|
|
|

VOLUME 87, NUMBER 320 DECEMBER 14, 1984

MUS. COMP. ZOOL

1 IMMARY
A Revised Radiolarian Zonation oec 26 1984
AARVARD
for the UNIVERSITY

Upper Jurassic of Western North America

by

Emile A. Pessagno, Jr., Charles D. Blome, and Jose F. Longoria

Paleontological Research Institution
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Ithaca, New York, 14850 U.S.A.

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I| VOLUME 87, NUMBER 320 DECEMBER 14, 1984

A Revised Radiolarian Zonation
| for the

Upper Jurassic of Western North America

by

Emile A. Pessagno, Jr., Charles D. Blome, and Jose F. Longoria

Paleontological Research Institution
1259 Trumansburg Road
Ithaca, New York, 14850 U.S.A.

Library of Congress Card Number: 84-62662

Printed in the United States of America
Allen Press, Inc.
Lawrence, KS 66044 U.S.A.

ADSttacti es etur ADS quie. A NR MON
Introduction
The Jurassic-Cretaceous Boundary Problem ................
Definition and Subdivision of the Tithonian and
Kimmeridgian Stages
Emendation of Upper Jurassic Radiolarian Zonal Units
Zone PRINOTU SINTAL ONES E tear Seer ORIUNTUR EROR
Zone 3 (Mirifusus baileyi Zone)
Zone 2 (Minst SUAQAIUDEASIS LOSA TE SE
ZONES (RAPVIGIN SUELOS) Hoke RA SCREEN rou m S
Integration of Biostratigraphic and Chronostratigraphic Data
Ristola altissima—-R. procera final occurrence events .......
“Eucyrtidium” ptyctum final occurrence event ............
Parvicingula jonesi firsvocctrrence event). eec
Mirifusus first occurrence event
INGOT AECA ss e p p ue mec M eke
Oer A eae re ee OS
Romania CAD ce cero E E ere a
Cape: Verde Basm SDP SGAS cers Ahonen aes
SUMMA e. Hut Ace OT AU CC AS
Parvicingula rst- occurrence Vellum. de cures s cer e eue ca
iG olen cof eontelalloD 0 a 14090 cria
Taxonomic problems affecting correlation ...............-
Paleolatitudinal/paleoclimatic considerations .............
Displaced terranes and their effect on
biostratigraphic correlation
Comments on the ranges of selected taxa..........+.+----
COIS ALOnPOn Zonal seems e. uu LE
DANA AS A
Systematic Paleontology
Introduction
Order Polycystida
Suborder Spumellariina
Superfamily Spongodiscacea
Subsuperfamily Pseudoaulophacilae
Family Orbicwlitormmidae eea a e aa see

CONTENTS
Page
5 GEnus OFDICU OTIA nan ee M TE 22
3 Subsupentauniysbiosphaeridec- v. 01 ee | 22
6 Lamriyspantauellidae c ewe IE I EDI 22
ELISA aupa. eee EU 22
6 Family Praeconocaryommidae .................. 23
8 Genus Praeconocaryomma TEE 23
o) Suborder Nassellariina
10 Family Epia 0:0). OA. 24
12 GEMUSSRENISDV NAMING is ene EN ee 24
12 FamilyWitranaponidde rear sos). ee 24
GENE NAPORE nn, ee EE SOT AES pi 24
13 bamuilssEisutdac en elie set TOUR, Sio 24
13 Genus SUP. CIS OON. Ur 45
13 Family PUV ONAA. e. eie i eS 29
Genus MANS PESTA A mote, UC 25
13 Genlsara VICIS. ODIO GEILE me 26
14 GiGDUSe RISO QE S duae ta, ti s niic vat usu 28
14 Famulysspolsocapsulidae-- o 29
16 SAUS QUOS GI Ad o Be ee er 29
27 Nassellariina jncertae sedis
18 Genera and included species not assigned to a family
18 Genus dndIoniedauu- nel SIEG 30
18 GENUS SOU Me ara ee farei Nodes: cen ee Ces 30
19 GEISHA xcd Up I E Ner 30
Species that need to be assigned to new genera
19 “Eucyrtidium” ptyctum Riedel and Sanfilippo .. 30
20 SEIS UU starieyense Possagno n. r eae te 31
20 Appendix: Locality Descriptions
21 IUroduUchionA sen a eie Te eise Ir cio Ste ees 31
Ca A S Met a elie eR AREE 31
21 LORS SOPs BUA atic deci MET 33
E NE AE E E IE RO 33
ROCCO EE A ENERO Ne 34
dao do Pd Ra Nue Wee eae dM. 38
dE, ecce NS UA a. co ie 44
po

LIST OF ILLUSTRATIONS

Text-figure Page
l. Emecudatonot Radiolarian Zones 2 asad 4yofPessasino: (197 7a) nn os id atau ds ae aad «apn 9 e REM TA TRECE ESL US 9
2. Correlation of volcanogenic-pelagic strata above the Coast Range ophiolite at

Port. Sal, Alamo Creek, and lanadareCalutomita o o rt ia on mb A ee e Inte re te eee X3 TOY ILU
3. Ammonite zonation for northwestern Europe (Boreal Realm) and central and

sombeta Europe Cea cl be eh DIRE <x ur someter hnc socie as a ETE TREES 18 foldout inside back cover

A REVISED RADIOLARIAN ZONATION FOR THE UPPER JURASSIC
OF WESTERN NORTH AMERICA*

By
| EMILE A. PESSAGNO, JR.,! CHARLES D. BLOME,? AND JOSE F. LONGORIA!

| ABSTRACT

An accurate radiolarian zonation for the Upper Jurassic is critical to unraveling the stratigraphy and tectonic history of much
| of western North America. To meet this end a revised zonation is presented for the Upper Jurassic of the California Coast
Ranges. Zones 1, 2, 3, and 4 of Pessagno (1977a, 1977b) are redefined and related as accurately as possible to Upper Jurassic
| chronostratigraphic units. Discrepancies between European, Deep Sea Drilling Project, and North American biostratigraphic and
n chronostratigraphic data are analyzed. We conclude that many of the problems surrounding the correlation of North American
| Jurassic strata with those in the Mediterranean area are due to paleo-oceanographic factors closely related to plate tectonics.
| Even if preservational and taxonomic problems are excluded, correlation of Tethyan European Upper Jurassic radiolarian

assemblages with those of either Boreal or Tethyan North America will continue to be a difficult problem. The southern European
Tethyan faunas differ from Tethyan faunas of eastern Mexico by lacking Parvicingula Pessagno, 1977, and may be representative
of a lower latitude province within the Tethyan Realm.

One new genus, Vallupus Pessagno and Blome, and four new species: Vallupus hopsoni Pessagno and Blome, Hsuum mclaughlini

Pessagno and Blome, Parvicingula colemani Pessagno and Blome, and P. excelsa Pessagno and Blome, are described from

others are pertinent to the definition of Upper Jurassic zonal units in California and elsewhere in western North America.

| volcanogenic-pelagic strata overlying the Stanley Mountain remnant of the Coast Range ophiolite. These taxa as well as many
|

INTRODUCTION

Nearly eighty years ago Steinmann (1905) stressed
the genetic association of serpentinized peridotites,
Spilitic basalts, and radiolarian cherts (“Steinmann’s
Trinity”). This early observation perhaps prophesied
the coming of the sea-floor spreading hypothesis and
the importance of radiolarian biostratigraphy in tec-
tonic studies.

The application of plate tectonics theory to the ge-
ology of complex mobile belts throughout the world
has greatly accelerated geological investigations. How-
ever, until recently geologists were often hampered by
a lack of biostratigraphic control at critical tectonic
interfaces such as that between the Franciscan Com-
plex and the Coast Range ophiolite in the California
Coast Ranges. Geologic terranes of this sort are usually
characterized by a paucity of invertebrate megafossils
and an abundance of Radiolaria occurring in radi-
Olarian cherts. In the past it was impossible to extract
Radiolaria from radiolarian cherts; all Radiolaria had
to be identified in thin-section. However, in 1972 Pes-
sagno and Newport developed the simple hydrofluoric
acid technique, which allows the extraction of matrix-
free Radiolaria from cherts, tuffs, siliceous mudstones,

* Contribution Number 429, Program for Geosciences, The Uni-
versity of Texas at Dallas.

! Program for Geosciences, The University of Texas at Dallas,
Richardson, TX 75080, U.S.A.

? Paleontology and Stratigraphy Branch, U.S. Geological Survey,
345 Middlefield Road, Menlo Park, CA 94025, U.S.A.

and other siliceous rocks. The development of the HF
technique and the introduction of the scanning electron
microscope (SEM) provided technological break-
throughs that opened the door to the study of Mesozoic
and Paleozoic Radiolaria.

Jurassic Radiolaria were first studied at the turn of
the century. At that time monographic studies, which
dealt both with Jurassic and Lower Cretaceous (Ber-
riasian to Valanginian) Radiolaria were presented by
Riist (1885, 1898), Parona (1890), and Vinassa de Re-
gny (1899). Curiously, no other comprehensive reports
dealing with Jurassic Radiolaria were published until
the 1970’s (e.g., Foreman, 1973; Pessagno, 1977a).

With the advent of the hydrofluoric acid technique
(Pessagno and Newport, 1972), we were immediately
supplied with a vast number of chert residues from
localities all over the world. Unfortunately, at this time
there was no independent way to date Jurassic and
most Triassic radiolarian assemblages. Radiolarian
chert terranes associated with subduction complexes
are notorious for their lack of biostratigraphically use-
ful megafossils like ammonites. Occasionally, how-
ever, pectenacids and conodonts occur in Triassic
cherts, and calcareous microfossils such as calpionel-
lids and nannoconids occur in pelagic limestones in-
terbedded with Upper Jurassic and Lower Cretaceous
radiolarian cherts in the Tethys.

Gradually, during the period from 1968 to the pres-
ent time, biostratigraphic data that could be utilized
to date Jurassic radiolarian assemblages accumulated
from the Deep Sea Drilling Project (e.g., Foreman,

1973, 1975; Riedel and Sanfilippo, 1974) and from
land-based sections (e.g., Pessagno, 1977a, 1977b; Pes-
sagno and Blome, 1980, 1982; Pessagno and Whalen,
1982). Pessagno, his colleagues, and students are now
involved in analyses of Jurassic radiolarian faunas from
western North America (Baja California, California,
east-central Oregon, the Queen Charlotte Islands,
Alaska, and east-central Mexico). The purpose of these
investigations is to develop a detailed system of ra-
diolarian zonation for the Upper Triassic and the Ju-
rassic that can be integrated as closely as possible with
that of the ammonites and other well-studied fossil
groups.

A major stumbling block in completing this zonal
scheme occurs in the Upper Jurassic (Oxfordian to
Tithonian). In North America and indeed elsewhere
in the world it is difficult to find Upper Jurassic strata
that contain both abundant well-preserved Radiolaria
and ammonites. In North America this problem may
in part be resolved by studies recently initiated by
Pessagno and Longoria in east-central Mexico. In this
area Upper Jurassic strata (“Santiago”, Taman, and
Pimienta formations) contain common to abundant
ammonites, pectenacids, calpionellids, nannoconids,
and Radiolaria.

Pessagno (1976, 1977a, 1977b) presented the first
detailed zonation for the Upper Jurassic (Kimmeridg-
ian/Tithonian) to Upper Cretaceous (Maestrichtian)
strata of western North America. As new biostrati-
graphic data accumulated from the Mediterranean area
(Baumgartner, DeWever and Kocher, 1980), the deep
sea, North America (Pessagno and Blome, in prep.),
and Oman (Tippit, 1981), it rapidly became apparent
that Pessagno’s Upper Jurassic zonal units were in need
of redefinition. Many zonal markers, for example, have
been found to be longer ranging than previously be-
lieved.

To establish a detailed system of radiolarian zona-
tion for the Upper Jurassic—closely integrated with
that of the ammonites, calpionellids, and other estab-
lished groups of fossils—is vital to the interpretation
of the geology of the California Coast Ranges and a
number of other areas in western North America. In
California, for instance, it not only has a tremendous
bearing on the age and time of emplacement of the
Coast Range ophiolite, but also on the age of the Ne-
vadian Orogeny (cf: Hopson, Mattinson, and Pessagno,
1981).

The purpose of this report is to redefine Zones 1, 2,
3, and 4 of Pessagno (1977a, 1977b), to describe new
taxa that are important in the definition of Zone 4 in
western North America, and to relate Zones 2, 3, and
4 insofar as possible to Upper Jurassic chronostrati-

BULLETIN 320

graphic units. Finally, we will attempt to discuss dis-
crepancies in the interpretation of European, Deep Sea
Drilling Project, and North American biostratigraphic
and chronostratigraphic data.

THE JURASSIC-CRETACEOUS
BOUNDARY PROBLEM

The definition of the top of the Tithonian and in
particular, the top of the Jurassic System remains a
matter of considerable debate. Whereas catastrophic
faunal changes occur at the base and top of the Triassic
and at the top.of the Cretaceous, those at the Jurassic—
Cretaceous (Tithonian—Berriasian) boundary are insig-
nificant. In theory, systemic boundaries should coin-
cide with major rather than minor breaks in the pa-
leontologic record. This sort of reasoning led Newell
(1966, p. 75) to propose that Jurassic and Cretaceous
strata might be included in a single supersystem. Wied-
mann (1973, p. 177), in an excellent report dealing
with changes in the ammonoid assemblage at Mesozoic
system boundaries, found no evidence for a sharp fau-
nal break either below or above the Berriasian. He
proposed (p. 180) that the Jurassic-Cretaceous bound-
ary be placed instead between the Berriasian and Va-
langinian and stated that “it would be placed— in anal-
ogy to the Triassic-Jurassic boundary — between the
final extinction of Tithonian perisphinctids (Berri-
asellidae) and the origin of Neocomian perisphinctids
(Neocomitinae) and the origin of Cretaceous Ammo-
nitina (Desmocerataceae)." In a later report Wied-
mann (1980) included the Berriasian as the uppermost
substage of the Tithonian and drew the Jurassic-Cre-
taceous boundary at the base of the Valanginian. It
should be noted that the faunal change displayed by
Radiolaria at the Jurassic-Cretaceous boundary is like-
wise of minor magnitude compared to that between
the Permian and Triassic, the Lower and Middle Ju-
rassic, and the Cretaceous and Tertiary. For the time
being, however, we follow the traditional school of
stratigraphy in our placement of the Jurassic-Creta-
ceous boundary between the top of the Tithonian and
the base of the Berriasian.

DEFINITION AND SUBDIVISION OF THE
TITHONIAN AND KIMMERIDGIAN STAGES

The Tithonian stage was first introduced by Oppel
(1865), who unfortunately failed to designate a stra-
totype. As a result the term “Tithonian” has been used
by a variety of investigators with completely different
meanings. Until boundary stratotypes (sensu ISSC,
1970) are designated for this stage, it is likely that
confusion about the definition of its upper and lower
boundaries will continue.

|
|
|
|

JURASSIC RADIOLARIAN ZONATION: PESSAGNO ET AL. x

Unbeknownst to most geologists and many geo-
chronologists, the definition ofthe Tithonian and Kim-
meridgian stages has been radically changed by am-
monite biostratigraphers in recent years. According to
Imlay (1980, pp. 31-32), the base of the Tithonian, as
now defined by most workers, corresponds to the base
of the Russian Volgian. This correlation is based on
the local association of the Boreal/Tethyan ammonite
Gravesia (Salfeld, 1913) with the Tethyan ammonite
species Hybonoticeras hybonotum (Oppel, 1863). In
Boreal northwestern Europe the base of the Tithonian
is marked by the elegans Zone (Text-fig. 3; Imlay, 1980,
p. 26).

The Tithonian has been subdivided into lower, mid-
dle, and upper units. Ammonite biostratigraphers dis-
agree on which ammonite zones to assign to each of
these three subdivisions (cf. Imlay, 1980, p. 27, fig.
16). Imlay (1980, p. 32), Enay (1964, pp. 363, 364;
1971, pp. 99, 100) and Enay and Geyssant (1975, p.
53) considered a bipartite division (i.e., lower and up-
per) of the Tithonian to be more practical, particularly
in correlations between North America and Eurasia.
These workers define the base of the upper Tithonian
by the first occurrence of calpionellids s./. [= base of
the Chitinoidella Zone of Remane (1969, 1978)]. Un-
fortunately, however, this biohorizon is difficult to rec-
ognize. Chitinoidella Doben, 1963, possesses a micro-
granular test wall whereas true calpionellids such as
Calpionella Lorenz, 1902, possess a hyaline test wall
comprised of radially arranged crystals of calcite. Chi-
tinoidella, because of its test structure, does not lend
itself to being preserved in limestones that are even
mildly altered; calpionellids with hyaline tests are not
as easily affected by minor diagenetic changes in Tethy-
an limestones. As a result, we choose to utilize the first
occurrence of hyaline calpionellids (= calpionellids s.s.)
to mark the base of the upper Tithonian. This bio-
horizon [= base of the Crassicollaria Zone of Remane
(1969, 1978)] is easily recognized throughout the Te-
thyan Realm.

In Mexico (Sierra Cruillas, Tamaulipas) Bonet (1956,
p. 82, locs. 44, 45, 48) recorded hyaline calpionellids
from a horizon just below beds containing abundant
ammonites assignable to Imlay’s Kossmatia—Duran-
gites Assemblage (see Imlay, 1980, p. 35: measured
section at Loma Rinconada, Sierra Cruillas). He noted
the presence of Calpionella alpina Lorenz, 1902, C.
elliptica Cadisch, 1932, and Tintinnopsella oblonga
(Cadisch, 1932) in these strata. According to Remane
(1978, p. 166) the last two taxa are restricted to the
Cretaceous (Berriasian and Berriasian to Valanginian,
respectively). One must assume either that Bonet’s data
is out of date taxonomically or that C. elliptica and T.

oblonga [= Calpionellopsis oblonga (Cadisch, 1932)]
are longer ranging in North America than in Europe
(cf. Remane, 1969, pp. 563, 568). Regardless of these
two options, it is evident that hyaline calpionellids first
appear below beds bearing Imlay’s (1980) Kossmatia—
Durangites Assemblage. In the Mediterranean area
Zeiss (1984, p. 104) correlates this calpionellid event
with the base of the transitorius Zone (Text-fig. 3).
However, investigations by Pessagno and Longoria on
the type Taman Formation (Taman-Tamazunchale
area, San Luis Potosi) indicate that the first hyaline
calpionellids (= base of the Crassicollaria Zone) occur
immediately above the Virgatosphinctes mexicanus—
Aulacomyella neogeae Zone and within the Mazapi-
lites Zone of Cantu Chapa (1971). Furthermore, our
Mexican studies indicate that the base of the Crassi-
collaria Zone corresponds closely to the base of radi-
olarian Zone 4 (see emended definition herein). In the
California Coast Ranges the base of Zone 4 occurs
below the first appearance of Buchia piochii (Gabb,
1869) and associated Kossmatia-bearing beds.

In the Boreal Realm of northwest Europe the top of
the Tithonian is marked by the top of the oppressus
Zone (Text-fig. 3); the base of the Berriasian is marked
by the base of the primitivus Zone (Zeiss, 1984, p. 104).
In the Tethyan Realm the top of the Tithonian is
marked by the top of the transitorius Zone (central
Tethys) or by the Durangites Zone (southern Tethys)
(Text-fig. 3); the base of the Berriasian is marked by
the base of the euxinus Zone (central and southern
Tethys) (Zeiss, 1984, p. 104; Jeletsky, 1984, p. 99).

Problems arise in the correlation of ammonite fau-
nas between North America and Europe and asa result,
in the placement of the Tithonian—Berriasian bound-
ary. In Mexico and California, Imlay (1980) utilized
the top of his Substeuroceras—Proniceras Assemblage
[= Substeuroceras—Berriasella Complex of Jeletsky
(1984, p. 99)] and the equivalent Buchia sp. aff. B.
okensis Zone (Jones, Bailey, and Imlay, 1969) to mark
the top of the Tithonian. In Mexico, Imlay and Jones
(1970, p. B9; see also Imlay, 1944a, p. 1017; 1944b,
p. 1120; Jeletsky, 1984, p. 99) indicated that Berriasian
strata overlying strata with the Substeuroceras—Pro-
niceras Assemblage include Subthurmannia tenochi
(Felix, 1891) and Spiticeras zirkeli (Felix, 1891). In
California, Imlay and Jones (1970, pp. B12, 13) in-
dicated that upper Tithonian strata including the Sub-
steuroceras—Proniceras Assemblage and the equivalent
Buchia sp. aff. B. okensis Zone are overlain by strata
assignable to the Buchia uncitoides Zone. They indi-
cated that the lower two-thirds of the B. uncitoides
Zone is characterized by the presence of Spiticeras (Ne-
greliceras) (Djanélidzé, 1922) and Spiticeras Uhlig,

1903, s.s.. Furthermore, these workers stated that

the subgenus Negreliceras is characteristic of the Berriasian, is rep-
resented by only one species from the upper Tithonian, and is un-
known from the Valanginian (Djanélidzé, 1922, pp. 48, 49, 51). The
subgenus Spiticeras ranges from the top of the Tithonian through
the Berriasian but no higher (Djanélidzé, 1922, p. 51). On the basis
of the ammonites, therefore, most of the Buchia uncitoides Zone
(lower two-thirds) in California cannot be younger than Berriasian
and is unlikely to be as old as Tithonian. The upper third of the B.
uncitoides Zone, however, has not furnished ammonites and could
be younger than Berriasian.

Zeiss (1984, p. 104), however, disagrees with the
correlations of Imlay (1980), Jones, Bailey, and Imlay
(1969), and Jeletsky (1984). He correlated North
American strata with the Substeuroceras—Proniceras
Assemblage and Buchia sp. aff. B. okensis (Pavlow,
1907) with the occitanica Zone of the European Ber-
riasian (Tethys). Furthermore, he correlated underly-
ing strata with Buchia piochii (Gabb, 1869), Parodon-
toceras Spath, 1923, and Buchia fischeriana (d’Orbigny,
1844) with the euxinus Zone (see above). Zeiss main-
tained that the Substeuroceras—Proniceras Assemblage
(Imlay, 1980)/Substeuroceras—Berriasella Complex
(Jeletsky, 1984) does not include Kossmatia Uhlig,
1907, and Durangites Burckhardt, 1912. However, data
presented by Verma and Westermann (1973, pp. 125,
129, 131, 134, 135) for the Sierra Catorce (San Luis
Potosi) of eastern Mexico indicate that the Substeu-
roceras—Proniceras Assemblage not only includes these
two taxa, but also Microacanthoceras Spath, 1925, Co-
rongoceras Spath, 1925, and Berriasella Uhlig, 1905,
as well. In Europe, the ranges of Durangites, Micro-
acanthoceras, and Corongoceras do not extend above
the Tethyan Durangites Zone.

One must assume that the absence of Kossmatia,
Durangites, Corongoceras, and Microacanthoceras
within the Substeuroceras—Proniceras Assemblage at
other North American localities is either due to un-
known paleoecological parameters or due to insuffi-
cient collecting. It is also possible that only the lower
portion of the stratigraphic interval marked by the
Substeuroceras—Proniceras Assemblage bears these Ti-
thonian ammonites.

Until these problems are reconciled in the North
American succession, we choose to follow the corre-
lations of Imlay (1980) and Jeletsky (1984) in defining
the top of the Tithonian. Furthermore, it is apparent
that a more integrated study of the calpionellid, nan-
noconid, radiolarian, buchiid, and ammonite faunas
both in North America and Europe is needed to resolve
the Tithonian-Berriasian boundary problem.

Finally, it should be noted that if the base of the
Tithonian is defined by the base of the hybonotum
Zone in the European Tethyan Realm and by the base

BULLETIN 320

of the Gravesia Zone in the European Boreal Realm
(= base of English elegans Zone), all of the Portlandian
plus the middle and upper Kimmeridgian of Arkell
(1956) would be included in the Tithonian (cf. Text-
fig. 3). The Kimmeridgian 1s therefore restricted to the
lower Kimmeridgian of Arkell (1956, pp. 21, 22). So
redefined, the top of the Kimmeridgian in northwest-
ern Europe would be marked by the autissidorensis
Zone and its base by the baylei Zone (Text-fig. 3). In
the central and southern Tethys the top of the Kim-
meridgian is delineated by the top of the beckeri Zone
and its base by the base of the platynota Zone (Text-
fig. 3). In this report we follow Imlay (1980) in dividing
the Kimmeridgian into only upper and lower divisions.
Accordingly, the lower Kimmeridgian in northwestern
Europe includes the interval from the base of the baylei
Zone to the top of cymodoce Zone; the upper Kim-
meridgian includes the interval from the base of the
mutabilis Zone to the top ofthe austissiodorensis Zone
(Text-fig. 3). In the European Tethys the lower Kim-
meridgian includes the interval from the base of the
platynota Zone to the top of the divisum Zone whereas
the upper Kimmeridgian corresponds to the interval
between the base of the acanthicum Zone and the top
of the beckeri Zone (Text-fig. 3). Associations with
ammonites and Buchia Rouillier, 1845 from equiva-
lent intervals in the Kimmeridgian of North America
are shown in Text-figure 3.

EMENDATION OF UPPER JURASSIC
RADIOLARIAN ZONAL UNITS

Taxa that are used as the primary means of defining
a zonal unit in this report are referred to as “primary
marker taxa”. Primary marker taxa are selected be-
cause they are distinctive in character, because they
have sturdy tests that are likely to be preserved in a
variety of rock types, and preferably because they have
been observed at more than two localities in both the
Boreal and Tethyan realms. Taxa used as a secondary
means of defining a zonal unit are referred to as “‘sup-
plementary marker taxa.” Generally speaking, these
taxa are not as distinctive or have been observed at
fewer localities. However, in the absence of the primary
marker taxa they may be used with a lower level of
confidence in helping to delimit a given zonal unit.
Other taxa that make their first or last appearance with-
in the body of a zonal unit are referred to as “corporeal
taxa” [from corporeal (adj.) = of the body]. It should
be emphasized that the formal definition of a given
zonal unit herein is based on the primary marker taxa
and not on the supplementary marker taxa. The terms
“interval zone” and “Oppel zone” used in the defi-
nition of the zonal units below are used in the sense

of ISSC (1971).

JURASSIC RADIOLARIAN ZONATION: PESSAGNO ET AL. 9

ZONE 4
(Ristola altissima Zone)

Type of zone.—Oppel zone (see Text-fig. 1).

Primary marker taxa.—

Base: First appearance of Parvicingula colemani
Pessagno and Blome, n. sp.

Top: Final appearance of Ristola altissima (Rist,
1885) and R. procera (Pessagno, 1977a).

Supplementary marker taxa.—

Base: First appearance of Vallupus hopsoni Pes-
sagno and Blome, n. sp., Parvicingula excelsa
Pessagno and Blome, n. sp., and Hsuum
mclaughlini Pessagno and Blome, n. sp.

Top: None utilized.

Corporeal taxa.—** Eucyrtidium" ptyctum Riedel and
Sanfilippo, 1974, Parvicingula colemani Pessagno and
Blome, n. sp., Parvicingula jonesi Pessagno, 1977b, P.
santabarbaraensis Pessagno, 1977a, P. blowi Pessagno,

PRIMARY MARKER
TAXA

Ristola Ristola
altissima procera

Parvicingula
colemani, n. sp.

SUPPLEMENTARY MARKER

Vallupus Hsuum
hopsoni, n. sp.

1977a, Perispyridium Dumitrica, 1978, and Orbiculi-
forma lowreyensis Pessagno, 1977a (see Text-fig. 1).
The initial or final appearance of these taxa offers a
means of further subdividing Zone 4. It should be not-
ed that two corporeal taxa, Perispyridium (P. ordinari-
um Pessagno, 1977a) and “E.” ptyctum, that make
their final appearance within Zone 4, are rare to very
rare where we have observed them in samples from
California and Baja California Sur. However, in east-
central Mexico (loc. MX-82-37; see Locality Descrip-
tions) strata assignable to the lower part of Zone 4
contain common Perispyridium spp. and no specimens
of “E.” ptyctum.

Discussion.—In California the base of Zone 4 can
best be observed in the volcanogenic-pelagic succes-
sion at Alamo Creek 90.2 m (296 ft) above the contact
with the Stanley Mountain remnant of the Coast Range
ophiolite (locs. SA-39; 81-CB-22; see Text-fig. 2; Lo-
cality Descriptions). The top of Zone 4 can best be

CORPOREAL

TAXA TAXA

Orbiculiforma
lowreyensis

Parvicingula
excelsa, n. sp. t

Parvicingula
colemani, n. sp.
“Euoyrtidium”
mclaughlini, n. sp. ptyctum
Parvicingula
Parvicingula s Parvicingula
santabarbaraensis blowi

Perispyridium

Mirifusus
baileyi

INTERVAL
ZONE

Ristola Parvicingula 4

hsui blowi talis

Hsuum
maxwelli Mirifusus
guadalupensis

Mirifusus

INTERVAL
ZONE

Mirifusus
guadalupensis

Obesacapsula
morroensis

Hsuum
cuestaense

Praeconocaryomma
immodica "Hsuum*
stanleyense

Detailed Subdivision

in progress

INTERVAL
ZONE

Not Designated

Text-figure 1.—Emendation of radiolarian zones 2, 3, and 4 (Pessagno, 1977a). The terms “Oppel zone" and “interval zone" are used in
the sense of the International Subcommission on Stratigraphic Classification (1971). Primary marker taxa refer to taxa used as the primary
means of defining a zonal unit. Taxa which are used as a secondary means of defining a zonal unit are referred to as supplementary marker
taxa. In the absence of primary marker taxa supplementary marker taxa may be used with a lower level of confidence in delimiting a zonal
unit. Corporeal taxa include taxa which make their first or last appearance within the body of a zonal unit. The relationship between the
radiolarian zones, ammonite zones, and Upper Jurassic chronostratigraphic units is shown in Text-figure 3.

observed in the Great Valley sequence of Northern
California at Grindstone Creek (Glenn County) and
McCarty Creek (Tehama County) where it conforms
closely to the top of the upper Tithonian Buchia sp.
aff. B. okensis Zone (Jones, Bailey, and Imlay, 1969;
Pessagno, 1977b). At Grindstone Creek rare Ristola
procera (Pessagno, 1977a) occurs at loc. NSF-804 and
abundant R. procera and rare R. altissima (Rüst, 1885)
occur at loc. NSF-805. Buchia sp. aff. B. okensis (Pav-
low, 1907) and Lytoceras sp. were collected from un-
derlying strata at loc. NSF-803 (identifications by D.
L. Jones, USGS; see Locality Descriptions). The first
specimens of Buchia uncitoides (Pavlow, 1907) occur
in overlying strata at loc. NSF-808. At McCarty Creek
sample loc. NSF-838 occurs in the uppermost part of
the Buchia sp. aff. B. okensis Zone just below the con-
tact with the overlying B. uncitoides Zone of the Ber-
riasian. Rare specimens of R. procera occur at loc.
NSF-838 but were not observed in overlying strata
assignable to the B. uncitoides Zone (Pessagno, 1977b,
fig. 2).

In east-central Mexico, Zone 4 Radiolaria have been
observed at locality MX-82-37 in the upper, thin-bed-
ded portion of the Taman Formation [= lower Pi-
mienta of Cantu Chapa (1971); see Locality Descrip-
tions]. The radiolarian assemblage at this locality
includes Parvicingula colemani Pessagno and Blome,
n. sp., Hsuum mclaughlini Pessagno and Blome, n. sp.,
common Perispyridium spp., Vallupus hopsoni Pes-
sagno and Blome, n. sp., and Acanthocircus dicrano-
canthos (Squinabol, 1914). The concurrence of Peri-
spyridium (Dumitrica, 1978), with Parvicingula jonesi
suggests an equivalence to the lower part of Zone 4.
The MX-82-37 horizon occurs above the final occur-
rence of the pectenacid Aulacomyella Furlani, 1910,
and hence is above the Virgatosphinctes mexicanus—
Aulacomyella neogeae Zone of Cantu Chapa (1971).
Cantu Chapa's V. mexicanus-A. neogeae Zone in-
cludes the uppermost part of the lower, more mas-
sively-bedded portion of the Taman Formation,
whereas his overlying Mazapilites Zone includes the
lower part of the upper, thin-bedded portion of Taman
Formation in its type area. It can be established from
preliminary investigations by Longoria that hyaline
calpionellids assignable to the lower part of Zone A [=
Crassicollaria Zone of Remane (1969, 1978)] occur in
the lowermost part of the upper, thin-bedded Taman
Formation. As a result, by the definition of lower and
upper Tithonian utilized herein, the MX-82-37 hori-
zon and part or all of Cantu Chapa's Mazapilites Zone
should be assigned to the upper Tithonian.

BULLETIN 320

ZONE 3
(Mirifusus baileyi Zone)

Type of zone. —Interval zone (see Text-fig. 1).
Primary marker taxa.—

Base: First appearance of Mirifusus baileyi Pes-
sagno, 1977a. See discussion below and System-
atic Paleontology.

Top: The top of Zone 3 occurs immediately below
the biohorizon defined by the first occurrence
of the primary marker taxa defining the base of
Zone 4.

Supplementary marker taxa.—

Base: First appearance of Parvicingula blowi Pes-

sagno, 1977a and Ristola hsui (Pessagno, 19772).

Corporeal taxa.— Turanta Pessagno and Blome,
1982, Mirifusus guadalupensis Pessagno, 1977a,
Hsuum maxwelli Pessagno, 19772, s.s., Saitoum pagei
Pessagno, 1977a (see Text-fig. 1).

Discussion.—Pessagno (19772) originally believed
that Mirifusus baileyi Pessagno, 1977a, evolved from
M. guadalupensis Pessagno, 1977a. We now believe
that M. baileyi evolved from a M. mediodilatata (Rüst,
1885) ancestor. Baumgartner, DeWever, and Kocher
(1980) include M. baileyi under M. mediodilatata. Our
investigations indicate that these taxa are not only dis-
tinct morphologically, but also have significantly dif-
ferent ranges. In continuous sections at Point Sal and
Alamo Creek (Stanley Mountain), M. baileyi always
makes its first appearance well above that of M. me-
diodilatata (Text-fig. 2). At Point Sal, for example, M.
mediodilatata first occurs at loc. NSF-904 and M. bai-
leyi first occurs at loc. NSF-908 at 4.5 m (15 ft) and
13.4 m (44 ft), respectively, above the contact with the
Coast Range ophiolite (cf. Pessagno, 1977a, text-fig.
3b). Detailed studies (Pessagno and Blome, in prep.)
at Alamo Creek (Stanley Mountain remnant, Coast
Range ophiolite) indicate that M. mediodilatata first

Text-figure 2.— Correlation of volcanogenic-pelagic strata above
the Coast Range ophiolite at Point Sal (Santa Barbara County), Al-
amo Creek (San Luis Obispo County), and at Llanada (San Benito
County, California). Numbering of localities 2, 3, and 7 corresponds
to that used by Hopson, Mattinson, and Pessagno (1981). The reader
is referred to the above report for a more detailed lithostratigraphic
summary at these localities.

Note that at Llanada (loc. 7) lenticular masses of green tuffaceous
radiolarian chert in tuff breccia rest in sedimentary contact beneath
strata of the Great Valley sequence containing Buchia piochii (Gabb,
1869). The cherts contain a radiolarian assemblage assignable to the
lower part of Zone 4 (upper Tithonian). Note also that the lower
part of the succession above the Coast Range ophiolite at Point Sal
(loc. 2) and Alamo Creek (loc. 3) is often too recrystallized to yield
a significant number of identifiable Radiolaria. Hence, the absence
of Mirifusus Pessagno, 1977a (first occurrence marks base of Zone
2), in the lowermost part ofthe Point Sal and Alamo Creek sequences
may be diagenetically controlled.

JURASSIC RADIOLARIAN ZONATION: PESSAGNO ET AL.

J

A A

;

==

MM |

POINT SAL

E + = =

E mim om oad qeu E bee

F. aw m des A

E o Lo E: à

* E g eem, Oum Cj e E

5 3 $ EL 9 z v

m $ S 3 E

o [^ a n z o E

e E [^5.
e af fq [os
El [6] == ÍA
M =f a

POINT SAL

12 BULLETIN 320

appears at loc. NSF-972, whereas M. baileyi first ap-
pears at loc. SA-31. These samples occur at 21 m (69.5
ft) and 62.1 m (204 ft), respectively, above the contact
with the ophiolite.

A reanalysis of the samples studied by Pessagno
(1977a) indicates that at Point Sal M. guadalupensis
actually ranges above the base of Zone 3. M. guada-
lupensis occurs at loc. NSF-908 and loc. NSF-909, 13.4
m (44 ft) and 15.8 m (52 ft), respectively, above the
contact with the ophiolite. Thus, an interval of con-
currence exists between the first occurrence of M. bai-
leyi and the final occurrence of M. guadalupensis in
the lower part of Zone 3. To date, we have not observed
the concurrence of M. baileyi and M. guadalupensis in
the Alamo Creek section (Text-fig. 2).

It should be noted that Subzone 2B of Pessagno
(1977a, 1977b) is included herein in the lower part of
Zone 3. The top of this subzone and accordingly, the
top of Zone 2 were first defined by the final appearances
of Emiluvia hopsoni Pessagno, 1977a, Perispyridium
ordinarium (Pessagno, 1977a), and Hsuum maxwelli
Pessagno, 1977a, s.s. Studies of the volcanogenic-pe-
lagic succession at Alamo Creek indicate that P. or-
dinarium and E. hopsoni range into the lower part of
Zone 4 (loc. SA-43B; see Locality Descriptions). The
final appearance of H. maxwelli s.s. remains the only
one of Pessagno’s original criteria for defining the top
of Subzone 2B. We feel that it is unwise to delimit the
top of a zonal unit on the basis of a taxon that is not
distinctive.

ZONE 2
(Mirifusus guadalupensis Zone)
[formerly Subzone 2A of Pessagno
(1977a, 1977b)]

Type of zone.—Interval zone (see Text-fig. 1).

Primary marker taxa.—

Base (only): First appearance of Mirifusus Pessa-
gno, 1977a.

Top: The top of Zone 2 occurs immediately below
the biohorizon defined by the first occurrence
of Mirifusus baileyi Pessagno, 1977a.

Supplementary marker taxa.—

Base (only): First appearance of Mirifusus gua-
dalupensis Pessagno, 1977a, and Obesacapsula
morroensis Pessagno, 1977a.

Corporeal taxa.—“Hsuum” stanleyense Pessagno,
1977a, Hsuum cuestaense Pessagno, 1977a, Praeco-
nocaryomma immodica Pessagno and Poisson, 1981
(see Text-fig. 1).

Discussion.—In continuous volcanogenic-pelagic
successions at Point Sal (Santa Barbara Co., Calif.) and
Alamo Creek (San Luis Obispo Co., Calif.) Mirifusus

Pessagno, 1977a, first occurs somewhat above the con-
tact with the underlying Coast Range ophiolite. At Point
Sal Mirifusus is first recorded at loc. NSF-904, 4.5 m
(15 ft) above the contact with the ophiolite. At Alamo
Creek Mirifusus is first recorded at loc. SA-5, 4.7 m
(15.5 ft) above the contact with the underlying ophio-
lite. Because strata at both localities become more re-
crystallized below the horizons with Mirifusus, its ab-
sence may be controlled diagenetically. “Eucyrtidium”
ptyctum Riedel and Sanfilippo, 1974, first occurs at the
base of the section at Point Sal (loc. NSF-900; cf. Pes-
sagno, 1977a). Itis now clear from our North American
studies that this taxon makes its first appearance below
the first occurrence of Mirifusus and accordingly the
base of Zone 2.

ZONE 1
(Parvicingula Zone)

Type of zone. —Interval zone (see Text-fig. 1).

Primary marker taxa.—
Base: First occurrence of Parvicingula Pessagno,
1977a.
Top: On an interim basis, the top of Zone 1 occurs
immediately below the biohorizon defined by
the first occurrence of Mirifusus Pessagno, 1977a.

Supplementary marker taxa.—
Base (only): First occurrence of Perispyridium
Dumitrica, 1978.

Discussion. — This zonal unit is in the process of being
divided into subzones (Pessagno, Blome, Whalen, and
Cheng, in prep.). At least eight subzones can be rec-
ognized for the Aalenian, Bajocian, Bathonian, and
Callovian from studies nearing completion in east-cen-
tral Oregon and Alaska. Studies of radiolarian-bearing
strata in east-central Mexico should allow us to sub-
divide the Oxfordian and Kimmeridgian portions of
Zone 1.

As noted by Hopson, Mattinson, and Pessagno
(1981), “Zone 0” of Pessagno (1977a, 1977b) has been
abandoned and is in effect encompassed by the upper
part of Zone 1.

Criteria for defining the base of Zone 5 of Pessagno
(1977b) are still being re-evaluated. For the time being,
the base of Zone 5 is considered to occur above the
final occurrences of Ristola altissima (Rüst, 1885) and
R. procera (Pessagno, 1977a). The top of Zone 5 is as
defined by Pessagno (1977b).

j

JURASSIC RADIOLARIAN ZONATION: PESSAGNO ET AL. 13

INTEGRATION OF BIOSTRATIGRAPHIC
AND CHRONOSTRATIGRAPHIC DATA

Ristola altissima-—R. procera final occurrence events
(top of Zone 4)

In the California Coast Ranges these events corre-
spond closely to the top of the Tithonian and to the
top of the Buchia sp. aff. B. okensis Zone (Jones, Bailey,
and Imlay, 1969). According to Imlay and Jones (1970,
p. B12) “The beds in California that contain Buchia
aff. B. okensis (Pavlow [, 1907]) are considered to be
of latest Jurassic (late Tithonian) age because they con-
tain the ammonites Substeueroceras [Spath, 1923],
Parodontoceras [Spath, 1923], Blanfordiceras [Coss-
mann, 1907], Proniceras [Burckhardt, 1919], and Spi-
ticeras (Spiticeras) [Uhlig, 1903] and are stratigraph-
ically just beneath a sequence characterized by the
pelecypod Buchia uncitoides (Pavlow [, 1907]) and the
ammonite Spiticeras (Negreliceras) [(Djanélidzé,
1922)]."

Baumgartner, DeWever, and Kocher (1980, p. 45)
indicate that the top of their “Biochronozone” C is
dated by calpionellids as late Tithonian and that the
base of their Biochronozone D is dated by calpionellids
as early Berriasian (Early Cretaceous). The top of
Biochronozone C of these workers also corresponds to
the final occurrence of Ristola altissima (Riist, 1885).

“Eucyrtidium” ptyctum final occurrence event

Davila (in prep.) has found “E.” ptyctum Riedel and
Sanfilippo (1974) occurring with Parvicingula cole-
mani Pessagno and Blome, n. sp., P. jonesi Pessagno,
1977b, Ristola altissima (Riist, 1885), and other taxa
common to Zone 4 in the lower part of the Eugenia
Formation (Baja California Sur). Significantly, this as-
semblage was extracted from limestone nodules also
containing common Buchia piochii (Gabb, 1869) and
is, hence, late Tithonian in age. “E.” ptyctum is rare
in Zone 4 strata both in Baja California Sur and in
California (e.g., locs. SA-39 to SA-43B; Alamo Creek;
see Locality Descriptions herein).

Data presented by Baumgartner, DeWever, and
Kocher (1980, table 3b) for the Mediterranean area
and various deep sea sites and data from California
likewise seem to indicate that “E.” ptyctum becomes
extinct below the top of the Tithonian.

Parvicingula jonesi first occurrence event

In California P. jonesi Pessagno, 1977b, has never
been found below the Buchia piochii Zone (upper Ti-
thonian). In the Lowrey area of the northern Coast
Ranges it has been only observed as low as the middle
part of the B. piochii Zone (loc. NSF-821). However,
in the Geysers—Clear Lake area (cf. McLaughlin and

Pessagno, 1978), it has been observed 76 m (249 ft)
above the depositional contact with the Coast Range
ophiolite at locality MG-77-3. Radiolaria occurring at
this locality, in addition to P. jonesi, include P. cole-
mani Pessagno and Blome, n. sp., P. excelsa Pessagno
and Blome, n. sp., and P. blowi Pessagno, 1977a. Else-
where in the same area strata that rest in depositional
contact on the Coast Range ophiolite contain B. piochii
(Gabb, 1869) and possibly represent the lower part of
the B. piochii Zone (loc. 17 of McLaughlin and Pes-
sagno, 1978, p. 722, table 2).

No specimens of P. jonesi Pessagno, 1977b, were
observed in the continuous volcanogenic-pelagic
successions above the Coast Range ophiolite at Point
Sal or at Stanley Mountain (Alamo Creek) (e.g., locs.
SA-39 through SA-43; see Locality Descriptions). Fur-
thermore, we have not observed P. jonesi where lower
Zone 4 volcanogenic-pelagic strata immediately un-
derlie Great Valley sequence strata containing B. pi-
ochii (Gabb, 1869). At Llanada (Bitterwater Canyon;
loc. SA-58), this contact is clearly a depositional con-
tact.

In east-central Mexico near the village of Taman,
San Luis Potosi, Parvicingula jonesi Pessagno, 1977b,
occurs in a lower Zone 4 assemblage that is assignable
to the Mazapilites Zone of Cantu Chapa (1971) (see p.
11 and loc. MX-82-37, Locality Descriptions).

Mirifusus first occurrence event

North America.—New biostratigraphic data from
east-central Mexico and Northern California indicate
that the first occurrence of Mirifusus Pessagno, 1977a,
and accordingly the base of Zone 2 occurs in the up-
permost part of the lower Kimmeridgian or in the up-
per Kimmeridgian. Jones (1975, p. 330) found Buchia
rugosa (Fischer, 1830-1837) in the California Coast
Ranges near Paskenta (loc. 74-JP-1 of Jones; see Lo-
cality Descriptions). Imlay (1980, p. 63) stated that
“Assignment to the late Kimmeridgian is also favored
by the presence of a few specimens that bear very fine
ribs, as on B. concentrica (Sowerby), and by the ab-
sence of B. mosquensis (Von Buch) (D. L. Jones, oral
communication, 1975), an associate of B. rugosa, which
becomes more common upward.” The absence of B.
mosquensis (Von Buch, 1844) from the assemblage does
not appear to be a significant factor. B. mosquensis
sometimes occurs with B. concentrica (Sowerby, 1827)
in both Mexico and northern Alaska. Imlay (1980, pp.
30, 31) noted that Burckhardt (1906, pp. 144, 155;
1912, pp. 50, 67, 80) recorded species of “Aucella”
which are now referred to as B. concentrica and B.
mosquensis in the lower part of a bed containing Glo-
chiceras sp. cf. G. fialar (Oppel, 1862-63). In northern

Alaska Imlay (1955, p. 83) noted an association of B.
concentrica, B. mosquensis, and B. rugosa (Fischer,
1830-1837) at USGS Mesozoic localities 22761 and
22766. From other data presented by Imlay (1980, pp.
24, 25; fig. 15) it would appear that the top of the
horizon of concurrence (= final appearance of B. con-
centrica) of all three species of Buchia equates with the
top of the horizon characterized by the presence of
Glochiceras fialar, the base of the horizon of concur-
rence (= first occurrence of B. rugosa and B. mos-
quensis) is questionably correlated with the base of the
G. fialar “Zone” (Text-fig. 3). The Glochiceras fialar
Assemblage is in turn correlative with the eudoxus
Zone and the underlying mutabilis Zone of north-
western Europe and the eudoxus and acanthicum zones
of the Tethys (Text-fig. 3).

The association of B. rugosa (Fischer, 1830-1837)
at locality 74-JP-1 (Jones, 1975) with some specimens
that are transitional to Buchia concentrica (Sowerby,
1827) suggests an equivalence to the interval of Buchia
concurrence discussed above. Pessagno (1977a) orig-
inally assigned the Radiolaria from the Jones’s Buchia
rugosa locality to his Subzone 2A (= Zone 2 herein)
and noted the presence of Hsuum cuestaense Pessagno,
1977a, and “H.” stanleyense Pessagno, 1977a. Re-
cently, a fragment of Mirifusus sp. was found during a
careful re-examination of the residue.

Mirifusus Pessagno, 1977a, also occurs in the type
Taman Formation (Heim, 1926) of east-central Mex-
ico. In its type area near the village of Taman, San
Luis Potosi, the Taman Formation can be divided into
an upper thin-bedded limestone unit and a lower more
massively-bedded unit. The lower more massively-
bedded unit is characterized by the presence of lime-
stone concretions in its upper part. Mirifusus was re-
covered at locality MX-82-8 from the lower, more
massively-bedded unit. Investigations recently initi-
ated by Pessagno and Longoria indicate that the MX-
82-8 horizon is slightly above the first occurrence of
Aulacomyella (Furlani, 1910). According to Cantu
Chapa (1971, p. 27; see also Imlay, 1980, p. 31) 4u-
lacomyella ranges from his Idoceras Zone (= upper
lower Kimmeridgian) to his Virgatosphinctoides mex-
icanus-Aulacomyella neogeae Zone (lower Tithonian).
Locality MX-82-8 is 1.2 km (straight line) north-north-
east of locality MX-80-20 where an ammonite sub-
mitted to Dr. R. W. Imlay (USGS, Washington, D.C.)
for identification was tentatively identified as Subneu-
mayria profulgens (Burckhardt, 1906) (Imlay, written
commun., 1980). Subneumayria Spath, 1924, accord-
ing to Arkell, Kummel, and Wright (1957, p. L327),
is characteristic of the ““Idoceras beds" in Mexico and,
hence, occurs at a horizon equivalent to the Idoceras

BULLETIN 320

Zone of Cantu Chapa (1971). Aulacomyella also occurs
at this locality in the same bed containing the am-
monite specimen. Significantly, no specimens of Mir-
ifusus are present at locality MX-82-3, which is situ-
ated 0.3 km north-northeast of locality MX-80-20 (see
Locality Descriptions). In that the MX-82-8 horizon
occurs above the MX-80-20/82-3 horizon in the Ta-
man succession, it is at least slightly younger. There-
fore, it is likely that the Mirifusus-bearing assemblage
at locality MX-82-8 is either assignable to the upper
part of the Idoceras Zone (= upper lower Kimmeridg-
ian) or the lower part of the Glochiceras gr. fialar Zone
(= lower upper Kimmeridgian) of Cantu Chapa (1971).
The precise dating of the Mirifusus first occurrence
event in east-central Mexico awaits further investiga-
tion by Pessagno and Longoria.

In summary, the North American evidence, though
neither abundant nor absolute, suggests that Mirifusus
Pessagno, 1977a, first occurs in Kimmeridgian strata
that are equivalent to the lower part of the Glochiceras
gr. fialar Zone or the Idoceras Zone of Cantu Chapa
(1971). The lower part of the G. gr. fialar Zone is
correlative with the mutabilis and eudoxus zones of
Boreal northwestern Europe and with the acanthicum
and eudoxus zones of the central and southern Tethys
(Text-fig. 3). The Idoceras Zone is in turn correlative
with the upper part of the cymodoce Zone of Boreal
northwestern Europe and the divisum Zone of the Eu-
ropean central and southern Tethys (Text-fig. 3). Hence,
Mirifusus seems to make its first appearance either in
the upper part of the lower Kimmeridgian or the lower
part of the upper Kimmeridgian.

Other localities. — Data pertaining to the age of the
Mirifusus first occurrence event were also presented by
Baumgartner, DeWever, and Kocher (1980). Mirifusus
Pessagno, 1977a, extends at least to the base of Bio-
chronozone A of these workers. However, they stated
that there are indications of an Oxfordian age for the
upper part of Biochronozone A and offered supporting
biostratigraphic data. Their most meaningful data come
from the Romanian Carpathians and from DSDP Site
367 (Cape Verde Basin). Baumgartner, DeWever, and
Kocher (1980, p. 45) admit that their data depend on
assumptions and that an early Kimmeridgian age for
Biochronozone A cannot be excluded.

Romanian Carpathians.—In the Romanian Carpa-
thians Baumgartner, DeWever, and Kocher (1980) re-
covered Mirifusus from four of five samples from the
“Jasper Beds.” The Jasper Beds contain no fossils other
than Radiolaria. As a result, their age can only be
deduced by superposition. According to these workers
the Jasper Beds overlie late Bathonian deposits with
“Belemnites” subhastatus Quenstedt or early Callo-

JURASSIC RADIOLARIAN ZONATION: PESSAGNO ET AL. 15

vian nodular limestones with ammonite faunas be-
longing to the macrocephalus and calloviense Zones
(Bancila, 1941; Patrulius, 1969). Baumgartner, De-
Wever, and Kocher (1980, p. 29) state that “The Jasper
Beds are in turn overlain by nodular and cherty lime-
stone (Aptychus Beds) attributed to the late Oxford-
ian-early Kimmeridgian (Jekelius, 1920-21; Bancila,
1941; Turculet, 1971) based on the presence of am-
monites and aptychi such as Aspidoceras acanthicum
[Oppel, 1862-1863], Sowerbyceras tortisulcatus (d’Or-
bigny [, 1849]), Streblites tenuilobatus (Oppel [, 1862-
1863]), Taramelliceras sp., Hemihaploceras sp., La-
mellaptychus lamellosus (Parkinson [, 1811]), L. spar-
silamellosus (Guembel [, 1861]), L. rectecostatus (Pe-
ters [, 1854]), etc. Hence, it can be stated that the Jasper
Beds are no older than early Callovian and no younger
than late Oxfordian." This list of megafossil taxa is
hardly indicative of the upper Oxfordian. It is indic-
ative rather of the lower and upper Kimmeridgian as
defined herein (cf. Text-fig. 3 and discussion of data
from DSDP Site 367, Cape Verde Basin). The assem-
blage cited above is more characteristic of the Acan-
thicus Beds in Romania (Neumayr, 1873; Herbich,
1878) and elsewhere in southern Europe (Arkell, 1956).

In the Hághimas (Bicaz Gorge-Lacu Rosu area, Ro-
manian Carpathians) Dragastan (1975, p. 124) stated
that the Acanthicus Beds are 30 to 32 m thick. The
lower 20 m are assigned in ascending order to the
platynota, hypselocyclum, uhlandi (= divisum herein),
acanthicum, and beckeri zones. Dragastan assigned the
platynota, hypselocyclum, and uhlandi zones to the
lower Kimmeridigian and the acanthicum and beckeri
zones to the upper Kimmeridgian. The upper 10 m
include the lithographicum and ulmense zones. Ac-
cording to Westermann and Zeiss (written commun.,
1983) these latter two zones cannot be distinguished
and are currently included in the Gravesia Zone or
hybonotum Zone (lower Tithonian) of the central and
Southern Tethys (Text-fig. 3). Dragastan notes no upper
Oxfordian ammonites in the Acanthicus Beds of the
Hághimas.

The Mesozoic strata in the Hághimas Mountains
(Bicaz Gorge area) are, according to Dragastan (1975,
Pp. 123, 124, fig. 1), included in two nappes, each
displaying a different stratigraphic succession. The Jas-
per Beds (radiolarites) are included in the Bucovienne
Nappe whereas the Acanthicus Beds are included in
the Hághimas Nappe. In the Bucovienne Nappe the
Jasper Beds (radiolarites) and associated siliceous
sandstones and shales overlie Middle Jurassic (Bajo-
cian-Bathonian) limestones containing Bositra buchii
(Roemer, 1836) and are in turn overlain unconform-
ably either by the Beds of Lunca (Tithonian-Neoco-

mian) with numerous aptychi or by Barremian to Al-
bian wildflysch (Dragastan, 1975). In the Hághimas
Nappe it is difficult to understand how the Jasper Beds
can be dated as strictly late Callovian to Oxfordian in
that underlying strata are Bathonian (youngest possible
age) and overlying strata (Beds of Lunca) are Tithonian
to Neocomian.

The age of the Jasper Beds in the Romanian Car-
pathians must be examined through a window of com-
plex structure and stratigraphy as well as differences
of opinion pertaining to the ranges of fossils in over-
lying strata. Bancila (1941) studied the stratigraphy in
the Hághimas in the Ciuc Region immediately to the
south of the Bicaz Gorge-Lacu Rosu area. According
to Bancila (1941, p. 71) the Jasper Beds overlie fos-
siliferous Dogger sandstones and are in turn overlain
by the Acanthicus Beds (Kimmeridgian). One suspects
because of the proximity of this area to that studied
by Dragastan (1975) that the contact between the Jas-
per Beds and the Acanthicus Beds in the Ciuc Region
is a tectonic contact (see discussion above).

In the Raráu-Breaza area of the northeastern Ro-
manian Carpathians the Jasper Beds are either overlain
conformably by the Aptychus Beds (e.g., between Mol-
dova Valley and Valea Caselor) or unconformably by
Lower Cretaceous strata (e.g., wildflysch at Pecistea)
(Turculet, 1971). Turculet (1971, fig. 5) divided the
Aptychus Beds into a lower horizon (upper Oxfordian-
lower Kimmeridgian) and an upper horizon (upper
Kimmeridgian, Tithonian, Berriasian). In that Tur-
culet appears to follow the older definition of the Kim-
meridgian (Arkell, 1956; Gasiorowski, 1962, table 1)
all of his lower Kimmeridgian equates with both the
lower and upper Kimmeridgian as defined herein. Tur-
culet (1971, pp. 32, 38) correlated his upper Aptychus
horizon with Zones VI and VII of Gasiorowski. Ga-
siorowski equated the lowermost part of Zone VI with
the beckeri Zone (= uppermost Kimmeridgian herein);
the top of Zone VI corresponds to the top of the Ti-
thonian whereas Zone VII corresponds to the Berria-
sian. Except for calpionellids in the upper Tithonian
and Berriasian other fossils (e.g., ammonites) are rare
in the Aptychus Beds.

Turculet's assignment ofthe lower Aptychus horizon
to the *upper Oxfordian-lower Kimmeridgian" is neb-
ulous. It is not clear whether he meant to indicate that
this horizon definitely included both upper Oxfordian
and "lower" Kimmeridgian strata or that it included
strata that might be placed anywhere in the upper Ox-
fordian to "lower" Kimmeridgian interval. The fact
that Turculet made no attempt to correlate this interval
with Gasiorowski's Zones IV and V appears to support
the latter assumption.

Turculet’s chronostratigraphic assignment of the
lower Aptychus horizon is based primarily on the pres-
ence of three Aptychi (Turculet, 1971, pl. 42): La-
mellaptychus grupa A, aff. rectecostatus (Peters, 1854)
em. Trauth f. typ. Trauth, 1938; Lamellaptychus, gru-
pa B, sparsilamellosus (Guembel, 1861) f. typ. Trauth,
1938; Lamellaptychus grupa B, lamellosus (Parkinson,
1811) em. Trauth f. typ. Trauth, 1938. A fourth species
is listed. However, it is only known from Romania.
The other three taxa also occur in Kimmeridgian, Ti-
thonian, and Berriasian strata elsewhere in Europe
(Turculet, 1971, pl. 42).

In our opinion the assignment of even a portion of
the lower Aptychus horizon to the upper Oxfordian
based on these long-ranging taxa would be tenuous.
Gasiorowski (1962, p. 45) indicated that the base of
his Zone IV (= bimammatum Zone; Text-fig. 3) is the
moment of diversification among aptychi. Whereas
Gasiorowski (1962, pp. 46-52) cited as many as 15
specific and (or) subspecific taxa from Zone IV in the
western Carpathians, Swabian Alb, Friburg Alps, and
other localities, Turculet cited only the four taxa noted
above from the lower Aptychus horizon.

During the 14th European Micropaleontological
Colloquium the senior author with the help of Dr.
Paulian Dumitrica (Instit. Geol. and Geophys., Bu-
charest) collected eight samples from the radiolarites
(Jasper Beds) exposed along the highway near Lacu
Rosu. Sample RO-8A from near the base of the ra-
diolarian chert exposure contains Mirifusus guadalu-
pensis Pessagno, 1977a (fragment), M. mediodilatata
(Rúst, 1885) (fragment), Hsuum maxwelli Pessagno,
1977a, s.s., Acanthocircus variabilis (Squinabol, 1914),
Tritrabs rhododactylus Baumgartner, 1980a, and Ar-
chaeospongoprunum imlayi Pessagno, 1977a. The
presence of M. guadalupensis definitely indicates that
this sample is assignable to either Zone 2 (see emended
definition herein) or to the lower part of Zone 3.

Although Baumgartner, DeWever, and Kocher (1980,
table 1) did not note Mirifusus at their Lacu Rosu
locality in the Haghimas, they did record its presence
in the Jasper Beds at localities in the Drocea Mountains
and Rárau Mountains (eastern Carpathians). Unfor-
tunately, their “blanket treatment” of the megafossil
data is misleading.

Cape Verde Basin (DSDP Site 367).—As noted in
Baumgartner, DeWever, and Kocher (1980), data per-
taining to the integration of biostratigraphic data for
radiolaria with those of other fossil groups are pre-
sented for Deep Sea Drilling Project [DSDP] Site 367
(Cape Verde Basin). Unfortunately, most of the data
pertaining to the age of their Biochronozone A or the
Mirifusus first occurrence event are hardly compelling.

BULLETIN 320

According to Baumgartner, DeWever, and Kocher
(1980, table 1), Mirifusus occurs near the base of the
sedimentary section in Core 37 (sect. 1; 147-149 cm).
No megafossils were found at this horizon. However,
benthonic foraminifera (Kuznetsova and Siebold, 1978)
and dinocysts (Williams, 1978) were recorded in un-
derlying Core 38. Kuznetsova and Siebold (1978, p.
522) assign the lower part of the section to the late
Oxfordian based on the association of numerous Den-
talinae, Lenticulina quenstedti (Guembel, 1862), L.
uhligi (Wisniowski, 1890), L. semiexpleta (Schwager,
1865) and the “Spirillinae.” Curiously, they stated
(1978, p. 522) that the boundary between the Kim-
meridgian and Oxfordian cannot be placed utilizing
their foraminiferal assemblages.

Williams (1978, p. 783) on the basis of his study of
the dinoflagellates, found diagnostic assemblages in
Cores 38 and 35. He stated “The dinocysts include
Epiplospheara bireticulata Klement [, 1960], Prolix-
osphaeridium mixtispinosum (Klement) Davey [, 1966],
Scriniocassis dictyotum (Cookson and Eisenack) Beju
[, 1971], Sirmiodinium grossi Alberti sensu Gitmez
and Sarjeant, 1972, Systematophora fasciculigera Kle-
ment [, 1960], and S. turonica (Alberti) Downie and
Sarjeant [, 1964] (figure 2). E. bireticulata, P. mixti-
spinosum, and S. grossi sensu Gitmez and Sarjeant are
only known from the Kimmeridgian (Sarjeant, 1975).”
Riley and Sarjeant (1972) indicate that E. bireticulata
Klement, 1960, and P. mixtispinosum (Klement, 1960)
range from the cymodoce Zone (= upper lower Kim-
meridgian herein) to the eudoxus Zone (= middle up-
per Kimmeridgian herein) of Germany whereas the
third species, S. grossi Alberti, 1961, sensu Gitmez
and Sarjeant (1972), ranges from the cymodoce Zone
to the rotunda Zone (= upper lower Tithonian herein)
of England (Text-fig. 3). It should be noted that Wil-
liams (1978), Riley and Sarjeant (1972), and Sarjeant
(1975) follow Arkell's (1956) definition of the Kim-
meridgian. By this definition even the rotunda Zone
would be included in the Kimmeridgian. Nevertheless,
their data correspond well with those from North
America.

Renz (1978) found numerous aptychi in Upper Ju-
rassic strata at DSDP Site 367. In Core 36 (sect. 2, 72-
73 cm) he recorded Laevaptychus mexicanus (Castillo
and Aguillera, 1895). Castillo and Aguillera (1895, p.
45) originally described this taxon from Upper Jurassic
strata in the Sierra Catorce, San Luis Potosi, Mexico,
but did not cite its stratigraphic position. Renz assumed
that Core 36 is of late Oxfordian age because of its
position below Core 35, sections 4 and 5 where the
aptychi are supposedly also late Oxfordian. However,
it should be noted that detailed studies of the Upper

JURASSIC RADIOLARIAN ZONATION: PESSAGNO ET AL. 17

Jurassic stratigraphy and ammonite faunas of the Sier-
ra Catorce by Verma and Westermann (1973, pp. 107-
320) indicate that the oldest fossiliferous strata are
Kimmeridgian in age and are included in the El Pastor
Member of the La Caja Formation. Verma and Wes-
termann record Idoceras sp. cf. I. inflatum Burckhardt,
1906, J. sp. cf. I. mutabilis Burckhardt, 1912, and J.
ex gr. I. neohispanicum Burckhardt, 1912, from 3 m
(9.8 ft) above the base of the El Pastor Member. These
ammonites are clearly assignable to the Idoceras Zone
(Cantu Chapa, 1971; Imlay, 1980) and are indicative
of late early Kimmeridgian (= upper part of cymodoce
Zone of northwest Europe; cf. Text-fig. 3). Renz (1978,
p. 502) recorded the following taxa from Core 35 (sects.
4 and 5): Lamellaptychus sp. cf. L. thoro (Oppel, 1863),
L. (?) lithographicus (Oppel, 1863), L. sp. cf. L. cras-
sicauda (Quenstedt, 1846-49), L. sparcilamellosus
(Guembel, 1861), L. mucrocostatus Trauth, 1938, and
Laevaptychus latus seriporus Trauth, 1931. Most of
these aptychi, according to Renz, occur in both the
Oxfordian and Kimmeridgian; some, such as L. mu-
crocostatus and L. thoro, are also known from the Ti-
thonian. Renz indicated that one species, L. sparci-
lamellosus, is only known from the upper Oxfordian.
However, Turculet (1971, pl. 42) showed this taxon to
also occur in the Kimmeridgian and Tithonian. Fi-
nally, from overlying Core 34 (sect. 4) Renz recorded
Punctaptychus punctatus (Volz, 1837), Granulapty-
chus planulati (Quenstedt, 1858), Lamellaptychus
Dleiadensis Trauth, 1938, and L. latus vermiporus
Trauth, 1931. Of these aptychi, G. p/anulati is the most
Significant. According to Renz (1978, p. 503) this ap-
tychus “has repeatedly been observed within the body
chambers of Perisphinctidae, especially of Lithacoce-
ras ulmensis (Oppel, 1858).” Ziegler (1971, p. 65, fig.
22) indicated that Lithacoceras ulmensis (Oppel, 1858)
ranges from the upper part of the beckeri Zone to the
top of the Gravesia Zone in southwestern Germany
(uppermost Kimmeridgian to lowermost Tithonian)
(Text-fig. 3). Renz, in part following the earlier defi-
nition of the Kimmeridgian (e.g., Arkell, 1956) as-
Signed this core interval to the lower Kimmeridgian.

Summary. —

(1) Data from California and elsewhere in western
North America indicate that Mirifusus Pessagno, 1977a,
Occurs in upper Kimmeridgian strata that are correl-
ative with the eudoxus and the mutabilis zones of
northwestern Europe (Text-fig. 3).

(2) In east-central Mexico, Mirifusus first occurs in
the lower more massively-bedded part of the Taman
Formation at a horizon (loc. MX-82-8) that is above
the first occurrence of the pectenacid Aulacomyella
(Furlani, 1910) and somewhat above strata containing

an ammonite that is characteristic of the Idoceras beds
in Mexico (= Idoceras Zone of Cantu Chapa, 1971).
Based on the range of Aulacomyella and the presence
of this ammonite, it can be established, therefore, that
Mirifusus makes its first appearance in strata that are
no older than the ZIdoceras Zone (late early Kimme-
ridgian). It is likely that this horizon is no younger than
the lower part of the Glochiceras gr. fialar Zone (late
Kimmeridigian) of Cantu Chapa (1971). An assign-
ment of the MX-82-8 horizon to this latter zonal unit
is further reinforced by the fact that it appears to occur
more or less along strike with a locality near La Cuesta
where Burckhardt (in Heim, 1926) identified Glochi-
ceras fialar (Oppel, 1858) and other ammonites char-
acteristic of the G. gr. fialar Zone of Cantu Chapa
(1971). The Idoceras and G. gr. fialar Zones of the
Mexican Tethys are correlative with the divisum, acan-
thicum, and eudoxus zones of the European Tethys
(Text-fig. 3).

(3) In the Romanian Carpathians, Mirifusus Pes-
sagno, 1977a, occurs near the base of the Jasper Beds
in the Haghimas Nappe succession (Bicaz Gorge-Lacu
Rosu area). It also was noted by Baumgartner, De-
Wever, and Kocher (1980) in the Jasper Beds in the
Raráu and Drocea Mountains (eastern Carpathians).
Unfortunately, the age of the Jasper Beds can only be
deduced by superposition; they overlie strata of Batho-
nian or early Callovian age and underlie aptychus-
bearing strata whose precise age is controversial. In the
Raráu Mountains, Turculet (1971) indicated that the
lower Aptychus horizon included strata of both late
Oxfordian and early Kimmeridgian age. Curiously, all
of the taxa he utilized to support this determination
also occur in the Kimmeridgian, Tithonian, and Ber-
riasian. Hence, a Kimmeridgian age for the Jasper Beds
cannot be excluded.

(4) Data from DSDP Site 367 (Cape Verde Basin)
derived from studies of benthonic foraminifera, apty-
chi, and dinoflagellates are contradictory and contro-
versial. Baumgartner, DeWever, and Kocher (1980)
established that Mirifusus occurs near the bottom of
the section in Core 37. Renz (1978) maintained that
the interval from Core 36 (sect. 2: 72-73 cm) to Core
35 (sect. 4: 147-148 cm) is upper Oxfordian in spite
of the fact that the majority of his aptychi occur in
both the Oxfordian and Kimmeridgian. One aptychus,
Laevaptychus mexicanus (Castillo and Aguillera, 1895)
from Core 36, was originally described from Mexico
in strata that cannot be older than the Zdoceras Zone
(latest early Kimmeridgian). The presence of Granu-
laptychus planulati (Quenstedt, 1858), which has been
elsewhere observed to be associated with the body
chamber of Lithacoceras ulmensis (Oppel, 1858),

indicates an equivalence of Core 34 (sect. 4) to the
upper part of the beckeri Zone and all of the overlying
Gravesia Zone (= uppermost Kimmeridgian to low-
ermost Tithonian). Kuznetsova and Siebold (1978) as-
signed the interval from Core 38 to Core 35 to the
upper Oxfordian on the basis of their studies of the
benthonic foraminiferal assemblage. However, they
admitted they could not place the boundary between
the Oxfordian and Kimmeridgian on the basis of their
investigation. Williams (1978) found a diagnostic di-
noflagellate assemblage in Core 38 (bottom of sedi-
mentary section) and in Core 35 and assigned this
interval to the Kimmeridgian. Significantly, three
species, Epiplosphaera bireticulata Klement, 1960,
Prolixosphaeridium mixtispinosum Klement, 1960, and
Siriodinium grossi Alberti, 1961 sensu Gitmetz and
Sarjeant, 1972, make their first appearance in the cy-
modoce Zone (= upper lower Kimmeridgian) of Ger-
many and England. Two species, E. bireticulata and
P. mixtispinosum, range no higher than the eudoxus
Zone (middle upper Kimmeridgian; see Text-fig. 3).

Parvicingula first occurrence event
(base of Zone 1)

The first occurrence of Parvicingula Pessagno, 1977a,
occurs at a time of major change in the Mesozoic ra-
diolarian assemblage. Immediately below this horizon
a number of taxa (e.g., Canutus Pessagno and Whalen,
1982, s.s., Canoptum anulatum Pessagno and Poisson,
1981, and so forth) make their final appearance where-
as at this horizon Parvicingula Pessagno, 1977a, Peri-
spyridium Dumitrica, 1978, Higumastra Baumgartner,
1980a, Emiluvia Foreman, 1973, and other taxa sud-
denly appear. The magnitude of this faunal break is at
least as great as that occurring between the Upper
Triassic and Lower Jurassic and ranks as one of the
most catastrophic changes in the Mesozoic radiolarian
assemblage.

In east-central Oregon (John Day Inlier) Parvicin-
gula Pessagno, 1977a, first occurs in the Warm Springs
Member of the Snowshoe Formation (Lupher, 1941;
Dickinson and Vigrass, 1965). The Warm Springs
Member (Lupher, 1941; Smith, 1980) contains a con-
tinuous succession of strata ranging in age from Early
Jurassic (latest Toarcian) to Middle Jurassic (Aalenian,
early Bajocian). Ammonite faunas from these strata
have been described by Imlay (1968, 1973). Imlay
(1968, 1973, 1980), as well as Pessagno and Blome
(1980) and Pessagno and Whalen (1982), assigned what
most workers now call Aalenian to the lower Bajocian
(see Westermann, 1979). The Aalenian is now regarded
as a valid stage that marks the base of the Middle
Jurassic. Radiolaria associated with latest Toarcian

BULLETIN 320

ammonite faunas are correlated with the levesquei Zone
of northwestern Europe, lack Parvicingula, and are as-
signed to radiolarian Zone 01 (Pessagno, Blome, Wha-
len, and Cheng, in prep.). Radiolarian faunas closely
associated with the Aalenian ammonite T'metoceras
scissum (Benecke, 1865) contain Parvicingula and
Perispyridium Dumitrica, 1978, and are definitely as-
signable to radiolarian Zone 1.

PROBLEMS OF CORRELATION

Baumgartner, DeWever, and Kocher (1980) used a
computerized treatment of radiolarian biostratigraphic
data to compile their zonal scheme. The utilization of
a technique such as that of Guex (1979) is undoubtedly
quite valuable in sorting out biostratigraphic data and
subsequently developing a means of correlation. How-
ever, such computerized techniques are still dependent
on biostratigraphic data derived from paleontological
observations. If poor judgment is used by a paleon-
tologist in identifying existing taxa or defining new
taxa, errors in correlation will result no matter how
sophisticated the technique.

As noted elsewhere in this report, we admit that
many of the taxa cited by Pessagno (1977a) in his
definition of Upper Jurassic zonal units are longer
ranging than previously believed. This soon became
evident from our own work as well as that of Baum-
gartner, DeWever, and Kocher (1980). Detailed studies
in progress in California (Pessagno and Blome, in prep.),
Baja California Sur (Davila, in prep.), and east-central
Mexico (Pessagno and Longoria, in prep.) should even-
tually define the range zones of those taxa described
by Pessagno (1977a, 1977b), but not utilized in the
present report. Many differences in ranges of taxa cited
by Baumgartner, DeWever, and Kocher represent dif-
ferences in taxonomy, often coupled with paleo-ocean-
ographic and preservational factors.

TAXONOMIC PROBLEMS AFFECTING
CORRELATION

Baumgartner, DeWever, and Kocher (1980) claimed
that Syringocapsa rotunda (Hinde, 1902) [= Obesa-
capsula rotunda (Hinde), Pessagno, 1977b (part)] oc-
curs in the upper Tithonian. Although the specimen
figured from the Berriasian by Baumgartner, DeWever,
and Kocher (1980, pl. 3, fig. 12) is most certainly O.
rotunda s.s., we have not observed this morphotype in
either the upper Tithonian of California, Baja Califor-
nia Sur, or east-central Mexico. We suspect that Baum-
gartner, DeWever, and Kocher included the form re-
ferred to herein as O. sp. aff. O. rotunda under O.
rotunda (Pl. 4, fig. 9). O. sp. aff. O. rotunda is closely
related to and most likely ancestral to O. rotunda. In

JURASSIC RADIOLARIAN ZONATION: PESSAGNO ET AL. 19

California it has been observed in the lower part of
Zone 3 at loc. NSF-908 and in the lower part of Zone
4 at loc. SA-43B (see Locality Descriptions). In Baja
California Sur this form occurs at loc. BJV-20 in a
Sample also containing common Buchia piochii (Gabb,
1869) (middle to upper Zone 4; upper Tithonian).

As far as can be determined from data from the
Western Hemisphere, O. rotunda s.s. makes its first
appearance in the Berriasian, as emphasized by Pes-
Sagno (1977b). It is difficult to determine at the present
time whether the difference in range of O. rotunda is
due to a much broader taxonomic concept on the part
of Baumgartner, DeWever, and Kocher, or is due to
paleo-oceanographic or preservational determinants.
Until this problem is studied in more detail, we will
de-emphasize the importance of O. rotunda in defining
the base of Zone 5.

Baumgartner, DeWever, and Kocher included a va-
riety of morphotypes under Parvicingula boesii (Pa-
rona, 1890) [= Ristola boesii (Parona, 1890)]. Their
figured form is considerably different in shape from
Parona’s (pl. 6, fig. 9) type specimen; it is much more
Pointed apically, less spindle-shaped, and possesses
more weakly developed circumferential ridges. As far
as can be determined, no specimens corresponding pre-
cisely to Parona's type specimen have been figured in
recent literature (see Systematic Paleontology).

Napora lospensis Pessagno of Baumgartner, De-
Wever, and Kocher bears no resemblance to N. /os-
bensis Pessagno, 1977a. It possesses a longer, slender,
Structurally different horn; longer, less massive feet;
and much less massive pore frames.

The inclusion of Mirifusus baileyi Pessagno, 1977a,
by Baumgartner, DeWever, and Kocher in M. medio-
dilatata (Rüst, 1885) serves no purpose other than to
Obscure important biostratigraphic and phylogenetic
relationships (see Systematic Paleontology and emend-
ed definition of Zone 3).

PALEOLATITUDINAL/PALEOCLIMATIC
CONSIDERATIONS

The Upper Jurassic faunas reported by Baumgart-
ner, DeWever, and Kocher (1980) from the Mediter-
ranean area, by Tippit (1981) from Oman, and from
numerous DSDP sites (e.g., Foreman, 1973, 1975;
Moore, 1973) are representative of the Central Tethys.
These faunas are characterized by the presence of Ris-
tola Pessagno and Whalen, 1982, and by the absence
of Parvicingula Pessagno, 1977a (sensu Pessagno and
Whalen, 1982). On the other hand, the Tethyan faunas
of the Taman and Pimienta formations of east-central
Mexico are characteristic of the Northern Tethys and
Possess elements in common with both the Boreal fau-

nas of California and those of the Central Tethys.
Whereas Parvicingula is absent in the Central Tethyan
Ristola assemblage, it is quite common in the Northern
Tethyan assemblage of eastern Mexico and occurs in
Boreal strata as far north as Alaska (e.g., Brooks Range).
The presence of microfossils such as calpionellids and
megafossils such as Aulacomyella Furlani, 1910, Mi-
croacanthoceras Spath, 1925, and Mazapilites Burck-
hardt, 1919, substantiates the Tethyan character of
Upper Jurassic radiolarian assemblages of eastern
Mexico. The central and northern Tethyan radiolarian
assemblages differ from those of the Boreal Realm by
being more diversified. The Pantanellidae Pessagno,
1977b (sensu Pessagno and Blome, 1980), possess four
or five times the number of species level taxa (named
and unnamed) in Tethyan faunas that they do in faunas
from the southern part of the Boreal Realm. Our stud-
ies to date indicate that pantanellids are virtually ab-
sent at higher Boreal latitudes.

In summary, these simple but yet important differ-
ences in radiolarian faunal composition allow us to
separate the Tethyan Realm into a Central Tethyan
Province characterized by Ristola Pessagno and Wha-
len, 1982, and high pantanellid diversity and a North-
ern Tethyan Province characterized by the presence of
Parvicingula Pessagno, 1977a, and high pantanellid
diversity. Faunas from the southern portion of the Bo-
real Realm are characterized by the presence of Par-
vicingula and by a dramatic drop in pantanellid di-
versity; pantanellids are apparently lacking in high
latitude Boreal Middle and Upper Jurassic strata.

DISPLACED TERRANES AND THEIR EFFECT ON
BIOSTRATIGRAPHIC CORRELATION

Most geologists now recognize that much ofthe west-
ern part of the Cordilleran region is a collage of dis-
placed terranes that were accreted to the margin of the
North American craton during Paleozoic and Meso-
zoic times. The brilliant discovery of the first of these,
the Wrangellian terrane, by Jones, Silberling, and Hill-
house (1977), revolutionized geological thinking per-
taining to the North American cordillera and indeed
to the evolution of the entire Circum-Pacific margin.
Many terranes (e.g., Wrangellia) originated at near
equatorial latitudes and have been displaced north-
ward hundreds or even thousands of kilometers from
their point of origin.

It is now apparent from our studies of the radiolarian
fauna and from paleomagnetic investigations that the
Coast Range ophiolite and its cover of volcanogenic-
pelagic strata originated at near equatorial latitudes
and was displaced northward during the course of Mid-
dle Jurassic and Late Jurassic times. Paleomagnetic

20 BULLETIN 320

data from the Stanley Mountain remnant of the Coast
Range ophiolite at Alamo Canyon (locs. SA-4 through
SA-43B herein) indicate that these ophiolitic rocks
originated 14° + 7° north or south of the Jurassic pa-
leoequator (see McWilliams and Howell, 1982). Sim-
ilar results (unpublished) have been obtained from the
Coast Range ophiolite at Point Sal (Hopson, oral com-
mun., 1983).

Investigations of the radiolarian assemblage by Pes-
sagno and Blome (in prep.) agree well with the available
paleomagnetic data. For example, at Stanley Moun-
tain, the lower 72 m (238 ft) of the succession above
the ophiolite contain the Central Tethyan Ristola Pes-
sagno and Whalen, 1982, assemblage (Zone 2 to Zone
3). A sample from 73 m (239 ft) contains the first
Parvicingula Pessagno, 1977a, and poorly preserved
pantanellids; this sample may be either representative
of the Northern Tethyan Province or the Southern
Boreal Province. The interval from 79.5 m (261 ft) to
106.4 m (330 ft) contains a Southern Boreal assemblage
with Parvicingula and poorly diversified pantanellids.
The same changes in the radiolarian assemblage have
been observed at Point Sal, Cuesta Ridge, Llanada,
and at other localities where remnants of the Coast
Range ophiolite are exposed.

It is now also apparent that the Middle and Upper
Jurassic red, manganiferous ribbon cherts of the Fran-
ciscan Complex contain a Tethyan (predominantly
Central Tethyan) radiolarian assemblage. Cherts of this
sort, bearing Tethyan radiolarian faunas, are inherent
to subduction complexes (melange belts) from Cali-
fornia to Alaska (e.g., Otter Point complex, western
Oregon; Pacific Rim complex, British Columbia).

Obviously, paleolatitudinal changes due to displaced
terranes make it difficult to establish the ranges of many
radiolarian taxa. At Stanley Mountain, for instance,
one might conclude that Parvicingula Pessagno, 1977a
(sensu Pessagno and Whalen, 1982), does not range
below Zone 3 (lower Tithonian). Yet it can be estab-
lished from the investigations of Pessagno and Whalen
(1982) that this taxon in east-central Oregon first ap-
pears at the base of Zone 1 (Middle Jurassic: Aalenian).
Fortunately, a large number of radiolarian taxa occur
in both the Tethyan and Boreal faunal realms. As a
result, it is possible to correlate Central Tethyan faunas
of Baumgartner, DeWever, and Kocher (1980) with
those of Boreal North America. The Northern Tethyan
assemblage of eastern Mexico provides an important
link in these correlations.

COMMENTS ON THE RANGES OF SELECTED TAXA

Ristola procera (Pessagno, 1977a) has a longer range
in the California Coast Ranges than it does in the Cen-

tral Tethys of southern Europe. This difference in range
may be paleolatitudinally controlled. R. procera ranges
to the top of the upper Tithonian (Buchia sp. aff. B.
okensis Zone) in the Boreal strata of the Great Valley
sequence. In southern Europe R. procera ranges no
higher than the lower Tithonian.

We agree that Acanthocircus dicranocanthos (Squi-
nabol, 1914) ranges below the base of the Berriasian.
Tippit (1981) found this taxon associated with “E.”
ptyctum Riedel and Sanfilippo, 1974, Sethocapsa cetia
Foreman, 1973 (sensu Baumgartner, DeWever, and
Kocher, 1980), and Ristola altissima (Riist, 1885) in
the Halfa Formation of Oman. In addition, we have
recently encountered A. dicranocanthos in strata as-
signable to the lower part of Zone 4 in the Taman
Formation of east-central Mexico (loc. MX-82-37; see
p. 10 and Locality Descriptions). A. dicranocanthos is
strictly a Tethyan species. In California it occurs only
in the red, manganiferous cherts of the Franciscan
Complex and has never been observed in the Boreal
strata of the Great Valley sequence or in underlying
pelagic Boreal strata below the Great Valley sequence.

Parvicingula(?) cretacea Baumgartner, 1980b (in
Baumgartner, DeWever, and Kocher, 1980; = Ristola
cretacea Baumgartner, 1980b), though distinctive, ap-
pears to be a provincial southern European species. It
has not been observed in Tethyan samples from In-
donesia, Oman, or elsewhere. Baumgartner, DeWever,
and Kocher (table 1) noted this form in two samples
from Romania and in one from Italy.

Andromeda violae Baumgartner, 1980b (in Baum-
gartner, DeWever, and Kocher, 1980, table 3b) is said
not to range above the top of “Biochronozone” B (top
of unitary association 5). The top of “Biochronozone”
Bcorresponds to the final occurrence of Mirifusus gua-
dalupensis Pessagno, 1977a. In the California Coast
Ranges we have observed A. violae in the lower portion
of Zone 4 at locality SA-43B (Alamo Canyon; see Lo-
cality Descriptions). Whether the longer range of this
taxon in California is due to paleo-oceanographic, pa-
leogeographic, preservational, or observational factors
is unknown.

CORRELATION OF ZONAL SCHEMES

Text-figure 3 is an attempt to correlate the emended
zonation proposed herein with that of Baumgartner,
DeWever, and Kocher (1980). Although there are ma-
jor differences between the faunal assemblages as noted
above, a sufficient number of taxa occur in common
to allow the correlation of some zonal units.

The base of “Biochronozone” A of Baumgartner, De-
Wever, and Kocher (1980) corresponds approximately
to the base of Zone 2 as redefined herein. The top of

|
|
|

JURASSIC RADIOLARIAN ZONATION: PESSAGNO ET AL. Dal

“Biochronozone” B, due to the final occurrence of Mi-
rifusus guadalupensis Pessagno, 1977a, corresponds to
the lower part of Zone 3 as redefined herein. Possible
points of linkage within **Biochronozone" C appear to
be the final occurrence of“ Eucyrtidium" ptyctum with-
in the middle part of Zone 4 (upper Tithonian strata
with Buchia piochii (Gabb, 1869), Baja California Sur)
and the first occurrence of Acanthocircus dicranocan-
thos Squinabol, 1914, within the lower part of Zone 4
in east-central Mexico (lower Tithonian part of Taman
Formation at loc. MX-82-37; see p. 10 and Locality
Descriptions).

ACKNOWLEDGMENTS

This project has been supported by grants from the
National Science Foundation (GA-35094, DES-72-
01528-A01, EAR-76-22029, EAR-77-22457, EAR-78-
12934, EAR-81-21550) and by funding from the
Atlantic Richfield Company, the Exxon Production
Research Company, and the Mobil Oil Corporation.

The authors wish to thank the following persons for
their help during the course of this project: Dr. D. L.
Jones (U.S.G.S., Menlo Park, CA) for his guidance and
aid in identifying many of the megafossils from the
California Coast Ranges; Dr. C. A. Hopson (Univ. of
Calif., Santa Barbara, CA) for his helpful discussions
and for his aid in collecting samples from radiolarian-
bearing strata associated with the Coast Range ophio-
lite; Dr. R. W. Imlay (U.S.G.S., U. S. Nat. Mus.,
Washington, DC) for identifying megafossils from east-
central Oregon and Mexico and for his advice pertain-
ing to the Jurassic stratigraphy of these areas; Mr. T.
Six and Mr. W. T. Rothwell for their care in taking
the scanning electron micrographs (Mr. Six also pre-
pared the text-figures); and Mr. Y. Cheng for printing
the photographs for the plates.

Finally, we wish to express our appreciation to Dr.
Shinjiro Mizutani (Nagoya University, Japan), Dr. G.
E. G. Westermann (McMaster University, Ontario,
Canada), and Dr. A. Zeiss (Universitat Erlangen-
Niirnberg, Fed. Rep. of Germany) for their thorough
review of the manuscript and many helpful sugges-
tions. We are particularly indebted to Dr. Westermann
and Dr. Zeiss for their advice pertaining to European
ammonite biostratigraphy and the correlation of
chronostratigraphic units (Text-fig. 3). We, however,
take full responsibility for the biostratigraphic and
chronostratigraphic data presented in Text-figure 3.
The subdivision of the Tithonian Stage into lower and
upper Tithonian rather than lower, middle, and upper
Tithonian is not, for example, endorsed by Wester-
mann and Zeiss.

SYSTEMATIC PALEONTOLOGY
INTRODUCTION

The concept of the morphospecies varies greatly
among radiolarian specialists. This, to a large degree,
depends on whether one is a Cenozoic or a Mesozoic
specialist and furthermore, it appears to be related to
the mode of illustrating and studying radiolarian taxa.
Most Cenozoic Radiolaria have tests comprised of
opaline silica. When specimens are properly cleaned,
their internal and external features are readily discern-
ible and can be easily illustrated using transmitted light
optics. Few, if any, Mesozoic Radiolaria have tests
comprised of opaline silica. Their tests, instead, have
been replaced by quartz, chalcedony, smectite, pyrite,
limonite, and calcite. Even specimens whose tests are
still siliceous are often difficult to photograph with
transmitted light optics simply because test walls are
not sufficiently hyaline.

Whereas transmitted light optics are still the primary
tool of the Cenozoic specialist, the scanning electron
microscope by necessity has become the primary tool
of the Mesozoic specialist. Because the scanning elec-
tron microscope is capable of recording the minutest
details of radiolarian morphology, students of Meso-
zoic Radiolaria are presented with a wealth of mor-
phological data. Taxa are therefore described in more
detail than would be normal utilizing transmitted light
optics. As a result, Cenozoic specialists tend to be re-
garded by Mesozoic specialists as ultra “lumpers” and
most Mesozoic specialists are regarded by Cenozoic
specialists as ultra “splitters.” In spite of such differ-
ences in approach, radiolarian workers agree that the
classification presented by Haeckel (1887) is artificial
in character and needs to be replaced by a more phy-
logenetic classification (cf. Riedel, 1971; Pessagno,
1977c). Haeckel’s detailed classification was based to
a large degree on the geometry or shape of the radi-
olarian test. Pessagno (1977c, p. 928) stated “It is clear
that if one hopes to construct a more phylogenetic
classification of Mesozoic or for that matter Cainozoic
Radiolaria, one must consider how a radiolarian test
is constructed. This is particularly true at the super-
generic level.” This thesis is well illustrated in the re-
cent literature (e.g., Pessagno, 1973; Pessagno and
Blome, 1980; Baumgartner, 1980a; Pessagno and
Whalen, 1982).

In routine stratigraphic investigations of Mesozoic
Radiolaria the majority of specimens can be identified
using a good quality stereoscopic microscope with
magnifications ranging from 100x to 250 x. Diagnos-
tic features recognized from scanning electron micro-
graphs can usually be recognized with a stereoscopic
microscope.

In the systematic paleontology section to follow, the
designation USNM indicates that a type specimen has
been deposited at the U.S. National Museum, Wash-
ington, DC. All USNM types have been assigned cat-
alogue numbers. Holotypes are isolated on one hole
cardboard slides bearing a USNM catalogue number;
paratypes deposited at the U.S. National Museum are
mounted on glass slides also bearing a USNM cata-
logue number. Paratypes deposited in the Pessagno
Collection are isolated on one hole cardboard slides.

All new taxa described in this report are illustrated
by means of scanning electron micrographs. Where
preservation permits, transmitted light photomicro-
graphs are also utilized.

Measurements are made with an ocular micrometer
in either a stereoscopic microscope or a transmitted
light microscope. No measurements are made from
scales on the scanning electron micrographs. All mea-
surements are given in um.

Finally, it should be noted that the authorship of all
new radiolarian taxa is assigned to Pessagno and Blome.

Order POLYCYSTIDA Ehrenberg, 1838
Suborder SPUMELLARIINA Ehrenberg, 1838

Superfamily SPONGODISCACEA Haeckel, 1881
(emend. Pessagno, 1971, 1973)

Subsuperfamily PSEUDOAULOPHACILAE
Riedel, 1971 (emend. Pessagno, 1971)

Family ORBICULIFORMIDAE Pessagno, 1973

Type genus.— Orbiculiforma Pessagno, 1973.
Range and occurrence. — Triassic to Cretaceous; Bo-
real, Tethyan, and Austral realms.

Genus ORBICULIFORMA Pessagno, 1973

Type species.— Orbiculiforma quadrata Pessagno,
1973.
Range and occurrence. —Same as for family.

Orbiculiforma lowreyensis Pessagno
Plate 1, figures 9-11

Orbiculiforma lowreyensis Pessagno, 19772, p. 74, pl. 3, figs. 15, 16;

pl.:4, figs. 1-3.

Range.—Zone 4 (upper Tithonian) to Zone 5, Sub-
zone 5A (Berriasian).

Occurrence.— California Coast Ranges, Baja Cali-
fornia Sur. O. lowreyensis is quite abundant in the
California Coast Ranges in upper Tithonian strata as-
signable to the Buchia piochii Zone (Jones, Bailey, and
Imlay, 1969). It is also common in strata assignable
to the Buchia piochii Zone in Baja California Sur. Very
rare specimens of O. lowreyensis were also observed

BULLETIN 320

at loc. NSF-810 (Buchia uncitoides Zone; Berriasian;
see Locality Descriptions).

Superfamily LIOSPHAERACEA Haeckel, 1881
(emend. herein)

Description. —Spumellariina with a latticed, solid
cortical shell; medullary shells when present, solid, lat-
ticed.

Remarks.— This superfamily is subdivided herein
into the Entactiniilae Riedel, 1967, and the Liosphae-
rilae Haeckel, 1881. The Entactiniilae include all Lio-
sphaeracea possessing an array of internal spicules that
extend to, and often beyond the wall of the cortical
shell; the Liosphaerilae lack internal spicules. The En-
tactiniilae first appeared in the Early Paleozoic and
greatly declined at the end of the Early Jurassic. A
lineage of Entactiniilae most likely gave rise to the
Liosphaerilae during Triassic times.

Pessagno (1977a, p. 75) used the Sphaerellacea
Haeckel, 1881, as a superfamily name. Haeckel (1881)
originally treated as an order what Pessagno (19772)
called “Sphaerellacea” (i.e., the Order Sphaerellaria).
In that Haeckel's name is not based on any known
family, it cannot be used as a superfamily name.

Subsuperfamily LIOSPHAERILAE Haeckel, 1881

Range and occurrence.— Triassic to Holocene.
World-wide.

Family PANTANELLIDAE Pessagno, 1977b
(emend. Pessagno and Blome, 1980)

Type genus.— Pantanellium Pessagno, 19772.
Range and occurrence.— Upper Triassic to Lower
Cretaceous. World-wide.

Genus VALLUPUS Pessagno and Blome,
new genus

Etymology.— Vallupus (masc.) is a name formed by
an arbitrary combination of letters (ICZN, 1964, Ap-
pendix D, pt. VI, Recommendation 40, p. 113).

Type species.— Vallupus hopsoni Pessagno and
Blome, n. sp. i

Description. — Test consisting of a cortical shell and
a single medullary shell. Cortical shell elongate, hel-
met-like with symmetrical polygonal pore frames and
a prominent imperforate, cylindrical collar (Pl. 1, figs.
19, 21) having a circular aperture. Single medullary
shell spherical with small symmetrical polygonal pore
frames; pore frames of medullary shell connected to
pore frames of cortical shell by triradiate (axial section)
radial beams; triradiate radial beams joining both cor-
tical shell and medullary shell at sites of triple junctions

JURASSIC RADIOLARIAN ZONATION: PESSAGNO ET AL. 23

formed by adjoining pore frames. Cylindrical collar
lacking radial beams.

Remarks. —This bizarre, Nassellarian-like form dif-
fers from all other Spumellarians in the Mesozoic by
possessing an imperforate, cylindrical collar. Ongoing
studies of the Upper Jurassic radiolarian assemblage
of east-central Mexico by Pessagno and Longoria in-
dicate that Vallupus definitely evolved from Panta-
nellium Pessagno, 1977a (Pantanellium sp. to un-
named intermediate to Vallupus sp.). Intermediate
forms possessing two well-developed polar spines as
well as a cortical shell with a cylindrical collar struc-
ture, have been observed at six horizons within the
upper Kimmeridgian and lower Tithonian portions of
the Taman Formation.

Range. —Upper Jurassic: Tithonian.

Occurrence. — California Coast Ranges, east-central
Mexico, Costa Rica. According to Baumgartner (oral
commun., 1980) this taxon is also present in his south-
ern European faunas.

Vallupus hopsoni Pessagno and Blome, new species
Plate 1, figures 14-16, 18, 19, 21; Plate 5, figure 1

Etymology.— This species is named for Dr. C. A.
Hopson (Univ. of Calif., Santa Barbara) in honor of
his contributions to the geology of the California Coast
Ranges.

Description. — Test small with very thick-walled cor-
tical shell and thin-walled first medullary shell. Cor-
tical shell with mixture of massive pentagonal and hex-
agonal pore frames lacking nodes at vertices; pore
frames about two times thicker in Z direction than in
Y direction (terminology: cf. Pessagno and Blome, 1980,
text-fig. 5) tending to become elongate at junction with
collar (Pl. 1, figs. 19, 21). Secondary radial beams with
three broad longitudinal grooves alternating with three
narrow longitudinal ridges. First medullary shell with
fragile pentagonal and hexagonal pore frames.

Remarks.— V. hopsoni, n. sp., differs from all other
Pantanellid species by possessing a cylindrical collar
with a circular aperture and by lacking primary spines
(polar spines).

Measurements (in um).— Ten specimens (holotype
plus nine paratypes).

length of | width of diameter of latticed
collar collar cortical shell
Holotype
(USNM 340255) 37.5 75 Ta
Mean 42.5 76 si
Maximum TS 100 80
Minimum 25 60 50

Type locality. —SA-43B. See Locality Descriptions.

Deposition of types.—Holotype: USNM 340255.
Paratypes: USNM 340256 and Pessagno Collection.

Range.— Lower part of Zone 4 so far as known; up-
per Tithonian.

Occurrence.—Stanley Mountain remnant of Coast
Range ophiolite in volcanogenic-pelagic strata over-
lying ophiolite. Locs. SA-39, SA-40, SA-43B at Alamo
Creek. Upper part of Taman Formation at loc. MX-
82-37. See Locality Descriptions.

Vallupus species A
Plate 1, figure 20

Range and occurrence. — Lower part of Zone 4 at loc.
SA-43B; upper Tithonian.

Family PRAECONOCARYOMMIDAE
Pessagno, 1976

Type genus. —Praeconocaryomma Pessagno, 1976.

Range. —Lower Jurassic (Pliensbachian) to Upper
Cretaceous (Campanian).

Occurrence. —Boreal and Tethyan realms.

Genus PRAECONOCARYOMMA Pessagno, 1976

Conocaryomma Lipman. Empson-Morin, 1981 (part) [not Cono-
caryomma Lipman, 19691.

Type species. —Praeconocaryomma universa Pessa-
gno, 1976.

Remarks.—Pessagno (1976) differentiated Praeco-
nocaryomma from Conocaryomma on the basis of the
number of medullary shells. Praeconocaryomma con-
sistently possesses three medullary shells whereas Co-
nocaryomma possesses four(?) or five medullary shells.
There appears to be no direct phylogenetic link be-
tween these two superficially similar genera. Praeco-
nocaryomma becomes extinct in the middle Campan-
ian whereas Conocaryomma is only known from the
middle and upper Eocene (Pessagno, 1976; Lipman,
1969).

Empson-Morin (1981) regarded Praeconocaryom-
ma as ajunior synonym of Conocaryomma. She stated
(p. 260): “Since the medullary shell(s) represent growth
stages which almost certainly can show some variation
and comprise the immature portion of the skeleton,
their taxonomic significance at the generic level is ques-
tionable.” We believe, however, that test construction
should be the primary criterion for developing a mean-
ingful and more phylogenetic classification of Radi-
olaria. We agree that the features of the cortical shell
are the most important criteria for differentiating
species. Nevertheless, we regard the construction of
the entire test to be the most important criterion for
defining genera, families, and superfamilies. The num-
ber of medullary shells governs the manner in which

the test as a whole is constructed. This appears to be
a consistent feature among families that we have stud-
ied in detail. For example, specimens in the Panta-
nellidae Pessagno, 1977b (see Pessagno and Blome,
1980) always possess a single medullary shell through-
out their lengthy geologic history (Late Triassic to Early
Cretaceous). Similarly, the Praeconocaryommidae al-
ways possess three medullary shells during their tenure
from Early Jurassic (late Pliensbachian) to Late Cre-
taceous (middle Campanian) times.

Range.—Lower Jurassic (upper Pliensbachian) to
Upper Cretaceous (middle Campanian).

Occurrence. — World-wide in Boreal and Tethyan
realms.

Praeconocaryomma immodica
Pessagno and Poisson, 1981
Plate 1, figures 22-24
Praeconocaryomma magnimamma (Rist, 1885). Pessagno, 1977a,
p. 77, pl. 5, figs. 14-16; pl. 6, fig. 1.
Praeconocaryomma immodica Pessagno and Poisson, 1981, p. 57,
pl. 7, figs. 2-9.

Range. —Upper Zone 1 (undifferentiated) to lower
Zone 2; Kimmeridgian. Pessagno and Poisson (1981)
originally believed that this species ranged down into
the Lower Jurassic (upper Toarcian). These data were
derived from a sample from the Klamath Mountains
of California; however, a reanalysis of the fauna from
this sample indicates that the specimen thought to be
P. immodica represents a related but unnamed form.

Occurrence.— World-wide in Tethyan Realm and
southern part of Boreal. See Pessagno (19772).

Suborder NASSELLARIINA Ehrenberg, 1875

Family EPTINGIIDAE Dumitrica, 1978

Type genus.— Eptingium Dumitrica, 1978.
Range and occurrence.—Triassic to Upper Jurassic;
world-wide in Boreal and Tethyan realms.

Genus PERISPYRIDIUM Dumitrica, 1978

Type species.—Trilonche(?) ordinaria Pessagno,
1977a.

Range.—Base of Zone | to lower part of Zone 4;
Aalenian to upper Tithonian.

Occurrence.—Same as for family.

Perispyridium ordinarium (Pessagno)
(emend. Pessagno and Blome, 1982)
Plate 1, figure 7

Trilonche(?) ordinarium Pessagno, 1977a, p. 79, pl. 6, fig. 14.

not Perispyridium ordinarium (Pessagno). Dumitrica, 1978, pp. 35,
36, Dl so igs- L-23; pb 4, 1829,

Perispyridium ordinarium (Pessagno). Pessagno and Blome, 1982,
p. 294, pl. 6, figs. 4, 12, 15.

BULLETIN 320

Range. —Zone 2 to lower part of Zone 4; Kimmer-
idgian to upper Tithonian (see Text-figs. 1, 3).

Occurrence. — Tethyan Realm and southern part of
Boreal Realm so far as known. California Coast Ranges
(see Pessagno, 1977a and loc. SA-43B), Baja California
Sur, Greece.

Perispyridium tamanense Pessagno and Blome
Plate 1, figure 8

Perispyridium tamanense Pessagno and Blome, 1982, p. 295, pl. 6,
figs. 1, 7, 8-11, 13, 14; pl. 7, fig. 3.

Range. — Upper part of Zone 3; lower Tithonian.

Occurrence. —Upper part of lower more massively-
bedded portion of Taman Formation, east-central
Mexico.

Family ULTRANAPORIDAE Pessagno, 1977b

Type genus. — Ultranapora Pessagno, 1977b.

Range. —Lower Jurassic to Upper Cretaceous.

Occurrence. — World-wide in Tethyan and Boreal
realms.

Genus NAPORA Pessagno, 1977a

Type species. — Napora bukryi Pessagno, 1977a.

Remarks.— Napora differs from Ultranapora by pos-
sessing a much smaller cephalis and by lacking a ceph-
alocone. In addition, the thorax of Napora s.s. is in-
flated and nearly hemispherical whereas that of
Ultranapora is typically pyramidal.

Range and occurrence.— Lower Jurassic to Creta-
ceous. Boreal and Tethyan realms.

Napora lospensis Pessagno
Plate 2, figure 9

Napora lospensis Pessagno, 1977a, p. 96, pl. 12, figs. 9, 10 [not
Baumgartner, DeWever, and Kocher, 1980, p. 57, pl. 3, fig. 4].

Remarks.— The form figured by Baumgartner, De-
Wever, and Kocher as Napora lospensis Pessagno bears
no resemblance to Pessagno's figured holotype. It pos-
sesses a longer, structurally different horn; longer, less
massive feet; and much less massive pore frames.

Range. —Not fully established. Zone 2 to Zone 3;
upper Kimmeridgian to lower Tithonian.

Occurrence. — California Coast Ranges so far as
known.

Family HSUIDAE Pessagno and Whalen, 1982

Type genus.— Hsuum Pessagno, 1977a.

Range. — Zone 02 (Pessagno, Blome, Whalen, and
Cheng, in prep.); Zone 1 to Zone 5, Subzone 5C; lower
Pliensbachian to upper Valanginian part of Subzone
5C.

Occurrence. — World-wide in Tethyan and Boreal
realms.

JURASSIC RADIOLARIAN ZONATION: PESSAGNO ET AL. 25

Genus HSUUM Pessagno, 1977a

Type species. — Hsuum cuestaense Pessagno, 1977a.

Range.—Same as for family.

Occurrence. — Most diversified and abundant in Bo-
real Realm. Rare in Tethyan realm at least in Late
Jurassic.

Hsuum cuestaense Pessagno
(corrected name)
Plate 1, figure 5

Hsuum cuestaensis Pessagno, 19772, p. 81, pl. 7, figs. 12, 13.

Remarks.— Although Pessagno (1977a) originally
believed that this taxon ranged into Zone 5, he un-
doubtedly was confusing it with H. mclaughlini Pes-
sagno and Blome, n. sp., and undescribed forms that
likewise possess straight costae. There appears to be
no evidence that this taxon ranges above Zone 3.

Range.— Zone 2 to upper part of Zone 3.

Occurrence. — California Coast Ranges, San Juan Is-
lands (Trump Island), Pacific Rim complex of Van-
couver Island.

Hsuum maxwelli Pessagno
Plate 1, figure 6

Hsuum maxwelli Pessagno, 1977a, p. 81, pl. 7, figs. 14-16.

Range.— Upper part of Zone 1; Zone 2 to middle
part of Zone 3; upper Kimmeridgian to lower Titho-
nian (see Text-figs. 1, 3).

Occurrence. — California Coast Ranges (Pessagno,
19772), Vancouver Island, Baja California Sur, Greece
(Sample POB 899 from Baumgartner), Romania.

Hsuum mclaughlini Pessagno and Blome,
new species
Plate 1, figures 1—4, 12, 13, 17; Plate 5, figure 6

Etymology. — This species is named for Mr. Robert
J. McLaughlin (U.S. Geological Survey, Menlo Park,
Calif.) in honor of his significant contributions to the
geology of the Geysers-Clear Lake Area, California
Coast Ranges.

Description. — Test of medium width, rounded api-
cally. Cephalis broad, hemispherical with short, mas-
sive horn. Thorax and subsequent chambers trapezoi-
dal in outline, increasing rapidly in width (except for
final post-abdominal chambers) and very slowly in
length as added; final post-abdominal chambers nar-
rower. Complete specimens with ten to twelve post-
abdominal chambers. Inner latticed layer with small
tetragonal (usually square) pore frames aligned in rows.
Outer layer comprised of straight diverging costae and
intercostal projections; intercostal projections well de-

veloped on proximal one-fourth to one-half of test
tending to form a dense meshwork of massive irregular
polygonal pore frames that completely obscure mesh-
work of the inner latticed layer. Costae straight usually,
continuous distally, often tending to bifurcate in an
apical direction. Eight to nine costae usually visible
(side view) on final post-abdominal chambers.

Remarks.— Hsuum mclaughlini Pessagno and
Blome, n. sp., differs from H. cuestaense Pessagno,
1977a, by having a wider test that is rounded rather
than pointed apically and by usually developing a dense
outer latticed layer proximally.

Measurements (in um).— Ten specimens (holotype
plus nine paratypes).

number of
post-abdominal horn
length width chambers length
Holotype
(USNM 340257) 375 200 11 23
Mean 364:5 917355 10 20
Maximum 420 200 y, 25
Minimum 320 150 10 20

Type locality. —SA-43B. See Locality Descriptions.

Deposition of types.— Holotype: USNM 340257.
Paratypes: USNM 340258 and Pessagno Collection.

Range.—Zone 4; upper Tithonian. See Text-figs.
ihe Shs

Occurrence. — Volcanogenic-pelagic strata overlying
Stanley Mountain remnant of Coast Range ophiolite
at Alamo Creek. Locs. SA-39, SA-40, SA-42, SA-43B.
Taman Formation of east-central Mexico at loc. MX-
82-37; see Locality Descriptions. Southern part of Bo-
real Realm and northern part of Tethyan Realm.

Family PARVICINGULIDAE Pessagno, 1977a
(emend. Pessagno and Whalen, 1982)

Type genus.— Parvicingula Pessagno, 1977a.

Range.— Aalenian to lower Hauterivian.

Occurrence. — World-wide in Tethyan and Boreal
realms.

Genus MIRIFUSUS Pessagno, 1977a

Type species. — Mirifusus guadalupensis Pessagno.

Range.—Base of Zone 2 to Zone 5, Subzone 5C;
lower Kimmeridgian(?); upper Kimmeridgian to lower
Hauterivian.

Occurrence.— World-wide in Tethyan and Boreal
realms.

26 BULLETIN 320

Mirifusus baileyi Pessagno
Plate 2, figures 1-3, 10, 13, 17, 21-23

Mirifusus baileyi Pessagno, 1977a, p. 83, pl. 10, figs. 6-8; pl. 11,
figs. 9-11; Pessagno, 1977b, p. 48, pl. 8, fig. 1; not fig. 9; (?) fig.
8; Mizutani, 1981, p. 177, pl. 60, fig. 1.

Lithocampe mediodilatata Rüst, 1885. Moore, 1973, p. 828, pl. 2,
figs. 5, 6; Riedel and Sanfilippo, 1974, p. 779, pl. 7, fig. 3; not
figs. 1, 2, 4.

Mirifusus mediodilatata (Rist). Baumgartner, DeWever, and Koch-
er, 1980, p. 56, pl. 5, fig. 11; not pl. 5, figs. 9, 10 (= M. medio-
dilatata s.s.).

Remarks.—Baumgartner, DeWever, and Kocher
(1980) include Mirifusus baileyi Pessagno under M.
mediodilatata (Rüst, 1885). As noted elsewhere in this
report, these taxa not only display significantly differ-
ent ranges, but also are morphologically distinct. M.
baileyi possesses a very thick test wall. Most of its post-
abdominal chambers are comprised of three layers of
latticed meshwork. The inner layer consists of small,
symmetrical pentagonal (not hexagonal as stated in
Pessagno, 1977a) pore frames arranged in two stag-
gered rows between closely-spaced, very nodose cir-
cumferential ridges. The two outer layers consist of
two staggered rows of symmetrical triangular pore
frames arranged between the circumferential ridges.
On well-preserved specimens the bars of the triangular
pore frames can be observed to connect with the nodes
on the circumferential ridges. The circumferential ridges
appear to be wedge-shaped in cross-section because
they are considerably wider on the test exterior than
they are in the test interior. The outer latticed layer of
about the first eight post-abdominal chambers lacks
staggered rows of triangular pore frames and consists
rather of massive nodes interconnected by massive
bars that tend to form triangular pore frames. It should
be noted also that the two outer latticed layers of tri-
angular pore frames are missing on the tubular exten-
sion of the final post-abdominal chamber and may be
lacking on the last several post-abdominal chambers.

The test structure described above has been ob-
served on numerous specimens from all over the world.
In fact, it is well illustrated (except for the inner layer
of triangular pore frames) by Baumgartner, DeWever,
and Kocher (1980, pl. 5, fig. 11). The inner latticed
layer of pentagonal pore frames can easily be observed
by examining broken, well-preserved specimens.

M. mediodilatata (Rúst, 1885) sensu Pessagno
(1977a) differs from M. baileyi by having a thinner test
wall that appears to consist of an inner latticed layer
of pentagonal pore frames arranged in two staggered
rows between narrow, slightly nodose circumferential
ridges. A partially formed outer (second) latticed layer
consisting of nodes and interconnecting bars occurs on

the apical portion of the test. As noted by Pessagno
and Whalen (1982) in their analysis of parvicingulid
wall structure, a microgranular layer commonly covers
the latticed portion of Mirifusus apically.

Range.—Base of Zone 3 to top of Zone 5; upper
Kimmeridgian(?); lower Tithonian to lower Hauteri-
vian.

Occurrence. — World-wide. Tethyan and Boreal
realms: California Coast Ranges, San Juan Islands,
Alaska, Baja California Sur, east-central Mexico, Oman,
Greece, Japan.

Mirifusus guadalupensis Pessagno
Plate 2, figures 12, 16, 24
Mirifusus guadalupensis Pessagno, 1977a, pp. 83, 84, pl. 10, figs. 9-

14; Baumgartner, DeWever, and Kocher, 1980, p. 55, pl. 5, figs.
12-14.

Range.— Lower part of Zone 2 to lower part of Zone
3; upper Kimmeridgian; lower Tithonian(?).

Occurrence. —Southern part of Boreal realm; Tethy-
an Realm. See Pessagno (1977a) and Baumgartner,
DeWever, and Kocher (1980).

Mirifusus mediodilatata (Rüst)
Plate 2, figures 4, 5, 18, 19
Lithocampe mediodilatata Riist, 1885, p. 316, pl. 40 (15), fig. 9.
Mirifusus (?) mediodilatata (Rist). Pessagno, 1977a, p. 84, pl. 11,
figs; l 2.
Mirifusus mediodilatata (Rüst). Baumgartner, DeWever, and Koch-
er, 1980 (part), p. 56, pl. 5, figs. 9, 10; not pl. 5, fig. 11 (= M.
baileyi Pessagno).

Range.— Zone 2 to Zone 5; upper Kimmeridgian to
Valanginian.

Occurrence.— World-wide in Tethyan and Boreal
realms.

Genus PARVICINGULA Pessagno, 1977a

Type species. — Parvicingula santabarbaraensis Pes-
sagno, 1977a.

Range.— Base of Zone 1 to top of Zone 5: Middle
Jurassic (Aalenian) to Lower Cretaceous (lower Haute-
rivian).

Occurrence. —Boreal Realm and northern part of
Tethyan Realm. See discussion on pp. 18-19.

Parvicingula blowi Pessagno
Plate 2, figures 14, 15

Parvicingula blowi Pessagno, 19772, p. 84, pl. 8, figs. 11-14.

Range.— Base of Zone 3 to middle part of Zone 4;
upper Kimmeridgian(?); lower to upper Tithonian. See
Text-figures 1, 3.

Occurrence. — California Coast Ranges (cf. Pessagno,
19772), San Juan Islands (Trump Island).

JURASSIC RADIOLARIAN ZONATION: PESSAGNO ET AL. 29

Parvicingula colemani
Pessagno and Blome, new species
Plate 2, figures 6—8, 11, 20;
Plate 5, figures 2, 3

Etymology.— P. colemani, n. sp., is named for Dr.
Robert G. Coleman (U.S. Geological Survey, Menlo
Park, Calif.) in honor of his contributions to the study
of ophiolites.

Description. — Test elongate, cylindrical to subcylin-
drical in aspect, blunt apically. Cephalis small, hemi-
spherical with short, massive horn. Thorax trapezoidal
with massive, variably sized and shaped polygonal pore
frames. Abdomen trapezoidal to rectangular in outline,
likewise with irregular polygonal pore frames; abdo-
men separated from first post-abdominal chamber by
weakly-developed circumferential ridge. Eleven to 14
post-abdominal chambers, generally rectangular in
outline, increasing slightly in width and height as added;
separated by weakly-developed circumferential ridges.
Pore frames of post-abdominal chambers of most spec-
imens hexagonal in shape, arranged in three rows; cen-
tral row of pore frames smaller in size, staggered with
respect to those of two flanking rows. Some specimens
with four rows of pore frames distally; pore frames of
first and second post-abdominal chambers may be ir-
regular. Final post-abdominal chamber terminating in
broad tubular projection.

Remarks.— Parvicingula colemani Pessagno and
Blome, n. sp., differs from P. excelsa Pessagno and
Blome, n. sp., by having a cylindrical to subcylindrical
test, a shorter, less massive horn, more weakly-devel-
Oped circumferential ridges, and smaller pore frames
On its post-abdominal chambers.

Measurements (in um).— Ten specimens (holotype
plus nine paratypes).

number of
post-abdominal horn
length width chambers length
Holotype

(USNM 340259) A8713 125 12 SS
Mean 381 SUS US 49.5

Maximum 43715. 13150 14 60

Minimum 395 120 11 25

Type locality. —SA-43B. See Locality Descriptions.

Deposition of types.—Holotype: USNM 340259.
Paratypes: USNM 340260 and Pessagno Collection.

Range. —Base of Zone 4 to upper part of Zone 4.
Upper Jurassic: upper Tithonian. See Text-figures 1
and 3.

Occurrence.—In the California Coast Ranges P.
colemani has been observed at Alamo Creek (Stanley
Mountain remnant, Coast Range ophiolite) at locs. 81-
CB-22, SA-40, SA-41, SA-42, and SA-43B; at Bitter-

water Canyon (Llanada remnant, Coast Range ophio-
lite) at loc. SA-56; and in the Great Valley sequence at
loc. NSF-837 (upper part of B. piochii Zone; upper
Tithonian). Davila has encountered this species in a
Zone 4 assemblage that is directly associated with
Buchia piochii (Gabb, 1869) at his locality BJV-20 in
Baja California Sur. P. colemani also occurs in the
upper thin-bedded portion of the Taman Formation
in east-central Mexico (locality MX-82-37) (see Lo-
cality Descriptions).

Parvicingula excelsa
Pessagno and Blome, new species
Plate 3, figures 1-4, 11-13, 17, 22;
Plate 5, figures 4, 5

Etymology. —excelsus-a-um (Latin, adj.) = lofty,
high.

Description. — Test elongate, conical with small
hemispherical cephalis possessing a massive, moder-
ately long, conical, pointed horn; thorax and subse-
quent chambers trapezoidal in outline. Cephalis and
much of thorax covered by layer of microgranular sil-
ica. Apical portion of test (cephalis through abdomen)
inflated, turret-like. Abdomen with variably-sized
polygonal pore frames not arranged in rows. Abdomen
separated from first post-abdominal chamber, and sub-
sequent post-abdominal chambers separated from each
other, by well-developed circumferential ridges. Post-
abdominal chambers with three rows of hexagonal pore
frames; center row of pore frames somewhat smaller
than flanking rows; with elliptical rather than circular
pores, staggered with respect to pore frames of flanking
rows. Most complete tests with ten to fifteen post-
abdominal chambers that change rapidly in width and
more slowly in height as added. Terminal tube not
observed on type specimens.

Remarks.— Parvicingula excelsa Pessagno and
Blome, n. sp., differs from P. elegans Pessagno and
Whalen, 1982, by possessing a longer, somewhat more
slender test with a much larger and more massive horn
and by having its cephalis and thorax covered with
microgranular silica. Both species have tests that are
swollen and turret-like apically and have three rows of
hexagonal pore frames on their post-abdominal cham-
bers. The pore frames of P. excelsa n. sp., though sim-
ilar in shape to those of P. elegans, tend to be consid-
erably more massive.

Measurements (in wm).—Eleven specimens (holo-
type plus ten paratypes).

number of
post-abdominal horn
length width chambers length
Holotype
(USNM 340261) 375 150 11 50
Mean 374.4 139.5 12 60.6
Maximum 437.5 160 15 75
Minimum 300 125 10 45

Type locality. —SA-43B. See Locality Descriptions.

Deposition of types.—Holotype: USNM 340261.
Paratypes: USNM 340262 and Pessagno Collection.

Range.— Zone 4; upper Tithonian. See Text-figures
1 and 3.

Occurrence. — Volcanogenic-pelagic sediments oc-
curring above Coast Range ophiolite at Stanley Moun-
tain (Alamo Creek locs. SA-39, SA-40, SA-41, SA-42,
SA-43B) and at Llanada (Bitterwater Canyon loc. SA-
58). Near base of Great Valley sequence at loc. MG-
77-3 (see Locality Descriptions).

Parvicingula jonesi Pessagno
Plate 3, figures 5-7, 14, 19, 24, 25

Parvicingula jonesi Pessagno, 1977b, p. 48, pl. 8, fig. 14.

Remarks. — Pessagno (19770) supplied only one il-
lustration of the holotype of this species. Other illus-
trations are offered herein to demonstrate variations
in test breadth, length, and number of post-abdominal
chambers. The specimen (Pl. 4, figs. 6, 14, 19, 24) from
loc. MG-77-3 differs from the holotype by possessing
more post-abdominal chambers and by being some-
what more slender. Nevertheless, it displays the three
rows of equal-sized pentagonal pore frames between
circumferential ridges, the dome-like cephalis, and the
short horn that typify this species. Specimens similar
to this form (Pl. 4, fig. 7), but not as well preserved,
are common in the type material.

Range. — Zone 4 to Zone 5, Subzone 5A; upper Ti-
thonian to Berriasian. In California and Baja California
Sur this species has been only observed in strata as-
signed to the Buchia piochii Zone and the Buchia un-
citoides Zone (Jones, Bailey, and Imlay, 1969). How-
ever, in east-central Mexico P. jonesi occurs in the
upper thin-bedded part of the Taman Formation (loc.
MX-82-37; upper Tithonian).

Occurrence. — California Coast Ranges (locs. NSF-
805, NSF-818, NSF-821, NSF-823, NSF-825, NSF-
837, NSF-838, and NSF-945; loc. MG-77-3; upper
Tithonian). Lower Cretaceous occurrences shown in
Pessagno (1977b). Baja California Sur, Mexico in the
Eugenia Formation (loc. BJV-20). Upper thin-bedded

BULLETIN 320

part of the Taman Formation of east-central Mexico
at locality MX-82-37 (see Locality Descriptions).

Parvicingula santabarbaraensis Pessagno
Plate 3, figure 8

Parvicingula santabarbaraensis Pessagno, 1977a, p. 86, pl. 9, figs.
11-13.

Range.— Upper part of Zone 2 to lower part of Zone
4; upper Kimmeridgian to upper Tithonian.

Occurrence. — California Coast Ranges (see Pessa-
gno, 19772). Locs. SA-35, SA-42, SA-43B at Alamo
Creek (Stanley Mountain remnant of Coast Range
ophiolite) (see Locality Descriptions). Boreal Realm so
far as known.

Parvicingula vera Pessagno and Whalen
Plate 3, figures 15, 20, 21

Parvicingula vera Pessagno and Whalen, 1982, p. 144, pl. 11, figs.
3-5, 11, 19; pl. 13, fig. 8.

Range.—Middle Jurassic (upper Bathonian) to Up-
per Jurassic (upper Kimmeridgian). Zone 1 to Zone 2.

Occurrence. —Snowshoe Formation of east-central
Oregon. Taman Formation of east-central Mexico.
Northern part of Tethyan Realm to central part of
Boreal Realm.

Genus RISTOLA Pessagno and Whalen, 1982

Type species. — Ristola procera Pessagno (1977a).

Range.— Middle Jurassic to Lower Cretaceous.

Occurrence.— World-wide in Tethyan and Boreal
realms.

Ristola altissima (Riist)
Plate 3, figure 10

Lithocampe altissima Riist, 1885, p. 315(45), pl. 40(15), fig. 2.

Parvicingula(?) altissima (Rist). Pessagno, 1977a, p. 85, pl. 8, figs.
9, 10; Baumgartner, DeWever, and Kocher, 1980, p. 58, pl. 5,
figs. 4-7.

Range.—Lower part of Zone 3 to top of Zone 4;
upper Kimmeridgian(?); lower Tithonian to uppermost
Tithonian.

Occurrence.—World-wide in Tethyan and Boreal
realms. California, Baja California Sur, San Juan Is-
lands, Alaska, Oman, Greece, Romania, Italy, DSDP
Site 367 (Cape Verde Basin), Puerto Rico [see data
presented by Baumgartner, DeWever, and Kocher
(1980) and Tippit (1981)].

Ristola boesii (Parona) sensu lato
Plate 3, figure 9
Dictyomitra boesii Parona, 1890, p. 170, pl. 6, fig. 9.

Remarks.—To date, no form figured in the literature
as R. boesii (Parona) corresponds to Parona’s figured

JURASSIC RADIOLARIAN ZONATION: PESSAGNO ET AL. 29

type. Parona’s figured type possesses a short, moder-
ately spindle-shaped test with a rounded apical por-
tion. Thin circumferential ridges separate six post-ab-
dominal chambers. Three rows of equal-sized pores
occur between the circumferential ridges. It is impos-
sible to determine the shape of the pore frames from
the illustration.

The form figured herein shows some of the features
illustrated by Parona. It displays three rows of equal-
sized pore frames between circumferential ridges; the
ridges are of moderate relief; and the apical portion of
the test is rounded. It differs, however, in that the test
is slightly less inflated medially and is hence, less spin-
dle-shaped. The apical portion of the test, though
rounded, is slightly narrower and the test possesses
seven rather than six post-abdominal chambers. Since
this form differs somewhat from Parona’s type speci-
men, it is referred to herein as R. boesii s.l.

R. boesii (Parona) is rapidly becoming a “wastebas-
ket” name utilized by workers to include all remotely
similar Nassellaria. It is conceivable that Parona’s il-
lustration of his type specimen is too schematic to
allow accurate correlation with any known morpho-
type. To stabilize the already chaotic nomenclature
Surrounding this taxon, it may be necessary to re-il-
lustrate Parona’s type specimen if it can be located or
to erect a neotype.

Range and occurrence.—California Coast Ranges at
loc. NSF-1068 (B. pacifica Zone; lower to middle Va-
langinian) [see Pessagno (1977b)].

Ristola sp. aff. R. boesii (Parona, 1890)
Plate 3, figures 16, 18, 23

Remarks. — This form differs from Parona’s type by
being less inflated, having different pore structure be-
tween its circumferential ridges, and by having seven
rather than six post-abdominal chambers. It may ac-
tually be more closely related to R. Asui Pessagno,
1977a, than to R. boesii.

Range and occurrence. — Zone 5, Subzone 5B. Cal-
ifornia Coast Ranges at loc. NSF-845 (B. pacifica Zone:
lower to middle Valanginian; see Pessagno, 1977b).

Ristola sp. cf. R. boesii (Parona, 1890)
Plate 4, figures 7, 17

Range and Occurrence. — Zone 4 in California and
Baja California Sur. A similar, if not identical form,
Occurs in Tithonian(?), Berriasian to lower Hauterivian
Strata in Oman (Tippit, 1981).

Ristola hsui (Pessagno)
Plate 4, figures 2, 3

Parvicingula hsui Pessagno, 1977a, p. 85, pl. 8, figs. 15, 16; pl. 9,
figs. 1-5.

Remarks.— Although Pessagno (19772) originally
believed that this taxon possessed a short, massive
horn and hence, should be included in Parvicingula
Pessagno, this interpretation 1s now regarded as in-
valid. The short horn noted by Pessagno simply rep-
resents the pointed apical portion of the cephalis.

Range. —Zone 3 to lower part of Zone 4; upper Kim-
meridgian(?); lower Tithonian to upper Tithonian.

Occurrence. —Boreal Realm. California Coast
Ranges. In addition to occurrences noted by Pessagno
(19772), R. hsui also occurs in the Alamo Creek succes-
sion (Stanley Mountain remnant of Coast Range
ophiolite) at the following localities: SA-33 through
35; SA-37 through 43B. San Juan Islands (Trump Is-
land). Baja California Sur.

Ristola procera (Pessagno)
Plate 4, figure 6

Parvicingula(?) procera Pessagno, 19772, p. 86, pl. 9, figs. 6-9.
Parvicingula procera Pessagno. Baumgartner, DeWever, and Koch-
er, 1980, p. 60, pl. 5, fig. 8.

Range.— Zone 2 to top of Zone 4; Kimmeridgian to
upper Tithonian.

Occurrence.— California Coast Ranges (Pessagno,
19772). Southern Europe (Baumgartner, DeWever, and
Kocher, 1980).

Family SPONGOCAPSULIDAE Pessagno, 1977a

Type genus. — Spongocapsula Pessagno, 1977a.
Range and occurrence. — Middle Jurassic to Upper
Cretaceous. World-wide in Boreal and Tethyan realms.

Genus OBESACAPSULA Pessagno, 1977a

Type species. — Obesacapsula morroensis Pessagno,
1977a.

Range and occurrence.— Upper Jurassic to Lower
Cretaceous; world-wide in Boreal and Tethyan realms.

Obesacapsula morroensis Pessagno
Plate 4, figure 5

Obesacapsula morroensis Pessagno, 1977a, p. 87, pl. 11, figs. 5-8.

Range.— Zone 2 to Zone 5, Subzone 5C; upper Kim-
meridgian (Text-figs. 1, 3) to upper Valanginian.

Occurrence.— California Coast Ranges (Pessagno,
19772). Baja California Sur.

Obesacapsula rotunda (Hinde)
Plate 4, figures 8, 10

Stichocapsa rotunda Hinde, 1902, p. 41, pl. 3, fig. 24.

Stichocapsa(?) rotunda Hinde. Foreman, 1973, p. 265, pl. 11, figs.
1,225 pl- 16, fig «90:

Obesacapsula rotunda (Hinde). Pessagno, 1977b (part), p. 53, pl. 9,
figs. 12, 18; not pl. 9, fig. 4.

30 BULLETIN 320

Remarks.—The morphotype figured herein and by
Pessagno (1977b, pl. 9, figs. 12, 18; not fig. 4) corre-
sponds closely to those figured by Foreman (1973, 1978)
and Baumgartner, DeWever, and Kocher (1980). How-
ever, we have never observed this form below the base
of the Lower Cretaceous (Berriasian). Baumgartner,
DeWever, and Kocher (1980) extended the range of
O. rotunda into their Upper Jurassic Biochronozone
C. We suspect that these workers may have included
the form referred to herein as O. sp. aff. O. rotunda
(Hinde) under O. rotunda. This was also done in part
by Pessagno (1977b, pl. 9, fig. 4).

Range.—Zone 5. Berriasian to lower Hauterivian.

Occurrence.—Numerous localities in Boreal and
Tethyan realms. World-wide.

Obesacapsula sp. aff. O. rotunda (Hinde)
Plate 4, figure 9

Obesacapsula rotunda (Hinde, 1902). Pessagno, 1977b (part), p. 53,
pl. 9, fig. 4; not pl. 9, figs. 12, 18.

Remarks.—This form differs from O. rotunda
(Hinde, 1902) s.s. by having less inflated post-abdom-
inal chambers separated by less pronounced strictures.
The apical portion of the test of O. sp. aff. O. rotunda
tends to be much more elongate. It is likely that O. sp.
aff. O. rotunda gave rise to O. rotunda.

Range.—Zone 3 to Zone 5, Subzone 5B so far as
known; upper Kimmeridgian (?); lower Tithonian to
middle Valanginian.

Occurrence. — California Coast Ranges (locs. NSF-
845, NSF-908; SA-43B; see Locality Descriptions). Baja
California Sur (Davila, in prep.).

NASSELLARIINA incertae sedis

GENERA AND INCLUDED SPECIES
NOT ASSIGNED TO A FAMILY
Genus ANDROMEDA Baumgartner
in Baumgartner, DeWever, and Kocher, 1980

Type species. — Andromeda crassa Baumgartner,
1980b.

Range and occurrence. — Lower to Upper Jurassic in
Boreal and Tethyan realms.

Andromeda violae Baumgartner
Plate 4, figures 16, 18, 19

Andromeda violae Baumgartner, 1980b, in Baumgartner, DeWever,
and Kocher, 1980, p. 50, pl. 4, figs. 10-14; pl. 6, fig. 11.

Range.— Zone 2 to lower part of Zone 4 so far as
known; Kimmeridgian to upper Tithonian.

Occurrence. — Italy, Sicily, Greece, Cape Verde Basin
(See Baumgartner, DeWever, and Kocher, 1980). Cal-
ifornia Coast Ranges at Point Sal (loc. NSF-907) and

at Alamo Creek (Stanley Mt.; locs. NSF-973; SA-43B)
(see Locality Descriptions).

Genus SAITOUM Pessagno, 1977a

Type species. — Saitoum pagei Pessagno, 1977a.
Range and occurrence. — Mesozoic. World-wide.

Saitoum pagei Pessagno
Plate 4, figures 4, 11

Saitoum pagei Pessagno, 1977a, p. 98, pl. 12, figs. 11-14.

Range.— Zone 1(?); Zone 2 to Zone 3. Kimmeridgian
to lower Tithonian.

Occurrence. — California Coast Ranges. See Pessagno
(19772).

Genus TURANTA Pessagno and Blome, 1982

Type species. — Turanta capsensis Pessagno and
Blome, 1982.

Range.— Base of Zone 1 to lower part of Zone 3i
uppermost Toarcian/lowermost Bajocian to lower Ti-
thonian.

Occurrence.— California Coast Ranges, Baja Cali-
fornia Sur, and east-central Oregon. See Pessagno and
Blome (1982).

Turanta flexa Pessagno and Blome
Plate 4, figure 15

Turanta flexa Pessagno and Blome, 1982, p. 298, pl. 6, figs. 5, 6.

Range.— Zone 2 to lower part of Zone 3 so far as
known.

Occurrence.— California Coast Ranges, Baja Cali-
fornia Sur.

SPECIES THAT NEED TO BE REASSIGNED
TO NEW GENERA

“Eucyrtidium” ptyctum Riedel and Sanfilippo
Plate 4, figures 12-14
Eucyrtidium ptyctum Riedel and Sanfilippo, 1974, p. 778, pl. 5, fig.
7; pl. 12, fig. 13. Baumgartner, DeWever, and Kocher, 1980, p.
53, pl. 3, fig. 13.
Eucyrtidium(?) ptyctum Riedel and Sanfilippo. Pessagno, 1977a, p-
94, pl. 12, fig. 7.

Remarks.—This taxon is virtually unrelated mor-
phologically to Eucyrtidium Ehrenberg, 1847, and
should be assigned to a new genus. The type species
of Eucyrtidium, Lithocampe acuminata Ehrenberg,
1844, is a multicyrtid form lacking strictures. “E.”
ptyctum, however, is a tricyrtid form possessing à
weakly developed stricture between the cephalis and
thorax and a prominent stricture between the thorax
and abdomen. A cephalopyle (Pl. 4, figs. 13, 14) is
present at the base of the cephalis. Rows of small pores

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JURASSIC RADIOLARIAN ZONATION: PESSAGNO ET AL. 31

occur in the stricture between the thorax and abdomen
and at the base of the abdomen (Pl. 4, figs. 12, 13).

Range. —Upper Zone 1; Zone 2 to upper Zone 4;
Kimmeridgian to upper Tithonian. This species has
only been observed to date as high as the lower part
of Zone 4 in the California Coast Ranges (See Pessa-
gno, 1977a; locs. SA-4, SA-5, SA-16, SA-29, SA-30,
SA-39, SA-42, SA-43 at Alamo Creek). However, Dav-
ila (in prep.) has found it associated with common to
abundant Buchia piochii in Baja California Sur.

Occurrence.—Boreal and Tethyan realms, world-
wide [see Pessagno (1977a) and Baumgartner, De-
Wever, and Kocher (1980)].

“Hsuum” stanleyense Pessagno
(corrected name)
Plate 4, figure 1

Hsuum(?) stanleyensis Pessagno, 1977a, p. 82, pl. 8, figs. 5-8.

Remarks.— This species lacks the layered wall struc-
ture described by Pessagno and Whalen (1982) for
Hsuum Pessagno, 1977a, and other members of the
Hsuidae Pessagno and Whalen, 1982. At the moment
it cannot be assigned in good conscience to any known
Mesozoic genus.

Range. —Upper part of Zone 1(?) to Zone 2; lower
to upper Kimmeridgian.

Occurrence. — California Coast Ranges. See Pessagno
(1977a). Boreal Realm.

APPENDIX
LOCALITY DESCRIPTIONS

Introduction. —In the California Coast Ranges sam-
ples are prefixed by NSF, SA, MG, 74-JP, and BK by
the various collectors. NSF samples and SA samples
were collected by the senior author and by the senior
author and Mr. Stephen Atlas respectively. Samples
prefixed by MG and 74-JP were collected by Mr. Rob-
ert McLaughlin and Dr. David L. Jones (U.S. Geo-
logical Survey, Menlo Park, CA). The sample prefixed
by BK was collected by James Berkland.

The single sample prefixed by OR was collected by
Pessagno and Blome from east-central Oregon.

All samples from east-central Mexico are prefixed
by MX and were collected by Pessagno and Longoria
during the 1980, 1981, and 1982 field seasons. The
prefix BJV is used for samples collected by Pessagno,
Longoria, and Davila from the Vizcaino Peninsula,
Baja California Sur, Mexico.

California
Volcanogenic-pelagic Strata Associated
with the Coast Range Ophiolite

1. Point Sal, Santa Barbara Co.: 21 m (70 ft) of green to gray tuff-
aceous chert and lenticular masses or nodules of pelagic limestone
overlying Coast Range ophiolite (see Pessagno, 1977a; Hopson,
Mattinson, and Pessagno, 1981; Text-fig. 2). USGS Point Sal
Quadrangle (7.5’): T. 10 N., R. 36 W.; near western edge of sect.
34. 0.9 km (0.6 mi) N 15° W of west side of Lion Rock.
NSF-900. Greenish-gray, thin-bedded tuffaceous chert. Composite
sample from lower 0.9 m (3 ft) of chert. Zone 1?

NSF-904. Greenish-gray to gray, thin-bedded tuffaceous chert. 4.5
m (15 ft) above contact with ophiolite. Base of Zone 2. Note:
In that the tuffaceous chert becomes progressively more re-
crystallized below NSF-904 in the section, the absence of Mi-
rifusus in the assemblage may be diagenetically controlled.

NSF-907. Lens of gray tuffaceous limestone about 0.4 m (1.5 ft)
thick. 11.5 m (38 ft) above the contact with the ophiolite. Zone
2 (upper part).

NSF-908. Small limestone nodules occurring at 13.4 m (44 ft) above
the contact with the ophiolite. Zone 3 (near base).

NSF-909. Small limestone nodule in green tuffaceous chert; 15.8 m
(52 ft) above contact with the ophiolite. Zone 3.

2. Alamo Creek (Stanley Mountain remnant of Coast Range ophio-
lite), San Luis Obispo Co.: 103 m (338 ft) of tuffaceous chert,
tuff breccia, and pelagic limestone overlying Coast Range ophio-
lite (see Hopson, Mattinson, and Pessagno, 1981; Text-fig. 2).
USGS Huasna Peak Quadrangle (7.5): T. 12 N., R. 32 W.; north-
western part of sect. 32; southwestern part of sect. 29.

SA-4. Thin-bedded, reddish brown, tuffaceous chert. 3.8 m (9.4 ft)
above the contact with the ophiolite. These strata are ques-
tionably assigned to Zone 1. Chert strata below this horizon
are recrystallized and contain only poorly preserved Radi-
olaria.

SA-5. Same. 4.7 m (15.5 ft) above contact with ophiolite. Apparent
base of Zone 2 (with Mirifusus Pessagno, 1977a).

SA-11. Same. 17.0 m (56 ft) above contact with the ophiolite. Lower
part of Zone 2.

SA-16. Same. 20.7 m (68 ft) above contact with the ophiolite.
Zone 2.

NSF-972. Medium gray pelagic limestone (tuffaceous micrite) bed
30 cm (8 in) thick. 21 m (69.5 ft) above contact with the
ophiolite. Zone 2.

NSF-973. Dark gray limestone (micrite) bed 15 to 20 cm (6 to 8 in)
thick. 45.5 m (149.5 ft) above contact with the ophiolite. Zone 2.

SA-29. Thin-bedded, dark gray, tuffaceous chert. 58.5 m (192 ft)
above the contact with the ophiolite. Zone 2.

SA-30. Same. 60.6 m (199 ft) above contact with ophiolite. Apparent
top of Zone 2. Note: The absence of Parvicingula Pessagno,
1977a, s.s. (possessing narrow, elongate tube on final post-
abdominal chamber) may suggest that the interval from locs.
SA-30 to SA-4 is assignable to the lower half of Zone 2. Par-
vicingula s.s. makes its first appearance in the upper half of
Zone 2 in the Taman Formation of east-central Mexico. This

suggests that an unconformity and hiatus exist in the interval
between locs. SA-30 and SA-31.

SA-31. Thin-bedded, reddish brown, tuffaceous chert. 62 m (204.5
ft) above contact with ophiolite. Zone 3. The interval of con-
currence between Mirifusus guadalupensis Pessagno, 1977a,
and M. baileyi Pessagno, 1977a, has not been recognized in
this section. Either this interval is condensed or is absent due
to the unconformity and hiatus suggested above.

SA-33. Same. 75 m (247 ft) above contact with the ophiolite. Zone 3.

SA-35. Dark gray tuffaceous, micritic limestone bed 20.3 cm (8 in)
thick. 79.5 m (261 ft) above contact with ophiolite. Zone 3.

SA-37. Thin-bedded, reddish brown tuffaceous chert. 82 m (269 ft)
above contact with the ophiolite. Zone 3.

SA-38. Same. 84 m (277 ft) above the contact with the ophiolite.
Zone 3, near top.

SA-39. (= 81-CB-22) Same. 90 m (296 ft) above contact with ophio-
lite. Zone 4, at, or somewhat above, base (sample 81-CB-22
collected by C. D. Blome).

SA-40. Same. 92.6 m (304 ft) above contact with ophiolite. Zone 4.

SA-41. Same. 97 m (318 ft) above contact with ophiolite. Zone 4.

SA-42. Same. 98 m (322 ft) above contact with ophiolite. Zone 4.

SA-43B. Silty, dark gray limestone bed 5 cm (2 in) thick. 100.6 m
(330 ft) above contact with ophiolite: 2.4 m (8 ft) below top
of exposed section. Covered interval separates tuffaceous chert
from faulted contact with Great Valley sequence (See Hopson,
Mattinson, and Pessagno, 1981). Zone 4.

3. Llanada (Bitterwater Canyon), San Benito Co.: 1245 m (4083 ft)
of tuff breccia and tuffaceous chert overlying Coast Range ophio-
lite (see Hopson, Mattinson, and Pessagno, 1981; Text-fig. 2).
Tuff-breccia predominates in this section.
SA-56. Greenish-gray, tuffaceous chert near contact with Great Val-
ley Sequence. USGS Llanada Quadrangle (7.5'): T. 15 S., R. 9
E.; at point of juncture of sects. 26, 27, 34, and 35. Zone 4.

SA-58. Lens of greenish-gray, tuffaceous chert in tuff breccia. 4.5 m
(15 ft) below contact with Great Valley Sequence. Overlying
Great Valley Sequence in this area assignable to the Buchia
piochii Zone of Jones, Bailey, and Imlay (1969) (see Text-figs.
2 and 3). USGS Llanada Quadrangle (7.5'): T. 15 S., R. 9E;
southeast !4 sect. 26. 0.8 km (0.5 mi) southeast of Albanez
Spring (sect. 27), along southeast trending tributary of Bitter-
water Canyon. Zone 4.

4. Dismembered ophiolite at Wilbur Springs, Colusa County.

NSF-997. Red manganiferous chert interbedded with vesicular bas-
alt. Ridge west of east fork of Sulphur Creek. 0.56 km (0.35
mi) S 69° W of Eagle Rock. USGS Wilbur Springs Quadrangle
(L5) 1714 N5; K- 5 W; sect. 18. Zone 3.

Great Valley Sequence

1. Grindstone Creek, Glenn Co.: 365 m (1200 ft) of interbedded
sandstones and shales exposed along Grindstone Creek. Section
includes (ascending order) the Buchia piochii Zone (upper Ti-
thonian), the B. sp. aff. B. okensis Zone (upper Tithonian), the
B. uncitoides Zone (Berriasian), the B. pacifica Zone (lower to
middle Valanginian), the B. keyserlingi Zone (pt.) (middle to
upper Valanginian) [see Jones, Bailey, and Imlay (1969); Pes-
sagno (1977b)]. USGS Chrone Quadrangle (7.5'): T. 21 N., R. 6
W. Megafossils identified in samples below by Dr. D. L. Jones
(USGS, Menlo Park, CA).

NSF-803. Large dark gray limestone (micrite) nodule with calcified
Radiolaria, Buchia sp. aff. B. okensis (Pavlow, 1907), and Ly-
toceras sp. 248 m (815 ft) west of gaging station and eastern
border of sect. 16 along south side of Grindstone Creek. Zone 4.

BULLETIN 320

NSF-804. Small dark gray limestone (micrite) nodule with Radi-
olaria. 234 m (767.4 ft) west of gaging station and eastern
border of sect. 16 along south side of Grindstone Creek. Zone 4.

NSF-805. Small, dark gray limestone nodule (micrite) with pyritized
Radiolaria. 219 m (718 ft) west of gaging station and eastern
border of sect. 16 along south side of Grindstone Creek. Zone
4.

NSF-808. Large, dark gray limestone (micrite) nodule with Buchia
uncitoides (Pavlow, 1907). 183 m (603 ft) west of gaging station
and eastern border of sect. 16 along south side of Grindstone
Creek.

NSF-810. Dark gray limestone nodules with Buchia uncitoides (Pav-
low, 1907), and calcified Radiolaria. 16.3 m (537 ft) west of
gaging station and eastern border of sect. 16 along south side
of Grindstone Creek [see Pessagno (1977b)]. Zone 5, Subzone
5A.

2. Middle Fork of Elder Creek, Tehama Co. [see Jones, Bailey, and
Imlay (1969) and Pessagno (1977a)].

NSF-821. Dark gray limestone (micrite) nodule near middle of Bu-
chia piochii Zone. USGS Lowrey Quadrangle (7.5'): T. 25 N.,
R. 6 W.; northwest part of sect. 30 on side of hill immediately
east of Rouse Gardens; 2.6 km (1.5 mi) due west of Lowrey
Road. Zone 4.

NSF-823. Dark gray limestone (micrite) nodule. Upper part of Bu-
chia piochii Zone of Jones, Bailey, and Imlay (1969). 1.4 km
(0.9 mi) S 69° W of northwest corner of Lowrey Cemetery.
USGS Lowrey Quadrangle (7.5 T. 25 N., R. 6 W.; north-
central part of sect. 30. Zone 4.

3. McCarty Creek area, Tehama Co. [see Pessagno (1977a, 1977b)
and Jones, Bailey, and Imlay (1969)].

NSF-837. Dark gray limestone (micrite) nodule near McCarty Creek.
Upper part of Buchia piochii Zone. Road between Paskenta
and Patton along Digger Creek. Slightly less than 0.48 km (0.3
mi) east of BM 1009 along road. USGS Paskenta Quadrangle
(7.5: T. 24 N., R. 7 W.; sect. 25. Zone 4.

NSF-838. Dark gray limestone (micrite) nodule. Uppermost part of
Buchia sp. aff. B. okensis Zone along McCarty Creek (see Pes-
sagno, 1977b, p. 8, fig. 2). USGS Paskenta Quadrangle (7.5'):
T. 24 N., R. 6 W.; middle of boundary between sects. 19 and
30. Zone 4.

NSF-845. Medium gray limestone (micrite) nodule occurring in dark
gray mudstone. Upper part of Buchia pacifica Zone (see Pes-
sagno, 1977b, p. 8, fig. 2). USGS Paskenta Quadrangle (7.5'):
T. 24 N., R. 6 W.; NE '⁄ of sect. 29. Zone 5, Subzone 5B.

NSF-1019. Dark gray limestone (micrite) nodule. Upper part of
Buchia keyserlingi Zone (upper Valanginian; see Jones, Bailey,
and Imlay, 1969; Pessagno, 1977b, p. 8, fig. 2). USGS Paskenta
Quadrangle (7.5^): T. 24 N., R. 6 W.; at boundary between NE
Y and NW ' of sect. 28 along McCarty Creek.

NSF-1068. Dark gray limestone (micrite) nodule. Lower part of
Buchia pacifica Zone (lower to middle Valanginian; see Jones,
Bailey, and Imlay, 1969; Pessagno, 1977b) exposed along
McCarty Creek. USGS Paskenta Quadrangle (7.5'): T. 24 N.,
R. 6 W.; NW % of sect. 29. Zone 5, Subzone 5C.

Miscellaneous Localities in the Franciscan
Complex and the Great Valley Sequence

BK-605. Red radiolarian chert in Franciscan melange. USGS Potter
Valley Quadrangle (7.5'): T. 16 N., R. 11 W.; NE % of sect. 8.
Potter Valley Road; 0.3 km (0.18 mi) southwest of junction of
Guntley Ranch Road with Potter Valley Road and California
Route 20. Sample from James Berkland (Univ. California,
Davis).

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JURASSIC RADIOLARIAN ZONATION: PESSAGNO ET AL. 33

MG-77-3. (= loc. 10 of McLaughlin and Pessagno, 1978, p. 721, fig.
2). Limestone nodule in mudstone of Great Valley sequence.
Approximately 76 m (249 ft) above sedimentary contact with
Coast Range ophiolite at Mount St. Helena. USGS Mount St.
Helena Quadrangle (7.5: T. 10 N., R. 7 W.; 701.5 m N, 793
m W, SE corner of sect. 20. Sample collected by Mr. R. J.
McLaughlin (USGS, Menlo Park). Zone 4.

74-JP-1. Great Valley sequence. Medium gray, laminated mudstone
with Buchia rugosa (Fischer, 1830—1837) and specimens tran-
sitional between Buchia rugosa and Buchia concentrica (Sow-
erby, 1827). Sample collected by Dr. D. L. Jones (USGS, Menlo
Park, Calif.) near Crowfoot Point. Zone 2.

Oregon

East-central Oregon. John Day Inlier (see Pessagno and Whalen,
1982).

OR-501C. South Fork Member of Snowshoe Formation of east-
central Oregon (see Smith, 1980). Dark gray mudstone with
common micritic limestone nodules. USGS Izee Quadrangle
(7.5): T. 17 N., R. 23 E.; SE % of sect. 29 (eastern edge).
Outcrop on north side of State Highway 63; about 0.64 km
(0.4 mi) east of Izee.

Mexico
East-Central Mexico

Taman Formation (Heim, 1926). Taman-Tamazunchale area, San
Luis Potosi.

MX-80-20. Middle portion of lower, more massively-bedded part
of Taman Formation. Medium bedded, dark gray, micritic
limestone with ammonites and abundant Aulacomyella Fur-
lani, 1910. An ammonite submitted to Dr. R. W. Imlay (US.
Geol. Survey, Washington, DC) for identification was said to
greatly resemble Subneumayria profulgens (Burckhardt, 1906).
Subneumayria Spath, 1924, is characteristic of the “Idoceras
beds” of Mexico (see Arkell, Kummel, and Wright, 1957, p.
327) and hence, would be characteristic of the Idoceras Zone
of Cantu Chapa (1971) (upper lower Kimmeridgian). 0.2 km
west of km post 264 on Rt. 85 (Mexico, D.F.—Nuevo Laredo
Highway); 3.8 km east-northeast of the village of Taman, S
Tees

MX-80-23. Upper portion of lower, more massively-bedded part of
Taman Formation. Dark gray, medium to massively-bedded
micritic limestone with abundant Aulacomyella Furlani, 1910.

- Interbedded black shales with limestone nodules. Idoceras Zone
or Glochiceras gr. fialar Zone of Cantu Chapa (1971); probably
G. gr. falar Zone. Uppermost lower Kimmeridgian to upper
Kimmeridgian; probably upper Kimmeridgian. About 6 km
south of Tamazunchale along Rt. 85 (Mexico, D. F.—Nuevo
Laredo Highway) near km post 267 (= old 350). Zone 2.

MX-81-54. Upper portion of lower, more massively-bedded part of
Taman Formation. Medium- to massively-bedded, dark gray,
micritic limestone with thin shale intervals containing lime-
stone nodules. Lower Tithonian part of Zone 3. Near final

occurrence of Aulacomyella Furlani, 1910, and top of Virga-
tosphictes mexicanus-Aulacomyella neogeae Zone of Cantu
Chapa (1971). 25 m below first occurrence of calpionellids in
lower part of upper thin-bedded Taman. 0.75 km west-south-
west of hanging bridge over Río Moctezuma at La Vega Larga
along Rt. 85 (Mexico, D.F. —Nuevo Laredo Highway); about
5.75 km west-southwest of Tamazunchale, S. L. P.

MX-82-3. Lower portion of lower, more massively-bedded part of

the Taman Formation. Platy, thin-bedded, dark gray, micritic
limestone interbedded with medium bedded dark gray, micritic
limestone. Above first occurrence of Aulacomyella Furlani,
1910, in the Taman Formation. 0.3 km east-northeast of MX-
80-20 (see above). Somewhat east-northeast of km post 264
on Rt. 85 (Mexico, D.F.—Nuevo Laredo Highway); 4.2 km
east-northeast of village of Taman, S. L. P. Zone 1.

MX-82-8. Lower portion of lower, more massively-bedded part of

Taman Formation. Predominantly medium bedded, dark gray,
micritic limestone with occasional thin beds 10.2 cm (4 in) to
20.3 cm (8 in) thick. Samples from adjacent 10.2 cm (4 in) and
20.3 cm (8 in) layers. First occurrence of Mirifusus Pessagno,
1977a. Apparent base of Zone 2. Adjacent to and slightly east
of km post 266 on Rt. 85 (Mexico, D.F. —Nuevo Laredo High-
way); 6 km east-northeast of village of Taman, S. L. P.

MX-82-37. Lower portion of thin-bedded upper part of Taman

Formation (= lower Pimienta of Cantu Chapa, 1971). Thin-
bedded, black micritic limestone with thick beds of black, yel-
lowish weathering shale containing abundant, black, micritic,
fist-sized limestone nodules. Thin-bedded upper Taman oc-
curring in tight, overturned, synclinal fold; infolded into lower
massively-bedded part of Taman. (Note: Same synclinal struc-
ture with infolded upper Taman exposed on Rio Moctezuma
below, slightly west of hanging bridge.) Zone 4 (lower part).
Above last occurrence of Aulacomyella Furlani, 1910, in more
massively-bedded part of Taman and hence, above the
Virgatosphinctes mexicanus—Aulacomyella neogeae Zone of
Cantu Chapa (lower Tithonian); equivalent to Mazapilites Zone
of Cantu Chapa (1971). The occurrence of calpionellids in the
lower part of the thin-bedded upper Taman suggests that the
MX-82-37 horizon as well as all or at least part of the Ma-
zapilites Zone of Cantu Chapa is assignable to the upper Ti-
thonian (see p. 10). On new unpaved road north of Río Moc-
tezuma and above north side of Taman; north-northwest of
hanging foot bridge over the Río Moctezuma.

Baja California Sur; Vizcaino Peninsula;
Eugenia Formation

BJV-20. Volcanogenic member (lower member) of Eugenia For-

mation (Barnes, 1982). Olistostromal unit bearing limestone
nodules containing common Buchia piochii (Gabb, 1869) and
associated Zone 4 Radiolaria. Underlying pillowed andesitic
basalt flow and Eugenia strata of Berriasian to early Haute-
rivian (Zone 5) age. East of road and near mouth of Arroyo
Amargura at coast.

34 BULLETIN 320

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Renz, O.

1978. Aptychi (Ammonoides) from the Late Jurassic and Early
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1967. Chapter 8 (Protozoa), pp. 291-332, in The Fossil Record.
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Riedel, W. R., and Sanfilippo, A.

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BULLETIN 320

Wimbledon, W. A., and Cope, J. C. W.
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1977. Some ammonites of the Klentnice Beds (upper Tithonian)
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Ziegler, B.

1971. Grenzen der Biostratigraphie im Jura und Gedanken zur
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Jurassique à Luxembourg, 1967. Mem. Bureau de Re-
cherches Geologiques et Minieries, Fr., No. 75. pp. 5-757.

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VOLUME 87

Y,

OG

'AN PALEONTOI

Cx
Lo

TINS OF AMERIC

JLLE

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All figures are scanning electron microgra

JURASSIC RADIOLARIAN ZONATION: PESSAGNO ET AL.

EXPLANATION OF PLATE 1

reference for the magnification of all figures.

Figure
1-4, 12, 13, 17.

—

14-16, 18, 19, 21.

20.

22-24.

Hsuum mclaughlini Pessagno and Blome, new species... sete senses:
Volcanogenic-pelagic strata overlying the Coast Range ophiolite (Stanley Mt. remnant) at Alamo Creek, San Luis
Obispo Co., California. loc. SA-43B: Lower part of Zone 4; upper Tithonian.

Diagnostic characters.—Test rounded apically with short, massive horn. Dense outer latticed layer formed from

costal projections obscuring inner latticed layer on proximal one-quarter to one-half of test. Costae straight, often

bifurcating.
1, 12, 17. Holotype (USNM 340257). Scale bar = 120, 75, 75 um respectively. Note density of outer latticed

layer proximally, caused by numerous costal projections.
2, 13, 3, 4. Paratypes (Pessagno Collection). Scale bar = 198, 66, 150, 171 um respectively.

< Hsuum cuestaense Pessachos 97/28. 2 4 ee o quent

Holotype (USNM 21976). Volcanogenic-pelagic strata overlying Coast Range ophiolite at Point Sal, Santa Barbara

Co., California. loc. NSF-907: Zone 2; Kimmeridgian. Scale bar — 171 um.
Diagnostic characters. — Test pointed apically with short horn. Outer latticed layer not dense, costal projections not

strongly developed. Costae straight, massive, and quite continuous.

C suum maxwell pessaeno Oia ert e tuc opu uL qu cuu ae

Holotype (USNM 21980). Same location as in figs. 1-4 above. loc. NSF-973: Zone 2; Kimmeridgian. Scale bar = 99

um.
Diagnostic characters. — Test narrow, somewhat rounded apically with very short horn. Outer latticed layer not

dense with few costal projections. Costae short, staggered, discontinuous.

. Perispyridium ordinarium (Pessagno, tra o eu co MM c NE MT E

Holotype (USNM 21972). Same location as in fig. 5 above. loc. NSF-908: Zone 3; lower Tithonian? Scale bar —

99 um.

Diagnostic characters. — Cephalis globular, large for genus. Peripheral latticed shell flat, weakly nodose, thin, markedly
triangular in outline. Apical and primary lateral spines outside of peripheral shell triradiate (axial section), of medium
length, bluntly terminating. Six large pericephalic pores. Pericephalic pores in areas between spines extending to edge

of test.

. Perispyridium tamanense Pessagno and Blome, TE ROR ee rc C uc cu a a rest

Holotype (USNM 319127). Taman Formation. loc. MX-81-54: Near Tamazunchale, San Luis Potosí, Mexico; Lower
Tithonian part of Zone 3. Note specimen is replaced by pyrite. Scale bar — 99 um.

Diagnostic characters. — Cephalis globular, medium sized. Peripheral latticed shell rounded, subtriangular in outline,
wide for genus, with very massive knoblike nodes at pore frame vertices. Apical and primary lateral spines outside
of peripheral latticed shell triradiate (axial section), pointed.

. Orbiculiforma lowreyensis Pessagno, 19778... cc 1.0... +. conan nan r eere eese nene ns

Great Valley sequence; upper part of Buchia piochii Zone of Jones et al., 1969. loc. NSF-823: Zone 4; upper Tithonian.
Middle Fork of Elder Creek, Tehama Co., California.
Diagnostic characters. — Medium sized, relatively shallow central cavity. Test periphery angled. Surface of test sloping
steeply between the central cavity and the periphery.
9. 10. Holotype (USNM 21960). Scale bar = 120 um.
11. Paratype (USNM 21961). Scale bar — 150 um.
Vallupus hopsoni Pessagno and Blome, new Bossi en eh c DUUM ett ies wie ie ae
Same location as in figs. 1-4 above. loc. SA-43B: Lower part of Zone 4; upper Tithonian.

Diagnostic characters. —Test with single medullary shell having fragile pentagonal and hexagonal pore frames.
Cortical shell with massive pentagonal and hexagonal pore frames lacking nodes at vertices and with prominent,
imperforate, cylindrical collar-like structure having circular aperture. Pore frames tending to become more elongate
at junction with collar.

14-16, 18, 19. Paratypes (Pessagno Collection). Note collar-like structure on cortical shell and presence of single
medullary shell. Scale bar = 48, 42, 39, 36, 42 um respectively.
21. Holotype (USNM 340255). Scale bar = 42 um.
Vallupus A ate eee ek y E A A
Same locality as in figs. 1-4 above. loc. SA-43B: Lower part of Zone 4; upper Tithonian. Scale bar = 48 um.
Praeconocaryomma immodica Pessagno AIAG POISSON eo ida ed TES

Diagnostic characters.—Cortical shell with prominent mammae which tend to be very high in relief. Mammae
pentagonal in outline. First medullary shell with meshwork comprised of equilateral triangular pore frames.

22. Specimen from volcanogenic-pelagic strata overlying Coast Range ophiolite (Stanley Mt. remnant) at
Alamo Creek, San Luis Obispo Co., California. loc. NSF-973: Zone 2; Kimmeridgian. Scale
bar = 75 um.

23. Holotype (USNM 264005). From radiolarian chert in Franciscan Complex, Mendocino Co., California.
loc. BK-605: Upper part of Zone 1; lower Kimmeridgian? Scale bar = 60 um.

24. Paratype (USNM 264006). Same location as cited for fig. 23. loc. BK-605. Scale bar = 75 um.

89

phs of Upper Jurassic Radiolaria. Scale bar (upper right) is used as a

25

25

24

24

22

25

23

24

BULLETIN 320

EXPLANATION OF PLATE 2

All figures are scanning electron micrographs of Upper Jurassic Radiolaria (Nassellariina) from volcanogenic-
pelagic strata associated with the Coast Range ophiolite, California Coast Ranges. Scale bar (upper right) is used
as a reference for the magnification of all figures.

Figure Page
13 10135314: 2125. Masts baileyi Possagno ida de dle. a ec ara ce ee 26

Diagnostic characters.—Test thick, consisting of three latticed layers: an inner layer of pentagonal pore frames
and two outer layers of triangular pore frames. Outer latticed layer of first eight post-abdominal chambers lacking
discrete circumferential ridges, consisting of massive nodes interconnected by bars to form triangular pore frames;
outer layer of remaining post-abdominal chambers with two staggered rows of triangular pore frames inserted
between closely spaced, generally wide and massive, nodose circumferential ridges. {

1, 21, 23. Holotype (USNM 21992). Strata overlying ophiolite at Point Sal, Santa Barbara Co., California.
loc. NSF-908: Arrow (fig. 21) points to inner layer of triangular meshwork. Lower part of Zone 3;
lower Tithonian? Scale bar = 240, 75, 66 um respectively.
2, 13, 17, 22. Specimens from strata overlying ophiolite (Stanley Mt. remnant) at Alamo Creek, San Luis Obispo
Co., California. Specimen in fig. 2 malformed due to probable injury during growth. Specimens in
fig. 13 and 17 show innermost layer of pentagonal pore frames. Specimen in fig. 22 lacks outer |
layers of triangular meshwork distally. loc. SA-43B: Lower part of Zone 4; upper Tithonian. Scale |
bar = 171, 171, 99, 99 um respectively. |
3. Specimen from red manganiferous chert interbedded with vesicular basalts in ophiolite at Wilbur i
Springs, Colusa Co., California. loc. NSF-997: Zone 3; lower Tithonian? Scale bar = 198 um. |
10. Topotype from strata overlying ophiolite at Point Sal, Santa Barbara Co., California. loc. NSF- |
908: Lower part of Zone 3; lower Tithonian? Scale bar — 198 um. |
AL LOMAS US Medio aa rara USAS or e Re IR es a IN HE 26

Diagnostic characters. — Test wall thin, consisting of an inner latticed layer of pentagonal pore frames. Pore
frames of inner latticed layer inserted in two staggered rows between narrow, slightly nodose circumferential
ridges. Partially formed outer (second) latticed layer consisting of rods and interconnecting bars which combine |
to form triangular pore frames apically. Circumferential ridges usually more widely separated than with M. baileyi
Pessagno, 1977a.

4, 19, 5, 18. Specimens from strata overlying ophiolite at Point Sal, Santa Barbara Co., California. loc. NSF-
908: Lower part of Zone 3; lower Tithonian? Scale bar = 240, 150, 240, 99 um respectively.
6-8, 11, 20. Parvicingula colemani Pessagno and Blome, new species o... 2/7
Strata overlying ophiolite (Stanley Mt. remnant) at Alamo Creek, San Luis Obispo Co., California. loc. SA-43B:
Lower part of Zone 4; upper Tithonian. |

Diagnostic characters. —' Test elongate, cylindrical to subcylindrical, blunt apically with short, massive horn. |
Eleven to fourteen post-abdominal chambers. Massive, irregular polygonal pore frames on cephalis, thorax, and
abdomen. Post-abdominal chambers separated by weakly developed circumferential ridges. |

9, 11. Holotype (USNM 340259). Scale bar = 171, 66 um.
7, 8, 20. Paratypes (Pessagno Collection). Scale bar = 171, 150, 48 um respectively.

9. NGpord:tospensissbessdpHosi07Ua5 a ur ed c mee o LIT Lt e Lr RE d ce 24
Topotype from strata overlying ophiolite at Point Sal, Santa Barbara Co., California. loc. NSF-907: Zone 2; |
Kimmeridgian. Scale bar = 54 um. |

Diagnostic characters. — Massive pore frames; short, massive horn; short massive, incurved feet. |

12, 16,24. Mirifusus.guadalupensis Pessaguo; 197735 IEA DC ERU 26
Specimens from strata overlying ophiolite at Point Sal, Santa Barbara Co., California. loc. NSF-907: Zone 2;
Kimmeridgian.

Diagnostic characters. — Test comprised of two latticed layers. Inner latticed layer of post-abdominal chambers
composed of three rows of very small tetragonal, pentagonal, and hexagonal pore frames set between massive,
closely spaced, often quite nodose, circumferential ridges. Outer layer of latticed meshwork on post-abdominal
chambers consisting of triangular pore frames formed by thin bars connecting with nodes on circumferential
ridges.

12. Paratype (USNM 21995). Scale bar — 150 um. |
16, 24. Holotype (USNM 21994). Scale bar = 198, 120 um. |

14,15 Parviciwigulayblow ROSS ano DITTE -reaa o eue a e ec Ok da oo 26 |
Holotype (USNM 21984). Strata overlying ophiolite at Point Sal, Santa Barbara Co., California. Scale bar = 150, |
84 um.

: Diagnostic characters. — Test short, cylindrical; dome-shaped, broad apically with short horn. Eleven to fourteen |
post-abdominal chambers. Cephalis, thorax, abdomen, and usually first two post-abdominal chambers with )
irregular, massive, polygonal pore frames. Remaining post-abdominal chambers with pentagonal pore frames |
arranged in three (rarely four) rows between circumferential ridges. Circumferential ridges becoming more strongly
developed in a distal direction.

BULLETINS OF AMERICAN PALEONTOLOGY, VOLUME 87 PLATE 2

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BULLETINS OF AMERICAN PALEONTOLOGY, VOLUME 87 PLATE 3

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JURASSIC RADIOLARIAN ZONATION: PESSAGNO ET AL. 41

EXPLANATION OF PLATE 3

All figures are scanning electron micrographs of Radiolaria (Nassellariina) from the California Coast Ranges. Scale
bar (upper right) is used as a reference for the magnification of all figures.

Figure
1-4, 11-13, 17, 22. Parvicingula excelsa Pessagno and Blome, new oan e eco pei Ie ene 27
Specimens from volcanogenic-pelagic strata overlying the Coast Range ophiolite (Stanley Mt. remnant) at Alamo
Creek, San Luis Obispo Co., California. loc. SA-43B: Lower part of Zone 4; upper Tithonian.
Diagnostic characters. —Test elongate, conical with massive, moderately long, conical, pointed horn. Apical portion
of test (cephalis through abdomen) inflated, turret-like in aspect. Post-abdominal chambers with three rows of
í hexagonal pore frames inserted between well-developed, weakly nodose circumferential ridges. Most complete tests
with up to fifteen post-abdominal chambers.
1, 11, 17, 22. Holotype (USNM 340261). Note inflated nature of test proximally with outer layer of microgranular
silica covering latticed meshwork beneath (figs. 1, 11). Scale bar = 171, 54, 54, 54 um respectively.
2, 12, 3, 13. Paratypes (Pessagno Collection). Scale bar = 198, 66, 132, 48 um respectively.
4. Topotype destroyed during SEM work. Scale bar = 150 um.
5-7, 14, 19, 24, 25. Parvicingula jonesi Pessagno, 1977b e e e a ee nee nee eee es 28
Note all specimens replaced by calcite.
| Diagnostic characters.—Test fusiform, dome-shaped apically with short horn and well-developed narrow terminal
tube on final post-abdominal chamber. Post-abdominal chambers with three rows of pentagonal pore frames inserted
between weakly nodose, prominent circumferential ridges. Eight to eleven post-abdominal chambers.
5, 25. Holotype (USNM 242813). Great Valley sequence at loc. NSF-823, Tehama Co., California. Upper
| part of Buchia piochii Zone. Upper part of radiolarian Zone 4. Scale bar — 120, 75 um.
| 6, 14, 19, 24. Specimen from Great Valley sequence at loc. MG-77-3, Napa Co., California. Lower part of B. piochii
Zone? Middle part of radiolarian Zone 4; upper Tithonian. Scale bar = 198, 48, 48, 48 um respectively.
7. Topotype. See fig. 5 above. Scale bar = 198 um.
. Parvicingula santabarbaraensis Pessagno, LOFT ig cp RE CIE ig tee Nus uM 28
Holotype (USNM 21990) from volcanogenic-pelagic strata overlying Coast Range ophiolite at Point Sal, Santa
| Barbara Co., California. loc. NSF-908: Lower part of Zone 3; lower Tithonian? Scale bar — 150 um.
Diagnostic characters. — Test broad, conical, pointed apically with massive, long horn terminating in crown-like
| mass where horn branches and forms four rays. Post-abdominal chambers with three rows of hexagonal pore frames
| inserted between well-developed, weakly nodose circumferential ridges. Well-preserved specimens with ten to fifteen
post-abdominal chambers and long, narrow terminal tube on final post-abdominal chamber.
9. Ristola boesii (Parona, 1890) sensu lato... ees 28
| Great Valley sequence at loc. NSF-1068, Tehama Co., California. Buchia pacifica Zone (Lower Cret.: iower to middle
Valanginian). Radiolarian Zone 5, Subzone 5B. Specimen not as rounded apically as Parona’s type; replaced by
calcite. Scale bar = 150 um.
10. Ristola altissima (Rüst, 1885) ne e a een erent rte eee cnet ere reece 28
From same location as cited for fig. 8 above. loc. NSF-908: Lower part of Zone 3; lower Tithonian? Scale bar = 300
um. .
| Diagnostic characters.—Test long, cylindrical with knoblike apical portion (cephalis through thorax) which lacks
| a horn. Proximal portion of test sometimes somewhat inflated on some specimens. Post-abdominal chambers with
three rows of small, hexagonal pore frames inserted between very closely spaced, highly nodose circumferential
ridges. Up to twenty-seven post-abdominal chambers present on complete specimens. Final post-abdominal chamber
with broad terminal tube.

| 15, 20, 21. Parvicingula vera Pessagno and Whalen, TORD E irs M a Dor d e RR RAO 28
Diagnostic characters. — Test broad, conical with long, thick, massive, pointed horn. Post-abdominal chambers

with three rows of hexagonal pore frames inserted between weakly developed circumferential ridges. Usually six to
eight post-abdominal chambers.
15, 21. Holotype (USNM 307268) from upper member of Snowshoe Formation, John Day Inlier, east-central
Oregon. loc. OR-501C; uppermost Bathonian. Scale bar = 48, 159 um.
20. Specimen from lower, massively bedded part of Taman Formation near Tamazunchale, San Luis
Potosí, east-central Mexico. loc. MX-80-23; Kimmeridgian. Scale bar = 99 um.
16, 18, 23. Ristola sp. aff. R. boesii (Parona, 1890) . ciiin ees 29
Calcified specimen from Great Valley sequence at loc. NSF-845, McCarty Creek, Tehama Co., California. Upper
part of Buchia pacifica Zone (Lower Cret.: middle Valanginian). Scale bar — 99, 48, 48 um respectively.

00

BULLETIN 320

EXPLANATION OF PLATE 4

All figures are scanning electron micrographs of Radiolaria (Nassellariina) from the California Coast Ranges. Scale
bar (upper right) is used as a reference for the magnification of all figures.

Figure
i5

Ze de

Nn

m

No)

12-14.

16, 18, 19;

“Fo. SUAMIICVCHISE CSSA LINO A ITTA a ri EE I Se SES E o TET ict E a Qe A a a
Holotype (USNM 21982). From volcanogenic-pelagic strata above the Coast Range ophiolite (Stanley Mt. remnant) at Alamo
Creek, San Luis Obispo Co., California. loc. NSF-973: Zone 2; Kimmeridgian. Scale bar = 120 um.

Diagnostic characters. — Test conical with short horn. Single latticed layer composed of linearly arranged square pore frames
with nodes at corners. Not showing two layers of latticed meshwork as typical of Hsuum Pessagno, 19772; costae and costal
projections absent.

'RUSTOTE HSHISPOSSADHOS IO ae TM IND TTE eae E. MN DM I Car MIP Ne ER RR DUE ID S RUNE
From volcanogenic-pelagic strata above Coast Range ophiolite at Point Sal, Santa Barbara Co., California. loc. NSF-908:
Lower part of Zone 3; lower Tithonian?

Diagnostic characters.—' Test conical lacking a horn. Pore frames of post-abdominal chambers arranged in three rows
inserted between nodose (^H-linked") circumferential ridges. Two flanking rows of pore frames pentagonal in shape, steeply
sloping away from circumferential ridges. Central row of pore frames tetragonal in shape, smaller in size. Seven to eight post-
abdominal chambers. Final post-abdominal chamber with a tubular projection.

2. Holotype (USNM 21986). Scale bar = 120 um.
3. Paratype (Pessagno Collection). Scale bar = 99 um.

ce SAILOUITEPALEIAPERSAGTION 197723: Ay ree RAE rx RM TR TE ME QI M MED cT LE

Holotype (USNM 22006). Same location as cited for fig. 2 above. loc. NSF-908: Lower part of Zone 3; lower Tithonian?
Scale bar = 75, 60 um.

Diagnostic characters. — Test monocyrtid with short triradiate horn and three long, incurved, triradiate feet. Test with
circular to subcircular pores set in widely spaced tetragonal and triangular pore frames.

se ODesucapsula-motroensis Possaeno 3194754. 5. p eei Sassi esos iE ALL TIE 1er E RI TOS ed De Ced er

Holotype (USNM 21996). Same location as cited for fig. 2 above. loc. NSF-907: Zone 2; Kimmeridgian. Scale bar —
198 um.

Diagnostic characters. — Proximal portion of test (cephalis to third post-abdominal chamber) conical. Fourth post-abdominal
chamber quite large and globular forming three-quarters of test. Wide, tubular, cylindrical extension occurring on fourth post-
abdominal chamber. Meshwork irregular, spongy.

OLO Pr Debra EERIE LIT TAi exuere Us Ur edu uM m UM ON CT NENNT US TUE]

Holotype (USNM 21988). Same location as cited for fig. 2 above. loc. NSF-908: Lower part of Zone 3; lower Tithonian?
Scale bar = 240 um.

Diagnostic characters. — Test extremely elongate when complete, conical apically. Most of test cylindrical. Post-abdominal
chambers closely spaced, numerous (thirty-three or more) with three rows of uniformly sized hexagonal pore frames between
circumferential ridges. Circumferential ridges thin, nodose, closely spaced.

Se RStolibsp. ch Re DoesnmParond;-19590y- o E A r. EAE VOEE ONE E EE E E A AE E EE MD Ed

From volcanogenic-pelagic strata above Coast Range ophiolite (Stanley Mt. remnant) at Alamo Creek, San Luis Obispo Co.,
California. loc. SA-43B: Lower part of Zone 4; upper Tithonian. Scale bar = 120, 60 um.

t opeacapma rouna (inde TIO eea NS UN. NO, EO NIE DTE ID o Tope

Diagnostic characters. — Apical portion of test (cephalis through second post-abdominal chamber) conical. Pronounced
(deep) strictures separating second from third and third from fourth post-abdominal chambers. Final post-abdominal chambers
quite inflated.

8. Specimen calcified. From Great Valley sequence at McCarty Creek, Tehama Co., California. loc. NSF-845: Upper
part of Buchia pacifica Zone; middle Valanginian. Radiolarian Zone 5, Subzone 5B. Scale bar = 198 um.
10. Pyritized specimen from Great Valley sequence at McCarty Creek, Tehama Co., California. loc. NSF-1019: Upper
part of Buchia keyserlingi Zone; upper Valanginian. Radiolarian Zone 5, Subzone 5C. Scale bar = 198 um.

< Qpesacapsnla spats... rotunda (EI a CENE TE GV a OON TER

Specimen from volcanogenic-pelagic strata overlying Coast Range ophiolite at Point Sal, Santa Barbara Co., California. loc.
NSF-908: Lower part of Zone 3; lower Tithonian? Scale bar = 300 um.

SEHCVFHODUm. Ply Cline ked md Sauk Os a QUTD E vate O E a ae
From volcanogenic-pelagic strata above Coast Range ophiolite. Note pores in strictures and presence of a cephalopyle (figs.
13, 14).

Diagnostic characters. — Test tricyrtid. Weakly developed stricture between cephalis and thorax; prominent stricture between
thorax and abdomen. Rows of circular pores occurring in stricture between thorax and abdomen and at base of abdomen.
Cephalopyle occurring at base of cephalis. Abdomen with widely spaced, massive costae.

12, 13. Specimens from Alamo Creek, San Luis Obispo Co., California. loc. SA-29: Upper part of Zone 2; Kimmeridgian.
Scale bar = 39 um.
14. Pyritized specimen from Point Sal, Santa Barbara Co., California. loc. NSF-900: upper part of Zone 1(?); Kimmer-
idgian. Scale bar = 30 um.

-Furano fled Pessagnor atid BION; 1982 tice Ean ai delevit ue o ale E A E a

Holotype (USNM 319135). Volcanogenic-pelagic strata overlying the Coast Range ophiolite at Point Sal, Santa Barbara Co.,
California. loc. NSF-908: Lower part of Zone 3; lower Tithonian? Scale bar = 190 um.

Diagnostic characters.— Long, incurved feet; feet triradiate in axial section. Distal half of one foot displaying curvature
outside of equatorial plane of test. Horn short, slender, curved, triradiate in axial section. Thorax with massive hexagonal
pore frames.

Andromeda violae Bara ne LIRO. o ets Sah ola Coa ere vasa ee ete A aE e sod B a AA
From volcanogenic-pelagic strata overlying Coast Range ophiolite (Stanley Mt. remnant) at Alamo Creek, San Luis Obispo
Co., California. loc. SA-43B: Lower part of Zone 4; upper Tithonian. Scale bar = 120, 48, 108 um respectively.

Diagnostic characters. — Test multicyrtid, hat-shaped with pronounced shelf-like stricture separating last two post-abdominal

chambers. Pore frames tetragonal, pentagonal, and hexagonal; increasing in size in a distal direction.

20

30

29

29

29

29

30

30

30

30

BULLETINS OF AMERICAN PALEONTOLOGY, VOLUME 87 PLATE 4

Y

se,
9.

BULLETINS OF AMERICAN PALEONTOLOGY, WOLUME 87 PLATE 5

wed
RE
MOE
EAN

JURASSIC RADIOLARIAN ZONATION: PESSAGNO ET AL. 43

EXPLANATION OF PLATE 5

All figures are transmitted light micrographs of Upper Jurassic Radiolaria from volcanogenic-pelagic strata
overlying the Coast Range ophiolite (Stanley Mt. remnant) at Alamo Creek, San Luis Obispo Co., California.

Figure Page
1. Vallupus hopsoni Pessagno and Blome, new Species. ... 0.6... hehehe] he eene 23
Paratype slide (USNM 340256). loc. SA-43B: Lower part of Zone 4; upper part of lower Tithonian or lowermost part of upper
Tithonian. Length of specimen = 260 um.
2, 3. Parvicingula colemani Pessagno and Blome, new species |... hehe ehh 2r
Paratype slide (USNM 340260). See fig. 1 above. loc. SA-43B.
2. Length of specimen (exclusive of horn) = 420 um.
3. Length of specimen (exclusive of horn) = 450 um.
4. 5.. Panvicingula excelsa Pessano and Blommie MEN SPEIR AE e ees pe verte sit ne «LE ee ae p
Paratype slide (USNM 340262). See fig. 1 above. loc. SA-43B.
4. Length of specimen (exclusive of horn) = 425 um.
5. Length of specimen (exclusive of horn) = 400 um.
6. Hsuumimelaughlini Possagno and Blome new SECIS o ca oda depuis ei mis cota ae ees estie ses eee mes era e EID as 25
Paratype slide (USNM 340258). See fig. 1 above. loc. SA-43B. Length of specimen (exclusive of horn) — 425 um.

44 BULLETIN 320

INDEX

Note: Page numbers are in lightface; plate numbers are in boldface type; F = foldout inside back cover.

AACHEN C Ru a EU Oe 12,18,20,24-26 OVANS OCA RR SRI RR E
WI a A E RA E ooo duge re enda 15 Rasenia a
ACNE AM fotos et ECT QOOQOE. 8,14,15,17,F SOME CCN AS e AME Carte Tape ers 15
Acanthicus Beds e 15 TONAS US ceva T ERA RR E Ee o 15
Acanthocirens Squinabol. 1903 ............. eee 10,16,20. 215 DICO a E ARDE E NERO OS ESL STIR
discranocanthos (Squinabol, 1914) ........................ 10,20,21,F VIRO Fe Aa Mcd Ms CSS e CS 7
VATION SH (SqumabO TILA) cose cope ce eee reor de eere rro derrocado Selena OT E I T T 15
ACUI TT ETE OCON ID T crios UNE RENNES LOHWIODOI MSS esi e ier ets alge RR eT Jis
v DEUDA c OS TERQUE ISHDneumaylid sees te tT T cee oso 14,33
Picchu c co ck Iro c d NNNM E Sa DIO ZENE e e etes OD 14,33
BEIGORS a PEN. E T A E een SUD DIATIILES tada, E I S E
IL C HU NEGOCIO A ISD STCUENOCEN OS™ eve cd ECCE I Se eS BE
e O EE x E EH NM E SUONO A dc A LEE RE Scd di
Esto oom Mec. 0003. qM M ME ULA eee MENU. co ac RO TOL 1
ACNE rM. ANA EA OH EA S ce SUE id o nc Tae elas cee ne ree: oc 15
altissima, Gh Salatynotasiti. da cab E
Lithocampe UCA iseki ieee a Ea E 15
PUTS TONAL aces E ES HEM ICLOCEPUS: a ss Galt SI ek sec 18
GES SUIT DUE AEVICI DM basar eee Inde ope eversa entrara events 28 US a 05 TRE NTR 18
Ammonites KORDUS PROTESE cmt TR e PRG. UE cade F
AEOS KAENA Cec rA CAR AA e VINEATOSPRIRCION feat n PERROS E re F
Amoeboceras .... Amoebites Backmann lOZS OUT X0 4903.4 ANN r F
Aspidoceras ...... AmoebocerastHyattelo 00e atra. Beber. 6 F
acanthicum ... Andromeda Baumgartner, 1980b .............ccccccsecceeeeeeeseees 20,30
Vo CC oA dude A ia ED RUE A N E crassa Bawmearinen OS OD monio ist dee Een 30
Aulacosphinctoides F yiolaesBatnigartierel 980 muto eter be RH d os 20,30
Blanfordiceras anguifoxnmJayZone Suo. bre onem mex sites ones ors 15
Corongoceras anilanim GANODTUTIIS, Bak ASSERERE SEU ANTI A 18
TALA A A N O F Aptychi
wr ae E TREE CN NIU E PUEDE Rd DEED F Granulaptyohustuson 3a ARIE. MOAR ume Y Nus y
plicatiloides F planulatiswen, mood dae Gg S wem em med 17
Discosphinctes .. F JiaevaptyohusbaA. et eme E DT St EER 16,17
caribbeanus F JO SOLON ERN re RD OE E S TREE 17
NOT ATONE Stree SU conte ree rue E E O TES UR ITA F VOPISSVOYOHIDOPHS ONERE SE EIE 17
D OTC Steet euentu M c 7,8,F VICOS AO IA E EA IEA ON 16,17
IE SAS. CIA E E O O F AMEN ADE CHUS eats E E telat Sesa taa a a 15-17
IOC AOS, coo, TAS NA CREA 13,14,17;38;E. SOV CEU eras SIC QUA aa eiie ET D ES it]
Wee... O D 14,17,F NTU ICUOS Seer etate ad 16)
Be OU aa) AA E E A E S 13 grupa B, lamellosus 16
o A dm E RIO ME 7,F (D TROSTADRICUSES Eo er EI EIE T ts 17
AIN UIA PES acs cue cerco retur s e dert op Ure SEC TES 15 IMUCTOCOSTATUS ses e AT E A E E aa de 17
UL NE A see ems 7,F DICIAGENSIS cerere vernederen E Re rete 17
TY OR A A O co 7 POOLECOSTALUS miii deu TR RU REDE 15
Pm coeur Do MT, PM ME V A E wapa A a. LL rectecostatus mosca ao E a sn 16
O A AAA E E eM s F SDAPSHOMELOSUS tii ta S home
RN et acess tate cocoa A EM 17 otapa B, Dar a melo Usar E UE cE its 16
ES erc MEME E E 17 SD-CUE IRMOTO E E RTT eee 17
CRAGIN L TE EUT S veces vete sty rnaus shag cotton roe IR 157) PUNGCEGDEY CHUS Sanciones RR SNE ds ao in
Pu) TI doe NM CD IS DUNCAN Se 157
TP AGUCC Secs noo cca E UM ^ EO Apy chus CO Site testes dd AA S bone 15
DU LAPYR RICO QUE TTC DUIS TIMES ZSDUy CIUS MOZO ereer ene ae a DERI. 15-17
Eas cv ni VO ET E NM AroHaeospongoprunumPoessapnio; 19739. tee ETT CNET 16
IGE TICS REN AS RAI He FOROR RA IT Pede ets paa opa Dea saran or a oA E A E 16
Microacanthoceras AO e e A E IR UT 8,15-17
Negreliceras Arkell, Kunmel and OI Seere er ierre rrii 14,33
Ochetoceras AAO ONR EET IOE E AEEA EA TT 15)
doe rS meter NG eB ES Mic Mp aki E acanticum ODD so 1803 e TT 15
Parodontoceras ATICO COIE Sls I aerea o IN ER EN EET EINE E

PYONICOPGS: oe rient E “ACEH A Sine) RO Ola a red cse Me e Ue MI T TRE 13

JURASSIC RADIOLARIAN ZONATION: PESSAGNO ET AL. 45

AMAYA Furlani, 1910 nesne 10,14,17,19,33
Aulacosphinctoides Spathy 1923 oeiee rnk e N F
AustralRealmes mis vetet vem tras orate erases 22
GULLS SIOAOTENSIS' ZONE. cer rs ka can eg Re ee e ds 8,F
AS cts E EE D 9,10,12,19,26,32,F
Baja California Sur ............... 6,9,13,18,19,21,22,24-28,30,31,33

IMizeaiosPeninsula. uote a 31,33
IPSO SORTI NEED 12,15,18,30

MATAR, ADA ML
Bonola GOA Deter cece airs
Bain esi (10.8 A cise any
Barron € 54 cc rain
Bathonian 12:14 5 47.28
Baumgartner (Is DMA teta ds 16,18,21
Baumgartner G98 Ob) ee consirier oo eos A
Baumgartner (1980, oral commun.)
Baumgartner, DeWever, and Kocher (1980) ............. 6,10,13-20,
24,26,28-31,F
DayleiZoncabebt: AE IN a inte E n US 8,F
DENCIA A ERE cvv RTO Rien EN Salo alos
SBGd SOF MUNG. correos bate S 15
BOLO Dos caceria a dubi d SEES ant 16
TEME E AAA A O 14
SubhastatusQuenstedb tn arar S 14
BeneckexG 865) os cod sd amma 18
'Benmasela Uhlie, 1905 occitano TD ato Sisa 8
BOr AA a cerescecc cccucscounaruene

bifurcatus ZONE a
bimammatum Zone
Biochronozone A of Baumgartner, DeWever, and Kocher .... 14,

16,20,F
Biochronozone B of Baumgartner, DeWever, and Kocher ..... 20,
2LF
Biochronozone C of Baumgartner, DeWever, and Kocher ..... 13;
20,21,30,F
Biochronozone D of Baumgartner, DeWever, and Kocher ..... 13
'DWencu AIG ADI LOSDINGELG TRAE ol Du esu eque
Blanfordiceras Cossmann, 1907
bowi RA VOLADOR RAS Score ii aa
boesii,
Dictyomitra
Parvicingula
PA A O DEE
Goe AERO oea a a AO Di 29
Doesiu(ob)RISTOlQ dde NE d$ 8 29
Bone te i956): Pase EROS tii cd seb DU ESI
BorealiRealm fes sesso AR Teese teres 7,8,19,22,24-26,28-31,
BOSiYCRDEGTEROMIOS L886 nde eo oen 15
ANA A eue O REO 15
Brins Column Manani asas bed 20,F
Buck sda tn das 13
Buchia Rouillier, 1845 .................... 7,8,10,13,14,19,21,31-33,F
GONGENTNIGA (SOW Oya SLT arsana 13,14,33,F
“fischeriana (C OLDIES TSAA) iaa 8
MOSGUeNSIS Vom Buoh AL S44) narran ce p 13,14,F
speal A: Okensis:(Paviow, 190795... eet omnes 8, 10,13,32.
pioch (Gabh 1869) 0090099 000 20D 7:8,10/13,19,2 805 335 E:
rugosa (MISCHO HM NSS USS) nope eie cavers CORE 13,14,33,F
uncitoides (BAVIOW 1907) a seen eren went 1041332
Buchar keyser EUZ BAG. oss ae toten petas RT MENS 39
Buchiaspeai Bokens On, oneic ain 7:10,13,20,32
BUEN MANC LONE ar TEC as oia 29,32

Buemia pioc Mi Zone eda. a a 111322289

"Bue hab ACES ZONE Uren E a 7,8,10,22,28,32
buchu BOA v EOS. A Da ass ohne ae RO

bukryi, Napora .......
Burckhardt (1906) ...
Burckhardt (1912) ...

Buro duels oe ARO
' @adischi (i932) it a 7
Galifotniali cet 5-10,12,13,17-20,28,29,31,F
jAlamoxeanyonziq ee v. sn a Scots aed 20
"Aa oS D6e ko e SUE siena there 9-13,23,25,27-31
Albano SPONE a apes atrial 32
Bittemvaten Canyon 4 catene MR Ue: 11,13,27,28,32
(a cesses eis 5-7,11-13,19,20,22-31,33
AM ea 5,6,9-13,19,20,23,25,27-29,31,32
Colusa County 32
Crowfoot Point 33
OTERI GEE a E dia da 20
IOA E IEE e 32
Eagle Rock
Elder Creek o ororen a eere A N mam E E 32
Mo ME 32
iErangiscan Complex se caba 5,20,32
A NE a T Lm T 92
(ey ser s Gear ak Sarco osas e dien stie 19
Glenn County 10,32
Great Valley SEQUENCO o 5.0.5... 10;14:13,20:27.28:32,33
Grindstone ¡Greta O andes E SQ IR 10,32
Guney Ranch Road: aaa rosse metodi aces 3%
Kamar Mountains curioses E sl 24
TOOR oroe

JEEE E a eee E rt E
Lowrey area
Lowrey Road

INICSAEUE ESK en N Sige a dape 10,32
Mounts t PEE ci o is 33
Paskenta
A A
Point Sal
Ridge
PotteuValleysROad- arniran nieda E 32
BRiouseiandbnsme E e Leu umecces sb ousc om soc RS OM
San Benito County
San Luis Obispo C QUI. acieirar a desea 10-12,31
SantasBarbarasountyss dra in 8 Ranna 10-12,31
Stanley MOuntain cns aisea 5,9-11,13,20,23,25,27-30
Sulfur: Greeks ct oss A eth 32
Reliaman e O UD eae re 9E A ia 32
volcanogenic-pelagic strata .......... 5:9,10;12,13,19,23,25,28:51
Wilbur Springs
Gall6sdame X roten
CANAS ALO Metal ES Lu s esse te ud ied basada e SUS
Gdipionelig Dorenn T902 ose NGA... ES La aont S svn TE
alpina Lorenz, 1902 7
INDICA EE SS Da E EA O a T g
Calpionellids
ORIPIODE ON EU comete sa oda at ARS, rame ba d ade F
DUNA Mee UL Pr MN O T T
EE E E T E IS SRE NTS fi
Calpionellopsis Y;
ML E A dele cri do umet oi dite en 2
UOTE pa EN. EUN eec ecce me Dv pcs ERES Te 7
(naso PIRE. d NR. ccs cuia ame i quii e Mn SU arcu RERUM Ue F

46 BULLETIN 320

EIUSMO EENE EEE PENTO Meee EHE E RE AE r 7
E SD E RET S S AINNE Ut IO 7
A A A A a men A ETS E
Gamionellopsis.Colom, 1948... score eed po crei dtt Donde od Tea 9
OA C adiseli;-D939 A A eade MEER 7
A Me de TIU MER 23,24
GO AOS CLOGENAN: nc cow ve ete A A Cos S F
COMO P TT DOBSHpTIO: 1979/59... A ote 18
anulatum Possagno and Poisson, 1981 ................ eese 18
AAA ATP aste eere erecto edes 7,10,13:14517;38; E.
Gants Bessagno-and. Whalen, 1982... dL Be tees 18
RY nee A veces idus da 14-17,28,30
a UTOTIEG a eher quero eset eos cabal EIE TE ETE VE 30
CGOZIDDOHWUS IDISGOSDhÜnctes-.. «2... uctor LRL F
A ee ee So TH ST 14-17
SAS) AAA e E c Ne in
Castillo and ¿Aguilera (1895)... e rr esq 16,17

cautisnigrae Zone

Central Tethyan Province
CENA DEIS oy isa oc see ON eet erunt tle y

Gellia, Sethocapsa roie

Chitinoidella Doben, 1963 ...

1277777 117 LAME ripe SERRE recta

troum- Pacto M A O E ESTIS
BOLETO Ae AI VICI QUI rere rores idee tee P1. des 5,9,10,13,27
CONCENTRA BUCAL peri e 13,14,33,F
Conocaryomma Lipman, 1969 ....

Cookson and Eisenack (1960) es oes E4283
Cope (198 copus O PERI S pir tree
Cordillera REPON ecce verre tr hee e EIU Te CH ths e etn
Corongoceras Spath, 1925 ..
Corpoteal.Daxa..«.... ene

Cossmann (1907) ........... wh wh ie
iro TA SC Puck
UI CU eco Lee O PESO
crassicauda (cf.), Lamellaptychus ............ b
Crassicollaniasdmemante; 1962 - aer a AA F
Grassicol arig, Zone: Gb Remata- ioi esie AAA. 7
ia A A AN er pe en 20
gio o 00 Rel NA viens feet Oe 20
CUCHACTSG AAA A Turon 9,12,14,25
GUESI QOIS E SW ces eeei ei deae evertere EE de SARA ea D5
EYMOAOCE LONE. entonar pee portas bos ES Eee ba tars TOUR 8,14,16-18,F
GOV WHIZ UB dr oirlo IRE PCR e TA T PAN. EORR E
IDEO UU OO) A E 16
o A ess veveivo A A 13,18,30,31
Dichotomosphinctes Buckman; 1926... 4: ee csi PEA. UTR F
AE A A O RETREAT A F
PUCAMOIIES LA nt de cc FALSE O F
Dickinson and Vistass (106) cisterna too rre TRIS ee 18
dicrahicUnthos, ACGTHNOCITCUS™. opone uo dao ii 10,20,21,F
Dicivomira Ziel Al Beo eoitecive cousedtedt ede eve ito EOS 28
boesii Parona, 1890 28
dictyotum, Scriniocassis 16
Dinoflagellates
VS DUDS ds 16,18
AA lege O cos, ARIS 16,18
Prolixosphaeridium
E Por voee sedis Mani sse Po Toe MERE eH PATA E
SOMO COI ERNETEN EEI IOE EVIE NT ITR TRENT UTR
dictyotum .......
Sirmiodinium
E ANN N

IS SECINIQTOD HONG IEE AEA EASE A E E E ETA 16
SIIA EENAA A A A A EN E re te 16
CAPO MC A REEE ETEA TN VOTE TT AAA AN 16
Discosphinctes Wacques, D914 eiris e RO E
COLD DECS: AWOLS Kyl O2 9 arenas tee vaca aie E
IVA A eH miae ASIE E F
CIVISUTIE LOMO eS S EE ETAS eae ae AO 8114515, IE
Diada ett UPPER HM 7S 19
Woben C96 Iiri :
Downie and Sarjeant (1964 fas
A o A stored ches hereon
IDEOCCANIIO OS eee EET ante meses es

DSDP [Deep Sea Drilling Project] ........
UD vienh navel 60995) 1 cot edet cU eerte

JouraugueseBurekhardt-1912/ caeco tome Ie
JOTT TIO GS OTIO A eerie iir E PI ERO Ma En

castas Fe UE E A RESET NEUE
Ehtemocrg 0898). O atom PAS YS Sn SR
Enten bena SAA cies re EIS IMEHIBLU eL I
BEhrenpenp (84 ans roe iit ID LO nU En
Binenbenp 37 Meana MISI IM eer
MAA SIA e essct tense IA eee er sy Aes e
elegans ones umi nce domo T S
eihpncaealpionellagpsee ee dide RS EM
Binihivia Hone mating! 9) Seis deno eet but

hOPSORTAPESS IMAN A taie RS
EMmpson Mora (19 81) 1 T esce ete aeter e
ELIANA ta eer tee TO
Endara (OT E receta m codes onde EDS
Enay and Geyssant (1975) 83.0 rr oe eet po
EDI Bes A sec rete riso i pe eons EA Tr n mir DIE
TINA AN O ooo a EE A

DYeUoularaaenmenoslo00.. v cero ttv ees RES
EPA O S TER etsy aa eat EER NE
Buasmaoceras Spat LISI ipsis oe Re tu RTT
Eucpriiduim Ehrenberg, 1847. 2 ire S

ptyctum Riedel and Sanfilippo, 1974 ............. Aah © LS,

Eucyrtidium (?) ptyctum Riedel and Sanfilippo, 1974 ............ 30
VIC IS ASA Eee E TRIES 14,16-18,F
Pige mio E Orman E neem Terr se 13,33
ERODI rtr M MER 7,8,14,16-18,20,29
European eilhyaniRealmon mo 1 TEE Y Pret rere 8,F
European Ammonite Zonation
European Boreal Realm 45 pem e
Butopeanuleuiys odere rere em tee E 8,14,F
OU DTUSEZONOR ERA PD cu Ire LG NEN EN ERR RS 7,8
CXCPIS ORB AEVICU SUI e eee oor. a SI 5,9,13,27

ATEOS LIE E EEEE E RA E PETS P
SUSCICULISC mS VSICINALOPNOTA oren i DA TE A E ae 16
OO a A LM ME
fialar, Glochiceras ........
fialar (cf.), Glochiceras ....
Fischer (1830-1837) ..... T Ba iv
JISCHETICTGABUGI ICR MOURN AROS EDU E Y ETC UM
JIeX AUT Eee DEPO aN eee DT eect sae
Foraminifera
Le LICULIN GMA AAA MUIR AN 16

QUOnstcat ss d OANA Dare cM TES 16

SCMICGUICLG eset OR d pr, OR ao ME 100 16

UNICA ert SR Ente RARE REPRE 16

JURASSIC RADIOLARIAN ZONATION: PESSAGNO ET AL. 47

Foreman (1975)
Foreman (1978) ..
Fourteenth Bitopean Mictopalegetolagical Colloquium ........ 16
FADOT ANDER das sese tont une tados Rete eee easy 16
Purani ELO) e eR aa dena era

(G3bbraliS60)mis mesita. T
(SENS aa E O itin DEREN ee
EN O mes
Gitmez and Sarjeant (1972)
ello reo] IRA AO SEA EET
Goes ceras bly att LIOU eee ier re RTT 19, 143127533; E
falar Opp RSs aa e contro ul. 10 nomeo x 14,17,F
sp. cf. G. fialar (Oppel 1862-1863)
Glochiceras halar Assemblage iyis pee EA cen AEE
Glochiceras falar ZONE mrissserrsespire eet tO OU
(OO TOL pet MALA MET etm
GLanalaptychusczbrautb L921- asat SA MON cee. ESNS,
panulat Quenstodi LEIS) arden a se cence e A
Gravesta(Salleld AQ US) ronca des EN N
Gravesia/hybonotum Zone ..
(RANES AON Cae Mk. o rai

[coule qut MM Rm ene ieee amt re ence soca 24-26,30
SL OSST S TINO UVA ral pa bae esas ARMAR TOS 16,18
guadalupensis, Mirifusus ..... DT 9:10712516:20:21525:26;325 E
(uembel A ORE 15-17
Guembel (1862) 16
(UC OMM e LH EEUU T US E 18
Haeckel (1881) 22
TAC CKCIE CESS E Nec eere ene REIS RHEIN 21
Hághimas Mountains

ARONA s e eet CS

TAU MINAC pe S e eee Eee DSTI E

WEE Trine (ISG) ks S a eens roan Rx eren ere EE IN

Hera nioceras Spathi 1923 ee EPIS
¡STD te ESO) ve s et tme ot data qee cos ede

Higumastra Baumgartner, 1980a

En a td e ea EE

Hopson (1983 Oral COMMU) sec ee UI ere cet:
Hopson, Mattinson, and Pessagno (1981) ............. 6,10,12;31,32

hopsoni, Emiluvia
hopsoni, Vallupus
hsui, Parvicingula

STARS O RE S EST
Hsuum Pessagno, 1977a ............. 5,9,10,12,14,16,24,25,30,31,F
GUEsTaense Rossa LA acaecida des | 9,12,14,25
Cuesta ens is tRESS ANO ID Dion esee pere ond eb s ARR USE 25
MEICUENIA MAS Pie SEHE eee E eere ctra d 52:38 5,9,10,25
maxwelli Pessagno, 1977a ................. li 9:10512:16;255E
Stanieyense;Pessagnojd9 778: e bone d sees 9:12,319B
Hsuum (2) stanleyense Pessagno;.19 7/78: € icc ARI 3l
hudenn ZONE «Gee s cose b E A E F
Hybonoticeras Breistronen 194-7 ranas cas alone dao a 7,F
iy DONOLUITE (Oppel O atacantes GEAN a EN 7
AHyDOnOtumisHybonolcerass eese eerte ERREUR UI E NEU 7
WybonOtumeZolexso seta pee crate teres ROW Ome aes a es 8,15
SAN A O. 15;F

ICZN [International Code of Zoological
Nomenclature (1964)]

Idoceras Burckhardt, 1906 .... as
GE DATO ORTA Operi R e Cen TOR HIR S PED sos
sprehlainfatum Burckhardt, 1906... «eres tereese e entem 17

span mutabilis Burckhardt, T912 orines: tia G Ly

ex. gr. I. neohispanicum Burckhardt, 1912 ...
Idoceras Beds .... 2 5417:33
Idoceras Zone .... e accitis AELS
Mir enya UO AAA) dut cu E scope scusa eo ERREUR f:
Imlay (1955)
Imlay (1968)
Imlay (1973)
Imlay (1980)

Es OO aaien e a E 14
tolay amd Jonesia) ieai UPS IURE tesis
imlayi, Archaeospongoprunum Rr
immodica, Praeconocaryomma ............. E iis DET 9,12,24
Indonesian a t. io idt 20
TELA C1) LG OG EROS e AAA A < SO eee 17
Intesa ODE. e a e AA 8-10,12
ISSC [International Subcommission on Siestincunbsie
Glassiication| LO O) adan tcl dates eee eek eee eS 6

ISSC [International Subcommission on Stratigraphic
Classification] (1971)
lupi sag eel a sade EM MEM MEE LOS LT

Tapane eese verse ces six MERI I E NU IAE
AS Pers DCG mue ee e eo scu etieni e utc br acc RENS
Jekelius (1920-1921) 3
TAMOS solis

TOMES AIDA e AT i
Tone oral COnN) eienaar EIE EORUM
Jones, Bailey, and Imlay (1969) ..................,

Jones, Silberling, and Hillhouse (1977)
HOMES CAI ICI OUNCES. eerie iecur sabes 5

[DENISE OD SR eae an AA ica code ANIME es
A ESA A CE RE e ROO BEBE Mods
Kimmeridgian

Klement (1960)
Kossmatia Uhlig, 1907
Kossmatia-Durangites Assemblage

Kuznetsoya and Siebold IE) iasanen E 16,18
a Caja Forna gi nsn a aire m MET ee 17
A EI DEL. A aia A ee diod 17
'uevaparchus lira ta 111997 1.35 oa eres cett rid ue NR 16,17
Tatussseriponus Trauth ThT s 3.41. esce aces Jd. coe 17
latus vermiporus Trauth, 1931 17
mexicanus (Castillo and Aguillera, 1895) ...................... 16
VoM pa S in ANNU, IZT nere sea eti 15-17
sp. cf. L. crassicauda (Quenstedt, 1846-1849) ................... 17
lamelami Paninson Lo d DS essei onto eerie eie tt e 15
grupatBsJamellosus.(Parkinson, 18145. 5555 iine T oii 16
mucrocostatus Trauth, 1938 17
pleiadensis Trauth, 1938 .......... 17
rectecostatus (Peters, 1854) 15
aff. grupa A, rectecostatus (Peters, 1854c m noranta 16
sparsilamellosus (Guembel, 1861) sü
grupa B, sparsilamellosus (Guembel, 1861) ....................... 16
Specie whore Opel $1863)... IS coepta ec e i
Lamellaptychus (?) lithographicus (Oppel, 1863) ................... 7
INCURRA ds 15
lamellosusíempa B), Lamellaptychusi $5. O a 16
Tarusiseriponus Tuevapiychuse a. dt wc A daas 17
MAGUS VENIND OTUS LAEV RUS aeneo S o AS IM 17
Tennent Bartels E809... ped att dt: ea 16
guenstedi(Guembsl;. 1962) exanime ne cet dos 16

48 BULLETIN 320

Lenticulina
senmexnicia(Schiwagets 1865)59 3 5098. Au Peete sa os 16
TIGA CW ASHAO WS aly OI OY AAA REI De TI 16
a E SOPRA RE O 18
a OO) A A A NC AS 23
Vray YA cebu Abe 17
A O a o A E o RRE 7
LX novampePhhrenberg; LBBB. A tye 26,28,30
atn Earenberz 1844550. 14 1 aou euenire det as lad 30
QUSS OD) rriena eno ITA AES, PORE LULA 8H 28
acia geo RIS ty US PRE A A AN 26
VIDT CD LID ARA OMBRE E ae 15
WobraphicusQ2)yLamellaptychus: ri ATEAN esa y
Lorenz (1902) 7
EIN DOE ARA A e 249Yan 19,24
IOV MEV ENSIS MOTDICULIONING. sese vene root etre eroe eene d 5 ss 9,22
annae Gode. QUE a Rad 18
d) LOGEUAI UCSB RL OOO AS DA E 10,32
Metaishlitand. Pessagno-(1978)......... EE 2 IR ERRAR 15,39
BIN CES narices lisa 5,9,10:25
MeWwiliams and ETovclb(1982)5. eee teeeeeeee pe ene nemmeno 20
BORD DU LOGIN RE Lo Latest E EE ENT EEE ES
E MMU Nel ie QUAERE UR A arin A E e 6
magnimamma, Praeconocaryommtia........ e, ee duele ee ee eve eT epe rea 24
a AE eed er eere ree en Fire a rad $5 9,10,12,16,25,F
MurapilitessBurekkbaucdiy DOR... ieu erdceseeeene rrt warts 19,F
WIFE LOS Ce. TOR LL RR HENNING EL M ES 710,1333;
mediodilatata,
SUT OO CRIN: art bette M RAI A RIAL aT 26
TET E o ERTE ub E T 2o 10,16,19,26
PCI uel) o yo ty2 LÀ ENAA nara can T 26
Ao A A hte 5-7,13,19
A M ET 20
POETE ORNS AAC VIP oso... see careo rente REOR TS 16,17
Joke «toro To ae cepa Ms CET LR 5,7,9,10,12-14,16-20,22-27,31,33,F
a A A E A 33
penal EE se 6,9,10,12-14,17-20,22-27,31,33
a e A A a do DT 5541912 ONE
Ot le a AAA OO RU Ad CARERE 17
TRAV N a oe iraan n ob MORENO TORE 33
Lonne MICO AAs oro creer a e RC. 7
northern

Nuevo Laredo—Mexico (D. F.) Highway
Rio Moctezuma
San Luis Potosi ....

RISE GSPN Al E EAS ERIS 8,16,17
aa e o BI a ae tuU E
A A IRAN OI 13,14,33,F
Tamam Tamazinchale diea" a. TRES LIBERIS AE, En 7,33
Tamaulipas

ra A vce O A AA O

Microacanthoceras Spath, 1925
ADI OO TOUETRS Zoe PE B uei LLL ER bes do ROS US F
Mirifusus Pessagno, 1977a 9,10,12-14,16,
17,19-21,25,26,31-33,F
baileyi Pessagno, 19778... he 2 43091 9,10,12,19,26,32,F
guadalupensis Pessagno, 1977a ................sss. DRNA 9710,12,
3 16,20,21,25,26,32,F
mediodilatato Rust; 1885) aa: D RON 10,16,19,26
Mirifusus (?) mediodilatata (Rüst, 1885) ................ssssuueuuss 26
NESS UAC) IL QU Er rec lau edo Re PURSE ROC AEN A 10,F
Mirifusus guadalupensis LONE ries oo tidi deo RESI ANNO LE

mixtispinosum, Prolixosphaeridium ................. sss 16,18

MUZE SES acta
IMO OTE (her c sect MT UE

morroensis, Obesacapsula ...
THOSQUCHSIS DACIA Eee
mucrocostatus, Lamellaptychus ...
muhlbachi, Dichotomosphinctes

DRA ESAS ALI AAA AAA na e EN UE
HUIDA
Naponi PETIN I dieque Os UNUS 19,24
Dua essaeio 97a ecc esses titer RE E 24
JOSDeXistssBessagno, LIT] Enersen dette nike 2I eres 19,24
lospensis Pessagno of Baumgartner, DeWever, and
dd OBO) A A ates a RH S ert dens 116)
Nassellarinancertaciócdis a. oron IA ME canoe 30
Mesrelteerdsspjaneldze T922 urna queres st em EROS Raa 8
ING GCOMMAT tres ales E. NES 15
neohispanicunmiers ely LdOCeraS ios oe dansa soon a. S 15
TNeu dy USE oec recreo rene CIMA EL 115)
Meyan OLGEN «2o coeer cer eeec eres sor eu ee ep tae DE mites 6
Ie well GIO 6) atra o oen MAR POE E S 6
NORAC IKA ersi or o cu dep PE 5-8,13,16,17,19,20,F
EO UE PALA E E A de 19,F
Cordilorn Room as coa ORE ORONO s 19,F
Northern reana PrO VINOS sener vtec. eere E tede 19,20
INGEUMWES Te ME INO DCm oreore eoe anrr Deesa YR EN 7,8,14,17,18
Northwestern Europe Boreal Realm .................. eerte F
Obgsacapsula Pessasno, LO d e ETE 9,12,18,19,29,30
morroensis Pessagno LO!) d TERES AER 9,12,29
rotunda (nds O as ets seat se 4 dt 18,19,29,30
spa O. Jonmnda Tunde, 902) E dy aon 18,30
oblonga,
CUPONES SA lobos MAEMO
NARROS CU aa M
OGGILA Ca ZONE er s

Ochetoceras Haug, 1885
canaliculatum (Buch, 1832) m A bc
OhfifestiandeZ6e155:(1980)69. 5 2o voe A ERES DOE
GRENSISHSP Alls) LUCA ems UTR Ee
OURENSE Ica VERE DO DEC S TORO ML ret
(oralio ias RERO SUN, E
(9 rorum Tavera (980) nda e RERO LES
nidi eA b Demo Ete T eM
DEINE A nooo RARO.
OPPsUGISGZSLS OS) ie He a SOL RET.
ODES OS) ue da dE AS ETERNI
OP Pel USGS) soreness en RR ERE TERRAE
OP PEC Neate 5 cisci risit resto TUNE Re
ODDEOSSUS OT E e E A healt
Orbiculiforma Pessagno, 1973
lowreyensis Pessagno, 1977a
GUGONGIGABESSALIIO NOT Ses estu s cote riae re REED ROS
d'Orbigny (1844)
d'Orbigny (1849)
ordinaria (?), Trilonche E s
ordinarium, HE CHISDVIVQVUT S en eran ae ero E dS 9,12,24
GUIPDOLD SOM Ui E esses Uds Cas 6,12,18,20,28,30,31,33
east-central .. 12,18,20,28,30,31,33
[28 Ed n ees
John Day Inlier
Otter Point Complex
AWE SUC TIU de Dod cove eve dae e Ete RA RERO S
OO ATS DEI. ranas ede ec E ES

JURASSIC RADIOLARIAN ZONATION: PESSAGNO ET AL. 49

Pacific RIM GOMIS cs E add ee 20,25
naseS a OU D NEC RENE as AR A At sens 9,10,30
¡DANOS LON trios eco UR TUN OP SR CNET F
PONNU LONE 6s eoe RR ERR BERE TT TOO TE F
Pantanellium Pessagno, 1977a 22123
Parkinson (LS) ree RE 15,16
Parodontoceras Spath, 1923 S3ISSE.
Parona (WO) ir e PEN MOETS 5,19,28,29
Parvicingula Pessagno, 1977a ..... 5,9,10,12,13,18-20,25-29,31,F
LOW PESSARTION LOU decetero DA 9,10,13,26
POCA PALOS O) a A cee cone sete 19
EMANAN tae DST 5,9,10,13,27
elegans Pessagno-and Whalen, O ii 27
IAN EE AS S OUT Sea 7.
Sti (PESSACHO; UO aM to NEN URS NT EC
YO RES IAS SANO aaa
procera (Pessagno, 1977a) ...............
santabarbaraensis Pessagno, 1977a ...
vera Pessagno and Whalen, 1982 ................... sess
Parvicingula (?)
MPSS TAS A A AAA A A e de Reim 28
cretacea Baumgartner, 1980b 20
POCTA (MESS ARO UI A e e QU ees 29
AAA AN ue Lc LS LU LUC LAN ONE 15
RAOR O KOTA O 8,10,13,32
NAIL NS RN AN E Puma HUP A F
CH ANG Verntaci cru ZONG noe DI S F
Perispyridium Dumitrica, 1978 ir TENEO 9,10,12,18,24,F
ordinarium Pessagno, 1977a aeea LEER 9,12,24
NA A sider eut mp glow Na UA O 10
tamanense Pessagno and Blome, 1982 ................... Ec 24
POSSABHO BOT) re ert aereo OR De day dE ORELL 22,
BOSSagio/ E s ossavine Deseos A EN R 21:22
SSA Eno 970)! (eoe e C NO SU LEER. 6.23
Pessagno (19772) ... 5,6,9,10,12-14,16-33
Pessagno (1977b) ... ... 5,6,9,10,12,13,18,19,24,26,28-30,32
Bosa oO OO o nan aa a MEC e 21
Possagno and Blome (1980). eee cae scce said ce 6,18,21,23,24
Pessagno and Blome (1982). 5 NU cewek ine 6,9,10,24,30
Ressagno and Blome Gn prop) eee ore RE 6,10,18,20
Possagno- and Longoria UN PrOD.) eater s 18
Bessagnorand NONDO UI iinn N ENG 5
Pessano and POISSOm GEO aa 9,12,18,24
Pessagno and Whalen (1982) .................... 6,18-21,24-28,31,33
Pessagno, Blome, Whalen, and Cheng (in prep.) ........... 12,18,24
RETETE I ES E las ec macte iS 15,16
o estere cer ION NE oy ace NOE 6,10,19,33,F
piochii, Buchia .......... 7,8,10,13,19,21,31,33,F
PaA ZONE eiit CERA eii t actin t tutes F
Dianulati, Granulaptycltus Nanas... oM deerme eases ate eran ky
DIatynotaXoby SUINETIC. e ERA. He: SE eT eel F
AMARILIS AS ce Bat COE OPEN 8,15,F
Bigiadensis Lamelaptvohts cenere eE NE 17
DUCATIOIGCSDICNOLOMOSDHINGIES Wen attacks S F
HAUGH SDAGHT AM i auccer ca al amen 23,24
ponti Zone F
Portlandian 8
Praeconocaryomma Pessano; 1976... c ue tees ce eren 9,12,23,24
immodica Pessagno and Poisson, 1981 ........... Ticks 9,12,24
magmmamma (RUST 188I) casacas ASUS EEN 24

universa Pessagno, 1976
Primary Marker Taxa

DEUDAS LOS SR RIOR ci A

procera (?),

a Soe Seem 29
Je MONET ete ER CUTE dl 9,10,12,13,20,28,29
IDIotlgense SUDAN I ELE inte cenar aria donc REOR REO 14,33
Brolxophaendium Davey- 19606 ceu 16,18
mixtispinosum Klement, 1960

"romper Burckhardt, 1919 ceins

INAT ANIA LESNE E E ES

'ESCUAOUSSOcenas S Path 1923 cs aa RES ORNA Res

IDE um EMO PHAR aces

iyu Bua NUS e cA Lco ERE EAR

PusrtosRuoos ee Li eel AREA ENDE wees

Punctaptychus Trauth, 1927
DVN GTA USAMOS C oon Sear imam

DNMGLALUSERUNGLADUVCNUS S cs iss eec ace Wok. GERI RTL ep

J NON LONE Wie eus c vases ble a IR One Ea

ALOU ACNL SIA T Anand 212.
QUESO route quic e ee eer E EE EAE IS 6
Quenstedt (1846-1849)
USM Stet (USO) in diced) I7
quenstedti, Lenticulina

Tactolapitescs E A T E e
Rarău Mountains .................
Rasenia:Salteld, 913... su
rectecostatus, Lamellaptychus
rectecostatus (grupa A, aff), Lamellaptychus ..................... 16
REDUNDE (CS. GO fae pad ota 7,103F
¡REM (978) ce da oU OE IURIS VE
ienza(lD Y) ced. odds QU dtr est Acer del e dente dtd: 16,17
DEodOU A SSMO E oh ee eR eB 16
Riüsdbl (67g O dale ence ped Way a m ear 22
aaa: o dba DOR COMMA 21,22
Riedel and Sanfilippo (1974) ....................... 6,9,12,13,20,26,30
Riley, andasareant (5972) cce inssucod ctas eteat ned 16
Ristola Pessagno and Whalen, 1982 ....... 9,10,12,13,19,20,28,29
altissima (Rüst, 1885) ................... Sadar 9,10,12,13,20,28,F
hoest Panona S90), eoe teessaccens ON 19,28,29
Sp. allt boasi (Parona 1890). scios eee ded 29
spici R. poesii (Parona, 1.890) na See eee 29
cretacea Baumgartner, 1980b Tema MN re TEE LT 20
Asu (Possagno 1977a)y8998 1. ono. darse 9,10,29
procera (Pessagno, 1977a) ............ 9,10,12,13,20,28,29
Ristola altissima Zone
NOEMI IO) ue lan M etus coto tene
NE UO E cd cti d A OM E E
sia CSUR ARE diz
ANA ONE NADIE A eee nae 15
Cape Verde Basin 14-17,28,30
A O cm ee MEI
(A A Pasce cda
Dogger Sands tonta ataca iaa p ad See
IP reciia alitna A A A REL el
Friburg Alps

Hághimas Mountains
HABAS NSDDOS as SAR AS
Lacu Rosu area .....
Moldova Valley ...
Pecistea

rotunda,
OG CLARE CES AAN ARA dee ert e 4 T 18,19,29,30
E a A ER O RENE 29
A A Ah 18
rotunda (E), Obesacapsulu...... 2029 SCIRE deum 18,30
HOVIMA CP SLICROCAD SARs enero O ts IS Cl RUNE 29
ONIL dai AG EARLE Lore secre: TOS 16,F
TROUT CES We O A MEE 8
TODOS aia lo A atte Cons esee a 13,14,33,F
Riist (1885) E 5,9,10,12,13,16,19,20,24,26,28
«POUSSER A deca onde Vvceor a BEDAE NN pe MEE Soe ti 5
DONOWHOPessapnos: 197 78-. isis eer in bee S98 9,10,30
pagei Pessagno, 1977a sin EF 4 UN 9,10,30
CHAM CLO Ayre eer E A not eve ecu pavo ERREUR RN QR y
Saa A ae 6n eee rca Certa tp eee tare cto emt eer ae ere 29.26:29
ES 300909 Loud vu verte etes ra O 25,26,29
SOMMAVATVANACHSIS, POTVICIN QUID o iari Pracatove + Sao 9,26,28
BAMA do do ron O O tuscan ier UTR 6
ea DONOR A CNN TOUS e A TE 16
Bola I GRO OUD) Es, esse Fora Veg 1a O RUM Hee He TEUER 16
DOS NECIOS ri ria vir Les FORT een 18
SES A MONO a aes F
DCMMEICUSOIS GOCE TOGAS IA ereere eo Fee EUN nate 16
dictyotum (Cookson and Eisenack, 1960) .................... sss. 16
SOPHPOSUSPZOTIG A BTN tds ood bbe Te Vora haa AUR aoe F
DOW WO DICE IDC CUINA vr rincon traera voe e Ru ORE Iu ORE 16
si E AA doeet eoo KV S Monee 20
CENA EMI Od iria 20
A e sis ON aOR 30
A ds AAA A ret el 16,18
AN A S E 16,18
o A A uU Tro 18,33
SHOW SOS POLEIA ODE 20s sors eee eru entere reto ro PIS 18,28,33
SUUS FOE MONDE oorr O ee EEUU LAUR OS 38
NATU SPEDESAMEIDDGE. AAA A Pod e VES 18

Southern Boreal Province ....
Southern Europe
Southern Tethys
Sowerby (1827)

Sowerbyceras Parona and Bonarelli, 1895 ....

tortisulcatus (d'Orbigny, 1849) ................ i
Spussuamellosus; Bamellaptychus VERA. a REUS
sparsilamellosus (grupa B), Lamellaptychus
A dorados patuere od
A DE
SHE 0192 ON OR 1.2 2 assduvovwvov ne O NOMA ES E e QUA
SUIWOCras A hie; 1908. Qu. arare oet oer retro ente EPI eS 7,8,13,F

a AS RA A A RINT O ee A 7
Spinceras (Negreliceras) Djaneélidze, 1922 casinos AI TAS
SPONBOCUP SULA a A Ronnie 29
Suiasob (LOLA A A RIVA 10,16,20,21
A PIDIN A 4 He: 9,12,14,31
SUN VENISON gli SUTIN be A Oe 91
Stanley Mountain remmnant.....« rece ciendo de 5,9,10,23,25-29
SUSI EO UD A A metre rites eate S ERR E SURO SET UP s
a E A d PE ur ee A T 5
Stichocapsa Fae cekel SO esee esi PUTA IR 29

VOLO ENIAC US OD) O O A tele 29
Sachocapsa(Dirotinda (inde, 1902) ic... Siva RA AH 29
DELO RICS Ey A A O I5

tenmlobatus(Oppel; 1862-1863)... aues ciet Hr RA 15
SUDO SBOIERWIOS sarao erre vei EET PERI 14

BULLETIN 320

SUGCNCUIN AV TIA Spat 1924- ovi vsse i every ENTRE 14,33

DUO TOU ZENS (Burckhardt L906) ire OPERE REND 14,33
STUPIGnies SDA LOLS s ceo piven coitu metrice NON ERN. F
AAKRE DANIO D ee. E A E eee OR 13,F
Substeuroceras-Berriasella Complex mier ikana eese 7,8
Substeuroceras-Proniceras Assemblage ................ssssssss 7,8,F
IS DTE AR a PAIDOS Loc ode opc 7

HANA A de da Ji
Subzome 2A 01. BeSSdello E et eee denn Xe: vov en 12,14
S'ubzohe MRE amO nicas qe CORTO ahaa EA 12
SUBZONE ARO MBE SAPNO cinirdsnucacscndicuan vaso i r NA 22,28,32
SUDZODIoBIODIBeSSde OR N 52. nuca e cec Cradle de o 29,30,32
Subzonee G'ofsbossdgnoN oer dotes ME 24,25,29,32
Suppl mentir Aike arica dua mee 8-10,12
MATA A a E

CORSA ROMEO ieren garters a A E
ISDPIHESOGQDSQUNCVLABISelo 00295. ean ee a E 18

roroa on IO a E SR 18
AA NOTE: Klement LIGO A n 16

AMM LR LIGO nrerin 2 XO en RE e 16

TURCOS D E E E E renin 16
Taman Formation ........ 6,7,10,14,17,19-21,23-25,27,28,31,33,F

lower more massively-bedded unit ................. 10,14,17,24,33

upper thin-bedded limestone unit ............... 10,14,23,27,28,33
VOTO A LES AE A AA ds BEAR 24
Taorameliceras el Ganipan DA ancora odon Ai ayes 115)
CANVAS ISAAC, 31 AE AA AE 9 A S 7
MELT OD AS DURAS s cnt Up AAA NUM T. Me ACIDS. 15
TOVA ln ede CIE Lee ruere nes 8,19,22,24-26,28,30,31,F
TO Dd EL e e ZONE
thoro (cf.), Lamellaptychus 17
Tintinnopsella Colom, 1948 M suede

(ojo aa peti XC svolto Yd HO) Piers ric dese sequi e Ml alc Ro atum, ain J
IO ADEL qm EEE E A ETE mcd MEE 6,19,20,28,29
O ITE OA tee 6-8,10,13-33,F

Tmetoceras Buckman, 1892
scissum (Benecke, 1865)

AA ERIEN NET MT t haat es EOS AT ET
Forgan pinete SPAIN 5 e na aa NOE F
TON UOA S O WerOY Ceras E Ee O NN A 15
SAS PA AD ID o er sets A
A A 2:0) RARE OE Ie PERLES NRI Se Soa dios a
O BRE OE Uit el E cena def 16,17
ia de os TRE 24
irilonche-@))ordinaria Pessagnoy 10774 Pae kerine T 24
WIDUCALOSA CAS EN d ten E
Trurdbs Bain canter, 98 Oaseaisricsiericsticdre te tt. ores 16
Thododaciylus- Baumgartner, 19808 cs ee ee nee 16
Tirant: pessaguo-andiBlopie:/1982: iria 9,10,30
Capsensis*Pessagnorand Blome nd 982: a. ees. ES 30
flexa Pessagno and Blome 1982 oi... 4:009 30

Turculet (1971)
turonica, Systematophora

UV ONAPLON C8 I Lore vet ite ec ER POO T5
Uhlig (1903)
Uhlig (1905)
Uhlig (1907)

WISE dL oH AAA NUR ARTI AIEO IAAT ERE 16
ulmense Zone 15
UIMENSISOIE A QR CET Wes ctonoveieomimercssts E ERAN 17
UITOUZDOLGABeSsagnopmdo 7/1 sero conan aia mes i e AN EM 24

USNM [U. S. National Museum] ...................... 22,23,25,27,28

JURASSIC RADIOLARIAN ZONATION: PESSAGNO ET AL. 51

UNCILOLGES BUGNA oe a E tenes 10,13,32
univera, Praeconocat VO MIA ie e A E A ete 23
Valanginian 4 SN NEUES 5,6,8,24,26,29,30,32
Kalupunan Ei sio CI DOT 5.9, 10,22,23, F

ODSONT DES Pao eC LES oan 5,9,10,22,23,F

Pacific Rim Complex
variabilis, Acanthocircus

VETA POIVICIN GUI Gece A RU OU os

Verma and Westermann (1973) 9 9 099999 99099 8,17
VET NEUS Z ODEA eR etc o cae Me te rem eee F
VanassaidesReeny2(s99)Re eee e OR E NUTS 3
MOLE ANAVOMEAU e UR TS 4o 20,30
V SatosphunctessUnlpaloloN c. ccc C T E

Virgatosphinctes mexicanus-Aulacomyella neogeae Zone .... 7,10,

virgulatiformis, Discosphinctes
iio

VOLADA: we wer c C MR cu e A
Viole (LSOU) e RE C T rene 17

Wiestetmianiny (O79) pc ees e UR leu dei c ee m
Westermann and Zeiss (1983, written commun.)
ACA ey AA A MM M i
Wiedmann (1973)
Wiedmann (1980)
wildflysch of Pecistea .... a
AM A iene erences eee
Wimbledon and Cope (1978)

WASTTOWS Kin US9O a E 16
A E el ee c S mL LN EI LM 19
Wrangel lante eso deese eie S DS 19

AEO Ye alae Sats cating me e IT
EONS OH OE) ete teen cer x mU i tau E
RASS UO BAN da e eere IA NU
Ziegler (1971) ae
zirkeli, Spiticeras
Zones

Zone 01 of Pessagno, Blome, Whalen, and

Chena Ca PLO’) irene hea ce M RIS 18
Zone 02 of Pessagno, Blome, Whalen, and
Chene (PLEDI c cec EE 24
Zono IDOLOS SAO ue cc cQ deu c LIE M 12
Zone 1 of Pessagno 5,6,9,11,12,18,20,24-26,28,30,31,F
Zone 2 of Pessagno ............ 5,6,9-14,16,20,24-26,28-31,33,F
Subzone 2A Ol RESSAQNO ses ert e eerie T EI 12,14
Subzone 2B'oRBessaghos v. ec ue ee 12
Zone 3*ofsBessagno s c s 5,6,9-12,16,19-21,24-26,28-33,F
Zone A ON POSSIEDO Heat ere ree 5-7,9-13,19-33,F
LAO DAMA esc ern 12,19,22,24-26,28-30,32,33
SUUDZON JA ON PESSANO war, E occ ane aes 22,28,32
Subzone 9B OF PESSANO ial ts a S 29:30:32
Subzone 5C of Pessagno 5
Zone IV of GISLOLOWSKI Ie. eee eek edet dodo 15,16
Zone V of Gasiorowski jS
Zone VI of Gasiorowski A 15
Zone VIL of GASIOLO WSK 6 eee deese RISE uU ee 15
Zone A [=Crassicollaria Zone of Remane] ................... TAGE
Zone BORM fs eec ee eem I eee eS F

Text-figure 3. — Ammonite zonation for northwestern Europe (Bo-
real Realm) [after Casey (1973), Cope (1978), Wimbledon and Cope
(1978) and Zeiss and Westermann (written commun., 1983)] and
central and southern Europe (Tethyan Realm) [after Enay and Geys-
sant (1975), Oloriz and Tavera (1981), Oloriz (1981), Zeiss (1977,
1979), Ohmert and Zeiss (1980), and Zeiss and Westermann (written
commun., 1983)].

Note that we define the base of the upper Tithonian by the first
occurrence of hyaline calpionellids [A = base of calpionellid Zone
A/Crassicollaria Zone of Remane (1969, 1978)]. Also note that the
correlation of Tithonian ammonite zones between Boreal north-
western Europe and Tethyan central and southern Europe is uncer-
tain (Zeiss and Westermann, written commun., 1983). In Boreal
northwestern Europe, we follow Imlay (1980, p. 34) in placing the
base of the upper Tithonian at the base of the albani Zone. However,
we realize that due to the absence of calpionellids in boreal strata
this assignment is only tentative. The use of radiolarian taxa that
make their first appearance at the base of calpionellid Zone A in the
European Tethys and that likewise occur in the European Boreal
Realm may help to resolve this problem.

In the northern Tethyan Realm of northeastern and east-central
Mexico it can be established that the base of calpionellid Zone A
occurs below the Kossmatia-Durangites Assemblage of Imlay (1980)
and includes all or part of the Mazapilites Zone of Cantu Chapa
(1971). At the village of Taman, San Luis Potosi, the lower part of
the upper thin-bedded portion of the Taman Formation (= lower
part of Pimienta Formation of Cantu Chapa) includes the Maza-
pilites Zone as well as Radiolaria assignable to the lower part of Zone
4. Elsewhere in this area Longoria records minute hyaline calpi-
onellids at the same horizon. These findings seem to be confirmed
by those of Imlay (1980, p. 34) in the Sierra Cruillas, Tamaulipas.
Imlay indicates that Bonet (1956) found calpionellids just below a
sequence containing the Kossmatia—Durangites Assemblage.

OXFORDIAN§ KIMMERIDGIAN TITHONIAN
UPPER

TEXT FIGURE 3

A
x
[e]
ql
E
O
|
fen
hJ
A,
A,
[oe]
hj
O
A
E
m
z
A
[ee]
hy
A,
A,

[A : FIRST OCCURENCE OF CALPIONELLIDS]

European Ámmonite Zonation

Eastern and Northern

Mexico Modified from

Northwestern Europe

Boreal Realm

oppressus

anguiformis

kerberus

okusensis

glaucolithus

albani

rotunda

pallasioides

pectinatus

hudlestoni

wheatleyensis

CORRELATION UNCERTAIN

1983)

(fide Westermann and Zeiss,

Tethyan Realm

Imlay, 1980
Cantu Chapa, 1971

Central

Southern

Durangites

Substeuroceras

- - Proniceras

Associated Ammonites
in California. Buchias
California, Alaska,

British Columbia
After Imlay [1980]

Substeueroceras
Proniceras
Spiticeras
Parodontoceras

Buchia aff.

B. okensis

Spiticeras
Parodontoceras

transitorius

scruposus

Microacanthoceras

Kossmatia

- - Durangites

*

Virgatosphinctes

Aul hinctoid

puschi

ponti

Torquatisphinctes

palmatus

admirandum

Subplanites

ciliata

fallauxi &
richteri

Pseudolissoceras (rare)

penicillatum &
rothpletzi

semiformis &
verraciferum

and Mazapilites

vimineus

triplicatus

darwini

scitulus

elegans

Gravesia

Gravesia/hybonotum

Hybonoticeras

autissiodorensis

beckeri

eudoxus

eudoxus

Glochiceras fialar,

mutabilis

acanthicum

Buchia mosquensis,

and Buchia concentrica

cymodoce

divisum

NE cf. L balderum

hypselocyclum

: Ataxioceras, Rasenia,

baylei

platynota

B and Sutneria cf. S. platynota

pseudocordata

planula

Discosphinctes carribeanus,

Ochetoceras canaliculatum,

cautisnigrae

bimammatum

Dichotomosphinctes

kerrense

plicatiloides

bifurcatus

and E id

Buchia piochii
Kossmatia

Buchia

mosquensis

and

Buchia

rugosa

Idoceras
and
Amoeboceras

[Amoebites]
Buchia

E " concentrica
Discosphinctes

virgulatiformis
and
Dichotomo -

sphinctes
muhlbachi

Radiolarian Zonation Radiolarian Events
Cordilleran Region

North America

Tethyan and Boreal
Realms

[See text-figure 1 herein]

!

Ristola altissima

ZONE 4 4

Eucyrtidium ptyctum

[Ristola altissima Zone] x dicranccantkus

A Vallupus hopsoni

| Perispyridum spp.

ZONE 3

Mirifusus baileyi Zone] Hsuum maxwelli

Mirifusus baileyi

|

Mirifusus guadalupensis

ZONE 2

[Mirifusus guadalupensis Zone] Mirifusus spp.

? ZONE 1 ?

Mirifusus Zone]

[Parvicingula -

[part]

NOT SUBDIVIDED

Radiolarian Zonation
Baumgartner et al.
[1980] Southern Europe
Atlantic

sane
"Biochronozone"

c

— 0

"Biochronozones"
A&B

2

Calpionellid Zones

After Remane [1978],
Correlation with ammonite
zones from Imlay [1980],
Bonet, 1956, etc.

ZONE B

Calpionella

ZONE A

Crassicolaria

NOT ZONED

NYIAHOJXO NYISCIYAWNWIS NVINOHLIL

e

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