Transactions and Proceedingsof thePalaeontological Society of Japan
New Series

No. 93

Palaeontological Society of Japan
April 20, 1974

Editor:Hiroshi UJIIE

Associate editors:

Ikuwo OBATA, Yasuji SAITO

Officers for 1973 - 1974
Honorary President:

Teiichi KOBAYASHI

President: Tatsuro MATSUMOTO
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Hiroshi UJIlE, Iku wo OBA TA, Yasuji SAITO

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Trans. Proc. Palaeont. Soc. Japan, N. S., No. 93, pp. 227-239, pis. 32. 33, April 20, 1974

627.

REPORT" OF LOW.ER TRIAS FROM PIR PANJAL,
NEAR QAZIGUND, KASHMIR, INDIA, WITH
DESCRIPTION OF A FEW AMMONOIDS;'HARI MOHAN KAPOOR
Geological Survey of India, Lucknow, India

and"YUJI BANDO
Department of Geology, Kagawa University, Takamatsu, Japan1 :/roo tJ -/ ~ -/I--~'I'I Qazigundfii!I:O) Pir Panjal J:1!!.!i.O)rgji=:''0:* : *'i'ivJ:t1E*",I.-J.* Zewan Series O)J:fflU:J!I/fJ(~~1.'"Ct':iI~, Claraia -'(o Ophiceras t,d:O)if!i:8',t:.J: I),~ t':"h -/ ~ - 11--0) Srinagar fii!IO) Guryul Ravine 1:: ge;~-t Q Ttfll=:':'&* c.1m~fliI~j;>1!~'"C~njJ.'J.-tQ;:b~pz:,rl'fIi=:'1i:*I::~-tQ;:cil~aJJz:,iI,ct.:-::>t,:o ;:0) Pir Panjal J:l!!.lKiI>z:,11€
I±l L. t,:~:f~I'l':Jt.: 7 :/-'C j-1 r c. L. '"C Lytophiceras aff. ptychodes DIENER, HYPophiceras?
sp., Glyptophiceras sp., Ophiceras sp. ~~l'.ilUl15- L. t':iI~, .:. ~1. z:, 0) 7 :/ -'C j- 1 r !liJJ¥On
t"ili'!lt.:"h -/ ~ -/1--0) Pastun S(> Spiti 0) Ophiceras JJJ!!1J)r.fc.;iHt~hQo
H. M. KAPOOR, ~*ttm

logical details. These discrepancies makeit difficult to correlate different strata
situated apart. Therefore, in the present
paper the authors have made an attempt
to review one of the areas of Pir Panjal, Kashmir, situated near Qazigund, on
the basis of latest data available fromtype sections.
TEICHERT, KUMMEL and KAPOOR (1970)
and NAKAZAWA and his collaborators(1970) in recent years carried out extensive study of the Guryul Ravine
section of Vihi Valley. They establishedthat advent of the Lower Trias in
Kashmir is marked by the appearanceof Claraia, and many of the Permianbrachiopods continued to survive in thelower part of the Lower Trias. The

Introduction
Kashmir has extensive developmentof Permian and Triassic formations.
Many of the geological sections, confinedto the Vihi and Traal valleys of Kashmir,
are famous in the annals of Himalayan
stratigraphy. A number of modifications,reviews and additions of data have also
been done from time to time on these
sections by geologists from India and abroad; but for other areas of Kashmir,
we still lack lithological and paleonto* Published with the permission of the
Director General, Geological Survey of India.
Received May 13, 1973: read June 23,
1973 at Niigata.

227

228

Hari Mohan KAPOOR and Yuji BANDO

Lower Triassic ammonoid fauna, how- /. et ai. (1970) considered the Pastun(=Pastannah) section as the type section
ever, made its first appearance whenof Lower Triassic beds in Kashmir. As
the typical Permian elements completely
the above papers revise the contact bevanished. The boundary between Permtween Permian and Lower Trias, theian and Triassic, considered by TEICHERT
et ai. (1970) and NAKAZAWA et ai. (1970),
position of the boundary is also likely
to change at Pastun. The revision ofis considerably lower than the boundary
Pastun has already been taken up byinferred by MIDDLEMISS (1910) and
KAPOOR, and he found that the boundaryW ADIA (1957); thus reducing the thickis actually quite below the one hitherto
ness of the Zewan Series and increasing
considered. The Pir Panjal area, which
the thickness of the Lower Triassic beds.
is far away from Vihi Valley, is comOut of the several known sections
pared with the above type section tofrom Vihi and Traal Valley, the Guryul
know the lateral extention and lithoRavine section, where maximum details
logical and faunal variations of thehave been worked out by NAKAZAWA
Zewan Series and the Lower Triassic
and his collaborators, is regarded as thetype for comparative study in this paper.
beds in Kashmir Himalaya, and also to
TEICHERT et ai. (1970) and NAKAZAWA
know the faunas at the Permo-Triassic

N

1'6 Km.
~-~I• Kontsul>< Kukilphiur Gali

9860
~

q

\..'

BUflotoP.
R.4

N

G

F:

,
H.M.Kapoor

Text-fig. 1. The sketch map of Pir Panjal, near Qazigund, Kashmir, showing theLower Gondwana, the Zewan Series and the Lower Trias. Inset: Key Map.

627.

Lower Trias from Pir Panjal, Kashmir

contact. This comparative study also
modifies the Zewan Series of Pir Panialof pioneer workers, as the upper partof it is included now into the Lower
Trias.
The area dealt with in the present
paper, lies north of the Pir Panial Range
between Upper Munda (33°32': 75°11'30//)in the east and 1 km west of Lamar(33°35'15//: 75°05') in the west (Textfig. 1). Several diagonal sloping ridges
emerge from the Pir Panial Range andfinally about on the flat terrain of the
Karewa (Pleistocene) formation. The
diagonal ridges are separated from eachother by the development of a small
valley formed due to water courses.
A number of short notes publishedbetween 1866 and 1928 by R. L YDEKKER,
C. S. MIDDLEMISS, H. S. BJON and D. N.
W ADIA of Geological Survey of India
give only an outline of the geology ofthis region of Pir Panial. HAZRA and
PRASAD (1963), however, reviewed andelaborated the earlier work and supplemented the geology of the region byadding more data observed by them. It
will not be out of the way to referhe~e the work on the western part of
the Pir Panial by W AUlA (1928, p. 251),
who reports the occurrence of Pseudomonotis d. aurita and Pseudomollotis
griesbachi in the upper part of the Zewan
Series. He thinks that the presence ofPseudomonotis indicates nearness of theTriassic horizon between which and the
Zewan Series of the type area there isa gradual and conformable passage.
This zone containing Pseudomonotis may
be the zone of 'Mixed fauna' (of TEICHERTet al., 1970) of the Lower Trias of the
Guryul Ravine and represents the lateralcontinuity of the Lower Triassic bedsof the Guryul Ravine in the Pir Panialarea, near Qazigund.

229

Geology
The geological sequence given in the
Table 1 is modification of HAZRA andPI~ASAD (1963) as observed by KAPOOR.
Text-fig. 1 is a geological map of Pir
Panial near Qazigund showing distribution of Lower Gondwana, Zewan Series
and Lower Trias; and Text-fig. 2 shows
geological section and column as seenin Upper Munda.
The Lower Permian to Jurassic formations, exposed on the northern ridges
emerging from Pir Panial Range, arepart of a broad overfold. The PanialTrap, the oldest formation in the area of
this report, forms high peaks. This is
succeeded by the Lower Gondwana beds.
A three-meter thick pebble bed above
the Panial Trap is characteristic in thisarea. It suggests probability of hiatus
and change before the sediments ofLower Gondwana were laid. The Zewan
Series, the second oldest formation is ofmarine nature. It is rich in bryozoan
and brachiopod fauna (Linoproductus,
Spinomarginifera,
Leptodus,Protoretepora, etc.) of Upper Permian age. The
complete succession of this formation is
not seen in any of the sections, all along
the strike of strata. It is due to a reversed fault running between the Lower
Gondwana and this formation; however,summing up all the sections the lithological succession can be established as
Limestone (=Basal limestone; rich incrinoids, corals, shells of brachiopods,etc.) succeeded by sandy shales with
abundance of brachiopods (equivalent toMarginifera himalayensis and Spirifer
rajah Zones). The Zewan Series areclosely folded; therefore it is difficult
to estimate the actual thickness of theformation (thickness given in the Textfig. 2 is the total this;kness of folded
sediments). The sandy shales pass into

Hari Mohan KAPOOR and Yuji BANDO

230

C
o ..

sw

°

10 ..

,

~
~

~~Q"
I ,f~
oq$.~

.

°

,..0" c;~.

,.,vt} ~~

c,

i'

~~/

~'
,
\

,
\

\

H.M. Kapoor
G.. S.I.CN.R.) D.O.No. 906.7-70-XI

Text-fig. 2. Geological Section and Column, near Upper Munda, Pir Panjal, near
Qazigund, Kashmir. Thicknesses of the Zewan Series and the Lower Trias are notactual but sum of the .folded strata.

flaggy shales.
The flaggy shale is the important rockunit. It marks the begining of theLower Trias •. This bed contain Ciaraia
spp. (C. concentrica Y ABE, C. stachei(BITTNER), ammonoids and also a number'of Permian brachiopods such as Linoproductus, Derbya etc;). . These shales inthis area are purple and very fragile.
They split along the bedding planes.
The original black colour is rarely seen.
The thickness given in the Text-fig. 2
is the total thickness of the folded sediments. These shales 'were included by'HAZRA and PRASAD (1963) in the Zewan
Series"imd appear to represent Bed No.
47 to 59 of the Guryul Ravine described'by NAKA'ZAWA et ai. (1970) and corre-

spond to the bivalve coquina zone or to·
the Ciaraia zone of TEICHERTet ai. (1970).
It is, however, difficult to say whetherthe upper part of the Lower Trias andthe Middle Trias were developed in thearea. as the flaggy shales are succeededby folded Upper Triassic limestones andcontact between them is inferred to be·a strike fault. In Kashmir, biostratigraphically, the upper part of the LowerTrias is characterised by limestone with
Meekoceras; while the Middle Trias by·shales and limestones with Ceratite andDaonella fauna. The Upper Triassic
limestones are mostly barren <of mega·fossils, but there are occassionallayers,.
10 to 20 cm. thick, rich in Spiriferina
stracheyi and Spiriferina haueri.

627.
Table 1.

Lower Trias from Pir Panjal, Kashmir

231

Showing stratigraphic sequence in Pir Panjal, Kashmir.
Lithology

Formation
Holocene
KarewaScree, moraines and alluvium
Clay, lignite, carbonaceous
shales, etc .

Jurassic

Limestones, sandstones, sandy
shales with bivalve fossils

Geological age
Holocene
Pleistocene.--- Unconformity-·
Lower Jurassic------------.. -.-? Unconformity---

Upper Triassic

Limestone with occassional
layers of Spiriferina spp.

Upper Trias------------------------------------------------------ -------------Fault---------------------Lower Triassic

Flaggy shales with thin limestonelayers. Layers of Claraia andammonoids in shales

Lower Trias(Lower Scythian)-----------------------------Conformity---------------------------------------Upper Permian
Limestones; argillaceous,
Zewan Series
calcareous and sandy shales with(? K ungurian-Tartarian)bryozoa, brachiopoda, etc .
.------.------------- ---------------------------------------------------------Reverse Fault----Sandstones, tuffs, pebble layers,
Lower Gondwana Seri,essometimes pinkish shales
overlying tuffs. Plant fossils
present in tuffs.
Panjal Trap--------------.- ? Unconformi ty----·---Mainly basic lava flows

In the crests of folded Upper Triassic
limestones, three bands of the Jurassic
sediments are present. The Jurassic
beds are rich in lamellibranch fauna,though a few brachiopods, ammonites(especially Perisphinctes) and fish remains are also known.
The Quaternary geology is of lesssignificance for the present work, hence
not dealt with here.
Permo-Triassic Boundary

The lithological and faunal comparisonof the Pir Panjal near Qazigund andthe Guryul Ravine has been indicatedin the above paragraphs_ The Zewan
Series marks the close of Permian in
Kashmir, but at both places it has been

Lower Permian(Upper Artinskian)Lower Permian

observed that Clamia which is developedin ftaggy shales marks the begining of
the Lower Trias. These Claraia-bearing
shales were included in the Zewan Series
by pioneer workers.
Recent contributions by TEICHERT et al. (1970) and
NAKAZAWA et al. (1970) in the Guryul
Rayine ha\'e already shown that theupper part of the Zewan Series is actually Lower Trias and there are many
Permian survivors in the lowermost
part of the Lower Trias. In thePir
Panjal area of Qazigund, though there
is a little variation in litho-units of the
Zewan Series with that of the Guryul
Ravine, almost complete faunal zones
are developed and likewise the boundary
between the Permian and Triassic beds
is between sandy shale and ftaggy shale.

232

Hari Mohan KAPOOR and YUj'i BANDOIn Pir Panial, only the lower part of theLower Trias is developed. The characteristic ammonoids of the Lowest
Scythian, i. e. Otoceras fauna, could not
be found in the Pir Panial. There is,however, possibility of finding Otocerasin the thin limestone layers in the fiaggy
shales.
Many of the Permian forms such as

Linoproductus, Spinomarginijera, Derbya,
Eumorphotis, Etheripecten are occasionally seen in the arenaceous limestonelayers in fiaggy shales. These are associated with Claraia stachei (BITTNER)
and are restricted only in the lower partof the fiaggy shales. The upper partof the shale abounds in Claraia concentrica Y ABE and ammonoids. Suchfaunal distribution is similar to that of
the Guryul Ravine. Ammonoids andpelecypods are usually in separate layers,
but layers containing both are not rare.
The fossils are collected from Upper
Munda (33°32': 75°11'30"), Malidar Gali
(33°33': 75°09') and Khowurwat Gali
(33°35': 75°06'), which show good andclear exposures. In other areas theseare either highly weathered or concealed
under scree.
Reference about the western part of
the Pir Panial has already been made in. the Introduction. W ADIA (1928, p. 251)
considers that the presence of Pseudomonotis spp. in the Zewan Series indicates nearness to the Lower Trias, but
the present authors feel that the beds
containing these are lowermost Lower
Trias and are equivalent to the fiaggy
shale horizon of eastern Pir Panial. The
presence of Pseudomonotis spp. in association with Permian forms indicatesa mixed Permo-Triassic fauna in thearea as is known in Guryul Ravine aswell as in the eastern part of the Pir
Panial. The contact between Permianand Trias in both parts of Pir Panial

is gradual and conformable.
It is really a matter of great interest
that a thick succession of the upper
part of Lower Trias and complete Middle
Trias is not known in these parts of the
Pir Panial. It is due to the strike fault
which caused elimination of thick strata
or due to non deposition of thesediments. The problem is open to the
future workers; but the present authors
support W ADIA'S (1928, p. 252) opinion
quoted below: "The Triassic development near Mandi and Trekana is restricted to only a small part of theUpper Trias, the whole of the Lower
Trias and Muschelkalk stages, which areso completely represented in the Vihi
hills, are totally absent. It is however,more probable that the resulting unconformity between these beds and thePermian is not of erosion, but may bereally due to non-deposition in thislocality, in that the Upper Trias hascome to occupy this position by a progressive overlap on all the lower division of the Trias. The Panial area
forms the southern limit of the marine
Triassic rocks of the Himalaya and hence
this thinning out of both the Permianand Trias is explicable as the natural
coastal boundary of marine calcareous
sediments at extreme limit of the geosynclinal zone of the central Himalaya."

Faunal Consideration

There is a large collection of ammonoids from the localities mentioned in
the above paragraphs. All of them comefrom fiaggy shale member. The preservation is very poor and fossils are friable. From the collection, a few were
sorted out and only four were recognized
and are described in detail by BANDO in
the next chapter. These are:

627. Lower Trias from Pir Panjal, Kashmir
Lytophiceras aff. ptychodes DIENER
Hypophiceras? (s. str.) sp.
Ophiceras (s. str.) sp.
Glyptophiceras? sp.
The forms listed above are characteristic of the Ophiceras fauna. These
are comparable with the fossils of the
Ophiceras fauna of Pastun (Pastannahin Traal Valley), Guryul Ravine andSpur 3km north of Barus (both in Vihi
Valley). The Ophiceras fauna from
Past un was described by DIENER (1897,
1915); who regarded the fauna to becomparable with the Ophiceras fauna ofGreenland. The fossils of other two
localities are still under study by NAKAZA w A and his collaborators.
Besides Kashmir, Ophiceras fauna isalso known from other parts of Indian
Himalayas, with which forms show similarity. Most famous are Spiti (HAYDEN,
1904, VON KRAFFT and DIENER, 1909)
and Painkhanda (Kumaon) (DIENER, 1912).
DIENER (1912, pp. 30-31) considers thatthe lowermost Eo-Trias of Painkhanda
seems to be similar to that of Spiti, in
both lithology and fauna. Also, the difference between Pir Panjal and these
localities seems to be very small.
Further east of Kumaon Himalaya
there are only a very few records of
Eo-Trias. FUCHS (1964, pp. 7-8) reports
Lower Triassic limestone in Dolpo regionof Nepal Himalaya with Meekoceras sp.,
Arpadites sp., Ophiceras sp., etc. In thesame region, FUCHS (1964, p. 7) has described Upper Permian beds of Barbung
Khala; upper part of which appears tocorrespond to Flaggy shale horizon
having the Mixed Permo-Triassic Fauna(Eo-Trias) of Kashmir. BORDET et ai.
(1967, pp. 888-889) have also reported
Lower and Middle Scythian sedimentsin Thakkhola region of Nepal Himalaya.
It is difficult, however, to compare themwith Kumaon, Spiti or Kashmir Himalaya

233

by the available data. The presence ofOphiceras, Meekoceras and. Clypeoceras
undoubtedly put them to Lower Trias.
The scanty data at far situated places
undoubtedly indicate the developmentof the Eo-Trias in the eastern Himalaya
and suggests that a thorough search ofthese beds will prove one day its continuity and lateral variations of lithogy
and faunas ..
The probability of its presence is also
supported by the Lower Triassic bedsof Burma at Na-Nahkam in the Yunan
State. SAHNI (1932, p. 66; 1938, p. 114
and in PASCOE, 1959, pp. 902-3) reportsthat the interstratified dolomites in aseries of thin bedded argillaceous
limestones and shales contain a richfauna apparently ranging from Otoceraszone (although this genus itself has notbeen found) to the Owenitan. Components of the fauna are Xenaspis
carbonaria W AAGEN, Glyptophiceras sp ..
Lytophiceras sp., Vishnuites sp., Owenites
sp., Kashmirites sp., etc. with a numberof gastropods and bivalves. Many of
the forms (such as Xenaspis) appear tobe the Permian survivors in the Lower
Trias. The fauna has affinity with the
Ophiceras fauna of Kashmir, Spiti andKumaon.
West of Kashmir, the Ophiceras fauna
is known from Salt Range, Pakistan(SCHINDEWOLF, 1954; KUMMEL and TEICHERT. 1966; TEICHERT and KUMMEL,
1970). SCHINDEWOLF in his paper included the description of Ophiceras
connectens SCHINDEWOLF which was later
reported by KUMMEL and TEICHERT
from a lower bed while working on thedetails of lower Scythian stratigraphy
and palaeontology. They found thisspecies from six inches above the baseof the Kathwai member (Lowest
Scythian Formation) of the Mianwali
Formation. Accordingly, KUMMEL (1966)

234

Hari Mohan KAPOOR and Yuji BANDO

correlated the Kathwai Member with theLowest Scythian (Ophiceras zone) age.
Further west, in Afghanistan, FISCHER (1971) also collected Ophiceras
from brown argillaceous limestone beds
just above the Permo-Triassic boundary
in Kohe Safi District of Eastern Afghanistan. This report was also substantiated by ISHII, FISCHER and BANDO(1971) in their report on the PermoTriassic boundary problems in Eastern
Afghanistan and occurrence of gyronitid
ammonoids from the Kohe Safi area.
From the study of the nature of lithofacies and presence of numerous verticalburrows made by suspension feeders at
the Permo-Triassic boundary, the above
authors derived conclusion that theUpper Permian calcium carbonate sediments were exposed to subaerial denudation and quick drying under the intertidal environments, thus causing a breakin the Eastern Afghanistan at theboundary zone.
It is not beyond scope to refer here
the recent work at Arctic Canada(TOZER, 1961). where Ophiceras commllne
SPATH with Otoceras boreale SPATH isreported from the beds near basal partof the Blind Fiord Formation in an
island of Queen Elizabeth Islands between Bunde and Bukken Fiords. It isslightly different from Guryul Ravineof Kashmir where Otoceras is known at
a later stage though within the Ophiceraszone.
The biostratigraphic significance of
the Ophiceras and Otoceras faunae from
Kashmir is being studied by one of theauthors (BANDO) and will be publishedelsewhere.
Systematic Description
The specimens described III detailwere collected by KAPOOR and werestudied in the Palaeontological Laboratory of Kagawa University by BANDO.
All the specimens are preserved in the
Palaeontological Division of the Geological Survey of India in Calcutta.
The views expressed in the following
pages are of BAN DO.
Family Ophiceratidae ARTHABER, 1911
Genus Ophiceras GRIESBACH, 1880
Subgenus Lytophiceras SPATH, 1930
Type species: Ophiceras charnunda DIEl':ER,1897, p. 123, pI. 12, figs. 3a-b.

Lytophiceras aff. ptychodes DIENER
DIENER, Pa1. Indica, Ser. XV, 11, p. 120, pI. xi, figs.
3, 5, 6.
1915. Ophiceras ptychodes, DIENER, Catalogue,
p. 213.
1930. Lytophiceras ptychodes, SPATH, Med.
om Gr¢nland, Bd. 83, 1, p. 21, pI. iv,
figs. 4a-b, pI. v, figs. 3a-b.
1934. Lytophiceras ptychodes, SPATH, Catalogue of Fossil Cephalopods, p. 78, pI.
i, figs. la-b.
1935. Lytophiceras aff. Ptychodes, SPATH,
Med. om Gr¢nland, Bd. 93, no. 2, p. 21,
pI. xix, fig. 9.

1897. Ophiceras ptychodes,

Description: - Shell laterally compressed. and also highly deformed laterally, with considerable strong falciradiateribs. Form of venter unknown due topoor preservation. Ornamentation ofshell surface shows characteristic falcoid
radial ribs and striations running fromumbilical margin and gradually diminishing toward ventral
margin.
Height of the last whorl about 1/3 ofthe diameter of shell; and diameter ofthe umbilicus a little less than half ofthe diameter of the shell. Width of theshell unknown.

627.

Lower T1"ias from Pir Panjal, Kashmir

235

Measurements (in mm)*:D

H

I

W

U

I

HID

I W/H I U/D

0.29 I
GSI. 18656
42. 2 1--15-.-6(-8.-6-)-1--=-119.9(11. 5)---------------1-----1--------.---------1------

I 0.47

O. 53

O. 28

1

DIENER'S
Lectotype--

38.8

16.0

!
8.6

10.9

O. 41

- D: Diameter of shell, H: Height of last whorl, W: \Vidth of last whorl, U: Diameterof umbilicus.
** DIENER (1897, p. 123, pI. xii, figs. 3a-b), SPATH (1934, p. 77)

Remarks:-The specimen described'above is highly deformed and compressed·laterally. The ornamentation of the shell:and the form of the whorl suggest it
belongs to Lytophiceras (a subgenus of
Ophiceras), not to the genus Glypto·
phiceras, which has stronger radial or
falcoid ribs from the body whorls to thejnner whorls of umbilical portion.
The genus Lytophiceras was consideredby SPATH (1934, p. 78) as the transitional.form from Ophiceras to Glyptophiceras
for the type specimen from the Ophiceras
bed of Pastun, Kashmir. The author
also agrees with SPATH'S view.
Lytophiceras ptychodes DIENER from
Pastun, Kashmir, resembles with Lytophiceras sakuntala DIENER. Both species
apparently look alike as remarked by
SPATH (1934, p. 78). However. in theopinion of the present author the two
species differ in the ornamentation ofshell. Lytophiceras sakuntala has more
feeble and weak falcoid striation thanthat of L. ptychodes.
Geological Horizon:- Flaggy shale.
Geological Age :-Otoceratan or Early
Induan stage of Eo-Trias. Scythian.
Locality:-Khowurwat Gali, Pir Panjal
Range, near Qazigund, Kashmir, India.
Regist. No. :-GSI (Geological Sun-ey·of India) 18651, 18656
Collector :-H. M. KAPOOR.

Subgenus Ophiceras SPATH, 1934
Type species: Ophiceras tibeticum, GRIESBACH, 1880, p. 109, pI. 5, fig. 4.

Ophiceras sp.
PI. 33, fig. 1

Description :-Shell rather evolute,
laterally compressed, with falcoid radial
fine striations. Umbilical shoulders considerably acute angled and their wall
shallow. Form of venter and sutures
unknown.
Remarks:-In the generic rank thepresent material may be belonged to thegenus Ophiceras judging from the shellornamentation and cross section of thewhorls. It is really unfortunate thatthe shape of the periphery is not clear
in this m3.terial.
Specifically. the present material iscomparable with some specimens of
Ophiceras (Discophiceras). The present
specimen. on the other hand, actuallyshows the same type of ornamentationofOphiceras greenlandicum SPA TH(SPATH, 1930, p. 16, pI. 11, figs. 12a-b;
1935, p. 15, pI. 11. figs. 1a-b, pI. 5, figs.
5a-b, pI. 10, figs. 1a-b, pI. 19, figs. 11ab), but high deformation of this specimen and missing septa unabled theauthor to identify with the boreal typeillustrated by SPATH.

Hari Mohan KAPOOR and Yuji BANDO

236

Glyptophiceras sp.

Geological Horizon:- Flaggy shale.
Geological Age :-Otoceratan or Early
Induan stage of Eo-Trias. Scythian.
Locality:- Malidar Gali, Pir Panial,
Kashmir, India.
Regist. No.:-GSI 18652
Collector:-H. M. KAPOOR.

PI. 33, fig. 5

Description:- Whorls evolute, laterallycompressed, with wide umbilicus. Shellsurface ornamented with widely spaced
radial ribs, which are most prominent at
one-third height of flanks and diminish
toward umbilical and ventral margin.
On surface of umbilical whorls ornamentation by faint radial folds become
gradually indistinct in the inner whorls.
Outer whorl overlaps about one-third
height of inner whorl. There are 12-13
radial ribs and faint sigmoidal striations
on shell surface of half part of outerwhorl. Suture unknown.

Genus Glyptophiceras SPATH, 1930
Subgenus Glyptophiceras TRUMPY, 1969
Type species: Glyptophiceras aequicostatum(DIDIER), DIEXER, 1913, p. 6, pI. ii,
figs. lOa-b.

Measurements (in mm):-

GSI. 18655

D

H

38.0?

12.5

Remarks:- The present specimen iscompletely crushed, so that the specificidentification is difficult. As to thecharacteristic ribbing or shell ornamentation in the outer whorl rather resemble
those of the genus Glyptophiceras andOphiceras s. str. The present author(BANDa) included subgenus Metophiceras(SPATH, 1935, p. 34, type species: Metophiceras subdemissum SPATH) in thegenus Ophiceras s. str. (BANDa, 1973).
Essentially, "Metophiceras" is a transitional form between the Glyptophiceras
and Ophiceras in the shell form, but it
is better to be included in the Ophiceras

W

U

HID

18. 7

0.33

W/H

U/D

0.49

s. str.
Hsu (1936-37) has described Ophiceras
from the Otoceras bed of the Chainglunglimestone (Lower Trias at Lungtan in
Kiangsu) and Ophiceras? sp. from the
Teyeh limestone (Lower Trias at Paoan
near Teyeh in Hupei), both in South
China. These Ophiceras ammonoids are
considerably crushed and secondarily
deformed like the Pir Panial specimens.
The shell ornamentation in the illus'
tration by Hsu (1936-37, p. 319, pI. 11,
fig. 3, not fig. 4), in comparison with Pir
Panial specimen, suggests that these be
included in Ophiceras s. str.

Explanation of ·Plate 32
Ophiceras fauna in the fiaggy shale. Locality: Khowrwat Goli, Pir Panjal Range,near Qazigund, Kashmir. Age: Otoceratan or Lower Induan stage, early Eo·
Trias. Collector: H. M. Kapoor.
Figured Specimen No. GSI. 18656 x 1.2

KAPOOR and BANDO:

Low e?" Trias from Pir Panjal, Ka shmir

Plate 32

627. Lower Trias from Pir Panjal, Kashmir
TRDMPY (1969, pp. 93, 94, pI. 1, figs.
4-6), in his descrition of a new speciesof "Metophiceras", i. e. "M." U;egeneri
TRDMPY (from the Lower Trias ofjameson Land in East Greenland), hasstated (op. cit., p. 93) that the genus" Metophiceras" is much closer to Glyptophiceras than to Ophiceras s. str., especially iIi the shell sculpture of theouter whorl and cross section of thewhorl, but the ornamentation of umbilical shell has a remarkable difference
from that of Glyptophiceras.
Geological Horizon:- Flaggy shale.
Geological Age :-Otoceratan or Lower
Induan stages of Early Eo-Trias.
Locality:- Khowurwat Gali, Pir Panjal
Range, near Qazigund, Kashmir, India.
Regist. No.:-GSI. 18655
Collector :-H. M. KAPOOR.
Subgenus HYPophiceras TRDMPY, 1969
Type species: Glyptophiceras triviale SPATH,
1935, p. 47, pI. 7, fig. 2.

HYPophiceras? sp.
PI. 33, figs. 2, 3

Description :-Shell evolute, laterallycompressed, with shallow umbilicus andnarrow venter. Shell surface ornamented
with falcoid radial fine ribs which arefiner on body whorl than on inner whorls.
Ribs most prominent at middle height
portion. on the flanks and graduallydiminish toward ventral and umbilicalmargin. Surface on umbilical whorls
ornamented with coarsely radial projections, but not on ribs and more obscurethan those of outer volution.
Remarks:-The specimen at hand isincomplete; especially the inner whorls
are not clear and the ornamentation ispoor; it is also highly deformed laterally.
However, generic identification

237

could be made though some dificulty,
but nothing could be ascertained on
species due to reasons given above.
The ornamentation of the outer whorl
and a part of umbilicus of the present
specimen shows its similarity to that of
Glyptophiceras and more closely to subgenus HYPophiceras TRDMPY (1969, p. 89).
Geological Horizon: - Flaggy shale.
Geological Age :-Otoceratan or Early
Induan stages of Early Eo·Trias.
Locality :-Khowurwat Gali, Pir Panjal,near Qazigund. Kashmir, India.
Regist. No. :-GSI. 18654, 18655.
Collector:-H. M. KAPOOR.
Acknowledgments·

The authors would like to record theirsincere gratitude to the Governments ofIndia and japan, for their kind support,cooperation and collaboration throughout
the work; without which this work
would not have been successful. The
present paper is one of the series of the
Indo- japanese collaboration in Geological
Sciences.
The authors are especially indebted to
Mr. M. S. BALASUNDARAM, Director
General, Geological Survey of India;
Professor K. NAKAZAWA of the Department of Geology, Kyoto University, japan; Dr. M. K. ROYCHOWDHURY, Duputy
Director General of Northern Region,
India; Dr. M. V. A. SASTRY, Director of
Palaeontological Division, Geological
Survey of India; Dr. K. ISHII of Osaka
City University, japan, and Mr. ]. P.
SRIVASTAVA, Palaeontologist-in-charge,
Northern Region, Geological Survey ofIndia, for their guidance, cooperationand providing facilities which enabled
the authors to excute the project on the
Permo-Triassic boundary in Kashmir
Himalaya. Lastly, but not the least,
help and useful suggestion of their

238

Hari Mohan KAPOOR and Yuji BANDO

colleagues Drs. D. SHIMIZU, Y. NOGAMI,
T. TOKUOKA and S. NORD A of Kyoto
University and Dr. T. MAEGOYA of Kyoto
University of Industry are duly acknowledged.
ReferencesY. (1973): On the Otoceratidae andOphiceratidae. Sci. Rep. Tohoku Univ.,
2nd ser. (Geo!.), Spec. Vo!. No.6 (Hatai
Mem. Vo!.), pp. 337-351, pis. 38-39.
BORDET, P., COLCHEN, M., LEFORT, P.,
MOUTERDE, R. and REMY, M. (1967):
Donnes nouvelles sur la geologie de la
Thakkhola (Himalaya du Nepal). Bull.
Soc. geol. France. 9(7), pp. 885-896.
DIE1'ER, C. (1897): Himalayan fossils. The
Cephalopoda of the Lower Trias. Pa/.
Indica, Ser. 15, 2, pp. 1-181, pIs. 1-25.
- - (1912): The Trias of the Himalayas.
Mem. Ceo/. Surv. India, 36(3), pp. 1-159.
- - (1913): Triassic fauna of Kashmir.
Pal. Indica, (N. S.) 5(1), pp. 1-133, pis.
1-15.
- - (1915): 'Fossilium Catalogus. 1, pt. 8.
Cephalopoda triadica '. pp. 1-369.
FISCHER, J. (1971): Zur Geologie des Kohe
Safi bei Kabul (Afghanistan). N. Jb.
Ceo!. Paliiont. Abh., 139, pp. 267-315.
FUCHS, G. R. (1964): Note on the geologyof the Palaeozoics and Mesozoics of the
Dolpo Region (Nepal Himalaya). Sand.
Verhand. Ceol. Bund. 1, pp. 6-15.
GRIESBACH, C. L. (1880): Palaeontologicalnotes on the Lower Trias of the HimaBANDO,

layas. Rec. Ceo!. Surv~ India, 13, pp. 94115, pis. 1-4.
HAYDEN, H. H. (1904): Geology of Spiti.
Mem. Ceol. Surv. India, 36(1).
HAZRA, P. C. and PRASAD, K. N. (1963): A
note on the stratigraphy of the Banihal
Region, Pir Panjal Range, Kashmir.
Rec. Ceo!. Surv. India, 93(2), pp. 121-128.
Hsu, Te-You (1936-37): Contribution to themarine Lower Triassic fauna of southern
China. Bull. Ceoi. Soc. China, 16, pp.
303-334, pis. 1-4.
ISHII, K., FISCHER, J. and BANDO, Y. (1971) :Notes on the Permian Triassic boundary
in Eastern Afghanistan. Jour. Ceosci.,
Osaka City Univ., 14, pp. 1-18, pis. 1-3.
KRAFFT, A. VON and DIENER, C. (1909):
Himalayan fossils.
Lower Triassic
Cephalopoda from Spiti, Malla Johar, andByans. Pa!. Indica, Ser. 15, 6, pp. 1-186,
pis. 1-31.
KUMMEL, B. (1966): The Lower Triassic
formation of the Salt Range and Trans
Indus Ranges, West Pakistan. BUll. Mus.
Compo Zool., Harvard Univ., 134(10), pp.
361-420, pis. 1-4.
KUM?vIEL, B. and TEICHERT, C. (1966): Relations between the Permian and Triassic
formations in the Salt Range and Trans
Indus Ranges, West Pakistan. N. Jb.
Ceol. Palliont. Abh., 125, pp. 297-333, pis.
27-28.
MIDDLE~IISS, C. S. (1910):
A revision of
Silurian-Trias sequence in Kashmir. Rec.
Ceo!. Surv. India., 40, pp. 206-268.
NAKAZAWA, K., KAPOOR, H. M., ISHII, K.,
BA:'\DO, Y., MAEGOYA, Y., SHIMIZU, D.,

Explanation of Plate 33
All figures x 1.2. Figure 1 from Malidar Gali and figures 2-5 from Khowurwat
Gali, Pir Panjal, near Qazigund, Kashmir. Age inferred for all ammonoid bearing
horizons is the Otoceratan or Lower Induan stages of early Eo-Trias. Collector:
H. M. KAPOOR.
Fig: 1. Ophiceras sp. GSI. 18652; from Ophiceras bed.
Figs. 2, 3. Hypophiceras? sp. GSI. 18654, 18655
Fig. 4. Lytophiceras sp. (aff. L. ptychodes DIENER) GSI. 18651
Fig. 5. Ciyptophiceras sp. GSI. 18653(All specimens preserved in the Palaeontological Division of the Geological Survey of India)

KAPOOR and BANDO : LoweT T1·ias !1"Om Pir Panjal, KashrniT

Plate 33

627. Lower Trias from Pir Pan:jal, Kashmir
NOGAMI, Y., TOKUOKA, T. and NOHDA,
S. (1970): Preliminary Report on the
Permo-Trias of Kashmir. Mem. Fac. Sci.,
Kyoto Univ., Ser. Geol. & Min., 31(2),pp. 163-172, pis. 28-29.
PASCOE, E. H. (1959): A manual of thegeology of India and Burma. 2., pp. 902905.
SAHNI, M. R. (1932): General report of thegeological survey of India for the year.
1951. Rec. Geol. Surv. India. p. 66.
- - (1938): Discovery of the Lower Triasat Na-hkam, Northern Shan States, anddescription of the fauna. (Abstract).
Proc. 25th Ind. Sci. Congr., Calcutta, pt.
3, p. 114.
SCHlNDEWOLF, O. H. (1954):
tiber dieFundenwende vom Palaozoikum zum
Mesozoikum.
Zeitsch. Deutsch. Geol.
Ges., 105, pp. 154-183.
SPATH, L.F. (1930): The Eo-Triassic Invertebrate Fauna of East Greenland.
Med. om Gr¢mland, 85, pp. 1-90, pis. 1-12.
- - (1934): Catalogue of fossil Cephalopoda
in the British Museum (Natural History).
Part 4, the Ammonoidea of the Trias(1). Brit. Mus. pp. 1-521, pis. 1-18.
- - (1935): Additions to the Eo-triassic

239

invertebrate fauna of East Greenland.
Med. om Gn/mland, 98(2), pp. 1-115, pis.
1-25.
TEICHERT, C., KUMMEL, B. and KAPOOR,
H. M. (1970): Mixed Permian-Triassic
fauna, Guryul Ravine, Kashmir. Science,(3915), pp. 174-175.
TEICHERT, C. and KUl\'IMEL, B. (1970):
Stratigraphy and palaeontology of thePermian-Triassic boundary beds, Salt
Range and Trans Indus Ranges, West
Pakistan. Strat. Bound. Problems: Perm.
& Trias of West Pakistan. Univ. Kansas,
Dept. Geol. Spec. Pub., 4, pp. 2-110.
TOZER, E. T. (1961): Triassic stratigraphy
and faunas, Queen Elizabeth Islands,
Arctic Archipelago. Mem. Geol. Surv.
Canada, 316, pp. 1-116, pis. 2-30.
TROMPY, R. (1969): Lower Triassic ammonites from Jameson .Land (East Greenland). Med. om Gn/mland, 168, (2), pp.
81-116, pis. 1-2.
W ADIA, D. N. (1928): The geology of Poonch
State (Kashmir) and adjacent portionsof the Punjab. Mem. Geol. Surv. India,
15(2), pp. 248-255.
- - (1957): Geology of India, Macmillan &Co. Ltd.

Trans. Proc. Palaeont. Soc. Japan, N. S., No. 93, pp. 240-248, pI. 34, April 20, 1974

628. A NEW SPECIES OF INOCERAMUS FROM THE
SHIMANTOGA WA GROUP OF SOUTH SHIKOKU*
MASAYUKINODA
Wasada Junior High School, Oita

1!!,lffill19J;-j'JlI:'¥-Hillrd:: I)iit:l', L t::.1 / t;7 J." ;J.O)Wlifill::.--::>v,-C: ~117J-j-)II~JflllrlpGI;t,
Hi k f:. Bill!~ltl.l;n[Hf G~c -C \" ~ i.J:, tJ:E*t':~ <0)AA:r.~'2~ L- -C \" ~ .:to)t:jr(:,r41 i1tit[i!(;/i::;::0) ®:1Jf:' 3tit-t ~ rXIJttM Uli{f!Ji) ;]' G:Itli!I~fiT[i.J'O) ifiJj* [(I)~ltl.li.J; t*1,{£ i:' ~c, 1T~)tJ:~ft
tk:7EO)jffli.J;1~ G ht::. 0) c':ltWi f:. --::>\' '-c.:to) ~ft '21f* -J- ~, '*- t::., illi:+', L- t::.1 / t ;7 J.,,;J.
0O)rl!l:'fH;'i'~UJ: 1fMJl'2 t --::> t 0)i.J: ~.2 Ii) G~l.,~ 0)-(', C. ::::'1:.WIiHU:: L -c)11< L

Introduction
The apparently thick deposits. generally called the Shimantogawa group, areextensively developed in the southernterrain of the Outer Zone of Southwest
Japan. The group consists mainly of
shale and sandstone in various gradesof thickness and has occasional' interbeds or lentils of conglomerate, basaltic
lava, tuffite, chert and limestone.
Recently the paleontological study ofthis group has been carried out on molluscan fossils found at some limited
places and offered important biostratigraphical data, as those descrived by
MATSUMOTO, KIMURA and KATTO (1952),
KATTO and OZAKI (1956), NAGAI, NAKANO, YOSHIDA and OHOTSUKA (1962),
NAKAI and HADA (1966), HAY AMI andKAWASAWA (1967), HASHIMOTO (1967),
MATSUMOTO and HIRATA (1969) and
MOROZUMI (1970).
Since 1969, I have examined the Inoceramids from this group. In this paper,
I deal with the geological age of the* Received June 8, 1973: read Oct. 28,
1972 at Matsuyama.

;b:/:H:t-C.:to)H m •Wn~~'2~~-t~,~"Misho formation", one of the Shimantogawa group and the paleontologicaldescription on a new species of Inoceramus from that formation, and do
not intend to give comprehensive comments on the classification of the Inoceramidae. Only a short remark is
given in connections with the allied
species.
Before going further, I wish to acknowledge my indebtedness to several
persons for their supporting of mywork. My gratitude is first due to Professor Tatsuro MATSUMOTO of Kyushu
University for much valuable ad vices
and kind supervision of this work.
Thanks are to Dr. Itaru HAY AMI for
his kindness to the laboratory work andthe bibliographic survey, to Professor
Kozo NAGAI of Ehime University andProfessor Michitoshi MIY AHISA of Ehime
University for their favours to supply
me with a number of specimens andthe valuable references. Finally mygratitude is dedicated to Mr. Yasushi
YUASA, Mr. Masaharu SEKI and Dr.
Hakuyu OKADA who have stimulated
through Prof. MATSUMOTO the present
study with valuable specimens of their240

Inoceram~ts from628.
collections.

Note on Geology

The "Misho formation" is exposed on
the northern coast of Sukumo Bay,
which is situated in the southwesternpart of the Shimanto belt of South
Shikoku. The northern margin is demarcated from another unnamed formation of the Shimantogawa group by
fault, and the east area also boundedby fault to the Arioka formation of theUpper Cretaceous developing in the
Nakasuji-Rift-Valley.
The name ofthis formation was proposed by NAGAI
and others (1962).
However, OKADA(1971) disapproves the name of the"Misho formation" by the reason of

241

Shimantogawa Groupphonetic confusion that the "undifferentiated Mesozoic" was called "misho
Mesozoic" in Japanese.
The geology of this district is shownin Fig. 1. The formation mainly consistof sandstone, shale and their alternation.
They are broadly arcuate in strike,showing a trend of NEE-SWW, E-W
and NWW -SEE, and divided into several
blocks by transverse faults. The geologic structure is generally complicate,with overturned strata and fractured
zones. Sandstone in various grades ofcoarseness is mainly distributed in thesouthern part of the mapped area. Eachsandstone bed is commonly more than
20 em in thickness, and in some partthin layers of mudstone are frequently
inserted. In some other part sandstone

EXPLANATION
Allvial depoaila

t:::::i000000Ttrrxial • .cIiment.

F'Lllt,..iI ic

locallt)'

10..

SCALE
114

Text-fig. 1.

Geological Map of the Johen area.

242

Masayuki NODA

and mudstone are alternateq.
Thenorthern part is occupied by mudstone
with subordinate intercalation of sandstone of .various thickness. Although
the thickness of this formation is notprecisely known, because of complicatedstructure, it is divided into two members, of which the Lower member isprobably represented by the sandstoneof the southern part.
Molluscan fossils occur in the mudstone bed near Nishi, Johen Town andNakanokawa and Naro, Ipponmatsu
Town, Minamiuwa County, Ehime Prefecture. The stratigraphic position of thefossiliferous bed is probably assigned tothe middle part of the Upper memberof this formation.
The faunal list is as follows:
Inoceramus balticus toyajoanus NAGAO
and MATSUMOTO
Inoceramus balticus subsp.
Inoceramus schmidti MICHAEL
Iuoceramus yuasai n. sp.
Maolites sp.
Ammonites gen. et sp. indet.
According to MATSUMOTO in T AKAI
and MATSUMOTO (1961), I. balticus toyajoanus probably indicates the Lower.
Hetonaian. NAGAI et al. (1962) reported
Inoceramus balticus toyajoanus from
Naro, Ipponmatsu Town, and considered
the geological age of this formation as
the Upper Urakawan to the Lower
Hetonain (approximately Upper Santonian to Campanian), and they referred
the flat large specimen (see NAGAI etal. 1962, PI. 1, fig. 3) to one of I. balticus
subsp. Now I am examining on thechronological change of morphology ofUpper Cretaceous Inoceramus. Thus, I
put off, at present, the subspecific determination of that specimen, which will
be proposed in a separate paper. Furthermore, MATSUMOTO (personal information) identified I. schmidti, an effec-

Text-fig. 2.

Locality Map.

tive indicator of the Lower Hetonaian,and Maorites sp. in the collection of
YUASA from the same bed of Ipponmatsu. On the paleontological evidence
mentioned above. the fossiliferous bedof this formation is probably referredto the Lower Hetonaian, i. e. Campanian
in term of international scale.

Paleontological Description
Family Inoceramidae GIEBEL, 1852
Genus Inoceramus J. SOWERBY, 1814

Inoceramus yuasai n. sp.
PI. 34, figs. 1-10

1962. Inoceramus sp., NAGAI et aI., Mem.
Ehime Univ., Sec. 2, Ser. D, vol. 4,
no. 3, p. 3, pI. 1, fig. 2.

Material:-Holotype: GK. H6823. (PI.
34,fig. 1) internal mould of left valve
from Nakanokawa, Ipponmatsu Town,
Minamiuwa County, Ehime Prefecture(coli. Y. YUASA). Paratypes: GK. H6824,(PI. 34, fig. 5), internal mould of rightvalve, in the same rock as the holotype.
GK. H6826 (PI. 34, fig. 3), internal mouldof right valve from the type locality(colI. Y. YUASA). GK. H6831 (PI. 34, fig.
4), external mould of left valve (colI. M.
SEKI), GK. H8005 (PI. 34, fig. 9), internal

628.

Inoceramus from Shimantogawa Group

mould of right valve, GK. H8004 (PI. 3,
fig. 7), and GK. H8006 (PI. ~, fig. 2a, 2b),internal moulds of left valve from Nishi,
lohen Town, Minamiuwa County, Ehime
Prefecture (colI. M. NOD A). Repository:
Department of Geology, Kyushu University. There are many other specimens
in NODA's private collection.
SPecific Characters :-Shell small to
medium in size, probably subequivalve
or slightly inequivalve, inequilateral,
moderately inflated from anterior toposterior and from umbo to ventral extremity, with an abrupt change in· comvexity along the growth axis. Anterodorsal part steep or perpendicular tovalve plane, postro-dorsal part abruptly
flattened to wing-like area without sharpboundary. Hinge-line straight and fairly
long, about two thirds of the shelllength. The growth axis gently concaveto the anterior. Umbo terminal, considerably inflated; left one more prominent than the right, rising above thehinge-line. Beak angle about 800, apicalangle slightly larger than a right angle.
Small individuals, less than 10 mm in
growth axis, slightly longer than high,Table 1.
Specimen*
GK. H6823*
holotype, internal mould of LV.
GK. H6826*
paratype, internal mould of RV.
GK. H6831
paratype, external mould of LV.
GK. H8002
paratype, internal mould of LV.
GK. H8005*
paratype, internal mould of RV.
GK. H8006*
paratype, internal mould of LV.

243

and gradually becoming higher withgrowth, resulting in the outline slightly
higher than long in the left valve andas long a,s high in the right one.
Antero-dorsal margin moderate inlength and straight or slightly concave,anterior margin broadly arcuate passing
gradually to the narrowly rounded ventral margin and then to the more
broadly curved postero-ventral one,which is in turn bent abruptly to themoderately long and nearly straight
posterior margin. The angle between
the posterior margin and the hinge-line
about 130°.
Surface ornamented with low, narrowand sharp concentric ribs which are
regular in strength and distance. Interspaces comparatively broad and concave.
Two or three round-topped radial folds
run from the umbonal part to the anterior and also to ,the postero-ventral
extremity. They vary in strength andstage of appearance. In some specimens
the radial folds are very weakened, only
showing abrupt bending in concentricribs.

Measurements :--Dimension in mm.
H

L

36

25

27

h

I

I

hll

HL

30

27

1.1

15

27

26

26

1.0

20

58

52

55

49

1.1

29

17

11

16

14

1.1

7

29

24

28

25

1.1

-

34

34

33

33

1.0

-

I

I

* Less deformed specimen.
.
L y,: left valve, RV: right valve, H: maximum dimension along the growth axis, L:maximum dimension along a line perpendicular to H, h: height; measured perpendicular to the hinge-line, I: length; measured parallel to the hinge-line, h/l: proportionof height to length, HL: length of the hinge-line.

244

Masayuki NODA
Table 2.
Specimen
GK. H6823, holotype
GK. H6826, para type
GK. H8001

Measurement of 'angle.
IX

f3

T

0

9595°
95°

80°
80°

130°
130°
130°

60°

80°

60°
55°

apical angle between hinge-line and.anJeriq.r IJ?':lrgin.
f3: beak angle of umbonal inflation.
'
T: postro-dorsal angle between hinge·line and posterior margin.
0: obliquity, the angle between hinge-line and the line from umbo to ventral extremity.
IX:

Table 3.

Change of obliquity with growth.
length of growth axis in mm.

SpeCimen
GK. H6823
GK. H6831. 'GK. H8007

30

35

56°

56°

60°

62°

60°
67°

-

-

5

10

15

20

25

35°
-

40°
50°

47°
57°

35°

48°

60°

50°
60°
70°

-

Remarks :-Only four specimens (GK.
tion. The specimen of GK. H8006 iscomparable to a certain form of InoH6823, GK. H6826; GK. H8005 and GK.
ceramus inconstans (WOODS, 1912a, p.
H8006) are fairly well preserved show·
285-291, pI. 51, figs. 2a, 4a; 1912b; p. 14,
ing the original outline, the shell convexity and the surface ornamentation.
text-figs. 69, 70), in abrupt change ofMany other specimens are more or lessconvexity and curvature of concentricribs, but differs from that form in its
modified by secondary deformation,
therefore, the marginal outline, the conless convexity and more clearly devexity and the proportion of hl1 areveloped concentric folds, as well as its
apparently varied. GeneralIy details ofradial ornament.
Inoceramus mihoensis MATSUMOTO,
the surface ornamentation are better
impressed on the external mould (e. g.
from the upper part of the Lower UraGK. H6831). 'The concentric ribs and'kawan (K5a), (approximately Upper
radial folds are variable in strength andConiacian) of Saghalien, Hokkaido andshape of cross-section, although apparKyushu, is also similar to the present
ently varied state sometimes occurs
species in in~Cjuivalveness and abrupt
owing to the secondary deformation.
change of convexity along the growthaxis but the former is distinguishedIn spite of the above situation, fromfrom the latter in its large size, absence
the synthetic judgement of availableof the posterior' wing-like area, curvaspecimens, the distinctive specificcharacters are recognized as above.
ture of the concentric ribs and absence
Comparison: - Inoceramus inconstansof the radial ornamentation.
According to WOODS (WOODS, 1917),
WOODS from the Upper Chalk of EngInoceramus
australis WObDS (WOODS,
land, .shows'considerable'variation
hi'
';
"..
. '::.
.
1917, p.27, 28, pI. 12, figs. 17-19; pI. 13,
margmaloutline, shell ,convexity, profigs. 1-3), from the Campanian of the
portion of hl1 and surface ornamenta(

628.

Inoceram1LS from Shimantogawa Gro1Lp

Amuri group of New Zealand, is allied
to Inoceramus inconstans. It is also
somewhat allied to the present species
in abrupt change of convexity but discriminated from the latter in large proportion of hl1 and absence of the radialfolds.
Inoceramus (Cordiceramus) brancoiformis SEITZ (SEITZ, 1961, p.15 9-163, pI.
13, fig. 4, pI. 14, figs. 1-3) from the Middle to Upper Santonian of northwest
Germany, also closely resembles thepresent species in abrupt changes ofthe shell convexity, presence of theposterior wing-like area and also presence of the radial ornamentation, butdiffer from the latter in larger apicalangle, larger obliquity and less proportion of hll.
NAGAI et a!. (1962) regarded that thepresent species somewhat resembles
Inoceramus balticus BOHM and the allies
from the Upper Urakawan to the Upper
Hetonaian (approximately Santonian to
Maestrichitian). Their material, however, as they explained, is a single imperfect specimen, which seems to be
specifically indistinguishable from oneof the present specimens (GK. H8005).
The present species is apparently
similar to Inoceramus subsulcatus WILSHIRE (1896) (WOODS, 1911, p. 268, pI. 42,
figs. 5, 6), from the Upper Gault of England, in the inequivalveness, development of the radial folds which vary innumber, shape of cross-section andstage of appearance, but distinctly differs from the latter in its less prominent umbo, less convexity, presence ofwing-like area, more strongly developed
concentric ribs and anteriorly curved
growth axis.
To sum up, the present species is not
identical with any previously described
species. Therefore, it is described undera new specific name which is dedicated245

to Mr. Y. YUASA who provided throughProf. T. MATSUMOTO valuable specimensof his collection for this study.
Consideration :-Cox (1969), (in MOORE
ed., p. 317) set up subgenus "Cremnoceramus"(=Cephaloceramus HEINTZ,
1932) for the species which are characterized by subequivalve or inequivalve
shell, slight or moderate obliquity,
abrupt change of convexity along the
growth axis and absence of narrow
postero-dorsal wing, and designated
Inoceramus inconstans WOODS as its
type species.
Regardless of the presence or theabsence of radial folds, the essential
characters of inequivalveness and abruptchange of shell convexity are in common between Cremnoceramus spp. andInoceramus yuasai. This may suggest
some connections between them. Although Inoceramus inconstans. is notfound in Japan, it is said to be very
persistent ranging from the Upper
Turonian· . to the Upper Campanian.
Furthermore, as WOODS (1912b) himself
has already admitted, the very variable
I. inconstans has been considered as
an ancester which gave rise to manyother species. Inoceramus mihoensis
from the upper part of the Lower Urakawan (K5a) (approximately Upper
Coniacian) is regarded by MATSUMOTO
as . a lateral off-shoot from the main
stock of the group of 1. inconstans. In
the essential characteristics mentioned
above, I. mihoensis is also similar to thepresent species, but the available specimens, are insufficient for linking stratigraphically these two species.
Inoceramus australis, from the Campanian of New Zealand, is probably
allied to I. inconstans, as WOODS (1917)
has mentioned, but I consider that there
is more intimate relation in morphology
between I. mihoensis and the present

Masayuki NODA

246.

species than that of I. australis and thepresent species.
SEITZ (1961) has pointed out that theimmature form of Cremnoceramus issimilar to that of Heanlainia (=Cordiceramus HEINTZ, 1932) and graduallydifferentiates from the latter withgrowth. It seems to suggest the intimate connection between the two subgenera. Regardless of the geographicaldistance, Inoceramus(Cordiceramus)
brancoifonnis SEITZ from the Middle toUpper Santonian of northwest Germany,
may be possible to link morphologicallyand stratigraphically the present species
with Inoceramus (Cremnoceramus) inconstans WOODS.
To sum up, in view of the above discussions, it is more reasonable to consider that the present species is probably
derived from some forms of I. (Cremnoceramus) inconstans.
Occurrence:- Rather crowded in theblack shale of the presumably middle
part of the Upper member of the "Misho
formation". Locality MS201; Nakanokawa, Ipponmatsu Town, Minamiuwa
County, Ehime Prefecture, location,Long. 132°37'52"E, Lat. 32°57'04"N. Locality MS202; Nishi, lohen Town, Minamiuwa County, Ehime Pref., location,Long. 132°36'37"E, Lat. 32°56'57"N.
NODA and TASHIRO (1973) reported thepresent species as Inoceramus n. sp. (seeNODA and TASHIRO, p. 494) from the basal
part of the Izumi group at Dogo-Himezuka,
Matsuyama City, associated with I. schmidti
andnumerous
speciesof Campanianpelecypods. Loc. IMI0l, location, Long.
132°51'00"E, Lat. 33°50'42"N.

References Cited
Ehime Prefecture (1967): Geological Map ofEhime Prefecture of scale 1: 100 ,000 and
its explanatory text, p. 1-182 (in Jap<,lnese).

HASHIMOTO, K. (HIRATA, M. ed.), (1967):
The Geology of Tosa. Rep. Hirata Geol.
Inst. Kochi Pref., p. 1-109 (in Japanese).
HAYAMI, 1. and KAWASAWA,. K. (1967):
Some Lower Cretaceous Bivalves fromthe Shimantogawa group of South Shikoku. Trans. Proc. Palaeont. Soc. Japan,
N. S. (66). p. 73-82, pI. 9.
KATTO, J. and OZAKI, H. (1956): Fossil_ Solemya found from the undivided Mesozoic complex of southern Shikoku. Res.
Rept. Kochi Univ., vol. 5, no. 10, p. 1-3,
pI. 1.
KATTO, J. et al. (1961): Geological andMineralogical Map of Kochi Prefectureof scale 1: 200 ,000 and its explanatory
text, p. 56-90 (in Japanese).
MATSUMOTO, T. (ed.), (1954): The Cretaceous system in the japanese Islands.
xiv+324 p., 36 pis. Japan Soc. Promot.
Sci., Ueno, Tokyo.
- - (1959): Zonation of the Upper Cretaceous in Japan. Mem. Fac. Sci., Kyushu Univ., D, vol. 9, no. 2, p. 55-93.
- - (1969): Study on the Cretaceous Ammonite of Circum-Pacific region. japanese
Scientific Monthly, vol. 22, no. 6, p. 7-17
(in Japanese).
MATSUMOTO, T. and HIRATA, M. (1969):
A new ammonite from the Shimantogawa group of Shikoku. Trans. Proc.
Palaeont. Soc. japan, N. S. (76), p. 177184, pI. 20.
MATSUMOTO, T., KIMURA, T. and KATTO,
J. (1952): Discovery of Cretaceous ammonites from the undivided Mesozoic
complex of Shikoku, Japan. Mem. Fac.
Sci., Kyushu Univ., D, vol. 3, no. 4, p.
179-186.
MOORE, R. (ed.), (1969): Treatise on Invertebrate Paleontology, (N), Mollusca 6,(1 of 3), p. 314-321, Geol. Soc. America,
Univ. Kansas Press.
MOROZUMI, Y. (1970): Upper Cretaceous
Inoceramus from the Shimanto belt of
the Kii Peninsula. Bull. Osaka Museum
Nat. Hist., no. 23, p. 19-24, pis. 2-4.
NAGAO, T. and MATSUMOTO, T. (1939,1940) :A monograph of the Cretaceous Inoceramus of Japan. Parts I and II. jour. Fac.

628.

Inoceramus from Shimantogawa Group

Sci., Hokkaido Imp. Univ., Ser. 4, vol. 4,
nos. 3-4, p. 241-299, pis. 23-34, vol. 6,
no. 1, p. 1-64, pis. 1-22.
NAGAI, K., NAKANO, M., YOSHIDA, M. and
OHOTSUKA, F. (1962): The Inoceramids,
discovered from the Shimantogawa groupof Ehime Prefecture, Shikoku. Mem.
Ehime Univ., Sec. II, Ser. D, vol. 4, no.
3, p. 1-7, pI. l.
NAGAI, K., HORIKOSHI, K., MIYAHISA, M.,
KASHIMA, N. and HAGA, Y. (1967):
Geological Map of Ehime Prefecture ofscale 1: 200,000 and its exPlanatory text,
p. 1-80, (in Japanese). Tomoeya, Matsuyama.
NAKAI, 1. and HADA, S. (1966): Discovery
of Aptian ammonites from the Shimanto
Terrain, western Shikoku. Trans. Proc.
Palaeont. Soc. japan, N. S. (62), p. 234250, pis. 29, 30.
NODA, M. and TASHIRO, M. (1973): The
fauna from Dogo-Himezuka, Matsuyama
City and its stratigraphic significance.
Jour. Geol. Soc. Japan, vol. 79, no. 7,
p. 493-495.
'OKADA, H. (1971): A pattern of sedimentation in clastic sediments in geosynclines. Mem. Geol. Soc. Japan, no. 6, p.

Dogo-Himezuka
Ipponmatsu
Johen
Minamiuwa
Nakanokawa

ill 'if;: ftil
;$:

!J&'
ri1

!f1

~

r·

J.,.

ill

+
/

fll
) II

247

75-85 (in Japanese with English abstract).
SUZUKI, T. (1938): Geological Map of Sukumo Sheet of scale 1: 75,000 and its explanatory text. Geol. Surv. Japan (inJapanese) .
SEITZ, O. (1961): Die Inoceramen des Santon von Nordwest-deutschland. Beih.
Geol. Jb., vol. 46, p. 1-186, pis. 1-15.
TAKAI, T. and MATSUMOTO, T. (1961): Cretaceous-Tertiary unconformity on Nagashima, Southwest Kyushu. Mem. Fac.
Sci. Kyushu Univ., D, vol. 11, no. 2, p.
257-278, pis. 11-12.
TAKAI, F., MATSUMOTO, T. and TORIYAMA,
R. (ed.) (1963): Geology of Japan. p.
114-117, Univ. Tokyo Press.
WOODS, H. (1911, 1912a): A monograph of
the Cretaceous Lamellibranchia. 2, part7, (1911), part 8, (1912), Inoceramus.
Palaeontgr. Soc. London.
- - (1912b): The evolution of Inoceramus
in the Cretaceous Period. Quat. Jour.
Geo!. Soc. London, vol. 68, p. 1-20.
- - (1917): The Cretaceous fauna of theNortheastern part of the South Island of
New Zealand. Palaeont Bull. no. 4, p.
1-41, pis. 1-20.

Nakasuji
Naro
Nishi
Sukumo

!f1

iltJ

:ft

JElJ

70

lI§

ill

O§

Masayuki NODA

248.

Explanation of Plate 34
Inoceramus yuasai n. sp.
Fig. 1. GK. H6823, holotype, internal mould of left valve. xL 3. Loc. MS201, Nakanokawa,
Ipponmatsu Town, Minamiuwa County, Ehime Prefecture (colI. Y. YUASA, 1968).
Fig. 2a, 2b. GK. H8006, paratype, internal mould of left valve, 2a, lateral view, 2b, anteriorview. xL 3. Loc. MS202, Nishi, Johen Town, Minamiuwa County, Ehime Prefecture·(colI. M. NODA, 1970).
Fig. 3. GK. H6826, paratype, internal mould of right valve. xL 3. Loc. MS202 (colI. M. SEKI,
1969) .
Fig. 4. GK. H6831, para type, rubber cast of left external mould, natural size. Loc. MS202(colI. M. SEKI, 1969).
Fig. S. GK. H6824, paratype, internal mould of right valve. xL 3. Loc. MS201 (colI. Y.
YUASA, 1968).
Fig. 6. JG. H20S1, internal mould of left valve, natural size. Loc. MS202 (colI. M. NODA,.
1971).
Fig. 7. GK. H8004, paratype, internal mould of left valve. xl. 3. Loc. MS202 (colI. M. NODA,.
1970) .
Fig. 8. GK. H8002, internal mould of left valve. x 1.3. Loc. MS202 (colI. M. NODA, 1970).
Fig. 9. GK. H800S, internal mould of right valve. xL 3. Loc. MS202 (colI. M. NODA, 1970).
Fig. 10. GK. H8003, internal mould of both valves. xl. 3. Loc. MS202 (colI. M. NODA, 1971).

JG:

Collection of Jonan Geological Association, Oita.

NODA:

Inoceramus j1"Om Shimantogawa Gro~~pPlate 34

Trans. Proc. Palaeont. Soc. Japan, N. S., No. 93, pp. 249-265, pis. 35, 36, 37, April 20, 1974

629. EARLY AND MIDDLE PENNSYLVANIAN FUSULINIDS
FROM SOUTHERN BRITISH COLUMBIA. CANADA ANDNORTHWESTERN WASHINGTON, U. S. A.*
KIMIYOSHI SADA
Department of Geology, Faculty of General Education,
Hiroshima University, Hiroshima 730

and
WILBERT R. DANNER
Department of Geological Sciences, University of British
Columbia, Vancouver, Canada

7J T~' British Columbia mffll c 7;-( ~ 7J-g.~~ffil Washington 1+1::jtl§j}~i.p GJ!flliT ~Pennsylvanian tJJWJ c if'WjO)*;Jj~:EJft: British Columbia m$O) Kamloops ->;" Keremeostil.(hJIC;[;;J: LF Vancouver lib, Washington 1+/0) Whatocom j:il.(lJlJ(~ San Juan f;'I'IIibR:5]::{flT:Q Pennsylvanian fflh:15-~tL:Q:fiEk¥il/:/;r.:'tJ':c'O)l=j:1f': Pennsylvanian tJJWliI'GI=j:1WH.:
v't.: :Q*Jj~!E.1t:fi!I!IJfJJMO)ff:ffHt3.(!, to ;: ;: '.:.f:'O)~HfIhi c: bb"CficT:Q PennsylvaniantJJltJ]0)*;Jj~!E.1t:fi!I!IJfJJMfi Millerella, Eostaffella, Ozawainella ? f.: J: -:> "Ct;'fi'i&--51t G:/1.,Endothyra, Endothyranopsis ?, Tetrataxis, Textularia, Climacammina t:J. EO)Jh~1f:rL
11~<b15-tro I=j:1JtJ]0)1t:fi!IiJJfJJRffi Nankinella ~ Eoschubertella ? tJ':c'f':J: -:>"Ct;Jil&--5ft
GtL"Cv':Qo tmtfJO)<bO)fi THOMPSON (1948) ~ Ross & SABINS (1965) GO)::jUj~O)
Pennsylvanian tJJltJ]0)*;Jj~!E.1t:fi!I!IJfJJg:H:M.ll ~:/1., ~ t::., /j>:;r·r,c6tliitil.(O) Millerella bigem.
micula 1t:fi!I!IJfJJRf o~m, 1957) ~ F>iiT'@:fiEk¥iO) Millerella bigemmicula.Eostafjellakanmerai 1t:fillil):j7l.Jm~ (ftc 13] , 1964, 1965), *~R:fiEkBO) Millerella 1t:fi[!I)~l.Jgf (ftc III ,1967) fC~f.C).l- "C v':Q 0
ftc III Ij} ~t. W. R. DANNER
0

these limestones may also contain inpart a Late Mississippian (Late Chesterian= Visean) fauna. This paper isthe first description of these fusulinid
faunas in southern British Columbia
and northwestern Washington and ispart of a continuing project on the description of Paleozoic faunas of this area.
The Early Pennsylvanian fusulinid
faunas of southern British Columbia
and northwestern Washington arecharacterized by Millerella marblensis, M.
sp., Eostaffella columbiana SADA & DANNER. n. sp., E. sp. A, E. sp. B, E. spp.,

Introduction
In southern British Columbia andnorthwestern Washington there is a
widespread sequence of Upper Paleozoic
rocks ranging in age from Middle
Devonian (in Washington) to Late Permian. A group of limestone lenses andpods within this sequence contains
Early to Middle Pennsylvanian fusulinids(DANNER, 1966, 1970a). In some areas* Received June 18, 1973; read Oct. 28,
1972 at Matsuyama.
249

250

K. SADA and W. R. DANNER

Ozawainella? sp. and Endothyranopsis?
sp. Associated microfaunas not describedin this paper include Endothyra spp.,
Climacammina sp., Textularia sp., Tetrataxis sp., Komia sp., pteropods and algae.
These fossils closely resemble the Early
Pennsylvanian faunas of North America
described by THOMPSON (1948) and Ross
& SABINS (1965), anda Iso the Japanese
Early Pennsylvanian faunas by IGO(1957) and SADA (1964, 1965, 1967). In
the western Cordillera of North America
they have been reported in the Fort St.
James area (THOMPSON, 1965), northwestern Washington (SKINNER & WILDE,
1966) and northern California (HARBAUGH, 1955; SKINNER & WILI)E, 1965).
The Middle Pennsylvanian fusulinid
fauna is much rarer and is characterized
by Eoschubertella ? sp. from Vancouver
Island and Nankinella plummeri THOMPSON from the Kamloops area of British
Columbia and the San Juan Islands ofWashington. The genus Eoschubertella
is a typical representative of early Middle Pennsylvanian age and is abundantin Middle Pennsylvanian rocks ofAmerica, Europe and Asia. In thewestern Cordilleran region it has beenreported. previously from the Fort St.
James area of central British Columbia(THOMPSON, 1965) and from the BallenasIslands off the east coast of Vancouver
Island (J. E. MULLER, personal communication in MONGER & Ross, 1971). Nankinella plummeri was originally describedby THOMPSON (1947) from the early
Middle Pennsylvanian Marble Falls
Limestone, Llano Uplift, Texas. The
genus is widespread in rocks ranging
in age from Early Pennsylvanian toLate Permian in Europe, Asia andNorth America but to our knowledge
no Early Pennsylvanian species has
been described from North America.
Unnamed species have been described

previously in Middle Pennsylvanianrocks of the western Cordilleran region
in the Fort St. James area of central
British Columbia (THOMPSON, PITRAT &SANDERSON, 1953) and from southeastern
Alaska (DOUGLASS, 1971).
Acknowledgments: Part of the fieldwork by DANNER was conducted under
grants of the National Research Councilof Canada, the National Advisory Committee of the Geological Survey ofCanada and the University of British
Columbia. Some of the field work innorthwestern Washington was performed
while DANNER was employed by theDivision of Mines and Geology of theState of Washington Department ofConservation. Re-examination and description of the material were undertaken
by SADA while he was at the Universityof British Columbia under a grant of the
National Research Council of Canada.
John W. SKINNER aided in preliminary
identification of some of the fusulinids
and furnished information on. the location of one of the Pennsylvanian fusulinid localities east of Kamloops, British
Columbia. We wish to thank all of themany property owners who kindly permitted access on their lands and collection of material. We also wish toacknowledge the numerous students of
the University of British Columbia and
Boy Scouts of the 80th University Hill
Troop who served as field assistants
over a period of several years in the
search for Pennsylvanian fossil localities
and who helped pack out a large
quantity of limestone samples. We give
special thanks to T. NEUFELDT, P. GARVIN, E. HUNTER and F. GLASS who prepared several hundred thin sections in
preliminary work on this project. Further work on this project was carriedout while DANNER was visiting Professor
at Hiroshima University under the aus-

629.

Pennsylvanian fusulinids from B. C. & Washington

251

I

x FORT ST. JAMES

!

~.

'"'"\

"

COLUMBIA

X CLINTON~~~'""-~ "~~~o.

\HO~~~\'PACIFICr)/'.

KEREMEOS CANADA.~~~ l.~

OCEAN~',"\,\.,\"KAMLOOPS"(HARPER RANCH)'-~r'-''-'-''''/-'+'~HILUWACK"""-SANJUANISLANDS \aJJWASHINGTON

U.s.lA. I
.'j..

'1

i .
I

.-.~.
N

'>

~

j
(
XSUPLEE

OREGON

"]

i
I

o

100
. MILE200'_._
I
CALI FOR Ni7\ . T' - ' - ' - ' j

Text-fig. 1. Map showing distribution of Lower Pennsylvanian sequence
in southwestern British Columbia and northwestern Washington. Black indicates Pennsylvanian limestone outcrops where fauna was collected and multiplication indicates other Pennsylvanian localities.

pices of the Japan Society for the Promotion of Science.
Stratigraphy and Discussionof Fauna

The Pennsylvanian limestones studied
in this paper are in the lower part ofthe eastern facies of the Cache Creek
Group in south central British Columbia.
In southwestern British Columbia andnorthwestern Washington they are in
the middle part of the Chilliwack Groupand on the San Juan Islands in north-western Washington they are in the
middle part of an as yet not formally
named sequence which is correlative with
the British Columbia central "oceanic"facies of the Cache Creek Group. On
Vancouver Island the Pennsylvanianlimestones are in the lower part of the
Sicker Group.
(1) Possible Late Mississippian limestones
Limestones that might be of Late
Mississippian age have so far proved tobe very rare in the study area. An as
yet undescribed species of the Late

252

K. SADA andW. R. DANNER

11\

LOW PERMIAN LIMESTONE\)

LOW. PENNSYlV.NlAN\

LO'H. PENNSYlVANIAN(
UP. MISSISSIPPIAN lIlo£STONELlMEST~V/\)

U~NOWN AGE UMESTONEI'VVV"FAULTN£

Text-fig. 2. Map showing the fossil
localities at Rayleigh near north of Cityof Kamloops in British Columbia.

Mississippian (Visean) coral Hexaphyllia
has been found in our collections fromthe limestones cropping out near thecommunity of Rayleigh north of Kamloops, British Columbia. This form,
along with a different species of Hexaphyllia from the Late Mississippian
Coffee Creek Formation of central Oregon (SADA & DANNER, 1973) is the only
known occurrence of Hexaphyllia in
North America. At the Rayleigh locality
we also found Eostaffella columbiana, E.
kanmerai, Millerella? sp. and endothyroid foraminifera which may indicatethat part of the limestone is of Early
Pennsylvanian age.
Some of the limestones exposed in the
Kendall limestone quarries on the westside of Red Mountain in northern Whatcom County, Washington, appear tocontain only endothyroid foraminifera
and this is also true of a small lime-stone lens located north of the road to
the Devonian limestones of the Red Cross
quarry on Orcas Island, Washington. It
is possible that these exclusively Endothyra-bearing limestones may be of Late
Mississippian age.
(2) Early Pennsylvanian limestones
Eastern Cache Creek Facies in Southern
British Columbia
Limestones containing an Early Pennsylvanian fauna are widespread in thearea north and east of the city of Kamloops in south central British Columbia_
The first indication of Pennsylvanian
age limestone was when M. Y. WILLIAMS(in COCKFIELD, 1948) tentatively identified the Early Pennsylvanian brachiopods, Neospirifer cameratus ? and Rhynchopora magnicosta, from this area but.
there is no indication of just wherethese brachiopods were collected. Later,
fusulinids of Early Pennsylvanian age
were found in limestone at Harper
Ranch (John W. SKINNER, 1965, written
communication). Subsequently we havefound Pennsylvanian fusulinids in limestones in the cliffs along the South
Thompson River, in the hills and meadowlands northeast and above the Harper Ranch, on the eastern side and top'of Mount Harper and in numerous lime-stone lenses in the hills along the east.
side of the North Thompson River north.
of the city of Kamloops.
The fauna is typified by Eostaffellacolumbiana, Eostaffella kanmerai, Millerella marblensis, Ozawainella? sp., Endothyranopsis? sp., numerous endothyroid
foraminifera, Tetrataxis, Climacammina,
Textularia, pteropods, large crinoid
columnals, large brachiopods and rare
corals.
Early Permian limestones characterized by large Pseudoshwagerina overlie
the Early Pennsylvanian limestone in
the Kamloops area. However, some of

629.

Pennsylvanian fusulinids from B. C. & Washington

253~ ....

o

SCALE

----

Text-fig. 3.

1 MILE

Locality map of Harper Ranch area near Kamloops, British Columbia.

the smaller Early Pennsylvanian limestone bodies form discrete lenses surrounded by clastic sediments. East of
the North Thompson River one of theselimestone lenses is inverted with beds
containing Early Pennsylvanian fusulinids overlying beds containing Early
Permian fusulinids. The contact is aparaconformity and is marked by alayer of chert pebbles and a zone ofsil icification.
At Keremeos, British Columbia in theBlind Creek Formation we have foundvery small primitive forms of Eostaffella,
E. sp. B, along with Endothyra andMillerella marblensis. The Keremeos
limestone also contains a coral identified
as of Permian or Late Carboniferous
age and a coral that resembles a Late
Mississippian species (SMITH, 1935). The

late Donald ANGOLD (personal communication) stated that there were two divisions of the limestone of the Blind
Creek Formation, one with abundantcorals and the other containing a few
poorly preserved brachiopods. His limestone specimens in which we have foundEostaffella, Millerella and Endothyracame from the non-coral part of theFormation so it is likely that the Blind
Creek Formation consists of an Early
Pennsylvanian limestone overlain by an
Early Permian limestone.
Chilliwack Group in British Columbia
and Washington
Large and small bodies of well-bedded
partly argillaceous limestone of Early
Pennsylvanian age are found in the
Chilliwack Group in southwestern British
Columbia and northwestern Washington.

254

K. SADA and W. R. DANNER

In the Chilliwack area of British Columbia (MONGER, 1966) they seldom exceed
100 feet in thickness but may be as
much as 600 feet thick or more in
Washington State (DANNER, 1966) andextend in discontinuous outcrops for atleast 65 miles southeastward into theNorthern Cascade Mountains.
The
Pennsylvanian limestones are overlain
by coarse- to medium-grained volcanic
arenites,
greywackes
andcobbleconglomerates. Some of the clastics
contain plant fragments identified as
Lepidodendron and Calamites by G. E.
ROUSE and may be of Later Pennsylvanian age. The .clastics are in turnoverlain by Permian fusulinid limestonesof Early Leonardian age.
The Early Pennsylvanian limestonesof the Chilliwack Group contain a fauna
similar to that of the eastern facies of
the Cache Creek Group exposed near
Kamloops, British Columbia and it includes Eostaffella columbiana, E. kanmeraz, Millerella sp., Ozawainella? sp.,
Tetrataxis sp., Textularia sp., Climacammin a sp., numerous endothyroids, large
crinoid columnals, coral, bryozoa andlarge brachiopods. The puzzling algaeor stromatoporoid Komia is locallyabundant.
San Juan Islands, Washington
On the San Juan Islands in northwestern Washington numerous .small
limestone bodies contain an Early Pennsylvanian fauna. They are overlain
on Orcas Island by a sequence of sedimentary and volcanic rocks containing
the Early and Late Permian faunas andon San Juan Island by volcanic andsedimentary rocks containing· a Late
Permian fauna.
The Late Permian
faunas on both islands contain Neoschwagerina and other Tethyan fusulinids
correlative with the middle or "oceanic"facies of the Cache Creek Group (DAN-

NER, 1970b; MONGER & Ross, 1971). The
Early Pennsylvanian limestones contain
Eostaffella spp., Millerella? sp., Ozawainella sp., Endothyra spp., Tetrataxis sp.,
Textularia sp., Climaca1nmina sp., large
crinoid columnals and corals. We havenot been able to obtain well enoughoriented material to identify the speciesof Eostaffella. On San Juan Island at
Roche Harbor Eostaffella sp. is associatedwith mats of filamentous algae in limestone interbedded with radiolariancherts.

~I'OU.lE~ ."OUNTCONSmUTION~
V /./-~\-\oc,~~~lOC.REDCRO.~~~==
.

N

••~

,,( A I

. A&if,\'.

ORCAS

SLAND

~,~t~~~·~WASHINGTONp~"--_....::._ _ _:.'..OMIl.ES

Text-fig. 4. Map showing the fossil localities
on San Juan Islands in Washington.

(3) Middle Pennsylvanian
Kamloops area and Vancouver Island,
British Columbia; Orcas Island, Washington
Nankinella plummeri THOMPSON was
found in limestones of the eastern faciesof the Cache Creek Group in the hills
and meadowland areas above and eastof the Harper Ranch near Kamloops,
British Columbia. Our collections containing it all come from the largest outcrop area of Pennsylvanian limestone
overlain by Early Permian limestone or
Triassic volcanic rocks and not fromthe small lenses of Pennsylvanian limestone in clastic rocks. Nankinella plum-629.

Pennsylvanian fusulinids from B. C. & Washington

meri is associated with Endothyra spp. inthese limestones.
On Vancouver Island Eoschubertella
was collected from a limestone bed on
the west side of Horne Lake and Eostaffella? sp. from limestone talus blocks
below the limestone cliffs on Mount
Mark on the north side of Horne Lake.
Endothyra sp. also occurs in these limestones. It had been suspected for several
years that Pennsylvanian rocks occur on
Vancouver Island (DANNER, 1960, 1965)
although YOLE (1963) could find only
evidence of Early Permian age. Morerecently the Middle Pennsylvanian fusulinids Wedekindellina and Eoschubertella
have been reported from North BalenasIsland just off the east coast of Vancouver Island in Georgia Strait CJ. E.
MULLER in MONGER & Ross, 1971). A

255

Pennsylvanian fusulinid fauna is also·
known to occur in the central "oceanic"facies of the Cache Creek Group inlimestones near the town of Clinton incentral British Columbia but it will be
discussed in a later paper when the·study of this area is completed.
On Orcas Island, Washington, our samples containing Nankinella came from asmall lens of argillaceous limestone on
the northeast slopes of Mount Constitution about 550 feet above sea level. The
limestone contains a microfauna of
Eostaffella sp., Millerella ? sp .. Endothyrasp., and crinoid columnals, bryozoa,
corals and one species of trilobite.
The thin sections used in this study
are deposited in the stratigraphic-paleontologic collections of the Universityof British Columbia, Department ofTable 1. Distribution of species of fusulinids and other microfossils by samples
from the Pennsylvanian limestone in British Columbia and Washington.

* As the sample containing Hexaphyllia sp. from Rayleigh is different from the·sample containing Early Pennsylvanian fusulinids, the species is not associated.
with Eostaffella columbiana, E. kanmerai, Millerella marblensis and M. sp.

K. SADA and W. R. DANNER

256
Geological Sciences.

Fossil Localities
British Columbia
Keremeos.-Blind Creek Limestone. Topof hill southeast of the town of Keremeos.
Rayleigh.-Road cut on east side of Yel·low head Highway about 8 miles north of thecity of Kamloops and just north of the com·munity of Rayleigh in SWI/. section 34, T.
21, R. 17.
Aspen Park.-Several small limestonebodies about 41/2 miles north on the Yellow·
head Highway from the city of Kamloops.
About one mile up hillside between 2000 and2500 feet in altitude. Near north boundaryof Kamloops Indian Reserve No.1 and southeast for 1/2 mile. Part of these same lime·stone bodies contain Early Permian fusul·
inids.
Harper Ranch.-Ridge of limestone in center of north 1/2 section 10, T. 20, R. 16, justwest of Harper Ranch buildings on Harper
Ranch Road.
South Thompson #l.-Lens of limestone
cropping out on south-facing cliff II. mile
north of South Thompson River and theriver road along eas,t section line of NEIl.
section 3, T. 20, R. 16.
South Thompson #2.-Breached anticlinlil
bed of limestone cropping out along' east
section line of section 2, T. 20, R. 16, on
top of terrace above So~th Thompson River
Valley about 1/2 mile north of South Thompson River and the river road.
North McGregor Creek.-Small knob oflimestone exposed at base of hills north sideof McGregor Creek valley, east end of Harper Ranch in SE II. section 12, T. 20, R. 16
about Jl/2 miles north of South Thompson
River at an altitude of approximately 1700
feet.
Upper Harper Ranch.-NEI/. section 7; T.
20, R. 15 in meadowlands in hills above eastend of Harper Ranch at an altitude of between 3000 and 3100 feet. Low ridges oflimestone north of small alkalie lakes.
Robins Lake.-Limestone outcrops aroundshores of Robins Lake, an alkalie Lake in the'NWI/. of section 8, T. 20, R. 15 in the hills
above the South Thompson River at an altitude between 3200 and 3300 feet.
Liumption Ridge. - Bedded argillaceous
limestone exposed up a stream bed near thebase of the steep slope forming the northside of Liumption Ridge. Above the south
side of a meadow area used for camping
which is about 1/2 mile up and south of
Liumption Lake. There was a cabin in themeadow in 1959. Altitude about 4600 feet.
Liumption Ridge is the southwestern extension of Church Mountain.
West Side Horne Lake.-Limestone exposedin outcrops along logging road above westside of Horne Lake.
North Side Horne Lake.-Talus blocks oflimestone at base of Mount Mark along logging road on north side of Horne Lake.
Washington
Black Mountain.-Limestone cliff near center of section 4, T. 40 N., R. 6 E., on anorthwestern spur ,of Black Mountain. Log, ging road at base of cliff. Northern Whatcom County.
Red Mountain.-Limestone outcrop on the
top of Red Mountain near its northern end
in the SWI/. section 12, T. 40 N., R. 5 E.
Upper Kendall Quarry.-Top of north endof large limestone quarry used for cement
rock. Section 14, T. ,40 N., R. 5 E.
Lower Kendall Quarry.-In east wall ofabandoned limestone quarry in the SWI/.
section 14; T. 40 N., R. 5 E.
Wright, Orcas Island.-Small area of limestone outcrop in the NEIl. section 19, T. 37
N., R. 1 W., at an estimated altitude of 900
feet on, the northwest side of Mount Constitution. Southeast of a large swampy area
and about lis mile south of Day Lake Road.
Double Hill #3, Orcas Island.-A 40 foothigh limestone knob on a north-facing slope
about the center of the SEll, of section
15, T. 37 N .• R. 2 W., on the west side of,the southern part of Double Hill. It is about
300 feet northwest and downslope from thepass between Double Hill and Lookout
Mouritain and about 120 feet north of the
Double Hill #2 limestone deposit:

629.

Pennsylvanian fusulinids fromB. c. & Washington

Mount Constitution, Orcas I sland.-Northeast slope of Mount Constitution in the SWI I,
section 16, T. 37 N., R. 1 W., just west of
the junction of a main logging road with
two abandoned spur roads. Knob-like exposure of limestone.
Orcas Knob, Orcas I sland:-Small limestonelenses and pods and large limestone cJastics
in'v'!»):eanic 'breccia in cliffs on west side ofOrcas Knob in the SEll, section 30, T. 37 N.,
R. 2 W. between top of knob and Soderberg
limestone quarries (Devonian age) at west
base of Orcas Knob.
Red Cross Quarry Road, Orcas Island.Small outcrop of oolitic limestone on vegetation covered ridge north above road into
Red Cross limestone quarry (Devonian age)in the NEIl." SEll, section 20, T. 37 N., R.
2 W. East of House.
Roche Harbor, San Juan I sland.-Southeast
side of northernmost limestone quarry at
Roche Harbor in the NEIl, section 23, T. 36
N., R. 4 W.

SY!jtematic Description
Family Ozawainellidae THOMPSON& FOSTER, 1937

Genus Millerella THOMPSON, 1942

Millerella marblensis THOMPSON
PI. 37, figs: 6-12, 14

1942. Millerella marblensis THOMPSON. Amer.
Jour. Sci., vol. 240, pp. 405-407, pI. 1,
figs. 3-14.
1944. Millerella marblensis, THOMPSON. Kansas Ceo!. Surv. Bull. 52, pp. 420-423,
pI. 1, figs. 1-9; pI. ,2, figs. 1-15.
1948. Millerella marblensis, THOMPSON. Kansas Univ., Paleont. Contr., Protozoa, art.
1, p. 76, pI. 23, figs. 1-12, pI. 24, figs.
1-9.
1951. Millerellamarblensis,
THOMPSON.
Contr. Cushman Found. Foram. Res.,
vol. 11, pt. 4, p. 118, pI. 13, figs. 14, 17.
1954. Millerellamarblensis, SKINNER &WILDE. Jour. Paleont., vol. 28, no. 4,257

p. 449; pI. 49, fig. 3.
1957. Millerella marblensis, IGo. Sci. Rep.
Tokyo Kyoiku Daigaku, Sec. C, vol. 5,
nos. 47-48, pp. 178-179, pI. 1, figs. 1314, 18-19.
1961. Millerella marblensis, RICH. Jour. Paleont., vol. 35, no. 6, p. 1159, pI. 142,
figs. 1-9.
1964. Millerella marblensis, MOORE. Jour.
Paleont., vol. 38, no. 2, pp. 295-305, pI.
47, figs. 1-24, pI. 48, figs. 1-23.
1965. Millerella marblensis, Ross & SABli"S.
Jour. Paleont., vol. 39, no. 2, pp. 183184, pI. 21, figs. 18-27.
1965. Millerella marblensis, Ross & TYRRELL. Jour. Paleont., vol. 39, no. 4, p.
621, pI. 76, figs. 38-42.
1967. Millerella marblensis, SADA. Trans.
Proc. Palaeont. Soc. Japan, N. S. no. 67,
pp. 140-142, pI. 12, figs. 13-14, pI. 13, .
figs. 1-3, 9.

Description:- The shell of Millerellamarblensis THOMPSON is discoidal· andshows rounded periphery and umbilicated poles. The shell of five volutions
illustrated as fig. 8 on PI. 37 (South
Thompson ~2-39-a) is 100 microns inlength and 400 microns in width, having
a form ratio of 0.25. The outer two or
three volutions are completely evolute.
The spherical proloculus of a specimen
measures 20 microns in its outside diameter. The radius vectors of the 1st
to the 5th volution of a specimen are30, 60, 100, 140 and 210 microns, respectively. The spirotheca consists of atectum and inner and outer tectoria andits thicknessof , the last volution is about.
20 microns. The septa are Closely
spaced. . The chomata are' small andprimitive.
Remarks:-As pointed out by THOMPSON (1948, p. 76)' Millerella marblensis
has a fairly broaq specific variation inits shell-shape and sizei In the shellshape and the internal characteristics,
the present specimens are identified

258

K. SADA and W. R. DANNER

with M. marblensis described by THOMPSON from the Lower Pennsylvanianrocks of Texas and New Mexico (1942,1948), Arkansas and Kansas (1944).
Occurrence:- M. marblensis was foundat the following localities: South Thompson #2, Harper Ranch, Robins Lake,
North McGregor Creek, Rayleigh, Aspen
Park, Keremeos and Mount Constitution
on Orcas Island.

in width, giving the form ratios of 0:26
to 0.49. The shell of the holotype is 300
microns in length and 820 microns inwidth, possessing a form ratio of 0.37.
The inner and outer volutions are involute but the last one is partly evolute.
The proloculus is large. Its outside
diameter ranges from 40 to 60 micronsin eight specimens. The radius vectorsof the 1st to the 6th volution of eightspecimens are 40-60, 60-120, 140-190, 210310, 340-450 and 520 microns, respectively. The spirotheca is fairly thickand is composed of a tectum and innerand outer tectoria in the inner volution
but in the outer ones it consists of atectum, inner and outer tectoria and a
discontinuous thin lighter layer. The
thickness of the spirotheca of the 1st
to the 2nd volution is less than 10
microns and of the 3rd to the 5th volution is 10 to 30 microns, respectively.
The septa are fairly thick and planer
throughout the shell. They bend anteriorly. The septal counts of the 1st
to the 5th volution of a typical specimen illustrated as fig. 5 on PI. 36 (South
Thompson #2-48-b) are 5, 12, 16, 18 andGenus Eostaffella RAUSERCHERNOUSSOVA, 1948
Eostaffella columbiana SADA
& DANNER, n. sp.
PI. 35, figs. 1-8; PI. 36, figs. 1-5

Description :- The shell of Eostaffellacolumbiana SADA & DANNER, n. sp. islarge for the genus and discoidal inshape with subangular to rounded periphery, slightly umbilicated poles andconvex lateral slopes. The mature shellsof five to six volutions are 250 to 370
microns in length and 680 to 950 microns
Table 2.

Measurements of Eostaffella columbiana SADA & DANNER, n. sp.
Radius vector

Slide

PI. fig.

L.

W.

R.

Prol.
1

-

Upper Harper
Ranch 93-a
Upper Harper
Ranch 93-b
Harper Ranch 4-c
Harper Ranch I-aHarper Ranch 4-bSouth Thompson~2-30-a

2

4

3

5

- - - - - - - - - - - - - -- - - -

-

35

1

0.30

0.82

O. 37

O. 06

0.06

0.11

O. 19

O. 28

0.45

35
35
35
35

2
3
6
7

0.37
0.37
0.35
0.36

O. 80
O. 76
O. 78
O. 78

0.46
0.49
0.45
0.46

O. 06
0.05
0.05
0.06

0.05
0.06
0.05
0.06

O. 10
O. 12
0.10
0.11

0.18
O. 19
0.16
0.16

-

0.31
0.27
0.27

0.43
0.41
0.45
0.45

35

4

0.27

0.68

0.40

0.05

0.05

0.09

0.15

0.24

0.36

35
36

5
1

0.23
0.25

0.47
O. 95

0.49
0.26

0.05
0.04

0.05
O. 04

0.06
0.08

0.17
O. 14

0.27
0.21

0.34

6

--

South Thompson~2-26-cHarper Ranch 62-66(Measurements in mm)

O. 52

629.

Pennsylvanian fusulinids from B. C. & Washington

19, respectively. The chomata are distinctly developed_ The tunnel ·anglesof the 1st to the 4th volution are 25, 25,
26 and 27 degrees, respectively, in a
specimen illustrated as fig. 3 on PI. 35(Harper Ranch 4-c).
Remarks :-A large number of thesectioned specimens are referable to thepresent new species. They show a fairly
wide range of variation in the lengthof the axis of coiling and the height ofthe chambers in the outer two or three
volutions. In the general shape of theshell Eostaffella columbiana SADA &DANNER, n. sp. somewhat resembles
Eostaffella circuli which was describedby THOMPSON (1945, pp. 46-47, pI. I, figs.
15-18) from the Pennsylvanian Belden
formation in Northwest Colorado andEast Utah, and by THOMPSON (1948, p.
77, pI. 24, figs. 16-18) from Powwow
Canyon, Hueco Mountain, Texas. However, E. columbiana, n. sp. is distinguished from E. circuli in having larger shell,larger proloculus and more rapid expansion of the shell in the outer volutions.
The present species has a close resemblance to Eostaffella gigantea (KANMERA)(1952, pp. 172-173, pI. 12, figs. 4-14) fromthe Kakisako formation of Southwest
Japan, but they are easily distinguishedby smaller shell of E. columbiana, n. sp.,larger form ratio, smallerproloculus
and thicker spirotheca of the last volution. E. columbiana, n. sp. is somewhat
allied to Eostaffella japonica (KANMERA)(1952, pp.170-172, pI. 11, figs. 1-19: pI.
12, figs. 1-3) from Japan. However, themore slender shell, smaller form ratio
and smaller proloculus of E. japonica
serve to distinguish it from E. columbiana, n. sp. Eostaffella columbiana, n.
sp. resembles Eostaffella britishensis described by Ross (1967, pp. 715-716, pI.
79, figs. 6-10) from locality 2B-15-63-54,
9 miles south of Trout Lake, British

259

Mountains, Yukon. However, the former
species is smaller in size and has smaller
proloculus and smaller form ratio.
Eostaffellacolumbianadiffers from
Eostaffella thompsoni (ANISGARD & CAMPAU) (1963, p. 102, pI. 9, figs. 1-15, pI. 10,
figs. 1-7, pI. 11, figs. 1-4) in that it has
a smaller shell, smaller form ratio,
smaller tunnel angles and larger number of volutions.
Occurrence: - Eostaffella columbiana
was found abundantly at many localities
including: South Thompson #1, South
Thompson ~2, Rayleigh, Aspen Park,
Harper Ranch, Upper Harper Ranch,
Robins Lake ~l, Liumption Ridge, in
British Columbia and Black Mountainin Washington State.

Eostaffella kanmerai (lGo)
PI. 37, figs. 1-3, 5, 18-19

1957. Alillerella kanmerai IGo. Sci. Rep. Tokyo Kyoiku Daigaku, Ser. C, vol. 5,
nos. 47-48, pp. 175-177, pI. I, figs. 2026, pI. 2, fig. 14.
1964. Eostaffella kanmerai, SADA. jour. Sci.
Hiroshima Univ., Ser. C, vol. 4, no. 3,
pp. 230-231, pI. 21, figs. 8, 16-17.
1967. Eostaffella kanmerai, SADA. Trans.
Proc. Palaeont. Soc. japan, N. S. no.
67, pp. 144-145, pI. 2, figs. 1-10.
1969. Eostaffella kanmerai, SADA. Trans.
Proc. Palaeont. Soc. japan, N. S. no.
75, pp. 120-121, pI. 12, figs. 1-13; pI.
13, figs. 1-2.

Description:- The shell of Eostaffellakanmerai (IGO) is discoidal in shapewith subangular to rounded peripheryand depressed at the umbilicated poles.
The lateral slopes are distinctly convex.
Shells with five volutions measure 190
to 230 microns in length and 390 to 680
microns in width, giving the form
ratios of 0.29 to 0.43. The inner volu-K. SADA and W. R. DANNER

260

tions are involute but the last one or
two volutions become partly evolute.
The spherical pro loculus measures 30
to 40 microns in the outside diameter.
The radius vectors of the 1st to the 5th
volution of seven specimens are 40-50,
70-100, 110-130, 190-330 and 280-380
microns, respectively.
The spitotheca is fairly thick in theouter two volutions and consists of atectum and inner and outer tectoria andTable 3.

its thickness of the 1st to' the 5th volution of seven specimens is 10 to 20
microns. The thickness of the proloculus
wall ranges from 10 to 15 microns. The
septa are thin and slightly bent anteriorly. The chomata are low andslightly asymmetrical. The tunnel angles"of the 1st, to the 3rd volution of a
specimen (PI. 37, fig. 1: North McGregor
Creek 11-a) are 20, 24 and 25 degrees,
respectively.

Measurements of Eostaffella kanmerai (IGo).
Radius vector

Slide

Pt fig.

R

W.

Prot
1

2

3

4

5

O. 05
0.04
O. 05
O. 05
O. 05

0.08
0.07
0.10
0.09
O. 09

O. 13
0.11
O. 15
O. 18
O. 18

0,21
0,19
O. 24
O. 31
0.33

O. 30
0.28
0.38

- - - - - - - - - -- -- -- -- -North McGregor CK. ll-a
South Thompson #2-18-b
South Thompson #2-18-aSouth Thompson #2-26-b
South Thompson #2-27-a

L.

37
37
37
37

1
3
2
19

-

-

O. 23
0, 19
O. 20
O. 19
O. 19

0.56
0,56
0.68
0.55
0.58

0.41
0,34
0.29
0.34
0.33

0,04
0,04
O. 03
0.04
O. 04

(Measurements in mm)

Remarks :-Eostaffella kanmerai was
originally described by IGO (1957) fromthe Ichinotani formation in Central
Japan, and then it was described fromthe Pennsylvanian limestones of Atetsu(SADA, 1964) and Taishaku (SADA, 1967,1969) in West Japan. The specimens
described above are quite identical withthe types and the hypotypes of Japanin the shell-shape, the size, the form
ratio, the number of volutions, the expansion of the shell," the spirothecal
thickness, the proloculus diameter, thetunnel angles and the septal counts.
Eostaffella ka?t1nerai somewhat resembles
Eostaffella circuli described from Utah
and Colorado (THOMPSON, 1945, pp. 4647, pI. 1, figs. 15-18) and from Texas(THOMPSON, 1948, p. 77, pI. 24, figs. 1618). However, E. kanmerai can be easily
distinguished from E. circuli, for theformer species has a shorter axial length,
smaller ,form ratio, smaller proloculus,
smaller chomata, higher chambers andfewer, septa for corresponding vol utions,thinner spirotheca and larger tunnel

Explanation of Plate 35
All figures x 100
Figs. 1-8. Eostaffella columbiana SADA & DANNER, n. sp.
1: 'Axial section of the 'holotype: Slide-Upp'er Harper Ranch 93-a.
2-8. - AXla'1 sections of paratypes: Slides-Upper Harper Ranch 93-b, Harper Ranch 4-c,South Thompson #2-30-a, South Thompson #2-26-c, Harper Ranch I-a, Harper Ranch 4-b
and Harper Ranch I-b, respectively.

SADA and DANNER :Pennsylvanian f~~s~dinidsfrorn B. C. & Washington Plate 35

3

5

629.

Pennsylvanian fusulinids from B. C. & Washington

angle.
Occurrence:- Eostaffella kanmerai wascollected at the following localities:
Rayleigh, Harper Ranch, South Thompson #1. South Thompson #2. North
McGregor Creek and Liumption Ridge.
Eostaffella sp. A
PI. 37, figs. 15-17

Descriptive remarks: - The shell of
Eostaffella sp. A is moderate for the
genus and discoidal in shape, having abroadly rounded periphery and slightly
umbilicated poles. The specimen illustrated as fig. 17 on PI. 37 (South Thompson #2-34-a) is 250 microns long and 430
microns wide, giving a form ratio of
0.58. The shell is involute in the inner
volutions but the last one is partly
evolute. The proloculus diameter is
uncertain due to secondary mineralization. The spirotheca is composed of atectum and inner and outer tectoria.
The thickness of the spirotheca of thepenultimate and the last volutions isabout 10 microns. The chomata are
obscure.
In the shell-shape, the number of volutions and some internal characteristicsof the shell, the present species has aresemblance to Eostaffella sp. B described by SADA (1964, pp. 232-233. pI. 21,
figs. 18-20; pI. 22, figs. 5-7) from thePennsylvanian beds of the Atetsu Limestone in West Japan. However, more
perfect specimens are necessary for thedefinite determination of the species.
Occurrence: - Eostaffella sp. A was
obtained from the following localities:
South Thompson #2, Harper Ranch andNorth McGregor Creek.
Eostaffella sp. B

261

PI. 36, figs. 6-7

Descriptive remarks:- W e have obtained a small species referable to the genus
Eostaffella from the Pennsylvanian bedsof the Blind Creek Limestone at Keremeos, B. C. and from the area around
Kamloops, B. C. However, we cannot
determine the accurate specific name,because the specimens are very poor
in preservation. The shell of Eostaffella
sp. B is small and discoidal in shapewith subangular to rounded peripheryand convex lateral slopes. The shell
ill ustrated as fig. 7 on PI. 36 (Keremeos,
B. C. S. W. 2-3-a) is 80 microns in lengthand 210 microns in width, giving a form
ratio of 0.38. The inner volutions are
involute but the last one becomes partially evolute. The proloculus diameterand the radius vectors are uncertain
due to the poor preservation of theshell. The spirotheca is composed of atectum and inner and outer tectoria,
and the spirothecal thickness of the last
volution is about 10 microns. The chomata are indistinctly developed.
Occurrence:- Eostaffella sp. B is common in the following localities: South
Thompson #1, South Thompson #2, Harper Ranch and Keremeos Limestone.

Family Staffellidae MIKLUKHOMAKLAY, 1949
Genus Nankinella LEE, 1933
Nankinella plummeri THOMPSON
PI. 37, fig. 41947. Nankinella plummeri TilOMPSON. Jour.
Paleont., vol. 21,pp. 155-157, pI. 32,
figs. 11-16; pI. 33, figs. 10-11.
1957. Nankinella plummeri, Ico. Sci. Rep.
Tokyo Kyoiku Daigaku, Ser. C, vol. 5,
nos. 47-48, p. 183, pI. 3, fig. 4.
1961. Nankinella plummeri, SADA. Jour. Sci.

262

K. SADA and W. R. DANNER
Hiroshima Univ., Ser. C, vol. 4, no. 1,
pp. 107-109, pI. 10, figs. 22-25.

Description:- The shell of N ankinella
plummeri THOMPSON is minute and discoidal in shape, having the angularperiphery in maturity, convex lateralslopes and slightly umbilicated poles.
The mature shell of six volutions illustrated as fig. 4 on PI. 37 is 450 microns
in length and 1050 microns in width.
The form ratio is 0.43. The outside
diameter of the proloculus is 50 microns.
The radius vectors of the 1st to· the 6th
volution of the illustrated specimen are
60, 100, 180, 260, 400 and 600 microns,
respectively. The spirothecal thicknessof. the outer volutions is less than 30
microns. The spirotheca is composedof three layers. The chomata are low.
Their tunnel sides are steep and poleward slopes are very gentle. The tunnel angles of the 3rd to the 5th volution are 16, 17 and 18 degrees, respectively.
Remarks :.-In the shell-shape, the form
ratio, the height of the chambers, thefeatures of the chQmata, and the number of volutions, the present form
closely resembles Nankinella plu,mmeri
described by THOMPSON (1947) from the
Marble Falls limestone, Llano Uplift,
Texas. They may be conspecific.

Occurrence:- Nankinella plummeri wascollected from the following localities:
Upper Harper Ranch, Robins Lake andMount Constitution on Orcas Island.

Subfamily Eoschubertellinae
SKINNER. 1931
Genus Eoschubertella THOMPSON, 1937
Eoschubertella ? sp.
PI. 37, fig. 13

Description:-The shell of Eoschubertella? sp. is small for the genus andinflated fusiform in shape and has
bluntly pointed polar ends and straightaxis of coiling. The shell of the specimen illustrated as fig. 13 on PI. 37 (Westside of Horne Lake, Vancouver Island 516 (V. 1.-1)) is 600 microns in length and
450 microns in width. The form ratio·is 1.32. The proloculus of the shell isinvisible due to the secondary mineralization. The spirotheca is composedof a tectum and inner and outer tectoria. The spirothecal thickness measures about 20 microns in the penultimate and ultimate volutions. The chomata are distinct in all but the last
volution. The tunnel'sides of the chomata are nearly vertical but the pole-

Explanation of Plate 36
All figures x 100
Figs. 1~5. Eostaffella columbiana SADA & DANNER, n. sp.
1, 3. Axial sections of paratypes: Slides-Harper Ranch 62-66 and South Thompson:112-54, respectively.
2, 4-5. Sagittal sections of paratypes: Slides-Upper Harper Ranch 93-c, South Thompson :112-26-a and South Thompson :112-48-b, respectively.
Figs. 6-7. Eostaffella sp. B
6-7. Axial sections: Slides.Keremeos B. C. S. W. 2-4-a and Keremeos B. C. S. W. 2-3-a.
respectively ...
Fig. 8. Endothyranopsis? sp.
8; Axial section: Slide-Harper Ranch 25-2-b.

SADA and DANNER: Pennsylvanian fusulinids from B. C. & Washington

Plate 36

629.

Pennsylvanian f1Lsulinids from B. C. & Washington

ward slopes are gentle. The tunnel.angle is about 20 degrees in the penultimate volution.
Remarks :-The present species is incompletely known owing to the scantiness of the material and it is difficult
to determine the generic affinities withcertainty. In the general shell-shape:and some internal characteristics of theshell, however, the single specimen described above has similarities to species
placed in Eoschubertella. So we refer
it to that genus with question as Eoschubertella? sp. The specific comparison
will be postponed until more information is obtained.
Occurrence: - Eoschubertella? sp. iscommon in the Pennsylvanian rocks at
the westside of Horne Lake on Vancouver Island.

Family Endothyridae BRADY, 1884
Subfamily Endothyranopsinae
REYTLINGER, 1958
Genus Endothyranopsis CUMMINGS, 1955
Endothyranopsis ? sp.
PI. 36, fig. 8

Description:- The shell of Endothyranopsis? sp. is large and subglobular
in shape with broad and rounded periphery and depressed umbilicated poles.
The axis of coiling rotates in the inner
volutions. The specimen (Harper Ranch
25-2-b) illustrated as fig. 8 on PI. 36 is
50 microns long and 70 microns wide.
The shell is tightly coiled in the inner
volutions but rapidly expands in thelast volution. The proloculus is small
and its outside diameter measures 4
microns. The spirotheca is thin andconsists of a tectum and inner and263

outer layers composed of granules ofcalcite bounded by calcareous cement.
Remarks:-The present species has
similarities to the type species of genus
Endothyranopsis, E. crassa BRADY, in
the general shell-shape and some internal characteristics. However, the present species differs from the typespecies in having three layered wallcomposed of a distinct tectum and innerand outer layers which consist of granules of calcite bounded by calcareous
cements. Therefore, the present species
is referred to the genus Endothyranopsis
with question.
Occurrence:- Endothyranopsis? sp. was
obtained from the following localities:
South Thompson #2 and Harper Ranch.
References
ANISGARD, H. W. & CAMPAU, D. E. (1963):
Paramillerella thompsoni, n. sp. from
Michigan and a redefinition of Paramillerella. Contr. Cushman Found. Foram.
Res., vol. 14, pp. 99-108, pIs. 10-11.
COCKFIELD, W. E. (1948):
Geology andmineral deposits of Nicola. Map-Area,
British Columbia.
Mem. Geol. Surv.,
Canada 249, pp. 1-164.
CUMI\I1!'\GS, R. H. (1955): New genera offoraminifera from the British lower
Carboniferous. jour. Washington Acad.
Sci., 45, pp. 1-7.
DANNER, W. R. (1960): An introduction to
the stratigraphy of southwestern British
Columbia and northwestern Washington.
Gu idbook for Geological Field Trips insouthwestern British Columbia. Vancouver
Geological Discussion Club, pp. 1-6. (Univ.
of B. C. Geological Reports No.1, W. H.
MATHEWS, editor).
- - (1965): Limestone of the western Cordilleran eugeosyncline of southwestern
British Columbia, western Washington
and northern Oregon. Dr. D. N. Wadia
Commemorative Volume, Mining & Metallurgical Institute of India, pp. 113-125.

264

K. SADA and W. R. DANNER(1966): Limestone resources of western
Washington. Bull. 52, State Washington
Div. Mines Ceol., pp. 1-474.
- - (1970a): Carboniferous System of thewestern Cordillera of south-western
British Columbia and north-western
Washington. Compte Rendu 6e Congres
Internat. Strat. Ceo!. Carboni/., vol. 11,
pp. 599-608.
- - ~1970b): Paleontologic and stratigraphic evidence for and against sea floor
spreading and opening and closing oceansin the Pacific Northwest. Ceol. Soc.
America Abs. with Programs, vol. 2, no.
2, pp. 84-85.
DOUGLASS, R. C. (1971):
Pennsylvanian
fusulinids from southeastern Alaska.
U. S. Ceol. Survey Pro/. Paper 706, pp.
1-20, pis. 1-7.
HARBAUGH, J. W. (1955) : Unpublished thesis.
University of Wisconsin.
IGo, H. (1957): Fusulinids of Fukuji, southern part of the Hida Massif, central
Japan. Sci. Rep. Tokyo Kyoiku Daigaku,
Ser. C, vol. 5, pp. 153-246, pis. 1-15.
KANMERA, K. (1952): The lower Carboni-ferous Kakisako formation of southern
Kyushu, with a description of somecorals and fusulinids. Mem. Fac. Sci.
Kyushu Univ., Ser. D, vol. 3, pp. 157177, pis. 8-12.
MO:'\GER, J. W. H. (1966): The stratigraphy
and structure of the type-area of theChilliwack Group, southwestern British
Columbia. Unpublished Ph. D. Thesis,
University of British Columbia.
- - & Ross, C. A. (1971): Distribution offusulinaceans in the western CanadianCordillera. Canadian Jour. Earth Sciences,vol. 8, no. 2, pp. 259-278.
MOORE, W. L. (1964): Note on the morphology and taxonomic position of thefusulinid Millerella marblensis THOMPSON. Jour. Paleont., vol. 38, pp. 294-305,
pis. 47-48.
RICH, M. (1961): Stratigraphic section andfusulinids of the Bird Spring formationnear Lee Canyon, Clark County, Nevada.
Ibid., vol. 35, pp. 1159-1180, pI. 5.
Ross, C. A. (1967): Late Paleozoic fusulinids
from northern Yukon Territory. Ibid.,
vol. 41, pp. 709-725, pis. 79-86.

Explanation of Plate 37
All figures x 100 except for Figs. 4 and 12
Figs. 1-3, 5, 18-19. Eostaffella kanmerai (IGo)
1-3, 18-19. Axial sections: Slides-North McGregor Creek 11-a, South Thompson :lf2-18-a,
South Thompson #2-18-b, South Thompson #2-42-a and South Thompson :lf2-26-b,
respectively.
5. Sagittal section: Slide-Harper Ranch I-c.
Fig. 4. Nankinella plummeri THOMPSON
4. Axial section: Slide-Mount Constitution, Orcas Is. OI-30F. x 50.
Figs. 6-12, 14. Millerella marblensis THOMPSON
6-10, 14. Axial sections: Slides-Harper Ranch 67-68, Mount Constitution, Orcas Island
0I-30F, South Thompson :lf2-39-a, Harper Ranch 67-72-b, Harper Ranch 25-2-a andRobins Lake 48-48d, respectively.
11-12. Sagittal sections: Slides-South Thompson #2-52-a and South Thompson :lf2-48-a,
respectively.
Figs. 15-17. Eostaffella sp. A
15-17. Axial sections: Slides-North McGregor Creek 11-b, Harper Ranch 67-72-a andSouth Thompson :lf2-34-a, respectively.
Fig. 13. Eoschubertella? sp.
13. Axial section: Slide-West Side Horne Lake Vancouver Island 5-16(V. 1. -1) x 51. 6.
Fig. 20. Endothyra sp.
Slide-North McGregor Creek ll-c.

SA DA and DA NNER:

5

Pennsylvanian fus~~linidsfro?n B. C. & Wa shington

Plate 37

629.

Pennsylvanian fusulinids from B. C. & Washington& SABINS, F. F. (1965): Early and middle Pennsylvanian fusulinids from southeastern Arizona. Ibid., vol. 39, pp. 173209, pis. 21-28.
& TYRRELL, W. W. (1965): Pennsylvanian and Permian fusulinids from theWheststone Mountains, southeast Arizona. Ibid., vol. 39, pp. 615-635, pis. 75-78.
SADA, K. (1961): Profusu/inella of Atetsu
Limestone. Jour. Sci. Hiroshima Univ.,
Ser. C, vol. 4, no. 1, pp. 95-116, pis. 9-10.
- - (1964): Carboniferous and Lower Permian fusulines of the Atetsu Limestone
in West Japan. Ibid., vol. 4, pp. 225-269,
pis. 21-28.
- - (1965):
Carboniferous and Permianstratigraphy of the Atetsu Limestone inWest Japan. Ibid., vol. 5, no. 1, pp. 2180.
- - (1967): Fusulinids of the .Mil/erel/azone of the Taishaku Limestone (Studiesof the stratigraphy and the microfossil
faunas of the Carboniferous and Permian
Taishaku Limestone in West Japan, No.
1). Trans. Proc. Palaeont. Soc. Japan, N.S.,
no. 67, pp. 139-147, pis. 12-13.
- - (1969):
Microfossils of the lowest
part of the Taishaku Limestone (Ditto,
No.4). Ibid., no. 75, pp. 119-129, pis.
12, 13.
- - & DANNER, W. R. (1973): Late Lower
Carboniferous Eostaffella and Hexaphyllia
from central Oregon. Ibid., no. 91, pp.
151-160, pis. 23, 24.
SKINNER, J. W. (1931): Primitive fusulinidsof the Mid-Continent region. Jour. Paleont., vol. 5, pp. 253-259, pI. 30.
& WILDE, G. L. (1954): Fusulinid wall
structure. Ibid., vol. 28, pp. 445-451, pis.
46-52.
- - & WILDE, G. L. (1965): Permian biostratigraphy and fusulinid faunas of
Shasta Lake area, northern California.
Univ. Kansas Paleont. Contr., Protozoa,
Article 6, pp. 1-98.

265- - & WILDE, G. L. (1966): Permian fusulinids from Pacific Northwest and Alaska. Univ. Kansas Paleont. Contr., Paper
No.4, pp. 1-64, pis. 1-49.
SMITH, S. (1935): Two anthracolithic corals
from British Columbia and related
species from the Tethys. Jour. Pa/eont.,
vol. 9, no. 1, pp. 30-42.
THO:l.IPSO:-1, M. L. (1937): Fusulinid of thesubfamily Schubertellinae. Ibid., vol. 11,
pp. 118-125, pI. 22.
- - (1342): New genera of Pennsylvanian
fusulinids. Am. Jour. Sci., vol. 240, pp.
403-420, pis. 1-3.
- - (1944): Pennsylvanian Morrowan rocks
and fusulinids of Kansas. Kansas Ceol.
Survey, Bu/l. 52, pp. 409-431, pis. 1-2.
- - (1945): Pennsylvanian rocks and fusulinids of east Utah and northwest Colorado correlated with Kansas section.
Ibid., 60, pp. 17-84, pis. 1-6.
- - (1947): Stratigraphy and fusulinids of
Pre-Desmoinesian Pennsylvanian rocks,
Llano Uplift, Texas. Jour. Paleont., vol.
21, pp. 147-164, pis. 31-33.
- - (1948): Studies of American fusulinids.

Univ. Kansas, Paleont. Contr. Protozoa,
Art. 1, pp. 1-84, pis. 1-38.
- - (1951): New genera of fusulinid foraminifera. Contr. Cushman Found. Foram.
Res., vol. 11, pt. 4, pp. 115-119, pis. 1314.
- - (1965): Pennsylvanian and early Permian fusulinids from Fort St. Jamesarea, British Columbia, Canada. Jour.
Pa/eont., vol. 39, pp. 224-234, pis. 33-35.
- - , PITRAT, C. W. & SANDERSON, G. A.
(1953): Primitive Cache Creek fusulinids
from central British Columbia. Ibid.,
vol. 27, pp. 545-552, pis. 57-58.
YOLE, R. W. (1963):
An early Permian
fauna from Vancouver Island, British
Columbia. Bull. Canada Petrol. Ceol.,
vol. 11, no. 2, pp. 138-149.

Trans. Proc.· Palaeont. Soc. Japan, N. S., No. 93, pp. 266-285, pIs. 38, 39, April 20, 1974

630.

MOLLUSCAN FOSSILS FROM THE MIOCENE EOIL
FORMATION, GAMPO AND ULSAN DISTRICTS,
SOUTHEASTERN-SIDE OF KOREA *BONG KYUN KIM
Department of Geology, Seoul National University, Korea

HIROSHI NODA
Institute of Geology and· Paleontology, Faculty of Science,
Tohoku University, JapanandSUN YOON
Department of Geology, Busan National University, Korea~OO*i¥illllitim, ift.lJtl!!.~O)~fJftit~ i31111t~{t:Plr: "?1t'-C: ~OO*i¥illll, ~(Wj~tiiit~~~~~~~~i¥iiiift.lJ~~K • • ~~~i3I111tWO)rut:p16.~.IU~, i3*O)~llII~
fkt!!:~lfO) Arcid·Potamid fauna cffJ\~:f1,~~!Ull.nx:cjhiJi~~;: c ~~~/JPt-:o~!i.jf;j·!BflIlmWJ·~~

underlying the Eoil Formation, both of
the Changgi Group. According to HUZIOKA (1972) the Changgi Flora corresponds to the Aniai type flora in northeastern Honshu, Japan. Beside theabove, some species of molluscan fossil
common between Japan and Korea havebeen known from the paleontologicalworks of T ATEIW A (1924), KANEHARA(1936a, b), MAKIYAMA (1926, 1936), HATAI
and NISIYAMA (1938), HATAI and KoTAKA (1952), KIM (1970) and HUZIOKA(1972). However, the biostratigraphy,
especially of the Neogene molluscs, hasremained untouched. The potamid-arcid
species herein described for the firsttime were collected from the Eoil Formation in the Gampo and Ulsan districts.
These fossils are significant for the

Introduction
The Eoil Formation, of which marine
molluscs are treated in this article, isdistributed in the Gampo and Ulsan
districts on south to southwest of
Yeongil Bay or the southeastern coast of
the Korean Peninsula. This formationand the other Neogene deposits are distributed in small areas of the Korean
Peninsula. The record of some plantand marine molluscan fossils are due
to TATEIWA (1924), KANEHARA (1936a,b) and KIM (1970). Recently, HUZIOKA(1972) stated that the fossil plants,
named by him the Changgi Flora, wascollected from the Keumkwandong Shale* Received June 23, 1973: read June 23,
1973 at Niigata.

266

630.

Molluscan fossils from Korea

correlation of the formations distributed
in southeastern Korea and also withthose in Japan. for their indicating the
Early Middle Miocene age in Korea,
and also for revealing the paleogeo·
graphy of the Asiatic borderland atthat time.

Acknowledgments
The writers express their hearty
thanks to Dr. Kotora HATAI, Professor
Emeritus of the Tohoku University forhis continuous encouragement and supervision during the present study. Deep
.appreciation is due to Professor Tamio
KOTAKA of the Institute of Geology andPaleontology, Faculty of Science, Tohoku University for his kind suggestions.and discussions on the biostratigraphyof Korea and Japan. Thanks are ex·tended to Mr. Kimiji KUMAGAI of the
Tohoku University for his photographic
work.

Geological notes on the occurrenceof molluscan fossils
T ATEIWA (1924) seems to have been
the first geologist to study the geology.around area of the present fossil loco
alities. He classified the rocks stratigraphically into the Ch6ki (Janggi),
Poumgongni (Beomgogri) and Ennichi(Yeonil) groups in ascending order in
his geological maps of the ChOy6 (Gam·po), Kyuryuho (Guryongpo) and Ennichi(Yeonil) sheets in the scale of 1: 50,000,.and their explanation text. The groups
were cut into finer stratigraphic units
based upon their lithology (Table 1).
Subsequently, the northern part ofGampo district was restudied by KIM(1970) for the purpose analysing and267

determining the sequence of the for·aminiferal fauna of the Neogene formations. During his geological survey,
KIM (1970) collected some interestingfossil molluscs from the Eoil Formation
but they were neither described nor
discussed. Some of the fossil molluscs
listed by TATEIWA (1924) and Vicaryacallosa recorded by KANEHARA (1936b)
were probably from near the locality
no. 1 of the writers. To determine theexact horizon of the fossil molluscs andto know their mode of occurrence,
therefore, the stratigraphy of the area
was made and the geological notes of
the Gampo district are given in the following lines.
The stratigraphic succession of the
Gampo district can be classified into theCretaceous Black Shale, Felsophyre, Granite porphyry, Miocene Gampo Conglomerate, Hyodongri Volcanics and Eoil
Formation in ascending order. The
Miocene formations are included into
the Janggi Group which covers theCretaceous rocks (Bulgugsa Series)
with unconformity. The Gampo Conglomerate, the basal part of the JanggiGroup, is composed mainly of wellrounded pebbles of the basement rocks
and of gray coarse· to medium· grainedsandstone with thin intercalations ofdark gray carbonaceous shale and whitetuffs. The Gampo Conglomerate about
600 meters in thickness, resembles inlithology, especially in containing similar
kind of gravels, the Janggi Conglomerate which is distributed mainly in the
Yeonil district. The shale intercalated
in the Gampo Conglomerate has yielded
abundant plant fossils as mentioned
already by TATEIWA (1924) and KANEHARA (1936a) and the flora according to
HUZIOKA is similar to the Aniai typeflora distributed in northeastern Honshu.
Japan.

268

B. K. KIM, H. NODA and S. YOON

Table 1.

Stratigraphic relationship between the geological maps of Kyiiryiiho (Guryongpo),
Ennichi (Yeonil) and Choyo (Gampo) published by TATEIWA (1924).
Kyuryiiho(Guryongpo)

Iseriesbrouptl-Ennichi(Yeonil)iI

ChOyo(Gampo)I

Ennichi Basalt andEnnichi Basalt andEnnichi Basalt
two Pyroxene Andesite two Pyroxene Andesite I
07 _ _ - --Unconformi t y - - ----Unconformity--- --Unconformity-~..... >.

"' ...

::l'"

-Ben
.-

Ennichi Shale
Sempoku Conglomerate

QJ

1::'I:: ...

(l:1~

Changam Andesite andits Tuff

Poumgongni Andesite
and its Tuff
Chinjyoundong Andesite
and its Tuff
Manghaisan Andesite
and its Tuff
Pangsailni Perlite
Kalpyoundong Breccia
Y ongdongni Tuff

0.
::l

...

0

c.!l

'cbO
I::
0

Chang am Perlite

bO

a

::l

a

0

Il.

QJ

.....

en

en

m

>.

.-... - -

>.

m

QJ

QJ

...

Upper basaltic Tuff
Keumori andestic Tuff
Upper coal bearing
Formation
Lower basaltic Tuff
Lower coal bearing
Formation
Kyiiryiiho Andesite

.!<:
0

.c

0.
::l

U

E-<

...

0

c.!l

:;;;
0

.c
U

I

Poumgongni Andesite
and its Tuff

Kalpyoundong Breccia
Y ongdongni Tuff
Andongni Conglomerate
Oaeumni andestic Tuff

~Unconformity-- ~-Ullconformity-- ~-Unconformity-~.-.....'..." .QJ

Sempoku Conglomerate- - -~----~~-------- ~-Unconformity-~ --Unconformity-- - -Upper basaltic Tuff
Keumori andestic Tuff
Upper coal bearing
Formation
Lower basaltic Tuff
Lower coal bearing
Formation
Keumgoangdong Shale
Sinjyoungdong Andesite
Nultairi Trachyte
Nultairi Trachyte Tuff
ChOki Conglomerate

Auil Formation andAuil Basalt

Hyotongni Volcanic
Rocks

Nultairi Trachyte
Nultairi Trachyte Tuff
Kampo Conglomerate
ChOki Conglomeratey-- ---Unconformity--- ---unconformitY~-I-----unconformity~~;;0.
Hasouri andestic Tuff
O::l

I

eno
...
::t:c.!lI Hasouri Andesite'"

Cretaceous
System4

I_____ ;_______ ;__FU:~O~::-~ Fukkokuji GroupThe Hyodongri Volcanics distributedin the southwestern corner of the areastudied consists of andesite lava andits tuff or tuff breccia. The Hyodongri
Volcanics cover directly the Cretaceous
black shale and granite porphyry with--Unconformity---

IFukkokuji Groupunconformity and without the development of the Gampo Conglomerate whichthins out towards the southwestern corner of the area mapped. The stratigraphic relationship between the Gampo
Conglomerate and the Volcanics is not630. Molluscan fossils from Korea

269

N

YEONGILBAY

LEGEND
~ 1

~9

~2
~3

L:?;.:::j 4[ITffi 5

I§§ 6
~7

BB

[]I]J10~11~

R' .;'y112
*-

o

5

10 Km

13

Text·fig. 1. Index map and fossil localities of the Gampo and Ulsan districts. Geological map from KIM (1970). 1: Pohang Formation, 2: Idong Formation, 3: Daegog Formation, 4: Songhagdong Formation, 5: Seoam Conglomerate (Cheonbug Conglomerate), 6:
Eoil Formation, 7: Janggi Conglomerate, 8: Mesozoic sedimentary rocks, 9: Hwabongri
Formation, 10: Coal bearing formation of Eoil Formation, 11: Tertiary igneous rocks, 12:Mesozoic igneous rocks, 13: Fossil locality.

270

B. K. KIM, H. NODA and S. YOON

clear because of their being distributed
in separated areas. Accordingly, thestratigraphic situation of the Hyodongri
Volcanics is due to the relationship between the Janggi Conglomerate andNuldaeri Volcanics in the neighbouring
north of the Yeonil district. The Hyo<iongri Volcanics lithologically may
correspond to the N uldaeri Volcanics
which are superposed on the Janggi
Conglomerate with unconformity around
Yeongil Bay (TATEIWA, 1924).
The Eoil Formation lies on the Hyo<iongri Volcanics with conformity andon the Cretaceous granite porphyry

Formation

Lithic characterswith unconformity at the eastern sideof the present area, but comes into contact with the Cretaceous rocks andHyodongri Volcanics with fault trending
NE-SW at the southern side. The formation is distributed zonally from thesouthwest of Jugjeon-ri to the northeastof Eoil (Fig. 1). The formation is composed mainly of coarse-grained sandstone and conglomerate intercalatedwith three sheets of basalt lava flow,
namely at the basal part, in the lower
middle part, and in the upper part of
the formation (Fig. 2). Except for thebasalt lavas, the Eoil Formation is some-SectionUpper basalt

(m)

10+

Eoil

Remarks

Sandstone

Formation
Arcid-Potamid. ..........
'. .
:: .....:. . . '.

'".

Hyondongri
Volcanics:'-::-.-: ___.... '.
'

Campo
Conglomerate

Basement

6

Sandstone

1.5

Os/rea-bed

12

Os/ rea-bearing
siltstone

15 +Sandstone,',.

.... -.

Text-fig. 2. Stratigraphic sequence of the formations in the area of Gampo,
showing the stratigraphic horizon of the molluscan fossils.

times intercalated with conglomerates,
sandy shales, siltstones, tuffs and somethin lignite beds. The siltstones andtuffs generally contain plant fossils thathave been studied by HUZIOKA (1972)
and named by him the Changgi Flora.
The formation is judged to attain athickness of more than 800 meters, because its upper part is cut by a fault
at eastern part of the field. The molluscan fossils discussed in the present
article were collected from the middle

part of the Eoil Formation (Figs. 1 and
2). T ATEIW A (1924) collected from theconglomerate bed molluscan fossils(KANEHARA, 1936a), such as Natiea sp.,
Cerithium sp .. Area sp., Peetunclus sp.,Ostrea sp., Dosinia sp. and Solen sp.
The stratigraphical position of the
newly collected arcid-potamid fauna isjust above the second basalt lava sheet
exposed in the road cliff between Songjeon-ri and Jugjeon-ri (Loc. no. 1, Fig.
1). As shown in the columnar section

630.

Molluscan fossils from Korea(Fig. 2), the fossils were collected fromtwo different stratigraphic horizons of
the same cliff; the lower bed consistedof gray tuffaceous siltstone yielded
mainly Crassostrea gravitesta eoilensis,
n. subsp., and the upper one situated atabout 10 meters above the lower bed,
consists of hard, massive pale gray,poorly sorted, tuffaceous sandstone withs\lch characteristic species as Vicaryacallosa japonica, Cerithium sp. (d. kanpokuensis), Anadara kiiensis, Anadara
kakehataensis,
Clementia
nakamurai,
Cyclina japonica and others (Table 2).
The sandstone bed of about 10 metersin thickness inserted between the fossiliferous siltstone and sandstone mentioned above is non-fossiliferous.
The characteristic marine molluscan-

Table 2.
Species271

fossils mentioned above have been foundcommonly in the Middle Miocene deposits distributed along the borderlandof the Japan Sea (NOD A, 1973).
Since the above stated characteristicmolluscs bearing formations are distributed in separated sedimentary basins
in Korea (KIM, 1970) (Fig. 1), they havebeen given different formation names_
But from the similar lithostratigraphic
order of succession and yield of thesame arcid-potamid fauna such as
Vicarya callosa japonica, Vicaryellaishiiana, Anadara Iwkehataensis, Dosinia
nomurai, Cyclina japonica, Clementia
nakamurai, Soletellina minoensis andothers (Table 2), the Eoil Formation in
the north and the Jeongjari Conglomerate in the south should be correlated---

Molluscan fossils from the Eoil Formation.
Localities

I no. 1

Anadara (Anadara) kiiensis MIZUNO
Anadara (Hataiarca) daitokudoensis (MAKIYAMA)I
Anadara (Hataiarca) kakehataensis RATAI and NISIYA:VIA I
Glycymeris sp.
Crassostrea gravitesta eoilensis KIM, NODA
and YOON, n. subsp.
" Ostrea" sp.
Thyasira sp.
Dosinia (Phacosoma) nomurai OTUKA
Cyclina (Cyclina) japonica KAMADA
Clementia (Clementia) nakamurai OTCKA
Soletellina minoensis YOKOYAMA
Panope d. nomurae KAMADA
Vicarya (Shoshiroia) callosa japonica YABE and RATAI
Vicaryella ishiiana (YOKOYAMA)
Vicaryella sp.
Cerithidea sp. (d. kanpokuensis MAKIY AMA)

no. I-I! no. 2
I

+
+
+

no. 3

+

+
+

+
+
+
+

+
+
+
+
+

+

+
+

+
+
+
+
+
+
I
I

+

+
+

Loc. no. 1: South of Songjeon-ri, Yangbug-myeon, Weolseong-gun, Gyeongsangbug-do.
Loc. no. 1-1: About 6 meters below at the same locality of no. 1.
Loc. no. 2: About 3 km west of Jeongja-ri, Gangdong-myeon, Ulju-gun, Gyeongsangbug-do.
Loc. no. 3: About 1 km east of Jangmyeong-gol, Sinhyeon-ri, Gangdong-myeon, Ulju.gun,
Gyeongsangbug-do.

272

B. K. KIM. H. NODA and S. YOON

are distributed along the eastern borderland of the japan Sea except the Yoshino and Asagawa formations. Amongthe molluscan species of the Eoil Formation, Anadara kiiensis, Anadara kakehataensis and Anadara daitokudoensis
are particularly important because they
are the representative forms of theNatorian of HATAI (1962) and also because they usually occur in association
with the Vicarya- Vicaryella species
Remarks on the molluscan fauna
which have equal biostratigraphicalof the Eoil Formation
value. Those Anadara species like the
The molluscan fauna collected fromtwo gastropod genera just mentioned
three isolated localities (Fig. 1) of theare restricted in their geological distriEoilo Formation consists of 9 pelecypod
butions. The occurrence of Anadara
and 4 gastropod species. The preservakakehataensis, Anadara kiiensis andAnadara daitokudoensis refer them totion of the fossils are rather good eve?
the zone of Anadara kakehataensisthough they were collected from a pale
Anadara makiyamai of NODA (1966) ingray, poorly sorted, tuffaceous sandstone
with plant fragments. The molluscan
terms of anadaran biostratigraphy. Tl:lefauna although a small one, is importantanadarid zone was correlated by NODA
(1966) with the stage II of KITAMURA
for the age determination and correla(1959), Nanaochlamys notoensis Assemtion of the formation with other areas,
blage zone of MASUDA (1962a), Turritella
and the assemblage serves for the inters-hataii zone of KOTAKA (1959) and thepretation of the paleoecological conditions under which the formation was
Natorian of HATAI (1962).
Beside the anadarids, Cyclina japonica,
deposited.
Clementia nakamurai, Dosinia nomurai,
The fauna of the Eoil Formation
Soletellina minoensis. Vicarya callosa
is characterized by Vicarya-Anadarajaponica. Vicaryella ishiiana, Cerithium
species (Potamid-Arcid Fauna of TSUDA,
kanpokuensis usually occur in associa1965) and the assemblage resembles thatof the formations which yielded thetion with the arcid-potamid fauna injapan (NODA, 1973). The vicaryan gasVicarya-Anadara species in the japaneseIslands (NODA, 1973), namely the Yoshitropods from the Eoil Formation are
identified with Vicarya callosa japonica
no Formation in Okayama Prefecture,
Kunimi Formation in Fukui Prefecture, - YABE and HATAI and Vicaryella ishiiana(YOKOYAMA), species that are known
Higashi-Innai Formation in Ishikawa
from the Natorian formations cited in
Prefecture, Kurosedani Formation in
Toyama Prefecture, Tsugawa and Orito
earlier lines. From the assemblage offormations in Niigata Prefecture, Oyama
the Eoil Fauna, the Eoil Formation is
Formation in Yamagata Prefecture, Asainferred to belong to the same paleogawa Formation in Ibaraki Prefecture,geographical province as the formations
Tanosawa Formation in Aomori Prefecmentioned above.
ture and Tsurikake Formation in HokSome species such as Anadara daitokaido. All of these stratigraphic units
kudoensis, Clementia nakamurai, Cyclina
with each other (Loc. nos. 2 and 3 inFig. 1). This correlation will contributeto the interpretation of the geologicalproblems of the Tertiary System in
Korea and also serve to make clear the
relation between the Tertiary deposits
distributed on opposite sides of theJapan Sea.

630.

Molluscan fossils from Korea

japonica and Soletellina minoensis were
found with conjoined valves in natural
position and some specimens of Vicarya
and Vicaryella are provided with wellpreserved tubercles. From the state ofpreservation of the fossils in the Gampo
and Ulsan districts, the Eoil fauna may
be ~{l.ns-idered to have been autochthonous and probably the molluscs lived
under a rather warm water embaymental
condition.
The present description is the first of
the Vicarya-Anadara fauna from the
Eoil Formation from the Gampo district,though KIM (1970) recorded some speciesof the arcid-potamid without discussion
or description. The present writers discriminated an arcid-potamid fauna suchas Vicarya callosa japonica, Vicaryellaishiiana, Anadara kakehataensis, Cyclina
japonica, Dosinia japonica, Clementia
nakamurai, Soletellina minoensis from aformation that corresponds to the Eoil
Formation at ]eongjari in the northeastern part of Ulsan (Fig. 1). Thus
the geographical distribution of thearcid-potamid fauna along the easternside of the Korean Peninsula seems toform a key to the geological correlation,
paleogeography and paleooceanography.
And here it should be added that thebiostratigraphic relationship between
the Neogene of the northern and southern parts of the Korean Peninsula still
remain to be worked out.

Descriptions of species
Genus Anadara GRAY, 1846
Subgenus Anadara s. s.
Anadara (Anadara) kiiensis

Area d. eamu/oensis, YOKOYAMA, 1929, p.
368, pI. 70, figs. Sa-c.
Anadara (Pectin area) kiiensis Mrzc);o, 1953,
p. 16, figs. Sa, 5b.
Anadara (Anadara) kiiensis Mrzu;--;o, NODA,
1966, p. 92-93, pI. 6, figs. 13-15.

The present species was originallydescribed from the Miocene Mitsuno
Formation in Wakayama Prefecture by
MIZUNO in 1953 based upon immatureforms. Subsequently NODA (1966) reported on the adult forms from the
Miocene Yoshino Formation in Okayama
Prefecture.
The present species is characterizedby having 28 non-dichotomous radialribs, squarish in cross section with granules on the anterior side, without aposterior depressed area, convex andswollen umbonal area, incurved beakand narrow triangular ligamental areawith chevron-shaped grooves.
Kiiensis resembles Anadara (Hataiarca)
kakehataensis HAT AI and NISIY AMA(1949) originally described from the
Miocene Kurosedani Formation in Toyama Prefecture in the swollen form andcharacteristic radial ribs but the latterhas strongly depressed area along theposterior side. Anadara makiyamai HATAl and NISIYAMA (1938) from the Miocene Heiroku Formation in North Korea
resembles the present species but theformer differs from the latter by having 24-25 radial ribs and· flatly narrowumbonal area.
Anadara ninohensis(OTUKA, 1934) is similar to the present
species in the non-dichotomous radialribs arid rather squarish, 28-30 radialribs, but the latter has wider swollen,
convex umbonal area and inclined beak.
Locality and Formation:-Loc. no. 1,
Eoil Formation.

MIZUNO, 1953
PI. 38, figs. la, 1b, 11273

Subgenus Hataiarca NODA, 1966

274

B. K. KIM, H. NODA and S. YOON

Anadara (Hataiarca) daitokudoensis(MAKIYAMA, 1926)
Pl. 3~ figs. 8a, 8b, 12
Area (Anadara) daitokudoensis MAKIY AMA,
1926, p. 153-154, pI. 12, figs. 10, 14, 15.
Anadara daitokudoensis MAKIY AMA, MAKIY AM A, 1936, p. 205; OTUKA, 1938b, p. 25,
pI. 1, figs. 3-4.
Anadara (Hataiarca) daitokudoensis (MAKI'
YAMA), NODA, 1966, p. 115-116, pI. 7, fig.

13.

The present species was originallydescribed from Miocene Heiroku Formation in North Korea by MAKIY AMA in
1926. It is characterized by the depressed area along the posterior side of
the shell extending from near the beakto the ventral margin, 27-28 strongly
elevated, non-dichotomous radial ribs
and rather narrow triangular ligamental
area with chevron-shaped grooves.
Daitokudoensis resembles Anadara(Hataiarca) kakehataensis in having depressed area and granules on the anterior ribs and also in the shell form,
but the former has a larger number ofthe radial ribs than the latter.
Locality and Formation :-Loc. no. 1.
Eoil Formation.

Anadara (Hataiarea) kakehataensis RATA I
and NISIYAMA, NODA, 1966, p. 116, pI. 2,
fig. 17, pI. 13, figs. 7-8, 10-15, 21; NODA,
1973, pI. 18, figs. 1, 3-16.
Anadara sp., KASE1\o, 1956, pI. 1, figs. 4a-b;I\\'AI, 1960, pI. 24, figs. 6a-b.

The present species was originallydescribed from the Miocene Kurosedani
Formation in Toyama Prefecture by
HATAI and NISIYAMA in 1949. The
species is characterized by the depressedarea along the posterior side extending
from the beak to the ventral margin,
wide triangular ligamental area withrather sharp chevron shaped grooves,
24-26 strongly elevated radial ribs with
granules on their anterior part.
Kakehataensis resembles
Anadara(Hataiarca) shimonakaensis HAY ASAKA(1969) from the Miocene Kawachi Formation in Kagoshima Prefecture in shellform and number of the radial ribs, but
the former differs from the latter inhaving more radial ribs, smaller shellheight and more elongated shell. The
differences from the Pliocene species,
Anadara (Hataiarca) kogachiensis from
Okinawa Prefecture were already mentioned by NODA (1971).
Locality and Formation :-Loc. nos. 1,
2, 3, Eoil Formation.

Anadara (Hataiarca) kakehataensis
HATAI and NISIYAMA, 1949

Genus Crassostrea SACCO, 1897

PI. 38, figs. 10, 13, 14

Crassostrea gravitesta eoilensis,
n. subsp.

Anadara (Anadara) kak'ehataensis RATAI andNISIY AMA, 1949, p. 88-89, pI. 23, figs. 810; MASUDA, 1955, pI. 19, figs. 2a-b (nodescription) .
Anadara kakehataensis RATAI and NISIYAMA
KAsENo, 1956, p. 5, pI. 1, fig. 2; IWAI:
1960, p. 204, pI. 24, fig. 4; FUJ[[, 1961, p.
496-497, pI. 27, figs. 1a-c, 3a-b; KITAMURA and IWAI, 1963, pI. 2, figs. 4, 6ab (no description).

PI. 38, fig. 15, PI. 39, figs. la-Ie

Shell very heavy, stout and thick, inequilateral, much higher than long.
Right valve somewhat convex, externalsurface smooth with fine concentric
growth lines. Younger shell somewhat
roundly quadrate with strongly incurved
and inclined anterior beak. Umbonal

630. Molluscan fossils from Korea
area fiat. Anterior and posterior margins rather straight and nearly parallelwith each other. Ligamental pit rather
wide and deep. Inner surface smooth.
Muscle scar large, rounded in form.
Growth lamellae oblique in lateral view.
Young shell lamellae highly inclined
against height of shell. Left valve
rather fiat, roundly quadrate. Surface
smooth with fine concentric growth lines.
Beak near central part of hinge, umbonal area fiat. Both anterior and posterior margins long, nearly straight andnearly parallel, ventral margin narrowly
and somewhat arcuated, anterior andposterior corners rather angular. Ligamental pit narrowly elevated with distinct grooves on both sides. Inner surface smooth, muscle scar rounded inform.
The specimens at hand are somewhat
incomplete but the right valve (Holotype)measures 31 cm in height and 9.5 cm inlength and the left valve (Paratype)28.8 cm in height and lOA cm in length.
Comparison and Affinities:- The present new subspecies is characterized
by the very high, large and thick shell.
The young shell form resembles that ofOstrea gravitesta YOKOYAMA (1926b)
which was originally described from
the Miocene Takasaka Bed in Akita
Prefecture. YOKOY AMA'S species seems
to be restricted to shallow and brackishwarm water facies of Early Miocene
formations. Ostrea gravitesta is distin;;guishable from the present subspecies
by the stout, thick rather fiatly rounded
shell form at the adult stage. Ostrea
gravitesta and' the present new subspecies have different shell form at the
young and adult stages with each other.
Ostrea gigas THUNBERG is allied withthe present subspecies. Some Ostrea
gigas with very long and enlarged shellform have been recorded from the Mio-275

cene (NOMURA and HATAI, 1937), Pleistocene (HAY AS AKA, 1960; ARAKI, 1959)
and Recent (W AKIY A, 1929; HIRASE, 1930
and others). However, the present subspecies differs from the above citedspecies in having roundly-quadrate shellform in the young stage and enlarged
shell form at the adult stage, with incurved, fiat beak, and series of growthlamellae. The characteristic of thepresent subspecies resembles the young
stage of Osl1'ea gravitesta and the adult;
form of Ostrea gigas.
Ostrea gigas from the Shigarami Formation (KURODA, 1931) and Ostrea gravitesta from the Tatsunokuchi Formation (NOMURA, 1938), both of Miyagianage, occurred in crowded form but not
as banks; they resemble the present
subspecies in shell form and growthform in the adult stage but differ inshell form at the immature stage. Theyrather resemble Ostrea gravitesta in shellform. Both of these species were once
considered to be synonymous with
Ostrea gigas by HAYASAKA (1960) andothers. Such data are important totrace the phylogenetical trend of Ostrea
gravitesta to such Recent forms as
Ostrea gigas and its allied species.
From the ecological point of viewconcerning the mode of occurrence andshell form, by HAYASAKA (1960) and
OHSHIMA (1971), it is of interest to notethe following. HAY ASAKA (1960) pointed
out that the large sized Ostrea gravitesta
has been usually recorded sporadicallyin occurrence but not as bank-builder
and is a representative form seems to.
have resulted from the high sea watertemperature of the Early Miocene. The
elongated Ostrea gigas found to occur
as bank in the Pleistocene is considered
to bea rather cool water form. W AKI·YA(1929) stated in his study 'of the Japanesefood oyster 'fthe shell (Ostrea.laperousii)

276

B. K. KIM, H. NODA and S. YOON

also varies according to environment asmuch as with age. Those that live ona soft bottom have a much more elongated shell than those living on a h.arderbottom".
Considering the above cited researches,the present specimens seem to have a
different mode of shell growth as compared with Ostrea gravitesta and Ostrea
gigas though the elongated shell form
might be caused by the crowded occurrence as pointed out by HAYASAKA(1960). The associated fauna and sedimentary facies of the present new subspecies are similar with those of theformations which yielded Ostrea gravitesta in japan.
Locality and Formation:-Loc. no.1-I,
Eoil Formation.

Genus Thyasira LEACH III
LAMARCK, 1818
Subgenus Thyasira s. s.
Thyasira (s. s.) sp.
PI. 38, fig. 7

The present species is characterized
by its small trapezoidal form with narrow depressed area along the posteriorside of the shell. The shell surface issculptured with concentric growth lines.
The inner surface is smooth with veryfine striations. The beak is small, incurved and situated anteriorly. The
species is not identified because of its
ill-preservation.
The genus Thyasira is a rather common genus in the northern part of the
Pacific Ocean, although it is distributed
to southern areas of warm water. From
the Miocene Oidawara Formation in
Gifu Prefecture, ITOIGAWA (1960) described Thyasira (s. s.) minoensis as a

new species. This species resembles
the present species in the shell form
but ITOIGAW A's species has a stepped
depressed area along the posterior sideof the shell. Though many species of
the genera Thyasira and Conchocele havebeen recorded in japan and the adjacentcountries by many paleontologists, it isdifficult to identify immature forms because the species sometimes shows
varied forms in the growth series. The
record of the genus from the present
formation is significant so far as the
paleoecology of the fauna is concerned.
Locality and Formation:- Loc. no. 1,
Eoil Formation.
Genus Dosinia SCOPOLI, 1777
Subgenus Phacosoma JUKESBROWNE, 1912
Dosinia (Phacosoma) nomurai

OTUKA, 1934
PI. 38, figs. 3a, 3b
Dosinia japonica nomurai OTUKA, 1934, p.
618, pI. 48, fig. 54; OTUKA, 1937, p. 29,
pI. 3, figs. 3-4.
Dosinia nagaii OTUKA, 1934, p. 618, pI. 48,
fig. 55.
Dosinia nomurai, NOMURA, 1935, p. 217, pI.
17, fig. 7; NOMURA, 1940, p. 26-27; ITO!GAWA, 1956, pI. 2, fig. 3; UOZUMI and
FU]IE, 1966, p. 151-152, pI. 12, figs. 3-11 ;TANAKA, 1967, p. 58, pI. 6, figs. 6-7.
Dosinia chikuzenensis NAGAO, HIRAYAMA,
1956, pI. 7, figs. 14-15 (Reproduction of
OTUKA, 1934).
Dosinia (Phacosoma) chikuzenensis nomurai
OTUKA, KAMADA, 1962, p. 112-113, pI. 12,
figs. 4, 5, 7-10.
Dosinia (Phacosoma) chikuzenensis nagaii
OTUKA, KAMADA, 1962, p. 113-114, pI. 12,
fig. 6.
Dosinia (Phacosoma) nomurai OTUKA, MASUDA, 1962b, p. 30-32, pI. 1, figs. 1-9;

630. Molluscan fossils from Korea
1973, p. 149-150, pI. 12, figs.
17, 20-21; HIRAYAMA, 1973, p. 176, pI.
15, fig. 14.

OGASAWARA,

The specific characteristics were already discussed by HATAI (1938), HIRAYAMA (1956) and MASUDA (1962b). The
Korean species has rather swollen shell,fine concentric growth lines, small lunuleand defined pallial line; these featurescharacterize the named species.
Locality and Formation :-Loc. nos. 2,
3, Eoil Formation.
Genus Cyciina DESHA YES, 1850
Subgenus Cyciina s. s.
Cyciina (Cyciina) japonica

KAMADA, 1952
PI. 38, fig. 9
Cyclina chinensis, YOKOYAMA, 1926a, p. 222,
pI. 28, fig. 7.
Cyclina (Cyclina) japonica KAMADA, 1952, p.
168-169, pI. 15, figs. 1-2; KAMADA, 1962,
p. 115-116, pI. 13, fig. 4.
Cyclina -japonica KAMADA, KASENO, 1956, p.
6, pI. 2, figs. 8a-d; IWAI, 1965, p. 41-42,
pI. 13, figs. 3, 4.

The present species was originallydescribed from the Miocene HigashiInnai Formation in Ishikawa Prefecture
by KAMADA in 1952. The species ischaracterized by the higher than long,inequilateral shell, inclined beak, convex
posterior side, sculpture of narrow
longitudinal ribs crossed with very fine
growth lines and triangular sinuatedpallial line.
The present species resembles Cyciina(Cyciina) orientalis (SOWERBY), a Recent
shell, in form and shape of sinuatedpallial line but the latter species has
rather more distinct striations than theformer.

277

Locality and Formation :-Loc. nos. 1,
2, 3, Eoil Formation.

Genus Clementia GRAY, 1842
Subgenus Clementia s. s.
Clementia (Clementia) nakamurai

OTUKA, 1938
PI. 38, figs. 5, 6a, 6b
Clementia speciosa, YOKOYAMA, 1925b, p. 119,
pI. 14, fig. 7.
Clementia nakamurai OTlJKA, 1938a, p. 14-15,
pI. 1, figs. 7, 11; ARAKI, 1960, p. 97, pI.
7, figs. 7a-c.

The present species was originallydescribed from the Miocene Shiroyama
Sandstone in Shizuoka Prefecture by
OTUKA in 1938a. The species is characterized by its rough concentric growthlines and folds with nearly straight
posterior margin and narrow anteriorone.
In the original description, OTUKA
mentioned the difficulty of the identification of Clementia species based upon
the external morphology. The present
species is allied to Clementia japonica
MASUDA (1955) which was describedfrom the Miocene Higashi-Innai Formation but the latter differs from theformer in not having so strong wavy
concentric growth lines and elongatedshell. Clementia vatheleti MABILLE resembles the present species but differsfrom the latter in having more convex
shell and rounded form.
Clementia
papyracea (GRAY) shows more variationin shape as already mentioned by SHUTO(1960) but can be distinguished from thepresent species by the short dorsal
margin.
Locality and Formation:-Loc. nos. 1,
2, 3, Eoil Formation.

218

R"K. KIM, H. NODA and S. YOON

Genus Soletelliria DE" BLAINVILLE, 1924

Soletellina minoensis YOKOYAMA. 1926
~I.

38,. fig. 4

Soletellina minoensis YOKOYAMA, 1926a, p.
221, pI. 28, figs. 13-16; MAsuDA, 1955, pI.
19, fig. 9;. KAMADA,.196?, p .. 126.-127, pI.
14, fig. 7; UOZUlv!l and JUJIE, 1966, pI.
'.
12, fig. 12. Sanguinolaria (Soletellina) minoensis (YOKOYAMA), OTUKA, 1934, p.619, pI. 49, figs.
., 65a-b ; OYAMA and SAKA, ~,944~ .p'. 141,
. ' :'
pI. 15, figs. 17-18.
Soletellina d. minoensis YOKOYA.~IA, KA.SE~O,
19~6; .p. 6, pI. 3, figs. 14a-c.··.... '.'

Some conjoined shells were examined.
The.. specie~ . is characterized by. its
e.iongated form, short anterior side andelong~t~d ppsterior side. Both sides.
a~e rounded and the ventrai margin is
bro'a~l:Y c.Ul:ved.. A small. beak is situateda;nt~l:io~ly. . Im?-er characteristics are notknown. The named species was origi-.
nally' described' from the Tsukiyoshi
Formation in GUu Prefecture by YOKOY AMA in ~926a. ..
Locality and For11lation:-Loc. nos. 1,
2, 3: ~oil Formation..... .

MENARD,. 1807
Genus Panppe.

Fanope' cf. nom'urae KAMADA, 1962

from Panope japonica ADAMS, a common
species in the seas around northeasternJapan and in the Pliocene to Pleistoceneof Japan by the proportion of shelllength to height. However, as alreadymentioned by NOMURA (1938), KAMADA(1962), AKUTSU (1964) and HATAI (1964),
considerable morphological changes canbe recognized in "Panope japonica .. '~from the Miocene to Recent of Japan.
Accordingly, some species, Panope kano-

11latazawaensis, Panope kanomatazawaensis fudoensis and also Panope n011lurae
were discriminated. The present specimen in this connection resembles Panopejaponica of KANNO (1960) described from
the Miocene Nagura Formation in Saitama Prefecture and which is clearly
distinguishable from Panope japonica A.
ADAMS, a Recent species. The specimen
described under the names of Panopejaponica, Panope generosa and also Panope
estrellana should be re-examined.
The usage of the generic name Panope
has been subjected to discussion' butfrom the International code of zoologicalnomenclature, STOLICZKA (1871), DALL(1912), OLDROYD (1924), STEWART (1930).
GRANT and GALE (1931), KANNO (1957,
1960) all favor to use the generic nameand it seems at present Panope of
MENARD, 1807.
Locality and Formation :-Loc. no. 3,
Eoil Formation.

PI. 38, fig. 2

C~mpared with:-Panope nomurae KAMADA,KAMADA, 1962, p. 135-136,. pI. 16, figs.
9-12.
.

The present specimen is characterized
by its transversely elongated form; both
extremities 'rather narrowly rounded,
anterior and posterior dorsal margins
slender and surface with wavy concentric
growth lines. Panop.e n011lurae, according to KAMADA (1962) is .distinguishable

Genus Vicarya D'ARCHIAE and
HEIME,1954
Subgenus Shoshiroia KAMADA, 1960

Vicarya (Shoshiroia) callosajaponica
YABE and HATAI, 1938
PI. 39, figs. 4, 5

Vicarya baculum YOKOYAMA, 1926a, p; 219,
pI. 28, figs. 4-6.

630.

Molluscan fossils from Korea

279

Vicarya vernuili, MAKIYAI-IA, 1932, pl. 1, fig.
5.
Vicarya callosa JENKINS, TAKEYAMA, 1933,
p. 137-140, pl. 13, fig. 3.
Vicarya callosa japonica SAGA (MS) , YABE
and RATAI, 1938, p. 156-157, pl. 21, figs.
12-13, 21-22, 28, 31.
Vicarya callosa japonica YABE and RATAI,MASUDA, 1955, p. 125; MASUDA, 1956, pl.
26, figs. la-b; Y AMANA, 1966, p. 34, pl.
1, figs. la-b.
Vicarya ct. callosajaponica YABE and RATAI,
IWAI, 1960, p. 206-207, pl. 24, figs. 1a-b,
2; KITAMURA and IWAI, 1963, pl. 2, figs.
1-2.
Vicarya callosa forma japonica SAGA (MS) ,OTATUME, 1943, p. 314, fig. l.
Vicarya (Shoshiroia) callosa japonica Y ABEand RATAI, KAyIADA, 1960, pl. 30, figs.
2a-b, 7, 8, pI. 31, figs. 2a-b; KAMADA,
1967, pI. 7, figs. 3-5; RAYASAKA, 1969,
p. 48-49, pI. 3, figs. 7-8.

morphological differences among theJapanese species seem to be not significant ", and he wrote that the specie~from the Pitogo Formation in the Philip~
pines is closer in shell form and surface
ornamentation to Vicarya callosa fromthe type locality of Java than that fromJapan. From the many literatures andspecimens preserved in the Institute ofGeology and Paleontology, Faculty of
Science, Tohoku University, the specimens from South Korea are identified toVicarya callosa japanica described by
YABE and HATAI in 1938.
Locality and Fonnation :-Loc. nos. 1,
2, 3, Eoil Formation.

Several specimens were examined.
The species is characterized by 9-10
distinct sub sutural tubercles on the
penultimate whorl, flat on upper sideand inclined on the lower side withspiral lines on a suture and somewhat
conical shape of suture. YABE andHATAI (1938) recognized two subspecies
among Vicarya callosa; one is callosa s. s,and other is callosa japonica based upon
the shape of the tubercles and development of grooves over the tips of the
tubercles. This classification has been
accepted by MATSUO (1951), MASUDA(1955, 1956), IWAI (1960), KAMADA (1960,1967), YAMANA (1966) and HAYASAKA·(1969). Whereas IKEBE (1939) questioned
the differences between Vicarya callosa
and Vicarya callosa japonica and concluded (IKEBE, 1952) that Vicarya callosa
should not be separated into subspecies
by the shape of the tubercles. Although
he examined the tubercles of Vicaryacallosa from Java, he did not figure thespecies. IWASAKI (1970) stated that .. theVicaryella ishiiana (YOKOYAMA, 1926)

Genus Vicaryella Y ABE andHATAI, 1938

Pl. 39, fig. 2
Cerithium baculum YOKOYAMA, 1925a, p. 12,
pI. 2, fig. 6.
Cerithium ishiianum YOKOYAMA, 1926a, p.
218, pI. 28, figs. 11, 12.
Cerithiu1n (Proclava) otukai NOMURA, 1935,
p. 227, pl. 17, fig. 7.
"Vicaryella" ishiiana (YOKOYAMA), YABE
and RATAI, 1938, p. 169.
Vicaryella ishiiana (YOI>:OYAMA), OYAMA and
SAKA, 1944, p. 139-140, pI. 14, figs. 7a8b; KAMADA, 1960, pI. 31, figs. 4a-b;
KA!vIADA, 1962, p. 152, pI. 18, figs. 15-16;
MASUDA, 1967, p. 1-2, pl. 1, figs. la, 2b.

The present species is distinguishedfrom Vicaryella notoensis MASUDA (1956),
which was originally described from
the Miocene Higashi-Innai Formation in
Ishikawa Prefecture, in having more
tubercles on the fine spiral cords.
Vicaryella tyosenica YABE and HAT AI,
1938, the type species of the genus,
which was originally described from

280

B. K. KIM, H. NODA and S. YOON

the Miocene Heiroku Formation in North
Korea, is another species allied to thepresent one but the species is characterized by conspicuous tubercles andfour or five spiral cords with smallbeads.
Locality and Formation :-Loc. no. 3,
Eoil Formation.
Vicaryella sp.
PI. 39, fig. 3

The poorly preserved specimens at
hand show no distinct tubercles on the
sub sutural area. The specimens possess
the vicaryellid aperture and spiral cords
but lack such beaded tubercles as seen
on Vicaryella tyosenica Y ABE and HAT AI,
V. ishiiana and V. jobanica. In thisrespect the present specimens are rather
more similar to V. notoensis MASUDA(1956). MASUDA's species is characterized by having many small beaded
spiral cords. Unfortunately the specimens from the Eoil Formation can not
be named until additional and better
material is obtained.
Locality and Formation :-Loc. no. 1,
Eoil Formation.
Genus Cerithid~a Sw AINSON, 1840
Subgenus Cerithidea s. s.
Cerithidea (s. s.) sp.
PI. 39, fig. 6

Compared with :-Potamides (Cerithidea) kanpokuensis MAKIYAMA, 1926, p. 149, pI. 12,
figs. 2, 3.

The specimen (unnamed) is characterized by its high conical shell with 911 longitudinal folds and rather distinct
spiral cords on the sutures; the aper-

tural part is broken. Cerithidea kanpokuensis (MAKIY AMA), comparable with.
the present specimen was originally described from the Miocene Heiroku Formation in North Korea by MAKIY AMA.
in 1926. That species has been recorded.
from the Miocene Higashi-Innai For-·mation in Ishikawa Prefecture (MASUDA,
1967), and Kawachi Formation in Kagoshima Prefecture (HAY ASAKA, 1969) but
the specimens from the recorded formations are all small in size comparedwith the specimen from the Eoil Formation.
Locality and Formation :-Loc. no. 1,.
Eoil Formation.

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282

B. K. KIM, H. NOD A and S. TOON

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KIM, NODA and YOON:KUMAGAI

photo.

Molluscan fossils from KO?'ea

Plate 38

630.

Molluscan fossils from Korea- - (1971): New anadarid and associatedmolluscan fauna from the Raneji Formation, Okinawa-jima, Ryukyu Islands.
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283

Univ., 2nd Ser., vol. 21, no. 1, p. 1-46,
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Explanation of Plate 38(All figures in natural size unless stated otherwise)
Figs. la, Ib, 11. Anadara (Anadara) kiiensis MIZUNO, p. 273, Loc. no. 1, IGPS coIl. cat. no.
92933.
Fig. 2. Panope d. nomurae KAMADA, p. 278, Loc. no. 3, preserved in Busan National Univ.
Figs. 3a, 3b. Dosinia (Phacosoma) nomurai OTUKA, p. 276, Loc. no. 3, IGPS coIl. cat. no. 92939.
Fig. 4. Soletellina minoensis YOKOYAMA, p. 278, Loc. no. 1, IGPS coIl. cat. no. 92940.
Fig. 5. Clementia (Clementia) nakamurai OTUKA, p. 277, Loc. no. 3, IGPS coIl. cat. no. 92941.
Figs. 6a-6b. Clementia (Clementia) nakamurai OTUKA, p. 277, Loc. no. 1, IGPS coIl. cat. no.
92942.
Fig. 7. Thyasira sp., p. 276, Loc. no. 1, IGPS coil. cat. no. 92943.
Figs. 8a, 8b, 12. Anadm'a (Hataiarca) daitokudoensis (MAKIYAMA), p. 274, Loc. no, 1, IGPS
coIl. cat. no, 92934.
Fig. 9. Cyclina (Cyclina) japonica KAMADA, p. 277, Loc. no. 1, IGPS coIl. cat. no. 92958.
Fig. 13. Anadara (Hataiarca) kakehataensis RATA I and NISIYAMA, p. 274, Loc. no. 3, IGPS
col I. cat. no. 92935.
Figs. 10, 14. Anadara (Hataiarca) kakehataensis RATA I and NISIYAMA, p. 274, Loc. no. 1,
IGPS coIl. cat. no. 92936.
Fig. 15. Crassostrea gravitesta eoilensis KIM, NODA and YOON, n. subsp., (Paratype) p. 274,
Loc. no.1-I, IGPS coli. cat. no. 92937, x 1/3.
IGPS coil. cat. nO.=collection catalogued number of the Institute of Geology and Paleontology,
Faculty of Science, Tohoku University, Sendai, Japan.

284

B. K. KIM, H. NODA and S. YOONOTUKA, Y. (1934): Tertiary structures of
the Northwestern End of the Kitakami
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SHlJTO, T. (1960): On some pectnids andvenerids from the Miyazaki Group.
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Univ., Ser. D., vol. 9, no. 3, p. 119-149,
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vol. 10, p. 129-141, pI. 13.
TANAKA, K. (1967): Fossils of Anan-machi.
Educ. Commit. Anan-machi, Shimoina·gun,
Nagano Prefecture, p. 1-160, pis. 1-38 (inJapanese, original title translated).

TATEIWA, 1. (1924): Explanatory text ofthe geological map, scale 1 : 50,000, Ch6y6,
Ennichi, Kyuryu. Ceol. Surv. Cov. Cen.
Chosen, 7 p., 3 maps. (in Japanese).
TSl-DA, K. (1965): Neogene molluscan assemblages in the inner zone of Northeast Japan-with the special reference
to the Middle Miocene assemblages.
Fossils, no. 10, p. 20-23, tabs. 1-2. (inJapanese) .
UOZU~II, S. and FC]lE, T. (1966): Neogene
molluscan fauna in Hokkaido. Pt. 2,
Description of the Okushiri fauna associated with Vicarya, from Okushiri
Island, Southwest Hokkaido. Jour. Fac.
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2, p. 139-163, pis. 11-13, figs. 1-4.
WAKIYA, Y. (1929): Japanese food oysters.
Japan. Jour. Zool., vol. 2, no. 3, p. 359367, pis. 8-10.
YABE, H. and HATAI, K. (1938): On theJapanese species of Vicarya. Sci. Rep.,
Tohoku Imp. Univ., 2nd Ser., vol. 19, no.
2, p. 149-172, pI. 21.
YAM ANA, 1. (1966): Neogene fossil Mollusca
from Akenabe, Tottori
Prefecture,
Japan. Bull., Japan. Mus. Assoc., no. 1,
p. 33-38, pis. 1-2, 2 figs. (in Japanese).
YOKOYAMA, M. (1925a): Molluscan remains
from the uppermost part of the Joban
coal-field. Jour., Coli. Sci., Imp. Univ.
Tokyo, vol. 45, art. 5, p. 1-34, pis. 1-6.
- - (1925b): Mollusca from Tertiary basinof Chichibu. Jour. Fac. Sci., Imp. Univ.
Tokyo., Sec. 2, vol. 1, pt. 3, p. 111-126,
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- - (1926a): Molluscan fossils from the
Tertiary of Mino. Ibid., vol. 1, pt. 7, p.
213-227, pI. 28.
- - (1926b): Fossil mollusca from the oilfields of Akita. Ibid., vol. 1, pt. 9, p.
377-389, pis. 44-45.
- - (1929): Neogene shells from the province of Chugoku. Ibid., vol. 2, pt. 8, p_
363-368, pI. 70.

K IM, NODA and YOON:

K UM A GAI

photo.

Molluscan fossils from Korea

Plate 39

630.
Andong·ri*
Aniai+
Asagawa+
Auil**=Eoil*
Bangsan·ri *Beomgog·ri*
Bulgugsa* = Fukkokuji**Changam*
Changgi* = Janggi* =Ch6ki**
Cheonbug*=Sempoku**
Ch6ki**=Changgi* = Janggi*
Ch6y6* = Gampo*
Daegog*Ennichi** = Yeonil*
Eoil*=Auil**
Fukkokuji**= Bulgugsa*
Galpyeong·dong*
Gampo* = Kampo*'
Geumo-ri*
Guryongpo* = Kyilryilho**
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H wabong·ri *Idong*
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Jangmyeong·gol*
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Kampo** = Gampo*
Keumgoangdong** =Molluscan fossils from Korea
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Explanation of Plate 39(All figures in natural size, unless stated otherwise)
Figs. la, Ib, lc. Crassostrea gravitesta eoilensis KIM, NODA and Yoo:-.r, n. subsp., p. 274, Loc.
no.1-I, IGPS colI. cat. no. 92938. (Holotype), x 2/3.
Fig. 2. Vicaryella ishiiana (YOKOYAMA), p. 279, Loc. no. 3, IGPS colI. cat. no. 92944.
Fig. 3. Vicaryella sp., p. 280, Loc. no. I, IGPS colI. cat. no. 92945.
Figs. 4, 5. Vicarya (Shoshiroia) callosa japonica YABE and HATAI, p. 278, Loc. no. I, IGPS
colI. cat. no. 92946.
Fig. 6. Cerithidea sp., p. 280, Loc. no. 1, IGPS colI. cat. no. 92947.

286

PROCEEDINGS OF THE PALAEONTOLOGICALSOCIETY OF JAPAN

D*~~~~~IW4~~~·~~~1~4~1

Fl 11 Il (1It). 12 IJ (±) ~:::jLHIj(~JJll~:nl;L:::t,\-' l fjFJ(W 2Q1.J: (~tm tf 72 15)
0

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1Y!J"t~~~~~ J:11'[j0) 51 f.Jj C illl1t~:::........................ i~IIIF!fl±"% =.Iill ~Ill fIiIllmi [1'11:f,~ ~ iii( ................ ;j' j110j jIi:l';=Prefecture, Japan ............ FUKUTA, O.
Pliocene planktonic foraminiferal faunafrom northern Mindanao, Philippines ..
.................. UJIlE, H. & SAMATA, T.
Lower Pleistocene to Upper Miocene planktonic foraminifera from the ShimajiriGroup of the Island of Miyako, Ryukyu...................... UJIlE, H. & OKI, K.
~di:--4i l',1m'i:E'Itl;:fiLIJ1=i~:{,ci·J\'tO)k:}j~T.f::: "?v' l ..

................................... fJRJtti0t;¥ 1)IJ ~~i ilii

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.........••..•........•............ 'tr:ID-r=:.ftF>
fffil A. ilf!i ill\:
Lower Cretaceous flora from the Akaiwa
Formation, the Tetori Supergroup, Central
Japan .......... KIMURA, T. & SEKIDO, S.
A new cycadophyte from the Liassic Iwamuro Formation, Gumma Prefecture,
Japan ........................ KIMURA, T.
~~lWfffO)t@17JJft:E~c"?v'l.

·tt j!i¥,l!i:i • ~~*I[lm1J;ffi

T ~ -, of- ~ of-TJill;J:;";flEL~lE~O)1t*,j}~¥~ ....

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13*itr.ii1i}~;lP/::,j*JIH.J: 1:::' 7- r :/ . ::z 7f::: ill:!
QrJlUl-j~Hn9:tJ1iIii!tIi~~f:l:R~c "?It'l ..... .
................................... /J\* tJ!r~~.T://~':/~r:/~il~Q.~D.c.Ul~.~~:~(T¥I1)················ iffi lI15!:.ftB

Microbiostratigraphy of some middle
Miocene sequence in northern Japan ....
.......... TAKAYANAGI, Y., TAKAYAMA,
T., SAKAI, T., ODA, M. & KITAZATO, H.
Foraminiferal research in the Geodynamic
Project, the First Cruise, 1972 (GDP-l)................................ KONDA, 1.
Globorotalia (Turborotalia) humerosa praehumerosa, n. subsp. and its stratigraphic
significance .................... NATORI, H.
Foraminifera from the Tachigase Formation along the Arakawa River, Saitama

Biostratigraphical Zonation of the Rat Buri
Limestone in the Khao Phlong Phrab
area, Sara Buri, Central Thailand ..... .
. ......... TORIYAMA, R., KAMMERA, K.,
KAEWBAIDHOAM, S. & HONGNUSONTHI, A .
Correlation of the Silurian stromatoporoid
reefs in Shropshire (England) and Gotland (Sweden) .................. MORI, K.
.~O)a~@Llm~9~~~:/~~.fQ ..

. ............ " .................. [lii]tiftzllj)
Gaudryceras 0) constriction ~c "? It \ l..... .

• .••••••••••.•••••••••••.•••••• '•••• IJ1. R'f-iJ1,:@:
Otoscaphites puerculusc..... ·fJlIJnJ;-.QX:

0) Jfq,ti,SO)n¥I:\J~':JJtit.l(-0)~fi8Jfq,f~*a':J~IJ;ld::: "?It'l

Cretaceous patelliform gastropods fromJapan and adjacent areas ...... KANIE, Y .
The differentiation of the species of Inoceramus in the Lower Urakawan (Coniacian) ........................ NODA, M .
On the type-species of Trigonioides (Studies
on the Cretaceous non-marine mollusca
from Korea. Part 1) ............ W;
On a new veneroid pelecypod genus"Mesochione" from the Himenoura Group· ............................. TASHIRO, M.
Associated occurrence of Adulomya and"Akebiconcha" from the Taishu Group of
Tsushima, Nagasaki Prefecture ....... .
............ KAMADA, Y. & TAKAHASHI, K.
Some interesting taxodontid bivalves from
the Miocene Osozawa Formation, Yamanashi Prefecture ....................... .
· .OMORI, M., AKIYAMA, M. & MANO, K.

**

287
A new abalone from the Miocene of Aomori Prefecture, Northeast Honshu,
Japan .... KOTAKA, T. & OGASAWARA, K.
~&O)m:oxt*c iW7.krilil.

.... /J'ililiR:::t: . :7;:j~.'1,;,)!tn!.LlE:JJi 0) .Y7J1:m: U~~ 0) ~ ~Ij 0) t1fjj)n:: ":) v' -C ..
................................... '§n:iiix!J5

Race formation in Suchium costatU11l (Trochidae, Gastropoda) ..... , . ~ ... OZA \V A, T.
The vicissitudes of the Diluvium Furuya
Mud Basin, Shizuoka Prefecture, Japan.
-A faunal analysis of fossil ostracodes- ................ KATO, M.& ISHIZAKI, K.
Balanus rostratus HOEK (~ 7 :; '/ ;G') c.:c0) "lffifffi" ~~":)v'-C ................ iJJJ:l~Z~1i&:Jl¥Jq,frrMEO) r -777- to' H :(H.Il 0)1 I:: ::fi~:: ":)\;'*-C ..................... ·J:!j!HqiiJfi . tf i.'lf.mo~:/,f,:;7A

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o 13 *r±l1:!fl;]"jt~¥I1,* . HC~ 1973 ~~jjitlE~Wifu3t:1tf:l:, 5fIJ~L.)!t;gO) rBiostratigraphic study of
I±\hlii.J;jj!;~~j ~ ht~,

the Jurassic Toyora Group. Pt. 3J fU~-9-~ht.:o<0 1974 ~"jt*'9't1iIb{Hl:. IJ'iN~=;g (fl::::fi~j!*Jl~O)liJfJE) .B J::: V:B:~ *;g (fftL:E.O)~1lL:· r±l1:!fl;]"jti3':JliJf}t) fct~-9- ~ :I1.t.:.
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291

CONSTITUTION

of the
PALAEONTOLOGICAL SOCIETY OF JAPAN;0-.

(Jan. 11, 1974)
ArticleArticle1. The Society shall be known as the Palaeontological Society of Japan.
2. The object of the Society is to promote the study and popularization of palaeontology and related sciences.
Article 3. The Society, to execute Article 2, shall undertake the following business:
1. Issue the Society journal and other publications.
2. Hold or sponsor scientific lectures and meetings.
3. Popularize the science by field trips, scientific lectures and other projects.
4. Aid and encourage research work; award outstanding contributions to theSociety; carry out the objectives stated in Article 2.
Article 4. To attain the object of the Society, the Society may, by decision of the General
Meeting, establish within it research committees.
Article 5. The Society shall be composed of members who are active or interested inpalaeontology or related sciences.
Article 6. The members shall be known as Regular Members, Fellows, Patron and Honorary
Members.
Article 7. Persons desiring membership in the Society are requested to fill out the necessary
application forms and receive the approval of the Council.
Article 8. Fellows are persons who have held Regular Membership in the Society for morethan ten years, have contributed to the science of palaeontology, have been
nominated by five Fellows and approved by the Council.
Article 9. Patrons are organizations supporting Article 2 and recommended by the Council.
Article 10. Honorary Members are persons of distinguished achievement in palaeontology.
They shall be recommended by the Council and approved by the General Meeting.
Article 11. The members of the Society shall be obliged to pay the annual dues stated in
Article 12. Members shall enjoy the privilege of receiving the Society journaland participating in the activities stated under Article 3.
Article 12. The rates for annual dues shall be decided by the General Meeting. Rates forannual dues are: Regular Members, Yen 3,000; Fellows, Yen 4,200; and Foreign
Members, U. S. $ 16. 00; Patrons are organizations donating more than a share(Yen 10,000) annually; Honorary Members are free from obligations.
Article 13. The budget of the Society shall be from meinbership dues, donations and bestowals.
Article 14. The Society, by decision of the Council, may expel from membership persons who
have failed to pay the annual dues or those who have disgraced the Society.
Article 15. The officers of the Society shall be composed of one President and fifteen Councillors, among whom several shall be Executive Councillors. The term of office
is two years and they may be eligible for re-election without limitation. The
President may appoint several persons who shall be Secretaries and Assistant
Secretaries. An Executive Council shall be nominated and approved by theCouncil. Councillors shall be elected from Fellows by vote of returned mailunsigned ballot.
Article 16. The President shall be a Fellow nominated and approved by the Council. The
President shall represent the Society and supervise the business affairs. The
President may appoint a Vice-President when he is unable to perform his duties.

292
Article 17. The Society may have the Honorary President. The Honorary President shall berecommended by the council and approved by the General Meeting. The Honorary
President may participate in the Council.
Article 18. The Society shall hold regularly one General Meeting a year. The President shallbe Chairman and preside over the administrative affairs. The program for the
General Meeting shall be decided by the Council. The President may call aSpecial Meeting when he deems it necessary. The General Meeting requires theattendance of more than one-tenth of the members. The President shall call aSpecial Meeting at the written request of more than one-third of the members.
The request shall be granted only if the written statement fully explains thereasons for assembly and items for discussion.
Article 19. Members unable to attend the General Meeting may give an attending member
a written statement signed by himself trusting the bearer with the decision ofbusiness matters. Only one attending member may represent one absentee.
Article 20. The decision of the General Meeting shall be by majority vote. When the numberof votes is equal, the President shall cast the deciding vote.
Article 21. The President and Councillors shall compose the Council. The dicision of theGeneral Meeting concerning administration shall be considered and implemented
by the Council.
Article 22. The Executive Council shall carry out the decisions of the Council.
Article 23. An auditor shall be elected by the Council from Fellows excluding Councillors
and Secretaries. The term of office is two years and he may be eligible forre-election.
Article 24. The fiscal year of the Society shall begin on the first of January each year andend on the thirty-first of December of the same year.
Article 25. The amendments to the Constitution of the Society shall be decided at the General
Meeting and must be approved by more than two-thirds of those members whoare in attendance.
Addendum 1) Voting in the Council shall be by unsigned ballot.

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Transactions and Proceedings of the PalaeontologicalSociety of Japan

New Series No. 93

April 20, 1974

CONTENTS
TRANSACTIONS
627. KAPOOR, Hari Mohan and BANDa, Yuji: Report of Lower Trias from Pir
Panjal, near Qazigund, Kashmir, India, with Description of a Few
Ammonoids .......................................................... 227
628. NODA, Masayuki: A New Species of Inoceramus from the Shimantogawa
Group of South Shikoku .............................................. 240
629. SADA, Kimiyoshi and DANNER, Wilbert R.: Early and middle Pennsylvanian
Fusulinids from Southern British Columbia, Canada and Northwestern
Washington, U. S. A. .. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 249
630. KIM, Bong Kyun, NODA, Hiroshi and YOON, Sun: Molluscan Fossils from
the Miocene Eoil Formation, Gampo and Ulsan Districts, SoutheasternSide of Korea .. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 266
PROCEEDINGS ................................................................ 286