section.
Location: Pb 6320 2 3 44.0 x 117.7
Pb 3805 5 ; 56.1 x 126.4
Pb 3873 1 3 50.5 x 120.5
Code: CP4sc-1

Genus BETULACEOIPOLLENITES Pot., 1951
Betulaceoipollenites bituitus (Pot.) Pot., 1951
(Plate 12, Figures 3 and 4)

The morphology is very similar to that of the genus
Betula, and this species was included in counts of that
group in Figure 11. The family Betulaceae is, however,

a difficult one to divide on the basis of pollen morphology
alone, and the genus Betula is only a suggested affinity

here.

 

134
Occurrence: Common to abundant, especially abundant
in some lignitic siltstone samples.
Location: Pb 3875 4 3 47.8 x 121.0
Pb 3809 6 3 48.4 x 110.6

Code: P3sm-2

Genus TRIVESTIBULOPOLLENITES (Pf.) Thom. and Pf., 1953

Trivestibulopollenites cf. salebrosus Pf., 1953

 

 

(Plate 10, Figure 6)

The comparison with T. salebrosus is only tentative.

 

The figured Species is very similar to some members of the
family Burseraceae, and in Figure 11 this type is shown as
a percentage under that heading. The family Burseraceae
is mainly subtropical in distribution.

Occurrence: Rare, although it occurs with great
consistancy throughout the section, reaching its highest
abundances in marine sediments.

Location: Pb 3840 6 3 39.0 x 121.0

Code: P3st-1

Genus INTRATRIPOROPOLLENITES Thom. and Pf., 1953

Intratriporopollenites rizophorus (Pot.)

 

(Plate 1, Figures 7 and 8)

The figured specimens match very closely illustrations
of this species from Eocene brown coals in Germany.
Krutzsch (1957) indicates that it is a typical lower
Tertiary form. Pflug, in his recombination of the Species,

indicates that it may be related to the family Malvaceae.

135
Occurrence: Rare, occurs consistently only in the
lower part of the section.
Location: Pb 3830 6 ; 47.0 x 110.5 (Fig. 7)
Pb 3867 5 ; 43.0 x 125.9 (Fig. 8)
Code: C3sp—4

Genus SUBTRIPOROPOLLENITES Pf. and Thom., 1953

Subtriporopollenites cf. constans Pf., 1953,
in Thom. and Pf., 1953

 

(Plate 10, Figure 5)

The botanical affinity of this species is unknown.
Pflug (1953) suggests a possible relationship with the
Myricaceae, but many of the several hundred Species of
this large family have not studied as regards their pollen
morphology, and the suggested affinity must be considered
very tentative. The comparison with S. constans is very
close, and Krutzsch (1957) indicates that it is a common
type in the Tertiary of Europe. It is shown on Figure 11

as Pollenites constans.

 

Occurrence: Generally common, but becoming rare near
top of section. The highest frequencies of this species
occur in some lignitic siltstones of apparent estuary or
lagoon environment.

Location: Pb 5622 - l 3 49.0 x 120.0

Code: C3g-l

 

136

Genus TRIATRIOPOLLENITES (Pf.) Thom. and Pf., 1953
Triatriopollenites rurensis Thom. and Pf., 1953
(Plate 12, Figure 2)

This Species matches Myricipites dubius WOde. quite
closely, and an affinity with the family Myricaceae is
probable. The percentages of this species are Shown in
Figure 11 combined with pollen of other Myricaceous and
Betuloid types, including also Corylus-like pollen.

Occurrence: Common, especially in association with
Betula-like pollen in some coals and lignitic siltstones.
The Species occurs throughout the section.

Location: Pb 3883 4 3 34.8 x 111.8

Code: P3sm—4

Genus MOMIPITES Wode., 1933
Momipites coryloides Wode., 1933
(Plate 6, Figure 73 Plate 12, Figure 9)

The percentages of Momipites shown in Figure 6 are
combined values including pollen of Engelhardtia-type.
The affinity of the species figured is not known for certain,
but the morphology is Similar to the pollen of Momisia of
the family Ulmaceae. Figure 9, on plate 12, shows a
slight tendency toward thickening of an annular area around
the pores that is not present in pollen of Momisia, however.

Occurrence: Rare to common, throughout entire section,
but the highest frequency occurs in carbonaceous siltstones

of a nearshore marine environment.

137
Location: Pb 3877 4 ; 29.8 x 114.0 (P1. 6, Fig. 7)

Pb 3832 5 ; 46.2 x 125.0 (P1. 12, Fig. 9)
Code: P3sm-8

Genus ENGELHARDTIOIDITES Pot., Thom., and Thier., 1950
Engelhardtioidites microcoryphaeus (Pot.) Pot., 1950
(Plate 12, Figure 5)

This species is nearly identical to pollen of the
genus Platycarya of the family Juglandaceae. It is
commonly figured and referred to by that name in many
reports dealing with Tertiary palynology.

Occurrence: Generally rare, but distributed
consistently throughout the entire section.

Location: Pb 3895 4 3 38.1 x 115.2

Code: P3sm-6

Engelhardioidites (as Pollenites) quietus
(Pot., 1933, p. 556, Figure 133
Pot., 1934, p. 83, Plate 4, Figures 18 and 21) n. comb.
(Plate 12, Figure 10)

This Species is here placed in the genus
Engelhardtioidites in order to have a clear distinction
between the small triatriate pollen grains with the

characteristic grooves of the Platycarya type, and the

 

entirely smooth grains of the Engelhardtia type. The

 

species names microcoryphaeus and guietus were applied by
Potonie (1931) to species of the large form genus
Egllenites, and his original illustrations Show the

distinctive features mentioned. E. guietus is very similar

 

138
to pollen of Engelhardtia, and both E. guietus and E.
microcoryphaeus probably are representatives of the family
Juglandaceae, if not the genera Platycarya and‘Engelhardtia.
Occurrence: Generally rare, but very consistent
throughout the section.
Location: Pb 3836 1 3 91.1 x 33.0

Code: P3sm-9

Genus MYRICACEOIPOLLENITES Pot., 1951
Myricaceoipollenites cf. megagranifer (Pot.) Pot., 1951
(Plate 12, Figure 1)

The comparison with M. megagranifer is quite close,
although the pores of the figured species appear to be
slightly larger, and with a somewhat heavier annular
thickening. The species probably has affinities with the
family Myricaceae, and the morphology suggests a possible
relationship with the genus Myrica. This species is
combined with other Myricaceous and Betuloid types in the
counts of Figure 11, and its contribution is relatively
large.

Occurrence: Common to abundant, especially in lignitic
and coaly facies throughout the section.

Location: Pb 6320 2 3 49.8 x 113.0

Code: P3sm—2a

139

Genus TILIAPOLLENITES (Pot.) Pot. and Ven., 1934

Tiliapollenites instructus (Pot.) Pot. and Ven., 1934

 

(Plate 10, Figure 4)

The botanical affinity of this species is almost
certainly with the genus Tilia, and it is frequently
recorded from Tertiary deposits. This species is combined
with other Tiliaflike pollen types in the counts of Figure

11, but T. instructus comprises the bulk of the percentages

 

shown.

Occurrence: Rare to fairly common, the species occurs
consistently throughout the section.

Location: Pb 3837 1 3 44.5 x 121.2

Code: Til-2

Tiliapollenites indubitabilis (Pot.) Pot. and Ven., 1934

 

(Plate 1, Figure 2)

This is a smaller species of Tiliaflike pollen, and
13%: affinity with the genus Tilia is not certain, although
iii<3ertainly is related to the family Tiliaceae. Its
contribution to the Tilia_percentages on Figure 11 is
relatively small.

Occurrence: Rare to fairly common, with the highest
frequencies occurring in Zone A.

Location: Pb 3875 4 ; 39.0 x 121.0

Code: Til-7

l4O

Tiliapollenites (as Tilia) crassipites
(Wodehouse, 1933, page 510, Figure 48) n. comb.

 

 

(Plate 1, Figure 3)

This species, described by Wodehouse from the Green
River formation, is probably related to the family
Tiliaceae, but its affinity with the genus Tilia_is not
certain. Its coarse, even reticulum, and its relatively
open apertures distinguish it from the other species of
Tiliapollenites illustrated in this study.

Occurrence: Generally rare, restricted to lower half
of section (Zones A and B).

Location: Pb 3875 - 1 3 36.4 x 126.0

Code: Til—6

Genus PISTILLIPOLLENITES Rouse, 1962
Pistillipollenites mcgregorii Rouse, 1962
(Plate 1, Figure 43 Plate 5, Figures 2 and 3)
The botanical affinity of this Species is not known
for certain, although Rouse suggests a possible affinity

with the genus Rusbyanthus, a genus of the family

 

Gentianaceae. The Size of the body and the club-Shaped
ornamental elements is quite variable, as is the number and
distribution of the elements over the surface of the grain.
'The apertures appear to be short colpi with a raised margin
surrounding them, the margin sometimes being covered with

the pistilate projections.

Occurrence: Rare to common, the species is present in

the lower and uppermost part of the section, but is absent

141
in the middle portion (Zones C and D).
Location: Pb 3831 6 3 39.5 x 123.9
Pb 3867 5 ; 43.0 x 125.9
Pb 3811 1 ; 51.0 X 117.7

Code: P3gm—l

Genus BOMBACACIPITES Anderson, 1960

Bombacacipites cf. nacimientoensis Anderson, 1960

 

 

(Plate 10, Figure 8)

The comparison with this species is tentative. The
botanical affinity of the illustrated form is thought to be
with the family Bombacaceae, although the relationship is
not certain. Other bombacaceous—like pollen is included in
the percentages of the Bombax group in Figure 11, but this
species is the dominant type.

Occurrence: Rare to fairly common, it occurs
throughout the section, but its highest frequencies appear
in carbonaceous siltstones in the upper part.

Location: Pb 3826 3 3 46.8 x 111.1

Code: Bom-l

Genus BOMBACACIDITES Couper, 1960

Bombacacidites cf. bombaxoides Couper, 1960

 

 

(Plate 5, Figure 5)

The genera.Bombacacides and Bombacacipites, both

 

 

DUblished in 1960, are probably not both valid, although
no change is made here. This Species is very similar to

modern Bombax pollen, and affinity with the family

142
Bombacaeae if not Bombax is fairly certain. The family is
tropical to subtropical in distribution today.

Occurrence: Rare, but it occurs conspicuously in Zone

Location: Pb 5621 4 3 52.5 x 120.6

Code: Bom—4

Genus PROTEACIDITES Cookson, 1950

Proteacidites cf. marginus Rouse, 1962

 

 

(Plate 10, Figure 7)

The comparison with P. marginus is close, although, as

 

Rouse points out, considerable variation exists and this

Species may be gradational with P. terrazus. The botanical

 

affinity is probably the family Proteaceae.

Occurrence: Rare to common, especially in the lower
part of the section.

Location: Pb 3828 5 ; 39.6 x 113.8

Code: Prot-l

Proteacidites terrazus Rouse, 1962

 

(Plate 6, Figure 12)

This species together with P. cf. marginus, comprise

 

the total percentage of Proteacidites shown on Figure 6.
Illustrations of similar types are common in studies of
lower Tertiary sections, and it appears that this species
is an excellent marker for Eocene rocks.

Occurrence: Rare to common, generally throughout the

section, but with decreasing frequency in Zones D and E.

143
Location: Pb 3843 2 3 43.3 x 112.0

Code: Prot-2

Genus CARYAPOLLENITES Raatz 1937
Caryapollenites simplex (Pot.) Raatz, 1937
(Plate 12, Figure 8)
The botanical affinity of this species is probably the
family Juglandaceae, and possibly the genus Capya, although
C. simplex is considerably smaller than pollen of most

modern species of Carya. This species comprises the total

shown under Carya in Figure 11.

Occurrence: Common to abundant, occurs throughout the
section; its highest frequencies occur in carbonaceous
siltstones apparently deposited in brackish lagoons or bays.

Location: Pb 3829 5 3 41.6 x 113.8

Code: Car-1

Caryapollenites Spackmanius (Traverse) Pot., 1960
(Plate 5, Figure 4)
This species is about twice as large as C. Simplex.
It appears that the larger C. gpackmanius type may be the
product of an evolutionary trend to larger pollen from the
Smaller C. simplex type. C. Spackmanius occurs only in a
Jflew samples in the uppermost part of the section, and

though C. simplex is still present in those samples, its

at>undance is considerably reduced. This species compares
Closely with modern Carya pollen, and an affinity with that

genu s is probable .

144
Occurrence: Rare, the species occurs only in Zone E.
Location: Pb 3897 4 3 50.3 x 121.0

Code: Car-2

Genus ALNIPOLLENITES Pot., 1931

Alnipollenites versus (Pot.) Pot., 1934

 

(Plate 12, Figure 6; Plate 4, Figure 9)

The botanical affinity of this species is almost
certainly with the genus Alppp, family Betulaceae. It is
a commonly identified form in Tertiary deposits. This
species comprises most of the percentages shown under Alppp_
in Figure 11.

Occurrence: Common in most samples throughout the
section, although its relative abundance decreases generally
in most coal samples. A six pored form of this Species
(Plate 4, Figure 9) occurs only in Zones D and E.

Location: Pb 3838 4 3 43.4 x 120.8 (P1. 12, Fig. 6)

Pb 3897 4 ; 46.5 x 116.5 (Pl. 4, Fig. 9)

Code: Al-l

Alnipollenites sp.

 

(Plate 12, Figure 7)

This species may be referable to the Species A. versus,
altmmugh the pores appear to be consistently oriented
ESlightly off the equator, and the pore annulus is generally
11388 well developed. Only four pored forms of this type
VWKPe observed, while four and five pored A. versus were

persent in nearly equal numbers. The affinity with the

145
genus Alpp§_is less certain for this Species, although
it was included in counts under that heading in Figure 11.
Occurrence: Rare, the species ranges throughout the
section.
Location: Pb 3883 4 3 47.5 x 128.0
Code: Al-2

Genus ULMIPOLLENITES Wolfe, 1934

Ulmipollenites undulosus Wolfe, 1934

 

(Plate 2, Figure 11; Plate 12, Figure 11)

Anderson (1960) used the name Ulmoidipites for grains

 

very similar to the types illustrated here. The botanical
affinity appears to be with the family Ulmaceae, although
the generic affinity is not certain. Four and five pored
forms of this species are present, and both types are
included in counts of H1mp§_in Figure 11.

Occurrence: Generally common throughout the section,
although the five pored form occurs only in samples from
Zone B and above.

Location: Pb 5615 1 ; 52.2 x 113.8 (Pl. 2, Fig. 11)

Pb 3883 4 ; 36.2 x 125.1 (P1. 12, Fig. 11)

Code: Rprug—l

Ulmipollenites sp.

 

(Plate 1, Figure 13)
This is a smaller, three pored pollen which is in other

respects similar to U. undulosus. ‘Anderson (1960)

 

illustrates a similar type referring to it as Ulmoideipites

 

146

krempi. It appears that an evolutionary sequence from three
pored to polyporate aperture condition is present in this
group of pollen, which are probably related to the family
Ulmaceae.

Occurrence: Rare to common, this species does not
range above Zone D.

Location: Pb 3831 6 3 47.5 x 117.2

Code: P3rug-l

Genus PTEROCARYAPOLLENITES Thierg., 1937

Pterocaryapollenites stellatus (Pot.) Raatz, 1937

 

(Plate 6, Figure 10; Plate 12, Figure 15)
The botanical affinity of this species appears to be

with Pterocarya. The percentages of Pterocarya shown in

 

 

Figure 11, and of Pperocaryappllenites in Figure 6, are
comprised entirely of this species. The sporadic
occurrence of extremely high abundances of this Species in
particular swamp or brackish environments reduces its
stratigraphic value, although it provides some indication
of the ecological setting of the parent plant.

Occurrence: Rare to abundant, the species occurs
throughout the section with the highest abundances occurring'
in some coals and lignitic siltstones in the upper part of
the section.

Location: Pb 3872 3 ; 49.0 x 122.0 (P1. 6, Fig. 10)

Pb 3801 5 ; 35.0 x 125.3 (P1. 12, Fig. 15)

Code: Bnp-l

147

Genus LIQUIDAMBARPOLLENITES Raatz, 1937
Liquidambarpollenites stigmosus (Pot.) Raatz, 1937
(Plate 4, Figure 11)
The botanical affinity of this species appears to be

with the genus Liquidambar of the family Hemamelidaceae.

 

It is a frequently identified form from Tertiary deposits.
This species comprises about half of the counts shown

under Liquidambar in Figure 11.

 

Occurrence: Rare to common, this species occurs in
Zones D and E and the highest frequencies appear in some
lignitic siltstone samples.

Location: Pb 3802 2 3 50.3 x 120.2

Code: Bwr—l

Liquidambarpollenites cf. mangelsdorfiana
(Traverse) Pot., 1960

 

 

(Plate 3, Figure 15; Plate 12, Figures 12 and 13)
The illustrated species compares quite closely with

L. mangelsdorfiana from the Oligocene Brandon Lignite. The

 

pores are slightly more elongate and the exine somewhat
thicker in the illustrated species than in the original

illustration of L. mangelsdorfiana. It is included in the

 

percentages of Liquidambar in Figure 11.

 

Occurrence: Generally rare, but it is consistently
present in and above Zone B.
Location: Pb 3827 5 ; 38.0 x 125.1 (P1. 3, Fig. 15)
Pb 3872 3 ; 48.2 x 123.3 (P1. 12, Figs.12,13)

Code: Rfir-3

148

Genus MULTIPOROPOLLENITES Pf., in Thom. and Pf., 1953

Multiporopollenites ludlowensis Stanley, 1960

 

(Plate 12, Figures 17 and 18)
This identification is based on a thesis description,
and it is therefore not a valid name. The species almost

certainly represents the genus Pachysandra of the family

 

Buxaceae. This pollen species has been identified from a
number of Tertiary localities in North America.
Occurrence: Rare, although it occurs with some
consistency throughout the section.
Location: Pb 3873 l 3 45.5 x 121.9

Code: Pac-l

Genus JUGLANSPOLLENITES Raatz, 1937

Juglanspollenites versus Raatz, 1937

 

(Plate 12, Figure 16)

The botanical affinity of this Species appears to be
with the genus Juglans. The pollen possesses the
characteristic feature of pores arranged equatorially with
one to three pores in one hemiSphere, off the equator.

Occurrence: Rare, the species occurs very consistently
in nearshore marine sediments, especially in the upper part
of the section.

Location: Pb 3806 2 3 34.3 x 111.7

Code: P sm-3

149

Genus POLLENITES H. Pot., 1893

Pollenites oculuS-noctis Thierg., 1940

 

(Plate 1, Figure 10; Plate 11, Figures 14 and 15)
Couper (1960) has illustrated very similar forms and

referred them to the genus Epilobium. The two pored form

 

illustrated in this paper (Plate 11, Figure 15) is identified
as Fuchsia by Couper (1960). Traverse (1955) illustrates a
nearly identical form and refers it to the modern genus

Jussaea. The botanical affinity of P. oculus-noctis is

 

almost certainly with the family Onagraceae.

Occurrence: Rare, although it occurs consistently
throughout the section with the highest frequencies
appearing in the lower half of the section.

Location: Pb 3831 6 ; 51.3 x 113.7 (P1. 1, Fig. 10)

Pb 5622 1 ; 61.0 x 122.8 (P1. 11, Fig. 14)
57.8 x 111.3 (P1. 11, Fig. 15)

Code: P3sm-4

Pollenites cf. ventosus Pot., 1931

 

 

(Plate 3, Figure 3)
The comparison of the illustrated specimen with PotonieS
original drawing iS only suggestive of an identity. The
form present in the Samples studied is tricolpate with a
suggestion of pore development at the equator. It is nearly
always seen in polar View, with the colpi narrow and Slit—
like. It is a frequently occurring Eocene form in the

German brown coals.

150
Occurrence: Common to rare, the species occurs
throughout the section.
Location: Pb 3809 6 3 45.9 x 110.9

Code: C3g-4

Pollenites genuinus Pot., 1934

 

(Plate 2, Figure 1)
The illustrated species usually shows a slight
constriction or pore—like development within the colpi at
the equator, much as Potonie describes as a genuculus in

P. genuinus. It is common in some Eocene sediments of

 

Europe. The botanical affinity is not known.
Occurrence: Rare to common, in and above Zone C.
Location: Pb 3895 2 3 48.2 x 110.0

Code: C3r—l8

Pollenites anulus (Pot.) Pot. and Ven., 1934

 

(Plate 12, Figure 14)

This species possibly represents the genus Celtis,
although that is not certain. The number of pores is
variable from three to six, but most commonly there are
five. This is a frequently identified lower Tertiary
Species.

Occurrence: Generally rare, however it is very
consistent in the upper part of the section.

Location: Pb 3806 2 3 44.5 x 116.3

Code: Rxsm-5

151

Genus SPORITES H. Pot., 1893

Sporites cf. vegetus Pot., 1934

 

(Plate 1, Figure 5)

Despite the misleading name, this species is a
tricolpate pollen, as pointed out by Krutzsch (1957).
The botanical affinity is unknown. The comparison of the
illustrated form with S. vegetus is close.

Occurrence: Rare to fairly common, especially in the
lower part of the section.

Location: Pb 3839 l 3 45.7 x 127.3

Code: C3r-9

152
FUNGI

 

FAMILY MICROTHYRIACEAE
(Plate 7, Figures 4, 8 and 9)

A great variety of fungi are present in nearly all of
the samples examined. The illustrated Specimens represent
only an example of the most abundant types. The family
Microthyriaceae is today a tropical—subtrOpical group of
ectoparasites commonly found on ferns, broadleaf trees and
cenifers.

Occurrence: Common to abundant, especially abundant
in some lignitic siltstones and coals. The fungi as a
whole show an inverse relationship in abundance with the
microplankton.

Location: Pb 5607 1 3 38.2 x 119.0

Pb 3805 5 3 41.0 x 114.7
Pb 3805 5 3 52.4 x 124.9

 

153

ALGAE

 

Genus CYCLONEPHELIUM (Deflandre and Cookson)
Cookson and Eisenack, 1962

Cyclonephelium Sp.

 

(Plate 7, Figure 1)

The genus Cyclonephelium is a commonly identified

 

Mesozoic to lower Tertiary form. It is a Significant
contributor to the percentages of microplankton in Figure 6.
Occurrence: Rare to common in samples of marine origin,
especially those away from the swampy shoreline.
Location: Pb 3836 5 3 41.0 x 110.3

Code: ny—2

Genus WETZELIELLA Eisenack, 1938

Wetzeliella glabra Cookson, 1956

 

(Plate 7, Figures 2 and 7)

This species has been described from the Eocene in
Australia, and it is likely that it will prove to be an
excellent stratigraphic marker for lower Tertiary rocks.

Occurrence: Rare, apparently in open marine environments.

Location: Pb 5616 2 ; 38.5 x 127.1 (Fig. 2)

Pb 5617 3 ; 36.4 x 115.3 (Fig. 7)

Code: Dino—5

154

Wetzeliella Sp.

 

(Plate 7, Figure 5)
Occurrence: Rare to common, especially in samples from

upper part of the section.
Location: Pb 5618 4 3 50.8 x 118.1

Code: Dino-6

Genus DEFLANDREA Eisenack, 1938

Deflandrea cf. Spinulosa

 

(Plate 7, Figure 6)

This Species is commonly seen in lower Tertiary
sediments. It exhibits a considerable range of morphologi-
cal features, but the illustrated specimen is by far the
most common type seen in the samples studied.

Occurrence: Common to abundant, occurring in large
numbers in some apparently nearshore or even brackish
environments.

Location: Pb 5616 2 3 32.3 x 123.6

Code: Dino-2

Deflandrea sp.

 

(Plate 2, Figure 12)
Occurrence: Rare to common, mostly in middle part of
section (Zone C).
Location: Pb 3838 l 3 35.5 x 115.3
Code: Dino-l

155
Genus CYMATIOSPHAERA (wetzel) Deflandre, 1954

gymatiosphaera sp.

 

(Plate 1, Figure 9)

This genus is comprised of species most of which are
Paleozoic to Mesozoic in age. The figured specimen appears
to be referable to the genus, however, although no Specific
comparisons were found.

Occurrence: Generally rare, it occurs most frequently
in the lower part of the section, especially in Zone A.

Location: Pb 5603 l 3 46.3 x 114.9

Code: ny-8

Genus CANNOSPHAEROPSIS Wetzel, 1932

Cannosphaeropsis sp.

 

(Plate 2, Figure 13)
This genus is composed mostly of Mesozoic species, and
has not been recognized from North America.
Occurrence: Rare to common, it is restricted to Zone
C and appears to be an excellent marker for that zone in
marine rocks.
Location: Pb 3874 4 3 46.2 x 122.0

Code: ny-4

156

Genus TYTTHODISCUS Norem, 1955

Tytthodiscus sp.

 

(Plate 5, Figure 8)

Occurrence: Rare to common, it occurs with highest
frequency in the upper part of the section, especially
Zone E.

Location: Pb 3896 2 3 52.5 x 115.2

Code: Tyth-l

INCERTAE CEDIS
(Plate 1, Figure 12; Plate 5, Figure 7)
This specimen may be an encystment or budding state of
a brown edge alga (Phaeophyta) (Prescott, G. W. personal
communication). It bears some resemblance to the genus

Halogoras Cookson, 1956 which is also assumed to be an

 

algal cyst by that author.

Occurrence: Rare to common, it occurs in the lowermost
and uppermost part of the section and is totally absent in
between.

Location: Pb 3828 5 3 39.5 x 127.5 (P1. 1, Fig. 12)

Pb 3830 6 ; 42.7 x 124.2 (P1. 5, Fig. 7)

Code: Alga-l

157

INCERTAE CEDIS
(Plate 5, Figures 6 and 9)

This Specimen appears to be a marine microplankton
species, probably a member of the Dinoflagellatae. It
appears in abundance in Zone E, and may be an excellent
marine marker for latest Eocene and/or earliest Oligocene.

Location: Pb 3896 2 ; 54.0 x 109.0 (Fig. 6)

Pb 3896 2 ; 36.3 x 115.0 (Fig. 9)

Code: ny—9

SELECTED LIST OF REFERENCES

Anderson, R. Y., 1960, Cretaceous-Tertiary Palynology,
Eastern Side of the San Juan Basin, New Mexico, State
Bur. Mines and Min. Res., New Mex. Inst. Min. and
Tech., Mem. 6.

Barghoorn, E. S., 1951, Age and Environment: A Survey of
North American Tertiary Floras in Relation to a
Paleoecology, Journ. Paleo., vol. 25: 736-744.

Beck, R. S., 1943, Eocene Foraminifera from Cowlitz River,
Lewis County, washington, Journ. Paleo., vol. 17:
584-614.

Berthiaume, S. A., 1938, Orbitoids from the Crescent
Formation (Eocene) of Washington, Journ. Paleo., vol.

494-497.

Boyko, H., 1947, On the Role of Plants as Quantitative
Climatic Indicators and the Geo-ecological Law of
Distribution, Journ. Ecol., vol. 35: 138-157.

Bravinder, K. M., 1932, Stratigraphy and Paleontology of
the Oligocene in the Eastern Portion of the Puget
Sound Basin, Masters Thesis, Washington Univ., Seattle.

Brown, R. W., 1944, Temperate Species in the Eocene Flora
of Southeastern United States, Wash. Acad. Sci. Journ.,
vol. 34: 349—351.

Brown, R. D., Jr., Gower, H. D., and Snavely, P. D., Jr.,
1960, Geology of the Port Angeles—Lake Crescent Area,
Clallam County, Washington, U.S. Geol. Sur. Oil and
Gas Inv. Map OM 203.

Chibrikova, E. V., 1963, Conditions of Formation of Spore-
pollen Complexes and Their Use for the Restoration of
the Environment of Sedimentation and Paleogeography,
Izvestiya, U.S.S.R. Acad. Sci. Geol. Series, Number 123
102—110.

Cookson, I. 0., 1953, Records of Occurrence of Botrycoccus
braunii, Pediastrum and the Hystrichosphaeridae in
Cenozoic Deposits of Australia, Mem. Nat. Mus.
Melbourne, no. 18: 107-123.

, and Pike, K. M., 1954, Some Dicotyledonous Pollen
Types from Cainozoic deposits of the Australian Region,
Austral. Jour. Bot., vol. 2: 197-219.

158

159

Couper, R. A., 1953, Upper Mesozoic and Cainozoic Spores
and Pollen Grains from New Zealand, New Zealand Geol.
Sur. Paleo. Bull., vol. 22: 77 pp.

, 1954, Plant Microfossils from New Zealand, No. 1,
Tran. Royal Soc. New Zealand, vol. 81: 479-483.

, 1960, New Zealand Mesozoic and Cainozoic Plant
Microfossils, New Zealand Geol. Sur. Paleo. Bull.,
vol. 32: 82 pp.

Cousiminer, H. L., 1961, Palynology, Paleogloras and
Paleoenvironments, Micropaleo, vol. 7: 265-268.

Effinger, W. L., 1938, The Gries Ranch Fauna (Oligocene)
of western Washington, Journ. Paleo., vol. 12: 355-390.

Engelhardt, D. W., 1964, Plant Microfossils from the Eocene
Cockfield Formation, Hinds County, Mississippi, Miss.
Geol. Res. Papers, Miss. Geol. Econ. and Topo. Sur.
Bull., vol. 104: 65-96.

Erdtman, G., 1943, An Introduction to Pollen Analysis,
Chronica Botanica, Waltham Mass., 239 pp.

Faegri, K., and Iversen, J., 1964, Textbook of Modern
Pollen Analysis, Ejna Munksgaard, C0penhagen.

Foster, R. J., 1960, Tertiary Geology of a Portion of the
Central Cascade Mountains, Washington, Geol. Soc. Am.
Bull., vol. 71: 99—125.

Gerhard, J. E., 1958, Paleocene Miospores from the Slimm
Buttes Area, Harding County, South Dakota, Unpublished
Masters Thesis, Penn. State Univ.

Good, Ronald, 1958, The Geography of Flowering Plants,
John Wiley and Sons, New York, 518 pp.

Gower, H. D., and Warek, A. A., 1963, Preliminary Geologic
Map of the Cumberland Quadrangle, King County,
Washington, Wash. Div. Mines and Geol., Map GM-2.

Gray, Jane, 1960, Temperate Pollen Genera in the Eocene
(Clairborne) Flora of Alabama, Sci., vol. 132: 808-810.

, and Sohma, K., 1964, Fossil Pachysandra from
western America with a Comparative Study of Pollen in
Pachysandra and Sarcocca, Amer. Jour. Sci., vol. 262:

1159-1197.

Groot, J. J., and Groot, C. R., 1960, Some Plant Microfossils
from the Brightseat Formation (Paleocene) of Maryland.

Paleontographic B, vol. 111: 161-171.

160

Henrikson, D. A., 1956, Eocene Stratigraphy of the lower
Cowlitz River Valley and Eastern Willapa Hills Area,
southwest Washington, Wash. Div. Mines and Geol. Bull.,
vol. 43: 122 pp.

Jekhowsky, B., 1960, Distance Between Populations in
Quantitative Palynology and Its Use for Stratigraphical
Purposes, abs., Pollen et Spores, vol. 4: 354.

Jeletzky, J. A., 1965, Is It Possible to Quantify
Biochronological Correlation? Journ. Paleo., vol. 39:
135-140 0

Jones, E. L., 1961, Plant Microfossils of the Laminated
Sediments of the lower Eocene Wilcox Group in south—
central Arkansas, Ph.D. Thesis, Oklahoma Univ., Norman.

, 1962, Palynology of the Midway-Wilcox Boundary in
south-central Arkansas, Trans. Gulf Assoc. Geol. Soc.,
vol. XII: 285-294.

Krutzsch, W. 1959a, Mikorpalaontologische (sporenpalaonto—
logische) Untersuchungen in der Braunkohle des
Gerseltales: Geologie Jg. 8, Beih. 21/22 425 pp.

, 1962 and 1963, Atlas der Mittll-und Jimgtertiaren
Dispersen Sporen und Pollen Sowie der Mikroplanktonformen
des Nordlichen Mitteleurppus: vols. l (1962) and 3
(1963), Deutscher Verlag der Wissenschaft, Berlin.

Kuyl, O. S. J., Muller, and H. Th. Waterbolk, 1955, The
application of Palynology to Oil Geology with
Reference to Western Venezuela, Geol. en Mijub. 17:

49-76.

Mac Ginitie, H. D., 1941, A Middle Eocene Flora From the
Central Sierra Nevada, Carnegie Inst. Wash. Pb. 534,

178 pp.

Miner, E. L., 1935, Paleobotanical Examinations of

Cretaceous and Tertiary Coals, pt 2 Amer. Mid. Nat.
16: 616-625.

Misch, Peter, 1958, Geology of the Northern Cascades of
Washington, The Mountaineer, 45: 4—22.

Mittre, Vishnu, 1964, Contemporary Thought in Palynology —
Phytomorphology 14: 135-147.

Moore, R. C., and Vokes, H. E., 1953, Lower Tertiary
Crinoids from N. W. Oregon, U.S. Geol. Sur. Prof. Pap.

233-E o

161

Murriger, F., and Pflug, H., 1952, Uber Eine Palynologische
Untersuchung des Braunkohlenlargers der Grube Emma bei
Marxheim (Untermaingeniet). Notizbl. hess. Landesamtes
Bodenforsch., Folge 6, Heft 3, s. 56-66.

Nagy, Esther, 1955, Some New Spore and Pollen Species from
the Neogene of the Mecsek Mountains, Acta Botanica IX:
387-404.

Norem, W. L., 1955, Tytthodiscus, A New Microfossil Genus
From the California Tertiary Jour. Paleo. 29: 694-695.

Nuey-Stolz, G., 1958, Zur Flora der Niederrheinischen Bucht
Wahrend der Hauptflozibilduing unter Besonderer
Berucksichtingung der Pollen und Pilzrests in den Hellen
Schicten. Fortschr. Geol. Rheinld. u. Westf. Band 2
p. 503-525, Krefeld.

Pease, M. H., Jr. and Hoover, Linn, 1957, Geology of the
Doty-Minot Peak Area, Wash. U.S. Geol. Sur. Oil and
Gas Inves. Map OM 188.

Pflug, H., 1953, Zur Entstehung und Entwicklung des
AngiOSpermiden Pollens in der Erdgeschickte.
Paleotographica Bd 94: 60-171, Abt B.

Potonie, R. 1931, Pollenformen aus Tertiaeren Braunkohlen
(3 Mitt). Jb. Preuss. Geol. L.A. f. 52: 1-7.

, 1934, Zur Mikrobotanik der Kohlen und Iher
Verwandten I Zur Morphologie der Fossilen Pollen and
Sporen. Arb. Inst. F. Paleobot. U. Petrogr. d.
Bennsteine 4, 5.

, 1934, Zur Mikrobotanik des Eocaenen Humodils Des
Geiseltals. Arb. Inst. Palaeobot. U. Petrogr. Brennst.,
Preuss. Geol. L. A Berlin 4: 25-125.

, 1951, Revision Stratigraphisch Wichtiger
poromorphen Mittlleurpaischen Tertiars. Paleontographica
91: 131-151 Ab B.

, 1956, Die Behandling der Sporae Dispersae und Der
Fossilen Pflanzen Uberhaupt Nach Dem Internationalen
Code Der Botanischen Nomen Klalur. Palaeont. Z. 30:
69-87 0

, 1956, Synopsis Der Guttungen Der Sporae Dispersae.
I Teil Sporites Beih. Geol. Jb. 23: 103 p.

, 1958a, The Taxonomy of Fossil Plants (includes Spore
Dispersae) in the International Code of Botanical
Nomenclature The Paleobotanist 7: 32-42.

162

Potonie, R., 1958b, Synopsis der Gattungen der Sporae
Dispersae II Teil: Sporites (Nachtrage Saccites,
Aletes, Pracecolpates, Polyplicates, Monocolpates)
Beih. Geol. Jb 31: 114 pp.

, 1960, Synopsis der Gattungen der Sporae Dispersae.
III Teil: Nachtrage Sporites Fortsetzurg Pollenites
Mit General Beih Geol. Jb. 39: 189 pp.

, and Gelletich, J., 1933, Uber Pteridophyten—Sporen
Einer Eozaden Braunkohle Aus Dorog in Ungarn. Sber.
Ges. Nat. Freunde, vol. 33, pp. 517—528.

, and Venitz, A., 1934, Zur Microbotanik des Miocanen
Humodils der Niedeuheinischen Bucht. Preuss. Geol.
Landes., Inst. Palaobot. U. Petrog. Brennsteine, Arb.,
vol. 5, pp. 1-54.

Raatz, G. V., 1937, Mikrobotanisch-stratigraphische
Untersuchung der Braunkohle des Muskauer Bogens:
Pruess. Geol. Landes., Abh., Neue Folge, vol. 183,
pp. 1-48.

Rau, W. W., 1951, Tert. Foraminfera from the Willapa River
Valley of southwest Washington. Jour. Paleo. 25:

pp. 417-453.

, 1958, Stratigraphy and Foraminiferal Zonation in
some of the Tertiary Rocks of southwest Washington,
U.S. Geol. Sur. Oil and Gas Inv. 00 57.

Roberts, A. E., 1958, Geology and Coal Resources of the
Toledo-Castle Rock District, Cowlitz and Lewis Counties,
Washington, U.S. Geol. Sur. Bull., 1062: 71 pp.

Ross, N. E., 1949, On a Cretaceous Pollen--and Spore-
bearing Clay Deposit of Scania: Bull. Geol. Inst.
Uppsala, vol. 34, pp. 25-43.

Rouse, J. G., 1962, Plant Microfossils from the Burrard
Formation of Western British Columbia, Micropaleo,
8: 187-218.

Rouse, Glenn E. and Mathews, W. H., 1960, Radioactive
Dating of Tertiary Plant-bearing Deposit, Science 133:

Rudolph, K., 1935, Microfloristische Untersuchungen Tertiarer
Ablagerungen im Nordlichen Boehmens. Bot Zentrbl. Beih.
Bd. 54: 244—328 Abt. B.

Sharp, A. J., 1951, The Relation of the Eocene Wilcox Flora
to Some Modern Floras. Evolution, vol. 5, No. 1, pp. 1—5.

\J‘

163

Simpson, J. B., 1961, The Tertiary Pollen-flora of Mull and

Ardnamurchan. Trans Roy. Soc. Edinburgh, v01. 64, no.
16, pp. 421-488.

Snavely, P. D., Jr., Brown, R. D., Jr., Roberts, A. E., and
Rau, W. W., 1953, Geology and Coal Resources of the
Centralia-Chehalis District Washington, U.S.G.S. Bull.

1053, 154 pp.

, Rau, W. W., Hoover, L., Jr., and Roberts, A. E.,
1951, McIntosh Formation, Centralia-Chehalis Coal
District Washington, Am. Assoc. Pet. Geol. Bull. 35:
1052-1061.

, and Wagner, Holly C., 1963, Tertiary Geologic
History of Western Oregon and Washington, Wash. State
Div. of Mines and Geol. Rept. Inv. 22-25 pp.

Stanley, E. A., 1960, Upper Cretaceous and Lower Tertiary
Sporamorphae from Northwestern South Dakota, Ph.D.
Diss. Pennsylvania State University.

Teichmuller, M. Von, 1958, Rekonstruktionen verschiedener
Moortypen Des Haupflozes der Niederrheinischen Braunkohle.
Fortschr. Geol. Rneinld. u. Westf. Krefeld Band 2,

pp 0 599‘6120

Teichert, Curt, 1958, Concepts of Facies, Am. Assoc. Pet.
Geol. Bull., 42: 2718-2744.

Thiergart, F., 1958, Die Sporomorphen-Flora von Rott im
Siebengegire. Fortschr. Geol. Rheinld. u. Westf.
Krefeld Band2, pp. 447-456.

Thomson, P. W., 1949, Alttertiare Elements in der Pollenflora
der Rheinischen Braunkohle und Einige Stratigraphisch
Wichtige Pollenformen Derselben. Neues. Jahrb. Minera1.,
Monatsh. Abt. 13.

Thompson, P. W. and Pflug, H., 1953, Pollen und Sporen des
Mitteleurepaischen Tertiars. Palaeontographica 94B
Lief. 1-4.

Traverse, A., 1955, Pollen Analysis of the Brandon Lignite
of Vermont. U.S. Bur. Mines Rept. Inv. no. 5151 107 pp.

Vine, James D., 1962, Preliminary Geological Map of the
H0bart and Maple Valley Quadrangles, King County
Washington, Wash. Div. Mines and Geol. Map gm-l.

, 1962, Stratigraphy of Eocene Rocks in a Part of
King County Washington, Wash. Div. of Mines and Geol.
Rept. Inv. no. 21, 20pp.

164

Warren, W. C., Norbisrath, Hans, et a1., 1945, Preliminary
Geological Map and Brief Description of the Coal Fields
of King County Washington, U.S.G.S. Survey Coal Map.

, and Norbisrath, Hans, 1946, Stratigraphy of Upper
Nehalem River Basin, N. W. Oregon, Am. Assoc. Pet.
Geol. Bull. 30: 213—237.

Weaver, C. E., 1916, The Tertiary Formations of Western
Washington, Wash. Geol. Sur. Bull. 13.

, 1937, Tertiary Stratigraphy of Western washington
and N. W. Oregon, Wash. Univ. (Seattle) Pub. in Geol. 4:
266 pp.

Wilson, L. R. and webster, R. M., 1946, Plant Microfossils
of a Fort Union Coal of Montana, Amer. Jour. Bot. 33:
271-278.

Wodehouse, R. P., 1933, The Oil Shales of the Eocene Green
River Formation, Bull. Torr. Bot. Club, 60: 479-524.

, Tertiary Pollen II the Oil Shales of the Green
River Formation, Bu11.'Torr. Bot. Club, 60: 479-524.

Wolfe, Jack A., 1962, A Miocene Pollen Sequence from the
Cascade Range of N. W. Oregon, U.S. Geol. Sur. Prof.
Paper 4500: c31-c84.

Wolfe, J. A., Gower, H. D., and Vine, J. D., 1961, Age and
Correlation of the Puget Group in: Short Papers in
Geol. Sci. U.S. Geol. Sur. Prof. Paper 424-0, 230-232.

Wolfe, H., Mikrofossilen des Pliozanen Humodils. Preuss.
Geol. Landes., Inst. Palaobot. u. Petrog. Brennsteine,
Arb., VOlo 5) pp. 55-86.

Younquist, Walter, 1961, Annotated Lexicon of Names Applied
To Tertiary Stratigraphic Units in Oregon and washington
West of Cascade Mountains with Bibliography, W. Younquist,
Eugene Oregon.

APPENDIX A

The location of the sections collected and studied are
presented in this section. The position and lithologic
description for each sample is also provided. The lithologic
descriptions are based on field examination only, and are
not intended as accurate petrographic analyses. The sample
numbers correspond to those mentioned in the text and shown
in the illustrations.

Skookumchuck River Section 64-DS-XII
Sec. 33, T15N, R2W

Position
Sample in
Number Section Lithology
4 590 ft. dark gray, soft, fissile, carbonaceous
shale, some molluscan fossils
3 500 ft. 12" coal seam, with underclay where
roots are in place
2 360 ft. lignitic siltstone and thin coal, many
leaf fossils
1 base of thick coal and parting clay sequence,
exposed some logs and stumps appear to be in
section growth position

Willapa River Section 64-DS-XIII and 65-DS-XI
Secs. 3, ll, 14, 24, 25, 36, T13N, R8W, Pacific County, Wash.

Position
Sample in
Number Section Lithology
7 900 ft. hard, dark gray, fissile, micaceous

siltstone

800 ft. same lithology as above

700 ft. dark gray, massive, poorly sorted,
micaceous siltstone, possibly graded

600 ft. gray, concretionary shale, with associated
coarse agglomerate zone

200 ft. dark gray, carbonaceous, concretionary,
sandy siltstone

150 ft. dark gray, poorly sorted, coarse sandstone

50 ft. dark gray, fissile siltstone, with
associated coarse volcanic sandstone

P—‘I’D LA) 42‘ mm

A-l

Sample
Number

50

49
48

47
46
45
44

43
42

Position
in

A-2

Rock Creek Section 65-DS-XIV
T4N, R5W3 T5N, R5W3 T5N, R4W, Columbia County, Oregon

Section

85O

750
700

600
450
350
250

125
50

ft.

ft.
ft.

ft.
ft.
ft.
ft.

ft.
ft.

Lithology

soft, tuffaceous, dark gray, well bedded,
silty shale

soft, massive, concretionary siltstone
same lithology as above, with calcareous
horizons

dark gray, tuffaceous, sandy, siltstone,
with CaCOs stringers

gray, well bedded, slightly fissile,
silty sandstone

hard, dark gray, fissile, well bedded
siltstone and Shale

same lithology as above

dark gray, fissile, carbonaceous siltstone
gray, very carbonaceous, micaceous
siltstone with plant fossils and
associated bluish sandstone

Chehalis River Section ‘65—Ds—x

Sec. 12, 13, T12N, R5W, Lewis County, Washington

Sample
Number

6

5
4
3
2

Position
in

Section

4000
3900
3700
3000

2500

1000

ft.
ft.
ft.
ft.

ft.

ft.

Lithology

lignitic, micaceous, siltstone with
associated channel sandstone
brownish-gray, well bedded, carbonaceous
shale

dark gray, poorly sorted, concretionary
siltstone

hard, dark gray, fissile, concretionary
shale

dark gray, micaceous siltstone with
carbonaceous stringers possibly graded
bedding

hard, dark gray, fissile, silty shale
with associated volcanic sandstones

 

Sample
Number

2

1

A-3

McIntosh Lake Section 64-DS—XI

Sec. 14, T16N, R1W, Thurston County, Washington

Position
in
Section Lithology
100 ft. hard, dark gray, thin bedded, fissile,
concretionary shale and siltstone

base of same lithology as above

exposed

section

Stillwater-Olequa Creek Section
64-DS-XIV, 64-DS-XV and 65-DS4VIII

Secs. 4, 5, 6, T1ON, R3W3 Secs. 25, 26, 34 T11N, R3W,

Sample
Number

41
40
39
38
37
35 7

L‘I—‘RDUJ-D'Ulm

32
31
3O
29

Lewis and Cowlitz Counties, Washington

Position
in

Section Lithology

7925 ft. lignitic, micaceous siltstone with much
plant debris

7900 ft. coarse channel sandstone with coalified
logs and thin clay stringers

7840 ft. interbedded coals and bluish Shales,
roots seen in place

7800 ft. channel sandstone cutting through
lignitic siltstone and coal

7600 ft. bluish, micaceous, carbonaceOus sand-

stone with coaly horizons

7250 ft. gray, thinnly bedded, Shale and
siltstone, very carbonaceous

7240 ft. same lithology

7230 ft. same lithology

7220 ft. same lithology

7215 ft. same lithology

7210 ft. same lithology

7200 ft. same lithology

7000 ft. gray, tuffaceous, concretionary siltstone
with some sandy layers

6825 ft. thinnly interbedded sandstone and
siltstone, associated channel sandstone

6600 ft. interbedded carbonaceous Shales, sand-
stone and siltstone

6500 ft. lignitic siltstone, interbedded with
massive to crossbedded sandstone lenses

6450 ft. gray, fairly well sorted, fissile
siltstone with foraminifera

6400 ft. same lithology, but containing molluscan

fossils

A-4

Position
Sample in
Number Section Lithology
28 6250 ft. same lithology
27 6150 ft. gray siltstone, with molluscan fossils
and associated fairly well sorted sand-
stones
26 6000 ft. same lithology
25 5600 ft. fossiliferous, poor to well sorted gray
siltstone
24 5400 ft. lignitic siltstone interbedded with gray
siltstone and fossiliferous
23 5300 ft. bluish massive sandstone with carbonaceous
stringers
22 4900 ft. gray, carbonaceous, micaceous, poorly
sorted siltstone
21 4600 ft. same lithology
20 4250 ft. soft, bluish-gray, micaceous, fairly
massive siltstone
19 4100 ft. gray, micaceous, fine sandstone and
siltstone
18 3950 ft. dark gray, massive, poorly sorted
siltstone
17 3900 ft. hard, bluish, fissile shale with some
concretions
16 3750 ft. dark gray siltstone and bluish sandstone,
some concretions
15 3650 ft. dark gray, poorly sorted, well bedded
siltstone with woody fragments
14 3600 ft. same lithology as above
13 3500 ft. dark gray, bedded siltstone and sand-
stone with carbonaceous fragments
12 3400 ft. thinnly bedded, concretionary, micaceous
siltstone
1O 26OO ft. gray, micaceous, carbonaceous, poorly
sorted siltstone
9 2400 ft. same as above
8 2300 ft. dark gray, and well bedded,carbonaceous,
fissile siltstone
7 2100 ft. 10 inch coal seam, with associated
massive sandstone
5 1750 ft. blue-gray, poorly sorted sandy siltstone
4 1700 ft. concretionary, dark gray, sandy siltstone
3 1600 ft. thinnly interbedded fine sandstone and
siltstone, possibly graded
2 1500 ft. hard, dark gray, poorly sorted, massive
siltstone
1 800 ft. hard, dark gray, poorly sorted siltstone

PLATES

PLATE 1

Figure
1 Polypodiisporites sp. 1 x500
2 Tiliapollenites indubitabilis
3 Tiliapollenites crassipites
4 Pistillipollenites mcgregorii
5 Sporites cf. vegetus
6 Ilexpollenites iliacus
7 Intratriporopollenites rizophorus
8 Intratriporopollenites rizophorus
9 Cymatiosphaera X500
10 Pollenites oculuS-noctis x500
11 Gothanipollis sp.
l2 Incertae cedis, algal cyst?
l3 Ulmipollenites sp.
l4 Tricolpor0pollenites Sp. 3

All illustrations xlOOO unless otherwise indicated.

 

PLATE l

PLATE 2

Figure

1 Pollenites genuinus

2 Syncolporites sp. 2

3 Syncolporites sp. 1

4 Tricolpites sp. 2

5 Tricolpites sp. 2

6 Rhoipites Sp.

7 Rhoipites sp.

8 Symplocoipollenites Sp. 2
9 Symplocoipollenites
lO Symplocoipollenites
ll Ulmidollenites undulosus
12 Deflandrea sp. x500

l3 Cannosphaeropsis Sp. x500

All illustrations xlOOO unless otherwise indicated.

 

PLATE 2

Figure

\OCDNONUW-PUOID

+4 H F4 +4 P
4:00 ID |'-1 O

H
W

PLATE 3

Ilexpollenites cf. marginatus
Quercoidites henrici

Pollenites cf. ventosus

Cupanieidites cf. orthoteichus
Tricolporopollenites sp. 1
Tricolporopollenites sp. 2
Tricoloporopollenites cf. macrodurensis
Cupanieidites sp. 1
Tricolporopollenites cf. helmstedtensis
Nyssapollenites accessorius
Alangaceoipollenites Sp. 2 x500
Ilexpollenites Sp.

Ilexpollenites Sp.

Symplocoipollenites vestibulum

Liquidambarpollenites cf. mangelsdorfiana

All illustrations xlOOO unless otherwise indicated.

 

PLATE 3

PLATE 4

Figure
l Concavisporites minimus
2 Piceapollenites sp.
3 Tsugaepollenites viridifluminipites x500
4 Tricolpites cf. striatus
5 Tricolpites sp. 4
6 Tricolpites sp. 4
7 Alangaceoipollenites Sp. 1 x500
8 Rhoipites dolium
9 Alnipollenitites versus
10 Symplocoipollenites sp. 1
11 Liquidambarpollenites stigmosus
l2 Quercoidites sp. 2

All illustrations xlOOO unless otherwise indicated.

 

PLATE 4

PLATE 5

Figure

1 Baculatisporis cf. baculatus
Pistillipollenites megregorii
Pistillipollenites megregorii
Caryapollenites spackmanianus
Bombacacidites cf. bombaxoides
microplankton, affinity uncertain x500
Incertae cedis, algal cyst?

Tytthodiscus Sp. x500

\OCDNCDU'I-P‘UOR)

microplankton, affinity uncertain x500

All illustrations x1000 unless otherwise indicated.

 

 

PLATE 5

PLATE 6

Figure
1 Osmundacites wellmanii x500
2 Trilites asolidus x500
3 Trilites asolidus x500
4 Podocarpidites x500
5 Abietineaepollenites microalatus x500
6 Cicatricosisporites cf. hallei x500
7 Momipites coryloides
8 Ilexpollenites inaequaliclaviata
9 Ilexpollenites inaequaliclaviata
lO Pterocaryapollenites stellatus
ll Liliacidites intermedius
l2 Proteacidites terrazus
l3 Ephedra cf. notensis

All illustrations xlOOO unless otherwise indicated.

 

PLATE 6

Figure

\OCD‘QONU'l-P-‘UUM

[...]
O

PLATE 7

Cyclonephelium sp. x500
Wetzellia glabra. x250
Dinoflagellate x500
Microthyriaceae xlOOO
Wetzeliella sp. x500
Deflandrea cf. spinosa x500
Wetzeliella cf. glabra x250
Microthyriaceae x250

fungus x250

fungus x1000

 

PLATE 7

Figure

\OCD'NICMU’IL'UOR)

H r4 +4
n) +4 O

H
LA)

PLATE 8

Polypodiisporites sp. 1
Polypodiisporites cf. favus
Polypodiisporites cf. favus
Trilites cf. paravallatus
Cicatricosisporites cicatricosoides
Cicatricosisporites cicatricosoides
Laevigatisporites cf. pseudomaximus
Polypodiaceoisporites sp.
Polypodiaceoisporites sp.
Foveotriletes crassifovearis
Osmundicites wellmanii
Concavisporites minimodiversus

Concavisporites minimodiversus

All illustrations x500.

 

PLATE 8

Figure

\OCID'KJONU‘l-I—‘UUIU

H r4 14 F1 +4 14 H‘ r4 14 H
\o a: ~q Ch \fl t- U) h) +4 O

PLATE 9

Abiespollenites cf. absolutus x500
Abiespollenites cf. absolutus x500
Abiespollenites cf. absolutus x500
Podocarpidites sp. x500
Tsugaepollenites viridifluminipites x500
Taxodiaceaepollenites hiatus
Quercoidites henrici
Sabalpollenites cf. convexus
Sequoiapollenites Sp.
Taxodiaceaepollenites hiatus
Quercoidites henrici

Castaneoidites cf. exactus
Tricolpites Sp. 3

Ilexpollenites iliacus
Tricolpopollenites cf. retiformis
Tricolpopollenites cf. retiformis
Platanoidites sp.

Platanoidites sp.

Tricolpites sp. 3

All illustrations xlOOO unless otherwise indicated.

 

PLATE 9

Figure

\OCD’QCDU'l-Il’wm

H! r4 14 F1 r4 14
(m 3- O) n) +4 o

[...]
N

PLATE 10

Tricolpites Sp. 1

Tricolpites sp. 1

Tricolpites sp.

Tiliapollenites instructus
Subtriporopollenites cf. constans
Trivestibulopollenites cf. salebrosus
Proteacidites cf. marginus

Bombacacipites cf. nacimientoensis
Rhoipites cf. bradleyensis
Araliaceoipollenites cf. edmundi
Tricolporopollenites satzveyensis

Rhoipites cf. pseudocingulum forma navicula
Rhoipites cf. pseudocingulum forma navicula
Rhoipites pseudocingulum

Rhoipites pseudocingulum

Cupuliferoipollenites cf. pusillus

All illustrations xlOOO

 

' \

 

 

 

PLATE l0

Figure

\OCDK'IONUl-L'UJM

F4 14 r4 +4 F1
3- U) n) +4 O

15

PLATE 11

Nyssapollenites sp. 2

Nyssapollenites Sp. 2

Faguspollenites sp.

Nyssapollenites accessorius
Nyssapollenites cf. Thompsoniana
Symplocoipollenites vestibulum
FaguSpollenites cf. versus
Nyssapollenites sp. 1
Alangiaceoipollenites barhoornianum x500
Cyrillaceaepollenites cf. megaexactus
Sapotaceoidaepollenites cf. sapatoides
Sapotaceoidaepollenites cf. sapatoides
Sapotaceoidaepollenites cf. sapatoides
Pollenites oculus-noctis x500

Pollenites oculus-noctis x500

All illustrations xlOOO unless otherwise indicated.

 

Figure

KOCIDNONU‘l-PUOR)

+4 F4 +4 F4 :4 F4 IA F4 14
a) ~Q (m \fi t- O) n) +4 O

PLATE 12

Myricaeoipollenites cf. megagranifer
Triatri0pollenites rurensis
Betulaceoipollenites bituitus
Betulaceoipollenites bituitus
Engelhardtioidites microcoryphaeus
Alnipollenites versus

Alnipollenites sp.

Caryapollenites simplex

Momipites coryloides

Engelhardtioidites quietus

Ulmipollenites undulosus
Liquidambarpollenites cf. mangelsdorfiana
Liquidambarpollenites cf. mangelsdorfiana
Pollenites anulus

Pterocaryapollenites stellatus
Juglanspollenites versus
Multiporopollenites ludlowensis

Multiporopollenites ludlowensis x1250

All illustrations x1000 unless otherwise indicated.

 

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