DEC 1 a W

ABSTRACT

PALEOECOLOGY OF PALYNOMORPHS

IN THE MANCOS SHALE, SOUTHWESTERN COLORADO
by Gary C. Thompson

TWO stratigraphic sections were measured and sampled for
palynomorphs in the Upper Cretaceous marine Mancos Shale in southwestern
Colorado. The two sections are located about 30 miles apart on a line
that is normal to the trend of the Upper Cretaceous shoreline in this
area. The position of the shoreline relative to all levels in the two
sections was determined from published detailed stratigraphic studies
in the area.

A graphic correlation technique was used to correlate between
the two sections. This correlation was based on the lowest or highest
stratigraphic occurrences of 25 selected pollen and spores.

Distance offshore is reflected in the fossil assemblages when
the data from counts are subjected to factor analysis. By combining the
results of factor analysis of 22 selected microplankton taxa in 72 samples
with results of the correlation a picture is revealed of tranSgressing
and regressing microplankton assemblages within the essentially homo-
geneous marine shale environment. These tranSgressions and regressions
of the assemblages parallel the regressions and transgressions of the
shoreline farther to the south.

The diversity of microplankton tends to vary directly with
distance offshore while the diversity of pollen and spores tends to
vary inversely with distance offshore.

Relative frequencies and numbers per gram of rock of some

palynomorph taxa tend to reflect distance from shore. Among these the

Gary C. Thompson

best correlations exist for the following categories. Classopollis spp.,

 

Tricolpopollenites cf. 2, micromunus, 1, sp. 7, gymatiosphaera Spp.,

 

Form C. sp. 1, acritarchs with processes, chorate dinoflagellate cysts,

microplankton without processes, and cuticle fragments.

PALEOECOLOGY OF PALYNOMORPHS

IN THE MANCOS SHALE, SOUTHWESTERN COLORADO
By

Gary GffiThompson

A THESIS

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

DOCTOR OF PHILOSOPHY
Department of Geology

1969

ACKNOWLEDGEMENTS

This study could not have been accomplished without the assis-
tance that was given so freely to the writer by so many people.

Sincere thanks are given to Dr. Aureal T. Cross, Department of
Geology and Department of Botany and Plant Pathology, Michigan State
University, under whose guidance this study was undertaken and completed.

Dr. Cross, Alan Gnad, Evan J. Kidson and Lee Cook, all of
Michigan State University, assisted in the field.

The Tribal Council of the Ute Mountain Indian Reservation and
the National Park Service permitted sampling on lands under their respec-
tive jurisdictions. '

Dr. Don Merritt, McClure Oil Company, prepared the COVAP com-
puter program for the CDC 3600 computer at Michigan State's Computer
Center. Dr. William C00per, Department of Zoology, Michigan State
University, volunteered the use of the computer program for calculating
diversity indices.

This research was supported in part under a National Science
Foundation grant (Aureal T. Cross, prinicipal investigator). The final

‘phase, including computer time, drafting and reproduction, was supported

by Shell Development Company. J. M. Lampton, P. W. Fairchild, and

Dr. M. R. Thomasson, Shell Exploration and Production Research Center,
Houston, Texas, were especially helpful in seeing this work to completion.
The Department of Geology, Michigan State University, supported part of
the field work.

Evan J. Kidson and J. M. Lampton held valuable discussions
with the writer concerning the interpretation of the data.

Drs. C. E. Prouty, Jane E. Smith, James H. Fisher, Department
of Geology, and Dr. John E. Cantlon, Department of Botany and Plant
Pathology, Michigan State University, in addition to Dr. Cross (Chairman),
served on the advisory committee for this thesis.

ii

TABLE OF CONTENTS

INTRODUCTION . . O . . . ......... I 0000000000000000 . I . . . . . . O . . . . . . . . Q
Purpose .. ........ . ................................ ..
scope ........ OOOOOOOOOOOOOO . . ......... . ....... . ..

Part

1. METHODS ...... 00000000000 . 000000000 O 000000 . 000000 .00....
Field methods . ..................................... .
Maceration procedures ...... .... . ...... . . ..... ..
Mounting techniques ............. . . . ...... ..
Examination procedure . ........................... ...
Photographic techniques ...... .............. . ... ...

II. STRATIGRAPHY ....... ..... 0.... 0000000000000000 .... ..... .
Nomenclature ........... .......... .. ......... . . ...
Description of the rock units in the measured
stratigraphic sections 0 O O O O . . O . . . . . . . . O .
Dakota Group ......O.... OOOOOOOOOOOOOOOO . ...
Naturita Formation ........................ .
Mancos Shale 0.00.0.0....O.... . . . . . I...
Graneros Shale Member ...... .. . . .. ..
Greenhorn Limestone Member ... ........ .. .
Lower Carlile Member ....... ......... .......
Juana Lopez Member 0 . O . . . . O . . O . O . . . . .
Upper Shale Member ....... ............. ....
Mesaverde Group ............................
Point Lookout Sandstone ....................
Correlation of the two stratigraphic sections .......
III. SYSTEMATICS ................... ' .........................

General statement ...........

Systematic descriptions ..... ........................
Group Acritarcha . ........ .... .. . . . ......
Algae ....................... ........... .. . ....

Dinoflagellates . ................ . ..... .....
Other algae .. ........ .... . . ........... ..
Trilete Spores ................... ....... . . .
Monolete spores ................... . ........ .. .
Gymnospermous pollen ... ........................ .
AngiOSpermous pollen ........ .. . ........ . ..

iii

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24
25
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47
53
53
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Part Page
IV. PALEOECOLOGY .....0.0....O..O......O.........O.......... 71

Approaches to studying the relationships between
diSpersed palynomorphs and ocean-bottom
environments ....................................... 71

"Model of tranSgressions and regressions .............. 73
Basis for model .................................... 73
Steeply-dipping "time lines" ....................... 75
The Carlile-Niobrara unconformity .................. 78
Time-transgressive nature of the Juana Lopez

. Member ........................................... 85

V/ Redeposition of palynomorphs ....................... 85
‘ Analysis of the data ................................. 86

Assemblage approach versus taxon approach .......... 86
Factor analysis .................................... 86
Estimation of distance offshore .................... 91
Diversity .......................................... 93
"Paleoautecology" .................................. 96
Distribution of individual taxa .................... 97
Pollen and spores .................................. 99
Microplankton ...................................... 103
Total palynomorphs per gram of rock ................ 112
Ratio of microplankton to pollen and spores ........ 114
Coal particles (2 50 u) per gram of rock ........... 114
Cuticle fragments per gram of rock ................. 114
Interpretation assuming only time-related affects .. 115

Environmental causal factors ........... ...... ........ 116

V. CONCLUSIONS . . . O O . O O . O . O . . . . O O . . . 0 . . . . 0 . . . . . . . . . . . . . . O O . 1 18
REFERENCES I . . O . . . . . . . . . . . . . . . . . . O O . . . . O . O . . O . I . . . . . . . O . . . . O . O . 1 20
APPENDICE S . . . O . O . . O . . . . . . . . . O . . I I . . . . . . . O . . O . O O . . . O . . . . . O . . . . . 1 2 9

PIATES ....O............. ...... ............O.........O......... 162

iv

Figure

10.

11.

12.

13.

14.

15.

LIST OF FIGURES

 

 

Page
Map of Four-Corners Area showing location of
study area, location of measured and sampled
stratigraphic sections, and line of section
A-A’ ShOWI‘l in figure-7............o.......o.........o 3
Map of study area showing location of measured
sections and outcrop of Mancos Shale ................. 4
Curves used to determine sum of palynomorph
counts ........0...................O..............O... 12
Correlation chart showing time relationships of the
rocks in the study area with the European type
section and Western Interior standard section ........ 16
Columnar sections and time correlation between
Point Lookout and Ute Reservation sections ........... 18
Graph of correlation between Point Lookout and
Ute Reservation Sections ....O0.0.........0.0......... 22
Cross-section A-A’ showing the position of the
strandline sandstones and related formations ......... 74
Diagrams illustrating the development of a elastic
wedge, and the "time lines" within it ................ 76
Local range chart for palynomorphs in the
Point Lookout section ............... ....... .......... 81
Local range chart for palynomorphs in the Ute
Reservation section .................................. 83
Diagram showing the results of factor analysis ....... 90
Curves used for determining distance offshore for
eaCh sample .......O.... ...... ........................ 92
Diversity of microplankton and of pollen and spores
plotted against distance offshore .................... 95
Relative frequency and number per gram of rock of
,fllasfigpgllis spp. and of bisaccate grains plotted
against distance offshore ............................ 100
Relative frequency and grains per gram of rock of
Inaperturopollenites sp. 1 and of Tricolpites cf.
.1° micromunus plotted against distance offshore ...... 102

 

Figure

16.

17.

18.

20.

21.

22.

23.

Page

Relative frequency and numbers per gram of rock
of Tricolpopollenites sp. 7 and of Michrystridium
spp. plotted against distance offshore ............... 104

 

 

Relative frequency and numbers per gram of rock
of QymatiOSPhaera Spp. and of Form C sp. 1 plotted
against distance offshore .... ...... .................. 105

 

Relative frequency and numbers per gram of rock
of fiystrichosphaera spp. and of Palaeohystrichophora
infusoroides plotted against distance offshore ....... 106

 

 

 

Relative frequency and number per gram of rock of
Dinogymnium sp. 1 and of proximate and cavate cysts

 

plotted against distance offshore . ...... ...... ..... .. 107

Relative frequency and number per gram of rock of
acritarchs without processes and of microplankton
Without processes ......O........ ....... ......O....... 108

Relative frequency and number per gram of rock
of chorate cysts and of acritarchs with processes .... 109

Relative frequency and number per gram of rock of
microplankton with processes ......................... 110

Log palynomorphs per gram, log coal particles
10 . $0
per gram, log cuticle fragment per gram and
ratio of microplankton to pollen and spores all
plotted against distance offshore .................... 113

vi

LIST OF APPENDICES

Appendix Page
A. Measured Stratigraphic Sections .. ..... . ....... ....... 130
B. List of Raw Data ... ............ ................ ...... in
pocket

vii

INTRODUCTION

Purpose

The purpose of this investigation is to determine if fossil
palynomorph Species or fossil palynomorph assemblages reflect in any way
their sedimentary environment as it can be interpreted from the lithology
and facies relationships of the rocks that contain them. This is another
approach to the classic problem of separating those variations in fossil
assemblages through time that are due to reversible environmental change
(facies change) from those that are due to irreversible changes such as
evolution. Rather than seeking out only irreversible evolutionary or
phytogeographical changes in the palynomorph assemblages that can be
used for time correlation, the reversible environmentally-controlled
changes in assemblages will be sought out in an effort to determine if
some palynomorphs or palynomorph groups might be restricted in such a
way that they could be employed as "environmental indicators." In addi-
tion, some insight into the autecology of some fossil palynomorphs might

be gained.

Scope

The Upper Cretaceous rocks of the Western Interior of the
United States contain a remarkable record of the transgressions and
regressions of the shoreline of an epicontinental sea. This sea at
times connected the Arctic Ocean with the Gulf of Mexico. At other
times it was limited to an embayment of the Gulf and/or the Arctic
Ocean (Reeside, 1957). As a result of the variation in areal extent
and the influence of northern or southern waters, fluctuations occurred
in temperature, salinity, water depth, turbidity and other parameters of

the marine environment. Consequently these changes and the tectonic

and/or eustatic movements related to them are reflected in the sedi-
ments that were laid down at that time - reflected not only in the
inorganic detritus but in the organic remains as well.

Over the years many stratigraphic sections have been measured
throughout the Cretaceous of the Western Interior. Utilizing the abundant
fossil mollusks for correlation, a detailed record has been compiled of
the events of onlap and offlap of the Cretaceous shoreline (Weimer, 1960;
Reeside, 1957; Young, 1955, 1957, 1960; and others).

Because of this remarkable record of events, the site of this
study was chosen in this area and in these rocks. Two stratigraphic
sections were measured in southwestern Colorado through Upper Cretaceous
marine shales of the Mancos Shale (figs. 1 and 2). One section, here
called the Point Lookout section, was measured at Point Lookout in Mesa
Verde National Park, and is located in sections 26, 29, and 31, T. 36 N.,
and sections 5 and 6, T. 35 N., R. 14 W., Montezuma County, Colorado.

The other section, here called the Ute Reservation section, is located
within the boundaries of the Ute Indian Reservation in sections 9, 10,
11, 12, 13, 16, T. 32 N., R. 18 W., sections 9, 16, 20, 21, T. 32 N.,

R. 19 W., and section 18, T. 32 N., R. 17 W., Montezuma County, Colorado.
These sections are approximately thirty miles apart and are on a line
that is normal to the shoreline trend during the Late Cretaceous. The
rock record contained in the two sections includes two major shoreline
transgressions-regressions within which five minor transgressions-
regressions are contained.

Samples for palynomorphs were taken at closely Spaced intervals
throughout both sections so that the palynomorph assemblages would be
sampled through the entire time interval at various stages of shoreline

transgression or regression. Ideally, the study of many more such

 

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FIGURE l.--Map of Four-corners Area showing location of study area (cross
hatching), location of measured and sampled stratigraphic sections and
line of section A-A’ shown in figure 7.

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stratigraphic sections would be desirable in order to determine the
true distribution of the palynomorphs, but reasonable time limitations
allowed for the study of only two sections.

The inferred evolutionary or phytogeographical changes that
took place during the Upper Cretaceous in this area are utilized for
time correlation. Ranges of selected land-derived palynomorphs are
used to achieve relatively fine time control. This is essential in
delimiting within the rocks the "time surfaces" across which variations
in the environment may be expected.

Basic to all of these interpretations is a consistent taxonomy
of the microfossils.

It follows then that there are four essential parts of this
study. These are (1) a taxonomy of the fossil palynomorphs, (2) a time
correlation, (3) an environmental interpretation of the rocks based on
lithology and facies relationships, and (4) a correlation of the variations
in palynomorphs and palynomorph assemblages with variations in the

environments interpreted in (3).

I. METHODS

Field Methods

Because the rocks in the area of study are essentially hori-
zontal, most of the two stratigraphic sections was measured using a
hand level. In the upper part of the Ute Reservation section dips
reached 10° and the use of the Brunton compass was required. Small
measurements were made by sighting over a graduated mattock handle or
over a tape measure. A composite sample was collected every 16 1/2 to
17 1/4 feet (three eye-heights using the hand level) and at every marked
change in lithology. To sample shale a trench was made that was long
enough to expose five feet of vertical section (less where the exposure
was poor) and deep enough, where possible, to reach mechanically-
unweathered rock. From this trench were picked about two pounds of
shale pieces representing all minor variations in lithology over the
five-foot interval.

The limestones in both sections are generally less than two
feet thick. Samples of these limestones consist of chips that were
taken a few inches apart in a vertical line across the bed. When an
interval containing concretions was encountered, the nearest concretion
was sampled by breaking off a few chips from freshly exposed surfaces.

Shaly partings in sandstones were sampled over their entire
thickness. No well-sorted, quartzitic sandstones were sampled.

The fresh samples were placed in cloth sample bags. Later
these bags were wrapped in several thicknesses of newsprint for.their

transport.

Maceration Procedures

In the laboratory a total of 234 samples were selected from

the suite of samples brought from the field. These samples were selected

at approximately a fiftyefoot interval through both sections and at

important lithologic changes. Each sample was subjected to the following

treatment:

1.

10.

Crush the whole sample into pieces about one-fourth inch in largest
dimension (avoid powdering). Use a large mortar and pestle and a
pounding motion.

Mix the crushed sample thoroughly by placing it in a cone-shaped
pile on a clean surface. Then scoop repeatedly with a Spatula
from the bottom of the pile and dump at the top of the pile.

Remove the desired amount (10 grams of limestone, 5 grams of shale)
for maceration by scooping from the flank of the pile.

Place the sample in a 250 m1. plastic beaker and cover the sample
to a depth of three-fourths inch with 10% hydrochloric acid and
replenish the concentration, if needed, until effervescence ceases.
Wash the residue three times with distilled water.

Slowly add hydrofluoric acid to the residue, agitating constantly,
until the residue is covered by about one inch of liquid. Allow
the beaker to sit 24 hours, agitating frequently for the first one-
half hour, then occasionally during the remaining period.

Wash the residue three times in distilled water.

Transfer the residue to a 90 ml. glass centrifuge tube.

Add 25 m1. Schulze's solution (one part concentrated nitric acid

to seven parts saturated potassium chlorate solution) and place

the tube in a hot water bath for 15 minutes agitating frequently.

Wash the residue three times in distilled water.

11.

12.

13.

14.

15.

16.

17.
18.

19.

20.

21.

6

Add 25 m1. 5% potassium hydroxide solution to the residue and
place the tube in a hot water bath for five minutes, agitating
frequently.

Wash the residue in distilled water three times (or as many times
as necessary to obtain a colorless supernatant liquid).

Transfer the residue to tapered 40 ml. glass centrifuge tube and
add 13 m1. zinc chloride solution (sp. gr. 1.80) to the residue,
mixing it thoroughly.

Place tube in a centrifuge (International Centrifuge Model K) and
centrifuge at 1600 rpm for 15 minutes.

Pour the suspended residue and supernatant into a 90 ml. glass
centrifuge tube and fill the tube with distilled water, mixing
thoroughly.

Place the tube in the centrifuge and centrifuge for seven minutes
at 1300 rpm.

Wash the residue three times with distilled water.

Transfer the residue to a 15 ml. tapered glass centrifuge tube.
Add five drops of 2% alcohol solution of Safranin "O" and then
two drops of 10% ammonium hydroxide solution to the residue,

allow to stand for 1 1/2 hours with occasional agitation.

‘Wash residue with distilled water.

Transfer the residue to a 2 dram vial and add 1 ml. of Cellosize

solution containing 2% phenol.

Mounting Technique

Of the 234 samples that were macerated, the residues of 157

were mounted on slides. These 157 residues were selected as representa-

tive of the two sections as time became a factor in restricting the

number of samples that could be studied. These residues were mounted

according to the following procedure.

Add distilled water to the residue in the vial until the density of
the suspended residue is suitable for one drop per slide.

Extract the suspended residue from the vial into a Pasteur

capillary pipette equipped with a 1/4 oz. rubber bulb and count the
number of drops of suspended residue as they fall with a regular
frequency as the pipette is emptied back into the vial. Record the
number of drops.

Prepare the microscope slides by cleaning the slide and cover slip
with a dust-free cloth and then temporarily anchoring the cover slip
to the slide with a fraction of a drop of distilled water.

Place two drops of a Cellosize (hydroxyethyl cellulose) solution on
the cover slip (see Jeffords and Jones, 1959).

Thoroughly mix the suSpended residue in the vial by a pumping action
with the pipette and bulb. When a uniform suspension is obtained,
quickly take up about 1/3 of a pipette of the suspension and transfer
one drop to the Cellosize solution on the cover slip letting the
drop free-fall from the pipette. Repeat this step for each drop
that is transferred. Record the number of drops that are placed on
the slide.

Rinse the pipette into the vial with a few mls. of distilled water.
Using a clean flat toothpick thoroughly mix the residue and the
Cellosize solution on the cover slip and strew it evenly over the
cover slip to within 1/2 mm. of the edge.

Cover the slide and cover slip and allow the water to evaporate

from the residue leaving a hard film on the cover slip.

Remove the cover slip from the slide and wipe the slide dry with a

dust-free cloth.

10

10. Place three drops of a 70% toluene solution of canada balsam on
the center of the slide.
11. Place the cover slip film—side down onto the canada balsam solution
and center the cover slip on the slide. Move any bubbles to the
edge of the cover slip by pressing on it with a toothpick.
12. Allow the slides to dry for 24 hours in a 60° C. oven before attempt-
ing to examine them with oil-immersion objectives.
Of these 157 residues that were mounted, 72 of them were used in the study.
This smaller number of samples resulted from discarding those samples with
low yields or poor preservation of palynomorphs and from time limitations
for examining each sample critically. Few, if any, samples could be con-

sidered totally barren.

Examination Procedure

Before any counts were made, preliminary examinations made
possible the differentiation of most of the taxa of palynomorphs which
are present in the samples.

A sum of 500 palynomorphs was counted from each sample. This
sum included all palynomorphs that were preserved well enough to permit

identification to about the genus level. Because Michrystridium spp.

 

are extremely abundant so as to "dilute" the frequencies of other paly-
nomorphs in some samples and are rare in others, the taxon was excluded
from the sum. Other categories that were counted in addition to those
within the sum of 500 reflect various stages of corrosion. These cate-
gories are: corroded trilete spores, corroded monolete spores, corroded
bisaccate pollen, corroded tricolpate pollen, corroded triporate pollen,
corroded monocolpate pollen, corroded pollen, corroded pollen or Spore

and corroded microplankton.

11

The sum of 500 was selected after first plotting a curve of
the number of species encountered against the number of Specimens iden-
tified in a sample, preferably one with a large number of taxa. These
curves are similar to Species-area curves used in terrestrial plant
ecology to determine number and size of sample quadrats. Such curves
for two samples are shown in figure 3. The dashed line on the graphs
represents the probable shape of the curve if a truly random distribution
of the residue were on the slide. The dashed lines were constructed
free-hand by arbitrarily removing the major diSplacements in the line
of points. Differential sorting of particle sizes on the cover slip
appears to be the main cause of these displacements in the curve. In
these samples the tiny Specimens of Michrystridium Spp. were counted.
They are abundant and tend to be predominant near the edges of the cover
slip. Whether this is due to movement of larger particles to the center
of the cover clip or of smaller particles to the edges or both has not
been demonstrated.

A Sum that lies to the right of the sharp change in slope on
the curve (represented by the points) would tend to include most of the
taxa in the sample. Five hundred lies well to the right of the point.

Another curve was also referred to before selecting the sum. This
curve is from a set of curves that was constructed by Rittenhouse (1940)
to determine the proper number of heavydmineral grains to be counted.
These curves show the relationship between the probable error in per-
centage calculations and the number of grains that are counted. As
shown in these graphs the calculation of percentages based on a sum of
500 would result in a probable error of t 0.7% for a calculated 5.0%,

t 1.57. for a calculated 50.07. and t 0.97. for a calculated 90.07..

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13

This indicates the reliability of interpretations made using low per-
centages of palynomorphs. For the purposes of this study the precision
does not increase appreciably above sums of 500.

In counting the 500 specimens an intuitively prescribed pattern
of traversing the cover slip was devised in an attempt to produce a
random sample. The order of counting and position of the traverses
was set. At least five traverses were made and no more than 100 Specimens
were counted in any one traverse. If 100 Specimens were encountered
before completing a traVerse, the position of the one-hundredth specimen
was recorded and the next traverse in the pattern was begun. Counting
was carried out under a magnification of 800x. When 500 well-preserved
Specimens had been counted the fraction of the total area of the cover
slip that was examined was recorded. Knowing (l) the mass of rock that
was macerated, (2) the number of drops of suSpended residue in the vial
at the time the slide was prepared and (3) the number of drops of suSpended
residue that were placed on the cover slip; an estimate of the number of
well-preserved palynomorphs per gram of rock can be calculated using the

following formula (see also Traverse and Ginsburg, 1966):

Dr x T
G x Dc x Tc

 

Number per gram = 500

where G = grams of rock macerated
Dr = number of drops of residue in vial

Dc = number of drops of residue placed on the
cover slip

T a number of traverses necessary to cover the
whole cover Slip

Tc 2 number of traverses counted to reach sum
of 500

The total palynomorphs (including corroded categories) per gram was also

calculated by substituting a larger sum for 500 in the formula.

14

In addition the slides were scanned until at least 2000
identifiable specimens had been examined from each sample. This estab-
lished somewhat of a standard for determining first and last occurrences
(an "occurrence" being at least one in 2000 or .05%). Statistically,
at the .99 confidence level an occurrence would be about 0.2% or one

in 500.

Photographic Techniques

Photographs of palynomorphs were taken with a Leitz Orthomat
automatic camera attached to a Leitz Ortholux microscope or a Zeiss
GFL Standard microscope. Adox KB-l4 film was used and developed with
Kodak Microdol developer. The prints were made on Kodabromide F-2, F-3,
and F-4 and Adox bromide F-S papers. The prints were developed using
Kodak D-76 developed. The original magnification of the palynomorphs

was 1000K or 540x.

\

II. STRATIGRAPHY
Nomenclature

The Mancos Shale was named by Cross (1899) for a sandy gray shale
about 2000 feet thick exposed in the Mancos River Valley in southwestern
Colorado. Since that time lithologic units have been separated from this
mass of shale and the Upper Cretaceous rock units east of the RoCky Moun-
tains have been extended into the Mancos area. There is some controversy
about the rock units that make up the old Mancos Shale (Dane, Kauffman, and
Cobban, 1968, p.16) and the nomenclature as used here is tentative. The
names and age relationship used in this study are shown in figure 4. This
follows the nomenclature of Dane (1960) except for the use here of the term
"Upper Shale Member" of the Mancos to include Dane's Upper Carlile Member,
Niobrara Shale Member and Upper Shale Member. This term is used here be-
cause it is felt that in the two sections measured in this study the units
referred by Dane and Lamb (1968) to the Niobrara and Carlile are indistin-
guishable from the Upper Mancos Shale Member.

The name "Tocito Sandstone" of Lamb (1968) is not applied in the
two sections studied here. No sandstones were found just above the Juana
Lapez in either section. The Tocito sandstone has a patchy distribution and
extends across the San Juan Basin to the south-east. It is considered to be
a transgressive sandstone laid down on a Carlile-Niobrara unconformity (Dane,
1960; Lamb, 1968). Lamb traces this unconformity into the vicinity of the
Ute Reservation section but is unsure of its position and magnitude in the
Point Lookout section. As interpreted in this study the unconformity is
considered to be absent or to be represented by only a small diastem at Point
Lookout. This interval and the problems it presents in environmental inter-

pretations will be discussed later.

15

 

 

 

 

 

 

 

 

 

 

 

 

 

 

   

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

PEA STANDARD NORTHERN SAN JUAN
EURO N FOR WESTERN
STAGES INTERIOR BAS|NI9:OMEsSA VERDE AREA
DANE A
COBBAN B REESIDE , |952 MODIFIED BY LAMBI967 THIS STUDY
< EAGLE § 55
5;; a 908‘ UPPER a
2 TELEGRAPH OR 2 ,
FORMATION L4 MANCOS SHALE ,2.
SANTONIAN MEMBER
S SMOKY UPPER
*- HILL NIOBRARA SHALE
g CHALK MEMBER MEMBER
‘t MEMBER
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TURmIAN 2 a H-UE HILL. 8" H LOWER cARLILE m LOWER CARLILE
a: g 3 FAIRPORT cm. M 8 "5"“ 8 "“35"
"15T GREENHORN
§ 5’ 5.1 ”5 FF“ ‘- - c2: 3E:&N MEM. g LIMESTONE MEM.
0 m2 JETMORE can. M. < 2
3 §§ W 2 GRANEROS GRANEROS
NC a .
LI OLN L M SHALE SHALE
MEMBER MEMBER
CENOMANIAN BELLE FOURCHE
SHALE
DAKOTA GROUP DAKOTA GROUP

 

 

 

 

 

 

WOOOO’IO

FIGURE 4.--Correlation chart showing time relationships of the rocks in
the study area with the European type section and the Western Interior
standard section.

17

Description of the Rock Units in the Measured Stratigraphic Sections

A detailed description of both stratigraphic sections is given in
Appendix I. Stratigraphic Columns of the two sections are presented in

figure 5.

Dakota Group

Naturita Formation - The Naturita Formation of the Dakota Group
(Young, 1960) consists of massive to thin-bedded sandstones interbedded with
gray shales and coals in the vicinity of the measured sections. It is over-
lain by the clearly-demarcated sandy shales of the Graneros Shale. Only the

upper few feet of Dakota rocks were measured and sampled in this study.

Mancos Shale

Graneros Shale Member - In both sections the Graneros Shale Member
consists of sandy shale which immediately overlies the Dakota and becomes
less sandy upwards. At Point Lookout the member is 104 feet thick and all
but the lower 45 feet is calcareous. In the Ute Reservation section the
entire unit, about 65 feet thick, is calcareous. The lower non-calcareous
part of the formatiOn at Point Lookout may be older than the base of the
Graneros in the Ute Reservation section. This is indicated by the position
of lowest occurrences of three palynomorphs at lower relative positions in
the Ute Reservation section than in the Point Lookout section. Numerous
thin bentonites, large limestone concretions, and thin, light to medium-gray,
lenticular limestones occur in the upper part of the Graneros Shale Member
in both sections.

Greenhorn Limestone Member - The Greenhorn Limestone Member con-
sists of fine-grained, gray limestones one inch to one foot thick that are
interbedded with calcareous gray shale. The thickest limestones occur near
the top of the unit. The Greenhorn is 35 feet thick in the Ute Reservation

section and 20 feet thick at Point Lookout. It is gradational with the

19

Graneros Shale Member below and the Lower Carlile Member above. gryphaea
newberryi is abundant in the lower one-half of the Member.

Lower Carlile Member - The Lower Carlile Member consists of about
300 feet of gray and olive-gray shale in both sections. Widely-spaced thin
limestones and large limestone concretions occur in the upper 250 feet.

The shale is calcareous only in the lower 50 feet. At the base is a two-
inch thick calcarenite containing animal trails.

Juana Lopez Member - The Juana LOpez Member is characterized by
thin, hard calcarenites one inch to two feet thick that weather brownish-
red, contain abundant fossils and have a petroliferous odor. Although this
unit is characterized by these calcarenites it consists mainly of gray
shale between the calcarenites (Dane, et a1, 1966). The interval here
assigned to the Juana LOpez is 106 feet thick in the Ute Reservation
section and 64 feet thick at Point Lookout. It is gradational with the
rocks above and below.

Upper Shale Member - The term "Upper Shale Member" is used here
to include all of the Mancos Shale above the Juana LOpez Member. The Upper
Carlile Member, the Niobrara Shale Member and the Upper Mancos Shale Member
of Dane (1960) and Lamb (1967) are included in this unit. It consists of
gray and olive-gray calcareous and non-calcareous shales interbedded with
widely-spaced lenticular limestones and large limestone concretions. This
member is about 1550 feet thick at Point Lookout and about 1100 feet thick
in the Ute Reservation section. The upper part is interbedded with the
quartz sandstones of the overlying Point Lookout Sandstone. Below, it has a

gradational contact with the Juana LOpez Member.

Mesaverde Group
Point Lookout Sandstone - The Point Lookout Sandstone intertongues

with the upper part of the Mancos Shale. The contact between the two forma-

20
tions is placed just below the lowest massive sandstone above which sand-
stone predominates over the interbedded shale. Most of the Point Lookout
is a massive cliff-forming sandstone with occasional very-thin shale part-
ings. The only samples from the Point Lookout that were examined were from

shale partings near the contact of the formation with the Mancos.
Correlation of the Two Stratigraphic Sections

The graphic correlation method was used to correlate between the
two stratigraphic sections in this study. This method was introduced by
Shaw (1964) and is explained in detail by him. Briefly, the method consists
of plotting the stratigraphically lowest and highest occurrences of taxa on
a graph the abscissa of which is the stratigraphic thickness (in feet) of
one section and the ordinate of which is that of a second stratigraphic
section. For example, the lowest occurrence (bottom of local range) of a
species might be at 500 feet above the base of the Point Lookout Section
while the lowest occurrence of the same species is at 200 feet above the
base of the Ute Reservation section. This would be plotted as a point with
coordinates (500,200). All true lowest and highest occurrences (tops and
bottoms of local ranges) of the species or other taxa that are found in the
two sections are plotted in the same manner. The line that is fitted to
these points is called the "line of correlation" and is identical with the
regression line used in statistics. Because this correlation is statistical
one may correlate any level in one section with its assumed time-correlative
level in another section and be able to give in feet the confidence limits
of such a correlation.

The graph of correlations of the Point Lookout section and the
Ute Reservation section is shown in figure 6. The correlation line is in

two parts. The displacement in the line is interpreted to be the result

21

of a great difference between the sedimentation rates at the two sites.
Because there is a certain error in such a purely statistical correlation
(the solid line) the rock column must of course be compared with it.
Slight adjustments in the graphic correlation of the sections were made
after the positions of transgressions and regressions as reflected in the
factor analysis (to be discussed below) were considered. The resulting
correlation (shown by the dashed line in figure 6) is still within the
95% confidence limits of the original line of correlation as shown in
figure 6. The correlation of the Point Lookout and Ute Reservation sec-
tions is shown in figure 5. This diagram incorporates the correlation
line and the factor analysis interpretations. The correlation shown will
be referred to later in the discussion of environmental interpretations.

The highest and lowest stratigraphic occurrences of 25 taxa
were selected for the construction of the line of correlation. These taxa
were selected because (1) they are morphologically distinctive and (2)
their highest and/or lowest occurrence is well established within both
sections. The species or other taxa used in this correlation are listed
below.

Inaperturopollenites sp. 3

Classopollis sp. 1

Quadripollis krempii Drugg

Triatriopollenites cf.‘T. rurensis Pflug and Thompson

Tricolpopollenites sp. 4

2. sp. 8

?Trialapollis sp. 1

Retitricolpites cf. .3. georgensis Brenner

Duplopollis cf. ‘2. orthoteichus (Cookson and Pike) Krutzch

large Tricolpites cf. ‘3. explanata (Anderson) Drugg

Hexacolpate pollen grain

Tripor0pollenites cf. [2. scabrqporus Newman

‘2. cf. .2. scabroporus Newman (with annulus)

2, cf. tectus Newman

1, sp. 1

Sporopollis lagueaeformis Weyland and Greifeld
Conclavipollis cf. .9. wolfcreekensis Newman

 

 

22

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23

?Plicapollis silicatus Pflug

Labrapollis globosus Krutzsch

Proteacidites thalmanii Anderson, var. l

P. thalmanii var. 2

P. thalmanii var. 4

Peromonolites peroreticulatus Brenner

?Extratriporopollenites spp.

Trudopollis cf. ‘E. hemiparvus Pflug

Only land-derived pollen and spores were used in an effort to
eliminate some of the error in the time correlation that is due to environ-
mental influences. The distribution of a phytoplankton species is probably
more directly controlled by the marine environment than are pollen and
spores. The phytoplankton respond as living organisms to the marine en-
vironment whereas the pollen and spores respond merely as sedimentary part-

icles. The lowest occurrences (bases) of each taxon in the list were utir

lized except Peromonolites peroreticulatus whose highest occurrence (top)

was used.

III. SYSTEMATICS
General Statement

Identification of the palynomorphs was difficult because they
were often poorly preserved. This has limited the number of taxa repre-
sented in this treatment for two reasons. (1) Specimens were simply
too poorly preserved to be identified. (2) To be able to compare all
samples with each other and to follow the changes in abundance of each
taxon from sample to sample one must be able to recognize the same taxa
in all the samples. Therefor the Splitting was limited by the "weakest
link" - the most poorly preserved sample.

A common damage to the palynomorphs was due to crystal growth
within the central cavity and within the wall. Walls were often punctured
in the six-sided outline that is attributable to the growth of pyrite
crystals (Neves and Sullivan, 1964).

In the systematic treatment that follows, question marks and
"cf." are used frequently. In some cases this reflects the poOr preserva-
tion and the necessary lumping that was done to facilitate the sample
comparisons for paleoecological interpretations. In other cases it
reflects an inadequate knowledge of type specimens which results in
unsure identifications.

Because this is not primarily a taxonomic study the treatment
is brief.

Qualitative terminology for abundance is as follows: Rare,
.05 to 1%; common, 1 to 2%; frequent, 2 to 10%; abundant, greater than

10%.

24

 
 

Plus Q

.8 15

R. I: ~

25

Systematic Descriptions
INCERTAE SEDIS

Group ACRITARCHA

Subgroup ACANTHOMORPHITAE Downie, Evitt and Sarjeant, 1963

Genus Baltisphaeridium Eisenack, 1937, emend.
Downie and Sarjeant, 1963

Baltisphaeridium cf. B. ypensis Wall, 1965
P1. 1, Fig. l

Occurrence: rare, in lowest 200 feet of both sections.

Reference specimen: slide Pb6273-4, 50.3 x 96.4

Baltisphaeridium cf..§. infalatum Wall, 1965
Pl. 1, Fig. 2

Occurrence: rare to abundant (sample Pb6222), in Lower Carlile Member,

Juana Lopez Member, lower part of upper Carlile Member.

Reference specimen: slide Pb6273-3, 46.7 x 93.1

Baltisphaeridium sp. 1
Pl. 1, Fig. 3

Diagnosis: Central body spherical,ellipsoidal to pear-shaped; psilate
to granular (corroded?); processes numerous (ca. 50), tapering solid

(?), with flat flared tips; diameter of central body 30 to 40 u; pro-
cesses about 10 to 12 u long.

Occurrence: rare to frequent, throughout section

Reference specimen: slide Pb638703, 39.5 x 93.2

Genus Michrystridium Deflandre, 1937, emend.
Downie and Sarjeant, 1963

Michrystridium spp.
Pl. 1, Figs. 4-7

 

...
.-

 

26

Occurrence: rare to extremely abundant, throughout section

Reference specimens: slide Pb6273-1, 33.5 x 93.7, 33.2 x 99.0; slide
Pb6368-9, 34.0 x 106.5.

 

Remarks: Numerous species of this genus were encountered in the Mancos.
Because of the varied degree of preservation of these very small forms
consistent identification could be made only to genus.

Form N sp. 1
Pl. 1, Fig. 10

Diagnosis: circular in outline; densely covered with fine hairs about
3 u long; overall diameter about 20 u.

Occurrence: rare, Lower Carlile Member in Ute Reservation section,
Upper Shale Member of both sections.

Reference specimen: slide Pb6340-6, 125.8 x 30.5.

 

Form L sp. 1
P1. 1, Fig. 9

Diagnosis: rounded pentagonal in outline; covered with hairs; overall
diameter about 25 u.

Occurrence: rare, in Lower Carlile Member and Upper Shale Member.
Reference specimen: slide Pb6357-7, 33.4 x 93.1.

Form X sp. 1
P1. 1, Fig. 8

Diagnosis: oval in outline; "periphragm" held up by numerous crowded
very short (1—2 u) processes; overall diameter 15-20 u.

Occurrence: rare to abundant, throughout sections except upper part of
Upper Shale Member of Mancos.

Reference specimen: slide Pb6337-7, 34.1 x 100.4.

Form S sp. 1
P1. 1, Fig. 12

Diagnosis: Spheres, 5 to 20 u in diameter; densely covered with tiny
spines less than one micron long, wall thin.

Occurrence: rare to frequent, throughout sections.

Reference specimen: slide Pb6351-7, 38.3 x 105.5.

 

Form S sp. 2
P1. 1, Fig. 14

27
Diagnosis: Spheres, greater than 20 u to about 35 u in diameter; covered
with tiny spines, but more widely spaced than in species 1, wall thick.
Occurrence: rare to common, in Upper Shale Member of the Mancos.
Reference specimen: slide Pb6282-6, 37.1 x 90.9.

Form T sp. 1
P1. 1, Fig. 11

Diagnosis: spherical, about 30 to 40 u; granulate with very short hair-
like extension on each granule giving the appearance of "terry cloth".

Occurrence: rare to common, throughout sections except for the upper
part of the Upper Shale Member of the Mancos.

Reference specimen: slide Pb6295-6, 114.5 x 43.7.
Subgroup POLYGONOMORPHITAE Downie, Evitt and Sarjeant, 1963
Genus Veryhachium Deunff, emend. Downie and Sarjeant, 1963
Veryhachium cf. 2. eurogeaum Stockmans and Williere, 1960

P1. 1, Fig. 16

Occurrence: rare to abundant (lowest sample in each section), through-
out section except for the upper part of the Upper Shale Member.

Reference specimen: slide Pb6227-10, 29.4 x 118.1.

Remarks: The specimens in the Mancos are consistently smaller than the
specimens described in the literature as this species.

Veryhachium cf. stellatum Deflandre, 1945

..‘_’-______
P1. 1, Fig. 13

 

Occurrence: rare (Pb6262) and abundant (Pb6932) in its only two occur-
rences, one in the Graneros Shale and one in the Lower Carlile Member
of the Mancos Shale.

Reference specimen: slide Pb6273-3, 41.8 x 102.0.

Veryhachium sp. 1
P1. 1, Fig. 15

 

Diagnosis: Central body slightly polygonal spheroid; psilate; processes
5 to 7, tapering, with acuminate tips, some curved, solid, with inden-
tation of body cavity into bases a few microns; central body about 15

28

to 22 u in diameter, processes about 12 to 15 u long.
Occurrence: rare, in two occurrences in the Graneros Shale.

Reference specimen: slide Pb6227-10, 114.5 x 43.9.

Subgroup NETROMORPHITAE Downie, Evitt and Sarjeant, 1963
Genus Leiofusa Eisenack, 1938
and
Genus Metaleiofusa Wall, 1965
Leiofusa spp. and Metaleiofusa spp.
P1. 1, Fig. 18
Pl. 2, Fig. 1

Occurrence: rare, in Graneros Shale, Greenhorn Limestone and Lower
Carlile and Upper Shale Members of the Mancos.

Reference specimens: slide Pb6357-10, 40.9 x 91.7, Pb6227-10, 112.8 x
44.0.

Remarks: Specimens identified with these two genera were grouped because
the state of preservation did not always permit determination of the
number and position of the processes.

Subgroup HERKOMORPHITAE Downie, Evitt and Sarjeant, 1963

Genus_§ymati9§phaera O. Wetzel 1933,
emend. Deflandre, 1954

gymatiosphaera spp.
P1. 2, Figs. 2,5

_ Occurrence: rare to abundant, throughout the sections.
Reference specimens: slide Pb6273-l, 33.9 x 99.3, Pb6273-l, 33.7 x 97.2.
Remarks: Specimens identified with this genus were not determined to
species.
Subgroup PTEROMORPHITAE Downie, Evitt and Sarjeant, 1963
Genus Pterospermopsis W. Wetzel 1952

Pterospermopsis SPP-
Pl. 2, Fig. 3

Occurrence: rare to abundant, throughout sections except upper part of
Upper Shale Member at Point Lookout.

29

 

Reference specimen: slide Pb6273-2, 49.0 x 98.4.
Subgroup SPHAEROMORPHITAE Downie, Evitt and Sarjeant, 1963

Within this subgroup are placed several smooth, granular, or low-spinned
spherical, discoidal and ellipsoidal forms. They are referred to by
informal code names only.

Form B sp. 1
Pl. 2, Fig. 7

Diagnosis: smooth to faintly granular or with scattered granules; 30 u
to 40 u spheres; often broken and/or folded, thin-walled.

Occurrence: common to abundant throughout section.

Reference specimen: slide Pb6871-2, 38.0 x 88.6.

 

Form B sp. 2
P1. 2, Fig. 6

Diagnosis: granular to coarsely granular, 30 u to 55 u spheres; often
broken and/or folded, thin-walled.

Occurrence: rare to abundant, throughout sections.
Reference specimen: slide Pb6337-8, 46.4 x 92.4.
Form B sp. 3
P1. 2, Fig. 4

Diagnosis: smooth to granular, 20 u to 30 u spheres; sometimes wrinkled
and folded, thin-walled.

Occurrence: abundant throughout sections.

 

Reference specimen: slide Pb6273-1, 35.4 x 91.4.

 

Form B sp. 4
P1. 2, Fig. 8

Diagnosis: smooth, 60 u to 70 u, ellipsoidal, wrinkled, thin-walled.

Occurrence: rare to common (abundant in sample Pb6902), in Lower Carlile
Member and Upper Shale Member of Mancos.

 

Reference specimen: slide Pb6900-2, 38.9 x 91.1.

30

Form C sp.l
Pl. 2, Fig. 10

Diagnosis: smooth, 15 u to 20 u, discoid to spherical, with medium to
thick wall.

Occurrence: common to abundant throughout section.

Reference specimen: slide Pb6902-6, 115.7 x 31.3.

 

Form C sp. 2
P1. 2, Fig. 9

Diagnosis: smooth, less than 15 u, spherical, with medium wall thickness.
Occurrence: rare_to abundant throughout sections.

Reference specimen: slide Pb6273-1, 36.1 x 87.4.

Form C sp. 3
P1. 2, Fig. 11

Diagnosis: smooth, 25 u to 35 u, spherical, thick-walled, characteris-
tically a fold in surface.

 

Occurrence: rare to common, in Lower Carlile, Juana Lopez and Upper
Shale Members of Mancos. '

Reference specimen: slide Pb6223-2, 43.4 x 101.4.

 

ALGAE

DINOFLAGELLATES

Family Hystrichosphaeridiaceae Evitt
emend. Sarjeant and Downie

GenUs_flxstrichosphaeridium Deflandre, 1937,
emend. Davey and Williams in Davey et al, 1966

 

Histrichosphaeridium cf. fl. tubiferum (Ehrenberg)
O. Wetzel, 1933
P1. 2, Fig. 13

Occurrence: rare, in Lower Carlile Member and Upper Shale Member.

 

Reference specimen: slide Pb6289-6, 121.0 x 29.8.

31

fiystrichosphaeridium cf. fl. deanei
Davey and Williams in Davey et a1, 1966
P1. 2, Fig. 12

Occurrence: rare, throughout sections except upper part of Upper Shale
Member of Mancos.

Reference specimen: slide Pb6255-7, 39.5 x 96.7.

Remarks: Specimens here referred to this species could in some instances
be corroded members of another species. _flystrichokolpoma unispinum
Williams and Downie 1966 could take on a similar appearance. In all
specimens a large antapical process with a broad attachment was present.
This process is not mentioned or shown in figured specimens of this
species in the literature.

Hystrichosphaeridium spp.
Specimens are included in this taxon when their state of preservation

allows them to be identified only as having_fiystrichosphaeridium-like
characters.

 

Genus Oligosphaeridium Davey and Williams
in Davey et a1, 1966

Oligosphaeridium_pulcherrimum (Deflandre and Cookson),
Davey and Williams in Davey et a1, 1966
P1. 3, Fig. 1
Occurrence: rare, throughout sections.

Reference specimen: slide Pb332-3, 40.8 x 92.5.

Oligosphaeridium spp.

. Specimens were referred to this taxon if their state of preservation
only allowed the recognition of a central body with process of the type
and number most like Oligosphaeridium species.

 

Genus Cordosphaeridium Eisenack 1963, emend.
Davey and Williams in Davey et a1, 1966

Cordosphaeridium difficile (Manum and Cookson)
Davey and Williams in Davey et a1, 1966
P1. 3, Fig. 3

Occurrence: in Point Lookout section only, rare to common, in Greenhorn
Limestone and lower part of Upper Shale Member.

 

‘7...

 
 
 

32

Reference specimen: slide Pb6220-9, 36.0 x 91.2.

Cordosphaeridium sp. 1
Pl. 3, Fig. 2

I)iagnosis: central body oval in outline; endophram granular, closely
arppressed to epiphram except at bases of processes; periphram striate
saith striae aligned along processes and radiating from the bases of the
Iarocesses; processes about 25, all about 12 u long, hollow, closed,
tLapering, branched or simple or two single processes with attached bases
fHDrming a "web" between them, tips bifid; overall diameter 60 u to 70 u;

archeopyle haplotabular apicle (‘2).

()c:currence: rare, restricted to Greenhorn Limestone and to very base
of Lower Carlile Member.

_§3§Efiference specimen: slide Pb6273-5, 50.2 x 102.9.

Genus TanyOsphaeridium Davey and Williams
in Davey et a1, 1966

Tanyosphaeridium cf. 2, variecalamum
Davey and Williams in Davey et al, 1966
P1. 3, Figs. 4-5

.S)!:<:urrence: rare to common, in Graneros Shale, Greenhorn Limestone,

'Ia<>‘aer Carlile Member and Upper Shale Member of Mancos.

Biference specimen: slide Pb6222-7, 41.0 x 87.2.

Genus Litosphaeridium Davey and Williams
in Davey et al, 1966

Litosphaeridium siphoniphorum (Cookson and Eisenack)
Davey and Williams in Davey et a1, 1966
P1. 4, Fig. 1

.Slsu;urrence: rare, Point Lookout section only, in upper Graneros Shale.

 

Rerference specimen: slide Pb6252-6, 38.2 x 96.5.

Genus flystrichokglpoma Klumpp 1953
emend. Williams and Downie in Davey et al, 1966

flystrichokolpomg ferox (Deflandre)
Williams and Downie in Davey et a1, 1966
P1. 3, Fig. 6

 

1..~

 

 

33

Occurrence: rare, Point Lookout section only, in GreenhOrn Limestone,
Lower Carlile Member, Juana LOpez and lower part of Upper Shale Member
of Mancos. '

Reference specimen: slide Pb6289-6, 121.1 x 41.8.

 

Genus Diphyes Cookson, 1965,
emend. Davey and Williams in Davey et al, 1966

Diphyes cf. 2. colligerum (Deflandre and Cookson)
' Cookson, 1965
P1. 4, Fig. 2

Occurrence: rare to common, throughout sections except for upper part
of Upper Shale Member of Mancos.

Reference specimens: slide Pb6222-5, 42.5 x 103.3.

 

Genus Polysphaeridium Davey and Williams
in Davey et al, 1966

Polysphaeridium spp.
Pl. 4, Figs. 3-5
Occurrence: rare, throughout sections.

Reference specimens: slide Pb6382-3, 35.5 x 91.1; slide Pb6387-3,
44.0 x 99.3.

 

Remarks: Because of their rareness and generally poor state of preser-
vation specimens referable to this genus were not identified to species.

Form 0 sp. 1
Pl. 4, Fig. 7

Diagnosis: central body oval to pear-shaped; endophragm granular; numer-
ous processes, solid, with orthogonal to recurved aculeate tips; processes
10 u to 15 u long; central body 40 u to 50 u in diameter; archeOpyle
uncertain.

Occurrence: rare, limited to lowermost Graneros Shale imlboth sections.

 

Reference specimens: slide Pb6227-10, 115.0 x 39.9; slide Pb6227-12,
110.1 x 40.5.

Genus Surculosphaeridium
Davey, Downie, Sarjeant and Williams, 1966

34

Surculosphaeridium cf. S. vestitum (Deflandre)
Davey, Downie, Sarjeant and Williams 1966
P1. 4, Fig. 6

 

Occurrence: rare, throughout Point Lookout section, one sample each in
Lower Carlile and Upper Shale Members of the Mancos.

Reference specimen: slide Pb6857-2, 37.5 x 100.9.
Remarks: Specimens are rarely well-preserved. The forking of the pro-

cesses is at a more acute angle than the type. One well-preserved
specimen showed a good apical archeOpyle.

Family Exochosphaeridiaceae Sarjeant and Downie

Genus Exochosphaeridium Davey and Williams
in Davey et al, 1966

 

?Exochosphaeridium_phragmites Davey, Downie,
Sarjeant and Williams in Davey et al, 1966
P1. 5, Fig. l

 

Occurrence: rare to common (Graneros Shale and Greenhorn Limestone),
throughout sections except upper part of Upper Shale Member in the Ute
Reservation section.

Reference specimen: slide Pb273-l, 34.8 x 94.5.

 

Remarks: the characteristic apical process is rarely seen in the speci-
mens in the Mancos.

?Exochosphaeridium sp. 1
Pl. 5, Fig. 2

 

Diagnosis: like E. phragmites but with much shorter spines; obvious
precingular archeOpyle; may be 2. phragmites specimens with processes
corroded away.

 

 

Occurrence: rare to common, in upper Graneros Shale, Greenhorn Limestone
and Upper Carlile Member of Mancos.

 

Reference specimen: slide Pb6357-4, 30.7 x 104.2.

 

?Exochosphaeridium sp. 2
Pl. 5, Fig. 4

 

Diagnosis: central body oval in outline with apical "nubbin"; endo-
phram granular to striate near bases of processes, closely appressed
to periphram except at the bases of the processes; periphram smooth,

35

drawn into ca. 50 closed, tapering, branched or simple processes, some
specimens with fused bases forming a "web" (intratabular process com-
plexes?), faintly striate at bases, with bifid or trifid tips, 20 u

to 25 u long; one open antapical process ca. 10 u long, cylindrical,
ca. 6 u in diameter; overall diameter 65 u to 75 u.

Gecurrence: rare, in Lower Carlile Member and Upper Shale Member of
Mancos.

 

Reference specimen: slide Pb6379-3, 40.8 x 101.2.

Family Hystrichosphaeraceae O. Wetzel, emend. Evitt,
emend. Sarjeant and Downie

Genus flystrichosphaera 0. Wetzel 1933,
emend, Davey and Williams in Davey et a1, 1966

 

Bystrichosphaera ramosa (Ehrenberg) Davey and Williams
in Davey et a1, 1966
P1. 5, Fig. 3

Occurrence: rare to common, throughout sections.

Reference specimen: slide Pb6273-3, 48.5 x 97.1

_flystrichosphaera ramosa var. 1
Pl. 5, Fig. 5

Diagnosis: conforms to the circumscription of 5. ramosa but is larger
(80 u to 90 u overall diameter), has a heavier endophram and periphram,

and stouter processes, compared with other specimens.

Occurrence: rare, in Greenhorn Limestone, Lower Carlile and Upper Shale
Members of the Mancos.

Reference specimen: slide Pb6273-l, 35.0 x 89.5.
_flystrichosphaera ramosa var. 2
Pl. 5, Fig. 6

Pl. 6, Fig. 2

Diagnosis: conforms to the circumscription of,fl. ramosa but is consis-
tently smaller (35 u to 45 u overall), compared with other specimens.

Occurrence: rare to frequent, throughout sections.

 

Reference specimen: slide Pb6371-1, 43.1 x 89.1.

 

36

_flystrichosphaera sp. 1
P1. 6, Figs. 1-2

Diagnosis: central body circular to oval in outline; endophram granular,
periphram faintly granular to smooth; processes 6 u to 12 u long, most
about 8 u; crests consistently about 3 u high. Separated from E. ramosa
on bases of granular sculpturing and short processes.

Occurrence: rare to common, throughout sections except upper part of
Upper Shale Member of Mancos.

Reference specimen: slide Pb6273-1, 36.5 x 92.0

_flystrichosphaera spp.

Any specimens resembling the genus fiystrichosphaera that are too corroded
to show specific characters are placed in this category.

 

Genus Heslertonia Sarjeant
in Davey et a1, 1966

 

Heslertonia heslertonensis (Neale and Sarjeant)
Sarjeant in Davey et a1, 1966
P1. 6, Fig. 4

Occurrence: rare, in Upper Graneros Shale, Greenhorn Limestone and lower
part of Upper Shale Member of the Mancos.

Reference specimen: slide Pb6272-6, 108.2 x 41.3.

Family Microdiniaceae Eisenack
emend. Sarjeant and Downie

Genus Microdinium Cookson and Eisenack 1960,
emend. Sarjeant in Davey et a1, 1966

 

Microdinium cf. M. ornatum Cookson and Eisenack 1960
P1. 6, Fig. 3

 

Occurrence: rare, in Greenhorn Limestone and Upper Carlile Member of
Mancos.

Reference specimen: slide Pb6295-6, 39.5 x 92.8.

Family Gonyaulacystaceae Sarjeant and Downie

37

Genus Gonyaulacysta Deflandre 1964
emend. Sarjeant in Davey et al, 1966

 

Gonyaulacysta spp.
Pl. 6, Figs. 6-7

Occurrence: rare, throughout section except upper part of Upper Shale
Member.

 

Reference specimens: slide Pb6288-6, 36.7 x 99.3; slide Pb6289-7,
29.5 x 100.1; Pb6295-7, 49.5 x 109.7.

 

Remarks: Because of their rare occurrences and often poor state of
preservation most specimens referable to this genus were not identi-
fied to species.

?Gonyaulacysta sp. 1
P1. 7, Figs. 1-2

 

Diagnosis: circular to oval in outline, apparently spherical to oval;
endophram granular, periphram thin, faintly granular; complete tabu-
lation not determined because of inadequate specimens; sutures marked
by a row of delicate slender processes to 6 u long, branched and con-
nected distally and at various levels of branching, thus forming an
open crest; central body 50 u to 60 u in diameter; archeopyle precingu-
lar (?).

Occurrence: rare, only in Greenhorn Limestone of Ute reservation section.

Reference specimen: slide Pb6357-6, 40.1 x 90.2; slide Pb6357-4.
30.7 x 92.7.

 

Remarks: Like (?) Evitt's (1967) Forms AB which has a 6P archeopyle.

Genus Leptodinium Klement, 1960
emend. Sarjeant in Davey et a1, 1966

 

?Leptodinium dispertitum
Cookson and Eisenack, 1965
P1. 6, Fig. 5

Occurrence: rare to common, in Graneros Shale and Greenhorn Limestone.

 

Reference specimen: slide Pb6250-10, 37.0 x 92.7; slide Pb6289-6.
32.5 x 100.1.

 

Family Areoligeraceae Evitt
emend. Sarjeant and Downie

38

Genus_§yclonephelium Deflandre and Cookson 1955,
emend. Williams and Downie in Davey et al, 1966

 

,chlonephelium spp.
Pl. 7, Figs. 5-6

 

Occurrence: rare, in Lower Carlile and Upper Shale Members of the Mancos.

Reference spscimen: slide Pb6878-3, 47.0 x 3.0

Remarks: Because of generally poor preservation specimens referred to
this genus are not identified to species. Included here are specimens
possibly referable to Areoligera and Tenua.

 

Genus Areoligera Lejeunne-Carpentier, 1938
emend. Williams and Downie in Davey et al, 1966

Areoligera spp.
Pl. 7, Figs. 3-4

 

Occurrence: rare to common, in upper Graneros Shale and upward through-
out sections.

Referencegspecimens: slide Pb6345-3, 44.5 x 95.4.
Remarks: Because of their generally poor state of preservation speci-
mens here referred to this genus have not been identified to species.

Included here are some specimens possible referable to chlonephelium
and Tenua.

Family Fromeaceae Sarjeant and Downie
Genus Tenua Eisenack, 1958
Tenua spp.
Pl. 8, Fig. l
Occurrence: rare to common, throughout sections.
Reference specimen: slide Pb6227-2, 38.9 x 105.0
Remarks: Because of their generally poor state of preservation speci-
mens here referred to this genus are not identified to species. This

has also resulted in the inclusion of poor specimens possibly referable
to Cyclonephelium and Areoligera.

 

39
'Genus Fromea Cookson and Eisenack, 1958

Fromea amphora Cookson and Eisenack 1958
P1. 8, Fig. 4

 

Occurrence: rare to frequent, in Graneros Shale, Lower Carlile Member
and Upper Shale Member of Mancos.

 

Reference specimen: slide Pb6282-6, 39.4 x 99.1.

Remarks: The specimens in the Mancos generally lack the "girdle" of the
holotype. ,

Family Endoscriniaceae Vozzhennikova
emend. Sarjeant and Downie

Genus Palaeohystrichophora Deflandre, 1934,
emend. Deflandre and Cookson, 1955

 

Palaeohystrichophora infusoroides Deflandre, 1934
P1. 8, Fig. 2

Occurrence: rare to extremely abundant, throughout sections

Reference specimen: slide Pb6899-2, 121.8 x 37.9.

Palaeohystrichophora infusoroides var. 1
P1. 8, Fig. 3

 

Diagnosis: larger than 3. infusoroides of type; girdle nearer antapex;
hairs shorter and commonly fewer.

 

Family Deflandreaceae Eisenack emend.
Sarjeant and Downie

Genus Deflandrea Eisenack, 1938,
emend. Williams and Downie in Davey et a1, 1966

 

Varied combinations of intercalary archeopyles (some of the archeopyles
on endophragms may be apical) on the endophragm and periphragm are present
among the specimens examined in this study. Forms without archeopyles
and forms with 3I/3I, -/3I, I/3I, I/I, I/- types (Evitt, 1967) were found.

40

The Species identifications below are tentative because it is felt that
more work must be done on this genus and particularly those species that
are represented here. They intergrade in shape and ornamentation making
separation into Species difficult. In reference to archeopyles the code
of Evitt (1967) is used.

Deflandrea cf. 2, minor Alberti, 1959
P1. 8, Fig. 5

 

Occurrence: rare to common, in Graneros Shale and Lower Carlile Shale
Member of Mancos.

 

Reference_specimen: slide Pb6227-10, 124.1 x 29.6.

 

Deflandrea cf. 2. acuminata Cookson and Eisenack, 1958
P1. 8, Fig. 8

 

Occurrence: rare to frequent, in Lower Carlile Shale Member and Upper
Shale Member.

Reference Specimen: slide Pb626846, 38.0 x 99.0.

Remarks: Archeopyle is I/3I in all Specimens observed in this study.

Deflandrea cf. 2. gssnulifera Manum, 1963
P1. 8, Fig. 7

 

 

Occurrence: rare to frequent, in Graneros Shale, Lower Carlile and
Upper Shele member of the Mancos.

Reference specimen: slide Pb6340-7, 47.8 x 87.4.
Remarks: Archeopyle is I/3I. Specflmens are generally smaller than the

holotype and paratypes. Grades into 2. verrucosa characteristics.

Deflandrea cf. 2, verrucosa Manum, 1963
P1. 8, Fig. 6

 

Occurrence: rare to frequent, in Lower Carlile and lower part of Upper
Shale Members.

Reference specimen: slide Pb6268-7, 43.5 x 95.5.
Remarks: Archeopyle is I/I (some Specimens show accessory sutures on

the endophragm that gave the appearance of 31). Smaller than types,
grades into characteristics of 2, granulifera.

 

41

Deflandrea cf. 2. balmei Cookson and Eisenack, 1960,
' nov. nom., 1962
P1. 9, Figs. l-3,5

 

Occurrence: rare to frequent, in Lower Carlile and Upper Shale Members
of the Mancos.

 

Reference Specimen: slide Pb6902-6, 39.1 x 88.9.

 

Remarks: Archeopyle is I/- (some larger specimens included in this species
appear to be I/3I). Larger specimens appear to grade into forms resembling
2. echinoides Cookson and Eisenack,l960.

Deflandrea cf. 2, micracantha Cookson and Eisenack, 1960
P1. 9, Fig. 7

 

 

Occurrence: rare to frequent, in upper part of Upper Shale Member of
the Mancos.

 

Reference specimen: slide Pb6823-3, 41.0 x 89.2.

 

Remarks: Specimens encountered were without "shoulders" of the holotype.

Deflandrea sp. 1
Pl. 9, Fig. 6

 

Diagnosis: ambitus oval elongated anterior-posterior, surmounted by low
truncated acuminate apical horn; two antapical projections, one low, the
other slightly longer--a pointed horn; endophragm smooth, oval to pear-
shaped, not quite touching periphragm but roughly conforming to the shape
of periphragm granular; archeopyle 3I/3I.

Occurrence: rare to abundant, in Graneros Shale, Greenhorn Limestone,
Lower Carlile and lower Upper Shale Members of Mancos.

 

Reference specimen: slide Pb6340-7, 124.8 x 47.0.

 

Remarks: This species might be placed in Typythrodinium Drugg if it
could be determined that the three epithema plates were removed as a
unit. Like Evitt's (1967) Forma Q but with the inner body.

Deflandrea sp. 2
Pl. 9, Fig. 8

 

Diagnosis: ambitus circular to oval surmounted by high rounded acuminate
apical horn, two antapical projections, one a low bump, the other a long

42

acuminate horn; cingulum marked by sharp low ridges; inner capsule circu-
lar, smooth, touching periphragm on one side; periphragm faintly granular;
no archeopyle.

Occurrence: rare to frequent, in Graneros Shale, Greenhorn Limestone,
Lower Carlile Member and lower part of Upper Shale Member of Mancos.

 

Reference specimen: slide Pb6282-6, 30.8 x 90.8.

 

RemarkS: Resembles Palaeopystrichophora infusoroides var. 1 but without
hairs.

Deflandrea Sp. 3
P1. 10, Fig. 2

 

Diagnosis: epitract a broad bell-shape with small blunt but acuminate
apical horn (some specimens without apical horn but with thickened apical
area); hypotract trapezoidal with concave sides with two antapical pro-
cesses at the corners, one a low bump the otherailonger acuminate horn;
wide cingulum separates epi- and hypotract and is marked by low interrupted
ridges; endophragm smooth; periphragm either punctate, smooth or granular;
archeopyle I/I; inner capsule circular to oval not touching periphragm

as seen in dorso-ventral view.

Occurrence: rare to frequent, in Lower Carlile and Juana Lopez Members
and in lower part of Upper Shale Member of Mancos.

Reference specimen: slide Pb6899-2, 120.9 x 43.0.
Rgmsggs; More than one Species are probably represented here but until

more specimens can be studied it does not seem practical to Split them.

Deflandrea sp. 4
P1. 9, Fig. 4

 

Diagnosis: overall shape like 2. acuminata but without a prominent
antapical horn; periphragm smooth with small scattered worts or beads;
endophragm smooth; cingulum marked by 5 or 6 paired linear groups of
beads or worts; inner capsule circular in dorso-ventral view; archeopyle
I/I.

Occurrence: frequent, in lower part of Upper Shale Member.

Reference specimen: slide Pb6327-6, 41.5 x 86.9.

Family Hexagoniferaceae Sarjeant and Downie

Genus Hexagonifera Cookson and Eisenack, 1961

 

43

Hexagsnifera suspecta Manum and Cookson, 1964
P1. 10, Fig. 4

 

A

 

Occurrence: common to abundant, throughout sections.
Reference Specimen: slide Pb6899h4, 118.6 x 35.7.

Hexagonifera suspecta var. 1
P1. 10, Figs. 1,3

Diagnosis: conforms to Species description except that the endophragm is
thinner and is smooth to granular, but not coarsely granular.

Occurrence: common to abundant, throughout sections.

 

Reference spscimen: slide Pb6899-4, 120.1 x 43.7.

 

Remarks: Included within this variety of the Species are possibly the
isolated inner capsules of some of the Deflandrea Species. Like Evitt's
(1967) Forma P.

 

Hexsgonifera suspecta var. 2
P1. 10, Fig. 5

Diagnosis: conforms to the description of the Species except that the
endophragm is slightly thicker and the longer radial elements in the wall
are aligned to form a reticulate sculpturing; specimens of this variety
tend to be larger than the smooth and granular varieties.

Occurrence: rare, to frequent, in the middle part of the Upper Shale
Member of the Mancos.

 

Reference specimen: slide Pb6900-2, 41.9 x 90.3.

 

Family Canningiaceae Sarjeant and Downie

Genus Canningia Cookson and Eisenack, 1960

Canningia cf. Q. colliveri Cookson and Eisenack, 1960
P1. 11, Fig. 6

Occurrence: rare, in Graneros Shale, Greenhorn Limestone and Lower
Carlile Member of the Mancos.

Reference specimen: slide Pb6255-6, 43.8 x 103.9.

44

Family Pseudoceratiaceae Eisenack emend. Sarjeant and Downie

Genus Odontochitina Deflandre, 1935

 

Odontochitina striatoperforata Cookson and Eisenack, 1962
P1. 11, Figs. 1-2

Occurrence: rare to common, in Graneros Shale, Greenhorn Limestone and
the Lower Carlile and lower part of Upper Shale Members of Mancos.

Reference specimen: slide Pb6222-7, 50.0 x 89.2.

Form F sp. 1
P1. 11, Fig. 3

Diagnosis: a distinct form; three large processes, one apical, one
antapical and one "dog-leg" postcingular; in addition smaller fiystrichos-
phaeridium-like processes; tabulation not determined; apical (tetratabular)
archeopyle.

 

 

Occurrence: rare, throughout Point Lookout section, Lower Carlile and
lower part of Upper Shale Members of Mancos in Ute Reservation section.

Reference specimens: slide Pb6881-4, 40.6 x 87.4; Slide Pb6250-9,
36.5 x 93.6.
Family Gymnodiniaceae Bergh

Genus Dinpgymnium Evitt, Clarke and Verdier, 1967

Dinpgymnium sp. 1
P1. 11, Figs. 3, 4, 5, 7, 8

Diagnosis: tiny, 8 to 20 u long; wide girdle up to 1/4 length of specimen;
may have folds in epitract; apical archeopyle.

Occurrence: rare to frequent, throughout sections.

Reference specimen: slide Pb6244-3, 31.5 x 92.4.

Remarks: This is Dinogymnium Sp. 6 of Evitt (1967).

45

Dinogymnium sp. 2
P1. 12, Figs. 1-10

Diagnosis: included in this taxon are all species of Dinogymnium not
referable to 2. sp. 1.

Occurrence: rare to frequent, throughout sections.

 

Reference specimens: slides Pb6845-3, 38.1 x 94.2, 35. 1 x 98.0,
36.2 x 105.5, 40.5 x 93.5; Pb6848-3, 37.8 x 98.3; Pb6888-3, 38.6 x 88.1;
Pb6892-1, 43.6 x 98.4; Pb6891-3, 39.4 x 96.7.

 

Remarks: Included here are Dinogymnium sp. 1, 2. sp. 2, 2. sp. 5 of
Evitt (1967).

Family Uncertain
Genus Diconodinium Eisenack and Cookson, 1960

?Diconodinium arcticum Manum and Cookson, 1964
P1. 12, Fig. 11

 

Occurrence: rare to frequent, throughout sections.

 

Reference specimen: slide Pb6282-6, 48.2 x 91.4.

 

Remarks: Poorly preserved and folded specimens that have been assigned
to this Species may be Specimens of Deflandrea or corroded Palaeohystich-
Ophora. Archeopyle is I in many Specimens.

Genus Horologinella Cookson and Eisenack, 1962

 

?Horologinella spinosa Cookson, 1965
P1. 12, Fig. 12

 

Occurrence: rare to common, in Graneros Shale and Lower Carlile and
Upper Shale Members of the Mancos.

Reference specimen: slide Pb6899-4, 110.9 x 42.4.

 

Genus Trigonopyxidia Cookson and Eisenack, 1961

46

?Trigpngpyxidia spp.
P1. 13, Fig. 2

Occurrence: rare, in Graneros Shale, Greenhorn Limestone, Lower Carlile
Shale Member and lower part of Upper Shale Member of Mancos.

Reference specimen: slide Pb6273-2, 44.7 x 91.2.

 

Remarks: The overall shape ranges from a blunt rounded form to a more
pointed tetrahedral form.

Form D. sp. 1
P1. 13, Fig. 1

Diagnosis: circular in outline in all Specimens encountered; dense
concentration of fine hairs about 5 u long at periphery in places fused
together; endophragm granular; overall diameter including hairs, 65 to
75 u.

Occurrence: rare, in Lower Carlile Member and lower part of Upper Shale
Member of Mancos.

Reference spschmen: slide Pb6295-6, 38.1 x 92.5.
OTHER ALGAE

Genus Palembages O. Wetzel, 1961

'Palambages cf. 2. deflandrei Gorka, 1963
P1. 12, Fig. 3

Occurrence: rare, in Lower Carlile Member and Upper Shale Member of
the Mancos.

Reference Specimen: Slide Pb6899-4, 124.1 x 42.6.

 

Remarks: The colonies are not all circular in outline. Some consist of
only a few assymetrically arranged spheres. All spheres have a polygonal
plate situated on that part of a sphere opposite the center of a colony.
This gives the impression of a "colonial dinoflagellate" if the polygonal
openings are considered as archeopyles. Some isolated spheres were
recognized.

Genus Pediastrum Meyen, 1829

47

Pediastrum spp.
P1. 13, Fig. 4

 

Occurrence: rare, in upper part of Upper Shale Member of Mancos, plus
one occurrence in the sandy interval in the Ute section equivalent to the

Tocito Sandstone.

 

Remarks: All specimens encountered were badly corroded.
TRILETE SPORES

Genus Gleicheniidites Ross, 1949 ex Delcourt
and Sprumont, 1955

 

Gleicheniidites senonicus Ross, 1949
P1. 13, Fig. 5 '

Occurrence: rare to common throughout sections.

 

Reference specimen: slide Pb688l-4, 34.5 x 105.3.

 

Gleicheniidites circinidites (Cookson) Brenner, 1963
P1. 13, Fig. 7

Occurrence: rare, throughout Point Lookout section, in Graneros Shale
and Upper Shale Member of Mancos at Ute Reservation section.

 

Referencesspecimen: slide Pb6881-4, 39.0 x 92.1.

Genus Leiotriletes Naumova, ex Potonie and Kremp, 1954

 

Leiotriletes pseudomaximus (Pflug and Thomson), Stanley, 1965
P1. 13, Fig. 8

 

Occurrence: rare, in upper part of Upper Shale Member of Mancos.

 

Reference specimen: slide Pb688l-4, 33.8 x 91.8.

Large smooth Trilete spores
P1. 14, Figs. 5, 10, 13

Occurrence: rare, throughout sections.

 

Reference specimens: slide Pb6227-10, 111.9 x 43.7; slide Pb6354-1,
37.1 X 9301; Pb6227‘3, 44.5 X 106090

 

48

Remarks: large smooth trilete Spores are grouped together because they

are often indistinguishable due to their poor state of preservation.
Possibly included are species assignable to a number of genera such as
Dictypphyllidites, gyathidites, Lygodium5porites, TodiSporites, Hymeno-
psyllumsporites, Leiotriletes, MatoniSporites, etc.

Genus Sphagpumsporites Raatz, 1937

Sphagpumsporites antigsaspprites (Wilson and Webster)
Potonié, 1956
P1. 13, Fig. 6

Occurrence: rare, throughout Point Lookout section, in Lower Carlile
Member only of Ute Reservation section.

Referencesspecimen: slide Pb6227-3, 32.2 x 96.6.

Genus Cardioangulina Malawkina, 1949,
emend. Potonie, 1960

Cardioangslina disphana (Wilson and Webster)
Stanley, 1965
P1. 13, Fig. 9
P1. 14, Fig. 1

Occurrence: rare, throughout Point Lookout section, in Lower Carlile

Member and Upper Shale Member of Ute Reservation section.

Reference Specimen: slide Pb6340-6, 115.5 x 35.9.

Genus DeltoidOSpora Miner, 1935, emend. Potomie, 1956

?Deltoidospora hallii Miner, 1935
P1. 14, Fig. 2

Occurrence: rare, throughout Point Lookout section, in Upper Shale
Member of Mancos in Ute Reservation section.

Reference spscimen: slide Pb6227-2, 40.9 x 94.3.

49

Genus Cyathidites Couper, 1953

Gyathidites cf. 9, mesozoicus (Thiergart) Potonié, 1956
P1. 14, Fig. 6

 

Occurrence: rare, in Upper Shale Member of Mancos in both sections, in
Lower Carlile Member in Ute Reservation section.

Referencepgpecimen: slide Pb688l-4, 44.5 x 95.3.
Genus UndulatiSpprites Pflug in Thomson and Pflug, 1953

Undulatisporites sp. 1
P1. 14, Fig. 3

Diagnosis: Semiangular in Polar view; psilate; wall about 0.5 microns
thick; leasurae sinuous, tectate (about 1.2 u high); diameter 18 to 22 u-
Occurrence: rare, upper part of Upper Shale Member of Mancos.

Reference specimen: slide Pb6881-4, 32.7 x 87.4.

 

Genus Concavisporites Pflug, 1953,
emend. Delcourt and Sprumont, 1955

?Concavigporites sp. 1
P1. 14, Fig. 8

Diagnosis: Semilobate in polar view; punctate to vermiculate with muri
about 0.5 u wide, but contact area apparently smooth; wall about 0.5 u
thick; leasurae sinuous, extending to margins, about 1.4 u wide; Kyrtome
on distal face; diameter 27 to 35 u.

Occurrence: rare, throughout sections.

Reference specimen: slide Pb6227-3, 33.2 x 92.4.
Genus Triplan0§porites Pflug in Thomson and Pflug, 1952
Triplanosporites sinuosus Pflug in Thomson and Pflug, 1952

P1. 14, Fig. 7

Occurrence: rare, throughout Point Lookout section, in Lower Carlile
Member and Upper Shale Member of Mancos.

Reference specimen: slide Pb6227-10, 119.0 x 36.4.

50

Triplanosporites cf. 2. terciarius Pflug in Thomson and Pflug,
1953
P1. 14, Fig. 4

 

Occurrence: rare, in Upper Shale Member of Mancos.

Reference Specimen: slide Pb6881-4, 41.8 x 101.6.

 

Genus Cingplatisporties Thomson, 1953, emend. Potonié, 1956

Cipgulatisporites radiatus Stanley, 1965
P1. 14, Fig. 9

Occurrence: rare, throughout Point Lookout section, in lower part of
Upper Shale Member of Mancos in Ute Reservation section.

Reference specimen: slide Pb6379-2, 42.9 x 46.5.
I
Genus Kuy1i3porites Potonie, 1956

Kuy1i5porites scutatus Newman, 1965
P1. 14, Fig. 11

Occurrence: rare, Upper Shale Member of Mancos, Point Lookout section

only.

Reference specimen: slide Pb6869-3, 35.7 x 98.9.

Genus Concavissimisporites Delcourt and Sprumont, 1955,
emend. Delcourt, Dettmann and Hughes, 1963

Concavissimisporites variverrucatus (Couper) Brenner, 1963
P1. 14, Fig. 14

Occurrence: rare, in middle of Upper Shale Member of Mancos in Point
Lookout section only.

Reference specimen: slide Pb6881-4, 43.0 x 97.2.

Genus Acanthotriletes Naumova, 1937,
emend. Potonié and Kremp, 1954

51

?Acanthotriletes varispinosus Pocock, 1962
P1. 14, Fig. 12

Occurrence: rare to common, throughout sections.

 

Reference specimen: slide Pb6227-2, 41.5 x 103.0.

 

Genus Lycopodiumsporites Theirgart, 1938

Lycopodiumsporites cerniidites (Ross) Delcourt and Sprumont, 1955
P1. 15, Fig. 1

Occurrence: rare to common, throughout sections.

 

Reference spgcimen: slide Pb6227-2, 42.2 x 92.0.
Genus Camarozonosporites Potonié, 1956, emend. Klaus, 1960

?Camarozonosporites insigpis Norris, 1967
P1. 15, Fig. 2

Occurrence: rare, throughout Point Lookout section, no occurrences in
Ute Reservation section.

 

Reference specimen: slide Pb6227-2, 33.1 x 93.6.
Genus Converrucosi3porites Potonie and Kremp, 1954

platyverrucosus, Brenner, 1963

Converrucosi3porites cf. Eb
P1. 15, Fig. 3

Occurrence: rare, Upper Shale Member in Point Lookout section, in
Lower Carlile Member and Upper Shale Member of Mancos in Ute Reservation

section.

 

Reference specimen: slide Pb6227-11, 115.2 x 42.2.

Genus Appendicisporites Weyland and Krieger, 1953

Appendicisporites cf. 5. tricornatatus Weyland and Greifeld
P1. 15, Fig. 4

 

Occurrence: rare, throughout Point Lookout section; no occurrences in
Ute Reservation section.

 

52
Genus Cicatricosisporites Potonie and Gelletich, 1932

Cicatricosisporites cf. hallei Delcourt and Sprumont, 1955

£-.______
P1. 15, Fig. 5

 

Occurrence: rare, in Lower Carlile Member and Upper Shale Member of
Mancos in Point Lookout section, only in upper sample of Upper Shale
Member of Mancos in Ute Reservation section.

Reference specimen: slide Pb6865-2, 45.5 x 99.4.

 

Remarksz~ Some specimens of g. dorogensis Potonie and Gelletich may be
included here.

Cicatricosisporites cf._§. dorogensis Potonie and Gelletich, 1932,
emend. Kedves, 1961
P1. 15, Fig. 6

Occurrence: rare, middle of Upper Shale Member of Mancos in Point Lookout
section, Lower Carlile Member and Upper Shale Member of Mancos in Ute
Reservation section.

Reference specimen: slide Pb6227-2, 41.3 x 92.1.

 

Remarks: Specimens are much smaller than those described for this Species
in the literature.

Cicatricosisporites cf._§; carlylensis Pocock, 1962
P1. 15, Fig. 10

 

 

Occurrence: rare, Upper Shale Member in Point Lookout section only.

Reference Specimen: slide Pb6881-4, 44.2 x 97.2.

 

Genus Corrugatisporites Thomson and Pflug, 1953
non Ibrahim ex Weyland and Greifeld, 1953

 

?Corrugatisporites toratus Weyland and Greifeld, 1953
P1. 15, Fig. 7

Occurrence: rare, in Graneros Shale and Upper Shale Member of Mancos in
Point Lookout section, in Lower Carlile Member and Upper Shale Member of
Mancos in Ute Reservation section.

Reference specimen: slide Pb6227-2, 36.3 x 95.8.

 

53

MONOLETE SPORES

Genus Laevigatosporites Ibrahim, 1933

 

ovatus Wilson and Webster, 1946

Laevigatosporites cf. L,
P1. 15, Fig. 8

Occurrence: rare to common, throughout both sections.

 

Reference specimen: slide Pb6227-11, 124.7 x 42.2.

 

Genus Verrucatosporites Pflug and Thomson, 1953

VerrucatOSporites cf. !. favus (R. Potonié)
Pflug and Thomson, 1953
P1. 15, Fig. 2

 

Occurrence: rare, in Lower Carlile Member of Mancos in Point Lookout
section and Ute Reservation section, in Upper Shale Member of Mancos
in Point Lookout section only.

 

Reference Specimen: Slide Pb6881-4, 47.9 x 106.7.

 

Reticulate Monolete Spores
P1. 15, Fig. 13

Occurrence: rare, in Upper Shale Member of Mancos (only uppermost sample
in Ute Reservation section).

 

Reference specimen: slide Pb6881-4, 44.9 x 98.9.

 

Remarks: This category includes all monolete spores with a reticulate
sculpturing. Most are large, 35 u to 50 u.

GYMNOSPERMOUS POLLEN

Few bisaccate pollen grains were well-preserved. Because of their poor
preservation they have been lumped in the categories or taxa listed below.

54

Large PinuS-type pollen
P1. 15, Fig. 14

Occurrence: rare to common, throughout both sections.

 

Reference Specimen: slide Pb6282-6, 48.2 x 98.7.

 

Remarks: Included in this group are all grains that are like large pine
pollen in shape and size. Overall length from 50 to 90 u.

Small PinuS-type pollen
P1. 15, Fig. 9

Occurrence: rare, Upper Shale Member of Mancos in Point Lookout section,
lower part of Upper Shale Member in Ute Reservation section.

 

Reference specimen: slide Pb6881-4, 37.5 x 95.0.

Remarks: Size (overall long dimension) 30 to 40 u.

Picea-type pollen
P1. 16, Fig. 1

Occurrence: rare, throughout Point Lookout section, in Graneros Shale
and Lower Carlile Member of Mancos in Ute Reservation section.

 

Reference_§pecimen: slide Pb6282-6, 44.3 x 90.7.

 

Remarks: Included here are those grains like Picea pollen in shape and
size.

Abies-type pollen
P1. 16, Fig. 9

Occurrence: rare, Upper Shale Member of Mancos Point Lookout section only.

 

Reference specimen: Slide Pb6869-2, 41.0 x 95.2.
Remarks: Included here are those pollen grains that are like Abies grains
in Size, shape, and apparent thickness of cap.

Genus Rugubivesiculites Pierce, 1961

Rugubivesiculites cf. 3, reductus Pierce, 1961
P1. 16, Fig. 7

 

55

Occurrence: rare, lower Carlile Member and Upper Shale Member of Mancos.

 

Reference Specimen: slide Pb6327-7, 36.5 x 107.7.

 

Genus Vitreisporites Leschik, 1955

 

VitreiSporites ppjlidus (Reissinger) Nilsson, 1958
P1. 15, Fig. 11

Occurrence: rare, in Juana Lopez Member in Upper Shale Member of Mancos
in Point Lookout section, in Upper Shale Member of Mancos in Ute Reserva-
tion section.

 

Reference specimen: slide Pb688l-4, 33.7 x 99.1.

Genus Parvisaccites Couper, 1958

 

?Parvisaccites Sp. 1, new species
P1. 16, Fig. 4

 

Diagnosis: oval in polar view; bladders appear as thick granular folds
with uneven margins; radially extending folds of the bladders opposite the
sulcus; this pattern extends to the equator; rest of grain is granular;
exine about 2 u thick, proximal cap about 4 u thick; total breadth 60 to
70 u, length 50 to 60 u.

Occurrence: rare, upper part of Upper Shale Member, Point Lookout section
only.

Reference specimen: slide Pb6881-4, 35.7 x 102.1.

Genus Classopollis Pflug, 1953,
emend. Pocock and Jansonius, 1961

 

Classopollis cf. 9: classoides Pflug,
emend. Pocock and Jansonius, 1961
P1. 16, Figs. 2-3

 

 

Occurrence: rare to frequent, throughout both sections.

Reference Specimens: slide Pb6340-7, 112.8 x 32.7; slide Pb6808-3,
30.7 x 89.4.

Remarks: TWO size classes were counted, one less than 27 u, the other
greater than 27 u. There appears to be two distinct size modes for this
group in the Mancos.

56

Classopollis sp. 1
P1. 16, Figs. 5-6

Diagnosis: consistently discoid and commonly with tetrad mark; tetrads
appear deflated compared with g. classoides and angular in outline; in
other respects similar to Q. classoides.

 

Occurrence: rare to frequent, Upper Shale Member of Mancos.

Reference specimen: slide Pb688l-4, 45.7 x 86.6; 45.3 x 103.3; 45.8 x 96.3.

Genus Eguisetosporites Daugherty, 1941
emend. Singh, 1964

 

Large gguisetosporites spp.
P1. 16, Fig. 8

Occurrence: rare, throughout Point Lookout section, in lower part of
Upper Shale Member of Mancos only in Ute Reservation section.

'Rgference Specimen: slide Pb6357-10, 34.7 x 91.2.
Remarks: All Ephedra-like pollen grains greater than 25 u in length

(longitudinal dimension) are included here. These grains generally have
a higher length to breadth ratio than the other group and have more ridges.

Small Equisetosporites spp.
P1. 16, Fig. 10

 

Occurrence: rare, throughout Point Lookout section, in Greenhorn Limestone
and Lower Carlile Member of Mancos in Ute Reservation section.

Reference specimen: slide Pb6282-6, 35.5 x 97.3.
Remarks: All Ephedra-like pollen less than 25 u in length are included

here. These grains generally have a length to breadth ratio of about 2:1
and 8 or 9 ridges.

Genus Insperturppollenites Thomson and Pflug, 1953

Inaperturopollenites limbatus Balme, 1957
P1. 17, Figs. 1-2

 

Occurrence: 'rare to frequent, throughout Point Lookout section, in Lower
Carlile Member and Upper Shale Member of Mancos in Ute Reservation section.

57

Reference specimen: slide Pb6881-4, 42.9 x 96.9, 46.3 x 105.4.

Remarks: Two forms of this species were counted separately, one like
the type,the other generally smaller and with faint "rudimentary" bladder
or frill around the thin-walled area.

Inaperturopollenites sp. 1
P1. 16, Figs. 11-12

 

Diagnosis: granular to granulate; usually Split open; 25 to 40 u,,
similar to l, dubius (Potonie and Venitz) Thomson and Pflug.

Occurrence: abundant, throughout sections.
Reference specimen: slide Pb6357-10, 38.2 x 87.6.

Inaperturopollenites sp. 2
P1. 16, Fig. 13

 

Diagnosis: granular to scabrate; rarely split open; 15 to 20 u.

Oceurrence: rare to frequent, throughout sections.

Reference specimen: slide Pb6865-2, 48.9 x 98.7.
Inaperturopollenites sp. 3

P1. 16, Fig. 14
P1. 17, Fig. 7

Diagnosis: smooth to granular; circular in outline; sometimes split open;
few showing possible tetrad mark; 30 to 40 u.

Occurrence: rare to common, Upper Shale Member of Mancos.

Reference specimen: slide Pb6881-4, 37.4 x 101.8, 44.5 x 105.8.

Genus Quadripollis Drugg, 1967

 

gguadripollis krempii Drugg, 1967
P1. 17, Fig. 4

Occurrence: rare, Upper Shale Member of Mancos.

Reference specimen: slide Pb6907-6, 32.3 x 101.3.

 

58
Genus Pflggipollenites Pocock, 1962

Pflugipollenites dampieri (Balme) Pocock, 1962
P1. 17, Fig. 16

Occurrence: rare, Upper Shale Member of Mancos.

Reference specimen: slide Ph688l-4, 42.7 x 101.2 .‘

Genus Exesippllenites Balme, 1957

 

Exesipollenites tumulus Balme, 1957
P1. 17, Fig. 11

Occurrence: rare to common, Upper Shale Member of Mancos.

Reference specimen: slide Pb688l-4, 46.3 x 92.5.

Genus gycadopites Wodehouse ex Wilson and Webster, 1946

 

?chadopites sp. 1
P1. 17, Fig. 3

Diagnosis: smooth; exine less than one micron thick; pointed to bluntly
pointed tapered oval in polar view; colpus full length of grain; 20 to
40 u.

Occurrence: rare, throughout sections.
Reference specimen: slide Pb6881-4, 42.0 x 96.8.

Remarks: Two size classes were counted separately, one 20 to 25 u (length),
the other 25 to 45 u.

?chadopites sp. 2
P1. 17, Fig. 6

Diagnosis: smooth; exine less than or equal to one micron thick; slightly
tapered oval; colpus full length of grain, widened at ends; 20 to 24 u by
10 to 15 u.

_gpcurrence: rare, Greenhorn Limestone, Lower Carlile Member and Upper
Shale Member of Mancos in Point Lookout Section; Lower Carlile Member and
Upper Shale Member of Mancos in Ute Reservation section.

Reference specimen: slide,Pb6252-6, 40.7 x 97.3.

59

?chadppites sp. 3
P1. 17, Fig. 5

Diagnosis: foveolate: exine less than one micron thick; tapered oval
in polar view; colpus full length of grain, often wider at its ends; 20
to 40 U long.

Occurrence: rare, uppermost sample of Point Lookout section only.

 

Reference specimen: slide Pb6244-3, 40.9 x 99.7.

Genus Eucommiidites Erdtman, 1948, emend.
Hughes, 1961

 

Eucommiidites cf. E, couperi Anderson, 1960
P1. 17, Fig. 9

Occurrence: rare to frequent, throughout both sections.

 

Reference specimen: Slide Pb688l-4, 32.1 x 99.9.

Eucommiidites cf. E. troedssonii Erdtman, 1948.
emend. Hughes,'l961
P1. 17, Fig. 8

 

 

Occurrence: rare, in Graneros Shale, Lower Carlile Member and lower
two-thirds of Upper Shale Member of Mancos in both sections.

 

Reference specimen: slide Pb6881-4, 43.7 x 104.1.

 

Euccommiidites sp. 1, Sp. nov.
P1. 17, Fig. 10

Diagnosis: like E. troedssonii in arrangement of furrows; psilate; oval
in polar view; oval appearing pointed at the ends and assymetrical in
lateral view; about 8 to 18 u long, 5 to 12 u wide.

 

Occurrence: common to abundant, throughout both sections.

Reference Specimen: slide Pb6357-10, 46.9 x 92.1.

60

ANGIOSPERMOUS POLLEN

Genus Tricolpopollenites Potonié, 1934

 

Tricolpoppllenites cf. 1, retiformis Pflug and Thomson
in Thomson and Pflug, 1953
P1. 17, Figs. 12-14, 17

 

Occurrence: common to frequent, throughout sections.

Reference specimens: slide Pb6881-4, 43.5 x 98.6, slide Pb6337-6,
38.1 x 92.9.

 

Remarks: Because of the poor preservation in some samples other Species
may be included here. Other possibilities are Tricolpites hians Stanley,
1965, I, parvus Stanley, Pseudotricolpites reticulatus Stanley, Fraxinoipol-
lenites crassimurus Groot and Penny.

 

Tricolpppollenites cf. 1, micromunus Groot and Penny, 1960
P1. 17’ Figs. 15, 17‘20

 

 

Occurrence: common to abundant, throughout sections.

Reference specimen: slide Pb6282-6, 35.1 x 105.5.

Tricolpopollenites henrici (R. Potonié)
Thomson and Pflug, 1953
P1. 17, Fig. 18

Occurrence: rare to common, throughout sections.

 

Reference specimen: slide Pb6288-7, 45.3 x 92.2.

Tricolpopollenites Sp. 1, Sp. nov.
P1. 18, Fig. 1

Diagnosis: usually preserved in polar view; polar view wide open circular;
psilate, apparently ektexine thicker than endexine; exine thickest in
inter-colpate areas, about 1 u thick; colpi with smooth margins, rounded
ends with constriction at equator; polar area index 1:3.5; diameter 20

to 25 u.

Occurrence: rare, Graneros Shale in Ute Reservation section, Lower
Carlile Member of Mancos in both sections, Juana Lopez Member of Mancos
in Point Lookout section.

 

Reference specimen: slide Pb6373-4, 37.0 x 101.8.

61

Tricolpppollenites sp. 2, sp. nov.
P1. 18, Fig. 11

 

Diagnosis: usually preserved in polar view; polar view open angular to
semiangular to subangular; psilate to granular; exine less than one micron
thick; colpi with smooth margins; polar area index 1:2 to 1:3; diameter

10 to 18 u.

Occurrence: rare, Lower Carlie Member and Upper Shale Member of Mancos.

 

Reference Specimens: slide Pb6881-4, 50.3 x 97.0, 41.9 x 91.8; slide
Pb6255-6, 111.7 x 40.00

 

Tricolpppollenites Sp. 3, sp. nov.
' P1. 18, Fig. 9

Diagnosis: preserved in polar view; polar view open circular to inter-
subangular; psilate (corroded?); exine about one micron thick; colpi
with smooth margins, endexine extending across colpi as a thin granular
membrane; polar area index 1:3.5; diameter 15 to 20 u.

Occurrence: rare, Lower Carlile Member of Mancos in Ute Reservation
section, Upper Shale Member of Mancos in Point Lookout section.

 

Reference specimen: Islide Pb6282-6, 35.0 x 92.7.

 

Tricolpopollenites sp. 4, sp. nov.
P1. 18, Fig. 7

 

Diagnosis: preserved in oblique view or polar view; polar view open
semiangular; baculate (Erdtman); exine about 1.0 - 1.511thick thinning
towards colpi from inter-colpate area; ektexine thicker than endexine,
tectate; colpi with smooth margins, with faintly granular margo about

2.0 - 2.5 upwide formed by extension of endexine (ekt - O, mem; code of
Faegri and Inversion, 1964); polar area index 1:2 to 1:3.5; diameter 25 to
35 u.

Occurrence: rare to common, Upper Shale Member of Mancos in both sections.

Reference Specimen: slide Pb6881-4, 32.0 x 100.5.

Tricolpppollenites sp. 5, Sp. nov.
P1. 18, Figs. 4, 10

 

Diagnosis: preserved in polar view; polar view open semiangular; psilate
(corroded?) to punctate; exine less than one micron thick, thicker at
poles than elsewhere; colpi with smooth margins, with margo about one
micron wide (ekt = O, mem); polar area 1:3.25; diameter 13 to 16 u.

62

Occurrence: rare, in Upper Shale Member of Mancos in both sections,
Lower Shale Member of Mancos in Point Lookout section.

 

Reference specimen: slide Pb6881-4, 40.4 x 94.5.

 

Tricolpopollenites sp. 6, sp. nov.
P1. 18, Figs. 2-3

 

Diagnosis: very slightly rhomboidal circle in equatorial view, wide

open semiangular in polar view; punctate; exine about one micron thick in
intercolpate areas and poles thinning towards the colpi; colpi with
smooth margins, with margo (ekt - 0, mem) about 2.25 n wide; polar area
index about 1:7; diameter 18 to 22 u.

Occurrence: rare, in Upper Shale Member of Mancos in both sections,
in upper Lower Shale Member of Mancos in Ute Reservation section.

 

Reference Specimen: slide Pb6881-4, 35.3 x 106.1, 39.9 x 93.7.

 

Tricolpopollenites sp. 7, sp. nov.
P1. 18, Fig. 6

 

Diagnosis: nearly circular in all orientations; open circular in polar
view; punctate to permicroreticulate, exine less than one micron thick;
colpi with smooth margins; polar area index about 1:3.5; diameter 5 to
10 u.

Occurrence: rare to frequent, Graneros Shale and Upper Shale Member
of Mancos in both sections, upper Lower Carlile Member of Mancos in
Point Lookout section.

 

Reference specimen: slide Pb6857-2, 41.0 x 103.1.

 

Tricolpppollenites sp. 8, sp. nov.
P1. 18, Fig. 19

Diagnosis: polar view circular to slightly semiangular; exine less than
one micron thick; reticulate, lumina one micron or less across, muri about
.75 micron wide; colpi with smooth margins; polar area index about 1:3.5;
diameter 15 to 2011.

Occurrence: rare to common, Graneros Shale, Greenhorn Limestone, Lower
Carlile Member and lower part of Upper Shale Member of Mancos in both
sections.

 

Reference specimen: slide Pb6337-l, 35.6 x 96.0.

 

63

Genus Tricolpites Cookson ex Couper, 1953

 

Tricolpites cf. 1. explanata (Anderson) Drugg, 1967
P1. 18, Figs. 12'13

 

Occurrence: rare to frequent in Upper Shale Member of Mancos in both
sections, in Lower Carlile Member of Mancos in Point Lookout section.

 

Reference specimen: slide Pb6881-4, 42.0 x 100.3.

 

Remarks: Two size classes were counted in this group. Those less than
about 20 u.were counted separately. The smaller group also tended to
be more circular in polar view with a proportionally reduced Size of
lumina and muri.

Tricolpites cf. I, bathyreticulatus Stanley, 1965
P1. 18, Fig. 16

 

 

Occurrence: rare to common, in Lower Carlile Member and Upper Shale
Member of Mancos in Point Lookout section, in Greenhorn Limestone, Lower
Carlile Member and lower part of Upper Shale Member of Mancos in Ute
Reservation section.

 

Reference spscimen: slide Pb6293-7, 35.5 x 94.9.

 

Tricolpites cf. 2, angploluminosus Anderson, 1960
P1. 18, Fig. 18

 

Occurrence: rare, throughout Point Lookout section, in Lower Carlile
Member and Upper Shale Member of Mancos in Ute Reservation section.

 

Reference Specimen: slide Pb6244-3, 40.0 x 94.3.

Genus Retitricolpites (Van der Hammen) ex Pierce: 1961

 

Retitricolpites cf. 2, geranioides (Couper) Brenner, 1963
P1. 18, Fig. 20

 

Occurrence: rare, uppermost Point Lookout section.

 

Referencesspecimen: slide Pb688l-4, 41.9 x 93.9.

64

Retitricolpites cf. 5, georgensis Brenner, 1963
P1. 18, Fig. 15
Occurrence: rare, Upper Shale Member of Mancos in both sections.

Reference specimen: slide Pb6282-6, 33.0 x 91.4.
Genus Trialappllis Stanley, 1965

?Trialapollis sp. 1
P1. 18, Fig. 14

Diagnosis: tricolpate (?); spherical rhomboidal to spherical apiculate
in polar view; exine about one micron thick; punctate to perdmicroreticulate;

colpi not obvious, what appear to be colpi may be folds; dimensions about
20 11.x 18 u.

Occurrence: rare, Upper Shale Member of Mancos in both sections.
Reference specimen: Slide Pb6878-3, 43.4 x 101.4.

Remarks: Stanley's description of the genus states that these grains
are acolpate. The specimens included here may not possess colpi and
fit well in this genus.

Genus Tricolporites Erdtman, 1947

Tricolporites rhomboides Anderson, 1960
P1. 18, Fig. 8
Occurrence: rare to common, throughout sections.
Reference specimens: slide Pb6881-4, 44.3 x 94.2, 42.7 x 93.5.

Tricolporites traversei Anderson, 1960
P1. 18, Fig. 5

Occurrence: rare to common, Upper Shale Member of Mancos in both sections,

questionable occurrence in Lower Carlile Member of Mancos in Point Lookout
section. '

Reference specimen: slide Pb6244-2, 42.0 x 97.5.

65

Genus Duploppllis Krutzsch, 1959

Duplopollis cf. 2, orthoteichus (Cookson and Pike) Krutzsch, 1959
P1. 18, Figs. 17, 21, 22

Occurrence: rare, Upper Shale Member in both sections.
Reference specimens: slide Pb6875-2, 49.0 x 87.2.
Remarks: Possibly included here are some Specimens of Cgpanieidites

reticularis Cookson and Pike, and C. major Cookson and Pike. Some speci-

mens were syncolpate at only one psle. The colpi not reaching but one-
half the way to the other pole.

 

Genus Porocolpopollenites Pflug in Thomson and Pflug, 1953

?Porocolpopollenites, Sp. 1, sp. nov.
P1. 19, Fig. 2

Diagnosis: Tricolpate (tricolporate?); very flat oblate oval in equatorial
view, open semisubangular in polar view; scabrate; exine less than one

micron thick; colpi with straight smooth margins; polar area index 5:7;
diameter about 20 u.

.Qgcurrence: rare, Upper Shale Member of Mancos in Point Lookout section,

in upper sample of Lower Carlile Member of Mancos in Ute Reservation
section.

Reference Specimen:, slide Pb6881-4, 43.5 x 89.3.
Genus Dicotetradites Couper, 1953

Dicotetradites cf. 2, clavatus Couper, 1953
P1. 18, Fig. 25

Occurrence: rare to common, throughout Point Lookout section, in
Graneros Shale, Lower Carlile Member and lower part of Upper Shale
Member of Mancos in Ute Reservation section.

Reference Specimen: slide Pb6227-10, 120.0 x 37.2.

66

Hexacolpate Pollen Grain
P1. 18, Fig. 24

Diagnosis: Hexacolpate; circular in all orientations; tectate perforate,
punctate; exine about 1.5 u thick, ektexine thicker than endexine; colpi
about 7 to 8 u long, with smooth margins; colpi arrranged so the inter-
sections of their extended ends form three congruent Spherical triangles
on the pollen grain's surface (see Wbdehouse, 1935, p. 170, fig; 27); dia-
meter 25 to 30 u.

Occurrence: rare, Upper Shale Member of Mancos; uppermost part only in
Ute Reservation section.

 

Reference Specimen: slide Pb6907-6, 33.4 x 94.3.

 

Remarks: This form of pollen grain may be simply a variant of the tricol-
pate grains referred to Tricolpopollenites retiformis Pflug and Thomson.

Genus Triporopollenites Pflug and Thomson
in Thomson and Pflug, 1953

 

Triporopollenites cf. 2, scabroporus Newman, 1965

 

 

Occurrence: rare to frequent, Upper Shale Member of Mancos in both
sections, in Juana Lopez Member of Mancos in Point Lookout section.

 

Reference specimen: slide Pb6881-4, 50.4 x 87.9.

 

Remarks: Those specimens with especially protruding pores were counted
separately.

Triporopollenites cf. 2, tectus Newman, 1965
P1. 19, Fig. 8

Occurrence: rare to common, in Upper Shale Member of Mancos.

Reference specimen: slide Pb6845-2, 33.1 x 96.4.

Triporopollenites sp. 1
P1. 18, Fig. 23

 

Diagnosis: preserved in polar view; semiangular in polar view; psilate
to granular; exine less than one micron thick; pores 4 to 51$ wide, with
ulcerate margin; diameter 13 to 181i.

,Qscurrence: rare to common, in Upper Shale Member of Mancos in both
sections, in upper sample of Lower Carlile Member in Point Lookout section.

 

67

Genus Extratriporppollenites Pflug, 1952

?Extratriporopollenites spp.
P1. 18, Fig. 29

Occurrence: rare, Greenhorn Limestone in both sections, in Lower Carlile

Member and Juana Lopez Member of Mancos in Point Lookout section.

Reference specimen: slide Pb6289-5, 37.7 x 88.7.

Remarks: All of these Specimens are poorly preserved. All are

semilobate to lobate in polar view and many exhibit what may be inter-
loculi and prevestibuli.

Genus Trudopollis Pflug, 1953, emend. Potonie, 1960

Trudopollis cf. 2, hemiparvus Pflug, 1953
P1. 19, Fig. 4

Occurrence: rare, Upper Shale Member of Mancos.

Reference Spscimen: slide Pb6881-4, 41.7 x 98.2.

Genus Labrspollis Krutzsch, 1968

Labrapollis globosus (Pflug) Krutzsch, 1968
P1. 19, Fig. 6

Occurrence: rare, in Upper Shale Member of Mancos.

Reference Specimen: slide Pb6881-4, 33.2 x 95.8.
Genus Triatrippollenites Pflug in Thomson and Pflug, 1953

Triatriopollenites cf. 1, rurensis Pflug and Thomson
in Thomson and Pflug, 1953
P1. 19, Fig. 1

Occurrence: rare to common, in Upper Shale Member of Mancos.

Reference specimen: slide Pb6880-4, 38.2 x 95.2.

68

Genus Plicapollis Pflug, 1953

?Plicspollis silicatus Pflug, 1953
P1. 19, Fig. 3

Occurrence: rare to frequent, in Upper Shale Member of Mancos.

Reference spscimen: Slide Pb6851-3, 37.3 x 94.8.

Genus Sporopollis Pflug, 1953

 

_§porgpollis cf. §, lsgueaeformis Weyland and Greifeld, 1953
P1. 19, Fig. 7

Occurrence: rare to common, in Upper Shale Member of Mancos.

Reference specimen: slide Pb6881-4, 45.8 x 97.1.
Genus Conclavipollis Pflug, 1953

Conclavipollis cf. 9, wolfcreekensis Newman, 1965
P1. 19, Fig. 5
Occurrence: rare, in Upper Shale Member of Mancos.

Reference specimen: slide Pb6881-4, 39.9 x 95.1.
Genus Proteacidites Cookson, 1950

Proteacidites thalmanii Anderson, 1960
P1. 19, Fig. 12

Diagnosis: 15 to 22 u in diameter; size of lumina decreases to punctate
towards poles.

Occurrence: rare to common, in Upper Shale Member of Mancos of both
sections.

Reference spscimen: slide Pb6244-3, 35.4 x 104.5.

69

Proteacidites thalmanii var. 1
P1. 19, Fig. 11

Diagnosis: 25 to 32 u in diameter; semiangular in polar view.

Occurrence: rare, in Upper Shale Member of Mancos in both sections.

 

Reference Specimen: slide Pb6244-3, 46.7 x 94.3.

Proteacidites thalmanii var. 2
P1. 19, Fig. 10

 

Diagnosis: 30 to 45 u; angular to slightly semilobate in polar view.

Occurrence: rare, in one sample in upper part of Upper Shale Member of
Mancos in Point Lookout section.

 

Reference specimen: slide Pb6869-3, 40.7 x 93.5.

 

Proteacidites cf. 2. thalmanii var. 3
P1. 19, Fig. 9

 

Diagnosis: 14 to 2011; lumina of uniform size or only slightly smaller
at the poles.

Occurrence: rare to common, Upper Shale Member of Mancos in both sections.

 

Reference specimen: slide Pb6881-4, 45.2 x 103.7.

 

Genus Liliacidites Couper, 1953

 

Liliacidites cf. 2, leei Anderson, 1960
P1. 19, Fig. 15

 

Occurrence: rare, throughout section except for Graneros Shale amd
Greenhorn Limestone in Ute Reservation section.

 

Reference specimen: slide Pb6881-4, 49.9 x 91.4.

 

Genus Peromonolites Couper, 1953

 

Peromonolites peroreticulatus Brenner, 1963
P1. 19, Fig. 14

70

Occurrence: rare, in Greenhorn Limestone of both sections, in Lower
Carlile Member of Mancos in Point Lookout section, in one sample in
lower Upper Shale Member of Mancos in Ute Reservation section.

 

Reference specimen: slide Pb6273-5, 34.5 x 96.3.
Genus Trichotomosulcites Couper, 1953

Trichotomosulcites cf. 2, contractus Anderson, 1960
P1. 19, Fig. 13

Occurrence: rare, upper part of Upper Shale Member of Mancos in
Point Lookout section only.

 

Reference specimen: slide Pb6881-4, 41.6 x 102.3.

71

IV. PALEOECOLOGY

Approaches to Studying the Relationships Between

and Ocean-Bottom Environments

To determine where different kinds of dispersed plant micro-
fossils tend to occur in marine sediments two empirical approaches might
be taken. One approach involves an examination of palynomorphs in modern
marine environments and in modern plant communities. The other approach
involves an examination of palynomorphs in rocks that can be identified
with environments of desposition. The first type of approach has been
carried out in a number of places around the world with greater or lesser
degrees of experimental design, statistical reliability and areal coverage
(Muller, 1959; Rossignol, 1961; Groot, 1966; Stanley, 1965, 1966; Traverse
and Ginsburg, 1966; Cross, et a1 , 1966; Williams and Sargeant, 1967;
Koroneva, 1957, 1964).

Aside from Staplin's (1961) study of Devonian reefs and de
Jekhowsky's (1963) study of the Triassic of Madagascar, few deliberate
approaches of the second type have been made. Usually they are in the form
of secondary interpretations that are made after a large number of data have
been gathered on certain fossils. Often these data are of varying reliabil-
ity and often are not directly comparable from worker to worker. "Paleo-
ecological" interpretations of rocks have been made by comparing them with
vaguely documented analog models in the modern environment (Upshaw, 1959,
1964; Sarmiento, 1957; Zaitzeff, 1967). It seems that after the suggestion
was made by Hoffmeister (1954) and Woods (1955) that certain ratios and
quantities of palynomorphs may reflect distance offshore, palynologists
have not rigorously tested its validity. Apparently nowhere have the data
been published that are basic to these suggestions. Some of Hoffmeister's

original ideas appear to be based on the assumption of wind transport of

72

pollen and spores from their source to the sea. Recent work has shown
that wind may commonly not be a factor (Mfiller 1959; Cross, et a1 1967;
Stanley, 1965). Although Hoffmeister's hypotheses may well stand the test
in some instances, they should be subjected to more testing before they
are considered reliable tools.

Ideally, the second type of approach requires the identifica-
tion of environments of deposition by simply examining the rocks and their
facies relationships. These environments might be identified by estima-
tions of water depth, distance offshore, water temperature, salinity, tur-
bulence, or ion and particulates concentrations. In addition, all hori-
zontal variations in these parameters should be detectable along firmly
established "time surfaces".

An interpretation of pre-existing terrestrial plant communities
might be based on extensive collecting and study of plant macro- and micro-
fossils that are preserved in rocks of continental as well as of marine
origin. But because little is actually known about how the continental
part of the fossil record can be interpreted, there is essentially no
record of the terrestrial communities when compared with the record of
marine communities and environments. This limits the scape of interpreta-
tions that are based on this type of approach.

Because the distribution of the plants within the terrestrial
environment is unknown, fossil pollen grains and spores occurring in rocks
of marine origin might be considered merely as sedimentary particles origi-
nating from a stream mouth at the Shore. This need not be the case for
marine phytoplankton pOpulations. Although algal cysts in settling to
the bottom may drift from directly below their planktonic population, many
of these cysts are, in fact, benthonic organisms (Wall and Dale, 1968) and

their fossils may then be considered as part of a biocoenose. This second

73

type of approach is the most direct approach to learning about the habitats
of extinct organisms, especially extinct micrOplankton.

This study is an example of this Second kind of approach. The
well-documented sequence of transgressions and regressions that is preserved
in Upper Cretaceous rocks of southwestern Colorado was chosen as a CODCGP'

tual model. -This model is discussed below in detail. An explanation of
this model is basic to the understanding of how the interpretations of the
palynomorphs and their relation to the sedimentary environment were made.

The data gathered during this study were interpreted by subject-
ing them to multivariate analysis (factor analysis) in addition to simply

plotting them in the form of relative frequencies of palynomorphs and num-

bers of palynomorphs per gram of rock.

Model of Transgressions and Regressions

Basis for Model

The conceptual model of a transgressing and regressing shore-
line that is utilized in this study is based on the interpretations of
Pike (1947), Dane (1960) and Lamb (1968) (see also Krumbein and Sloss,
1951, p. 261; Weller, 1960, p. 484-501) and is represented diagrammatically
in figure 7. This diagram illustrates the stratigraphic relationships of
the rock units present in a cross-section along a line that is normal to
the trend of the shoreline and that includes the Point Lookout and Ute Res-
ervation sections. The line of section is shown in figure 1 as line A-A'.
It will be determined whether or not palynomorph assemblages from within
the Mancos Shale reflect. transgressing and regressing environments that
parallel this oscillating shoreline.

The major transgressions and regressions that are represented

by the Greenhorn Limestone, the Carlile Shale and the Upper Shale Member

74

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75

of the Mancos as Shown in figure 7 are equivalent to T1 R1 T2 and R2
of Weimer (1960); Transgressions 1 and 2 and Regressions l and 2 of
Kauffman (1967); and in part to the Greenhorn Cyclothem of Hattin (1964).

These oscillations of the shoreline are recognized over the whole western

interior of the United States.

Steeply-Dipping "Time Lines"

Some explanation may be in order concerning the steeply-dipping
"time lines" that have resulted from the graphic correlation between the
two sections. Pike's (1947) correlations based on molluscs Show the same
steeply-dipping "time lines". Assuming this correlation is a good approxi-
mation of the actual case (this assumption is the basis for further inter-
pretations made in this study), the sloping "time lines" may be explained
in the following way.

One may consider that the Upper Cretaceous sea-bottom in south-
western Colorado was a plain with water depths and slope similar to those
of a modern Shelf environment. Sand, silt and clay were being dumped from
rivers flowing into the west edge of the Seaway. In the modern shelf en-
vironment, the profile of the surface over which sediment is accumulating
offshore is generally in the shape of a sigmoid curve (fig. 8A). This
curve is also a "time line" since it represents the present sea bottom. An
example of this profile is the longitudinal profile of a delta. However,
the geomorphic feature of a delta may not always be manifested. In an area
undergoing active sedimentation, a profile offshore from an interdeltaic
barrier island-type shoreline should have a similar although subdued pro-
file. It is commonly assumed that this profile is near equilibrium with
regard to water turbulence, current velocities, sediment supply, grain-size
frequency distribution, etc. (Twenhofel, 1950, p. 230-233; Weller, 1960,

p. 498-501; Shepard, 1960, p. 65; Scruton, 1960, p. 88-93; Curray and Moore,

1964).

76

 

 

 

 

 

 

 

 

 

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- SEA SURFACE ......
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APPROX. IO MI.
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STRATIGRAPHIC STRATIGRAPHIC
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"time lines" within it at times, t
bottom profile; (B) illustrates sedwarg mig
straight-line time correlations that could

3, t , t , and t (A) shows
ration - a regression; (C) shows
be made between sections A and B.

 

 

 

77

If the shoreline regressed in response to seaward accretion of
sediments the profile of equilibrium would migrate seaward. If the whole
sediment pile is subsiding, a wedge-shaped mass of sediment would be out-
lined as this profile migrates (Scruton, 1960; Curray and Moore, 1964).
This wedge would be contained between two "time lines" (or "surfaces" in
the three dimensional sense). Figure 8B is a diagram depicting slight
subsidence and the migration of the profile seaward and its position at
several instants in time. In no case do the "time lines" (profiles) rise
seaward.

If these sediments are preserved intact, the "time lines" should
retain their same relationships. (With compaction and with subsidence that
tends to be greatest in a seaward direction, the "time lines" may become
even more steeply-inclined seaward.) Should two stratigraphic Sections be
examined at the positions indicated in figure BB, the inclined "time lines"
would cut the two sections as shown in figure 80.

A transgressing shoreline would be accompanied by a shoreward
movement of the profile. If there were subsidence and the sediments were
preserved, this would result in a similar sequence of change in slope of
the "time lines" between the two sections.

The rocks in the upper part of the Ute Reservation and Point
Lookout sections reflect the northeastward migration of a elastic wedge
associated with the regression of the shoreline represented by the Point
Lookout Sandstone.

The position of the thickest part of a wedge in relation to the
shoreline is probably chiefly determined by the grain-size frequency dis-
tribution of the contributing river's load and the velocity of the vector
of water movement in a seaward direction. Apparently the thickest part

of the wedge that is represented by the Upper Mancos Shale was composed

78
of silty and slightly-sandy clays and lay roughly 30 miles offshore.
(Evidence for this is presented later.)

In a situation like the Upper Cretaceous of Southwestern Colorado
such a convergence and divergence of "time lines" between two sites can be
interpreted as a change in the position of the elastic wedge.

Because the classic area of the standard Upper Cretaceous section
in the Missouri Valley and the Great Plains is situated on the very thin
seaward-edge of the wedge, the "time lines" between Sections there will be
essentially parallel. Probably only in the area of nearer-shore environ-

ments in western Colorado, eastern Utah and the Four-corners area can these

dipping "time lines" be drawn between stratigraphic sections.

The Carlile-Niobrara Unconformity

The position of the "Carlile-Niobrara" unconformity in the dia-
grams (fig. 7) represents the latest published regional interpretation._
This was made by Lamb (1968) and incorporates correlations that are based
on Foraminifera in addition to that based on molluscs that were utilized
in earlier correlations.

As depicted in figure 7 the unconformity truncates the Gallup
Sandstone and to the north moves down through shale of Carlile age finally
cutting into the Juana LOpez Member. Farther north it rises in the section
and may terminate before it reaches the Point Lookout section.

The exact position at which the unconformity is placed in the
Point Lookout and Ute Reservation sections is disputable. The unconformity
is recognizable throughout the area to the south and southeast where the

Tocito Sandstone unconformably overlies shale or.the Gallup Standstone.

79

(Lamb, 1968). Unfortunately the Tocito Sandstone is absent from both the
Ute Reservation and the Point Lookout sections. The Tocito is a coarse-
grained, commonly cross-bedded, clean quartz sandstone up to 40 feet thick.
Aside from some quartz sandstones up to a few inches thick the only sandv
stones present in the two sections over this interval are calcarenites and
these are up to only a few feet thick. These calcarenites are reasonably
assigned to the Juana Lopez member. The decision to place the unconform-
ity in the Point Lookout and Ute Reservation sections as it is Shown in
the diagram is based on the following pieces of evidence.
(1), The only quartz sand in this interval in either section
9 is situated in the Ute Reservation section about 50 feet
above a unit of thin calcarenites interbedded with shale
that is attributable to the Juana LOpez Member. This
would correspond closely with the level of the unconform-
ity as interpreted by Lamb.
(2) A sandy (calcarenite) interval with very thin calcarenites
occurs 225 feet above the Juana Lopez at Point Lookout.
This probably reflects shoaling that can be correlative
with a shallower area to the south which was undergoing
appreciable erosion. As Lamb suggests, the unconformity
is higher in the section at Point Lookout than in sections
to the south. At Point Lookout it probably does not repre-
sent an appreciable hiatus.
(3) In the range chart of palynomorphs arranged according to
lowest occurrences in the Ute Reservation section (fig. 10)
there are 17 forms that first occur just above the interval
of thin sands and sandy shale that lies 50 feet above the
Juana LOpez. This indicates an appreciable break in the
rock record. No hiatus of such magnitude is indicated at

Point Lookout (fig. 9). .

80

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section. See oppOSite for taxon names.

 

 

 

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(4)

(5)

84

Factor analysis (to be discussed later) indicates that a
sample within the quartz sandy interval mentioned in (1)
above in the Ute Reservation section was laid down "nearer
shore" than samples immediately above or below. In this
interval at Point Lookout no "near-shore" samples occurred.
The upper of two "time lines" based upon the graphic corre-
lation in this interval rises going from the Ute Reserva-
tion section to Point Lookout. This could result from the
removal of some of the rock column at the Ute Reservation

section relative to the Point Lookout section.

Other possible interpretations of the position of the unconform-

ity are summarized separately below. These are rejected hypotheses.

(1)

(2)

In both sections the unconformity cuts the Juana Lopez
Member. The sand immediately above the unconformity may
be formed from shell debris (producing a calcarenite) at
these sites rather than being formed from quartz sand.

The uppermost calcarenite assigned to the Juana Lopez at
Point Lookout weathers lighter in color, has fewer fos-
sils and is more regularly thin-bedded than the next lower
calcarenite which is 30 feet below. This could be a cal-
carenite facies of the Tocito.

The unconformity is situated immediately above the Juana
Lopez Member in the Ute Reservation section and is absent
from the Point Lookout section. The Tocito equivalent in
the Ute Reservation section might be a calcarenite that is

indistinguishable from the Juana Lopez Member as in the

85
last paragraph. According to Lamb's interpretation the
unconformity could lie immediately above the Juana Lopez
at this locality.
(3) The unconformity is not present in either section. The
lack of any unequivocal lithologic evidence of an uncon-

formity within the two measured sections suggests this.

Time-Transgressive Nature of the Juana Lopez Member

As interpreted here and in Lamb (1968) the Juana Lopez Member
crosses time planes and is younger to the northeast. The correlation
made here indicates that the sediments that were laid down at the time
of the Pescado tongue transgression lie above the Juana Lopez in the Ute
Reservation section and below the Juana Lopez in the Point Lookout section.
The rocks of the Juana LOpez represent a shoal that migrated northeastward
with the regression that laid down the sediments of the Gallup Sandstone

further south.

Redeposition of Palynomorphs

Recycling, reworking or redeposition of palynomorphs has often
been demonstrated and can intuitively be expected in any rock that con-
tains terrigenous detritus. It is obvious that the presence of unrecog-
nized redeposited palynomorphs could cause one to draw erroneous conclu-
sions.

In the Mancos Shale one should expect to find some pre-Mancos
palynomorphs. However, only about a dozen spores of recognizable pre-
Mancos age were observed in the examination of all the residues used in
this study. This indicates that reworking may not be statistically sig-
nificant here. Of course reworking of long-ranging palynomorphs from
pre- or older Mancos into younger Mancos may go undetected. However,

the thickness of Upper Cretaceous rocks preserved in this area from both

86
continental and marine environments suggests that there was considerable
subsidence relative to sea level during their deposition. This subsidence
would tend to allow sediment to collect with little further erosion and
transport once it had been deposited. The amount of reworking of micro—
fossils within the Upper Cretaceous could be negligible on the time scale
considered here. No "reworked palynomorph" group was recognized and all
interpretations of the data assume that there is no reworking of palyno-
morphs. I

Analysis of the Data

Assemblage Approach versus Taxon Approach

Two approaches to the interpretation of the fossil assemblage
data can be made. One kind of approach considers the assemblage of each
sample as a whole and is analogous to the interpretation of whole modern

La mogIeI a
communities. The other kind of approach considers the distribution of
each taxon separately and is analogous to interpretations of individual
modern species populations. (8 Vi)

Factor analysis in the Q-mode, to be discussed below, is a
community-type of approach. (although not applied in this study, factor
analysis in the R-mode is of the pOpulation-type of approach.) In this
study, in addition to Q-mode factor analysis, the calculation of diversity
indices for each sample is of the first type of approach. The identity
of each taxon is unimportant in this approach.

Interpretations of relative frequencies and numbers per gram of
the individual taxa is the second type of approach. Here one is interest-

ed in learning something about the distribution of the original living

population represented by the individual fossil taxa.

87

Factor Analysis

Instead of comparing samples qualitatively or graphically using
a few common palynomorphs, as has been commonly done in palynology, it is
desirable to compare each sample with all other samples on the basis of its
complete assemblage considering the abundance of each species in each sample.
A number of multivariate mathematical analyses are now known that can do
just this. Among these is factor analysis. Factor analysis, as Opposed to
other methods, was used in this study because (1) a computer program was
readily available (this type of analysis is essentially impossible without
the use of a high-speed computer) and (2) this analysis technique had been
used to interpret a number of different kinds of data, including paleontologic,
with satisfactory results.

The specific objectives of factor analysis as given by Imbrie
and van Andel (1964) are as follows:

"...vector (factor) analysis of a set of compositional data may

be initiated with one or more of the following three objectives:

(1) to achieve a parsimonious statement of the information

contained in the table of data; (2) to classify the samples

into natural groups; and (3) to resolve each sample into a

small number of components, each component representing the

contribution of a functional unit (or end member)."

The computer program utilized in this study is the Columbia
Vector Analysis Program (COVAP) developed by Manson and Imbrie (1964).
It was adapted for use on the CDC 3600 computer at Michigan State Univer-
sity and later on the UNIVAC 1108 computer at Shell Oil Company's Houston
Data Service Center. A preliminary program was developed by Don Merritt
of Michigan State University to simplify data input into COVAP. The math-

ematics of the program and some of the underlying theory is discussed in

88
Imbrie (1963, 1964), Manson and Imbrie (1964), and Imbrie and van Andel
(1964). The theory of factor analysis is covered in detail by Harman
(1960), Catell (1952) and others.

COVAP as it is utilized in this study handles the counts of
palynomorphs as percentages and analyzes them in the Q-mode (see Catell,
1952). The program utilizes the principal components method of factor
solution and the varimax method of factor rotation. In addition an oblique
projection analysis is performed which resolves the samples into and mem-

bers that are themselves actual samples (Imbrie and van Andel, 1964).

In addition to factor analysis of the whole set of data that
included the samples from both sections and 220 taxa (variables), the
analysis of each of the following sub-sets was also carried out.

(1) pollen grains and spores (120 variables)

(2) microplankton (100 variables)

(3) all pollen grains, spores and microplankton that range

completely over both sections (65 variables)

(4) All pollen and spores that range completely over both

sections (43 variables)

(5) All microplankton that range completely over both sections

(22 variables)

The analyses were performed using 10, 9, 8, 7, 6, 5, 4, and 3
end members for each set of variables. Reducing the number of variables
from 220 to 65, from 120 to 43 and from 100 to 22 in the different sub-sets
of data generally did not affect the and members that were chosen in each
sub-set.

The simplest factor analysis of the data using 22 long-ranging

microplankton and three end members with 70% communality appears to give

89

the most meaningful results. By restricting the number of variables to
those species or other taxa that range completely through both sections
it was hoped that the influences of evolutionary change on the analysis
would in part be removed. Also, the changes in the marine environment
should be more clearly shown by further restricting the variables to the
micr0plankton. An interpretation of this analysis was made with objective
(2) of Imbrie and van Andel in mind with the samples being distributed
into three groups. Each group contains one end member together with all
those samples that are most heavily "loaded" on that end member.

In figure 11 each factor group of samples is represented by a
pattern. The distribution of the members of each group is shown in each
stratigraphic section and "facies boundaries" are drawn between the samples

/

These boundaries directly reflect the transgressions and regres-

of different groups.

sions of the shoreline as indicated in figure 11. As alluded to above, the
occurrence of a member of factor group 3 immediately above a member of
group 1 in the middle of the Ute Reservation section suggests the position
of an unconformity. The inference is made here that these three factors
are all largely correlated with distance offshore. Group 1 tends to be
farthest from shore, Group 3 tends to be nearest to shore, and Group 2
appears to be intermediate.

The influences of environmental factors other than those related
to distance offshore might be uncovered with further study. In this study
however, "distance offshore" is the only environmental parameter that is
"controlled" and its "effect" is the only one that can be realiably inter-
preted. The possible real environmental factors controlling this distri-
bution, if this is indeed what they are, will be discussed after other

kinds of evidence are presented.

90

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91

The following microplankton were used in the factor analysis.

Hystrichosphaera ramosa var. 2
H. ramosa var. 3

Form F sp. I
Oligosphaeridium(gulcherrimum
Cordosphaeridium spp.
Exochosphaeridium_phragmites
Palaeohystrichophora infusoroides
.2. infusoroides var. l
Palaeohystrichophora spp.
Diconodinium arcticum
Hexagonifera suspecta var. 1
,fl. suspecta

Dinogymnium sp. 1

Dinogymnium sp. 2

 

Form B sp. 1
Form B sp. 2
Form B sp. 3
Form C sp. 1
Form C sp. 2
Form S sp. 1

Michyrystridium spp.

Surculosphaeridium cf.,§. vestitum
Estimation of Distance Offshore

The distance offshore at which each rock sample was deposited
was determined by interpolation from curves (fig. 12). These curves
were constructed from information shown in figure 7 (which is based on
figure 7, page 94, and plate 11 of Pike, 1947, and figure 3, page 51,
of Dane, 1960). The distances of the shoreline from the sites of the
two stratigraphic sections as determined from these published illus-
trations were plotted on two graphs, one for each section. One graph
has as its ordinate the distance (in feet) above the base of the Point
Lookout section. The other graph has as its ordinate the distance (in
feet) above the base of the Ute Reservation Section. Both graphs have
distance offshore on the abscissa. The positions of each transgression
and regression in either section was determined from the correlation
lines and the pattern of factor groups shown in figure 11. Because the

exact geometry of the rock record and the rates of change in subsidence

92

 

 

 

 

2000 —
I800 #-
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0 I00 200 300 0 I00 200 300

MILES OFFSHORE

FIGURE 12.--Curves for the Point Lookout section (left) and the Ute

Reservation section (right) used to determine distance offshore for each

sample. These curves are based on the results of the factor analysis,
Pike (1947) and Dane (1960).

93
and in shoreline oscillation are not known, the control points on the
graph (positions in each section of changes from transgression to regres-
sion or regression to transgression) are connected simply by straight
lines. The distance offshore at which each sample was deposited is taken
as the X-coordinate of the intercept of the zigzag curve with the line
representing the distance of the sample above the base of the section.
These values for distance offshore for each sample are the basis

for the interpretations made below concerning diversity, relative fre-

quency and numbers per gram of rock.

Diversity

"Diversity" as used here denotes both richness (number of
species) and the distribution of numbers of individuals among the species.
Diversity has thus been recognized as a character that is useful in com-
paring communities regardless of their genetic composition. To make such
comparisons one must calculate same index of diversity for each community
that is to be compared. Commonly within a community there are only a few
species that are abundant while many are relatively rare, but e degree
to which this is true varies from community to community. The sanctity
of the physical or chemical environment or the intensity of interspecific
competition within a community appears to be reflected in the diversity
of that community (Odum, 1957; Odum, Cantlon, and Kornicker, 1960). When
compared along gradients of latitude or of environmental factors (salin-_
ity, temperature fluctuation, insolation, etc.) communities vary in diver-
sity. For example, a tropical rain forest is more diverse than an arctic
tundra and a quiet-water environment is more diverse than a turbulent-

water environment.

 

I.I

.k.

 

94

In this study diversity indices were calculated for the palyno-
morph assemblage in each sample in an effort to determine if an empirical
relation exists between the estimated distance offshore (above) and the
diversity of a fossil assemblage (being analogous to a community).
Although several diversity indicies have been pr0posed, one that is widely
used in current ecological studies is an index derived from information
theory. 'This form is used here. The advantages of this form of diversity
index are discussed in Margalef (1957) and Patten (1962). The assemblage

diversity index of a sample is given by:

k
D = {Eini log(ni/N)
i=1
where ni = number of individuals in species i
k = number of species in the sample
N = number of individuals in the sample (sample size)

These calculations are based on only those palynomorphs that were counted
within the sum of 500 in each sample.

In figure 13 the diversity indices for (l) microplankton and
(2) pollen and spores are plotted against the estimated distance offshore.
The points on the graph appear to reflect distance offshore.

The diversity of microplankton tends to increase offshore while
the diversity of pollen and spores decreases offshore. The specific causes
for these changes are not known. However, it would appear that the causes
are related to some environmental factors that correlate with distance off-
shore. The diversity of the pollen and spores assemblage might decrease
offshore simply because of a sorting process. As the grains settle from
suspension only those that have reached the sea in great abundance, have

high buoyancy and that are resistant to corrosion may reach greater dist-

95

 

 

 

 

POLLEN + SPORE DIVERSITY ‘
HICROPLRNKTON DIVERSITY o
700 o 0
° 0
600‘ 00 a o o o
A A 6 ‘ O O
t 500 I, 6 fig, . 0 ° 0 0 °
I—I 0 05 AA “‘00 (g o
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9<>o<> . ‘
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0 I I I I I I I I
0 50 100 150 200 250

MILES OFFSHORE

FIGURE 13.--Diversity of Microplankton and of pollen and spores plotted
against distance offshore.

H.

"J

96

ances offshore. Thus only a "specialized" few would reach far offshore.

Perhaps the micr0plankton are more diverse farther offshore
because the environment is more stable there. There would be less fluc-
tuation in salinity, turbidity and nutrients due to variations in the
influx of stream waters. Because the water depths were probably greater
farther offshore there would be less frequent agitation due to wave motion
below certain depths.

The variation in diversity of both groups decreases with dis-
tance offshore. rThis, to may reflect the stability of the environment.
Greater variation in diversity indices would indicate that the stability

of the environment fluctuated.

"Paleoautecology"

As stated above, the factor analysis in the Q-mode and diver-
sity indices fail to reveal any specific information about the individual
taxa of palynomorphs. The term "paleoautecology" infers that some know-
ledge is gained about the autecology of the once-living organisms whose
existence is recorded in the form of fossils. With our present state of
knowledge inferences are usually limited to those concerning the habitat
of some of these organisms and are commonly based on somewhat gross as-
sumptions.

When interpreting fossil dinoflagellate cysts we must assume
that (1) large numbers of cysts of a species reflect large numbers in
its living population; (2) the cysts are found in their natural (but
lithified) substrate (if it is assumed that they are benthonic life
stages) or they are in the sediment directly beneath their motile_plank-
tonic population (if they are not considered benthonic); (3) a dominant
of a fossil cyst assemblage was a dominant of the dinoflagellate plankton
population in life - in other words, the intrinsic rates of cyst produc-

tion and preservation are the same in all dinoflagellate species.

97

A check of the above assumptions applied to modern dinoflag-
ellates would require studies of living populations. Because many dino-
flagellate cyst-species are extinct these studies would have limited
value. Even extant cyst-species that are found in the fossil record can
not always be identified with their motile form. Wall and Dale (1968)
have shown the apparent multiplicity of some cyst types attributable to
single living motile species as well as the multiplicity of some motile
species attributable to a single cyst type. Obviously many more data
are needed on the morphology, life cycles, and population dynamics of
living dinoflagellates before the ecology of fossil cysts can be inter-
preted correctly. Despite the realization of these shortcomings in
interpreting these fossils, some interpretations will be made here that
are based on (1), (2), and (3), above. These interpretations as well
as those of pollen and spores are based on graphs of relative frequencies
and numbers per gram of rock of various palynomorph taxa plotted against

distance offshore.

Distributions of Individual Taxa

To interpret the relationship between distance offshore and
the abundances of various palynomorphs two approaches are taken. (1)
The abundances of a palynomorph in each of the two sections may be com-
pared simply by considering the sections as two gross samples situated
at different distances offshore. (2) The relative frequencies and numbers
per gram of common long-ranging palynomorphs may be plotted on a graph
against the estimated distance offshore to determine if they tend to
reflect distance offshore.

When the two sections are compared as two gross samples most

of the taxa occur in higher relative frequencies in the Point Lookout

98

section or they have essentially equal values in both sections. Those
forms with higher relative frequencies in the Ute Reservation section

are: Cyamtiosphaera spp., PterispermOpsis spp., Form C sp. 1, Form S

 

 

sp. 1 and ?Horologinella spinosa Cookson. These few taxa tend to be

 

more abundant nearer shore than the Point Lookout section and tend to
lower the relative frequencies of all the other palynomorphs nearer
shore.

In figures 14 through 22 are shown the graphs of percentages
and numbers per gram of rock of the common palynomorphs found in the
Mancos plotted against the estimated distance offshore.

By examining these graphs one should gain some idea of where
the individual palynomorphs taxa tend to be differentially concentrated
in relation to the shoreline. These distributions may be interpreted in
light of the palynomorph sedimentation rates which in turn may be deter-
mined by the size and hydrodynamic properties of the palynomorphs, their
supposed initial production, their susceptibility to decay, the location
and size of their supposed source area and their mode of transport.

Distributions of numbers of various palynomorphs per gram of
rock should aid in the interpretations of relative frequency distribu-
tions. However, they must be considered in view of sedimentation rates
of inorganic detritus as well as those of the organic particles.

Although trends in some palynomorph distributions are suggested
by these graphs, control of more lithologic parameters, more well-chosen
stratigraphic sections and more samples taken at closer intervals are
needed before one can really begin to understand the role of environment
in controlling these distributions.

An attempt is made here to interpret the distributions of the

more common palynomorphs in the Mancos Shale as reflecting reversible

99
environmental factors. Although they are not clear-cut, these dis-

tributions may at least serve to cast some doubt on the wide use of

relative abundance peaks for time correlation.

Pollen and Spores

Class0pollis spp. --> The distributions of the relative fre-

 

quency (all percentages of pollen grains shown in the graphs are based
on the sum of pollen and spores only) and the number per gram of rock
of Classopollis spp. are shown in figure 14. The highest relative
frequencies occur in samples from farthest offshore.

This distribution perhaps reflects the mode of transport of
the grains. Contrary to what Pocock and Jansonius (1961) state,
Classopollis pollen grains may have been relatively buoyant. The tegil-
late exine (see Petitt and Chaloner, 1964) could serve to make them less
dense than most other pollen types. Also, they were probably produced in
large numbers comparable to modern pine.

How such distributions of the pollen grains might be produced
is suggested in the modern Gulf of California. In sample transects off
the river mouths in the Gulf, percent pine pollen is high in the most
seaward samples (Cross, et.al, 1967). this may represent the distribu-
tion of pollen grains that are transported through the air to the sea
surface as Opposed to the distribution of grains that are transported to
the sea by water. The air-transported grains would tend to be carried
farther out to sea than the water-transported grains which would be de-
posited nearer shore. In addition to its being more widely dispersed by
wind, pine pollen tends to predominate simply because it is so abundant
relative to other pollen grains. Classopollis pollen may have behaved

in a manner similar to pine pollen.

PERCENT

PERCENT

60

U)
D

25

20

a...
GI

H
O

CLHSSOPOLL I 3 SP? .

 

 

 

 

 

 

100

a o o
.I 00.0 o 0
° 0
I . ° . 0°
1’ W5 3 °
0 50 100 150 200 250
MILES OFFSHORE
BISHCCRTE GRQINS
I % °
0
0 O o
0‘ .0 o.
4| 0 v 0 0° 0.
J’CIOI o e.
Luce.” .. ..

 

O 50 100

MILES OFFSHORE

 

150 200 250

GRRINS/GRRM X 10’

O

t-o 0-0 N N
O 0'! 0 GI

GRRINS/GRRM X 10’

CLFISSOPOLL I S SPP .

 

 

 

 

0

J
.. O
-I s o

0
.4 000 °
I 0°00. 0°

'50 0 o ‘
0 50 100 150 200 25

MILES OFFSHORE

BISFICCFITE GRFI I N8

 

 

 

.°
0 If.
. .0 :Zd.. £I'.
o
A: I'M. 0.9.'; | ‘
O 50 100 150 200 25

MILES OFFSHORE

FIGURE 14.--Relative frequency and grains per gram of Classopollis spp.

and of bisaccate grains plotted against distance offshore.

 

The percentages

are based on the sum of pollen and spores.

101

Another explanation is that Classopollis pollen may simply
be more durable to the corrosion accompanying seaward transport. This
reasoning can also be applied to the distribution of pine pollen since
it has been shown to be more durable than most common pollen grains

(Sangster and Dale, 1964; Havinga, 1964).

The highest numbers of Classopollis grains per gram of rock

 

occur at intermediate distances offshore. A possible cause for this
will be mentioned later.

Bisaccate Pollen -- If Classopollis pollen behaved similar to
bisaccate pollen one would expect them to have similar distributions.
Unfortunately bisaccate pollen is not overly abundant in the Mancos Shale.
The distributions of bisaccate pollen shown in figure 14 show a slight
tendency to increase offshore.

Inaperturopollenites sp. 1 -- The percentage of this taxon

 

tends to increase offshore (fig. 15) this may reflect air transport

for this Taxodiaceous pollen. Taxodium grows in mostly coastal, swampy
riverside habitats and probably contributes pollen to the air for long-
distance transport. Some may also be supplied to the stream's suspended
load which could result in the moderate relative frequencies in the near-
shore samples. Numbers per gram of rock are high over a wide range.

Tricolpopollenities cf. 2, micromunus -- The distributions of

 

 

percent of total pollen and spores and numbers per gram of rock of
Tricolpopollenites cf.,3. micromunus are shown in figure 15. The highest
relative frequencies tend to occur near shore with the highest number per
gram of rock at 75 to 100 miles offshore. Its abundance, size and form
would suggest that it is wind pollinated. The approximate mean distance

is 16 u.. As suggested by Hoffmeister (1954) the ratio of small diameter

. 7. JIM. .r.

..rL

~ 2

IM‘ L 11‘

2‘ Aw‘

INRPERTUROPOLLENITES SP. 1

 

 

 

 

 

 

 

 

 

102

100 3* 100
.I 0
CD
. F480
_ ><
I" o :50
2: ‘ ° 0
OJ 0 E
050 "‘ o O
0: ° 3 \\
LLJ a o 0 0 40
O_ o 0 (O
a o J? 0 o 0 2:
II ':,0‘E:o So “’09 o h”
. GI. o o CI:20
.0 0 .° 0 % °° 2‘3
0 o
. o- s
0 :; T I I I I r r T 0
O 50 100 150 200 250
MILES OFFSHORE
TRICOLPITES CF. I. HICROHUNUS
80 150
.I n
o a: CD
4 '_'120
o ><
F— . o
I:
:3 o 00 0:90
0‘0 “ 0° 0 O (r
0: CD
In o “’0 \60
l 1L 0 0 o O U)
db‘3 0 o :5
0° 93 o o 0:30
0 0130‘, o 2%
0 0° 0 o
0 pr T r $cr I r T 0
0 50 100 150 200 250

MILES OFFSHORE

FIGURE 15.--Relative frequency and grains per gram of Inapgrturopollenites
sp. 1 and of Tricopites cf. 1. micromunus plotted against distance off-
Percentages are based on the sum of pollen and spores.

shore.

INRPERTUROPOLLENITES 5P.

 

l

 

 

O
0 0
- o
o
o
a o
a o
o
I 0
0° 0
.4 o 0 0
1 %,d29§; oo’ o
jL4ih‘hR4F!>:Lfl£%r‘LT-T—‘H—°1QJH

O 50

100

150 200 250
MILES OFFSHORE

 

 

IRICOLPITES CF. I. HICRDHUNUS
o
o
0
° 0
. o
o
4 o
o o “I 0 ‘29
I33 «90
43 3| ° on
0 50 100 150 200 250

MILES OFFSHORE

 

 

103

grains to larger diameter grains should increase with distance offshore.
This does not appear to be the case when this grain's distribution is
compared with that of the larger Classopollis and the smaller‘z. sp. 7.

Tricolpopollenites sp. 7 -- This grain has a mean diameter of

 

about 8 H. It occurs in greatest numbers nearer shore than the larger
common pollen grains (fig. 16). One might reason that its small size
and form indicate that it comes from a wind pollinated plant. Wind pol-
linated plants commonly produce large amounts of pollen., Because this
taxon occurs in low frequencies one might then assume that it grew some

distance inland.

Micr0plankton

Micr0plankton with processes -- Most of the hystichosphere
(microplankton with processes) taxa tend to increase offshore. The
relative frequency and number per gram of rock of the following hystrich
categories were plotted. Michrystridium spp. (fig. 16), acritarchs
with processes (fig. 21), Hystrichosphaera spp. (fig. 18), Palaeohystri-
chophora infusoroides (fig. 18), chorate cysts (fig. 21), and micr0plank-
ton with processes (fig. 22).

All of the above taxa tend to increase in relative frequency with
increase in distance of sample offshore except PaleohystichOphora infus-
oroides. ‘2. infusoroides tends to have higher relative frequencies in
samples from intermediate distances offshore. This dinoflagellate might
be considered a proximate cyst because its processes consist only of hairs
and it exhibits a definite peridinoid shape. All of these taxa except 2.
infusoroides tend to have highest numbers per gram in samples from about
125 to 175 miles offshore. .2. infusoroides has its high numbers per gram

in samples from nearer shore.

PERCENT

PERCENT

sp. 7 and of Michrystridium spp. plotted against distance offshore.
centage of T. Sp. 7 is based on the sum of pollen and spores.
of Michrystridium is based on the sum of microplankton.

TRICOLFOPOLLENITES 3P. 7

 

104

 

 

 

 

 

 

25
o
20 -
15 -
o
10 ‘
0"0
8 8 '00
5 J . o
0 ‘W’ 0 o
0 . 9%,
0 4%
0 50 100 150 200 250
MILES OFFSHORE
HICHRYRSTRIDIUM SPF.
80
. o o o
. o
o
. o 0
40 4 0° 0 o o
-I o w
.J o 0 °° °
0
':°.- =
"' ....“ 0.0 0.0
o I SI!:&:V r r I r r

 

 

0 50 100

MILES OFFSHORE

150 200 250

TRICOLPOPOLLENITES SP. 7

 

 

..-
O

 

 

 

 

 

 

T o
, I ....
O
H8 _' o
x -I
z . o
0:6 °
g - .
\x4 .
U) o "oo
.2. ~ . ,
CE 90
0:2 4 .....o o
C) . no
i I o a I
0
0 50 100 150 200 250
MILES OFFSHORE
MICHRYRSTRIDIUH SPF.
300 T
0 732.2
2250- o
x
200‘
Z
85
0150- o,
\
$1004 °
00
I:
2350 d .
Z O
o 4 . o . ° ° °
0 50 100 150 200 250

MILES OFFSHORE

FIGURE l6.--Relative frequency and number per gram of Tricolpopollenites

 

value off the graph.

Per-

Percentage
Arrow denotes

PERCENT

PERCENT

30

...-
01

30

u.-
0"

105

CYMRTIOSPHHERR SPF.

 

 

-I o o
0 o
o
4. o
0
° 0
a U; ‘9
0 0°
° .9
.4, o O 0 0° '0

 

 

" .I|°@:03cl 33 R 0‘

150 200 250

O 50 100
MILES OFFSHORE

 

 

 

 

FORM C SP. 1
RI
4
I 0 °
0
fl
00°
I o o o
o :’ o o o
-I 0 0
o 00
“god‘flfik’” . 0
° 0 cfi’e " ‘b o
4 I’AfiY—or
O 50 100 150 200 250

MILES OFFSHORE

*‘ N 0) #
O O D O

NUMBER/GRRM X 10’

O

H H N
0 tn 0

NUMEER/GRRM X 103

0 $9 il‘l ,. c’ox o o

CYMHTIOSPHRERR SPP.

 

 

 

a131, .eIOIyo 0°

39%

 

 

O 50 100 150 200 250
MILES OFFSHORE

FORM C 5?. l

j o

I 0 0

d

d

 

50

100

“’30,
s

 

150 200 250

MILES OFFSHORE

FIGURE l7.--Re1ative frequency and number per gram of Cymatiosphaera Spp.
Percentages are

and of Form C Sp.

1 plotted against distance offshore.

based on the sum of microplankton.

106

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

HYSTRICHOSPHRERR SPP. HYSTRICHOSPHRERR SPF.
16 10
0 0
4 ED ‘
Ha -I
. >< .
-I 0
*2 Es .
“J 0:
Us -I o o -I
0: .\ ‘
LLJ a 0: ‘ o
0- .J 0 ° % 4 °
.1! o 2: . O o
-I :0 o. o 0 :32 .8 0
° ;;’49 " G).°‘%’ o d 0
0 Irlhulln¢I~r4imiiHjiLP‘ Tease r 0 <5aIIIIJ|HIFlil:‘:4:° OHaJFTo .
O 50 100 150 200 250 50 100 150 200 250
MILES OFFSHORE MILES OFFSHORE
PRLREOHYSTRICHOPHORR INFUSOROIDES PnLnEOHYSTRICHOPHORH INFUSOROIOES
40 30
0
‘ ° ° ézs . o
J R: ><
O
,_ A 2204 o o
a: 0 CE 0 .
020 4 ° gIS-I o
0: o .\ °
OJ 4 o oo o a:
0. o o o o 0,, lLJIO 4 . o
J .0 o o g? o ‘9 IESNI
J o o 2“: o :35 d . o o 0
0 Q“ ’85 Z O. ' O ‘0 O
0W.°,°.T. oWTf.‘s°.°
0 50 100 150 200 250 0 50 100 150 200 250
MILES OFFSHORE MILES OFFSHORE

FIGURE 18.--Relative frequency and number per gram of Hystrichosphaera spp.
and of Palaeohystrichophora infusoroides plotted against distance offshore.
Percentages are based on the sum of microplankton.

 

DINOGYMNIUM SP- 1

 

 

 

 

107

N
O

DINOGYMNIUM SP. 1

 

 

 

 

 

 

 

 

 

 

25 ‘u
o o
C) a
m - “‘
o ><15
'— 0 Z 4
215 '4
“J o o 821“] H o
L.) o o O
3310 4 °° \ .
0- ° 0 0 a: 0 0
GD 8'8 o “J
00 0 m5 . '
5 4 00° Z 0 °
15 o :3 - o o 0
9° 0 2: e'oo
', O " 0 0 do 0
o $4&“¥r++iflwfiwfir5+*31- 0 +u-AN¥3#-«fi%»r¢+++~
0 50 100 150 200 250 0 50 100 150 200 250
MILES OFFSHORE MILES OFFSHORE
PROXIHRTE + CQVRTE CYSTS FROXIHRTE + CHVRTE CYSTS
100 75
d o
u 6 .1
+ ° Hso~ o
J >< ‘
n o
E_ 4 E: -
UZJ 0 0 G45 -1 0
USO 0 0 0 El: 0
a: 0 0° 0 O 0 as d 8
“J ‘J 06’ g? d! \‘30 4 o
O. 0 O m -1 0
q 000% 0 LIJ o o
o 0 age; 0 ° a3 ‘ ° 0 o
'4‘ o °eo :15 — 08 we
0190 o o .3 o :3 . o oo o
‘ o o cfgo 2: at 0 o 0
° 49 0 ° ‘ a' 03%} 9 o
0 F r f r # F 1* fat 0 I f l M
0 50 100 150 200 250 O 50 100 150 200 250

MILES OFFSHORE MILES OFFSHORE

FIGURE 19.--Re1ative frequency and number per gram of Dinogymnium sp.1
and of proximate plus cavate cysts plotted against distance offshore.
Percentages are based on the sum of microplankton.

 

PERCENT

PERCENT

108

RCRITHRCHS HITHOUT PROCESSES RCRITQRCHS HITHOUT PROCESSES

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

60 200
. ° 33 ‘
o “q d o
0 0 x -1
< o
o 0 2: _
. o a. . g
30 0 800° 0 90 01001
\ _
0009'?% 0% o 83 80
.00 0 0° ao0 CD - 0
a 0:00 0 0° 0 fig 0 ° E; q 0
° ° 2 - ° . o o a
O
0 T T—.F r I % r r f I 0 8 Go 0
0 50 100 150 200 250 0 so 100 150 200 250
MILES OFFSHORE MILES OFFSHORE
MICROPLRNKTON HITHOUT PROCESSES MICROPLHNKTON HITHOUT PROCESSES
100 200 f
A 0 200.9
0 C3
'1 o o H
o o 150‘
. ><
I °°: 0" o
- N.," 3 z
00 0° 0 CE 0
o
50 4 09ml; 0 o E55100: 0
JP °° '° 0 \\ g:
0 0° 0 m
° 0
I ° . ° 5 . °
_ 3 ° 0 :50 d . .8
o 0 0 3 0
o o 0 0 o o o
A 0 Z O o 3 ’.o. o
a f 1— r I I I r r r 0 W? T I I L'f'_n‘l°_'."l'
O 50 100 150 200 250 0 50 100 150 200 25

MILES OFFSHORE MILES OFFSHORE

FIGURE 20.--Re1ative frequency and number per gram of acritarchs without
processes and of microplankton without processes. Percentages are based
on the sum of microplankton. Arrow denotes value off the graph.

_ Z

1— a“.

I

.

PERCENT

PERCENT

0)

N

80

p
D

CHORRTE CYSTS

 

CHORQTE CYSTS

 

 

 

 

 

 

 

 

 

 

 

 

 

 

e 25
'6:
. H20~ °
><
4 E15 -4 0
0:
0 CD
- aw .
o “J 0
00 o
-1 o o 0 0 g5 " o g 0
Z 0 .0 Q o
’ o ocnad° .g
4 a $0 0009 I 0I I 0 {WI IOTOFo
0 50 100 150 200 250 0 50 100 150 200 .250
MILES OFFSHORE MILES OFFSHORE
HCRITHRCHS HITH PROCESSES HCRITRRCHS HITH PROCESSES
180
o
4 0 o B " 0
a 0 *4 ‘
><
4 ° 1200
o on I:
0 CE .
4 ° 0 ° 3.. ° 05 q
o \
- o O:
o 00%0000 g o 0 meow o
it 00 0'0 0 o :2 ‘
062flg'1f o 0 0 :3 ‘0
f. "o‘. ° 0 2: d o o
‘F fig roI I I r I I 0 WW
0 50 100 150 200 250 0 50 100 150 200 250

MILES OFFSHORE

MILES OFFSHORE

FIGURE 21.--Re1ative frequency and number per gram of chorate cysts and

of acritarchs with processes plotted against distance offshore.

Percent-

ages are based on the sum of microplankton.

110

MICROPLRNKTON HITH PROCESSES

 

 

 

 

 

 

80
o
0 o
q
q 9
o
o
E; 4 o oo
UJ ° gm. 0 o
040‘ 0 0
0
E5 0
a. ‘ 10° 0 o
o ¢> 01,0 0"0 0 °
1» Go 8’0 0
CD 0
-R::3° 0° °
0 o
0 :0 <9 0 °
0 I e! T I T I I I f
0 50 100 150 200 250
MILES OFFSHORE
MICROPLRNKTON HITH PROCESSES
180n
0 o
C) -J
H
X
1200
2'.
CE -
O:
3' 1
O:
LLJSOOT 0
03
Z -1
:3 o as
2: 4
o o
[I 4LaIIIIlli‘ullitTll4fLT—d;_nql.4

 

0 50 100 150 200 250
MILES OFFSHORE

FIGURE 22.--Relative frequency and number per gram of microplankton with
processes. Percentages are based on the sum of microplankton.

111

Michrystridium is the most abundant hystrich in most of the

 

samples and dominates any more inclusive group into which it is placed.
The distribution of total microplankton with processes reflects the dis-
tribution of Michrystridium.

MickroPlankton without Processes -- In this group the distri-
butions of the following catagories are illustrated. .Qymatiosphaera spp.
(fig. 17), Form C sp. 1 (fig. 17), Acritarchs without processes (fig. 20),
Dinogymnium sp. 1 (fig. 19), proximate and cavate cysts (fig. 21), and
microplankton without processes (fig. 20).

These distributions show high relative frequencies nearer shore

than do the hystrichs. Qymatiosphaera (the most abundant) has high re-

 

lative frequencies in samples from between 50 and 150 miles offshore
while Form C sp. 1 and Dinogymnium sp. 1 have high relative frequencies
in samples that are less than 75 miles offshore. All have highestrnmv-»
bers per gram in samples that are nearer shore than those containing
large numbers of hystrichs.

The relative frequency of the category "micr0plankton without
processes" is the complement of "microplankton with processes" because
in all cases the sum of the two is 100 percent. Either graph could be
interpreted as the ratio of one to the other.

The distributions of the various fossil micr0plankton taxa dis-
cussed above probably reflect the position of the living plankton pOpula-
tions in relatiOn to the shoreline. Although the exact position of the
living population may not be indicated, the original position of the liv-
ing p0pu1ation probably influenced the present distribution of the cysts.
The source for a given cyst was a living population and its position

relative to the other living p0pu1ations should produce distinct cyst

81‘

a c
P‘U

112

distribution in the bottom sediments even though the cysts may have been
moved about by currents. Complete mixing does not seem likely in light
of studies of palynomorphs in modern sediments.

The inverse relationship between the relative frequency of hy-
strichs (micr0plankton with processes) and that of microplankton without
processes as distance offshore increases contradicts somewhat the sugges-
tions made by Wall (1965) concerning acritarchs in the Jurassic of the
British Isles. However, Wall's offshore samples may represent open deep-
sea conditions rather than great distances offshore in an epicontinental
sea. However, the above relationship is similar to that found by Staplin
(1961) off Devonian reefs. It has been suggested that the processes
serve to present more surface area to the water and thus make the cysts
more resistant to sinking in the deeper, less turbulent water offshore

(see brief discussion in Davey and Williams, 1967, p. 393-394).

Total Palynomorphs per Gram of Rock

The number of total palynomorphs (all pollen, spores and micro-
plankton) per gram of rock (e.g., Classopollis spp.) tend to be highest
in samples from intermediate distances offshore (fig. 23). .this re-
flects the distribution of rates of sedimentation of the organic parti-
cles superimposed on that of the inorganic particles. Near shore the rate
of inorganic sedimentation is high because of streams dumping their loads.
This rate of sedimentation decreases at intermediate distances offshore
and the rate of sedimentation of land-derived palynomorphs probably in-
creases. This increase may be due to the fact that the less dense or-
ganic particles are carried farther along in the direction of transport.

Also, the micr0plankton apparently produce more cysts at intermediate

anu\.hwz u .LIAJ

O~03,a

Emo\~LU4mLZDZ

O- m. he 3

:~

113

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

TOTRL POLYNOHORPHS 0 RHTIO HICROPLRNKTON! POLLEN + SPORES
5 F I 30 1
o octa d%fl’ egg 0
Z
c: 1. :‘%0°:°,o,° o 4
\ o o '3 ° oo
00 o ‘°¢: o o J
E4 d 093 (/ ° 35.
a: 0 L55. o
‘5 - 215 «
E
82 J CK " o 0
(D o o
O
_J .4 H o
O o 0
0 T T T r T T r r r o o o o v or or 0'00
O 50 100 150 200 250 0 50 100 150‘ 200 250
MILES OFFSHORE MILES OFFSHORE
CORL PRRTICLES CUTICLE FRRGHENTS
6 5
o
g o 0 0° (2.5) o
\ ‘ .00 ‘&v.§°€°° ° ° \4 1’ o:.§%o° °
{:34 30 0:5? ° {0 :1. ° 0 Si ogr:f%l cc: 0?
(D o 0 CD3 4 0 00¢? 08
2 ° {as L5. 2 0 0 a
I) 4 :3 o 8 0 °
2: z: o ooléno
2 ‘ o o o
532 J 53 ° 0 0
CD CD 0
0 D1 .
_J -: _l
o r ‘T T r 1T I 1T r 1' 0 I T T I T ‘7 r T T
0 50 100 150 200 250 O 50 100 150 200 250
MILES OFFSHORE MILES OFFSHORE

FIGURE 23.--Log of palynomorphs per gram, log coal particles per gram

and ratio of the number of microplankton cysts Io the number of pollen

and spores all plotted against distance offshore. Arrow indicates value
off the graph. Limestones are indicated by "Ls".

113

TOTRL POLYNOMORPHS 0 RRTIO MICROPLQNKTON: POLLEN + SPORES

 

 

LOG10 GRHINS/GM

 

 

 

 

 

 

5 F F 30 1
o 8 .3 o o
°ofia§bupd§bWb 9b
H 0 65 o ‘
0 it 0 °
03 o o o 010
9b
4 J 09000 0 0 L05 J
at (as o
- E35 .
F—
CE
2 4 Cr 4 o o
o o
a - o
o: o
0 r T f r T r f r r 0 Mororofo
O 50 100 150 200 250 O 50 100 150 200 250

MILES OFFSHORE MILES OFFSHORE

CORL PRRTICLES CUTICLE FRRGMENTS

 

 

 

 

 

 

 

 

6 5
o

I: I:
o 0 00 O q 00
a: I 3%??{2 .° ° ;‘ 0 saw °
$4 3” ° 0:" ° 5 36:: .1 0°
5: o 1055 L: ‘233 J oo‘fia 8 g
:3 q :3 o 8 0 °
2: 2: o 00 6mo
c3 c32 4 o o o
..2 J —~ ° 0 o
CD CD 0
C3 C3 1 a
_J - _J

O r r T IT r I fr r 0 I I I I Ief I T

0 50 100 150 200 250 O 50 100 150 200 250

FIGURE 23.--Log

MILES OFFSHORE

of palynomorphs per gram, log
and ratio of the number of microplankton cysts

and spores all plotted against distance offshore.
off the graph.

I8

MILES OFFSHORE

coal particles per gram
the number of pollen
Arrow indicates value
Limestones are indicated by "Ls".

114

distances offshore. Still farther offshore the land-derived palynomorphs
and the micr0plankton sedimentation rates drop off.

The limestones that were examined consistently contain low
numbers of palynomorphs per gram of rock. This would indicate that there
were either (1) short spurts of high rates of calcium carbonate sedimenta-
tion, or (2) early lithification and subsequently less compaction of the
limestones compared with the shales, (3) some palynomorphs that are not
destroyed in the shales are destroyed during the formation of the lime-
stones. Because the somewhat more resistant land-derived coal particles
show a similar low density (fig. 23) in the limestones, the second hyp-
othesis seems to be the more tenable. The sedimentation rate of coal
particles would probably be independent of the special conditions re-

sponsible for the limestone deposition.

Ratio of MicrOplankton to Pollen and Spores

The distribution of this ratio is shown (fig. 23) because it
is frequently used in the literature as a measure of distance offshore.
Here it shows essentially no such relationship to distance offshore. In

fact, the largest value is quite nearshore.

Coal Particles (2 50 u) per Gram of Rock

The distribution of coal particles (vitinite and fusainite,
2 50 u in largest dimension, per gram of rock) is similar to that of
the total palynomorphs per gram. As mentioned above, the limestones

contain small numbers of coal particles per gram (fig. 23).

Cuticle Fragments per Gram of Rock
The distribution of cuticle fragments (all recognizable sizes)

shows a definite decrease with distance offshore. This is similar to the

115

d istribution of these particles that was shown by Muller (1959) in sedi-

ments off the Orinoco Delta. This distribution may reflect the disinte-

gration of the cuticle as it is transported. If fragments became so

small that they showed no cuticular suture pattern they would not be

counted.

Interpretation Assuming Only Time-Related Effects

Another interpretation of the diversity indices, relative fre-

quencies, and numbers per gram of rock is possible. This interpretation

is the kind that is made when abundance peaks are used for time correla-

tion and eliminates the role of the local environment in determining the

a bove d istribut ions .

The correlation between distance offshore and distance above

the base of the Mancos is better than between any of the other variables

in this study. Also, the correlation between the diversity index, rela-

t ive frequency or number per gram and distance offshore is rough. The

d iversity indices, relative frequencies, and numbers per gram also corre-

late roughly with distance above the base of the Mancos and thus may be

related to time. This would reflect evolutionary or phytogeographical

Changes in the flora. As it is, a taxon that is abundant in the upper

Parts of the sections would tend to appear more abundant near shore and
one abundant in the lower parts would appear more abundant far offshore.
This relationship between the position of the strandline and the distance

above the base of the Mancos was not realized until the study was well

underway. Further study must be carried out in area where such a re-

lationship can be avoided. Only then can any effect of the environment

be unequivocally demonstrated.

116

Environmental Casual Factors

The only so-called "environmental parameter" that is control-
leacl in this study is distance offshore. In the modern oceans, factors
snaxih as water depth, salinity and turbidity are commonly correlated with
cliestance offshore. Because distance offshore correlates with these other
et1xrironmental factors it would be impossible to determine that a single
faacztor strongly influences the abundance of a fossil palynmorph if that
faac:tor also correlates with distance offshore.

In the modern ocean the distribution of plankton can be expect-
eci to be affected by water depth, salinity, and turbidity as well as tem-
1>errature, substrate microenvironments, nutrient concentration, turbulence,
<:errent direction and duration, proximity to river mouths, wind direc-
tzixan, wind velocity and wind duration. Some of these factors also af-
:E<3c¢.the distribution of purely sedimentary particles such as pollen and
Spores. Climatic influences on both land and sea such as rainfall and
Illusolation are also involved.

A few examples of apparent control of palynomorph distribution
‘3)? an environmental factor or group of factors have been found in the
Duodern environment. Plankton blooms are known to occur in water masses
‘Ihat are rich in nutrients such as occur in upwellings and off some river
tnouths (Raymont, 1963; van Andel, 1964). In the Gulf of California, cysts

<3f dinoflagelletes occur in bottom sediments below some of these areas of
plankton blooms although not below others (Cross, et a1, 1967). Also,
pollen and spores are known to be concentrated off river mouths (Cross,
at al, 1967).

It follows that within the limits of this study it would be

very difficult to determine what environmental factor actually might

(f)

117

predominate in the control of the distribution of the various palynomorphs.
Nevertheless, it is felt that simply a determination of the distance off-
shore at which a rock sample was probably laid down is extremely valuable
in itself.

The most widely recognized value of being able to estimate the
d istance offshore at which a rock was deposited lies in the determination

of paleogeography. What is sought is the position of the strandline in

relation to various other facies.

V. CONCLUSIONS

It may be concluded that, coupled with good time correlation,
faactor analysis appears to be useful in detecting the influence of en-
vironment on (the composition of palynomorph assemblages. However, more
vacrrk must be done in situations where more real environmental parameters
can be measured and related to palynomorph assemblages. Perhaps then

C(305 a more complete interpretation of a more rigorous factor analysis

(rnore end menbers, greater communality) could be made.

A better understanding of environmental parameters might also
£11.1ow one to determine the factors controlling the relative frequencies
and numbers per gram of individual taxa.

The empirical use of diversity indices, factor analysis and, to
in limited extent, relative frequencies and numbers per gram of rock, as
‘tuools for determining distance offshore is suggested as the result of
tztiis study. Although, the use of these methods has not been adequately
tzested in this work or in previous work, it is felt that the application
<>f the relative frequency and number per gram of rock would be limited
tn) the region surrounding the site of this investigation (where there is
£3 similar assemblage of microfossils and a similar sediment regime).
Factor analysis and the diversity indices could probably be applied in
any area and to any group of fossils (especially microfossils because
of their abundance; see Streeter, 1963).

The logical extension of the results of this study would be in
determining distance offshore in the rocks of the Upper Cretaceous of
the Western Interior purely on the basis of palynomorphs. However,

coupled with all other lithologic and paleontologic data available, a

much better reconstruction of ocean-bottom environments could result.

118

119
The use of relative abundance peaks of palynomorphs in correla-
tion must be used cautiously and only after one understands the role of
the local environment in affecting palynomorph abundances.
In general, the information contained in fossil assemblages
that reflects environment 32 retrievable. Multivariate analysis tech-
nigues should be tested with reliable paleontologic data, measurements

of environmental parameters, and adequate mathematical direction.

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Von Quendlinburg: Palaeontographica, Abt. B., v. 95, pp. 30-52.

Williams, D. B., and Sarjeant, W.A.S., 1967, Organic-walled microfossils
as depth and shoreline indicators: Marine Geol., v. 5, pp. 389-412.

Wilson, L. R., and Webster, R., 1946, Plant microfossils from a Fort
Union coal of Montana: Am. J. Bot., v. 33, pp. 271-278.

Woods, R. D. 1955, Spores and pollen - a new stratigraphic tool for the
oil industry: Micropaleontology, v. 1, pp. 368-375.

Young, R. G., 1955, Sedimentary facies and intertonguing in the Upper
Cretaceous of the Book Cliffs, Utah-Colorado: Bull. Geol. Soc.
Am., v. 66, pp. 177-201.

128

Young, R. G., 1957, Late Cretaceous cyclic deposits, Book Cliffs,
eastern Utah: Bull. Am. Assoc. Petr. Geol., v. 41, pp. 1760-1774.

, 1960, Dakota Group of the Colorado Plateau: Bull. Am. Assoc.
Petr. Geol., v. 44, no. 2, pp. 156-194.

Zaitzeff, J. B., 1967, Taxonomic and stratigraphic significance of
dinoflagellates and acritachs of the Navarro Group (Maestrichtian)
from east-central and southwest Texas: Ph.D. Thesis, Michigan
State Univ., East Lansing.

APPENDICE S

APPENDIX A

Measured Stratigraphic Sections

 

POINT LOCKOUT SECTION

Section measured in sections 26, 29 and 31, T. 36 N., Sections 5 and 6,
T. 35 N., R. 14 W., Montezuma County, Colorado

Distance
Thickness above base of
formation

Point Lookout Sandstone
Ft in Ft in
Sandstone, buff-yellow, fine to medium- 72 0
grained, massive to platy, calcareous,
one half inch to six feet thick; inter-
bedded with shale..................... 72 0

72 0
Mancos Shale

Upper Shale Member

Ft in
Shale, sandy; interbedded with tan-' 2056 10
yellow, calcareous, flaggy sand-
stone about five inches thick
and from six inches to one foot
apart ............. . ........... 96 6

Concretion layer; light-gray, weathers 1960 4
buff, fine-grained, sandy limestone;
septarian (?) core and calcite
crystals lining fractures and in
center of spherical concretions
about two feet six inches in
diameter....................... 2 6

Shale, sandy; interbedded with tan- 1957 10
yellow, calcareous, flaggy sand-
stone beds about five inches thick
and from six inches to one foot
apart ...... . ....... ............ 53 l

Shale, silty to sandy; interbedded with 1904 9
a few widely-spaced very-thin sand-
stone beds..................... 12 4

130

131

Mancos Shale--Continued

Concretion layer; light to medium-gray,
weathers buff to orange or reddish

brown, silty to fine-grained, massive
to platy, limestone concretions about

two feet six inches in diameter; no
fossils ........ .. ...... ..........

Shale. silty to sandy; interbedded with

a few widely-spaced sandstone beds one

half to two inches thick... ......

Sandstone, light-gray to tan, flaggy to
platy, calcareous; plant fragments,
animal trails. .............. .....

Shale, silty to sandy; interbedded with
a few widely-spaced very-thin sand-
stone beds ...... . ...... .... ......

Shale, silty to sandy ....... . .......

Concretion, light to medium-gray
weathers buff to orange or
reddish-brown, silty to fine-
grained, massive to platy lime-
stone; no fossils..... ..... ......

Shale, medium to dark olive-gray to
medium to dark gray-olive, silty,
fissile to starchy (tending to
"massive" mudstone in some layers),

Ft

33

17

slightly calcareous to non-calcareous;
small plant fragments; interbedded

with light-gray to whitish limestones;

one inch thick increasing to two inches
towards the top; some lenticular; fine-
sand-sized grains (calcarenite).... 24

Mudstone, friable, massive, non-calcareous;

no fossils......................... 25

in

Ft

1892

1889

1856

1856

1839

1835

1834

1809

in

11

11

132

Mancos Shale--Continued

Ft in Ft in
Shale, dark gray-olive,fissile, non-calcareous, 1783 10
silty, with sandy laminae; iron oxide (?)
concretions throughout, two inches in
diameter in zones about five feet
wide ......................... . ...... S 7

Shale. dark gray-olive, silty, sandy, 1778 3
starchy, non-calcareous...... ....... 5 7

Shale, dark-gray, fissile to starchy, 1772 8
slightly calcareous; with some silt
laminae, no sand; no fossils ........ 4 3

Bentonite. tan to pink, fissile, non- 1768 5
calcareous, gypsiferous (marked by
conspicuous spring on slope)........ 6

Shale, dark-gray, some silt laminae, - 1767 ll
fissile to starchy, slightly cal-
careous; no fossils ................. 21 4

Shale, as above; with white to light- 1746 7
gray (at cores) limestone concretions
about one foot in diameter, scattered
throughout ........... ............... 5 7

Shale, dark-gray to medium to dark olive- 1741 0
gray, fissile, sandy silt laminae; a
few iron oxide-stained and cemented
layers with concretions about one half
inch thick .......................... 22 4

Concretion layer; light to medium-gray, 1718 8

weathers buff to orange-yellow,

massive to platy, limestone con-

cretions to one foot 10 inches in

diameter; baculites; compressed

water-worn coalified wood frag-

ments... ..... ....................... 1 10

Shale, dark gray to dark to medium-gray, 1716 10
fissile, sandy silt laminae; a few
iron oxide-stained and cemented layers
with small concretions about one half
inch thick ............. ............. 8 10

133

Mancos Shale--Continued

Ft
Concretion layer; orange-brown to light to
medium-gray at cores, platy to massive,
discoid limestone concretions about
four inches thick and two feet wide;
baculites, wood and other plant
debris...............................

Shale, medium to dark olive-gray to
medium to dark-gray, fissile to
starchy, slightly calcareous to cal-
careous, gypsiferous; with silty
laminae; no fossils.................. 15

Mudstone, lenticular, medium-gray, weathers
buff to orange-yellow, massive to platy,
laminated; animal trails on top; no
fossils..............................

Shale, medium to dark olive-gray, silty,
starchy, slightly calcareous; no laminae;
a very few calcarenite layers about
three-fourths inch thick; no fossils. 33

Shale, medium to dark olive-gray, fissile,
slightly calcareous; with sandy laminae;
no fOSSils.O.......OOOIOOOOOOOOOOIOOO 16

Concretion layer; medium-gray, weathers buff
to orange-yellow, massive to platy,
slightly calcareous, laminated mudstone
concretions about three feet in diameter;
baculites............................. 3

Shale, medium to dark olive-gray, fissile,
slightly calcareous; with sandy laminae;
no fOSSiIBOOOOOOOOOOOC......OIOOOOOOOO 48

Concretion layer; large, medium-gray,
weathers buff to orange-brown, slightly
calcareous mudstone concretions; a
few baculites.........................

in

11

Ft
1708

1707

1691

1691

1658

1641

1638

1590

in

134

Mancos Shale--Continued

Ft in Ft
Shale, medium to dark olive-gray, fissile 1589
non-calcareous to slightly calcareous;
with sandy laminae; with some inter-
bedded sandstones about one-fourth
inch thick. ........... ...... ......... . 58 4
Concretion layer; yellow-orange to light- 1531

gray at center, weathers platy at edges,
calcareous, discoid mudstone concretions
about seven inches thick and three feet
wide; gypsum in fractures; baculites,

fish scales, coalified wood fragments. 7
Shale, as above. ........... .............. l 0 1523
Sandstone, light-gray to yellow, slightly 1522
calcareous, laminated; plant fragments 4
Shale, as above, sandstones about three- 1522
fourths inch thick.......... .......... 8 5
Sandstone, platy, conspicuous............ 1 1513
Shale, medium to dark olive-gray, 1513

fissile, non-calcareous to slightly

calcareous; with sandy laminae; inter-

bedded with some thin sandstone layers
one-fourth inch thick increasing to

about three-fourths inch thick up-
wards................................. 32 6

Mudstone, lenticular, light to medium-gray, 1481
weathers buff, massive to flaggy
laminated, slightly calcareous;
fractures into prismoidal pieces;
inoceramus, plant fragments........... 9

Shale, dark olive-gray, platy to blocky, 1480
slightly calcareous, gypsiferous;
iron oxide stain on fractures; inter-
bedded with white to yellow, cal-
careous, cross-laminated, very thin
sandstones about one-fourth inch
thick and about one foot apart; fish
scales................................l32 3

135

Mancos Shale--Continued

Ft in Ft in
Mudstone, lenticular, light to medium- 1348
gray, weathers buff, massive to platy,
slightly calcareous, laminated;
plant fragments..... ..... .... ..... l 10

£\

Shale, sandy, medium to dark olive-gray, 1346 6
fissile, slightly calcareous; inter-
bedded with a few very thin sand-
stone layers about one-fourth inch
thick; fish scales................ 35 3

Shale, medium to dark olive—gray, fissile, 1311 3
slightly calcareous; with silty
laminae.............0.... ......... 16 9

Shale, sandy, medium to dark olive-gray, 1294 6
fissile, slightly calcareous; inter-
bedded with very thin sandstones
about one-fourth inch thick and con-
taining animal trails and plant
fragments. (The steepness of the
310pe varies with the concentration
of the thin sandstones in the shale). 46 5

Mudstone, light-gray, weathers buff to 1248 l
orange-yellow, flaggy to platy,
laminated; abundant plant debris--
conifer needles, stem compressions,
amber. ...... ..... ................. 1 0

Shale, medium to dark olive-gray, 1247 l
fissile, slightly calcareous; with
sandy silt laminae; interbedded with
cross-laminated, calcareous to
slightly calcareous thin sand-
stones about one inch thick contain-
ing animal trails, fine to coarse
plant debris (including large leaf
fragments), fine sand-sized grains... 16 ll

Shale, medium to dark olive-gray, 1230 2
fissile, slightly calcareous; with
sandy silt laminae becoming more
concentrated upward.. ..... .. ...... 41 l

136

Mancos Shale--Continued

Ft
Mudstone, lenticular, light-gray, weathers
buff, massive to platy, non-calcareous,
calcite in some fractures, laminated;
Inoceramus, baculites, fish scales,
plant fragments............ ........... 1

Shale, light to medium to dark olive-
gray, fissile, non—calcareous except
along some bedding planes; thick-
shelled Inoceramus; with sandy
laminae thickening to one half inch
cross-laminated sandstones every
five to ten feet; quartz sand;
animal trails, plant fragments.. ...... 58

Mudstone, medium to light-gray,
weathers buff, massive to platy,
laminated; tiny plant fragments (?)... 1

Shale, medium olive-gray to medium
gray-olive; light sandy laminae becoming
more concentrated upwards; inter-
bedded with few one half inch thick
(two beds about four inches thick)
calcarenite (?); no fossils........... 49

Mudstone, light-gray, weathers buff,
flaggy to thin-bedded,calcareous;
no EOSSi-ISOCOOOOOCO0.0000000000000000.

Shale, medium olive-gray to medium-
olive, fissile to platy, calcar-
eous to slightly calcareous (appears
due only to fine-sand laminae); with
fine-sand laminae; hard sandy layers
about one-fourth inch thick, inter-
bedded in upper twenty to thirty feet;
few fish scales; white specks on
bedding p1anes........................ 88

Mudstone, light-gray, weathers buff to
orange-yellow, flaggy to platy;
InoceramUSoooocesses-00000000.. .......

Shale, medium-gray to medium gray-olive,
fissile, calcareous, gypsiferous;
fiSh scaleSOOCOOOO......OOOOOOOOOOOQOO 37

in

Ft
1189

1188

1129

1128

1079

1078

990

990

in

11

137

biancos Sha le- -Continued

Ft
Mudstone, light-gray, weathers buff,
flaggy to thin-bedded, calcareous;
fish scales, Inoceramus............

Shale, medium-olive gray, fissile,
calcareous, gypsiferous; with light
silt laminae; Inoceramus, fish scales. l4

Mudstone, light to medium-gray, weathers
buff to orange-yellow, massive to thin-
bedded; fish scales, Inoceramus, plant
fragments (a leaf!)................

Shale, light to medium olive-gray,
fissile to platy, calcareous, gypsiferous;
fish scales common................. 22

Mudstone, lenticular, light to medium—
gray, weathers buff to orange-yellow,
thin-bedded to platy; large Inoceramus,
fish scales, baculites (?).........

Shale, medium olive-gray to medium-
gray, platy to fissile, calcareous,
gypsiferous; fish scales, shell frag-
ments.............................. 12

Bentonite, yellow, gypsiferous... .....

Shale, medium olive-gray to medium-gray,
fissile to platy, hard, brittle,
calcareous, gypsiferous; fish scales,
shell fragments.................... 11

Bentonite, yellow-orange, gypsiferous.

Shale, medium olive-gray to medium-gray,
fissile to platy, calcareous, gyp-
siferous; fish scales, shell frag-
ments.............................. 11

in

10

Ft
952

951

936

936

914

913

901

901

890

890

11

10

138

‘2-Iancos Shale--Continued

Ft in Ft in
Mudstone, lenticular, light to medium- 878 11
gray, weathers tan to orange yellow,
massive to platy; fish scales,
large Inoceramus, oysters,
baculites (?), ammonites, fish scales. 6

Shale, medium gray, fissile to platy, 878 5
calcareous, gypsiferous............... 4 6

Bentonite, yellow-orange, slightly 873 11
calcareous...O.......OOOOOCCCIOOOOOOOO 1

Shale, medium gray, fissile to platy, 873 10
calcareous, gypsiferous ...... ......... 10 8

Shale, medium olive-gray, fissile, 863 2
calcareous, gypsiferous..... ....... .. l9 4

Shale, medium-gray, hard fissile to
platy (upper part more fissile),
Calcareous, gypsiferous; large,
thick-shelled Inoceramus, fish
scales; white specks on bedding
planes................................ l4 0 843 10

Bentonite, yellow-orange to white ........ 2 829 10

Shale, medium-gray, hard, fissile to
platy, calcareous, gypsiferous;
large thick-shelled Inoceramus;
white specks on bedding planes ........ 5 7

Limestone, medium to dark-gray, 824 l
fissile to crumbly, hard, thin-
bedded on weathered ridges; large
Inoceramus shells, encrusted with ,
oysters, together with other oysters. 1 5

Shale, sandy, gray-brown; weathers into 822 8
tan plates one half inch thick (t0p
of ridge).. ...... ..................... 22 5

139

Mancos Shale--Continued

Ft
Shale, sandy, medium olive-gray to medium

to dark-gray, fissile to platy, calcareous;
interbedded with sandstone (calcarenite)
layers a few millimeters thick; steepness
of sIOpe varies with concentration of sand-
stone layers; lower 33 feet six inches forms
a steep 810pe, the next 16 feet nine
inches forms a cliff................. 61

Calcarenite, light to medium-gray; beds from
a few millimeters to two centimeters;
interbedded with sandy fissile to platy
calcareous shale (beds a few mm. thick).
Gradational with beds above and below
but forms a distinct ledge; tiny plant
fragments (?)........................ 4

Shale, medium olive-gray to medium to
dark-gray, fissile to platy, cal-
careous, gypsiferous, with sandy
laminae that are especially con-
centrated in the upper five feet;
shale becomes harder upwards
forming steep cliffs in the valley
heads; fish scales, few Inoceramus... 32

Shale, medium olive-gray to medium to
dark-gray, fissile to platy, cal-
careous, gypsiferous, slightly
bentonitic (?-rounded slape, "pOp-
corn" surface texture); fish scales,

few lngggramgs....................... 50

Shale, silty to sandy, light to medium
olive-gray to olive-brown, starchy-
fissile to starchy-platy and fissile,
calcareous; contains three three-
fourths inch light to mediumagray
calcarenite beds, one at base, one in
middle, and one at tap, in places con-
taining fossil hash of Inoceramus
and oyster fragments; petroliferous
odor................................. 6

Ft
800

738

734

702

651

in

10

10

10

140

MancOS Shale--Continued

Ft
Shale, olive-gray to oliveabrown'to olive
(color may be due to strong oxidation on
ridge crest), fissile to platy, cal-
careous............................. l6

Shale, medium to light olive-gray to medium
to light-gray, fissile to platy, cal-
careous ..... ..... ..... .............. 20

Shale, orange, fissile, non-calcareous
(bentonite?)0......ICOOOOOOOOCIOCOOO

Shale, medium to light olive-gray to
medium to light-gray, fissile, cal-
careous ...... . .......... ............ l

Shale, light to medium olive-gray, hard,
platy; forms steep cliffs........... 22

Shale, sandy, light to medium olive-gray,
fissile to starchy-platy, bentonitic
("popcorn" surface texture), cal-
careous; sand grains consist of calcite
prisms of broken Inoceramus shells;
upper 24 feet forms steeper slope... 44

Shale, medium olive-gray, fissile,
bentonitic, slightly calcareous
at base, more calcareous upwards,
gypsiferous; hard sandy one-fourth
inch beds scattered throughout; dark-
gray, weathering light-tan to buff,
fine-grained, smooth, rounded, discoid,
limestone concretions about one foot
thick and two to three feet wide
scattered throughout; concretion size
decreased in upper part of unit;
Inoceramus... ....... ........... ..... 31

Bentonite, orange-yellow to white,
gypsiferous; two one-inch beds

separated by one foot of shale...... l

in Ft

645
9

629
8

608
8

607
0

606
4

584
8

539
11

507
2

in
10

10

141

Mancos Shale--Continued

Ft
Shale, medium olive-gray, fissile,
bentonitic, gypsiferous, slightly
calcareous; with sandy layers and
concretions like above............ 6

Juana LOpez Member

Calcarenite, medium to dark-gray weather-
ing than to orange-yellow, platy thin
beds interbedded with dark-gray to
dark olive-gray, fissile, non calcareous,
gypsiferous shale with calcareous
sandy laminae..................... l

Bentonite, orange-yellow, gypsiferous

Calcarenite, medium to dark-gray,
weathering tan to orange—yellow,
thin beds; slight petroliferous
odor; interbedded with shale like
above; Inoceramus................. 2

Bentonite, orange-yellow, gypsiferous

Calcarenite, medium to dark-gray
weathering tan to orange-yellow,
platy to flaggy, thin to thick
beds; slight petroliferous odor;
interbedded with dark-gray to dark
olive-gray, papery to fissile,
gypsiferous shale with calcareous
sandy laminae; Inoceramus,
ammonites......................... 4

Shale, medium to dark-gray to medium
olive-gray, fissile, slightly cal-
careous to non-calcareous, gypsiferous;
with some calcareous sandy laminae; some
cemented one-fourth inch sandy layers
near tap; Inoceramus, ammonites... 33

Calcarenite, medium-gray weathering orange-
brown, thin-bedded; petroliferous odor;
ammonites, Inoceramus, oysters, other
mollusks..........................

in

Ft
506

500

499

499

497

497

493

459

142

Mancos Shale--Continued

Ft in Ft
Shale, light to medium olive-gray to olive- 459
brown, non-calcareous except on planes
of parting, fissile to platy, gypsiferous;
iron-oxide stain on some planes;
Inoceramus impressions common......... 10 8

Shale, medium to dark olive-gray, fissile, 448
gypsiferous, non-calcareous; Inoceramus
impressions; interbedded with some one-
half inch calcarenites, with petrolifer-
ous odor.............................. 10 2

Calcarenite, medium-gray, weathering tan 438
to orange-brown, thin-bedded; petrolifer-
ous odor; contains a few one-half inch
layers of dark gray shale; Inoceramus,
other pelecypods...................... l 0

Lower Carlile Member

Shale, medium to dark olive-gray to black, 437
fissile, brittle, non calcareous,
gypsiferous; interbedded with a few
‘medium gray, weathering yellow~orange
to buff very thin calcarenites; two '
two-inch bentonites near tOp.......... 37 6

Concretion layer; light-gray, weathering 399
orange-yellow, large limestone con-
cretionSOO00............OOOOOOOOOCOOOO 1 0

Shale, medium to dark olive-gray to 398
black, fissile, brittle, non-cal-
careous, gypsiferous.................. 10 2

Limestone, lenticular, light-gray, weathers 388
orange-yellow; with fractured septarian
structure; Inoceramus................. l 0

Shale, medium to dark olive-gray to 387
medium to dark-gray, fissile, non-
calcareous; large spherical lime-
stone concretions scattered
throughout............................ 38 6

Bentonite, light tan to white to orange, 349
gYPSiferOUSOO.......OOOUOOOOOOOOIOOOOO 7

143

Mancos Shale--Continued

Ft
Shale, medium to dark olive-gray to

medium to dark-gray, fissile, non-
calcareous; fractured with iron oxide
stain on planes; large selenite
crystals at surface; spherical dark-
gray limestone concretions about two
to three feet in diameter, with rinds
of cone-in-cone and hollow septarian
cores with one-half to one inch calcite
crystals at centers, scattered through-
out................................. 13

Bentonite, yellow-orange to white,
sticky, fissile, gypsiferous.. ......

Shale, like above with concretions like
aboveOOOO0............OOOOOOOOOOOC0.0 42

Shale like above; with scattered bluish
dark-gray discoid to spherical lime-
stone concretions, weathering orange
brown with a rind of cone-in-cone and
about six inches thick and three feet
in diameter......................... 67

Shale like above; with scattered
light-gray to medium-gray, weathering
buff to tan, fine-grained, smooth,
discoid limestone concretions up
to six inches thick and three feet
wide; one compressed ammonite
in concretion near t0p.............. ll

Shale, medium to dark olive-gray to
medium to dark-gray, fissile, non-
calcareous; compressed ammonites.... l6

Shale, medium to dark olive-gray to
medium to dark-gray, hard, platy
to fissile, softer and more fissile
near top, calcareous, gypsiferous;
hard thin sandy layers common in
about four feet about fifteen feet
above base; Inoceramus (in lower
eleven feet) oysters, compressed
ammonites (especially abundant
about 34 feet above base)........... 55

in Ft in
348 5

6
334 11

2
334 9

2
292 7

0
225 7

2
214 5

9
197 8

10

144

Mancos Shale -Continued

Ft in
Bentonite, orange-yellow to white,
gYPSiferous, fiSSileCCOOOCOCOOCOOOOO 5

Shale, medium-gray, weathers light-
gray to tan, platy, some fissile,
calcareous; lower few feet with
one or two one-half inch calcarenite
layers; upper few feet with iron
oxide-stained fractures and pyritized
fossils; Inoceramus, oysters........ l6 4

Calcarenite, medium-gray, weathers buff
to brown, laminated and cross-
laminated; petroliferous odor;
animal trails on t0p and bottom,
Inoceramus.......................... 6

Greenhorn Limestone Member

Shale, medium grayish-brown, fissile,
weathers papery, calcareous; shell
fragments; interbedded with two two-
inch calcarenite beds (like above);
contains three-inch bentonite....... 2 l

Shale, medium gray-brown, fissile,
calcareous; a few interbedded one-
half inch "cemented shales"......... 2 2

Limestone, medium-gray, fine-grained;
InoceramUSOOOICOOOOOIOOOOOIOOOOOOOOO 1 0

Limestone, medium-gray, fine-grained;
interbedded with olive-brown, cal-
careous, fissile shale containing
shell fragments and forams.......... 2 ll

Bentonite, yellow, gypsiferous,
fiSSileCOCOOOOO0.0000000000000000... 10

Shale, dark-gray to olive, some mottled,
fissile to platy, gypsiferous, cal-
careous; Gryphaea (eSpecially in
concentrated layer at tOp).......... ll 2

Bentonite, yellow to white, fissile,
gYPSiferOUSOOOOOOOOO0.00.00.00.00... 4

Ft
141

141

125

124

122

120

119

116

115

104

in
10

145

Mancos Shale--Continued

Ft

Graneros Shale Member

Shale, light to medium-gray to light
to medium olive-gray, fissile to platy,
calcareous; no fossils.............. 15

Limestone, light to medium-gray, weathers
tan, platy, laminated, fine-grained;
no fOSSiISoooocooooooooooooocooooono 1

Shale, light to medium olive—gray,
fiSSile to starChYOOOOOOOCOOOO...... 9

Limestone, lenticular, light-gray,
weathers tan to buff, massive, fine-
grained; calcite crystals in
fractures...................... .....

Shale, dark to medium-gray, fissile,
calcareous, gypsiferous; discoid
limestone concretions about five
inches thick and two feet wide
scattered throughout................ l4

Limestone, lenticular, medium to
light-gray, weathers orange-yellow
to buff, massive, weathers into
one-half to two inch blocks; well-
rounded sand grains scattered
throughout; calcite crystals in
fractures; no fossils............... l

Shale, sandy, dark-gray, fissile,
calcareous, well-rounded sand
grains floating in matrix........... 3

Sandstone, white, weathers tan to pink,
calcareous; rounded to well-rounded
sand grains; animal trails, shell
fragments...........................

in

Ft in
104 l
89 0
87 6
78 4
77 9
63 6
62 5
59 5

146

Mancos Shale-~Continued

Ft
Shale, dark to medium-gray, fissile to
papery, calcareous; with sand laminae;
becomes almost shaly sand in thin
layers; well-rounded sand grains
floating throughout matrix.......... 11

Bentonite, white and yellow, gypsiferous 1

Concretion layer; light-gray, weathering
yellow-orange, fine-grained, discoidal
limestone concretions about six to 12
inches thick and three feet wide; calcite
crystals in fractures; no fossils... 1

Shale, dark-gray, fissile, non-calcareous,
gypsiferous ............ . ............ 1

Bentonite, white and yellow, gypsiferous

Shale, sandy, olive-gray, fissile, non-
calcareous; olive to yellow sand
laminae.O0.00.00.00.000.000.000.0000 14

Sandstone, tan, cross-bedded (with
channel pattern), very irregular.... 4

Shale, sandy (sand content increases
in lower part), platy at top, blocky
at bottom.(asilts'tone2)............. 4

Sandstone and siltstone, gray to tan,
carbonaceous; mica grains; inter-
bedded with shale................... 8

Shale, medium-gray,platy to Chippy;
interbedded with dark green-gray
siltstone with a two to three
inch hard sandstone about two
feet from top....................... 5

Shale, sandy, light to medium gray-olive

above, olive green-gray below,
bIOCkYOO......OOOCOOOOOOOOOOO. ...... 5

Concealed 2

 

in

Ft
59

47

46

45

44

44

29

25

20

12

10

10

10

10

147
UTE RESERVATION SECTION

Section of Mancos Shale measured in sections 9, 16, 20, 21, T. 32 N.,
R. 19 W., sections 9, 10, ll, 12, l3, 16, T. 32 N., R. 18 W., and
section 18, T. 32 N., R. 17 W,

Distance
Thickness above base of
formation
Point Lookout Sandstone Ft in Ft in
Sandstone... ..... . .......... .. ..... 3 0 46 l
Sandstone interbedded with shale; 43 1
sandStonesxqato three feet thick... 43 1
46 1
Mancos Shale
Upper Shale Member
Shale interbedded with sandstones 1641 7
and siltstones one to five inches
thick..... ..... . ....... ... ..... . 6 0
Siltstone, dark-gray calcareous; with 1635 7
shale partings and tan sandstone
streaks; plant fragments........ 7 10
Siltstone with thin lenticular mud- 1627 9
stones and concretions.......... 9 2
Siltstone, non-calcareous; cliff- 1618 7
forming; plant fragments........ 7 7
Shale, b1ack,crumb1y to platy; contains 1611 0
sandstone partings, and very thin beds;
sandstone contain plant fragments and
oyster shell fragments.......... 77 6
Limestone, brown-gray, weathers red,
SiltyOCOCO......OOOOOOOOOOUOOOO. 8 1533 6
Dakota Sandstone
Sandstone, massive, tan, cross- 41 6
beddedCCCOOOIC......OOOOOOOOOOOOOOO 9 O
Shale, with thin, laminated carbon- 32 6
aceous micaceous sandstones........ l 0
Sandstone, tan, massive, cross- 31 6
beddedCOOOOOOOOOOOO ............ 0... —3-]-_ i

41 6

148

Mancos Shale--Continued

Shale, black, fissile to platy; inter-
bedded with sandstones a few milli-
meters to a few centimeters thick;
sandstones vary from twenty to
eighty percent of rock.... .........

Limestone, gray, weathers pink, silty.

Shale, black, sandy; interbedded with
very thin sandstones a few milli-
meters to a few centimeters thick;
sandstone vary from twenty five to
sixty percent of rock..............

Siltstone, calcareous, gray to pink,
weathers redOCOCCCCCCCCCCCCO......O

Shale, black, fissile to crumbly; inter-
bedded with very thin sandstones
from a few millimeters to a centi-
meter thick; concentration of sand-
stones varies but less than forty
percent of rock....................

Mudstone, lenticular, calcareous,
laminated; plant fragments... ......

Shale, light to medium olive-gray, calc-
areous, gypsiferous; interbedded with
sandstone laminae a few millimeters
thick; sandstone makes up fifty per-
cent of rock in some layers........

Mudstone, lenticular, medium-gray,
weathers buff to orange-yellow,ca1c-
areous, blocky to p1aty............

Shale, light to medium olive-gray, cal-
careous,gypsiferous; interbedded
with sandstone layers a few milli—
meters thick; sandstone makes up
fifty percent of rock in some
layers................... ..........

Ft

86

30

119

49

in

10

11

Ft
1532

1446

1445

1414

1414

1294

1292

1243

1242

in

10

149

Mancos Shale~-Continued

Mudstone, lenticular, medium-gray,
weathers buff to orange-yellow,
massive tO'platysooooooooooooooo

Shale, light to medium olive-gray,
calcareous gypsiferous; inter-
bedded with sandstone laminae and
layers up to two inches thick...

Mudstone, lenticular, light-gray,
weathers buff to orange-yellow,
calcareous, laminated, platy to
massive ................. ... .....

Shale, light to medium olive-gray,
~calcareous, gypsiferous; inter-
bedded with light sandstone laminae
and a few beds up to one-half inch
thick which appear concentrated in
groups..........................

Mudstone, lenticular, light-gray,
weathers buff to orange-yellow,
calcareous; Inoceramus impressions

Shale,medium to dark-gray, calcareous,
gypsiferous,with light sandy laminae
and some widely separated sandstone
beds a few millimeters thick....

Bentonite..... ...... . ..............

Shale, medium to dark gray, calcareous,
gypsiferous; with sandy laminae and
some widely separated sandstone beds
a-few millimeters thick.........

Mudstone, lenticular, light-gray to
buff, weathers buff to orange-
yellow, platy to massive, lami-
nated; Inoceramus, trace of a
"horny" coiled ammonite.........

Shale, medium to dark-gray, fissile,
calcareous; with light sand lami-
nae and widely separated sandstone
beds a few millimeters thick....

Ft in
10

26 2
l 0
32 5
6

l6 9
l

39 7
l 8
23 1

Ft

1219

1218

1192

1191

1159

1158

1141

1141

1102

1100

in

10

150

Mancos Shale--Continued

Ft in Ft in

Mudstone, lenticular, light to medium- 1077 5
gray, platy to thin bedded, slightly
calcareous....................... l 0

Shale, medium to dark-gray, fissile, 1076 5
calcareous, with light sand laminae
and widely separated sandstone beds
a few millimeters thick; fish scales,
large Inoceramus weathers out on
surface .......................... 32 8

 

Sandstone, calcareous ............... 6 1043 9

Shale, medium to dark-gray, fissile, 1043 3
calcareous; with light sand laminae
and a few widely separated sandstone
beds a few millimeters thick..... 2 4

Mudstone, lenticular, medium-gray 1040 ll
weathers orange-yellow, slightly
calcareous....................... 2 0

Shale, medium to dark-gray, fissile, 1038 11
calcareous; with light sand laminae '
and a few widely separated sandstone
beds a few millimeters thick..... 3 ll

Calcarenite ......... .......... ...... 6 1035 0

Shale, sandy, light to medium-gray to 1034 6
light to medium olive-gray, brittle
to papery, calcareous, gypsiferous;
with a few sandstone beds a few
centimeters thick.......... ..... . 5 7

Mudstone, lenticular, light to medium- 1028 ll
gray, weathers buff to orange-yellow,
slightly calcareous.............. l 0

Shale, sandy, light to medium-gray to 1027 11
light to medium olive-gray, brittle,
fissile to papery, calcareous,
gypsiferous; with a few sandstone
layers up to two centimeters thick 11 3

151

Mancos Shale--Continued

Mudstone, lenticular, light to medium-
gray, weathers buff to orange-
yellow, massive to platy, slightly
calcareous to calcareous..........

Shale, sandy, light to medium-gray to
light to medium olive-gray, brittle,
fissile to papery; with a few sand-
stone beds up to about two centi-
‘meters thick......................

Mudstone, light-gray, weathers buff,
massive, slightly calcareous; with
parallel vertical fractures.......

Shale, sandy,silty,light to medium gray-
brown, fissile to papery,calcareous;
with a few sandstone beds up to two
centimeters thick.................

Sandstone, somewhat lenticular, cal-
careous; bedding planes appear
"pitted".............OOCOIOCIO....

Shale, sandy, silty, light to medium
gray-brown, fissile to papery, cal-
careous; with a few sandstone beds
in the upper part up to two centi-
meters thick......................

Mudstone, lenticular, medium-gray,
weathers orange-yellow, slightly
calcareous; plant fragments.......

Shale, sandy, silty, gray-brown to
brownish gray, fissile; with some
sand laminae a few millimeters
thick................. ....... .....

Mudstone, lenticular, medium-gray,
weathers orange-yellow, massive to
platy, calcareous. ........ . ...... .

Ft

18

20

in

11

Ft
1016

1015

996

996

990

988

968

965

956

in

11

ll

11

10

11

152

Mancos Shale--Continued

Shale, slightly sandy, medium-gray
layers alternating with light-
brown layers, fissile, calcareous;
with sand laminae up to a few
millimeters thick................

Mudstone, lenticular, medium-gray,
weathers orange-yellow, massive to
platy, calcareous; plant fragments,
Inoceramus impressions, traces of
coiled ammonites and baculites...

Shale, medium to light olive-gray to
medium-gray, paperx to fissile, cal-
careous; with sand laminae and sand-
stones a few millimeters thick; large
thick Inoceramus ...... ... ........

Mudstone, lenticular, medium-gray,
weathers orange-yellow, platy, cal-
careous; breaks up into large flat
concretions in two layers along out-
crop; trace of baculite..........

Shale, medium to light olive-gray to
medium-gray, papery calcareous; sand
laminae and sandstones a few milli-
meters thick;upper part hard,
brittle; large thick lnoceramus..

Mudstone, lenticular, light to medium-
gray, weathers buff to orange-yellow,
calcareous; fish scales, plant frag-
ments (?)... ..... . ........ .......

Shale, medium-gray, fissile to papery,
calcareous; with sandstones a few
millimeters thiCk. I O O O I O ..... C O O O

Concretion layer; medium-gray, weathers
orange-yellow, massive, calcareous
mudstone concretions; large, dis-
coidal...........................

Fl:

14

21

in

Ft
954

949

948

993

931

910

909

907

in
11

10

153

Mancos Shale-~Continued

Ft

Shale, medium to dark gray to olive-
gray, papery to fissile, calcareous;
a few sandstones a few millimeters
thick; large thick Inoceramus..... 9

Mudstone, lenticular, light to medium-
gray weathers buff, massive to platy,
calcareous; ammonite impressions.. l

Shale, light to medium olive-gray to
gray to medium to dark-gray, fissile,
papery to platy, calcareous; platy
layers hold up steeper s10pe; with a
few sandstones in the lower few feet
a few millimeters thick; Inoceramus
impressions....................... 22

Mudstone, light-gray, weathers orange-
yellow, platy, calcareous; Inoceramus

Shale, medium to dark-gray, papery to
fissile, calcareous; with a few sand-
stones a few millimeters thick.... 7

Mudstone, lenticular, medium-gray,
weathers orange-yellow, massive to
platy, calcareous; ammonites......

Shale, light to medium-gray to light to
medium olive-gray, fissile, calcareous;
with tan to light gray calcarenites a
few millimeters thick; large thick
Inoceramus........................ 17

Mudstone, lenticular, light to medium-
gray, weathers buff to orange-yellow,
massive to platy, slightly calcareous

Shale, black, papery to platy; with some
sandstones a few millimeters thick
interbedded....................... 60

Sandstone, thin, platy; interbedded with
thin fossiliferous, calcareous mud-
stone. ........ . .......... ......... 12

in

11

10

10

Ft
906

896

895

873

872

864

863

846

846

785

in

10

10

10

154

Mancos Shale--Continued

 

Ft in Ft in
Shale, black, fissile to platy; parts
with tan partings ..... ........ . 113 6 773 0
Sandstone, brown-red, thin, platy... l 659 6
Shale, black; weathers into tan,papery 659 5
plates; interbedded with thin platy
calcarenites (?).......... . ..... . 27 11
Shale, black, fissile to platy, slightly 631 6
calcareous; some weathers into papery
gray p1ates0000 ...... 0.0.000.00.. 50 3
Sandstone, red-brown, platy ......... 2 581 3
Shale, light to medium olive-gray, 581 l
papery to fissile, calcareous; thick- ’
shelled Inoceramus ............... 26 7
Bentonite....00.0.0.0. ..... 0 00000000 6 554 6
Shale, light to medium olive-gray, 554 0
fissile, calcareous, slightly
bentonitic .............. . ........ 3 9
Bentonite.... 00000000000000 000.00... 2 550 3
Shale, light to medium olive-gray, 550 l
fissile to papery, calcareous; thick- ‘
shelled Inoceramus; interbedded with
a few calcarenites a few millimeters
thick,more concentrated at bottom. 5 8
Bentonite....00.000.000.00000000000. 5 544 5
Shale, light to medium olive-gray,fissile 544 0
to papery, calcareous; with a few cal-
carenites a few millimeters thick. 17 0
Sandstone; weathers reddish; platy,with 527 0
shale partings ........ ............ l O

Juana Lopez Member

155

Mancos Shale--Continued

Ft in Ft

Sandstone (calcarenite), tan, cross- 526
laminated; animal trails; some beds
to two inches thick; interbedded
with light to medium olive-gray
fissile to papery calcareous shale;
thick-shelled Inoceramus....... 15 0

Sandstones (calcarenite), tan to buff, 511
platy, laminated and cross-laminated,
ripple-marked; up to a few centi-
meters thick; with animal trails;
interbedded with medium to dark-gray,
fissile to papery, non-calcareous
shale; contains large discoidal to
spherical, light-gray limestone con-
cretions with cone-in-cone and

. 27 10
septarian structures...........

Bentonite...... .......... ......... 2 491

Sandstones (calcarenite), tan to buff, 491
platy, laminated and cross-laminated,
ripple-marked; up to a few centi-
meters thick; with animal trails;
interbedded with medium to dark-gray,
fissile to papery, non-calcareous
shale; contains large discoidal to
spherical, light-gray limestone con-
cretions with cone-in-cone and
septarian structures........... 4 8 486

Sandstone (calcarenite?); weathers
brown................... ....... 5

Sandstone (calcarenite), tan to buff, 485
platy, laminated and cross-laminated,
ripple-marked; up to a few centi-
meters thick with animal trails; inter-
bedded with medium to dark-gray,
fissile to papery, non-calcareous
shale.......................... 5 9

Sandstone (calcarenite)........... 6 480

156

Mancos Shale-~Continued

Ft

Sandstone (calcarenite), tan to buff,
platy, laminated and cross-laminated,
ripple-marked; up to a few centi-
meters thick, with animal trails;
interbedded with medium to dark-gray,
fissile to papery, non-calcareous
shales........................ 12

Calcarenite, medium-gray, flaggy to
platy; petroliferous odor; pele-
cypods and ammonites.......... l

Sandstone (calcarenite), platy, to few
inches thick; interbedded with medium-
gray, non-calcareous shale with petro-
liferous odor; Inoceramus other clams,
shark teeth................... 15

Calcarenite, medium to light-gray,
weathers orange brown flaggy to
platy, cross-laminated; petro-
liferous odor; Inoceramus, other
clams......................... 3

Shale, light to medium-gray to tan to
buff to yellow, fissile to platy,
non-calcareous, gypsiferous;
Inoceramus; interbedded with light-
gray, weathering to buff, platy,
cross-laminated calcarenite; animal
trails, Inoceramus, tiny plant
fragments..................... 14

Concretion layer; concretions with light-
gray limestone cores that weather tan
to buff and have an earthy pink shell
on underside; spherical to three feet
in diameter; thin sandstone beds are
draped over them.............. 3

Shale, light to medium-gray to tan to
buff to yellow, fissile to platy, non-
calcareous, gypsiferous; Inoceramus;
interbedded with light-gray
weathering to buff, platy, cross-
laminated calcarenite; animal trails,

Inoceramus000.0000000...00.0.00 2

in

Ft
479

467

466-

450

447

425

422

in

10

10

10

10

157

Man¢os Shaleu-COntinued

Ft

Lower Carlile Member

Shale, light to medium-gray to tan to
buff to yellow, fissile to platy,
non-calcareous, gypsiferous; inter-
bedded with light-gray, weathering
buff, platy, cross-laminated cal-
carenite; animal trails, Inoceramus ll

Bentonite... ............. . ...... .....

Shale, dark-gray, fissile to papery,
brittle, non-calcareous, gypsiferous;
large limestone concretions and a few
thin lenticular limestones scattered
throughout; also some one to two inch
diameter (pyrite) concretions; some
interbedded calcarenites a few milli-
meters to two centimeters thick... 5

Bentonites (two); separated by a few
inches of shale; bentonites two inches
th1CR..0000000.00.000000000000000.

Shale, dark-gray, fissile to papery, non-
calcareous, gypsiferous; large lime-
stone concretions scattered throughout;
some interbedded calcarenites a few
millimeters to two centimeters thick 35

Limestone, lenticular, medium to dark-gray,
weathers buff to yellow-orange, massive,
fine-grained; calcite crystals in
center in septarian like fractures;
Inoceramus, coiled ammonite im-'
pressions.. ........... .... ....... . 1

Shale, dark-gray, fissile to papery, non-
calcareous, gypsiferous; some inter-
bedded calcarenites a few millimeters
to a centimeter thick; (snails, fish
teeth, clams, in float)........... 2

Shale, dark-gray, fissile to papery, non-
calcareous, gypsiferous; fractured
with iron-oxide and yellow stains
on planes......................... 30

in

10

Ft

419

415

407

402

401

366

365

362

in

158

Mancos Shale--Continued .

Ft
Bentonite, tan to yellow-orange, l
fissile to blocky... ..... .........
Shale, medium to dark-gray, blocky to
fissile, non-calcareous, gypsiferous;
iron-oxide stain on fractures; softer
than shale above.................. 14

Bentonite; layer of large spherical
medium-gray limestone concretions
centered at same level; they weather
buff, are one to four feet in dis-
meter and have a shell of cone-in-
cone structure....................

Shale, medium to dark-gray, soft, fissile
to platy, non-calcareous, gypsiferous;
iron-oxide and yellow stain on bedding
and fracture planes; large spherical,
medium to dark-gray, fine-grained
limestone concretions scattered
throughout, up to four feet in diameter
with calcite crystals at cores of
septarian structure and a shell of cone-
in-cone ......... .................. 34

Shale, medium to dark-gray, soft, fissile
to platy, non-calcareous, gypsiferous;

iron-oxide and yellow stain on plates 22

Shale, medium to dark-gray, hard, brittle
fissile to platy, non-calcareous... ll

Shale, medium to dark-gray, soft, fissile
bentonitic (?), non-calcareous.... l8

Bentonite, tan to yellow to orange...

Shale, medium-gray, hard, brittle,

fissile to platy, non-calcareous.. 8

Bentonite....000000.0000000000000000.

in

Ft
332

330

316

316

282

259

248

229

229

221

in

11

10

159

Mancos Shale--Continued

Ft
Shale, medium to dark-gray to medium
to dark olive-gray, fissile to
platy, non-calcareous, gypsiferous;
with silty laminae about one milli-
meter or less thick; coiled com-
pressed ammonite; a calcareous layer
a few feet thick near base....... 43

Bentonite.....0000.0.0.0....00000000

Shale, black, platy, non-calcareous;
compressed coiled ammonite....... ll

Bentonite....00.0......0.....0.0.000

Shale, black, platy, calcareous,
gypsiferous; abundant oysters,
ammonites, fish scales; lowest
occurrence of compressed coiled
ammonite at 15 feet below base... 26

Shale, black, platy, hard, calcareous;
amonites cmon0000.0.0000000.00 10

Bentonite......0.00....0....00...0..

Shale, black to gray, platy;hard, cal-
careous; ammonites common; hard
enough to be called a limestone in
places (7); plant fragments (?).. 25

Calcarenite, light to medium-gray,
weathers reddish-brown; fossil-
iferOUSsaaooaaao00000000000000...

Greenhorn Limestone Member

Shale medium-gray platy, hard, cal-
careous; weathers into papery plates;
one six-inch harder layer two feet
from tap......................... 13

Limestone, medium-gray, weathers buff,
fine-grained, massive; Inoceramus l

in

Ft
218

174

174

163
163

136

126

126

101

101

87

ll

160

Mancos Shale--Continued

 

Ft
Shale, medium-gray, fissile to platy,
calcareous0.0.. ........ .....0... 2
limestone, medium-gray, weathers buff,
fine-grained, platy to massive,
InoceramUSOooooooooooa0000.00.00 1
Shale, medium-gray fissile to platy,
calcareous...0000000000....0.00. 3
Limestone, medium-gray, weathers buff,
fine-grained, massive; Inoceramus l
Shale, medium-gray, platy to fissile,
calcarQOUSOOOoooooooa00000000000 2

Limestone, medium-gray, platy to massive,
fine-grained; Inoceramus........ l

Shale, interbedded with limestone or
calcareous mudstones; tan to light to
medium-gray; one inch to one foot
thick; calcareous, gypsiferous;

Gryphaea in lower part.......... 6

Bentonite.........00.00............
Graneros Shale Member

Shale, medium to dark-gray, fissile to
platy, calcareous, gypsiferous;
iron-oxide stain on some planes;
Gryphaea restricted to upper five
feet two inches and concentrated
in a three-inch layer nine inches
from the tOp; oysters, shark teeth 10

Bentonite......0.00..............0.

Shale, medium to dark-gray, fissile to
platy, calcareous, gypsiferous; iron-
oxide stain on some planes...... 7

Limestone, lenticular, light to medium-
gray, weathers buff to tan, fine-
gfained; oysters;tends to break up into
concretion layer.... ..... .......

in

10

ll

10

‘Ft

85

83

82

78

77

75

73

66

65

55

54

46

in
10

10

11

161

Mancos Shale--Continued

Ft

Shale, medium to dark-gray, fissile to
platy, calcareous, gypsiferous;
oysters.0......0000.........0.0. 1

Limestone, light to medium-gray,
weathers buff to tan, fine-
grained... ................... ...

Bentonite (three beds), separated from
limestone above and each other by
shale like below; upper bed is four
inches thick, middle five inches,
lower one and one-fourth inch thick
and separated by nine inches and one
foot two inches, respectively... 2

Limestone, lenticular to concretionary,
light-gray to tan, weathers buff,
massive, fine-grained weathers into
two inch blocks................. 1

Mudstone, shaly, light to medium olive-
gray, weathers light-gray, fissile
to platy to starchy, calcareous,-
gypsiferous; small clams........ 8

Mudstone, as above; with fine-grained,
massive light to medium-gray,
weathers to brown; limestone con-
cretions from a few inches to over
one foot in diameter; bottom is
marked by layer of "basketball-size"
concretions; oysters............ 5

Mudstone, shaly, sandy, light to medium
olive-gray, starchy to fissile,
calcareous, gypsiferous......... 9

1641

Dakota Sandstone
Sandstone, thick-bedded............ 12
Lignitic shale..................... l

Lignite.. ....... ... ..... . ..... ..... l

in

10

O O O O \ll-L‘

Ft
45

44

44

24

23

14

14

in

10

PLATE 8

10
' 11
12
13
14
15
16
17

18

163

PLATE 1

‘Baltisphaeridium cf. 2. expensis, X 1000

Baltisphaeridium cf. B. infalatum, X 1000

Baltisphaeridium sp. 1, X 750

 

Michrystridium spp., X 1000

 

Form X 8p.

Form

Form

Form

Form

L

N

T

S

sp.

sp.

sp.

sp.

1, X 1000
1, X 1000
1, X 1000
1, X 1000

1, X 1000

Veryhachium cf. 1. stellatum, X 750

Form S sp. 2, X 1000

Veryhachium sp. 1, X 1000

Veryhachium cf. 2. eurogeum, X 1000

Veryhéchium sp., X 1000

Leiofusa 3p., X 1000

. on...‘ v
a..ro.n

» I 0 Ounovr
amass...
. 0

 

.s

PLATE 1

2,5

10
ll
12

13

165

PLATE 2

Metaleiofusa sp., X 1000
,Qymgtiosphgera spp., X 1000
Pterospermopsis Sp., X 1000
Form B sp. 3, X 1000

Form B sp. 2, X 1000

Form B sp. 1, X 1000

Form B. sp. 4, X 750

Form C sp. 2, X 1000

Form C Sp. 1, X 1000

Form C sp. 3, X 1000
Hystrichosphaeridium cf. 3. deanei, X 750

Hystrichosphaeridium cf. 3. tubiferum, X 750

u p a
Brit .flpVI’ .
a.”

 

PLATE 2

167

PLATE 3

l Oligosphaeridigm,pulcherrimum, X 750
2 Cordosphaeridium sp. 1, X 750
3 Cordosphaeridigm difficile, X 750
4-5 Tanyosghaeridium cf..2. variecalamum, X 1000

6 Hystrichokolpggg ferox, X 750

 

 

PLATE 3

 

169

 

 

PLATE 4
l lgtosphaeridium si hono horum, X 1000
2 Diphyes cf. 2. colligerum, X 750
3-5 Polysphaeridium spp., X 750
6 Surculosphaeridium cf. S. vestitum, X 750

 

7 Form 0 sp. 1, X 750

 

PLATE 4

171

PLATE 5

?Exochosphaeridium phragmiggg, X 750
?ExochOSQhaeridium sp. 1, X 750
fiystrichosphaera £39223, X 750
?Exochosphaeridium sp. 2, X 750
Bystrichosphaera £52223 var. l, X 750

gystrichosphaera ramosa var. 2, X 750'

30.0"": 's'lo‘t -

 

       

       

r .h..............“
Rum-son 4
ca... ... .... .5.

PLATE 5

1-2

6-7

173

PLATE 6

HystrichOSQhaera sp. 1, X 750
Microdinium cf. 11. ornatum, X 1000
Heslertonia heslertonesis, X 750
?Leptodinium dispertitum, X 1000

Gonyaulagysta spp., X 750

l
v

3%.. ‘1 .
a Humane...

\

 

PLATE 6

1-2

5-6

175

PLATE 7

?Gonyaulacysta sp. 1, X 750.
Areoligera spp., X 750

Cyclonephelium spp., X 750

 

2 shows crests missing(?)

 

PLATE 7

177

PLATE 8

22223 sp., X 750

Palaeohystrichophora infusoroides, X 750. three specimens
Paleohystrichophora infusoroides var. 1, X 750
Eggggg.amorpha, X 1000

Deflandrea cf. 2. gig-95, X 1000

Deflandrea cf.

IU

verrucose, X 750

Deflandrea cf.

IU

granulifera, X 750

Deflandrea cf.

'5

acuminata, X 750

 

PLATE 8

l-3,5

179

PLATE 9

Deflandrea
Deflandrea
Deflandrea
Deflandrea

Deflandrea

. D. balmei, X 1000

4, X 750
1, X 1000
D. micracantha, X 750

2, X 750

 

PLATE 9

181

 

 

PLATE 10
1,3 Hexagonifera suspecta var. 1, X 750
2 Deflandrea sp. 3, X 750
4 Hexagonifera susEecta, X 750

 

5 Hexagonifera suSpecta var. 2, X 750

 

PLATE 10

183

 

PLATE 11
1-2 Odontochitina striatoperforata, X 500
3 Form F sp. 1, X 750
4-5,7-8 Dinogymnium sp. 1, X 1000

 

6 Canningia cf. Q, colliveri, X 750

 

 

              
   

PLATE 11

1-10

11

12

185

PLATE 12

Dinogymnium sp. 2, X 1000
?Diconodinium arcticum, X 1000

?Horologinella spinosa, X 1000

 

  

cucuskuun

            
       

     

.
. u...o-..<~Oo..‘
..nccoo-w.
.ll'.

  

        
 

    

.' ...
....l- 0'. GI...
use... I p .
1"... n

.10

  

. “newsman-nonu- use.

    

Isaac-
Inca-aoo-aaou

...-II.OO§IIII0II.

,~- 0 p

. .1.

I.

7’

 

PLATE 12

187

PLATE 1 3

Form D sp. 1, X 750

?Trigonqpyxidia sp., X 1000

Palambages cf. 2, deflandrei, X 750
Pediastrum sp., X 750

Gleicheniidites senonicus, X 1000
Sphagnum3porites antiggasporites, X 1000
Gleicheniidites circinidites, X 1000

Leiotrilets pseudomaximus, X 1000

 

Cardioangulina diaphana, X 1000

 

 

PLATE l3

11

12

14

189

PLATE 14

Cardioangulina diaphana, X 1000

 

?Deltoidospora hallii, X 1000
Undulatisporites sp. 1, X 1000
Triplanosporites of. l, terciarius, X 1000

Undifferentiated large smooth trilete spores, X 1000

.anthidites cf. Q, mesozoicus, X 1000

 

TriplanosPorites sinuosus, X 1000

 

?Concavisporites Sp. 1, X 1000

Cingulatingrites radiatus, X 750

 

 

Kuylisporites scutatus, X 1000
?Acanthotriletes varispinosus, X 1000

Concavissimi8porites variverrucatus, X 750

 

 

PLATE l4

10

ll

12

13

14

191

PLATE 15

Lycopodiumsporites cerniidites, X 1000
?CamarozonoSporites insi nis, X 1000
ConverrucosiSporites cf. Q. plgtyverrucosus, X 1000
Appendicisporites cf. A. tricornatatus, X 1000
Cicatricosisporites cf. Q. hallei, X 1000
Cicatricosisporites cf. 9. dorogensis, X 1000
?Corrugatisporites toratus, X 1000
Laevigatosporites cf. L. ovatus, X 1000
Small‘giggs-type pollen grain, X 1000
Cicatricosisporites cf. 9, carlylensis, X 1000
Vitreispgritesgpallidus, X 1000
Verrucatosporites cf. 3. faygg, X 1000
Reticulate monolete spore, X 750

Large Pinus-type pollen grain, X 750

 

PLATE 15

10

11-12

13

14

193

PLATE l6

Picea-type pollen grain, X 750

Classopollis cf. Q, classoides, X 1000. 2 shows a tetrad
of small-size class; 1 is large-size class

 

 

?Parvisaccites sp. 1, X 750

 

Classopgllis sp. 1, X 1000. 5 shows a tetrad; 6 shows
tetrad mark on a single grain

 

Rugubivesiculites cf. 3, reductus, X 750

 

Large Eguisetospgrites Sp., X 1000

 

Abies-type pollen grain, X 750
Small Eguisetosporites Sp., X 1000
Inaperturopollenites Sp. 1, X 1000

Inaperturopollenites Sp. 2, X 1000

 

Inaperturopollenites sp. 3, X 1000

          

v

   
                     

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da'l. .11 n
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n. b
. I

             

   

scour-n
a o I no I I

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on.

on.

a)

        

  

  

         

(graft...
no .
tout-InI-Ion on. o... .
.. . 0"90.‘
. o . .1I
. o . . 4
o . .I II
I
.v... u-
». I .0
I I I .0
I - l V.
4 . u o I
III<..
O \ .
_Q _
I I '.
I Q ...
. I I
. u.
. I.
. I
a c . .
. 0
. c o
c
. . .
. ‘
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U
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I '
I I I Q
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0
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PLATE 16

1o
11
12-14,17
15,19-20
16

18

195

PLATE 17

Inaperturopollenites limbatus, X 750. 2 shows type with
rudimentary "bladder"

 

?chadopites sp. 1, X 1000

 

,Quadripollis Krempii, X 750

?chadopites Sp. 3, X 1000

 

?chadopites sp. 2, X 1000

 

Inaperturopollenites sp. 3, X 1000

Eucommiidites cf. E, troedssonii, X 1000

 

Eucommiidites cf. E, couperi, X 1000

 

Eucommiidites Sp. 1, X 1000

 

Exesipollenites tumulus, X 1000

Tricolpgpollenites cf. 2, retiformis, X 1000; 17 X 750

 

 

Tricolpopollenites cf. T. micromunus, X 1000

 

 

Pflugipollenites dampieri, X 1000

Tricolpopollenites henrici, X 1000

 

PLATE 17

2-3

4,10

11

12-13

14
15
16
17,21-22
1s
19
20
23
24
25

26-28

29

197

PLATE 18

Tricolpopollenites sp. 1, X 1000

 

Tricolpopollenites sp. 6, X 1000

 

Tricolpopollenites sp. 5, X 1000

 

Tricolporites traversi, X 1000

Tricolpopollenites Sp. 7, X 1000

 

Tricolp0pollenites sp. 4, X 1000

 

Tricolporites rhomboides, X 1000

 

Tricolpopollenites sp. 3, X 1000

 

Tricolpopollenites sp. 2, X 1000

Tricolpites cf. 1. explanata, X 1000. 12 shows the larger

 

size, 13 shows the smaller Size
?Trialapollis Sp. 1, X 1000
Retitricolpites cf. 3, georgensis, X 1000

Tricolpites cf. 1. bathyreticulatus, X 1000

 

Duplopollis cf. 2. orthoteichus, X 1000

 

 

Tricolpites cf. T, anguloluminosus, X 1000

 

Tricolpopollenites sp. 8, X 1000

 

Retitricolpites cf. 3, ggranioides, X 1000

 

Triporopollenites Sp. 1, X 1000

 

Hexacolpate pollen grain, X 1000
Dicotetradites cf. 2. clavatus, X 1000

Triporopollenites cf. 1, scabroporus, X 1000. 27 shows
form with protruding pores

 

?Extratriporopollenites sp., X 1000

 

 

PLATE 18

10

ll

12

l3

14

15

199

PLATE 19

Triatriopollenites cf. 2, rurensis, X 1000

 

?Porocolpopollenites sp. 1, X 1000

 

?Plicapollis silicatus, X 1000

Trudopollis cf. 1, hemiparvus, X 1000

 

 

Conclavipollis cf. 9, wolfcreekensis, X 1000

 

Labrapgllis globsus, X 1000

 

Sporopollis cf. §. laqueaeformis, X 1000

 

Triporopollenites cf. 2, tectus, X 1000

 

Proteacidites cf. 2, thalmanii var. 4, X 1000

 

Proteacidites thalmanii var. 3, X 1000

 

 

Proteacidites thalmanii var. 2, X 1000

Proteacidites thalmanii var. l, X 1000

 

Trichotomosulcites cf. 2, contractus, X 1000

Peromonolites peroreticulatus, X 1000

 

Liliacidites cf. L, leei, X 1000

 

 

PLATE 19

 

 

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