Stratigraphic distribution of some pollen 

types from the Campanian and lower 

Maestrichtian rocks (Upper Cretaceous) 

of the Middle Atlantic States

GEOLOGICAL SURVEY PROFESSIONAL PAPER 977

Stratigraphic distribution of some pollen 

types from the Campanian and lower 

Maestrichtian rocks (Upper Cretaceous) 

of the Middle Atlantic States

By JACK A. WOLFE

GEOLOGICAL SURVEY PROFESSIONAL PAPER 977

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1976
UNITED STATES DEPARTMENT OF THE INTERIOR 

THOMAS S. KLEPPE, Secretary

GEOLOGICAL SURVEY 

V. E. McKelvey, Director

Library of Congress Cataloging in Publication Data

Wolfe, Jack A. 1936-

Stratigraphic distribution of some pollen types from the Campanian and lower Maestrichtian rocks (Upper Cretaceous) of

the Middle Atlantic States.

(Geological Survey Professional Paper 977)

Bibliography: p.

Supt.ofDocs.no.: 119.16:977

1. Pollen, Fossil. 2. Paleobotany-Cretaceous. 3. Paleobotany-Middle Atlantic States. I. Title. II. Series: United States.

Geological Survey Professional Paper 977. 

QE993.2.W64 560M3 76-608052

For sale by the Superintendent of Documents, U.S. Government Printing Office

Washington, D.C. 20402

Stock Number 024-001-02816-6
CONTENTS

Page

Abstract _________________________________________ 1

Introduction ____________________________________________ 1

Geologic occurrence.________________________________ 1

Biostratigraphy ___________________________________ 3

Significance to lithostratigraphic units-______________ 7

Correlations with pollen assemblages from the Mississippi

embayment __________________________________________ 8

Correlations with pollen assemblages from the Cape Fear 

arch __________________________________________ 9

Paleoecology ___________________________________________ 9

Significant pollen types ____________________________________ 11

Fossil localities_________________________________ 17

References cited ____________________________________ 17

ILLUSTRATIONS

[Plates follow references]

PLATE 1. Campanian and Maestrichtian pollen, NA-1 NH-1.

2. Campanian and Maestrichtian pollen, NJ-1 PR-7.

3. Campanian and Maestrichtian pollen, C3A-1 CP3B-5.

4. Campanian and Maestrichtian pollen, CP3B-6 MPI-1.

FIGURE 1. Map of the sample locations in the Middle Atlantic States

2. Post-Magothy Cretaceous rock sections ____________

3. Graph showing abundance of major pollen types ______.

Page

2

3

10

TABLES

Page

TABLE 1. Stratigraphic distribution of selected taxa of dicotyledonous pollen in the Campanian

and Maestrichtian rocks of the Middle Atlantic States ________________________ 4

2. Comparison of ages predicted on the basis of climatic cycles with radiometric ages in

Campanian and Maestrichtian rocks of the Middle Atlantic States_______ 11

III

STRATIGRAPHIC DISTRIBUTION OF SOME

POLLEN TYPES FROM THE CAMPANIAN AND

LOWER MAESTRICHTIAN ROCKS (UPPER CRETACEOUS)

OF THE MIDDLE ATLANTIC STATES

By JACK A. WOLFE

ABSTRACT

Analysis of 74 pollen samples from the Cliffwood beds of the upper 

part of the Magothy Formation and from the younger marine Cretaceous rocks indicates that 10 informal biostratigraphic subdivisions 

can be made of this Campanian and lower Maestrichtian section. 

Comparison of these subdivisions in the northern Raritan embayment 

with those in the southern Salisbury embayment indicate that the 

Woodbury Clay in the north is a facies of the upper part of the 

Merchantville Formation to the south. The pollen data can be interpreted to support the concept that the lower part of the Mount Laurel 

Sand in the south is the biostratigraphic equivalent to the Wenonah 

Formation in the north. The "Matawan" previously recognized on the 

west shore of Chesapeake Bay is shown to be "Monmouth" and equivalent in age to part of the Navesink Formation of the Monmouth Group. 

The biostratigraphic subdivisions proposed form the basis for correlations of the Late Cretaceous rocks of the Mississippi embayment with 

those of the Atlantic Coastal Plain. Fluctuations in the relative abundance of bisaccate coniferous pollen are interpreted as climatic fluctuations. A total of 104 dicotyledonous pollen types are briefly discussed 

and illustrated.

INTRODUCTION

The difficulties of correlating the Campanian and 

Maestrichtian (Upper Cretaceous) rock units on the Atlantic Coastal Plain have been amply discussed by Sohl 

and Mello (in Owens and others, 1970). The marine 

faunas contain few ammonites, and many of the faunas 

contain long-ranging taxa or are of low diversity. 

Further, because of preservational factors, determinable mollusks are uncommon in many of the units. It was 

thought, therefore, that pollen studies might provide a 

supplementary and more consistent means of correlating these rocks. Some pollen assemblages had, in fact, 

been described from these rocks (Gray and Groot, 1966), 

but the described taxa were few, and some of the samples were obviously stratigraphically misplaced (Owens 

and others, 1970), particularly those from the 

Chesapeake and Delaware Canal.

In 1969 an extensive series of samples was collected 

for analysis. These samples, which were collected with 

the assistance of J. P. Minard, J. P. Owens, and N. F. 

Sohl, were supplemented with a few samples collected 

earlier by Owens and Sohl. The productivity of the samples was remarkable; of the 58 samples collected from 

these marine horizons, 57 contained determinable 

material. With the exception of the Tinton Sand, all the 

Campanian and Maestrichtian units have produced pollen assemblages. In addition, the assemblages of the 

upper part of the Magothy Formation have been preliminarily studied based on 17 samples; these samples 

are also of Campanian age.

For their advice and assistance on various aspects of 

this study, I wish to thank E. B. Leopold, J. P. Minard, 

J. P. Owens, N. F. Sohl, and R. T. Tschudy.

GEOLOGIC OCCURRENCE

In the Middle Atlantic States, the Campanian and 

Maestrichtian rocks occur in a belt extending from 

northeastern New Jersey south to the vicinity of 

Washington, B.C. (fig. 1). Studies of these rocks (Owens 

and others, 1970) indicate that the depositional history 

in the northern area the Raritan embayment (central 

and northern New Jersey) was somewhat different 

than in the southern area the Salisbury embayment 

(Maryland, Delaware, and southern New Jersey). Several of the units can be traced from one embayment to 

the other, but other rock units are present in only one 

embayment (fig. 2). Whether the absence of some lithostratigraphic units is due to facies changes and time 

transgressive phenomena cannot be certainly determined without resort to paleontologic work.

Older studies (for example, Clark, 1916) divided the 

Campanian and Maestrichtian rocks into two basic 

units: the Matawan Formation (or Group) and the 

Monmouth Formation (or Group), the Matawan of supposed Campanian age and the Monmouth of supposed 

Maestrichtian age. Further, the underlying Magothy 

Formation was considered to be of Turonian age and 

unrelated to these other units. From the east shore of 

Chesapeake Bay and north, Owens, Minard, Sohl, and 

Mello (1970) have shown that the subdivision into 

Matawan and Monmouth along the age-stage boundary
STRATIGRAPHIC DISTRIBUTION POLLEN, CAMPANIAN AND MAESTRICHTIAN ROCKS

PENNSYLVANIA

39'

76' 74°

FIGURE 1. General location of sampling sites in the Coastal Plain of the Middle Atlantic States. Numbers refer to USGS paleobotany

localities, details for which are given in the section on "Fossil localities."

is simplistic and that much of the "Monmouth" is, in 

fact, of Campanian age. Further, the upper part of the 

Magothy Formation (the Cliffwood beds and equivalent 

horizons) has been shown to be of probable earliest 

Campanian age (Wolfe and Pakiser, 1971). On the west 

shore of Chesapeake Bay, where mapping has not yet 

progressed to the stage where the units mapped by 

Owens, Minard, Sohl, and Mello (1970) can be recognized in most areas, the older terminology of Matawan 

and Monmouth is still applied.

About half the samples were collected from central 

and northern New Jersey and represent all the Campanian and Maestrichtian units except for the Mount

Laurel Sand (the one sample collected from this unit 

was barren) and the Tinton Sand. In eastern Maryland, 

Delaware, and southern New Jersey, all the units recognized by Owens, Minard, Sohl, and Mello (1970) produced pollen assemblages. On the west shore of 

Chesapeake Bay, the supposed Matawan was sampled, 

but, as discussed in the section on "Biostratigraphy," 

this Matawan is equivalent in age to part of the 

Navesink Formation and is thus assignable to the 

Monmouth.

The Campanian-Maestrichtian boundary recognized 

in this report (within the Navesink Formation) is based 

on the work of Sohl and Mello (in Owens and others,
BIOSTRATIGRAPHY

FIGURE 2. Generalized sections of the post-Magothy Cretaceous 

rocks of the Middle Atlantic States. A, New Jersey; B, Delaware 

and eastern Maryland; C, Western shore of Chesapeake Bay. 

Numbers indicate approximate stratigraphic position of 

localities. A and B modified from Owens and Minard (in Owens 

and others, 1970).

1970). Other workers, specialists in planktonic Foraminifera in particular, would place the boundary lower, 

probably at or near the base of the Mount Laurel Sand.

BIOSTRATIGRAPHY

Six major divisions are proposed for Campanian to 

lower Maestrichtian rocks of the Raritan and Salisbury 

embayments; the divisions are based on the stratigraphic ranges of dicotyledonous pollen (table 1). Four 

of these major divisions have recognizable subzones; 

thus a total of 10 informal biostratigraphic units are 

recognized. A sequence of informal palynologic zones for 

the Potomac Group and Raritan Formation, which has 

been proposed (for example, Brenner, 1963), are numbered sequentially in roman numerals. Although it 

might be desirable to continue the numbering sequence 

for the zones discussed in this report, the number of 

zones between the Raritan and Magothy Formations 

cannot now be determined and the Magothy pollen 

floras need further study to determine the zonation.

Considering the unknown number of zones that may

eventually be recognized between the Raritan Formation and the rock units of Campanian age, I have started 

a new numbering sequence prefixed by "CA," which 

stands for Campanian, and "MA," which stands for 

Maestrichtian. Subzones within the major zones are 

denoted by suffixes, for example, "A" for the lowest 

subzone. Zone 6, which is of both Campanian and Maestrichtian age, has the prefix CA-6/MA-1.

The fact that most zonal and subzonal boundaries 

proposed here are approximately coincidental with 

lithostratigraphic boundaries (table 1) may be a reflection of incomplete sampling across lithostratigraphic 

boundaries. For example, one of the most distinct assemblages, that of Zone CA-4, is based on samples from 

the middle part of the Englishtown Formation. Had the 

lower and upper parts of the Englishtown been sampled, 

Zone CA-4 might not appear as palynologically distinctive as described in this report. However, in the instance 

of the boundary between Zones CA-1 and CA-2, the 

assemblage from 11217-H at the top of the Magothy 

Formation is clearly distinct from that from 11218 at 

the base of the Merchantville; the latter assemblage, 

nevertheless, does have features intermediate between 

the uppermost Magothy assemblage and the assemblages from the middle part of the Merchantville 

(11219-A-F). The differences between the assemblages 

such as those from 11217-H and 11218 may reflect a 

definite hiatus; indeed, a sharp disconformity separates 

the Magothy and Merchantville (Owens and others, 

1970).

Zone CA-1 and older Magothy strata Pollen assemblages from the Magothy Formation have been discussed and partly illustrated elsewhere (Wolfe and 

Pakiser, 1971). Additional samples not reported on before have been studied to a limited extent, but the work 

has not progressed to the stage of presentation other 

than to indicate that the Magothy sequences in the 

Raritan embayment appear different than those in the 

Salisbury embayment. I emphasize that these suggestions may be premature. The Magothy sequence in the 

Raritan embayment (in descending order) appears to be: 

Cliffwood beds (Zone CA-1): Normapollesdominated assemblage that has some strong 

similarities to the Merchantville, particularly 

the basal Merchantville.

Morgan beds (Santonian): Similar to the 

Cliffwood, as well as to the Amboy stoneware 

clay.

Amboy Stoneware Clay Member (Santonian): 

Normapolles dominated, but greater diversity 

than in Morgan beds.

Old Bridge Sand Member (Coniacian?): Conifer 

dominated (bisaccates), low diversity of Normapolles (Pseudoplicapollis, Trudopollis,
STRATIGRAPHIC DISTRIBUTION POLLEN, CAMPANIAN AND MAESTRICHTIAN ROCKS

TABLE 1. Stratigraphic distribution of selected taxa of dicotyledonous pollen

SALISBURY EMBAYMENT POLLEN SPECIES

FORMATIONS AND

LOCALITIES

1 1 2 1 2 -H 

1 1 2 1 2 -G 

1 1 2 1 0 -E 

1 1 2 1 2 -F 

1 1 2 1 0 -D

Monmouth JJJlJlJ; 

Formation \\l\l_g

1 1 2 1 2 -C 

1 1 2 1 2 -B 

1 1 2 1 0 -B 

1 1 2 1 2 -A 

1 1 2 1 0 -A

Mount Laurel Sand 11233

Wenonah £ Formation 1121ii °

MarshaUtown l * 2 3 4 

Formation n2g()

11176 

Englishtown

F 

E

11231 °

B

A

Merchantville 

Formation

11174 

11173 

11172 

11156

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11228, 11229, 11232 

Magothy Formation

Plicapollis, Complexiopollis) and Trisectoris. 

In the Salisbury embayment, the Magothy samples 

from exposures in the Chesapeake and Delaware Canal 

and at Florence Bluffs contain assemblages that are 

very similar palynologically to the Cliffwood assemblages. The assemblages from the Magothy on the 

Severn River (a short distance from the type Magothy) 

are not directly comparable to any assemblages from

samples from the Raritan embayment Magothy. The 

Severn River Magothy has a low diversity of Normapolles types, although somewhat greater than in the Old 

Bridge. Unlike the low occurrences in the Old Bridge, 

Normapolles are common in the Severn River Magothy, 

along with an assemblage of tricolpate and triocolporate 

types; some of these types are found in the Amboy 

Stoneware Clay member. On this basis, I suggest that
BIOSTRATIGRAPHY

in the Campanian and Maestrichtian rocks of the Middle Atlantic States

POLLEN SPECIES RARITAN EMBAYMENT

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FORMATIONS AND 

LOCALITIES

11224 Red Bank Sand

C

B 11223

A

Navesink 

Formation

^ 11222

Mount Laurel Sand

C

B 11225 Wenonah

A Formation

7

Marshalltown

11351 Formation

C Englishtown 

B 11226 Formation

A

A 11221

Woodbury 

Clay

D

g 11227

A

G

F

E

D 11219

^ Merchantville 

Formation A

11218

11217, A-H 

Magothy Formation

SUB 

ZONE

B

__ ____

A

B

 _

A

B

A

B

A

ZONE

CA-6/MA-1

CA-5

CA-4

CA-3

CA-2

CA-1

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the Severn River Magothy (and probably the type section of the Magothy) represents the interval between 

the sampled Old Bridge and the sampled Amboy Stoneware. This in turn indicates the possibility that the 

Magothy Formation as now recognized in the Salisbury 

embayment may represent two units separated by an 

hiatus. The stratigraphy at the Salisbury embayment 

appears to be more complicated than heretofore

thought. It should be pointed out that the samples of 

Cliffwood age in the Salisbury embayment typically 

contain dinoflagellates and thus they may represent 

estuarine conditions. Marine mollusks, as well as dinoflagellates, occur in the Cliffwood beds at Cliffwood 

Beach, and dinoflagellates were found in some samples 

from the Morgan beds. 

Zone CA-2. Zone CA-2 encompasses the Mer-
6 STRATIGRAPHIC DISTRIBUTION POLLEN, CAMPANIAN AND MAESTRICHTIAN ROCKS

chantville Formation. A sample (11218) from the basal 

Merchantville immediately above the contact with the 

Cliffwood beds at Cliffwood Beach contains at least 10 

pollen species not yet found in samples from the 

Cliffwood beds (11217-A through G). This basal Merchantville sample, however, also contains three species 

that occur in the Cliffwood but not in other Merchantville samples. Particularly significant is the fact 

that, as in the Cliffwood samples, "Proteacidites" is lacking in 11218 but the probable pre-"Proteacidites" 

(NQ-1) is present. On this basis, the basal Merchantville beds at Cliffwood Beach, from which 11218 

was collected, are recognized as Subzone CA-2A, as 

distinguished from the Merchantville samples from the 

Oschwald pit (11219A through G), in which "Proteacidites" is present in most samples and NQ-1 is absent in 

all. Further, at least 12 species are found in the Oschwald Merchantville but not in 11218 or the Cliffwood 

beds. Analyses of samples from the interval between 

11218 and 11219-A (approximately middle part of Merchantville), might show the compositions between 

11218 and other Merchantville samples to intergrade.

The Merchantville Formation exposed in Maryland 

and Delaware was sampled at four localities (11172, 

11173, 11174, and 11231). The pollen assemblages from 

three of these localities (11172, 11173, 11174), correspond well with Subzone CA-2B. At 11231, (samples 

A-F) in the upper part of the Merchantville along the 

Chesapeake and Delaware Canal, the pollen assemblages do not correlate with the Oschwald Merchantville; as discussed below, these Merchantville 

samples that represent Zone CA-3, are from an age 

equivalent of the Woodbury Clay. Indeed, Owens, 

Minard, Sohl, and Mello (1970) indicate that along the 

Sassafras River, the Merchantville grades upward into 

the Englishtown Formation and the Woodbury Clay is 

absent. Such data clearly indicate that the age equivalent of the Woodbury Clay is here within either the 

Merchantville or the Englishtown, and the pollen data 

indicate that the Woodbury equivalent is within the 

Merchantville. More recently, Minard (1974, p. 20) has 

revised earlier concepts on the supposed pinching out of 

the Woodbury in southern New Jersey, proposing that 

the Woodbury is present (but coarser than to the north) 

and was erroneously included in the upper part of the 

Merchantville. The molluscan evidence within the Merchantville exposed in the canal section indicates that 

possibly the Woodbury Clay equivalent is absent (Sohl 

and Mello in Owens and others, 1970), but Sohl (oral 

commun., 1975) considers the molluscan data based on 

new collections to be equivocal in determining the presence or absence of a Woodbury equivalent.

A sample (11156) from the east shore of Maryland on 

Elk Neck is also from Subzone CA-2B. Although the

beds from which this sample was collected had previously been assigned to the Magothy Formation (Owens 

and others, 1970), the palynologic data strongly indicate an age equivalent of the Oschwald Merchantville. 

Owens (oral commun., 1975), moreover, states that the 

assignment of these Elk Neck beds to the Magothy was 

uncertain and that these beds could, on geologic 

grounds, represent either Merchantville or Englishtown, as well as Magothy.

Zone CA-3. This zone includes the Woodbury Clay 

of central and northern New Jersey and the upper part 

of the Merchantville Formation in the Salisbury embayment. At least 10 species occur in samples 11227 (A 

through D; lower part of Woodbury) and not in the 

Oschwald Merchantville (11219). An additional four 

species occur in samples 11221 (A and B; upper part of 

Woodbury) and not lower in the section. In addition, 

four species range from the Oschwald Merchantville up 

into the lower part of the Woodbury but not into the 

upper part. On this basis, the lower part of the Woodbury Clay is assigned to a subzone (CA-3A) distinct 

from that (CA-3B) of the upper part. In the upper part of 

the Merchantville exposed in the Chesapeake and Delaware Canal (locality 11231), samples A-D in particular bear a strong resemblance to assemblages characterizing Subzone CA-3A, whereas sample D and 

particularly sample E more closely resemble the assemblages from Subzone CA-3B.

Zone CA-4. Three samples (11226-A through C) 

from the middle part of the Englishtown Formation in 

the Raritan embayment and one sample (11176) from 

the Englishtown of the Salisbury embayment all closely 

resemble one another and concomitantly are highly dissimilar from samples from higher or lower units. Ten 

species are restricted to the Englishtown, eight have 

their lowest occurrence in this unit, and nine have their 

highest occurrence. According to Sohl and Mello (in 

Owens and others, 1970), the Englishtown Formation is 

probably of latest early Campanian age.

Zone CA-5. This zone includes the Marshalltown 

Formation, Wenonah Formation, and at least the lower 

part of the Mount Laurel Sand. More than 20 species 

have their lowest occurrence in this zone, whereas 11 

species that occur lower in the section have their last 

occurrence. Six species have their highest occurrence in 

the Marshalltown Formation, six have their lowest occurrence, and two are restricted to this unit; on this 

basis, the Marshalltown assemblages form the basis for 

Subzone CA-5A. An additional 10 species have their 

highest occurrence in the Wenonah or Mount Laurel, 

whereas six species have their lowest occurrences in 

these units, which are assigned to Subzone CA-5B. On 

the basis of present data, it would be difficult, if not 

impossible, to distinguish between the pollen as-
SIGNIFICANCE TO LITHOSTRATIGRAPHIC UNITS

semblages from the Wenonah Formation and the one 

assemblage from the lower part of the Mount Laurel. 

Indeed, Sohl and Mello (in Owens and others, 1970) 

suggest that the lower part of the Mount Laurel in the 

canal section (from which the one Mount Laurel pollen 

sample was obtained) may in fact represent the time 

equivalent of the Wenonah to the north in New Jersey. 

The pollen data are consistent with such an interpretation.

Zone CA-6IMA-1. This zone includes the Navesink 

Formation and at least the basal part of the Red Bank 

Sand in the Raritan embayment. In the Salisbury embayment, the Monmouth Formation exposed at Round 

Bay on the Severn River falls within this zone. At least 

18 species are known in this zone but not in lower zones; 

the upward extent of the ranges of many of these species 

is not known.

Subdivisions of this zone are not entirely satisfactory. 

A considerable number of species are known only in the 

Red Bank, but as only one Red Bank sample has been 

examined, the stratigraphic significance of these 

species (most of which are not discussed or illustrated in 

this report) is uncertain. The samples from the uppermost part of the Navesink closely resemble those from 

the lowermost part: of the 22 uppermost Navesink 

species, for example, 18 occur in the lowermost 

Navesink. Although reliance on a single lineage may be 

tenuous, NK-2 is consistently found through 11223-B 

in the uppermost Navesink, whereas NK-3 occurs in 

11223-C and in the Red Bank. Lending some support for 

a biostratigraphic division between 11223-B and 

11223-C is the fact that 11 species are known through 

11223-B but are not known in either 11223-C or the 

Red Bank. Although admittedly tentative, the uppermost Navesink sample and the Red Bank sample form 

the basis for Subzone CA-6/MA-1B (this subzone is, of 

course, entirely of Maestrichtian age), whereas the 

samples lower in the Navesink form the basis for Subzone CA-6/MA-1A.

The Monmouth Formation along Severn River contains several species that have not yet been found in the 

New Jersey section. Of the species common to both sections, the Severn River Monmouth clearly correlates 

with Subzone CA-6/MA-1 A. Four of the Severn River 

species are not known in the upper Navesink or Red 

Bank; three are not known in the lower Navesink or 

older samples. In general, the Monmouth Formation 

along Severn River would appear to be approximately 

equivalent to the middle part of the Navesink Formation, although age equivalents of both the upper (but not 

uppermost) and lower Navesink could be represented. 

The ammonite found in the upper part of the Severn 

River Monmouth is a species that, in New Jersey, is 

restricted to the upper Navesink and Red Bank.

SIGNIFICANCE TO 

LITHOSTRATIGRAPHIC UNITS

Owens and Minard (in Owens and others, 1970) consider that the Woodbury Clay of New Jersey thins 

southwestward and is absent in the Chesapeake and 

Delaware Canal section. Minard (1974) has revised this 

interpretation; he suggests that the Woodbury may lose 

its identity by a facies change to the south. The 

palynologic data indicate that beds of Woodbury age 

(Zone CA-3) are present in the canal section in the 

upper part of the Merchantville Formation, that is, the 

upper boundary of the Merchantville is timetransgressive (or the Woodbury Clay is a facies of the 

upper part of the Merchantville).

Along the Sassafras River, the upper part of the Merchantville (but not the uppermost part) contains assemblages assignable to Zone CA-2B. Possibly beds of 

Woodbury age are present here; this could be determined with certainty if the uppermost Merchantville 

were sampled.

Owens, Minard, Sohl, and Mello (1970) state that the 

Mount Laurel Sand in the Chesapeake and Delaware 

Canal grades downward into the Marshalltown Formation, the intervening Wenonah Formation having 

thinned out in southern New Jersey. The palynologic 

data could be interpreted to substantiate this conclusion; the assemblage from the lower part of the Mount 

Laurel in the canal assemblage does not differ significantly from the Wenonah assemblages. In order to substantiate this interpretation with certainty, it would 

first be necessary to determine if the Mount Laurel 

pollen assemblage in central and northern New Jersey 

were recognizably younger than the one assemblage 

from the Mount Laurel in the canal. Unfortunately, the 

one barren sample collected was from the Mount Laurel 

in northern New Jersey.

Owens and Minard (in Owens and others, 1970) indicate that the Navesink Formation thins southward 

from northern New Jersey and is absent in the section 

along the east shore of Chesapeake Bay. On the west 

shore, however, rocks equivalent in age to the Navesink 

are well represented along the Severn River. Further, 

although the upper part of the Merchantville along the 

Chesapeake and Delaware Canal is equivalent in age to 

the Woodbury Clay (Zone CA-2), to the west along the 

Sassafras River the upper part of the Merchantville is 

equivalent in age to the Merchantville of northern New 

Jersey (Zone CA-2); to this time, no rocks of Zone CA-3 

have been determined along Chesapeake Bay. As discussed earlier in this report, the Magothy Formation 

exposed along the Severn River appears to be older than 

the Magothy Formation exposed along the Chesapeake 

and Delaware Canal and in southern New Jersey. Finally, rocks in southern New Jersey and Maryland tra-
STRATIGRAPHIC DISTRIBUTION POLLEN, CAMPANIAN AND MAESTRICHTIAN ROCKS

ditionally assigned to the Raritan Formation have been 

shown to represent the uppermost part of the Potomac 

Group, and beds of an age equivalent to the Raritan 

Formation of northern New Jersey are apparently absent in outcrop in southern New Jersey, Delaware, and 

Maryland (Doyle, 1969; Wolfe and Pakiser, 1971). The 

depositional history of the Raritan embayment thus 

appears to be significantly different from the depositional history in the Salisbury embayment (particularly 

in the areas now adjacent to Chesapeake Bay).

CORRELATIONS WITH POLLEN ASSEMBLAGES 

FROM THE MISSISSIPPI EMBAYMENT

A large number of species of the Normapolles complex has been described by Tschudy (1975) based on material from the Mississippi embayment. Additionally, 

Tschudy has allowed me to compare the Atlantic Coastal Plain assemblages with illustrations of unpublished 

assemblage plates from various samples from the Campanian and Maestrichtian rocks of the embayment.

Two points of disagreement exist between the ages 

suggested here for the Mississippi embayment assemblages and the ages assigned to the assemblages by 

Tschudy (1975). First, the sampled Coffee Sand of Tennessee clearly correlates with the Englishtown Formation (Zone CA-4), whereas Tschudy (1975) assigned the 

Coffee Sand to the upper Campanian and considered his 

sample to be younger than samples from the Cusseta 

Sand Member of the Ripley Formation (Zone CA-5). 

Tschudy's sample (D3412) is stated to be from the middle part of the type section of the Coffee Sand; the 

suggested correlation of these rocks with the lower 

Campanian Englishtown Formation is in accordance 

with correlations proposed by Sohl (1964a, 1964b) and 

Sohl and Mello (in Owens and others, 1970). Sohl considers only the upper part of the Coffee Sand to be 

equivalent to the lower part of the Cusseta Sand 

Member, the remainder of the Coffee Sand being of 

early Campanian age. Second, Tschudy (1975) assigns 

the Coon Creek Tongue of the Ripley Formation to the 

Maestrichtian. The data in this report support the opinion of Sohl (in Owens and others, 1970) that the Coon 

Creek Tongue is of late Campanian age.

The placement of Tschudy's sample D3412 from the 

Coffee Sand in Zone CA-4 is based on the number of 

species in common. The following forms illustrated in 

this report also occur in D3412:

NA-1 (CA-3B CA-4)

NB-1 (CA-2A CA-4)

NC-1 (CA-2B CA-4)

ND-3 (CA-3A CA-5B)

NE-1 (CA-1 CA-5A)

NE-2 (CA-4 CA-5A)

NJ-2 (CA-4 CA6/MA-1A

NM-1 (CA-4 CA-5B)

NO-1 (CA-3B CA-5B)

CP3B-5 (CA-4)

CP3E-1 (CA-2B CA-5B

The overlap of ranges of several species concomitant 

with the occurrence of CP3B-5 indicate that D3412 is 

assignable to Zone CA-4.

The following species occur in D3260 from the upper 

part of the Cusseta Sand Member of the Ripley Formation in Alabama:

NA-8 (CA-5B CA-6/MA-1B

NE-3 (CA-5A-CA-6/MA-1A)

NF-4 (CA-4 CA-5B)

NR-1 (CA-5A)

PR-7 (CA-4 CA-6/MA-1B)

MPH-1 (CA-5A CA-5B)

This assemblage is clearly indicative of Zone CA-5; Sohl 

and Mello (in Owens and others, 1970) correlate the 

Cusseta Sand member with the Marshalltown and 

Wenonah Formations and the lower part of the Mount 

Laurel Sand, a correlation in agreement with that 

suggested here. Which subzone of Zone CA-5 D3260 

should be placed in is not certain; NR-1 would indicate 

Subzone CA-5 A, but the occurrences of this species are 

so uncommon that I would prefer to rely on the range of 

NA-8 and suggest that D3260 is from beds correlative 

with the Wenonah Formation or the lower part of the 

Mount Laurel Sand. In fact, NR^-1 is known in probable 

CA-5B or CA-6/MA-1A samples in the Mississippi 

embayment.

Sample D3413 from the Cook Creek Tongue of the 

Ripley Formation in Tennessee contains the following 

species:

NA-3 (CA-5B)

NA-8 (CA-5B CA-6/MA-1B)

NC^2 (CA-2A CA-5B)

NE-3 (CA-5B CA-6/MA-1B)

NN-1 (CA-4 CA-5B)

NO-2 (CA-5A CA-5B)

NT-1 (CA-5B CA-6/MA-1A)

CP3F-2 (CA-5B CA-6/MA-1B)

The co-occurrence of these species is indicative of Subzone CA-5B; that is, this part of the Cook Creek Tongue 

is correlative with either the Wenonah Formation or the 

Mount Laurel Sand. Sohl (1964a) and Sohl and Mello (in 

Owens and others, 1970) correlate the Coon Creek in 

Tennessee with the Mount Laurel Sand and the uppermost part of the Wenonah Formation.

The McNairy Sand Member of the Ripley Formation 

has yielded specimens of NN-2 (CA-6/MA-1A and B) at 

locality D3358 and NA-8 (CA-5B-CA-6/MA-1B), 

NG-1 (CA-6/MA-1A), NK-2 (CA-6/MA-1A), and 

MPH-2 (CA-6/MA-1A) at locality D1967. The correlation indicated is of the bulk of the Navesink Formation
PALEOECOLOGY 9

with the McNairy Sand Member; that is, the McNairy 

can be assigned to Subzone CA-6/MA-1A. Sohl (1964a) 

also correlated the McNairy with the bulk of the 

Navesink.

The type locality of the Owl Creek Formation (D3410) 

contains the following species:

NH-1 (CA-6/MA-1A)

NK-3 (CA-6/MA-1B)

NO3 (CA-6/MA-1A and B)

PR-7 (CA-4 CA-6/MA-1B)

The assignment to Zone CA-6/MA-1 is clear, and probably locality D3410 is in Subzone B of this zone. The 

occurrence of NK-3, which is thought to be descended 

from NK-2 in Subzone A, is considered to be more significant than the occurrence of NH-1.

The basic similarity of the Atlantic Coastal Plain and 

Mississippi embayment pollen sequences from Zone 

CA-4 through Zone CA-6/MA-1B is strong evidence of 

the overall validity of the proposed zonation. It would, 

however, be desirable to sample the Mississippi embayment section in more detail, particularly in the Coffee Sand; presumably, the lower part of this unit would 

produce assemblages assignable to Zones CA-1 through 

CA-3. The correlations suggested here are in consistent 

agreement with those suggested by Sohl and Mello (in 

Owens and others, 1970, fig. 23).

CORRELATIONS WITH POLLEN ASSEMBLAGES 

FROM THE CAPE FEAR ARCH

Sampling of the Cretaceous units of North Carolina 

has been extremely limited; thus far, only two productive samples both from the Black Creek Formation 

have been analyzed. The oldest sample, D5019 from 

Walker's Bluff on the Cape Fear River, contains the 

following species:

NB-1 (CA-2A CA-4)

ND-3 (CA-3A CA-5B)

C3A-1 (CA-2A CA-4)

CP3B-3 (CA-3A and B)

The placement of this sample is in Zone CA-3, although 

it cannot be determined which subzone is represented. 

The second sample, D5018 from Jessup's Landing on the 

Cape Fear River, contains the following species:

ND-3 (CA-3A CA-5B)

NE-3 (CA-5A CA-6/MA-1B)

NN-1 (CA-4 CA-5B)

PR-7 (CA-4 CA-6/MA-1B)

C3B-3 (CA-5A CA-6/MA-1B)

This sample is assignable to Zone CA-5, but, as with the 

other Black Creek sample, the assemblage is too small 

to determine which subzone is represented. Nevertheless, the palynologic data are consistent with the invertebrate evidence (Sohl and Mello in Owens and others, 

1970), which indicates that the Black Creek Formation

contains correlatives of the Woodbury Clay (Zone CA-3) 

and Marshalltown and Wenonah Formations (Zone

CA-5).

PALEOECOLOGY

Most of the angiospermous pollen types found cannot 

be related with certainty to extant families or even 

orders, and this makes paleoecological interpretations 

based on distributions of extant related taxa of little 

value. One aspect of the various samples is notable: the 

percentages of bisaccate pollen in both the Raritan embayment and Salisbury embayment sections seem to 

fluctuate sharply (fig. 3). The bisaccate pollen represents various coniferous genera, particularly those included in Podocarpaceae and Pinaceae.

Two periods of deposition of abundant bisaccate pollen are apparent: one during Woodbury time (Zone 

CA-3) and another during Marshalltown through part 

of Navesink time (Zone CA-5 through part of CA-6/ 

MA-1A). In contrast during Cliffwood and Merchantville time (Zones CA-1 and CA-2) and Englishtown time (Zone CA-4), representation of bisaccate 

pollen is low to moderate whereas pollen of the Normapolles complex is well represented. Apparently 

another period of low bisaccate representation began in 

the upper part of the section during Navesink time.

The fluctuations in relative abundance of bisaccate 

pollen and Normapolles pollen have no obvious relation 

to the sedimentary cycles proposed by Owens and 

Minard (in Owens and others, 1970). For example, the 

Merchantville and Marshalltown Formations both represent the initial transgressive phase of their respective 

cycles, but the former has only a moderate representation of bisaccate pollen and the latter has a high representation of this type of pollen. A second example is 

that the Mount Laurel (high bisaccate) and Englishtown (low bisaccate) both represent the closing phase of 

their respective cycles. These examples indicate that 

factors such as water depth or distance from shore have 

little, if any, bearing on the pollen fluctuations.

If the sedimentary cycles have no relation to the pollen fluctuations, then possibly the fluctuations represent climatic changes, with the high bisaccate periods 

representing cool intervals relative to the low bisaccate 

periods. Such fluctuations in climate could represent 

the same series of cycles suggested for the Tertiary 

(Wolfe, 1971). In order to test this hypothesis, I calculated backward from the well-documented cooling that 

occurred about 32 m.y. ago, assuming that each complete cycle had a duration of 9.5 m.y. (Wolfe, 1971) and 

that a warm period of a given cycle had the same duration as a cool period of that cycle. The predicted ages of 

the warm and cool periods are given in table 2, as are the 

radiometric ages on the various rock units (Owens and
10 STRATIGRAPHIC DISTRIBUTION POLLEN, CAMPANIAN AND MAESTRICHTIAN ROCKS

11217

Raritan embayment 

Bisaccate conifers Normapolles

Zone or subzone 

CA6/MA-1B

Salisbury embayment 

Bisaccate conifers Normapolles

FREQUENCY, IN PERCENT

FIGURE 3. Relative abundance of certain major pollen types in the Campanian and Maestrichtian rocks of the Middle Atlantic States. 

Based on counts of 200 pollen grains per sample. Lined areas, the podocarpaceous Rugubivesiculites; shaded areas, structurally 

simpler Normapolles types.

Sohl, 1973). The agreement between the predicted and 

radiometric ages is extremely close and is certainly 

within the experimental error of the radiometric ages. It 

should be noted that the Magothy assemblages typically 

have a low bisaccate representation, except for the Old 

Bridge Sand Member assemblages from the base of the 

Magothy. The Old Bridge, then, would apparently be 

about 84 m.y. old the age predicted for the end of the 

next oldest cool period.

The percentages of bisaccate and Normapolles pollen

could be used in a general manner to indicate age in 

local correlations. High Normapolles representation, 

for example, occurs only in CA-4 and in CA-2 and older 

beds. Another trend in these samples is the increasing 

proportion of structurally simpler types of Normapolles 

relative to the more complex types (for example, Pseudoplicapollis, Trudopollis, Plicapollis, Endoinfundibulapollis). This increase is particularly apparent between 

Zones CA-4 and CA-5 and continues during the supposed cool period of Zone CA-5. One possible explana-
SIGNIFICANT POLLEN TYPES 11

TABLE 2. Comparison of ages predicted on the basis of climatic cycles with radiometric ages in 

Campanian and Maestrichtian rocks of the Middle Atlantic States

[Radiometric ages from Owens and Sohl 119731].

Climate Rock unit (or subdivision) Predicted age Radiometric ages 

im.v.l (m.y.l

Red Bank Sand

Warm Navesink Formation, upper part 

Navesink Formation, middle part

Cool

Warm

Cool

62.8±2.2, 63.2±1.9

65.3

Navesink Formation, lower part 

Mount Laurel Sand 

Wenonah Formation 

Marshalltown Formation 68.2±2.4, 71.4±2.5

Warm

Cool

Englishtown Formation

Woodbury Clay

fU.U

7/1 Q

7Q Z

74.0±2.5

Merchantville Formation

Cliffwood beds of Magothy Formation

Morgan beds of Magothy Formation 

Amboy Stoneware Fire Clay Member 

of Magothy Formation

80.7±4.0, 81.2+2.6

84.3

Old Bridge Sand Member of 

Magothy Formation

tion is that, contrary to earlier speculation (Wolfe, 

1973), the cooler climate of Zone CA-5 was an impetus 

to the rise of the wind-pollinated amentiferous groups 

from the Normapolles stock; at least some of the simpler 

Normapolles types can be related to some extant amentiferous groups (see discussion of types NK and NN on 

page 13).

SIGNIFICANT POLLEN TYPES

Rather than enter into the controversial area of 

nomenclature of fossilized pollen, I have chosen to adopt 

an expedient course of coding most of the pollen types. 

Where previously described genera and species can be 

recognized, the probably formal designation has been 

pointed out. As Hughes (for example, Hughes and 

Moody-Stuart, 1967) has exhaustively pointed out, 

there has been a definite tendency for palynologists to 

apply previously published names to new material that, 

to a greater or lesser extent, differs from the type specimen or suite on which the names are based. This, in 

turn, has led to apparently broad stratigraphic ranges, 

not of great use in biostratigraphy. I readily admit that 

some of the "code species" distinguished in this report 

may not be of specific rank to some palynologists, but 

the recognition of minor differences that appear to be 

correlative with stratigraphic differences will, I hope, 

make this report of more value to palynologists interested in stratigraphy.

In this section of the report, the pollen types of apparent stratigraphic, biogeographic, or evolutionary 

significance are discussed. The pollen types have been

broken down into several major categories: the Normapolles complex (N), tricolpates (C3), tricolporates 

(CP3), "Proteacidites" (PR), and miscellaneous pollen 

types (MP). A letter immediately following the above 

designations indicates that two or more genera are 

taken to have been included in the overall designation 

and the letters represent different genera. The number 

following the dash indicates the different pollen species.

Not all the pollen types found in the current study are 

discussed here or illustrated. Fern spores have been 

ignored, and most gymnospermous and monocotyledonous pollen; and though 104 dicotyledonous pollen types 

are discussed and figured, at least an equal number that 

were photographed in the surveys were found to be 

typically rare and therefore ignored.

Type NA (Basopollis and Choanopollenites). These 

two genera are characterized by the presence of a distinct mesopore and a broad endopore; the wall complex 

forming the mesopore protrudes toward the exopore. In 

erecting Choanopollenites, Stover (in Stover and others, 

1966) noted that Basopollis had a vestibulum, and, by 

inference, Choanopollenites does not. From Stover's 

figure la on plate 5, a distinct (albeit weak) endopore is 

apparent, and thus Choanopollenites does, in fact, possess a vestibulum. The only feature distinguishing the 

two genera is that the wall complex forming the mesopore is thickened at the mesopore in Choanopollenites, 

whereas the probably homologous wall complex in 

Basopollis is of uniform thickness. Were I considering 

formal nomenclatorial problems in this report, I would
12 STRATIGRAPHIC DISTRIBUTION POLLEN, CAMPANIAN AND MAESTRICHTIAN ROCKS

consider Choanopollenites a junior synonym of 

Basopollis.

Type NA-1 (pi. 1, fig. 1) is closely similar to 

Choanopollenites discipulus R. Tschudy from the late 

Maestrichtian and Paleocene of the Mississippi embayment (Tschudy, 1975). The Atlantic Coastal Plain 

species, however, has a larger atrium, and the walls 

forming the exopore are less thickened and less protruding than in C. discipulus. Type NA-1 occurs in the 

Woodbury and Englishtown. Tschudy (1973) suggested 

that C. discipulus was derived from C. transitus R. 

Tschudy, which in turn was derived from some species of 

Complexiopollis. The Atlantic Coastal Plain sequence, 

however, indicates that the C. discipulus type is in fact 

older than the C. transitus type. Whether Choanopollenites is directly derived from any type of Complexiopollis is, I think, open to question. Choanopollenites has an 

apertural structure fundamentally similar to that of 

Basopollis, which, as Goczan, Groot, Krutzsch, and 

Pacltova (1967, p. 487) have shown, is most similar to 

that ofPlicapollis. Further, Complexiopollis abditus R. 

Tschudy, one of the possible ancestors for Choanopollenites suggested by Tschudy (1973), is fundamentally 

different from both Complexiopollis and Choanopollenites. This species has equatorial thickenings of the 

outer wall layer that extend toward the poles (so-called 

arci), and these thickenings form the exopore (this is 

evident from Tschudy's photographs), not the mesopore 

(as misinterpreted in Tschudy's text-fig. 5); this species 

is common in the Merchantville and Woodbury (see 

discussion of type NB on page 00).

Type NA-2 (pi. 1, fig. 2) is similar to NA-3 (pi. 1, fig. 3; 

Choanopollenites transitus R. Tschudy) except that the 

outer wall is of consistent thickness, that is, there is no 

tendency for the wall to be enlarged around the exopore. 

Type NA-2, which is confined to the Englishtown and 

Marshalltown, is apparently ancestral to NA-3. Type 

NA-3 ranges from the Marshalltown-Wenonah transition through the middle part of the Navesink. Type 

NA-4 (pi. 1, fig. 4) is known only from the uppermost 

part of the Severn River Monmouth; this type has the 

mesopore extending almost to the inner part of the exopore (and hence the atrium is extremely small), bulbous, protruding ambs, and is larger than NA-2 and 

NA-3. Tschudy (1973, figs. 9-13) illustrated grains from 

the Paleocene Clayton Formation that conform to 

NA-4.

Type NA-5 (pi. 1, fig. 5) has been found in only one 

sample from the upper part of the Severn River Monmouth. Except for its smaller size, NA-5 is similar to 

Choanopollenites sp. A of Tschudy (1973), which is 

known from the Paleocene Clayton Formation. Type 

NA-5 is perhaps ancestral to this Tertiary species.

Type NA-6 (pi. 1, fig. 6) from the Merchantville is the

oldest known Choanopollenites. The more rounded 

ambs, larger atria, and more conspicuous radial baculae 

distinguish NA-6 from NA-2. NA-7 (pi. 1, fig. 7) from 

the Englishtown has thickened walls forming the exopore, and radial baculae are very indistinct. Similar to 

NA-7 but with conspicuous radial baculae is NA-8 (pi. 

1, fig. 8; Wenonah through Red Bank.) Type NA-8 also 

resembles C. conspicuus (Groot and Groot) R. Tschudy, 

but C. conspicuous is larger and has a narrower mesopore.

Type NB. As discussed above, this type is probably 

not closely related to Complexiopollis. Type NB-1 (pi. 1, 

fig. 9; basal Merchantville through Englishtown) compares well with "Complexiopollis" abditus R. Tschudy. 

Although Tschudy (1973) cited the range of "C." abditus 

as Coniacian through upper Campanian, Wolfe and 

Pakiser (1971) indicated that the Eutaw Formation, 

from which Tschudy's "Coniacian" sample came, is of 

Santonian through earliest Campanian age, and Sohl 

(in Owens and others, 1970) indicated that the Coffee 

Sand, from which Tschudy's "late Campanian" sample 

came, is of early Campanian age.

Type NB-2 (pi. 1, fig. 10) has, in the present study, 

been found only in the basal Merchantville. Wolfe and 

Pakiser (1971, fig. 5-m), however, reported the same 

form from the Cliffwood beds of the Magothy Formation. 

Type NB-3 (pi. 1, figs. 11, 12) differs from NB-2 by 

having the thickenings of the wall extend farther toward the poles; NB-3 closely resembles "Complexiopollis" microuerrucosus R. Tschudy, except that the latter 

has the walls thickened around the exopore. Possibly 

NB-3 is descended from NB-2; NB-3 is known from the 

upper part of the Merchantville through the upper part 

of the Severn River Monmouth.

Type NC (Pseudoplicapollis). At least three basic 

types of NC can be distinguished. Type NC-1 (pi. 1, fig13), which occurs from the Merchantville through the 

Englishtown, is characterized by a thickened wall surrounding the exopore; type NC^2 (pi. 1, fig. 14; Merchantville through Wenonah), which was described by 

Tschudy (1975) as P. endocuspis, has little or no enlargement of the wall around the pore, and also has less 

conspicuous plicae than NC-1. Type NC-3 (pi. 1, fig. 15) 

has no enlargement of the wall around the pore, very 

weak plicae, and a broad vestibulum; this type ranges 

from the Merchantville through the Severn River 

Monmouth.

Type ND. This Normapolles type falls outside of the 

bounds of previously described genera as circumscribed 

by Goczan, Groot, Krutzsch, and Pacltova (1967). Type 

ND is particularly close to Plicapollis but differs in that 

the endopore is V-shaped or U-shaped inwardly. Type 

ND-1 (pi. 1, fig. 16) is larger than ND-2 (pi. 1, fig- 17) 

and has distinct sculpturing in contrast to the almost
SIGNIFICANT POLLEN TYPES 13

psilate condition in ND-2. ND-1 is rare in the Merchantville through Englishtown; ND-2 is rare but is 

restricted to the Marshalltown and Wenonah.

Type ND-3 (pi. 1, fig. 18) typically has weakly developed Y-shaped thickenings and a broadly U- or 

V-shaped endopore. This species is common from the 

Woodbury through the Wenonah.

Type (NE) Plicapollis. Several distinct types ofPlicapolis have been recognized, but only four appear to be of 

common occurrence. Type NE-1 (pi. 1, fig. 19;P. rusticus 

R. Tschudy) is common from the Magothy through the 

Woodbury and occurs up into the Marshalltown. Type 

NE-2 (pi. 1, fig. 20; P. retusus R. Tschudy) has been 

found only in the Englishtown and Marshalltown, and 

type NE-3 (pi. 1, fig. 21; P. usitatus R. Tschudy) ranges 

from the uppermost Marshalltown through the 

Navesink and the Severn River Monmouth. From this 

stratigraphic distribution, it is tempting to suggest that 

NE-1 is the type ancestral to at least NE-3, which 

differs primarily by its smaller size and thinner walls.

Type NE-4 (pi. 1, fig. 22) differs from NE-1 by its 

smaller size, thin walls, and round body. Type NE-2 has 

conspicuous radial baculae on the interior of the exopore. Type NE-4 is most similar to NE-3, but NE-3 has 

a considerably larger atrium. Although NE-4 technically conforms to Plicapollis in pore structure, in other 

characters it closely resembles Pseudoplicapollis (type 

NC) and may be a species of this genus that has converged with Plicapollis. To this time NE-4 is known 

only from the lower part of the Merchantville.

Types NF (Trudopollis) and NM (Endoinfundibulapollis). NF (Trudopollis) and NM (Endoinfundibulapollis) are treated together because they are linked by 

intermediate forms. Type NF-1 (pi. 1, figs. 23,24) has an 

endopore of varying width, and in some specimens (particularly from the higher part of the Merchantville; pi. 

1, fig. 24) the vestibulum is large, apparently as a result 

of the collapse of the inner wall(s) inward into the grain. 

In NF-2 (pi. 1, fig. 25; restricted to the Woodbury), the 

wall around the exopore is considerably thinner (as is 

the wall elsewhere) than in NF-1, and the inner wall(s) 

is pulled even more inward. In NM-1, (pi. 1, fig. 26), 

which represents Tschudy's (1975) type species ofEndoinfundibulapollis, found from the Englishtown through 

the Wenonah, the vestibulum is consistently larger 

than in NF-2.

Type NF-3 (pi. 1, fig. 27) appears to represent a 

distinct Trudopollis, but one that has no obvious ancestral type lower in the section. NF-3 has been found only 

in the Mount Laurel.

Type NF-4 (pi. 1, fig. 28) is rare in the Englishtown 

and Wenonah. In shape, size, and sculpturing, this 

species appears to fall within Trudopollis variabilis R. 

Tschudy.

Type NG Pseudatlantopollis. Type NG (pi. 1, figs. 

29,30) appears to fall near Pseudatlantopollis simulatus 

R. Tschudy. Tschudy, however, stated that the size 

range of this species is 20-26 /xm (based on 35 specimens), whereas the two Navesink specimens are 29 and 

32 /xm. The size difference, coupled with the somewhat 

rounder shape of the Navesink grains, may indicate 

that the Navesink species is new.

Type NH (Interpollis). This species was included by 

Tschudy (1975) as Interpollis cf./. supplingensis. None 

of the specimens from the Severn River Monmouth display an equatorial constriction and all possess a thickened endopore; this morphologic consistency in the 

Maryland material indicates that Tschudy's (1975) 

specimens figured on plate 4, figures 14, 15, probably 

represent a species different from the other specimens 

he referred to /. cf. I. supplingensis.

Whether NH-1 (pi. 1, fig. 35) could be validly referred 

to Interpollis is highly questionable. The facts that arci 

are absent and that it lacks an equatorial constriction 

indicate that NH- probably represents a distinct genus. 

Although both NH-1 and Interpollis have subequatorial 

pores, other Normapolles genera and derivatives have 

this tendency. It seems clear that Carya has developed 

subequatorial pores independently, and that this 

character, in itself, is not an indication of close relationship.

Type NI. This Normapolles type has a pronounced 

Y-shaped polar thickening that enlarges into occuli 

around the pores. Of previously described genera, NI is 

apparently closest to Bohemiapollis but lacks the long, 

narrow canal of the exopore. NI-1 (pi. 1, figs. 31, 32) 

occurs in the basal Merchantville and in the Woodbury, 

whereas NI-2 (pi. 1, figs. 33, 34) occurs in the Englishtown. NI-2 differs by having a smaller atrium and 

exopore.

Type NJ (Extremipollis). One Woodbury sample 

contains a small type of Extremipollis (NJ-1; pi. 2, fig., 

1), the oldest known in North America or Europe. The 

larger E. vivus R. Tschudy (NJ-2; pi. 2, fig. 2) occurs 

from the Englishtown through the upper part of the 

Navesink.

Type NK. Goczan, Groot, Krutzsch, and Pacltova 

(1967) have suggested that certain structures in the 

grains of the extant Rhoiptelea are homologous with 

similar structures in the Normapolles genus Complexiopollis; by inference, therefore, Rhoipteleaceae 

and the allied Juglandaceae could be considered as relicts of the Normapolles complex. Wolfe (1973) 

suggested that certain pollen grains from the Severn 

River Maestrichtian were assignable to Rhoipteleaceae 

and Juglandaceae and had features indicative of a derivation from the Normapolles complex. Further study 

has now indicated the strong probability that both ex-
14 STRATIGRAPHIC DISTRIBUTION POLLEN, CAMPANIAN AND MAESTRICHTIAN ROCKS

tant families of Juglandales are, in fact, derivatives 

from certain Normapolles types.

A pollen type (NK-1 pi. 2, fig. 3) restricted to the 

Marshalltown, Wenonah, and Mount Laurel, is of definite Normapolles affinities, as indicated by the radial 

baculae on the interior of the exopore. These grains 

appear to be structurally less complex than Trudopollis, 

which also has a somewhat thicker wall (particularly at 

the exopore), larger vestibulum, and a narrower endopore. Type NK-1 has a polar thinning on one hemisphere; this thin area is more conspicuous on grains with 

somewhat thicker walls.

Grains (NK-2; pi. 2, fig. 4) from the Severn River 

section of the Monmouth Group are slightly less aspidate than in NK-1, lack radial baculae on the interior of 

the exopore, and have a somewhat thinner wall although the same type of conspicuous polar thinning is 

consistently present. Type NK-2 is similar to type 

NK-3 in the uppermost Navesink and Red Bank. NK-3 

differs by being smaller than NK-2 and having thinner 

walls. Pollen grains from the Paleocene of the Mississippi embayment that are perhaps the same entity as 

NK-3 (pi. 2, fig. 5) have been assigned to the extant 

Engelhardtia (for example, Elsik, 1968). I consider that 

the types NK-1, NK-2, and NK-3 represent a series 

transitional from the Normapolles complex (from 

Trudopollis or a close relative) to Juglandales.

TypeNL (Praebasopollis). TypeNL-1 (pi. 2, fig. 6) is 

confined to the lower Merchantville but is especially 

common in 11218. The bulbous pores are particularly 

characteristic of this species. Type NL-2 (pi. 2, fig. 7) 

from the Woodbury has less bulbous pores.

Type ATM. See type NF.

Type NN. Pollen type NN, which occurs from the 

Englishtown through the Mount Laurel, is characterized by the Y-shaped polar thickening, thick walls, 

and an exopore that has radial baculae on the interior. 

Except for the difference in structure of the wall in the 

polar area, NN-1 (pi. 2, fig. 8) is highly similar to NK-1 

(pi. 2, fig. 3). Type NN-2 (pi. 2, fig. 9), which occurs in the 

Navesink, Red Bank, and Severn River Monmouth, 

lacks radial baculae, has a smaller and rounder exopore, 

and has thinner walls than NN-1. As pointed out previously (Wolfe, 1973), the type represented by NN-2 is 

probably assignable to Rhoipteleaceae.

If, as suggested here, types ancestral to Juglandaceae 

and Rhoipteleaceae have Normapolles characteristics, 

then clearly some true Normapolles must be members of 

Juglandales. That is, both NK-1 and NN-1 would have 

had a common ancestor and that ancestor must be 

within Juglandales if this order is a clade rather than a 

grade.

Type NO (Osculapollis). Type NO-1 (pi. 2, fig. 10) 

conforms well to Osculapollis aequalis R. Tschudy. This

is a common species from the Englishtown through the 

Mount Laurel. A more rotund form of Osculapollis 

(NO-2 pi. 2, fig. 11) that has pronouncedly aspidate 

pores occures in the Marshalltown through Mount 

Laurel. A form (NO-3; pi. 2, fig. 12) similar to NO-2 

occurs in the Navesink through Red Bank and in the 

Severn River Monmouth; this form differs from NO-2 

by being smaller. NO-4 (pi. 2, fig. 13) is the oldest record 

of the genus; this basal Merchantville species is similar 

to O. perspectus R. Tschudy but has a smaller atrium 

and tends to have more aspidate exopores.

Type NO-5 (pi. 2, fig. 14; Wenonah) is a polyporate 

(5-7 pores) that has the basic pore structure of Osculapollis. Conceivably NO-5 is a variant of NO-1, but 

NO-1 occurs abundantly in several other samples in 

which NO-5 is lacking.

Type NP. This genus has pollen that is decidedly 

triangular in polar view with a broadly rounded amb. 

The outer and inner wall layers are of approximately 

equal thickness; the wall forming the endopore is ragged in the region of the pore. Type NP-1 (pi. 2, fig. 15) is 

thick-walled compared with the other species of the 

genus; this type is confined to the Marshalltown. NP-2 

(pi. 2, fig. 16), in the Wenonah, has markedly thinner 

walls. Forms assigned to NP-2 in the Navesink and 

Severn River Monmouth are somewhat smaller than 

NP-2 in the Wenonah.

Type NQ. Pronounced sculpturing is unusual for the 

Normapolles complex but is known in a few genera. 

That NQ (pi. 2, figs. 17-19) is indeed a Normapolles type 

is clear from the equatorial thickenings of the outer 

wall; the structure of this wall and the relation to the 

exopore are similar to NB. Type NQ, however, has a 

definite thickening of the exopore on the poleward parts 

of the slitlike aperture. The sculpturing in NQ tends to 

be irregular; some grains are uniform, others show a 

tendency for a gradation in size of the lumina from pole 

to equator.

The sculpturing in "Proteacidites" (or as this name is 

applied to many grains from the Northern Hemisphere) 

is typically thought to be gradational, from smaller luminae at the poles to larger luminae at the equator. In 

fact, some of the "Proteacidites" higher in the Coastal 

Plain section (see below) have uniform sculpturing and 

some have highly reduced sculpturing. The variability 

in sculpturing exhibited by these "Proteacidites" is similar to that exhibited by NQ. Perhaps the primary distinguishing feature of "Proteacidites" is the formation 

by the inner wall of a collar (or annulus) at the pore. 

Some specimens of NQ also have a tendency for the 

formation of a collar, although the collar does not completely envelop the pore. The similarities of NQ to both 

the Normapolles complex and to "Proteacidites" is here 

interpreted to indicate that, as Tschudy (1971) has
SIGNIFICANT POLLEN TYPES 15

suggested, at least some of the Northern Hemisphere 

supposed proteaceous grains are derivatives of the 

Normapolles complex and are not closely related to Proteaceae. Martin (1973) has shown that forms from the 

Southern Hemisphere that superficially resemble extant Proteaceae have been invalidly considered to be of 

proteaceous affinities.

Type NR (Pseudoccupollis). A single grain (NR-1; 

pi. 2, fig. 20) compares well with Pseudoccupollis admirabilis R. Tschudy, which is known from the upper 

Campanian of the Mississippi embayment. The New 

Jersey occurrence (Marshalltown) is in the same 

stratigraphic range; in Europe, the genus is known only 

from the Santonian and lower Campanian (Goczan and 

others, 1967).

TypeNS (Longanulipollis). NS-1 (pi. 2, fig. 21) from 

the Englishtown is the sole known representative of 

Longanulipollis in North America. This occurrence is 

apparently somewhat older than known occurrences of 

the genus in Europe (late Campanian-Maestrichtian). 

The North American species is, except for its smaller 

size, closely similar to the type species of the genus, L. 

longianulos (Gocz.) Gocz.

Type NT (Pseudovacuopollis). Tschudy (1975) records Pseudovacuopollis involutus (NT-1; pi. 2, fig. 22) 

from several samples from the Mississippi embayment 

(late early Campanian through Maestrichtian). Thus 

far, this species has been encountered in two Atlantic 

Coastal Plain samples which came from Marshalltown-Wenonah transition and the upper part of the 

Navesink.

Type NU. This type is one of the simpler Normapolles. The outer and inner walls are of about the same 

thickness and are thin. The pores are slightly aspidate 

and slit-shaped. Only a trace of sculpturing is present on 

the inner wall of the exopore. This species (NU-1; pi. 2, 

fig. 23) is known from the Englishtown through the 

Marshalltown-Wenonah transition.

Type NV. This presumed Normapolles type has the 

most simplified pore structure of the younger forms of 

NK and NN. The Y-shaped polar thickening in NN, 

however, has arms oriented towards the pores, whereas 

in NV-1 (pi. 2, fig. 24; Wenonah and Severn River 

Monmouth) the arms are oriented between the pores.

Type PR ("Proteacidites"). As discussed above, the 

pollen from the Atlantic Coastal Plain Cretaceous that 

is typically assigned to Proteacidites is probably a derivative of the Normapolles complex. Despite extensive 

search in over 40 samples from the Magothy Formation, 

no pollen of the type discussed below has been found, 

and this type is also missing from the sample from the 

basal Merchantville.

PR-1 (pi. 2, fig. 25) is characterized by a wide pore 

that has a thin collar; this type, the most wide-ranging,

is found from the Merchantville through the Navesink. 

PR-2 (pi. 2, figs. 26, 27) from the Merchantville has a 

narrower, more elongate pore that has a conspicuous 

collar; also, the wall layers are well differentiated. This 

differentiation may be a retention of a feature characteristic of the Normapolles complex. PR-3 (pi. 2, fig. 28) 

from the Englishtown has the coarsest sculpturing of 

these "Proteacidites." PR-4 (pi. 2, fig. 29) from the 

Wenonah has an elongated collar around the pore; this 

type is somewhat similar to PR-2 but has thinner walls 

and more distinct sculpturing. PR-5 (pi. 2, fig. 30) from 

the Navesink is a small, indistinctly sculptured grain 

that has thin walls and an elongated collar around the 

pore. PR-6 (pi. 2, fig. 31) from the Englishtown has a 

conspicuous collar around the pore but the sculpturing 

is most reduced of any of these species. PR-7 (pi. 2, fig. 

32) from the Englishtown through the Navesink has a 

pronounced collar around the pore and the sculpturing 

is fine but distinct.

Type C3A. Included in this type are grains that are 

circular in polar view, have broad and deeply incised 

colpi that are not bordered by thickenings, and have 

reticulate sculpturing. Type C3A-1 (pi. 3, fig. 1; upper 

part of Merchantville through Englishtown) is particularly common in the Woodbury. Type C3A-2 (pi. 3, fig. 2; 

basal Merchantville through Englishtown) is larger 

and has a finer reticulum than C3A-1. C3A-3 (pi. 3, 

fig. 3; uppermost Merchantville and lowermost Woodbury) is characterized by the exceptionally coarse reticulum. The Wenonah and Navesink C3A-4 (pi. 3, fig. 

4) also has a coarse reticulum, but the ridges are narrow 

and the size is smaller than in C3A-3. The ridges of the 

reticulum of C3A-5 (pi. 3, fig. 5; upper Woodbury 

through Englishtown) are thicker than in C3A-4.

Type C3B. This type differs from C3A primarily by 

having thickened colpal borders although typically the 

colpi are somewhat less broad. C3B-1 (pi. 3, fig. 6) is 

common in various Woodbury samples. The Englishtown C3B-2 (pi. 3, fig. 7) has a finer reticulum and less 

deeply incised colpi. C3B-3 (pi. 3, fig. 8) in the Wenonah 

and Navesink has a coarse reticulum. With an even 

coarser reticulum and a definitely larger size is C3B-4 

(pi. 3, fig. 9) in the Marshalltown.

Type CSC. This type is approximately triangular in 

polar view, has colpi that are bordered by thickenings, 

and has reticulate sculpturing. Because there is some 

indication of pores, this type might prove to be better 

classed as a trico]porate (CP3). C3C-1 (pi. 3, fig. 11; 

Cliffwood and basal Merchantville) has a coarse reticulum that has luminae of irregular shape and size. 

The Merchantville material of C3C-1 has somewhat 

less deeply incised colpi; in this character it is more 

similar to C3C-2 (pi. 3, fig. 12). C3C-2 (Woodbury) has a 

finer reticulum that has luminae of approximately reg-
16 STRATIGRAPHIC DISTRIBUTION POLLEN, CAMPANIAN AND MAESTRICHTIAN ROCKS

ular shape and size, and the Englishtown C3C-3 (pi. 3, 

fig. 13) has an even finer reticulum. It is possible that 

these three species are a phyletic series. The distinctiveness of the Woodbury C3C-4 (pi. 3, fig. 10) with its 

coarse and irregular sculpture, large size, and pronouncedly concave sides indicates little, if any, close 

relationship to the other species of C3C.

Type CP3A. This type is characterized by its circular shape in polar view, colpi that have thickened borders, and reticulate sculpturing. CP3A-1 (pi. 3, fig. 16) 

and CP3A-2 (pi. 3, fig. 14) have overlapping ranges 

(upper part of Merchantville and Woodbury) but appear 

to be closely similar. CP3A-2 is smaller and has less 

deeply incised colpi than CP3A-1. CP3A-3 (pi. 3, fig. 17; 

Navesink) is similar to CP3A-1 in size and degree of 

incision of the colpi but has a much finer reticulum.

Type CP3B. This type is similar to CP3A but is 

triangular rather than circular in polar view; the outer 

and inner walls are of equal thickness. CP3B-1 (pi. 3, 

fig. 15; Cliffwood beds and basal Merchantville) has 

colpi incised about halfway to the poles and a fine reticulum. CP3B-2 (pi. 3, fig. 18; upper part of Merchantville) has a coarser reticulum and thicker margoes 

than CP3B-1. A common form in several Woodbury 

samples is CP3B-3 (pi. 3, fig. 19), which has an exceptionally coarse reticulum, pronounced margoes, and 

short colpi. CP3B-4 (pi. 3, fig. 20; upper part of Woodbury) has sculpturing similar to CP3B-2 (except that 

the reticulum is thicker as in CP3B-5), but the margoes 

are similar in thickness to CP3B-3. CP3B-5 (pi. 3, 

fig. 21; Englishtown) has sculpturing and margoes similar to CP3B-2, but the colpi are short. If these various 

species represent a phyletic series, it is apparent that 

the trends toward coarse sculpturing and thickened 

margoes were reversed in late Woodbury times, in contrast to the consistent trends towards shortening of the 

colpi and increase in thickness of the reticulum.

Whereas the margoes in CP3B-1 through 5 tend to 

thin poleward, in forms CP3B-6, 7, and 8, they tend to 

be of uniform thickness. CP3B-6 (pi. 4, fig. 1; Woodbury 

and Merchantville) is similar to CP3B-2 in sculpturing, 

but the wall of the grain curves around the corners to 

make a slitlike colpus. CP3B-7 (pi. 4, fig. 2; Englishtown) is smaller than CP3B-6 and has the pore more 

deeply inset from the corners of the grain. CP3B-8 (pi. 4, 

fig. 3; Wenonah) is smaller than these two forms and has 

a finer reticulum.

Type CP3C. This type is similar to CP3B except that 

the inner wall is thicker than the outer wall. CP3C-1 

(pi. 4, fig. 4; Woodbury) is rare but is so distinctive that it 

would be readily recognizable and perhaps be an excellent marker. In wall structure and sculpturing, CP3C-1 

is similar and may be ancestral to CP3C-2 (pi. 4, fig. 5; 

Englishtown). CP3C-2 is smaller and the pores are

protruding.

Type CP3D. Type CP3D is recognized on the basis 

of the straight channeling of the inner wall and the 

baculate sculpturing. Tertiary material of this type has 

been referred to Holkopollenites Fairchild (in Stover 

and others, 1966), which has been recorded by several 

workers from the Paleocene and Eocene of the Mississippi embayment. The oldest record of this type is small 

grains from the Cliffwood beds and Merchantville; this 

species (CP3D-1; pi. 4, figs. 6, 7) varies, as do younger 

species of the genus, by having concave to convex sides. 

CP3D-2 (pi. 4, figs. 8, 9; Woodbury and Englishtown) is 

considerably larger than CP3D-1. CP3D-3 (pi. 4, fig. 10; 

Marshalltown through Red Bank) has more deeply incised colpi than CP3D-2; there is also a tendency for 

the sides of the grains to be more convex in CP3D-3 and 

more concave in CP3D-2. H. chemardensis Fairch. has 

colpi more deeply incised than in CP3D-3.

Type CP3E. In this type, the inner wall is channeled 

by anastomosing rather than straight grooves, and the 

sculpturing is decidedly finer than in Holkopollenites. 

CP3E-1 (pi. 4, fig. 11) occurs in the upper part of the 

Merchantville, Woodbury, and Englishtown; this type 

is questionably known in the Mount Laurel. The one 

grain of this type from the Mount Laurel sample is 

smaller than any of the Woodbury or Englishtown 

specimens, but more Mount Laurel specimens will be 

needed to determine whether this size difference is 

consistent.

Type CP3F. This type is pronouncedly brevicolpate, 

and is triangular in polar view; the apertures are located at the ambs. CP3F-1 (pi. 4, fig. 12; Merchantville 

through Englishtown) is very indistinctly sculptured 

relative to the more distinct sculpturing of CP3F-2 

(pi. 4, fig. 13; Mount Laurel through Red Bank).

Type CP3G. CP3G-1 (pi. 4, fig. 14; upper part of the 

Navesink, Red Bank, and Severn River Monmouth) is 

characterized by exceptionally thick walls. The 

sculpturing is inconspicuously punctate.

Miscellaneous pollen types. MPA-1 (pi. 4, fig. 15) is 

tricolporate, the colpi have thickened borders, and the 

apertures are located between the corners. This pollen 

type from the Merchantville is perhaps the forerunner 

of the bombacaceous type, which is present in the Navesink. Type MPB-1 (pi. 4, fig. 16) is similar in sculpturing 

and size to pollen of the extant bombacaceous Cavanellisia. MPC-1 (pi. 4, fig. 17) from the Severn River Monmouth is probably referable to Bombacidites on the 

basis of having larger meshes at the poles than at the 

equator (Srivastava, 1972).

MPD-1 (pi. 4, fig. 18) is a characteristic syncolpate 

known only from the Severn River Monmouth and the 

Red Bank. Types MPD-2 (pi. 4, fig. 19; Wenonah and 

Severn River Monmouth) and MPD-3 (pi. 4, fig. 20;
REFERENCES CITED 17

lower part of the Navesink) are less conspicuously 

sculptured than MPD-1. The sculpturing in MPD-3 is 

greatly reduced near the colpal borders compared with 

MPD-2. Fragments of the syncolpate Trisectoris occur 

throughout the section, and this genus is known in the 

Magothy (Wolfe and Pakiser, 1972). Other syncolpate 

types are rare; none are known in more than one sample. In general, more different types of syncolpates are 

known in the upper Campanian and Maestrichtian (at 

least seven types) than in the lower Campanian (two 

types).

Polyporates are unknown in the lower Campanian 

part of the section, whereas at least 10 types are known 

from samples in the Marshalltown through Red Bank 

interval. Of these types, only four occur in more than 

one sample. MPE-1 (pi. 4, figs. 21, 22), which is a 

polyporate grain that has weak sculpturing, is known 

from the Severn River Monmouth; this type is perhaps 

of centrospermous affinity. Polyporate type MPF-1 

(pi. 4, figs. 23, 24; Wenonah through Red Bank) has 

fewer pores than MPE-1, and the membranes covering 

the pores are flecked; similar pore membranes are found 

in extant families that are not closely related (for example, Hamamelidaceae and Pistaciaceae) and thus offer 

no certain clue of affinities. MPG-1 (pi. 4, fig. 25; 

Navesink and Severn River Monmouth) is a four-pored 

grain that has verrucate sculpturing; this type is almost 

certainly of ulmaceous affinity.

Types MPH-1 (pi. 4, fig. 26; Marshalltown and 

Wenonah) and MPH-2 (pi. 4, fig. 27; lower part of the 

Navesink and Severn River Monmouth) are polycolporates; MPH-2 differs by having a thinner wall and less 

conspicuous sculpturing.

MPI-1 (pi. 4, fig. 28) represents Aquilapollenites. I 

have found this in only one sample (from the Wenonah), 

whereas Evitt (oral commun., 1973) records the genus 

from the Marshalltown and the Red Bank.

FOSSIL LOCALITIES

11156. Lat39°28'42"N.,long75°59'36"W. Merchantville Formation. 

Collector J. P. Owens.

11172. Lat39°23'55"N.,long76°02'26"W. Merchantville Formation, 

lower part. Collector J. P. Owens.

11173. Lat39°22'15"N.,long76°05'30"W. Merchantville Formation, 

about 10 ft above beach. Collector J. P. Owens.

11174. Same locality as 11173, Merchantville Formation, about 13 ft

above beach. Collector J. P. Owens. 

11176. Lat 39°21'10" N., long 76°03'58" W. Englishtown Formation,

about middle. Collector J. P. Owens. 

11210. Lat 39°02'03" N., long 76°33'20" W. Monmouth Formation on

southwest side Severn River. A, near base; B, +8 ft; C, +16

ft; D, +20 ft; E, +24 ft. Samples collected about 4 ft apart.

Collector J. A. Wolfe. 

11212. Lat 39°02'03" N., long 76°33'20" W. Monmouth Formation, on

northeast side Severn River. Samples collected about 3 ft

apart. Collector J. A. Wolfe.

11213. Lat 39°03'40" N., long 76°33'17" W. uppermost Marshalltown 

Formation or lowermost Wenonah Formation. Samples collected about 3-4 ft apart. Collector J. A. Wolfe.

11217. Lat 40°26'49"N., long 74°12'39"W. Cliffwood beds of Magothy 

Formation. A, at mollusk horizon; B, about +15 ft; remainder samples about 2 to 3 ft apart, and H at top. Collector J. A. 

Wolfe.

11218. Same latitude and longitude as 11217. Merchantville Formation, basal part above reworked bed. Collector J. A. Wolfe.

11219. Lat 40°26'20"N., long 74°14'47"W. Merchantville Formation, 

middle and upper part. Samples collected about 3 ft apart. 

Collector J. A. Wolfe.

11221. Lat 40°22'19" N., long 74°18'30" W. Woodbury Clay, upper 

part. Samples collected about 7 ft apart. Collector J. A. 

Wolfe.

11222. Lat 40°24'50" N., long 74°01'35" W. Navesink Formation, 

lower part. A, just above contact with Mount Laurel Sand; B, 

+ 3 ft. Collector J. A. Wolfe.

11223. Lat 40°24'49" N., long 74°01'21" W. Navesink Formation, 

upper part. Samples collected about 3 ft apart. Collector J. A. 

Wolfe.

11224. Same latitude and longitude as 11223. Red Bank Sand, basal 

part. Collector J. A. Wolfe.

11225. Lat 40°08'16" N., long 74°33'18" W. Wenonah Formation, 

basal part. Samples collected about 2 ft apart. Collector J. A. 

Wolfe.

11226. Lat 40°07'57" N., long 74°36'27" W. Englishtown Formation, 

middle part. Samples collected about 3 ft apart. Collector 

J. A. Wolfe.

11227. Lat 40°07'35" N., long 74°42'31" W. Woodbury Clay, lower 

part. Samples collected about 4-5 ft apart. Collector J. A. 

Wolfe.

11228. Lat 40°07'40" N., long 74°43'47" W. Magothy Formation, 

upper part. Samples about 2 ft apart. Collector J. A. Wolfe.

11229. Lat 40°07'19" N., long 74°47'39" W. Magothy Formation,

lower part. Collector J. A. Wolfe. 

11230 Lat 39°32'37" N., long 75°42'23" W. Marshalltown Formation,

lower part. Collector J. A. Wolfe.

11231. Lat 39°32'24" N., long 75°44'35" W. Merchantville Formation, 

upper part. Samples collected about 2 ft apart. Collector J. A. 

Wolfe.

11232. Lat 39°32'22" N., long 75°44'35" W. Magothy Formation. A, at 

base above contact with Potomac Group; B, +10-12 ft; C, 

+ 15 ft; D, +25 ft, at top. Collector J. A. Wolfe.

11233. Lat 39°33'12" N., long 75°38'14" W. Mount Laurel Sand, lower 

part (same as USGS Mesozoic loc. 29585 of Owens and 

others, 1970, p. 48, "Gryphaea" bed). Collector J. A. Wolfe.

11234. Lat 39°33'12" N., long 75°38'14" W. Marshalltown Formation, 

near top. Collector J. A. Wolfe.

11351. Excavation along south bank of Mantua Creek, northeast of 

road and bridge of Rt. 45 at Mantua, Gloucester County, 

N. J. Same as USGS Mesozoic loc. 30252. Marshalltown 

Formation, middle part. Collector N. F. Sohl.

REFERENCES CITED

Brenner, G. J., 1963, The spores and pollen of the Potomac Group of

Maryland: Maryland Dept. Geology, Mines, and Water Resources

Bull., v. 27, 215 p. 

Clark, W. B., 1916, The Upper Cretaceous deposits of Maryland:

Maryland Geol. Survey, Upper Cretaceous [Volume], p. 23-110. 

Doyle, J. A., 1969, Cretaceous angiosperm pollen of the Atlantic

Coastal Plain and its evolutionary significance: Jour. Arnold

Arboretum, v. 50, p. 1-35.
18 STRATIGRAPHIC DISTRIBUTION POLLEN, CAMPANIAN AND MAESTRICHTIAN ROCKS

Elsik, W. C., 1968, Palynology of a Paleocene Rockdale Lignite, Milam 

County, Texas: Pollen et Spores, v. 10, p. 599-664.

Goczan, Ferenc, Groot, J. J., Krutzsch, Wilfred, and Pacltova, Blanka, 

1967, Die Gattungen des "Stemma Normapolles Pflug 1953b" 

(Angiospermae): Palaontologische Abhand., Abt. B, 

Palaobotanik, v. 2, no. 3, p. 429-539, 19 pis.

Gray, T. C., and Groot, J. J., 1966, Pollen and spores from the marine 

Upper Cretaceous formations of Delaware and New Jersey: 

Palaeontographica, Abt. B, v. 117, p. 114-134, pis. 42-43.

Hughes, N. F., and Moody-Stuart, J. C., 1967, Palynological fades and 

correlation in the English Wealden: Review Palaeobotany and 

Palynology, v. 1, p. 259-268.

Martin, A. R. H., 1973, Reappraisal of some palynomorphs of supposed 

proteaceous affinity. I. The genus Beaupreadites Cookson ex 

Couper and the speciesProteacidites hakeoides Couper: Geol. Soc. 

Australia Spec. Pub. 4, p. 73-78.

Minard, J. P., 1974, Geology of the Betterton Quadrangle, Kent 

County, Maryland, and a discussion of the regional stratigraphy: 

U.S. Geol. Survey Prof. Paper 816, 27 p.

Owens, J. P., Minard, J. P., Sohl, N. F., and Mello, J. F., 1970, 

Stratigraphy of the outcropping post-Magothy formations in 

southern New Jersey and northern Delmarva Peninsula, Delaware and Maryland: U.S. Geol. Survey Prof. Paper 674, 60 p.

Owens, J. P., and Sohl, N. F., 1973, Glauconites from the New 

Jersey-Maryland Coastal Plain; their K/Ar ages and application 

in stratigraphic studies: Geol. Soc. America Bull., v. 84, p. 2811- 

2838.

Sohl, N. F., 1964a, Neogastropoda, Opisthobranchia, and Basommatophora from the Ripley, Owl Creek, and Prairie Bluff Formations: U.S. Geol. Survey Prof. Paper 331-B, p. B153-B344.

 1964b, Gastropods from the Coffee Sand (Upper Cretaceous) of

Mississippi: U.S. Geol. Survey Prof. Paper 331-C, p. C345-C394. 

Srivastava, S. K., 1972, Some spores and pollen from the Paleocene

Oak Hill Member of the Naheola Formation, Alabama (U.S.A.):

Review Palaeobotany and Palynology, v. 14, p. 217-285. 

Stover, L. E., Elsik, W. C., and Fairchild, W. W., 1966, New genera and

species of early Tertiary palynomorphs from Gulf Coast: Kansas

Univ. Paleont. Contr., Paper 5, 11 p., 5 pis. 

Tschudy, B. D., 1971, Two new fossil pollen genera from upper Campanian (Cretaceous) rocks of Montana: U.S. Geol. Survey Prof.

Paper 750-B, p. B53-B61. 

Tschudy, R. H., 1973, Complexiopollis pollen lineage in Mississippi

Embayment rocks: U.S. Geol. Survey Prof. Paper 743-C, p. ClC14, 9 pis.

 1975, Normapolles pollen from the Mississippi Embayment: 

U.S. Geol. Survey Prof. Paper 865, 40 p., 20 pis.

Wolfe, J. A., 1971, Tertiary climatic fluctuations and methods of 

analysis of Tertiary floras: Palaeogeography, Palaeoclimatology, 

Palaeoecology, v. 9, no. 1, p. 27-57.

 1973, Fossil forms of Amentiferae: Brittonia, v. 25, p. 334-355.

Wolfe, J. A., and Pakiser, H. M., 1971, Stratigraphic interpretations of 

some Cretaceous microfossil floras of the Middle Atlantic States: 

U.S. Geol. Survey Prof. Paper 750-B, p. B35-B47.
PLATES 1-4

[Contact photographs of the plates in this report are available at cost, from the U.S. Geological 

Survey Library, Federal Center, Denver, Colo. 80225]
	PLATE 1

Campanian and Maestrichtian pollen. All figures x 1,000.

FIGURE 1. NA-1 Englishtown Formation, loc. 11226-A, slide 3, 103.4 x 14.0

2. NA-2. Englishtown Formation, loc. 11226-C, slide 1, 90.0 x 3.5.

3. NA-3. Wenonah Formation, loc. 11213-C, slide 3, 104.6 x 19.7.

4. NA-4. Monmouth Formation, loc. 11210-E, slide 2, 102.5 x 22.4.

5. NA-5. Monmouth Formation, loc. 11212-H, slide 1, 94.3 x 4.1.

6. NA-6. Merchantville Formation, loc. 11218, slide 3, 113.2 x 3.1.

7. NA-7. Englishtown Formation, loc. 11226-C, slide 2, 86.1 x 2.9.

8. NA-8. Red Bank Sand, loc. 11224, slide 3, 83.3 x 17.9.

9. NB-1. Woodbury Clay, loc. 11227-C, slide 2, 88.2 x 4.7.

10. NB-2. Merchantville Formation, loc. 11218, slide 3, 90.5 x 5.0.

11, 12. NB-3. Wenonah Formation, loc. 11225-C, slide 3, 100.0 x 7.5.

13. NC-1. Woodbury Clay, loc. 11221-A, slide 2, 89.0 x 5.9.

14. NC-2. Merchantville Formation, loc. 11219-E, slide 2, 100.2 x 20.6.

15. NC-3. Marshalltown Formation, loc. 11351, slide 2, 83.1 x 16.4.

16. ND-1. Merchantville Formation, loc. 11218, slide 3, 110.0 x 15.6.

17. ND-2. Marshalltown Formation, loc. 11230, slide 3, 103.8 x 15.6.

18. ND-3. Englishtown Formation, loc. 11176, slide 2, 103.2 x 13.9.

19. NE-1. Merchantville Formation, loc. 11219-G, slide 2, 95.3 x 10.0.

20. NE-2. Englishtown Formation, loc. 11226-C, slide 3, 80.8 x 5.2.

21. NE-3. Wenonah Formation, loc. 11225-C, slide 3, 102.6 x 6.2.

22. NE-4. Merchantville Formation, loc. 11219-B, slide 1, 98.4 x 15.0. 

23, 24. NF-1. 23, Merchantville Formation, loc. 11219-B, slide 1, 90.6 x 13.9. 

	24, Merchantville Formation, loc. 11219-E, slide 2, 83.9 x 13.3.

25. NF-2. Woodbury Clay, loc. 11227-B, slide 2, 89.9 x 18.0.

26. NM-1. Englishtown Formation, loc. 11176, slide 2, 103.8 x 12.6.

27. NF-3. Mount Laurel Sand, loc. 11233, slide 3, 78.9 x 15.5.

28. NF-4. Englishtown Formation, loc. 11176, slide 2, 90.3 x 3.0.

29, 30. NG-1. Navesink Formation, loc. 11223-A, slide 1, 91.7 x 5.0.

31, 32. NI-1. Merchantville Formation, loc. 11218, slide 3, 96.1 x 5.6.

33, 34. NI-2. Englishtown Formation, loc. 11226-A, slide 3, 112.7 x 4.5.

35. NH-1. Monmouth Formation, loc. 11212-E, slide 2, 96.1 x 3.3.
GEOLOGICAL SURVEY PROFESSIONAL PAPER 977 PE.ATE 1

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CAMPANIAN AND MAESTRICHTIAN POLLEN , NA-1 TO NH-1
	PLATE 2

Campanian and Maestrichtian pollen. All figures x 1,000.

FIGURE 1. NJ-1. Woodbury Clay, loc. 11227-D, slide 2, 105.3 x 20.8.

2. NJ-2. Mount Laurel Sand, loc. 11233, slide 4, 108.1 x 19.4.

3. NK-1. Wenonah Formation, loc. 11225-B, slide 3, 107.4 x 2.8.

4. NK-2. Monmouth Formation, loc. 11210-E, slide 2, 99.5 x 4.6.

5. NK-3. Red Bank Sand, loc. 11224, slide 3, 94.9 x 11.4.

6. NL-1. Merchantville Formation, loc. 11218, slide 2, 82.4 x 10.0.

7. NL-2. Woodbury Clay, loc. 11227-C, slide 1, 88.5 x 4.1.

8. NN-1. Wenonah Formation, loc. 11213-A, slide 3, 85.1 x 5.0.

9. NN-2. Monmouth Formation, loc. 11210-A, slide 1, 106.9 x 13.7.

10. NO-1. Englishtown Formation, loc. 11226-C, slide 1, 106.2 x 21.5.

11. NO-2. Wenonah Formation, loc. 11225-C, slide 3, 92.8 x 8.6.

12. NO-3. Monmouth Formation, loc. 11212-H, slide 2, 88.8 x 5.9.

13. NO-4. Merchantville Formation, loc. 11218, slide 3, 111.7 x 4.3.

14. NO-5. Wenonah Formation, loc. 11225-B, slide 3, 81.9 x 17.6.

15. NP-1. Marshalltown Formation, loc. 11234, slide 2, 103.7 x 13.9.

16. NP-2. Monmouth Formation, loc. 11212-E, slide 2, 101.6 x 12.9.

17-19. NQ-1. 17, Cliffwood beds, loc. 11217-A, slide 2, 102.5 x 2.9.

	18. Cliffwood beds, loc. 11217-B, slide 2, 81.7 x 5.2.

	19. Cliffwood beds, loc. 11217-D, slide 2, 99.4 x 4.8.

20. NR-1. Marshalltown Formation, loc. 11234, slide 4, 96.5 x 10.7.

21. NS-1. Englishtown Formation, loc. 11226-C, slide 3, 98.8 x 13.9.

22. NT-1. Navesink Formation, loc. 11223-A, slide 3, 101.8 x 6.6.

23. NU-1. Englishtown Formation, loc. 11226-C, slide 3, 94.9 x 2.7.

24. NV-1. Monmouth Formation, loc. 11212-H, slide 2, 83.5 x 9.9.

25. PR-1. Woodbury Clay, loc. 11221-A, slide 1, 103.8 x 12.2.

26, 27. PR-2. Merchantville Formation, loc. 11219-G, slide 2, 90.7 x 12.9.

28. PR-3. Englishtown Formation, loc. 11176, slide 2, 98.0 x 9.1.

29. PR-4. Wenonah Formation, loc. 11225-C, slide 2, 82.0 x 6.8.

30. PR-5. Navesink Formation, loc. 11222-B, slide 2, 106.3 x 16.5.

31. PR-6. Englishtown Formation, loc. 11226-A, slide 1, 101.2 x 17.2.

32. PR-7. Englishtown Formation, loc. 11226-C, slide 3, 86.1 x 8.4.
GEOLOGICAL SURVEY PROFESSIONAL PAPER 977 PLATE 2

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CAMPANIAN AND MAESTRICHTIAN POLLEN, NJ-1 TO PR-7
	PLATE 3

Campanian and Maestrichtian pollen. All figures x 1,000.

FIGURE 1. C3A-1. Merchantville Formation, loc. 11172, slide 1, 104.9 x 22.4.

2. C3A-2. Englishtown Formation, loc. 11226-A, slide 2, 84.4 x 8.0.

3. C3A-3. Woodbury Clay, loc. 11227-C, slide 1, 86.0 x 14.8.

4. C3A-4. Wenonah Formation, loc. 11225-B, slide 3, 87.8 x 15.2.

5. C3A-5. Woodbury Clay, loc. 11221-A, slide 2, 99.3 x 3.3.

6. C3B-1. Woodbury Clay, loc. 11227-C, slide 1, 100.1 x 3.0.

7. C3B-2. Englishtown Formation, loc. 11226-A, slide 1, 83.6 x 7.3.

8. C3B-3. Wenonah Formation, loc. 11213-B, slide 2, 81.4 x 10.6.

9. C3B-4. Marshalltown Formation, loc. 11230, slide 3, 105.7 x 7.5.

10. C3C-4. Woodbury Clay, loc. 11227-C, slide 1, 104.0 x 6.0.

11. C3C-1. Cliffwood beds of Magothy Formation, loc. 11217-C, slide 2, 106.6 x 3.7.

12. C3C-2. Woodbury Clay, loc. 11221-A, slide 1, 101.4 x 7.9.

13. C3C-3. Englishtown Formation, loc. 11226-A, slide 2, 82.6 x 11.1.

14. CP3A-2. Woodbury Clay, loc. 11227-A, slide 1, 108.7 x 13.3.

15. CP3B-1. Cliffwood beds of Magothy Formation, loc. 11217-C, slide 2, 88.7 x 14.2.

16. CP3A-1. Merchantville Formation, loc. 11219-E, slide 2, 107.7 x 3.7.

17. CP3A-3. Navesink Formation, loc. 11222-B, slide 2, 87.3 x 17.2.

18. CP3B-2. Merchantville Formation, loc. 11219-F, slide 2, 101.3 x 8.1.

19. CP3B-3. Woodbury Clay, loc. 11227-D, slide 2, 99.2 x 8.5.

20. CP3B-4. Woodbury Clay, loc. 11221 B, slide 3, 82.3 x 13.8.

21. CP3B-5. Englishtown Formation, loc. 11226-C, slide 3, 99.9 x 21.2.
GEOLOGICAL SURVEY PROFESSIONAL PAPER 977 PLATE 3

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CAMPANIAN AND MAESTRICHTIAN POLLEN , C3 A-l TO CP3B-5
	PLATE 4

Campanian and Maestrichtian pollen. All figures x 1,000.

FIGURE 1. CP3B-6. Merchantville Formation, loc. 11172, slide 1, 90.0 x 14.0.

2. CP3B-7. Englishtown Formation, loc. 11226-A, slide 2, 94.8 x 3.6.

3. CP3B-8. Wenonah Formation, loc. 11225-C, slide 3, 85.6 x 5.3.

4. CP3C-1. Woodbury Clay, loc. 11227-A, slide 2, 93.3 x 8.5.

5. CP3C-2. Englishtown Formation, loc. 11226-C, slide 3, 105.7 x 11.8.

6, 7. CP3D-1. 6, Cliffwood beds of Magothy Formation, loc. 11217-F, slide 2, 97.1 x 8.2.

	7, Merchantville Formation, loc. 11173, slide 1, 89.4 x 5.7. 

8, 9. CP3D-2. 8, Merchantville Formation (Woodbury age), loc. 11231-D, slide 1, 96.5 x 17.9.

	9, Englishtown Formation, loc. 11176, slide 2, 102.1 x 8.0.

10. CP3D-3. Wenonah Formation, loc. 11225-B, slide 3, 106.9 x 5.3.

11. CP3E-1. Woodbury Clay, loc. 11231-D, slide 1, 94.9 x 17.1.

12. CP3F-1. Englishtown Formation, loc. 11226-A, slide 3, 106.5 x 5.3.

13. CP3F-2. Navesink Formation, loc. 11223-B, slide 3, 106.5 x 17.8.

14. CP3G-1. Monmouth Formation, loc. 11212-A, slide 2, 102.3 x 4.5.

15. MPA-1. Merchantville Formation, loc. 11219-B, slide 1, 101.1 x 19.6.

16. MPB-1. Navesink Formation, loc. 11223-B, slide 3, 113.9 x 22.7.

17. MPC-1. Monmouth Formation, loc. 11212-G, slide 2, 83.0 x 2.6.

18. MPD-1. Monmouth Formation, loc. 11210-B, slide 2, 101.2 x 6.9.

19. MPD-2. Wenonah Formation, loc. 11225-C, slide 2, 86.4 x 16.4.

20. MPD-3. Navesink Formation, loc. 11223-B, slide 4, 106.3 x 1.8.

21, 22. MPE-1. Monmouth Formation, loc. 11212-E, slide 2, 90.0 x 7.7.

23, 24. MPF-1. Wenonah Formation, loc. 11213-B, slide 3, 100.4 x 16.2.

25. MPG-1. Monmouth Formation, loc. 11212-E, slide 1, 109.3 x 16.8.

26. MPH-1. Wenonah Formation, loc. 11213-A, slide 2, 83.4 x 9.4.

27. MPH-2. Monmouth Formation, loc. 11210-B, slide 1, 108.4 x 10.6.

28. MPI-1. Wenonah Formation, loc. 11213-B, slide 3, 111.6 x 16.8.
GEOLOGICAL SURVEY PROFESSIONAL PAPER 977 PLATE 4

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CAMPANIAN AND MAESTRICHTIAN POLLEN, CP3B-6 TO MPI-1