Transactions and Proceedingsof thePalaeontological Society of Japan
New Ser ies

No. 100

Palaeontological Society of Japan
December 25, 1975

EditorTakashi HAMADA
Associate Editor Ikuwo OBATA

Officers for 1975 - 1976
Honorary President: Teiichi KOBAYASHI
Presiden t : Tatsuro MATSUMOTO
Councillors (*Executive): *Kazuo ASAMA, Kiyoshi ASANO, *Kiyotaka CHINZEI,*Takashi HAMADA, *Tetsuro HANAI, *Itaru HAYAMI, Tadao KAMEl,*Kametoshi KANMERA, *Tamio KOTAKA, *Tatsuro MATSUMOTO, Tokio
SHIKAMA, Tsugio SHUTO, *Yokichi TAKA YANAGI, Toshimasa T ANAl,*Hiroshi UmE
Executive Committee:
General Affairs: Tetsuro HAN AI, Itaru HAY AMI, Kiyotaka CHINZEI, Saburo
KANNO, Yasuhide IWASAKIMembership: Kazuo ASAMA, Kazuhiko UEMURA
Finance: Hiroshi UmE
Planning: Tamio KOTAKA, Hiroshi NODA
Publications
Transactions: Takashi HAMADA, Ikuwo OBATA
Special Papers: Kametoshi KANMERA, Ienori FUJIY AMA, Tomowo OZAWA"Fossils": Yokichi TAKAYANAGI, Toshiaki TAKAYAMA

Fossil on the cover is the six leaves in a whorl of Trizygia oblongifolia(GERM. & KAULF.) ASAMA from the Maiya formation (Parafusulina zone),
Maiya, N. E. Japan.
All communications relating to this journal should be addressed to the
PALAEONTOLOGICAL SOCIETY OF JAPAN
c/o Business Center for Academic Societies, Japan
Yayoi 2-4-16, Bunkyo-ku, Tokyo 113, Japan
Sole agent: University of Tokyo Press, Hongo, Tokyo

Trans. Proc. Palaeont. Soc. Japan, N. S., No. 100, p. 175, December 25, 1975EDITORIAL
This is the 100th issue of our journalin the New Series. The PalaeontologicalSociety of Japan was founded in 1935,
and at the same time the Old Series of
the Transactions and Proceedings of the
Palaeontological Society of Japan commenced as a part of the Journal of theGeological Society of Japan. The New
Series started in 1951 as a separate
journal, and since· 1957 our Society has
become independent from the GeologicalSociety. Consequently, this 100th issue
appears just a quarter century after thatmemorial event of the Society.
Among some 80 extant jounals of theworld specialized in palaeontology andclosely related fields of earth sciences,
our journal, thus, has rather long historyof development. It represents one of the
career journals which have been publishedsince a period before World War II.
Excluding short notes and other occasional papers, 656 articles have been
published in the journal both in the Old
and New Series, of which 465 are in thelatter. 199 authors have contributed to
the New Series, and distinguished four ofthem have passed away, i. e. Professors
Hisakatsu YABE, Riuji ENDO, Seido ENDO
and Rokuro MORIKAWA who had greatly
promoted. our Society and the journal intheir own specialities.
The new taxa proposed throughhundred issues of the New Series attain
49 in supra-specific, 651 in specific and
46 in infra-specific levels, respectively.
They have been endorsed by many good
illustrations on 538 photographic plates.
It is quite evident that the journal has
developed as one of the leading scientificpublications in our country since its foundation. Actually, our Transactions andProceedings of the Palaeontological Society
was the first specialized journal in European languages in the fields of geologicalsciences in Japan except some university
publications. The character of this journal
was apparently to be international, andit has been much strengthened during
this past quarter century. 36 papers
written by Japanese palaeontologists in
the New Series have dealt with thematerials from abroad, and 26 articles
have been contributed by foreign scientists
from various countries.
Special Papers, another series publishedas monographic works by our Society,will be numbered 20th in 1976 also. The
Society decided to publish a supplementary issue of the New Series that entitled" A Concise History of Palaeontology inJapan" as N. S. No. 100s in this memorable year. The reader will find not onlya history of the development but also
the trends of the Japanese palaeontology
in this extensive presentation.
Quite recently, EDITEAST, an Association of Editors in Science in Southeast
Asia, Australasia and Oceania, was established being sponsored by UNESCO and
IUGS. The aim of the association is said
to promote improved communication inscience by cooperation of editors of serial
publications. This new movement will
be welcomed, and our journal would play
an important role as, for the time being,a unique international series that is
specialized in palaeontology in the region_(T. HAMADA)

175

176
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Trans. Proc. Palaeont. Soc. Japan, N. S. No. 100, pp. 177-187, pIs. 16, 17, Dec. 25, 1975

652.

ON A NEW NON-MARINE PELECYPOD GENUS FROM THE
UPPER MESOZOIC GYEONGSANG GROUP OF KOREA*SEONG-YOUNG YANG
Department of Geology, Kyushu University, Fukuoka, 812**~OOl:ifIl<=p~W~~~lW£~fi1i1~=tjU'lJJt*'TIll!.~::.":>\"-C: l:ifIl<=p~W~fi1i1nX;I®-e<bQ~OO~~~lW*Jlfilli:J~lWiJ'Q~£-rQ=:ttJ'l.~liif~L, *'T~ Nagdongia ~llltvt-C8C.~Lt.:o .:.hfiiJ'''? -C %1*iJ~ Nakamuranaia chingshanensis .!: L -Cllc~ L t~ t 0) .!: 7i-Mft {JjQ iJ~, P:lifIl
it~<=pOO£O) Leptesthes chingshanense GRABAU O)llc.~.!: ttl~~ft%1*O)llclt.!: ifhi',

ifht,(\',o JlJJ':'A.-.!:~t~~fttrL6 Nippononaia, Wakinoa, Plicatounio .!:~{Jj-rQiJ~, .:.
n QO)~.!: ft*ITfi~~-e 1R5.iIj~nQo .;en QO)fm~::., l3l~0) t o).!: L -C 77 1) 7J £0) Caelatura (Laevirostris) bourguignati (ROCHEBRUNE) 7JJ.. ry C. (Zairai) elegans (ROCHEBRUNE) iJ~~t~0)~,!:/,lC7U~::.:f.>\"-C*~.!: O)~{JjM:~~L "(\"Q,¢.i:iJ~i±13 ~nQo

~ ~*Introduction

Acknowledgements

Until now, there have been reported
four non-marine pelecypod genera fromthe Upper Mesozoic Gyeongsang Groupof Korea, i. e., Trigonioides, Plicatounio,
Schistodesmus and Nakamuranaia, all ofwhich were established by Japanese
authors about thirty years ago.
Recently I have collected a large number of specimens from four localities of
the Lower Gyeongsang Group (Nagdong
Subgroup) which represent a new speciesof a new genus.
In this paper I give a systematic description of it and a discussion on thecomparison with other non-marine Mesozoic pelecypod species from the Far
East.

express my hearty appreciations toProfessor Tatsuro MATSUMOTO for hiskind supervision and critical reading of
the typescript of this paper, and to Associate Professor Kametoshi KANMERA
for his continuous encouragement andadvice, and Dr. Tomowo OZAWA, Dr.
Hiromichi HIRANO, Mr. Kazushige T ANABE and Miss Mutsuko HAYASHIDA of
the Kyushu University for their kind
helps in various ways. And my sincere
thanks are due to Professor Yoshihisa
OHTA of the Fukuoka University of
Education for his instructive suggestions,and to Associate Professor Itaru HAY AMIof the University of Tokyo and Professor
Shiro MAEDA of the Chiba University
for the loan of their valuable specimens,
and to Assistant Professor Sangwook
KIM of the Kyungpook National University for sending me some papers whichwere inaccessible here.

* Received April 8, 1975; read June 15,
1974 at Osaka.
** Present address: Department of EarthScience, College of Education, Kyungpook
National University, Daegu, Korea.

177

Seong-Young YANG

178

KOR EA

12S030'E

3CN-4---~--------~~~-----Ur--------

national road- - - highway,"~adong\\-+-__~,,--::;=_'''E'''------;i\~nlr--35·N
126°E

12S0E

Text-figure 1.

Index and locality maps of Nagdongia soni.

Systematic description
Family U nionidae
Subfamily Unioninae
Genus Nagdongia, nov.

Type-species. Nagdongia soni, sp. nov.,
to be described below.
Generic diagnosis. Shell medium insize; fairly variable in outline, commonly
subtrapezoidal, sub elliptical or trigonallyelongate; rounded in front, more or lesstruncated behind, moderately inflated;
provided with a fairly distinct posteriorridge; inequilateral and equivalve. Beakfairly prominent, prosogyrous and situated rather anteriorly. Surface ornamented
with concentric growth lines only. Hinge

teeth well developed; 3 on each valve;
2 pseudocardinal and 1 posterior lateralon right valve; 1 pseudo cardinal and 2
posterior lateral on left valve; forming adental formula:
3

PIlI

1

2

PII

PIV.

Two adductor scars fairly distinct andthe anterior one accompanied with aminute but definite pedal scar on innerside.
Inner margin smooth.
Beakcavity deep. Pallial line simple. Test
fairly thick.
Remarks. The type-species of thisnew genus is fairly similar to a species
from Korea described under "Nakamuranaia chingshanensis (GRABAU)" by SUZUKI (1943). However, the hinge structure

652.

A New Non-Marine Pelecypod Genus

179

ri' •
12!f30E_ _ _....."""'_ _ _...:,1;.:2:,.:25::.. ::,E,-~~.....-:"""""--,,,----,---,,--,...--o,--:-,-:--:,--:-,-:-,-:,--:-,--:-,-,;-'7-+3tOON:,' , /

"

"

,
"

,
,

"

I

,,' "
I

I

I

'"
I

I

I

I' "
I

I

I

"

'
I

'

"

I
I

I

I,',',

,

I'

"
I

I

,,',,1,,' " II,. ',;//

",.

/

E;js
+

~4
~

0" ",

+

"////, 3,',,' /' ,,' :',++ + 2~+ +".'-------

Dl-----~-"-ll:........:-._----------=======::...2c===f_35·55·N

o_____~==~2~___3~==~4km

Text-figure 2. Geological map around the type-locality of Nagdongia soni.
1. Granitic gneiss
2, Granite
3. Yeonhwadong Formation
4. Hasandong Formation
5. Dongmyeong Formationof the present type-species is distinct
from that of the latter in SUZUKI'S description. Leptesthes chingshanense GRABA U, 1923, from North China, the typespecies of N akamuranaia SUZUKI, 1943,
is quite distinct from the type-species ofthe present genus in the hinge structure
as well as the shell-form and thicknessof the test, as is described in detail below.

The number of hinge teeth and theirdisposition are the same as of the recent
Caelatura(Laevirostris)
bourguignati(ROCHEBRUNE) and C. (Zairai) elegans(ROCHEBRUNE) from Central and Western
Africa, respectively. But in detail, therecent African bivalves and the present
genus are distinctly different from eachother as follows:

Characters

the African bivalves

the present genus

cardinals
hinge platepedal scar
adductor scarbeak
posterior part
test

blade likenarrow
nonsmall
not prominent
high
thin

blunt and stout striated in adultmoderate
present
fairly large
prominent
not so high
thick

180

Seong-Young YANG

and the disposition of hinge teeth, arefairly similar to those of Nippononaia,
Wa/linoa and Plicatounio, but this genus
has no radial ribs, the typical ornamentation on the disk of these genera.
The generic name is taken from the
Nagdong River, one of the largest rivers
in Korea, flowing near the type-locality(Text-figs. 1 and 2).
Nagdongia soni YANG, sp. nov.

A

PI. 16, Figs. 1-11; PI. 17, Figs. 1-44,
Text-figs. 3, 4 and 6

,

RV

.1

• 1

(<<~cA~1~~·1.1......__...

. / .

LV

......

-......... :...... .-... .. -:.....:..... _........

B
Text-figure 3. Internal structure of
Nagdongia soni.
A. immature
B. adult

And also taking account of much separated geographical distribution and thechronological difference, the similarityof the hinge teeth seems to be considered
not of genetic relation but of a convergence.
On the other hand, the internal structures, such as adductor scar, pedal scar

Material. The specimen KPE 1111, awell preserved right valve, is designatedas the holotype. It is one of the largest
specimens, with dimensions: 72.1 mm inlength, 47.3 mm in height, 31.7 mm in the
distance between the umbo and the anterior extremity and 11.6 mm in inflation.
The other specimens are the paratypes(KPE 1112-1242). All of the specimens
numbered with prefix KPE are preservedin the Department of Earth-Science, College of Education, Kyungpook National
University, Daegu, Korea. The plastercast of the holotype is kept in the Department of Geology, Faculty of Science,
Kyushu University, Fukuoka, Japan.
Etymology. The specific name is dedicated to Professor Chi-Moo SON of theSeoul National University who has contributed much to the development of
Geology in Korea.
Specific diagnosis. Shell fairly large
and subtrapezoidal or subelliptical in
outline. Hinge teeth 3 on each valve as
described in generic diagnosis. The posterior lateral teeth almost smooth andrather lamellar, but the pseudocardinalteeth provided with faint cross striationsin the adult shell. The other characterssame as presented in generic diagnosis.
Description. Shell outline is quite vari-652.

A New Non-Marine Pelecypod Genus

Text-figure 4.

181

Variation of the outline of immature shells(right valves) from Locality A.

able as shown in Text-fig. 4. For convenience' sake, the shells are divided
into 4 types. Type A is characterized
by the blunt umbo and fairly roundedventral margin and the high ratio of
H/L. Type B is similar to Type A except for the ratio of H/L. Type C seems
to be intermediate· between Type A andType B. Type D is relatively angularat the postero-ventral and postero-dorsal
corners. Among the above types, TypeD is a majority group and Type B aminority. Type B and Type D are quite
different from each other. However, thedifference in shell-form can not be regarded specific, for there are many
intermediate forms between them.
Surface is nearly smooth except for
the growth lines roughened at irregularintervals.
Hinge plate is moderate in breadth,provided with opisthocline antero-pseudocardinal and postero-lateral teeth. The
antero-pseudocardinal ones are 2 on rightvalve and 1 on left valve; they rathersmooth in immature shells but striatedfaintly in the adult; the postero-lateral
teeth are 1 on right valve, 2 on left
valve, lamellar in both immature andadult shells. The pseudo cardinal ones
are relatively higher and stouter, while
the postero-lateral ones are longer andsharper and originated from a point
apart posterior to the umbo; all of thehinge teeth are parallel to the dorsal
margin.
Two adductor scars are situated close
to the ventral ends of the pseudocardinal

182

Seong- Young YANG

and postero-lateral teeth, sub circular inshape and sub equal in size, but the anterior one is more impressed and slightly
smaller than the posterior one. In theadult specimens, the adductor scars are
distinctly marked by the nearly verticaland very fine riblets. The anterior adductor scar is accompanied with a subtriangular minute pedal scar. Pallial
line is shown immediately below the anterior adductor scar and running backward parallel to the marginal outline of
the shell and disappeared in the posteriorpart, without showing pallial sinus. The
inner marginal side is smooth (see Textfig. 3).
Formation and locality. The fossiliferous beds under consideration are
widely distributed in Nagdong Subgroupof the Gyeongsang Group, Korea. The
Nagdong Subgroup is lithostratigraphically divided into Yeonhwadong,
Hasandong, Dongmyeong and Chilgok
Formations in ascending order (CHANG,
1966). The present species has beenfound in the sequence from the lower
part of the Yeonhwadong Formation to
the middle part of the Hasandong Formation. However, the present knowledgeof the geological age and correlation of
Korean Mesozoic deposits is not sufficient to determine the chronological relationship between the fossil populations
between distant areas. The studied
specimens were collected from the following four localities (Text-fig. 1).
Yeonhwadong Formation:
Locality A, at a point south ofGeummu-san, Waegwan-ub, Gyeongsang-buk-do (type-locality).
Locality B, at a point north of
Buldong-ri, Jicheon-myeon, Chilgokgun, Gyeongsang-buk-do.
Hasandong Formation:
Locality C, on a seaside of Sumoondong, Geumnam-myeon, Hadong-gun, Gyeongsang-nam-do.
Locality D, at a point east of Cheonpyeong-gyo, Gasan-myeon, Chilgokgun, Gyeongsang-buk-do.
I have collected altogether about 200
shells, of which 93 are measurable forstatistical treatment, from these four
localities. The sample from Locality A
is the largest (more than 140) in sample
size, and those from Locality B (morethan 30) and Locality C (more than 10)
are much smaller than that from Locality
A, but they deserve statistical examination for comparison. The sample from
Locality D is the smallest (N =3) andconsists of too much deformed and fragmentary specimens to be measured.

Text-figure 5. Basic morphology
and measurements.

Simple ratios. From the bivariate data
the fundamental values are calculated
in relation to the characters L/H, D/L
and I/L. The results are summarized inTable 1. In Table 1, the mean values
are represented as range at 95% confidence level and the chi-square test on
the sample from Locality A is shown in
the right side. As seen in the Table 1, thecoefficients of variation of the ratio L/H
are smaller than those of other ratios.
In other words, the character L/H is thehighest in stability among the consideredcharacters, whereas D/L is shown most

652.
Table 1.

183

A New Non-Marine Pelecypod Gem~s

Arithmetic means of the simple rat ios L / B, D/ L and I/ L.

1)

L/H

Loc.

N

X ± tO.05 a X

V

s

ax

O.R.

X2

Remarks

A
B
C

77
11
5

1. 550 ± O. 028
1. 462±0. 064
1. 675 ± O. 183

7.93
6. 74
8. 80

O. 123
0.095
O. V170.014
0. 0290.066

1. 29- 1. 87
1. 33- 1. 59
1. 57 - 1. 83

3. 5101

N.S.

2)

D/ L

A
B
C

77
11

O. 298± 0. 013
O. 314 ± O. 053
O. 394 ± 0.107

19. 76
25. 26
16. 99

0.059
0.079
0.067

0.067
0.024
0.034

0.17-0.48
0.23-0.48
0.33-0.49

6. 8458

N. S.

3)

I/ L

A
B
C

38
9
4

O. 163 ± O. 009
O. 184± 0.025
0.169 ±0. 020

16. 34
17. 97
7. 48

0. 0270.033
0.01 3

0.004
o 011
0.006

0. 10- 0.20
014-0.24
0.16-0. 18

1. 1022

N. S.

11

ar ithmetic mean w i th 95% confidence leve l
V : Pearson's coefficient of va riations: standard dev iationax : standard error of the mean
O. R. : obser v ed range
X2 : chi·square
N. S. : not sig nificant at 95% confidence level
N: sample size

X ±tOO.5a X:

variab le and the va lue of the chi-squareis also largest. However, the resu lts ofthe chi-square test indicate that the n ull
hypothesis for a normal distribution is
not rejected for the characters con sidered.
Observation . In Text -fig . 6, the sizefrequency distribution of the shell length
in the sample from Locality A is shown.
All of the specimens possess well preserved test and severa l of them are conjoined. The shells at hand range widelyin size, i. e., 1.6- 74. 5 mm in length in thesample from Loca lity A, 4.2-80.0 mm inthat from Loca lity Band 5.8- 47.5 mm inlength from Locality C. This probably
means that shells of various growthstages are observable.
The internal
structures have been observed on the 11
specimens of wide range of growth stage
from 9 mm to about 67 mm in length.

The striations are distinctly developedon the anterio r pseudocardinal teeth in

Text·figure 6. Frequency histogram ofsize in leng th of Nagdongia soni from
Locali ty A.

184

Seong- Young YANG

the specimens larger than 60 mm, but
not in the smaller ones. This is probably
an ontogenetic variation.
All the fossiliferous beds consist ofvery fine sediments, black shale or veryfine siltstone. Although a definite orientation of a shell is not always examined,
the state of its preservation seems todepend on the orientation of the commissure plane to the stratification. Whenthe shell is embedded in parallel to thestratification, it is fairly well preserved,
but when it is oblique or vertical to thebedding plane, it is more or less deformed. This suggests that the fossil bearing beds were compressed normal to thebedding plane.
Discussion

As pointed above, the present species
possesses the same pattern of hinge
teeth as the African Recent bivalves,
Caelatura (Laevirostris) bourguignati and
C. (Zairai) elegans, but differs from thelatter species in many other characters.

And it seems to be related to certain
species of Nippononaia, Wakinoa andPlicatounio in some internal characters,
but the features of its hinge teeth are
not accord with those of the latter genera
as well as its surface is not ornamented
with the typical radial ribs of thosegenera.
In the surface ornamentation and theoutline, this species is fairly similar to theso-called Nalwmuranaia chingshanensis
from Korea described by SUZUKI (1943)(non GRABAU, 1923). Although SUZUKI's
specimens are not accessible to me (according to SUZUKI they were destroyedout during World War II) , that species
was reported to possess two pseudocardinal teeth on each valve and two
posterior lateral ones on right valve andone on left valve, while the present
species has two pseudo cardinal teeth onright valve and one on left valve, andone posterior lateral on right valve andtwo on left valve. Furthermore, in thepresent species the pseudo cardinal teeth
are distinctly striated, but in SUZUKI's

Explanation of Plate 16(All figures are of natural size.)
Figs. 1-11. Nagdongia soni YANG, gen. & sp. nov.
1. Right valve (KPE 1111), holotype.
2. Right valve (KPE 1112).
3. Right valve (KPE 1130) showing the shell thickness.
4. Left valve (KPE 1113) showing the shell thickness.
5. Right valve (KPE 1131)
6. Conjoined valve (KPE 1123) showing the dorsal part strongly deformed vertically.
7. Left valve (KPE 1138)
8. Right valve (KPE 1114)
All of the above specimens were collected from a point south of Geummu-san, Waegwanub, Chilgok-gun, Gyeongsang-buk-do, Korea (Loc. A).
9. Left valve (KPE 1146). Loc.: At a point north of Buldong-ri, Jicheon-myeon, Chilgokgun, Gyeongsang-buk-do, Korea (Loc. B).
10. Right valve (KPE 1151)
11. Internal mould of left valve (KPE 1152)
These two specimens were collected at the sea side of Sumoon-dong, Geumnam-myeon,
Hadong-gun, Gyeongsang-nam-do, Korea (Loc. C).

Y ANG:A new non-marine pelecypod genus

Plate 16

652. A New Non-Marine Pelecypod Genus
they are lamellar. In virture of Professor
MAEDA, I have observed one (R. 61102602)
of the specimens described by him under
the name "Nakamuranaia chingshanensis"
from the Kitadani alternation, Akaiwa
Subgroup, Tetori Group, Japan. It has
the same surface ornaments and outline
as the present species, but to my regret,its internal structure cannot be observable. According to his description (1962,
p. 349), the structure of the hinge teeth
is in accord with SUZUKI'S description.
KOBAYASHI and SUZUKI (1936) described Corbicula (Leptesthes?) coreanica
and Cristaria? sp. aff. "Leptesthes chingshanense GRABAU from the Nagdong Subgroup, here and there. After that, SUZUKI(1943) included them into the Nakamuranaia chingshanensis. I have observed
these fossils kept in the University ofTokyo. But the preservation is too bad
to examine clearly their characters,
especially the internal structures. The
specimens identified as "Cristaria? sp. aff.
Leptesthes chingshanense" may be regarded as the immature ones of mycollection.
And those of Corbicula(Leptesthes?) coreanica seem to be distinct
from the above Cristaria? sp. in outline,
thickness and the pointness of the umbo
and to be similar to my specimens from
Locality C. However, the differences
between those and mine can not be said
certainly.
Nakamuranaia chingshanensis(GRABAu,
1923) from China certainly differs fromthe present species in outline, shell
thickness and the internal structures.
GRABAU described the Chinese specieson the basis of much smaller specimens
compared with the Korean adult specimens. Thus, I took a special consideration on the specimens of similar size incomparison. In the present species
the test is never thin and the muscle
impressions are distinctly shown. Ac-

185

cording to GRABAU'S description, in the
Chinese species the test is thin and themuscle impressions are not clearly shown.
The difference in the shell outline isevident (compare GRABAU'S text-figure
with the present species in Text-figs. 4
and 5). GRABAU'S species is characterized by a fairly straight ventral margin,
but the present species is well rounded.
GRABAU observed the faint cross striations or transverse notching on thepostero-Iateral teeth, but the present
species shows no striations on thepostero-Iateral teeth, except for thoseon the antero-pseudocardinal teeth ofadult specimens larger than 60 mm inlength.
At the beginning of this study, I considered that the present species might
belong to Nakamuranaia chingshanensis
and that Locality A was the same asthat of SUZUKI'S original collection. But
I have never found at Locality A the
specimens which are in accord withSUZUKI'S description (1943). As there wasno locality map in his paper, I cannot
certify the identity of my locality A
with his.
So far as the accessible monographs
are concerned, there are no species, fossil
and the Recent, with which the present
species could be identified.

References cited
CHANG, K. H. (1966): Stratigraphy and sedimentation of Nagdong subgroup (Lower
Cretaceous), Gyeongsang Province, South
Korea. Jour. Geol. Soc. Korea, vol. 2,
no. 1, 17-51, figs. 1-7, pIs. 1-3.
CRAIG, G. Y. (1967): Size-frequency distributions of living and dead populationsof pelecypods from Bimini, Bahamas,
B. W. I. Jour. Geol., vol. 25, no. 1, 34-45.
EAGAR, R. M. C. (1952): Growth and variation in the non-marine lamellibranch

186

Seong-Young YANG

fauna above the Sand Rock mine of the
Lancashire Millstone Grit. Quart. jour.
Geol. Soc. London, vol. 107, 339-373, figs.
1-16.
GRABAU, A. W. (1923): Cretaceous fossils
from Shantung. Bull. Geol. Surv. China,
vol. 5, no. 2, 143-181.
- - (1923): Cretaceous mollusca from
North China. Ibid., 183-197.
HAYAMI, 1. and ICHIKAWA, T. (1965): Occurrence of Nippononaia ryosekiana from the
Sanchu area, Japan. Trans. Proc. Palaeont. Soc. japan, N. S., no. 60, 145-155,
pI. 17.
KOBAYASHI, T. (1968): The Cretaceous nonmarine pelecypods from the Nam Phung
Dam site in the northeastern part of the
Khorat Plateau, Thailand with a noteon the Trigonioididae. Geol. Palaeont.,
S. E. Asia, vol. 4, 109-138, pIs. 20-23.
- - and SUZUKI, K. (1936): Non-marine

shells of the Naktong-Wakino Series.
japan. jour. Geol. Geogr., vol. 8, nos. 34, 243-257, pIs. 27-29.
MAEDA, S. (1962): Some lower Cretaceous
pelecypods from the Akai wa subgroup,
the upper division of the Tetori groupin central Japan. Trans. Proc. Palaeont.
Soc. japan, N. S., no. 48, 343-351, pI. 53.
MATSUl\WTO, T. (1938): Geology of the
Goshonoura Island, Amakusa, withspecial reference to the Cretaceous
stratigraphy. jour. Geol. Soc. japan, vol.
45, no. 532, 1-46, pIs. 1-2.
MEEK, F. B. (1870): Preliminary paleontological report, consisting of lists offossils, with descriptions of some new
types, etc. U. S. Geol. Surv., Wyoming
Prelim. Rept., 285-318.
MOORE, R. C. (editor) (1969): Treatise on
Invertebrate Paleontology, pt. N, vols. 1
and 2, Mollusca 6, Bivalvia, 951pp.

Explanation of Plate 17
Figs. 1-44. Nagdongia soni YANG, gen. & sp. nov.
1-38. ImmatQre specimens showing the variation of outline. x 2.
Figs. 2, 5, 6, 8, 10, 11, 12, 13, 14, 16, 19, 20, 21, 22, 24, 25, 26, 27, 28, 29, 30, 31, 32, 33;
Right valves, and the others left valves. Figs. 1 (KPE 1199), 2 (KPE 1155), 3 (KPE 1158),
4 (KPE 1157), 5 (KPE 1156), 6 (KPE 1160), 7 (KPE 1159), 8 (KPE 1198), 10 (KPE 1161),
11 (KPE 1162), 13 (KPE 1167), 14 (KPE 1232), 15 (KPE 1165), 16 (KPE 1168), 17 (KPE
1196), 19 (KPE 1166), 20 (KPE 1164), 21 (KPE 1163), 22 (KPE 1170), 23 (KPE 1173), 24(KPE 1175), 25 (KPE 1171), 26 (KPE 1172), 27 (KPE 1174), 28 (KPE 1176), 31 (LPE 1177),
32 (KPE 1178), 33 (KPE 1179), 34 (KPE 1180), 36 (KPE 1182), 37 (KPE 1183); from
Locality A. Figs. 18 (KPE 1184), 29 (KPE 1185), 30 (KPE 1186), 35 (KPE 1237), 38(KPE 1187) ; from Locality B. Figs. 9 (KPE 1188) and 12 (KPE 1189) ; from Locality C.
39a and b: Internal mould and rubber cast, showing the internal structures of immature shells, left valve (KPE 1134).
40: Internal mould of right valve, showing the hinge teeth (KPE 1129).
41: Internal mould of conjoined valve, showing the hinge teeth (KPE 1190).
42a and b: Internal mould and rubber cast, showing the internal structures of immature shell, right valve (KPE 1135).
43: Rubber cast of the left internal mould, showing the internal structures of adult(KPE 1119). Posterior part strongly deformed.
44: Rubber cast of the left internal mould, showing the internal structures of adult(KPE 1118).
Figs. 39-44 of natural size, from locality A.
All of the above specimens are kept in the Department of Earth-Science, College of Education, Kyungpook National University, Daegu, Korea. A plaster cast of the holotype (KPE
1111) is kept in the Department of Geology, Faculty of Science, Kyushu University, Fukuoka,
Japan.

YA NG:A new non-l1WTine pelecypod g en~(,s

4

12

11

13

Plat e 17

6

5

14

15

23

24

28

29

30

34

35

36

7

16

31

390

37

420
40

8

9

10

17

18

19

26

27

32

33

652.

187

A New Non-Marine Pelecypod Genus

OTA, Y. (1959): Trigonioides and its classification (Studies on the molluscan faunaof the Cretaceous Inkstone Series, part2). Trans. Proc. Palaeont. Soc., Japan,
N. S., no. 34, 97-104.
- - (1959): On the "Nippononaia" from theCretaceous Wakino subgroup, north
Kyushu, Japan. Ibid., 105-110, pis. 10-11.
- . (1963): Notes on the relationship ofTrigonioides and Plicatounio, non-marine
Mesozoic bivalvia from eastern Asia.
Ceol. Rept. Hiroshima Univ., no. 12, 503512.
ROCHEBRUNE, A. T. de (1886): Sur quelqueslamellibranches nouveaux provenant duCong et de ses tribulaires. Soc. Malacol.
France, Bull., vol. 3, 1-14, pI. 1.
SIMPSON, C. T. (1900): Synopsis of thenajades or pearly freshwater mussels.

Buldong-ri
Busan
Cheonpyeong-gyo
Chilgok
Daegu
Dongmyeong
Gasan-myeon
Geumhodong
Geummu-sanGeumnam-myeon
Gwangju
Gyeongsang

{f,.

1i"J

~

1[

JlJ

7'R W f1.lj
:fr
~
j~

*-

~

31[
~
~lfi

III 00lIJl ii"J
JlJ
ill!
~

•
m-

OO

1t

HI

!1!

j'bj

U. S. Nat!. Mus., Proc., vol. 22, 501-1044,
pI. 18.
SON, C. M., et al. (1969): A study on thesedimentary environments and geologic
structure of Korea. Res. Rept. Minist.
Sci. Tech., 50pp.
SUZUKI, K. (1940): Non-marine molluscan
faunule of the Siragi Series in South
Tyosen. Japan Jour. Ceol. Ceogr., vol. 17,
nos. 3-4, 215-231, pis. 22-24.
- - (1943): Restudy on the non-marine
molluscan fauna of the Rakuto Series in
Keisyo-do, Tyosen. Jour. Sigenkagaku
Kenkyusyo, vol. 1, no. 2, 189-219, pis.
14-19.
YANG, S. Y. (1974): Note on the genus
Trigonioides (Bivalvia). Trans. Proc.
Palaeont. Soc. Japan, N. S., no. 95, 395408, pis. 54-55.

Gyeongsang-buk-do ~ j'bj ~t Jl[
Gyeongsang-nam-do ~j'bjm-Jl[
Hadong-gun
fnJ 31[ '1mHasandong
IDI. III 1I"J"'"
Jicheon-myeon~ )II 00
Nagdong31[
Nagsangyo
JlJ f1.lj
Namhaem~Sindong
1I"J!Ifr
Sumoon-dong
7.K
1I"J
Waegwan-ub~ ;%'g E.
Y eonh wadong
51 7E 1i"J**r,

Trans. Proc. Palaeont. Soc. Japan, N. S., No. 100, pp. 188-208, pI. 18, Dec. 25, 1975

653. NOTES ON INOCERAMUS LABIATUS (CRETACEOUS
BIV AL VIA) FROM HOKKAIDOTATSURO MATSUMOTO
Department of Geology, Kyushu University, Fukuoka 812

and
MASA YUKI NODA
Wasada Junior High School, Oita 870~tw~~ Inoceramus labiatus t;::'0~'-C: *:filtS]I!** ~ - P .::. 7:/ Illff'€lll O)jf.;*
ft:E c L -C-utm-t;::JA <~;(P-t 7.> t;~, bt;~IE-Clt"£ t.:.:tO)jgJjf.; • ac.t;~tJ:tJ' '? t.:o *:fit;::Il'fJ~-C~ 7.>~*O)~tw~t;:::toH'" 7.> £l±l a-, ~ff:a-!J.I:Iac L.t.r.:t;~ 1?ID?)Jij Lt.:o ~ 1, 2 jgJt;::~*9~.tL7.> J: ?
t;::, *:filt-*:!tBt;, I?~t.r.:t;, I?T~l±l L, :!tB~r~'~Jtt;::1i~-C.:!b 7.> 0 "£ t.:Il'fJ#:fi (~:E) t.r.: I? '0't;::J: • r &O)*l'l&:fi~ t 1*-1t~Ll-t.tLI!, '/!fft c IE~~ Jtt;:: t ~.1z:'00 tXt;:: tt~4W~i¥Jilc..a­rrt.r.:~', c <t;::~ff:i¥Jt;::J:rO)!iJIjO).:!b7.>~flt;::'0~'"L, ~Jl:a-*T~::I:i¥Jt;::~WL, ]I!:fi:§!~O)~a-jf.;-t.:. c a-~[JfJ {4t.:o .:. O)~Jl:O)f(fi[ti]lt* ~ - P .::. 7 :/<P'€lIl0) Inoc. teraokai ~1l'fJ1lM'
J:'€lIl0) Inoc. incertus cO)I*l~a-~!J.I:I-t7.>J:t;::tm:~-c.:!b7.>o "£t.:.:.O)~*a-~*t;:::toH'"7.>*:fit.r.: I? m;::JlI~:fi c Jt~ L "L, *:fia-~tr*1UO)~f1;;i¥J~ftt;:: '0 ~'-C'f~B1.Jt;::~~a-~~ 7.>
c c tt;::, 4-~0)7iIf~1.f[ti]t;::'0\',-c0)J!ma-;m~t.:.
t.t * ~ !!~.!f IE ~ Z.

p. 85) mentioned of the occurrence ofInoc. d. labiatus in a bed of the Cretaceous sequence along the River Ikushumbetsu, together with Kanabiceras
septemseriatum.
Subsequently KANIE(1966) found an unmistakable example ofthis species from an isolated locality in
the Urakawa area. Recently MATSUMOTO and OKADA (1973) have recordedin their stratigraphic paper, written injapanese, Inoc. labiatus and allied species
found at several localities, with detailsof the stratigraphic position. Furthermore, one of us (T. M.) has continued,
together with H. HIRANO and K. TANABE,
a biostratigraphic investigation of the
Obira and Oyubari areas, getting more
specimens. Most of these old and recent
acquisitions are included in the material

Introduction
Inoceramus labiatus (SCHLOTHEIM) isa world-wide guide species of the Lower
Turonian. For some reasons, however,it has been considered rather rare injapan. In a comprehensive monographof NAGAO and MATSUMOTO (1939-40)
this species was not described.
It was, however, pointed out that someof the specimens labelled as Inoceramus
incertus JIMBO, from a zone with Pseudaspidoceras sorachiense in central Hokkaido, closely resemble Inoc. labiatus(MATSUMOTO and HASHIMOTO, 1953, p.
100)_ Furthermore, MATSUMOTO (1959,
Received April 9, 1975; read Oct. 19, 1974
at Nagoya.

188

653.

Notes on Inoceramus labiatusof the present study.
In this paper we give a concise noteon the stratigraphic occurrence and apalaeontological description of Inoceramus
labiatus from Hokkaido. Although oneof us CT. M.) had opportunities to lookat some of the specimens labelled as
Inoceramus labiatus at several museumsin Europe and North America, we avoid
to mention too much of those extraJapanese specimens on this occasion. We
intend to present here what sort of forms
have been obtained at which stratigraphic
positions in the Cretaceous deposits of
Hokkaido and endeavour to find a way
how to improve our knowledge.

189

which are concerned with the palaeontological description in this paper.
(1) Saku area. For the general stratigraphy and geological mapping of thisarea see MATSUMOTO (1942), S. NAGAOo

Before going further, we wish to thankDr. Hakuyu OKADA, Dr. Hiromichi HIRANO and Mr. Kazushige TANABE for their
help in various ways and Professor Wataru HASHIMOTO, Dr. Yasumitsu KANIE
and Mr. Tatsuo MURAMOTO for theircooperation in offering some valuablespecimens for our study. Miss Mutsuko
HA YASHIDA assisted us in preparing thetypescript.
Stratigraphical Note
The outcropping areas of the postAptian Cretaceous deposits in the central
zone of Hokkaido are shown in Text-fig.
1. The places where Inoceramus labiatus
and allied forms have been obtained are
indicated by numbers in the same map.
In many areas geological mapping has
been laboriously achieved, resulting in
the geological maps on scale 1: 50,000 as
well as other stratigraphic papers. Field
works are still continued in some areas
to know more precisely the biostratigraphic sequences.
The following is a brief account of thestratigraphy relevant to the beds with
Inoceramus labiatus and allied forms

42'

142· E

50 km
!

!

!

,

Text-fig. 1. Map of central zone of
Hokkaido showing the outcrop of the post. Aptian Cretaceous deposits. 1. Saku area,
2. Soeushinai-Kotambetsu area, 3. Obiraarea, 4. Ikushumbetsu area, 5. Ashibetsu
area, 6. Oyubari area, 7. Furano area, 8.
Urakawa area; Chain: boundary between. western and eastern belts.

190

Tatsuro MATSUMOTO and Masayuki NODA

(1962), HASHIMOTO (ed.) (1967) and MATSUMOTO and OKADA (1973).
The Cenomanian to Turonian sequenceis well exposed along the streams of the
Saku-gakko-no-sawa, the Saku-gawa andthe Nio-no-sawa. It is subdivided into
units IIa, IIb, IIc and IId. Inoceramus
labiatus was found in a calcareous nodule
at loc T5090, Saku-gakko-no-sawa, in the
middle of unit IIc, about 130m sequenceof claystone. A large shell of Fagesia(?) sp. came from the same locality.
Fagesia thevestensis (loc. T610b), Fagesia
cf. rudra (loc. T1158-59), and Sciponocerasorientale (loc. T610 e) were found inother localities of the same unit (MATSUMOTO and OBA TA, 1963; MATSUMOTO,
1973), which indicates Lower Turonian.
Unit IIc is conformably underlain byunit IIb, greenish bluish grey fine sandy
siltstone, about 350m in thickness, whichcontains Inoceramus concentricus nipponicus, Inoc. pennatulus, Desmoceras(Pseudouhligella) japonicum, D. (P.)
ezoanum, Calycoceras orientale (loc.
T711b, T225b and c), Euomphaloceras cf.
meridionale (loc. T5031b), among manyothers. These species indicate Middle
to Upper Cenomanian. Unit IId, which
conformably overlies IIc, is characterizedby sandstone bedded in various thickness, frequently intercalated or intertongued with siltstone. IId is called the
Saku Formation, about 400-450m thick,and is subdivisible into three members,
IId1, IId2 and IId3. Inoceramus hobetsensis characteristically occurs almost
throughout the sequence, except forupper IId3, Inoc. iburiensis in lower IId3,
and Inoc. teshioensis in upper IId3.
Among many ammonites there is Collignoniceras woollgari bakeri found fromlower IId3 (loc. T1022 p7) (see MA TSUMOTO, 1965).
(2) Soeushinai-Kotambetsu area. The
area was geologically mapped by HASHI-

MOTO et al. (1965). In this area mudstone is more predominant than in the
Saku area. A thick monotonous sequenceof mudstone, nearly 1000m in thickness,is exposed along the Kiritachi pass ofthe highway No. 239 between Soeushinai
and Kotambetsu, as was explained by
MATSUMOTO and OKADA (1973, p. 284,
text-figs. 7-8). This is mainly Cenomanian, because of the occurrence of
Inoceramus concentricus nipponicus, Inoc.
pennatulus (or Inoc. reduncus), Desmoceras (Pseudouhligella) ezoanum andCalycoceras aff. asiaticum (loc. R100), butfrom its uppermost part (50m) Inoceramus
labiatus (loc. R114) and Sciponoceras
kossmati (loc. R117) were found. Thispart is conformably succeeded by thelithostratigraphic equivalent of the Saku
Formation, but here again the mudstone
is predominant and thinner units ofalternating sandstone and mudstone,
with some intraformational conglomerate,occur at four levels with thicker intervalsof mudstone. What was called Inoc. aff.
labiatus by MATSUMOTO and OKADA(1973, p. 285) was obtained from the
mudstone immediately above the firstalternation (loc. R123). The main part
including the second and the third unitsof alternation is characterized by Inoc.
hobetsensis, and among many others
Romaniceras cf. yezoense came from thispart (loc. R137).
(3) Obira [ObirashibetsuJ area. The
area was geologically mapped by TsuSHIMA et al. (1958) and IGI et al. (1958).
Among the co-authors TANAKA especiallydevoted himself to the Cretaceous
stratigraphy (see also TANAKA, 1963).
MATSUMOTO, OKADA, HIRANO andTANABE have recently carried out biostratigraphic investigations in this area,with whom T. MURAMOTO and K. MURAMOTO have cooperated for a while. As
their work has not yet been completed,653.

Notes on Inoceramus labiatus

the following is a preliminary informa·tion.
Fairly steeply inclined strata of Ceno·
manian to Turonian ages are well ex·
posed along the upper main course of
the River Obirashibetsu and its tribu·
taries, the Kanashiri·zawa and the Oku·
futamata·gawa. To the southwest closer
to Tappu [Tap], there is a dome called
the Nakakinembetsu dome, which is oc·
cupied mainly by Turonian strata, thoughwith some minor structural complexity.
As in the preceding area, the mainpart of the Cenomanian is represented
by a thick sequence of mudstone, charac·terized by the occurrence of Inoceramus
concentricus nipponicus, blOC. concentricus
costatus, Inoc. pennatulus and Desmoceras(Pseudouhligella) japonicum. This is
succeeded conformably by a member ofgreenish fine sandy siltstone or sility
fine·sandstone (called Member Mi by T A·
NAKA), 30-90m in thickness. Inoceramus
sp. and Tragodesmoceroides subcostatus
may occur in it. It is, in turn, succeed·
ed by another member consisting of
mudstone and compact tuffite, with inter·calated bentonitic tuft (Mj of TANAKA),
about 350m. Inoceramus labiatus andInoc. n. sp. (thin shelled type apparently
allied to but not identical with Inoc.
teshioensis) are characteristic. Fagesia
n. sp. (ioc. R5231b), Fagesia sp. (ioc.
R5235p), Vascoceras aft. durandi (ioc.
R2153), Pseudaspidoceras sp. (loc. R5211),
Mammites sp. (R2307), Damesites aft.
laticarinatus (ioc. R4519), Puzosia inter·media (R2101, several other localities) andSciponoceras d. orientale, as well as
Scaphites, Otoscaphites, Tetragonites andGaudryceras are found at various levelsof this member. Although zonal subdivi·
sion is impossible, this member, Mj, andprobably also Mi, are altogether referred
to Lower Turonian.
The succeeding sequence (Mk through191

Mn plus lower Ua of TANAKA), about
700m, of mudstone with sandstone inter·calations is characterized by the pre·dominance of Inoc. hobetsensis. Colligno.
niceras woollgari bakeri (iocs. R2004,
R2008, R2026) and then Subprionocyclus
bravaisianus (iocs. R2003, R2027c) areoccasionally found from its middle part
among many other ammonites. In thehigher part Inoc. iburiensis and Inoc.
Reesidites minimus
teshioensis occur.
was found at an isolated locality.
(4) Ikushumbetsu area. It may be call·ed the Mikasa district in accordancewith the recently given administrative
name. Fine exposures of the Cretaceous
strata were seen along the River Iku·
shumbetsu [=IkushumbetsJ and its tri·
butaries, but since the construction of
the Katsura·zawa dam, the condition has
become unfavourable. The data depend
much on the observation (of T. M.) andcollections before the appearance of theartificial lake. For the general geo·
logical maps see YOSHIDA and KAMBE(1955) and MATSUNO et al. (1964), andfor a route map and columnar sections
see MATSUMOTO (1965, figs. 2-5).
In this area the Cenomanian plus
Turonian are mainly represented by the
Mikasa Formation, which is characterized
by sediments of generally shallower andcoarser facies than in other areas. Twokinds of sequence are observable on bothwings of the Ikushumbetsu anticline,with shallower facies in the west. The
Mikasa Formation, about 400m, is sub·divisible into four members, IIa, lIb, IIc
and lId in ascending order on the easternwing. For the biostratigraphic successionof lIa to IIc see an up·to·date account of
MATSUMOTO (1975, p. 156). Althoughsandstone generally predominates in theformation, member lIe consists of silt·stone, about 60m thick, containing cal·careous nodules. Its main part (45m) is192

Tatsuro MATSUMOTO and Masayulci NODA

characterized by large shells of liloc.
pennatulusand a find of Calycoceras d.
naviculare. Its top 15m, as represented
by loco Ik 1038 and loco Ik 987, has adistinct faunule consisting of Kanabiceras
septemseriatum, Sumitomoceras jaustum,
Sciponoceras kossmati, Allocrioceras sp.,
Gaudryceras aff. varagurense and Puzosia
aff. intermedia orientalis. Recently Pseudocalycoceras aff. dentonense and Eucalycoceras (?) aff. collignoni have been foundfrom this zone, as reported by MATSUMOTO and KA w ANO (1975). Several
specimens of lnoc. labiatus were obtained
from the same zone (same locality). As
the top of lIc is demarcated by a basal.green sandstone of lId and the suceeding
lower part of IId is rather poor in fossils,
how far lnoc. labiatus ranges upward inthis sequence cannot be decided. It isnoted that bentonitic tuff is frequently
intercalated in the lower part of lId,
which may be correlatable with the tuff
and tuffite in the Lower Turonian of
the Obira area. IId is unfavourable forammonites, except for a record of fragmentary collignoniceratid, but lnoc. hobetsensis occurs in its main part, with larger
forms in the upper part.
The succeeding 130m sequence of silty
fine sandstone or fine sandy siltstone islithostratigraphically referred to thelower part of the Upper Yezo Group,
denoted as IlIa. Its lower part still contains Inoceramus hobetsensis but its mainpart, with an interbed of green sandstone, is characterized by lnoc. teshioensis,
with associated Subprionocyclus normalis
in the green sandstone and abundantReesidites minimus above that sandstone.
On the western wing the Mikasa Formation contains less commonly ammonites
and inocerami, except for the lowest
part, but more abundantly trigonians.
Therefore, Inoc. labiatus is not found.
Only a remarkable bentonitic tuff at the

midst of the sandstone formation (exposed at loco Ik 2017 of the Pombetsu
route) suggests the .possibleposition ofLower Turonian. A 130m sequence (IlIa')of fine sandy siltstone above the Mikasa
Formation exposed along the Pombetsu
route represents the Upper Turonian by
the occurrence of Subprionocyclus neptuni,
S. normalis (loc. Ik 2014) and then Reesidites minimus (loc. Ik 2013b) and also
Prionocyclus coMani, Pro aberrans and
Pro wyomingensis (loc. Ik 2012) (see MATSUMOTO, 1965, 1971). lnoc. teshioensis,
lnoc. tenuistriatus and lnoc. incertus occur in this part (especially common at
loco Ik 2014-2013). How far these species
range down cannot be decided along thisroute, because IlIa' is underlain by massive pebby sandstone of the upper partof the Mikasa Formation, which contains
trigonians (Steinmannella), the facies
unfavourable for inocerami.
(5) Ashibetsu area. For this area two
geological maps are available, one by
TANAKA and IMAI (1953) and the otherby YOSHIDA and KAMBE (1955). MATSUMOTO partly cooperated witn them inthe survey of selected routes and subsequently made another investigation,with OKADA, along the route of the
Soashibetsu, an eastern branch of theRiver Ashibetsu.
The area is divided to two parts by a
syncline. In the western part the Mikasa
Formation is extended northward fromthe Ikushumbetsu area, but in the easternarea a thicker sequence of mudstone
predominates in the Cenomanian andTuronian parts. Alternating sandstoneand shale of the flysch facies occur frequently there and especially in the mainpart of the Turonian, forming a lithostratigraphic equivalent of the Saku Formation. The strata are overturned andaffected by minor folding, thrusting andfaulting in the eastern part, but in a

653.

Notes on Inoceramus labiatus·rough estimation the Turonian may be
about 400m or more. Its upper part,about 100m, consists of shale and sandy
shale with some intercalations of thinlayers and laminae of sandstone. Inoceramus teshioensis occurs there. Its middle part, about 200m, is made up ofalternating sandstone and shale, withoccasional occurrence of thick sandstonewhich may show a channel structure.
Flute casts are common. Inoceramus
hobetsensis and Jimboiceras planulatiforme occur in the middle part. The
lower part is similar in lithologic constitution to the middle part but Inoceramus cf. labiatus was found there (loc.
As 1039), along with Puzosia intermedia
orientalis and Allocrioceras sp. Thesefossils were contained in a calcareous
nodule embedded in a mudstone of thealternation.
(6) Oyubari area. A geological map of
the Oyubari sheet by NAGAO et ai. (1954)
is available. The upper reaches of theRiver Yubari [=Shiyubari] in the northeastern part of the sheet was biostratigraphically studied by MATSUMOTO(1942, p. 215-243, maps of pI. 13-15). The
southern part of the same sheet has
recently been investigated by MATSUMOTO and OKADA (1973) and now underinvestigation by TANABE, HIRANO and
MATSUMOTO.
As in the eastern Ashibetsu area thestrata are overturned and cut at intervals
by minor thrusts and faults. Therefore
it is fairly hard to establish a precise
biostratigraphic succession. The Upper
Albian through Turonian is comprehensively called the Middle Yezo Group,
which consists primarily of mudstone
with members of alternating sandstoneand shale at intervals. On the basis ofa detailed field work on good exposures
along several routes in the upper reachesof the Shiyubari, MATSUMOTO (1942)

193

subdivided the group into 18 members ella
to lIs), of which lIm, lIn, IIp, lIq, lIr andlIs, about 400 to 500m thick, were regarded as lithostratigraphic equivalent of the
Saku Formation on account of generalsimilarity in lighology and fossil contents.
Member lIm, less than 100m, however,should be referred to a part of Cenomanian, because it contains Marshallites
olcostephanoides and Inoc. pennatulus.
The succeeding Member lIn, fine sandy
siltstone or silty fine sandstone, about
100m, with intercalated layers of calcareous sandstone and bentonitic tuff isregarded as Lower TuroIiian, since it
contains Inoc. labiatus. Inoceramus n.
sp. (undescribed species apparently allied
to Inoc. teshioensis), Puzosia intermedia
orientalis and Sciponoceras orientale arefound from lIn in addition to other longranging ammonites. The overlying members IIq to lIs contain more commonly
Inoc. hobetsensis and lIs has Inoc.
teshioensis. Among ammonites Yubariceras yubarense came from lIq and IIr,
whereas Subprionocyclus neptuni from lIs.
The biostratigraphic succession in thesouthern part of the Oyubari area is best
observable along the section of the
Hakkin-zawa [=Shirokin-zawa].
RecentlyTANABE. HIRANO and MATSUMOTO
have recognized a bed of shale at loco
Y5228 which contains remains of Inoc.
labiatus in abundance in several laminae.
Fossils of the same species were obtainedat another locality nearby Y5226. These
are within a unit of siltstone, more orless fine sandy, with occasional interbeds
of calcareous sandstone and noticeable
bentonitic tuff. This unit is exposedfrom loco Y5226 to loco Y5232, at least
150m in thickness and contains another
Inoceramus (Inoc. n. sp. aff. I. teshioensis),
Sciponoceras orientale, Damesites cf. laticarinatus, immature shells of desmoceratids, etc. It is very similar ·to.and194

Tatsuro MATSUMOTO and Masayuki NODA

probably an extension of Member IIn of
the Shiyubari section.
About 100m sequence which conformably underlies the above explained unit
consists of mudstone with more frequentinterbeds of sandstone and less frequentand thinner tuff, as is finely exposed atlocs. Y5233 and Y5234. It contains large
fossils of lnoc. pennatulus, Austiniceras
sp. and Pachydesmoceras sp. It is probably an extension of Member IIm of
the Shiyubari section. Thus the Cenomanian-Turonian boundary should besomewhere near the boundary of Y5232
and Y5233, although good guide species
have not yet been found at the very
boundary.
The sequence which comes above theunit with lnoc. labiatus is exposed ratherintermittently for a longer distance fromloco Y5225 to Y5200 along the lower
course of the Hakkin-zawa. It is madeup of clayey to silty mudstones oftenwith fine sandy laminae and sometimes
with thin interbeds of sandstone andtuff. The strata seem to be repeated byminor folding and thrusting and the true
thickness is hardly estimated. For themost part of this sequence occurs lnoc.
hobetsensis and in the uppermost partlnoc. teshioensis. Scaphites and otherheteromorph ammonites are common;
drifted fragments of wood which is often
suffered from Teredo tubes occur frequently in calcareous nodules along withammonites and inocerami as in othercases of the Saku Formation. At loco
Y5206 Collignoniceras woollgari andRomaniceras aff. deverianum were identified (MATSUMOTO, 1971, '73).
As a supplementary route the Takinosawa [=Penkemoyuparo], a branch of the
Hakkin-zawa, may be selected. MATSUMOTO and OKADA (1973) collected a number of specimens labelled provisionallyas blOC. aff. teraokai (which is revised

as lnoc. labiatus in this paper) from loco
Y5102 and Y5109. They are in a unitof fine sandy siltstone with intercalated
layers of bentonitic tuff and sandstone.
lnoc. n. sp. aff. 1. teshioensis occurs inthe same unit (iocs, Y5102-Y5113). A
large specimen of Fagesia sp. was obtained by K. MURAMOTO in a transported nodule at a point somewhat downstream of Y5102. In the mudstone (atloco Y5101) immediately above Y5102
occurs lnoc. hobetsensis, whereas lnoc.
pennatulus and lnoc. concentricus costatus
are found in the subjacent mudstone
with frequent interbeds of sandstone(iocs. Y5114-Y5117). Thus the lnoc.
labiatus-bearing unit is referable toMember lIn of the Shiyubari section.
The bed exposed at loco Y5102 probably
represents the uppermost part of IIn.
In the Hobetsu area to the south of
the Oyubari area lonc. labiatus has not
yet been found.
Middle to Upper
Turonian strata are more extensively
exposed there, as is expressed by the
specific names of lnoc. hobetsensis andlnoc. iburiensis. Lower Turonian strata
should crop out somewhere within thearea though narrowly, because Fagesia
n. sp. (undescribed) was found in one of
the transported nodules of the Nutapomanai (collection of the Hokkaido Colliery & Steamship Co., at Yubari). Although geological structure is fairly complicated in this area, future discoveriesof lnoc. labiatus as well as ammonites insitu would give valuable key to settle
certain problems.
(7) Furano area. This area belongs tothe eastern belt of the Cretaceous in central
Hokkaido, whereas the foregoing areas(1 to 6) all belong to the western belt.
The two belts are separated by a beltof the Kamuikotan blue schists and serpentllllte. The Cretaceous deposits inthe eastern belt, except for certain limited

653. Notes on Inoceramus labiatus
portions, are generally poor in fossils,
because sediments of the flysch facies
predominate there and because the strata
are tectonically much disturbed.
In the Furano area the fossiliferous
Turonian is exposed in a limited portion
along the River Sorachi between thevillages called Yamabe and Kanayama.
A geological map by W. HASHIMOTO(1953) is available for the area and a
sketch map around the fossil localities
was shown with a stratigraphic note by
MATSUMOTO and HASHIMOTO (1953, textfig. 1 and p. 100). Their description on
the stratigraphy of the fossiliferous beds
is essentially correct, but what theycalled lnoc. incertus in that paper should
be revised as lnoc. labiatus.
It should be noted that the lower half(i. e. KY9E) of the 70m sequence exposedat loco KY9, which consists of alternating mudstone and sandstone, contains a
fossiliferous bed rich in lnoc. labiatus,
whereas the upper half (i. e. KY9W),
made up of predominant mudstone, extends southward to loco KY301, where
Pseudaspidoceras sorachiense and a somewhat broader form of Inoc. labiatus (asrepresented by GK. H10060) were obtained.
As there is a major fault on the westside and as the strata are repeatedly
folded on the east side and then covered
by Cenozoic valcanic ejecta, more continuous succession cannot be observed at
this place.
(8) Urakawa area. This is situated in
the southern part of the eastern belt.
It is famous for rich fossils since the.
date of YOKOYAMA (1890), but the fossiliferous beds mostly belong to theSenonian. Turonian and older strata
are rather poor in fossils and tectonically complicated. KANIE (1966) reported
a revised stratigraphy of this area, inwhich Coniacian to Lower Maestrichtian

195

sequence was finely subdivided. According to him a specimen of Inoc. labiatus
was obtained at Higashi-horobetsu froma mudstone bed in the block of the Middle Yezo Group bounded by faults. The
stratigraphic sequence is not precisely
known in this block.
Summarizing the foregoing stratigraphical note, the following may be led asa conclusion.
(1) Inoceramus labiatus is distributed
widely in the Cretaceous deposits of
Hokkaido from north to south and inboth the western and the eastern belts.
(2) It occurs characteristically in thelower part of the Turonian. sequence.
The zone of Inoc. labiatus is distinguishable from that of lnoc. pennatulus below
and that of lnoc. hobetsensis above.
(3) The stratigraphic sections of theabove explained areas (which include thelocalities of lnoc. labiatus) may be correlated as shown in Text-fig. 2.
(4) The formational unit which contains
lnoc. labiatus occupies the part approximately as thick as or somewhat less thana third of the entire Turonian sequence,as far as the well investigated areas areconcerned.
(5) In the same unit occur certain ammonite species which indicate a Lower
Turonian age, such as Fagesia thevestensis, Fagesia sp., Vascoceras aff. durandi, Pseudaspidoceras sorachiense etc.
Allocrioceras sp., Scipono.ceras orientale,
S. kossmati, Damesites aff. laticarinatus
and Puzosia intermedia may be alsocharacteristic, although some of them
may slightly extend beyond the unit. At
present further subzonal subdivision of
the labiatus zone is practically impossible.
(6) lnoc. labiatus seems to have a certain stratigrapyic range, as is suggested
by its occurrences in the Kotambetsu.
Oyubari and Furano areas. Whether or196

Tatsuro MATSUMOTO and Masayulci NODA
OBIRA

a:
UJ

a.
a.

I KUSHUMBETSU

SAKU

KOTAMBETSUOVUBARI

,
,, ,
,
, ,

_._._.-

:::>

,

I

(

I III

(I

oR 2004
R2026

-

,
I

..... .

~Ir I 'I
\

(

f

c

r

(

I

\,

I
I

\
I

(

\

I I I

,,

(
{

,

z
o

I I \ I

I

1\

Z

<t

....

I

I

UJ

Cl
Cl

,,

,

0::

,,

a:
UJ

_R137/
v V""/",vv I'" -.-YsTo2:---- -~:....--:-:.... -----,.'._.~ .. ~. oV5109
oRI23

o T1158

o V5228

o T5090

O-TSO-4S-- _._._._. 0_V§Q~~5'pP

I \.........
. . . . . . . . .. ----"\

I

,,

~

"""VVVII'II

, ',
I

I

{
\

• R 522 2
oR5231ba:o R5243

, ,
\

I

I I

I

oRllO

S

I
(

\

,

I

f

VV!lV'"----\,

oT5031\

UJ

a.
a.
:::>

I

,, I \ I I\ \ \ Io RI06

,

-- --

,,
,,
,,
,,
,,

oRIOO

I( I I I I
I

I

I

\

\ I

Z

o R3011
UJ

....
®
_.

LEGE NOt-~0,,I, I , I oR 5211
VvvvVll VVI\

o R114:J,-----1

,
I

I

I

~

I

Cl
Cl

,

I I I

I

,_~_I.~

(

(

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\

\

I

I I I

1\

1\

\ I'

oR81

I

<t

Z

::;:

<t
~

!

0
Z
W

500 m

U

a:
UJ

I I , I,
I I

\ II

~
Cl

_~~.L.LJ_'-,·;~·.~.i~· j' -------

o

,
,,

........ ,. -----,

Text-fig. 2. Diagram showing the Cenomanian to Turonian sequences of selectedareas in Hokkaido. a: mudstone, b: fine-sandy siltstone, c: sandstone, d: conglomerate,e: alternation of sandstone and shale, f: slump structure, g: abnormal conglomerate(fluxoturbidite?), h: limestone.

653.

197

Notes on Inoceramus labiatus

not there is any chronological change
during that time range is to be palaeontologically examined (see below).
Palaeontological note
Material. The specimens listed inTable 1, from the localities in Hokkaido
explained in the preceding pages, areconcerned with the present description.
Some of the extra-Japanese specimens,
which one of us (T. M.) observed at the
British Museum (N. H.),
Sedgwick
Museum, U. S. National Museum, U. S.
Geological Survey (Denver), Universityof Kansas and California Academy of
Sciences, may be referred to for comparison.

Table 1. Material.
specimen(L) = left valve, (R) = right valve

area(Fig. 1)

samplesample
size

T5090

2

GK. Hl0044 (L), HI0046(R)

(1)

T.M.

R114

1

GK. H1OO39(L)(2)

T.M.+H.O.

R123

3

GK. Hl0041 (L), H10042(L), H1OO43(R)(2)

T.M.+H.O.

R2302p2

GK. Hl0056(L), H1OO57(L)(3)

M.;T.M.

R4802

3

GK. H10074(L), H10075(R), H1OO76(L)(3)

H.H.+K.T.

IklO38

1

GK. H1OO45(R)

(4)

M.

AsI0391

GK. H1OO47(L)

(5)

T.M.

Y418

1

GK. H519(L)

(6)

T.M.

Y500

1

GK. H522(L)

(6)

T.M.

Y502

5

GK. H520a(R), b(R), H521a(L), b(R), c(L)

(6)

T.M.

Y5102

9

GK. Hl0048a(R), beL), HlOO49(R),H10050(L), H10051(R), HlOO53(L),H10099(L), H10100(R), H101Ol(L)(6)

T.M.+H.O.

Y5109

3

GK. H10052(R), H10054(L), H1OO98(L)(6)

T.M.+H.O.

Y5228h8

GK. H10061(R), H10062(R), HlOO63(L),Hl0064(L), HlO065(L), H1OO66(R),H10067 (R), HlOO68(R)(6)

K. T.+H.H.
+T.M.

Y5194b1

GK. HI0078(R)

(6)

H.O.

KY9E

4

GK. H10040(L), HlO102(L),JG. H2128(L), JG. H2129(L)(7)

W.H.+K.F.
+T.M.

KY301

1

GK. HI0060(R)(7)

T.M.+W.H.

U413

1

G. P. Ur413001(L+R)

(8)

Y.K.

collector

Collector: H. H. =Hiromichi HIRANO, H.O.=Hakuyu OKADA, K. F. =Koji FUJII, K. T. =Kazushige TANABE, M.=Tatsuo MURAMOTO, T.M.=Tatsuro MATSUOMTO, W.H.=Wataru
HASIIIMATO, Y. K. = Yasumitsu KANIE. Repository. G. K. Type Room, Department of
Geology, Kyushu University, G. P. =KANIE Collection, JG. =NODA Collection.

198

Tatsuro MATSUMOTO and Masay'uki NODA
Table 2.

Dimension of L at successive growth stages.

above: length in mm.
SampleY5228h

Y5109

specimen

H=20mm

30mm

40mm

50mm

60mm

70mm

80mm

GK. HI0061
(R)

16.6
(0.83)

24.8(0.83)

29.5(0. 74)34.5(0.69)

38.2(0. 64)4l. 8(0. 60)47.0(0.59)

GK.HlO062(R)

16.9(0.85)

23.8(0.79)

27.5(0.69)

32. 1(0.64)

35. 7(0. 60)GK. HI0063
(L)

14.5
(0.73)

2l. 2(0.7l)

27.8(0. 70)30. 7(0.61)

33.3(0.56)

38.0(0. 54)

GK. HI0064
(L)

16.8
(0.84)

22.8(0.76)

28. 7(0.72)

32.4(0. 65)

36. 1(0. 60)4l. 5(0. 59)47. 7(0. 60)GK.HlO066(R)

15.6(0. 78)2l. 0(0. 70)26.6(0.67)

3l. 5(0. 63)36. 7(0.61)

GK. HI0067
(R)

14.9
(0. 75)2l. 0(0. 70)26.0(0.65)

3l. 0(0. 62)35.8(0.60)

38.2(0.55)

45.0(0. 56)

GK.HI0068
(R)

15. 7
(0. 79)21. 0(0. 70)26. 7(0.67)

33.0(0.66)

16. 7(0.84)

24.6(0.82)

31. 5(0. 79)36.2(0.72)

4l. 0(0. 68)47. 7(0.68)

53.4(0.67)

17.3

24.0(0. 80)32.0(0. 80)18. 7(0.94)

24.6(0. 82)34.9(0. 87)

GK. HI0049
(R)

18.0
(0. 90)24.2(0.81)

33.0(0. 83)

GK. HlO051
(R)

18.8
(0.94)

GK. HlO053
(L)

19.4
(0.97)

28. 1(0.94)

36.0(0.90)

GK. H520a(R)

17.9(0.90)

2l. 7(0. 72)27.6(0. 69)GK. H520b(R)

14.0(0.70)

20.2(0.67)

GK. H521a(L)

12.0(0.60)

18.3(0.61)

GK. H521b(R)

13.6(0.68)

GK. H521c(L)

18.4(0.92)

25.0(0.83)

35. 1(0.88)

GK. HI0039

16.0(0.80)

2l. 3(0.7l)

27.6(0.69)

GK. HlO052(R)
GK. HI0048a
(R)

I
I

I (0.87)

GK. HI0048b
(L)

Y5102

Y502

R1l4

below: L/H in parentheses.

(L)

I

43.8
(0.88)

II
30. 7(0.61)

35.0(0.58)

I

653. Notes on Inoceramus labiatus
SampleI

specimen

H=20mm

30mm

40mm

50mm

GK. HlO041

18.3(0. 92)26.3(0.88)

32.1(0.80)

35.6(0.71)

GK.HlO042

(L)

19.0
(0.95)

26.6(0.89)

GK. H10043
(R)

18.2
(0.91)

25.2(0.84)

GK. H10056

17.7(0.89)

25.4(0.85)

31. 7(0.79)

38.3(0.77)

GK. HlO057

19.5(0.98)

25.3(0.84)

33. 7(0.84)

41. 7(0.83)

18.4(0.92)

25.0(0.83)(L)

R123

R2302p(L)(L)

GK. H10074
(L)

R4802

GK. H10075(L)
GK.H10076

Ikl038

KY301
U413

60mm

70mm

43.8
(0.73)

46.8(0.67)

37.4(0.53)

19.8(0.99)

27.7(0.92)

34.5(0.86)

GK. H10045
(R)

18.0
(0. 90)25. 6(0.85)

31. 9(0.80)

39.5(0. 79)JG. H2128

11. 7(0.59)

18. 1(0.60)

23. 7(0.59)

30.5(0.61)

33.4(0.56)JG. H2129

15.2(0. 76)20.0(0.67)

23. 1(0.58)

27.0(0. 54)27.0(0.45)

GK. H100,lO
(L)

16. 7
(0.8el)21. 8(0.73)

25.8(0. 65)30.0(0. 60)34.6(0.58)

39.9(0.57)

GK. HI0060
(R)

19.2
(0.96)

24.8(0. 83)32.6(0.82)

40.0(0.80)

16.0

22.0(0.73)

27. 1(0.68)

33.5(0.67)

38.8(0.65)

43.2(0.62)(L)

GPUr413001

(L)

80mm

19.4
(0.97)

(L)

(L)

KY9E

199

I (0.80)

Diagnosis. Shell of moderate size,
nearly equivalve, inequilateral, oblique,typically mytiliform, much elongatedfrom the umbo to the postero-ventral
extremity; umbonal region moderately
convex, with steep or almost verticalantero-dorsal part; shell gradually becoming less convex with growth, withrather gently sloping anterior part andflattened posterior part. Umbo terminalor nearly terminal, slightly projected
over the hinge-line. Narrow posterior ear
may be discernible in some specimens,

41. 2(0. 52)48.8(0.61)

e. g. GK. HI0039, Hl0053, Hl0056 and JG.
H2129).
Hinge-line rather short, less than halfof the shell length, though variable to acertain extent. Obliquity of the shell
gradually enlarged with growth, withdecreasing angle between the hinge-line
and the growth-axis, resulting in anteriorly convex growth-axis. Anterior
margin gently curved, passing to a long,broadly arcuate ventral margin; posteroventral extremity narrowly rounded in
the typical from but less so in some

200

Tatsuro MATSUMO TO' and Masay~~ki NODA

others, and rather abruptly bent to thelong nearly stratight posterior margin,
which, in turn, forms an obtuse angle
with the hinge-line.
Surface ornamented with concentricribs and numerous concentric rings. The
concentric ribs of moderate intensity on
the convex younger part and also theanterior part but rather low on the rest
main part, wavy in cross section withrounded top, normally regularly disposed ,separated by inters paces nearly as narrow as the ribs, but occasionally crowded
or rather irregularly disposed (e. g. GK.

HI0056 and H519). The concentric rings
developed on ribs and inters paces inparallel to them, but may not be discernible on the internal mould. Fine
parallel striae may be discernible on theposterior ear.
Biometric analysis. To know the actual
state and meaning of the variation, abiometric analysis of selected charactersis here attempted on the samples of different stratigraphic and geographic positions, although the available material isinsufficient for more comprehensive examination at population level.
The basic morphology is illustrated in
Text-fig. 3, with indication of measurable characters. The proportion of L to
H is considerably variable as shown in
Table 2, but as a rule it grad ua lly decreases with growth. Measurements aredone at successive growth stage in eachspecimen.
Two samples from the Oyubari area
are specially taken, Y5228h (N=7) andY1202 (N =4). The former is probably
H

90
80
70 .

Text-fig. 3.
Basic morphology andmeas.u~ements of Ino ceramus labiatu s. HL:
hinge line (length of the- hinge-line andits proportion to shell length are to beme asured), H: maximum dimension f rom
the umbo to the postro-ventra l extremity(which s ho uld be measured along the
gr0:wth-ax is, but here conventionally measured a long the stra,ight line), L: maximum
dimension of t he line perpendicular to H,
L./H : proportion of L to H, 1: shell lengt h,i. e . the maximum dimension from anterior
to. posterior in parallel to the hinge-line,
h: shell length, i. e. the maximum dimension perpendicular to 1, l/ h: proportion of
1 to h , d: a·ngle between the hin ge· line
and growth-a xis, obliquity may be expressed, as gOO-d.

60

cP •
o

SO

0 0

40

o

o

.

....

•

•

0 0
o •

30

20

GK H 1 0061
GK H 10064
GKH1Q067
GK H 1 0053

10

9GKHIC049

7

a 910

:2 0

30

40

SO 60 7080lm m

Text-fig. 4. Scattered diagram s ho wing the correlation of bivariables of Hand
L in indi v idua l g ro wth. empty signs:
specimens of Sample Y5228h; solid signs:
specimens of Sample Y5102.

653. Notes on Inoceramus labiatus
of lower horizon than the latter in thesame area, as is explained in the stratigraphic note. The correlation of thetwo variables of Land H in individual
growth stage is examined. As is clearlyshown by the diagram of Text-fig. 4, distinction is clear in the relative growth
between the two samples.
As is evident from the numerical data
in Table 3, the correlation coefficient isvery high in most specimens and there
is a considerable difference in the growthratio (ex) between the two samples. The
significancy of difference in the meanvalue of the growth ratio (ex) in the two
samples is obtained in the following way.
As the order of calculation of Student's ttest, at first F-test should be examined by
the following equation,
F= S,2/ S z"=0. 083 2/0. 045 2 =3. 402
where, s=standard deviation of growthratio (a).
The value of F is less than the value of
5 percent limit of the same degree of freeTable 3.
SampleY5228h

Y5102

I

201

dam. Therefore the significancy of difference in the mean value between the two
samples is judged by the next formula,/~
1 2,\/ N,+N2

x-x=/(7-1)0.083 2 +(4-1)0.045 2
'\/
74-2

=7.581
where,
mean of Sample 1
mean of Sample 2
S,: standard deviation of Sample 1
S2: standard deviation of Sample 2
N , : size of Sample 1
N 2 : size of Sample 2.
From the above calculation, the t value isvery significant comparing the value of 5
percent significant limit at 9 in the degreeof freedom t o•o5 (IJ=9) =2.262.
On the other hand, calculating the coefficience of difference between the two
X,:

X2:

Data of redu.ced major axis of Land H.

Specimenralog {3{3

GK. HlO061
GK. H10062
GK. H10063
GK. H10064
GK. H10066
GK. HlO067
GK. H10068

0.994
0.995
0.989
0.997
0.999
0.998
0.998

1. 386
1..487-0.42090-0.54046-0.26199-0.38493-0.22550-0.21897-0.17133

0.. 379
0.288
0.547
0.412
0.595
0.604
0.674

mean
s

0.997
0.004

1. 3400.083

GK. HlO048a
GK. HlO048b
GK. H10049
GK. H10053

0.997
0.979
0.999
0.997

0.972
0.964
0.984
1. 061

mean
s

0.993
0.009

0.995
0.045

I

1. 323
1. 374
1. 283
1. 289
1. 2380.500
0.138
O. 10960
O. 12082
0.05905-0.02575

1. 287
1. 321
1. 1400.902
1. 163
O. 109

202

Tatsuro MATSUMOTO and Masayuki NODA

Table 4.

Angle between the hinge-line and growth-axis at successive growth stages.

~

10

20

GK. HI0049
GK. HI0056
GK. HI0048
GK. HI0052
GK. HI0053

52
41
45
45
42

45
35

GK. H6836

69

30

40

50

45
42
,10

40
33
42
38
37

36
32
38
35
35

35
31
36

58

50

49

47

Specimensamples by the method of 75 percent rule,
the formula is as follows.
C.D.= X1- X 2 = 1.340:-0.005 =2.695
S1-S2
0.083-0.045
The result suggests the significant value
which is more than the value of conventionalsignificant level of subspecific discrimination(i.e., C.D.=1.28).

In many species of Inoceramus theobliquity gradually decreases withgrowth, with enlarging angle between
the hinge-line and the growth-axis. In
the examined specimens, however, it
gradually increases as is evidently shownby the data in Table 4.
Discussion. The elongate mytiliformwith a small L/H and a large obliquity(90 -d) is a diagnostic character of Inoceramus labiatus (SCHLOTHEIM, 1813), as
represented by the illustrated specimens
of WOODS (1911, text-fig. 37, pI. 50, figs.
1-6) and SEITZ (1934, pis. 36-40). In thisand other characters described under
diagnosis our specimens, especially thoseof the samples Y5228h, Y5109, Y502,
KY9E, R114, R2302p, R4802 and U413,
are certainly identified with Inoceramus
labiatus. There are, however, considerable variations in the ratio between L
and H, obliquity, relative length of thehinge-line, degree of curvature of theribs and growth-lines, rib density andontogenetic changes of these characters.
The variation of L/H and its ontogenetic
0I-change are especially noted, as describedabove.
WOODS (1911) regarded Inoc. latus
SOWERBY, 1828, from the Upper Turonianof England, as a variety of Inoc. labiatus.
It has a relatively longer hinge-line andbroader curvature of the ribs. In otherwords it is a "broad form", having alarger L/H. SEITZ (1934) described indetail six varieties of Inoc. labiatus, inwhich such broad forms as blOC. labiatusvar. hercynica PETRASCHECK, 1904 andInoc. labiatus var. subhercynica SEITZ,
1934 were included.
In the meanwhile we described Inoc.
teraokai MATSUMOTO and NODA, 1968,
which occurs in the Tano Formation of
Kyushu. It is associated with Inoc.
hobetsensis and Subprionocyclus neptuni,
which indicate the middle part of theTuronian in the Japanese biostratigraphic
scale. We have written that Inoc. teraokai is probably intimately related tobrac. labiatus, Inoc. hercynicus and Inoc.
latus. As shown in Text-fig. 6, the scattered diagrams of the individual relative
growth of Land I--l overlap with eachother between the two samples, T A 213(from Kyushu) and Y5102 (from Oyubari,
Hokkaido). The fact implies the closeaffinity of the fossil populations represented by the two samples with respect
to this character. Furthermore, as shownin Table 4, the two samples show the653.

Notes on Inoce?"am~~s labiatus

same tendency in the change of obliquity
with growth. Our previous conclusion
is thus supported by the present examination.
The specimens which constitute thesample of Y5102 were collected by
MATSUMOTO and OK ADA (1973), whocalled them provisionally Ino c. aft. teraolwi. Most of them indeed resemble
typical specimens of Inoc. temolwi from
Kyushu, in their somewhat broader form,
but show more obliquity than the types
of Inoc. temokai (see Table 4 and also
MATSUMOTO and NODA, 1968, table in p.
320). A few of them, e. g. GK. H10099,
are closer to the ty pical form of Inoc.
labiatus in the smaller L/ H, as are thespecimens of sample Y5109, which isprobably of somewhat lower stratigraphic
position than Y5102 in the same Takinosawa route. All of these specimens from203

loco Y5102 and Y5109 do not show ananterior ear which is characteristic ofInoc. teraolwi. We now consider themwithin the extent of variation of Inoc.
labiatus. Sample Y5102 can be regarded
as representing a broader variety ofInoc. labiatus.
As is elucidated from the results ofStudent's t-test and the 75 percent rule,the sub specific discrimination between
the two pupulations of the samples
Y5228h and Y5102 is reasonable, since
they are chronologically separated. We
hesitate, however, to give a subspecificname, since it is necessary to examine
extra-Japanese materials to settle thenomenclatorial problem.
Although a sample size is small, othersamples in Hokkaido seem to support
the above conclusion. For example, three
specimens (one of which, GK. H10041 , iscaText-fig. 5. Ino ceramus labiatus (SCHLOTHE IM). GK. H521a- c, fromloco Y502, the Hinata-zawa , a branch of the Shi yubari, Member lIn (ofMATSUMOTO, 1942), Middle Yezo Group. The figure shows an associationof a t y pical (a), intermediate ( b) and broad (c) forms.

Tatsuro MATSUMOTO and Masayuki NODA

204

figured, PI. 18, Fig. 5) of sample R123
show larger L/H than a typical exampleof R114 of somewhat lower stratigraphic
level in the same Kotambetsu section.
Similarly an example of KY301 represents a broader form as compared withthe typical one of KY9E of somewhat
lower level in the Furano (Sorachi-gawa)section. It is noted that at loco Y502 acomparatively broader form occurs together with an intermediate and a typicalones (GK. H521 a-c, Text-fig. 5). However, whether this locality is allocatedat a level between Y5228h and Y5102 orotherwise is hardly decided by the available field data.
In the meanwhile HASHIMOTO and
KOIKE (1973), based on MATSUMOTO'S
preliminary identification, recorded theoccurrence of "lnoc. teraokai or lnoc.
latus" in the Kakaan Formation of Kalimantan in association with a "typicalform of lnoc. labiatus." This fact isinteresting in that it shows the same
H

90
80
70

60
50
40

30

20
GKH6836
JGH 2123
JGH2125
GKH 10053

10
9
8

•

GKH 10049·40

50607080

7
7 8910

20

30

L mm

Text-fig. 6. Scattered diagram showing the correlation of bivariables of Hand
L in individual growth. solid signs: specimens of Sample Y5102, (broad form of
Inoc. labiatus); empty signs: specimens ofSample T A 213 (Inoc. teraokai MATSUMOTO
and NODA, 1968).

case as that of Y502.
In Germany SEITZ (1934) concluded
that the six varieties of lnoc. labiatus,in which broad forms are included, do
not show orderly succession but occur
together in the two shafts of Gneisenau
and Sieletz.
In England WOODS (1911, p. 283) remarked that "this species [i. e. lnoc.
labiatusJ is mainly characteristic of thezone of Rhynchonella cuvieri. In thezone of Terebratulina lata it is not common, and the shell is usually relatively
longer than in typical forms of thespecies." WOODS furthermore described
the specimens from the zone of Holaster
planus under lnoc. labiatus var. latus.
We should like to know how this classic
record would be expressed in terms of
the up-to-date palaeontology.
In the United States COBBAN and
SCOTT (1972) have recently shown thatlnoc. labiatus is considerably long ranging, from the zone of Watinoceras coloradoense via that of Mammites nodosoides
to that of Collignoniceras woollgari, inthe Bridge Creek Limestone Member of
the Greenhorn Limestone and furthermore recorded (in p. 19) a broad variety"lnoc. labiatus var. subhercynica" in theuppermost part of the same sequence(i. e. in the lower part of the Fairport
Chalky Shale Member).
This "variety" is associated with Collignoniceras woollgari, a distinct index
of the Middle Turonian. The association
is similar to that of lnoc. teraokai andSubprionocyclus neptuni in the Tano Formation of Kyushu.
In Japan lnoc. incertus JIMBO, from theUpper Turonian of Hokkaido, resembles
a broad form of lnoc. labiatus, but isdistinguisded from the latter and also
from lnoc. teraokai in having a decreasing obliquity with growth. In otherwords the growth axis is concave to the653. Notes on Inoceramus labiatus
d
75
70
65

r

60

~ ~ ~•'n. incertus

55
50~ II ~ ~ E •In.leraokai

45~ ~ HB

40
35.t.
In. lab iatus

30

10

20

30

40

50

60

Hmm

Text-fig. 7. Diagram showing the
ontogenetic change in obliquity of lnac.
labiatus, lnac. teraakai and lnac. incertus.

anterior in lnac. incertus but convex inlnac. labiatus.
The diagram of Text-fig. 7 shows the
ontogenetic change of obliquity in thethree species, lnac. labiatus, lnac. teraakai
and lnac. incertus. With respect to theobliquity lnac. labiatus and lnac. incertus
are indistinguishable at the immature
stage with H=10mm. This fact is not
negligible for the phylogenetic relationship of the two species.
Should the tendency to decrease theobliquity be still more exaggerated, together with lengthening of the hingeline, such forms as lnac. yubarensis NAGAO and MATSUMOTO, 1940 and lnac.
mantelli BARROIS, 1879 (see SEITZ, 1962)of the Coniacian could be led.
Turning back to the Upper Cenomanian,
we have little material in Hokkaido toconsider the origin of lnac. labiatus. As
has been explained in the stratigraphical205

note, the upper part of the Cenomanianin Hokkaido is characterized by lnac.
cancentricus castatus NAGAO and MATSUMOTO, 1939 and lnac. pennatulus PERGAMENT, 1966, (with which lnac. reduncus
PERGAMENT, 1966 may be included). The
last species is probably an enlarged
offshoot of the inequivalve cancentricus
group and has nothing to do with thelabiatus group. The only available material is a few imperfectly preserved
specimens, from loco R5404 about 100m
below the key tuffite in the Obira area,
which may be comparable with lnac .
reachensis.
WOODS (1912) interpreted that lnac.
reachensis ETHERIDGE, 1881 [=lnac.
crippsi var. reachensis of WOODS, 1911J,
from the zone of Halaster subglabasus,
was the ancestor of lnac. labiatus. According to a preliminary observation by
one of us (T. M.) of the type specimens
in the Sedgwick Museum and the British
Museum (N. H.), lnac. reachensis has alarger L/H and less obliquity than typicalforms of lnac. labiatus and, accordingly,
more similar to lnac. latus. It could
then be considered as a working hypothesis that there was a slowly evolving
main series from lnac. reachensis of theUpper Cenomanian to lnac. latus of theUpper Turonian and that lnac. labiatus
was a specialized offshoot in the Lower
Turonian which acquired a mytiliform
outline.
The above discussion may have connection with the definition and scope of
Mytilaides BRONGNIART, 1822, but we do
not intend to go into this problem on
this occasion. For the time being we
use the generic name lnaceramus in a
broad sense.
In conclusion we should like to suggestthat examination ofmorphologicalchanges from population to population

206

Tatsuro MATSUMOTO and Masayuki NODA

would be useful not only for the refinement of biostratigraphic subdivision but
also for the elucidation of phylogenetic
relationships. The study of [noc. labiatus
and its allied species should be carriedon in such areas where numerous wellpreserved specimens are obtainable atsuccessive stratigraphic levels.
References

CJ +E=in Japanese with English abstract)
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near Pueblo, Colorado. U. S. Geol. Surv.
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(ed.) (1967): Geology and Mineral Re·
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vol. 13, p. 163-184, pIs. 18-21.
HASHIMOTO, W., NAGAO, S. and KANNO, S.
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(1958) : Horokanai. Expl. Text Geol. Map
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KANIE, Y. (1966): The Cretaceous deposits
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--- (1959): Zonation of the Upper Cretaceous in Japan. Ibid. vol. 9, no. 2, p.
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- - (1965): A monograph of the CoIIignoniceratidae from Hokkaido. Part I.
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Hokkaido. Mem. Fac. Sci., Kyushu Univ.
ser. D, vol. 22, no. 2, p. 99-163, pIs.
11-23.
MATSUMOTO, T. and HASHIMOTO, W. (1953) :A find of Pseudaspidoceras from Hokkaido, Japan. Trans. Proc. Palaeont. Soc.
Japan, N. S., no. 12, p. 97-102, pI. 10.
MATSUMOTO, T. and KAWANO, T. (1975):
A find of Pseudocalycoceras from Hok·kaido. Ibid, no. 97, p. 00-00, pI. 00.
MATSUMOTO, T., MURAMOTO, T. and TAKA·HASHI, T. (1969): Selected Acantho·
ceratids from Hokkaido. Mem. Fac. Sci.,
Kyushu Univ., ser. D, vol. 19, no. 2, p.
251-296, pIs. 25-38.
MATSUMOTO, T. and NODA, M. (1968): An
interesting species of Inoceramus fromthe Upper Cretaceous of Kyushu. Trans.
Proc. Palaeont. Soc. Japan, N. S. no. 71,
p. 317-325, pI. 32.
MATSUMOTO, T. and OBATA, I. (1965): A
monograph of the Baculitidae from Ja·
pan. Mem. Fac. Sci., Kyushu Univ., ser.
D, vol. 13, no. 1, p. 1-116, pIs. 1-27.
MATSUMOTO, T. and OKADA, H. (1973): Saku
Formation of the Yezo geosyncline. Sci.
Repts., Dept. Geol., Kyushu Univ., vol.
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MATSUNO, K., TANAKA, K., MIZUNO, A. and
ISHIDA, M. (1964): Iwamizawa. Expl.
Text Geol. Map Japan, 1: 50,000, 168+
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NAGAO, T. and MATSUMOTO, T. (1939,1940) :A monograph of Cretaceous Inoceramus
of Japan. Part I. Jour. Fac. Sci. Hokkaido
Imp. Univ., ser. 4, vol. 4, nos. 3-4, p.
241-299, pIs. 23-24 (1939); Part II, Ibid.,
vol. 6, no. 1, p. 1-64, pIs. 1-12 (1940).
NAGAO, S. (1962): Teshionakagawa. Expl.
Text. Geol. Map Japan, 1: 50,000, GeoI.
Surv. Hokkaido, 39pp., 1 map (J +E).
NAGAO, S. OSANAI, H. and SAKO, S. (1954):

653. Notes on Inoceramus labiatus

207

Oyubari. Expl. Text. Ceo!. Map japan,
1: 50,000, Geol. Surv. Hokkaido, 121pp.,
9 pis., 1 map U +E).
PETRASCHECK, W. (1904): tiber Inoceramen
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50,000, Geol. Surv. Japan, 78+2Ipp., 8
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31pp., 1 map U +E).
P. S. This work has been done within theframework of the IGCP project entitled"Mid-Cretaceous Events".

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mJi:'*

208

Tatsuro MATSUMOTO and Masayulci NODA

Explanation of Plate 18(All figures of natural size)
Figs. 1-6. Inoceramus labiatus (SCHLOTHEI"-'I).
Fig. 1. JG. H2128, plaster model of a left valve originally preserved at GK. Loc. certainly
same as that of GK. H10040.
Fig. 2. GK. H10056, left valve (MURAMOTO ColI., 1971), from loco Ob. rp. 002p=R2302p of
T. MATSUMOTO, 82 Rimpan, Nakakinembetsu, Obira area.
Fig. 3. GP. Ur413001, both valves. (KANIE ColI., 1966), from loco U413, Higashi-horobetsu,
Urakawa area. Lateral view of the right valve (a) and anterior view (b).
Fig. 4. GK. H10040, left valve (MATSUMOTO, HASHIMOTO and FUJII Coil., 1952), from loco
KY9E, right bank of the River Sorachi, about 100m downstream from the confluencewith the Nishitappu-zawa, Furano area.
Fig. 5. GK. H10041, left valve (MATSUMOTO ColI., 1967), from loc. R123, a branch of the
Futamata-zawa, on road side, about 1600m west of the Kiritachi pass, Kotambetsu area.
This was called Inoc. sp. aff. Inoc. labiatus by MATSUMOTO and OKADA, 1973.
Fig. 6. GK. H10048 a, right valve (MATSUMOTO and OKADA ColI., 1969), from loco Y5102 h,
Takinosawa, Oyubari area. This was labelled as Inoc. sp. aff. Inoc. teraokai by MATSUMOTO and OKADA, 1973.
Fig. 7. Inoceramus teraokai MATSUMOTO and NODA. JG. H2125, left valve (NODA Coil. aided
by A. KAI, 1969), from loco TA213, an eastern hill-side near the Meiji-bashi, Ushirogawachi, Notsu-machi, Ono-gun, Oita Prefecture, Kyushu, upper member of the Tano
Formation.

MATSUMOTO and NOD A :Inocemmus labiatus

Plate 18

Trans. Proc. Palaeont. Soc. Japan, N. S., No. 100, pp. 209-219, pIs. 19-22, Dec. 25, 1975

654.

AN ARMORED WORM FROM THE MIOCENE YOKO-O
FORMATION, NAGANO PREFECTURE, JAPAN*
KOTORA HATAI and HIROSHI NODA
Saito Ho·on Kai Museum of Natural History
and Institute of Geoscience, the University of Tsukuba..

*!l!fJli!<*~;f1t~~JfI~1f%l!:~=B.!F,1t;{:it;::"?\,'"(; *!I!f!Jf!-*~;f1t~~JfI*$J: f) ~I±l Lt':1fm!:~=B.!F,1t;{:i0)5tJiJtJ:0)~M C, -=to)~1±l-t o~f3J(;'fiO):ltmmmt;::"?\, ,"(~ 0':0%I!:

1f%l!:~=B.!F,1t;{:iltifH~~ 2-3 mm, *~~ 50 mm t;::~-to'lf~O)IE'ilt%l!:~~i'$£c L,~t;::lt, :iG:J;lBlIJtJ:~*~, 1*~m:&Lf;f$E~O)kffiHP¥a-1f-too 7'HfJJ:M1t.t-to Terebellina~ongjtubus, Makiyama, Bathysiphon, Siphonites ~c.ltilil(~MLt.:;b~, ~~, %I!:*~~tl,
m!:mijl(>~5t~t;::J: f)

Serpulidae fj-O) 1 ~~c L "(~~;g Yokoia a-tI!P~ Lt.:om* IJ\ JJf. • !I!f m~ i'l]The tubular specimens occurred bothhorizontally and vertically as a crowded
assemblage of complete to fragmental(broken) individuals. Vertically the tubular specimens were found to superpose
others obliquely, horizontally or as amixed assemblage of broken tubes asshown in the annexed illustrations (PI.
19, Figs. 1-2; PI. 22, Fig. 1). All of thespecimens were found at a locality geographically not remote (about 1.2 km
north from the present locality) fromthe one where HATAI and SAITO (1962)
recorded the occurrence of Terebellina
kattoi HAT AI and SAITO. At the timeof description of Terebellina kattoi, HATAI and SAITO (1962) considered that
their new form occurred from the Bessho
Formation. However, the stratigraphicalwork by SHIMIZU (1975MS) and Y AMAGISHI (1958, 1964) shows that the blackmassive siltstone distributed around thearea mentioned above should be placedin the middle part of the Yoko-o Formation, a stratal unit proposed by Y AM AGISHI (1958) based upon the traceable tuff
layers. The discussions on the strati-

Introduction
During the summer field work in 1974
in the Sakaki area in Nagano Prefecture,abundant tubular structures were discovered in the black siltstone distributed
widely in the area. The majority of thetubular structures occurred in a position
parallel with the stratification of the tuff
layers interbedded in the black massive
siltstone, and only a few specimens werenoted to be preserved more or less oblique to the bedding of the formation.
The stratigraphic position of the blackcolored siltstone of the Yoko-o Formation in the surveyed area is shown in
Fig. 1. The Yoko-o Formation is about
1250m in total thickness; the alteredandesite and its tuff breccia are intercalated in the lower, and the black massive siltstone develops mainly at theupper part of the formation. The present tubular fossils were collected fromthe middle part of the formation.

* Received July 3, 1975; read June 14, 1975
at Morioka.
209

Kotara HAT AI and Hiroshi NODA

210

o

0.5

IKm

,'-----'-.- - - - - ' ,MIDDLE {MIOCENE

BESSHOFORMATION

YOKO-OFORMATION

I

I

[5251

TAROYAMA FORMATIONI~PORPHYRITEIFOSSIL LOCALITY

41

4

d

Vv v

vv

I

'k

Fig. 1. Stratigraphy and geological map around the fossil locality (SHIMIZU, 1975MS).

graphy will be published at another opportunity.
The tubular specimens are thought tobe worthy of description and illustration
for several reasons. The reasons are;(1) specimens comparable with but distinct from the present ones are known
to, or have been recorded (Hyalinoecia
tubicola) from the continental slope andshelf of the western north Atlantic Ocean(HEEZEN and HOLLISTER, 1971; WIGL Y
and EMERY, 1962) from depths of 2741170 meters in the former area and at
1935 meters depth at the latter area.
The Recent specimens called Hyalinoecia
tubicola show similarity with the fossil ones

dealt with in this article, and is statedby WIGLEY and EMERY (1961) to have a
depth range of 13-4380 meters for all
oceans. The average density of thatspecies is 461/m 2 on the Atlantic continental slope, 272/m 2 for the western
North Atlantic Ocean, 15/m2 for off
California. The length of the mentioned
Recent species is 6-15 cm, but most tubes
are 8-12 cm in length, (2) the fossil specimens are similar to the Recent species
cited above in some morphological features, but quite different in others; they
represent an undescribed form, (3) theblack colored siltstone in which the fossil
tubes were found suggests the kind of

654.

Miocene arm01"ed 'Worm from Nagano

marine bottom sediments on and in which
the living Hyalinoecia tubicola has beenrecorded. The resemblance of bottom
conditions seem to be noteworthy, (4)since little work has been published on
the fossil tubular structures of the kindpresented in this article, their descriptions and illustrations are thought tocontribute to our knowledge on thegroup, and (5) the rather rare and few
occurrences of fossils from the thickblack siltstone is a characteristic of theformation.
Before entering into the description
and discussion of the fossil tubular structures, sincere gratitude should be expressed to Professor Tamio KOT AKA of
the Tohoku University and Associate
Professor Yutaka SAITO of the Shinshu
University for their kind discussions on
the stratigraphy. Deep acknowledgements are due to Dr. Munemoto NEDACHI,
and Mr. Kenshiro OGASA w ARA of the
Tohoku University for their EPMA and
X-ray operations and analyses. The
writers also thank Mr. Toshihide SHIMIZU of the Teikoku Petroleum Company
for his information on the stratigraphy
and fossil locality, and Mr. Kimiji
KUMAGAI and Mr. Shohei OHTOMO ofthe Tohoku University for photographic
work.
Description and remarks

Family Serpulidae BURMEISTER, 1837
Genus Yokoia, new genus
Type species: Terebellina Iwttoi HATAIand SAITO, Yoko-o Formation, Miocene.
Diagnosis:
Straight, sigmoidal toslightly convex, calcareous and siliceous,solid tubular structures. Shell surface
with irregular concentric growth lines
and irregularly spaced periodic swellings.

211

Generally creased longitudinally along
middle.
Remarks: The genus Yokoia showsmorphological resemblance with thegenus Longitubus HOWELL, 1943 (HoWELL, 1962, p. 158, fig. 98-3) from theUpper Cretaceous of North America(HOWELL, 1962, p. 162) but differs fromit by "the concentric ridges not being
closely spaced" by the more irregular
growth lines and by the characteristic
development of irregularly
spacedperiodic buldges or swellings.
In order to know the characteristicsof the newly discovered tubular structure,
EPMA and X-ray analyses were made,and photomicrographs are annexed toshow the details. EPMA and X-ray analyses of the tubular structure show thatthey consists of siliceous material embedded in a matrix that is composed ofboth calcareous and siliceous materials.
The abundant spiculate structures noted
within the shell are all composed of Si0 2
and the abundant grains distributed
within the matrix also consist of Si0 2 •X-ray analysis of the Nagano tubes show
the first peak at 26.6 and the second one
at 20.8 degrees in 2{}, both of silica.
Terebellina shikokuensis KATTO (1960)
shows the first peak at 26.7 and thesecond one at 20.9 in 2{} also for silica.
In comparison the X-ray analyses of the
sponge hitherto known as Makiyama(previousely as Sagarites,- MAKIY AMA,
1931) from the Taga Formation in thejoban coal-field, Fukushima Prefectureand from the type area of the genus in
the Sagara oil-field, Shizuoka Prefecture
show the first peak of Silica at 26.7 andthe second one at 20.8 for the specimensfrom both of the areas. Thus from Xray analyses the Sagara and Taga socalled M ahiyama are identical in theirsilica peaks, and also similar to the Shikoku Terebellina and the Nagano Yokoia

212

Kotora HAT AI and Hiroshi NODA

(A I

( BI

2B( Cu/Ka)

Fig. 2. X-ray diffraction patterns of (A) Terebellina shikokuensis KATTO
from the Naharigawa Formation, (B) Yokoia kattoi (RATA I and SAITO) fromthe Yoko-o Formation, (C) "Makiyama" chitanii (MAKIYAMA) from the Sagara
Formation, and (D) "Makiyama" chitanii (MAKIYAMA) from the Taga Formation. Target/Filter: Cu/Ka, Intensity: 30 kV, 15 mAo

Explanation of Plate 19
Figs. 1-3. Yokoia kattoi (RATAI and SAITO).
Showing the. straight and slightly convexed shells with weak concentric .growth lines,
some swellings and medial creasing in part. The longest specimen (fig. 3 x 2, IGPS
colI. cat. no. 92616-b) measures 54.5 mm and a mixed assemblage of broken tubes (fig. 2
x 3, IGPS colI. cat. no. 92618-a) are illustrated: Some orientations of the worm tubes
are observable (fig. 1 x3, IGPS colI. cat. no. 92616-c).
Locality and geological formation is mentioned in the text.

H ATA I and NODA:

K. K UMAGA I

Miocene armored worm from Nagano

photo.

Plate 19

654-. Miocene armored worm from Nagano(n. gen.) (Fig. 2).
The spiculate structure found within
the tubular structure of Yokoia are all
monaxons in shape, silica in substance,
crowded in arrangement and generally
150-200 microns in length, being nearlystraight to weakly curved along theirlength. From the arrangement of the
spiculate structures it is difficult to decide whether they represent their originalorientation, subsequently arranged orientation, or secondary developed ones.
Whatever be the case it seems that theoriginal animal that occupied the tubular
structures may have been able to secrete
siliceous substance to make the spiculate
structures, to have devoured foreign
spiculate organisms and retained the
spicules in their shells as waste matter,or to have secreted siliceous spicules tomake the tubular structures, or lessprobably to have the spicules agglutinated on their shells for self protection.
Whatever be the real cause of the
spiculate structures, it is evident thatthe chemical and X-ray analyses madefor the tubular structures of Y okoia, theso-called Makiyama and the Terebellina
shikokuensis are almost identical andclosely similar with one another but
their structures differ. This may point
to the intimate relationship of the threekinds of tubular structures just mentioned.
Showing a remote similarity with
Yokoia is the genus Bathysiphon M.
SARS, 1872 which is described and illustrated by LOEBLICH and TAPPAN (inTreatise on Invertebrate Paleontology,
Part C, Protista, vol. 1, p. C186, fig. 105,4-10). It is said to have an agglutinatedshell that is long (up to 50 mm), narrow
and may have annular constrictions. The
wall is described to be agglutinated"commonly of siliceous sponge spicules
and fine sand or other mineral matter in

213

calcareous cement", features which seemto be similar to the shell of Yo koia kattoi(HATAI and SAITO). However, the agglutinated shell of Bathysiphon differsfrom both Yokoia and Makiyama (discussion reserved for another opportunity)in the following features, namely, (1) the
material filling the interior of the tubular
structure of Yokoia is composed of sediments the same as the matrix, (2) the
periodically and irregularly spaced concentric buldges or constrictions of Y okoia
are more defined on the calcareous tosiliceous shell, (3) the length of Bathysiphon is said to be up to 50 mm, whereasthat of the tubular structures of Yokoia
exceed that length, and the true length
remains unknown because both ends arebroken in all of the preserved specimens,and (4) the shell wall is not agglutinated as in Bathysiphon. From thesereason, the shell of Yokoia can not be
identified with that of Bathysiphon (Foraminifera). However, whether Bathysiphon is a true Foraminifera may be inneed of a re-examination. Dr. Yasumoti
MATOBA, foraminiferologist at the Akita
University of Mining, informed the juniorwriter that he has a similar thinking
about Bathysiphon with the writers.
Detail examination of Bathysiphon and
Makiyama will be reserved for anotheropportunity. Other organisms, such as
the foraminiferal genera showing a moreor less remote resemblance with the shellof Yokoia may be Nodellum RHUMBLER,
1913 (Op. cit., p. C179, fig. 97, 3-4); Protobotellina HERON-ALLEN and EARLAND(Op. cit., p. C190, fig. 106, 7-9); andSchixammina HERON-ALLEN and EARLAND, 1929 (Op. cit., p. C194, fig. 107,6-10). But these three genera can be
distinguished from Yokoia in the same
way as Bathysiphon.
The generic name is taken from thename of the formation.

214

Kotora HAT AI and Hiroshi NODA

Y okoia kattoi (HAT AI and SAITO, 1962)
PI. 19, figs. 1-3; PI. 20, figs. 1-7a;
PI. 21, figs. 1-7; PI. 22, fig. 1

Terebellina kattoi HATAI and SAITO, 1962,
Japan. Jour. Geol. Geogr., vol. 33, nos.
2-4, p. 246, fig. 2.

Description: Tube long, narrow, stringlike, orifices rounded, surface with strong
to weak concentric growth lines andperiodic, irregularly spaced concentricbuldges or swellings; tube rounded originally, generally creased medially andlongitudinally; tube straight to broadly
sigmoidal to more or less broadly bowshaped. Length exceeds 50 mm because
both ends lost, width about 2 mm when
not creased medially, but measuring 3
mm or a little more when creased. Concentric buldge or swellings or annulations
separated by distances of about 0.2 mm
to 1.5 mm in width.
Locality: Road side cliff at the entrance
to the forest road at Goshozawa (Hirasawa-rindo), Sakaki-cho, Hanishina-gun,
Nagano Prefecture.
Geological formation and age: Middle
part of the Yoko-o Formation, Middle
Miocene.
Depository: Illustrated specimens (IGPS
colI. cat. nos. 92615, 92616, 92617, 92618)
are preserved in the collection of theInstitute of Geology and Paleontology,

Faculty of Science, Tohoku University
and some specimens collected from thesame locality are in the collection of
the Saito Ho-on Kai Museum of Natural
History.
Associated fossils: Eutrephoceras izumoensis (YOKOYAMA), some thin shelledpelecypods, detached fish scales anddrifted plant leaves.
Remarks: Most of the specimens referred to Y okoia kattoi are creased medially and longitudinally, some due to compressive agencies after death of theorganism. But many specimens stillretain the original shape and are also
found mixed in the same assemblage ofindividuals. Some specimens are creased
only in part, and the creasing may be
hardly noticable to strongly impressed.
Creasing medially is also shown inmany specimens of Terebellina illustrated
by DANNER (1955) from the Neogene
rocks of several localities in western
Washington, U.S.A. This phenomenon
is a common feature in specimens of theso-called Makiyama chitanii (MAKIY AM A)
of wide distribution in Japan and recorded originally as a sponge from the Neogene rocks of the Sagar a district in Shizuoka Prefecture (MAKIY AM A, 1931), andprobably sometimes mistaken for thepresent new genus especially in Nagano
Prefecture. Besides the tubular structures known to be creased medially andExplanation of Plate 20
Figs. 1-7a. Yokoi kattoi (HATAI and SAITO).
(All figures x3 excluding figs. 3-3a x2)
All figures are different views taken with different focus depth. Figs. 3-3a, 4-4a, 5-5a,
6-6a and 7-7a show the pair of specimens photographed with different focus depths toshow how different the surface features will appear. Identification of the worm tubes
will arise from the magnification used, thus both natural and enlarged views are important for classification of the armored worms. Figs. 1-2, 6-6a, IGPS coli. cat. no. 92615b; Figs. 3-3a, 4-4a, 5-5a, IGPS coli. cat. no. 92615-a; Figs. 7-7a, IGPS colI. cat. no.
92615-c.
Locality and Formation is mentioned in the text.

HATA J an d N OD A:

K. K UMAGA I photo .

Miocene armored worm from Na gano

Plate 20

654. Miocene armored worm from Nagano
longitudinally, there are several speciesof so-called worm tubes that have been
described from the geological formationof Japan and of the North Pacific borderland. These are given in the list cited
below.

List of fossil armored worms fromthe North Pacific borderland
Terebellina shikokuensis KAT TO, 1960, Sci.
Rep., Tohoku Univ., Ser. 2, Ceol., SPec.
Vol., no. 4, p. 328, pI. 34, figs. 1, 3, pI.
35, fig. 7, Type loc.-Sea cliff at Kannoura, Toyo-cho, Aki-gun, Kochi Prefecture, Naharigawa Formation, Eocene.
Terebellina kattoi HATAI and SAITO, 1962
[Misspelled as TerebrellinaJ. This is
the type species of the genus Yokoia, n.
gen., japan. jour. Ceol. Ceogr., vol. 31,
nos. 2-4, p. 246, fig. 2. Type loc.-One
kilometer east of Minamihina, Sakakicho, Hagishina-gun, Nagano Prefecture,
Bessho Formation, Miocene.
Vermitubus sumitaensis HATAI, MURATA and
KA\YAKA:-'H, 1972, Saito Ho-on Kai Mus.,
Res. Bull., no. 41, p. 29, pI. 4, figs. 1-14.
Type loc.-Motoizawa, Kawaguchi, Sumita-cho, Kesen-gun, Iwate Prefecture,
Sakamotozawa Formation, Permian.
Terebellina palachei ULRICH, 1910, Howell,
B. F., 1962, in Treatise in Invertebrate
Paleontology, ed. by R. C. MOORE, Ceol.
Soc. Amer. and Kansas Univ. Press, p.
162, fig. 101-4. Type loc.-Yakutat Bay
area,
Alaska, Yakutat
Formation,
Jurassic.
Ditrupa miyazakiensis HATAI, NODA and
OGASAWARA, 1970, Trans. Proc. Palaeont.
Soc. japan, N. S., no. 87, p. 409, figs. 12. Type loc.-Uzutsumi near the Kagamisu Pass on the road from Nagayama
to Koguchi, south of Kiyotake-cho, Miyazaki-gun, Miyazaki Prefecture, Boroishi
Member of the Udo Formation, Miocene.

All of the species given in the list
above can be distinguished from the new
genus described in this article by several
important characters as, the strong concentric growth lines, periodic and irre-

215

gularly spaced buldges or swellings thatare especially noteworthy at and fromthe middle towards the anterior part of
the tube. The tube may be straight,
sigmoidal to slightly curved. The creasing medially and longitudinally is
noticed on both large and small specimens. None of the tubes seem to be
agglutinated as to consist of cemented
grains of rock, shells, sand or othersmall objects as in Terebellina.
Observations on the known fossil worm
tubes described from Japan reveal thatthe outstanding characteristics that arealso of taxonomic importance are thestrong growth lines, periodic and irregularly spaced buldges or swellings ofthe tube, irregular growth and nonagglutinated shell. The genus Siphonites
SAPORT A, 1872 described and figured by
HANTZSCHEL (1962, p. 215) is stated tohave the "Tubes about 1 cm in diameterwith sandy lining, mostly washed out
and collapsed on bedding planes." This
genus has been recorded from the Upper
Triassic of France. The figure given by
HANTZSCHEL (1962, p. 216, figs. 135-4)
shows specimens creased medially andlongitudinally, and in this respect, resemblance is found with the broken specimens of Yokoia. However, the diameterof Siphonites is stated to be about 1 cm
and in this respect it is much larger
than any of the specimens of Y okoia in
the present collection. The collapsed
specimens of Siphonites also show a remote resemblance with the compressed
and medially creased specimens of the
Miocene and Pliocene so-called Makiyama
distributed widely in Japan and with
Yokoia kattoi (HATAI and SAITO) from
the Miocene of Nagano Prefecture. Makiyama is in need of detail study to confirm its true characteristics and relation
with similar forms. Siplwnites differsfrom the two just mentioned in the

216

Kotora HAT AI and Hiroshi NODA

much larger diameter, much shorter andstouter tube. Among the species givenin the list, Terebellina shikokuensis KATTO, 1960, from the Eocene Naharigawa
and Muroto Formations of Kochi Prefecture is the first record to the genus
Terebellina from Japan. Terebellina shikokuensis is characterized by the wallbeing composed of "fine grained sands
firmly cemented". Subsequent study ofthe holotype of T. kattoi shows that its
wall is not composed of "minute siliceous
grains" as in Terebellina, and in thisrespect, kattoi should be referred to a
genus other than Terebellina. Examination of some of the tubes called TerebeZZina shikokuensis KATTO, taken from theoriginal mass of specimens illustrated by
KATTO (1960), shows that the external
shell is composed of minute grains andthat the matrix also consists of minutegrains. There is no periodic irregularly
spaced concentric swellings as in Yokoia,
and from the characteristics just mentioned its reference to the genus Terebellina is without doubt. Shikokuensis
can be retained in the genus Terebellina
and the genus is represented in the
Cenozoic rocks of Japan by the single
species, shikokuensis.
The wall of Yokoia, n. gen. proposedin this article is calcareo-siliceous, andin this respect its reference to the family
Serpulidae BURMEISTER, 1837 (HOWELL,
1962, p. 155) seems to be justified it theoriginal tube was calcareous but sub-sequently changed into silica. And it ischaracterized by the shape of the tube,
its longitudinal creased structure, andwith characteristic concentric, periodically arranged swellings.
Among the abundant specimens oftubular structures found in the black
mudstone in the Sakaki area, there weremany without the external shell that
could be identified with Terebellina
kattoi described by HATAI and SAITO.
Under the circumstances, it was decided
that the tubular shells are identical withthe mould specimens described and illustrated by HAT AI and SAITO. The presence of abundant siliceous material in
the matrix of both specimens, that is tosay in the ones described by HATAI and
SAITO and in the ones newly found isnoteworthy as stated already. Chemical
and X-ray analyses of both of them arealso identical.
Remarks in the paleoecologyof the worm
As mentioned already the tubes ofY okoia kattoi were all found in blackcolored siltstone, and in association withsome strongly and laterally compressedshells of the cephalopod genus Eutrephoceras, some thin shelled pelecypods,
many small detached fish scales arranged at random and also with some fragments of plant leaves which are now
under examination by Professor Hidekuni

Explanation of Plate 21
Figs. 1-7. Yokoia kattoi (HATAI and SAITO).
(All figures x35 excluding fig. 7, x87)
Microscopic figures show some vertical sections and longitudinal sections (figs. 1-4).
Spiculate structures shown in figs. 5, 6 and 7 (enlarged in part from figs. 5 and 6).
Shell material and spiculate structure composed of silica (analysed by EPMA and Xray opperations). (lGPS colI. cat. no. 92616-a).
Locality and Formation is mentioned in the text.

H ATA J and NODA:

K. KUMAGA I

Miocene armored worm from Nagano

and S. OllTO MO photo.

Plate 21

654. Miocene armored worm from Nagano
MATSUO of the Kanazawa University.
Among the several kinds of fossils, only
the worm tubes are abundant whereas
the nautiloid shells are common only
locality, the fish scales are rather common and of wider distribution than the
cephalopod but only of a few types afeature that does not point to that theoriginal fish were abundant, and thefragmental remains of plant leaves arevery rare, probably because of being
drifted to their place of burial. Fromthe massive nature of the black coloredsiltstone, kind of fossils and their resemblance to the present day marine bottom
sediments as well as bathymetric environment of the Recent Hyalinoecia
tubicola recorded by HEEZEN and HOLLISTER (1971) and by WIGLEY and EMERY(1967) and which resembles Terebellina
shikokuensis serve to bring forth thefollowing interpretation on the paleoecology of Yokoia kattoi.
The paucity of benthic and planktic(MARTINSSON, 1975) and the abundancy
of only worm tubes of the benthic community and the common occurrence ofnautiloids locally all serve for the following interpretation. During and after
deposition of the dark colored bottom
muds (Black siltstone) it is thought thatthe bottom conditions were oxygen-poorand sulphurous gas have generated in
the soft, dark colored, bottom muds.
Under the conditions probably of low
temperature, issuing sulphurous gas andoxygen-poor environment, the possibilityof benthic life was probably restricted
to armored worms that devoured debris
and planktic to pelagic invertebrates
that settled to the bottom. The nautiloids
that were swimming in the surface
waters or drifted to the area underlain
by the dark muds were probably affectedor paralised by the sulphurous gas issuing from the bottom muds and thus died217

and then sank to the bottom to becomeburied there. This seems to be an analogue to the graptoloids (TWENHOFEL,
1931) occurring in black shales. Alsofrom the occurrence of abundant broken
worm tubes, it may be probable that thenautiloids were predators of the worms.
Judging from the foregoing, it isthought that the bottom condition of thesea was influenced by oxygen-poor water
contrary to the warm surface waters inwhich the vagrant nautiloids wandered.
The association of fish scales with thearmored worms and nautiloids may notmean the existence there of a rich fish
fauna because a single fish can supply
many scales. Some fish bones occurredin association with some different typesof scales (TANAKA et al., 1966) or evenin the black siltstone adjacent to thearmored worm remains, they probably
were either destroyed by bacteria, decay
or devoured by the armored worms orsome other cause. The rare occurrenceof fragmental plant leaves may point to
the distance from the land. They werewind transported or current carried tothe sea area of their burial. Their presence in the marine fauna is of no use
for interpretation of the paleoecologicalconditions of the armored worms. Thatno planktic protozoans were found in
the black siltstone suggests that after
death they sank to sea bottom to become the food of the armored worms on
one hand and the oxygen-poor and sulphur gas generated bottom conditions
may have accelerated chemical destructionof the protozoan test, thus explaining
their absence in the bottom muds.
References cited
W. R., 1955, Some fossil
tubes of western Washington.
and Minerals, p. 451-457, 7 figs.

DANNER,

worm
Rocks

218

Kotara HAT AI and Hiroshi NOD A

HXNTZSCHEL, W., 1962, Trace fossils andproblematica. in Treatise on Invertebrate
Paleontology, Pt. W. ed. by R. C. MOORE,
Ceol. Soc. Amer. and Kansas Univ. Press.,
p. 177-245, figs. 110-245. (refer to p. 215,
fig. 135-4).
HATAI, K., MURATA, M. and KAWAKAMI, T.,
1972, Tubular structures from the Sakamotozawa Formation (Permian), Sumitacho, Kesen-gun, Iwate Prefecture, Northeast Japan. Saito Ho-on Kai Mus., Res.
Bull., no. 41, p. 29-34, pl. 1, fig. 1.
- - , NODA, H. and OGASAWARA, K., 1972,.
Scaphopoda-like fossils from the Udo
Formation (Miocene) of Miyazaki Prefecture, Japan.· Proc. Trans. Palaeont.
Soc. japan, N. S., no. 87, p. 409-413,2 figs.
- - and SAITO, Y., 1962, A problematica
from the Miocene Bessho Formation in
Bigashina County, Nagano Prefecture,
Japan. japan: jour. Ceol. Ceogr., vol. 33,
nos. 2-4, p~ 243-250, 2 figs.
HEEZEN,. B. C. and HOLLISTER, C. D., 1971,
The face of the deep. 659 pp. (refer top. 89, figs. 2-66, 2-67).
HOWELL, B. F., 1962, Worms. in Treatise on
Invertebrate Paleontology. ed. by R. C.
MOORE, Ceol. Soc. Amer. and Kansas
Univ. Press., Pt. W, p. 144-177, figs. 85108.
KATTO, J., 1960, Some problematica fromthe so-called unknown Mesozoic strataof the southern part of Shikoku, Japan.
Sci. Rep., Tohoku Univ. 2nd Ser., Ceol.,
SPec. Vol., no. 4, p. 323-334, pis. 34-35.
- - , 1973, Sedimentary structures and problematica of Tosa. (in Japanese). Ceol.

News, no. 231, Ceol. Surv. japan, p. 58-65,
31 figs.
MAKIYAMA, J., 1931, Stratigraphy of the
Kakegawa Pliocene in Totomi. Mem.,
Coll. Sci., Kyoto Univ., Ser. B, vol. 7,
no. 1, art. 1, p. 1-53, pis. 1-2, 4 figs.
MARTIXSSON, A., 1975, Editor's column;
Planktic, nektic,· benthic. Lethaia, vol.
8, p. 193-194.
SHIMIZU, T., 1975 (MS) , Geology of thenorthern part of Ueda City, Nagano Prefecture. (in Japanese). Graduation Thesisof the Institute of Geology and Paleontology, Faculty of Science, Tohok~ University.
TANAKA, K., NAKAZAWA, K., SEKI, Y: and
TSUKADA, S.; 1966, On the fossil fish
scales from the Bessho Formation, Nagano Prefecture. (in Japanese with English abstract). Earth Science (Chikyu
Kagaku) , no. 82, p. 17-30, pis. 1-2, figs.
1-28, tabs. 1-2.
TWENHOFEL, W. H., 1931, Environment insedimentation and stratigraphy. Bull.
Ceol. Soc. Amer.. , vol. 42, p. 407-423.
YAMAGISHI, I., 1958, "Green Tuff" in thenorthern district of Ueda City, Nagano
Prefecture. (in Japanese with English
abstract). jubl. Publ. Commem. Prof. H.
Fujimoto Sixtieth Birth., p. 245-250, figs.
1-2, 1 tab.
- - , 1964, Geology in the northern districtof Ueda City, Nagano Prefecture, withspecial reference to Green Tuffs. (inJapanese with English abstract) .. jour.
Ceol. Soc. japan, vol. 70, no. 825, p. ·315338, 1 pI., figs. 1-14, 5 tabs.

Explanation of Plate 22
Fig. 1. Yokoia kattoi (HATAI and SAITO) x9.
Vertical sections to show the mode of occurrence of Yokoia kattoi (HATAI and SAITO).
The specimens are arranged along the lamination dominantly. The most dominant partcontained 70-80 specimens per 2 ems. Figure shows the medial impression, thicknessof the wall, irregular buldges and arrangement to the bedding plane (longitudinal ofplate). (IGPS colI. cat. no. 92616-a).
Locality and Formation is mentioned in the text.
IGPS coli. cat. no. is of abbreviation for the collection catalogued number of the Institute ofGeology and Paleontology, Faculty·of Science, Tohoku University, Send ai, Japan.

H ATAJ and NODA:

K. K UMAGA I

photo.

Miocene armored wo?'m from Nagano

Plate 22

654. Miocene armored worm from Nagano
BesshoGoshozawa
Hirasawa
Kannoura
Naharigawa

m

-'OJ]

m ffl iR.
!f
Eft

iR.

(J)

rm

~ ~ fU JII

Sagar aSakakiTaga
Yoko-o

m

~

~

:Ii\{

219
~
~
~
ftj;

Trans. Proc. Palaeont. Soc. Japan, N. S., No. 100, pp. 220-229, pis. 23, 24, Dec. 25, 1975

655.

PALAEOFUSULINA-REICHELINA FAUNA CONTAINEDIN THE PEBBLES OF INTRAFORMATIONALCONGLOMERATE DISTRIBUTED IN THE
OKUTAMA DISTRICT,WEST TOKYO*
FUMIO KOBAYASHI
Institute of Geology and Mineralogy, Tokyo University of Education

Palaeofusulina-Reichelina 1lli;ifkJ1lf: ~1i.13 m-~t:J] 5 km ~:tm
Palaeofusulina nana LIKAREV,
Reichelina cribroseptata ERK, R. cfr. tenuissima K. M. MACLAY, Staffella sp. 0) 4
:fI~~JflI(:¥IH!j·i' Qo ~:b-lt-CitE*¥IH1f ~n -C~ 'Q Palaeofusulina 18 filv;::--::>~ '-C:fl~~W~
fitJ:~', P. prisca DEPRAT, P. nana LiI<AREV, P. laxa SHENG, P. ellipsoidalis SHENG,
P. minima SHENG and CHANG, P. simplex SHENG and CHANG ~ 6 fiJH;::~:J!l!.~n:f!}Q ~~~*£J\'i'il*I~:E9=IO)}~ -c':!*~ L. t.:.F,i'i l*I~:E 9=t ~ EEJ(:E~~ ~EK-1l;inQ

MRtuL.t.:.o

IJ\ it Jt ~of several biocharacters, I also discuss
the validity of the previously described
species of the genus Palaeofusulina.
Acknowledgement: I wish to express
my sincere thanks to Dr. Hisayoshi IGo,
Associate Professor of the University ofTsukuba, for his supervision, and Dr.
Toshio KOIKE of Yokohama National
University, for his valuable suggestions.
Cordial thanks are also due to Professor
Mosaburo KANUMA and Assistant Professor Atsushi ISHII of Tokyo Gakugei
University, for their encouragements andfruitful suggestions in many ways. Mr.
Masami SUGA Y A, post-graduate studentof Tokyo Gakugei University, helped mein statistical study.

Introduction

Late Paleozoic and Mesozoic sedimentary rocks are widely distributed in
the Okutama district, southern part of
the Kwanto Mountainland. These sediments are separated into narrow belts
by thrust faults running from NW to SE
and constitute the so-called sandwichstructures. FUJIMOTO (1932), SAKAGAMI(1956, 1958, 1972) and others engaged instratigraphical and paleontological studiesof this area. During my field study inthe northern part of Itsukaichi, Tokyo
Prefecture, I obtained many new informations concerning geological structure,
distribution of stratigraphic units andpaleontological evidence.
In this paper I intend to describe the
Palaeofusulina-Reichelina fauna yieldedfrom this area. Based upon the statistics

Summary of geology

A remarkable intraformational conglomerate is exposed in the northernpart of Itsukaichi. This conglomerate* Received July 9, 1975; read Oct. 20, 1974
at Tokyo.

220655. PalaeofuBulina-Reichelina fauna
was named "Nishinoiri Conglomerate"by SAKAGAMI (1958) and intercalated
within greywacke of about 100 m inthickness. Many limestone, sandstone,
shale, chert and schalestein pebbles andcobbles are cemented by the coarse to
medium grained sand. Fusulinacean fossils
ranging from Moscovian to Kungurian
are yielded from these limestone pebbles.
This intraformational conglomerate has
been considered to be chronologicallyequivalent to the Upper Permian Yasuba
Conglomerate inSouthwest Japan(SAKAGAMI, 1958). The stratigraphic
relationship between this conglomerate
and the Triassic conodont-bearing bedded
cherts show that the geologic age ofthis conglomerate must be revised as
Triassic instead of Upper Permian.
Detailed discussion concerning geologic
age, correlation, lithologic characteristics
and other fusulinids of this conglomerate
will be presented at another opportunity.
The materials studied were obtained
from the limestone erratics found at thetributary of Hirai-gawa, north of Kanyho,

Text-fig. 1. Index map showing
sampled locality.

221

5 km NNW of Musashi-Itsukaichi Station(Text-fig. 1). This limestone erratics
were derived from the above mentioned
intraformational conglomerate.
The
limestone is grey biomicrudite, andcontains
Palaeofusulina,
Reichelina,
Staffella and other smaller foraminifers.
One hundred and twenty thin sections
are prepared to discuss the intraspecificvariation of Palaeofusulina. All of them
are stored at the Institute of Geology
and Mineralogy, Tokyo University of
Education.
Description and discussionof species

Genus Palaeofusulina DEPRAT, 1912
Palaeofusulina nana LIKAREV
PI. 23, Figs. 22-29; PI. 24, Figs. 1-18

1926. Palaeofuslina nana LIKAREV, Comm.
Geol. Leningrad, Bull., Vol. 45, pp.5966, pI. 2, figs. 1-13.
1955. Palaeofusulina sinensis SHENG, Acta
Palaeontologica Sinica, Vol. 3, No.4,
p. 305, pI. 4, figs. 1-15, pI. 1, figs. 13,
16.
1955. Palaeofusulina
sinensis
fusiform is
SHENG, Ibid., p. 306, pI. 1, figs. 14-15.
1955. Palaeofusulina wangi SHENG, Ibid., pp.
303-304, pI. 3, figs. 1-5, 7.
1955. Palaeofusulina wangi chumipuensis
SHENG, Ibid., pp. 304-305, pI. 3, fig. 6.
1958. Palaeofusulina cfr. sinensis SHENG;
SHENG and CHANG, Ibid., Vol. 6, No.
2, p. 212, pI. 1, figs. 21-25.
1963. Palaeofusulina nan a LIKAREV; SHENG,
Ibid., N. S. B, No. 10, pp. 175-176, pI.
9, figs. 10-16.
1963. Palaeofusulina sinensis SHENG, Ibid.,
p. 175, pI. 9, figs. 1-9.
1963. Palaeofusulina fusiform is SHENG, Ibid.,
p. 176, pl. 10, figs. 5-9.
1963. Palaeofusulina bella SHENG, Ibid., pp.
179-180, pI. 10, figs. 25-27.

222

Fumio KOBAYASHI

Shell small, inflated fusiform in shapewith almost straight axis of coiling,broadly arched periphery, convex to
somewhat straight lateral sides androunded or bluntly pointed poles. The
first volution nautiliform but subsequentones inflated fusiform. Adult specimens
with 4 to 4.5, rarely 5 volutions, 1.49 to
2.03 mm in axial length and 1.03 to 1.56
mm in median width, giving form ratio
1: 1.2 to 1: 1.7. Proloculus spherical,
rather large for the size of shell and 0.06
to 0.13 mm in outside diameter. Spirothecathin, principally composed of distinct
tectum and translucent layer (diaphanotheca), but not differentiated at apart of inner three volutions in somespecimens. Septa closely spaced andstrongly fluted throughout shell. Fluting
makes septa in contact with each otherabout half of their height. Axial deposits
lacking, but frequently the last volution
filled with secondary calcite.
Remarks: There are broad variationsin the heights of volutions, size of
proloculus, form ratios of volution, septal
fluting and others within the present
specimens. The former three biocharacters are shown in Text-figs. 2 and 3. As
clearly shown in these figures, individual
variations are graditional from specimen
to specimen, and no significant differences
are recognized among them.
Reg. nos.: 27001-27008, 27010-27027.
Statistics of Palaeofusulina nana
LIKAREV from Itsukaichi (in mm.). N:
number of measurements, Max.: heighest
value recorded per each variate, Min.:
lowest value recorded per each variate,
X : arithmetic mean, s: standard deviation.

(Width)

1.6
I.f,

1.2

1.0

0.8

0.6

0.4

0.2

o

2

3

5

(Vol.)

Text-fig. 2. Variations in proloculus
size and width of volutions among twenty
three specimens of Palaeofusulina from
Itsukaichi.

(Form Ratio)!---.,------=-3-----,------,,,.- (Vol.)

Text-fig. 3. Variations in form ratioof volutions among twenty nine specimens
of Palaeofusulina from Itsukaichi.

655.

Palaeofusulina-Reichelina fauna
Half Length

L
N
Max.
Min.

X
s

W

23
2.03
1. 40
1. 76
O.lS

23

Radius VectorP29

1. 56 0.13
1. 03 0.05
1. 30 0.11

0.30 0.02

1

2

3

29
0.23
0.06
0.13
0.04

29
0.45
0.15
0.29
0.07

29
0.75
0.35
0.53
0.11

4

X
s

1

2

3

4

23
0.25
0.13
0.20
0.03

23
0.43
0.22
0.36
0.06

22
0.S3
0.41
0.66
0.11

IS
1. 56
o. 79
1.11
0.16

5

1

2

3

4

5

29
0.15
0.06
0.10
0.02

29
0.2S
0.11
0.19
0.04

29
0.51
0.23
0.37
0.07

23
0.96
0.44
0.61
0.10

3
0.75
0.72
O. 73
0.02

23

3

1. 06

1. OS

0.63
O.SO
0.11

0.9S
1. 01
0.06

Width of Volution

N
Max.
Min.

223

Thickness of Spiro theca

5

1

2

3

4

5

1

29
0.010
0.003
0.007
0.002

29
0.020
O.OOS
0.013
0.005

29
0.040
0.010
0.022
0.006

23
0.035
O.OOS
0.019
0.006

3
0.025
0.010
0.020
0.009

-

-

1. 32

Discussion: As already pointed out inthe earlier lines, the present materials
show considerable variations in septal
fluting, height of volutions, size of proloculus and form ratio of shell. However,these variations seem to be intraspecificrather than specific. Gradational variations of these characters are also
recognized in the previously described
species, such as P. sinensis SHENG, P.
fusiformis SHENG, P. wangi wangi SHENG,
P. wangi chumipuensis SHENG, P. bella
SHENG and P. nana LIKAREV. Although
SHENG (1955, 1963) mentioned these six
species are distinctive, I become tobelieve that P. sinensis, P. fusiformis, P.
wangi wangi, P. wangi chumipuensis and
P. bella are junior synonyms of P. nana.
Palaeofusulina prisca DEPRAT, P.
pseudoprisca (COLANI) and P. mutabilis
SHENG are characterized by large size ofshell and proloculus and great heightof volutions than those of P. nan a andthe above mentioned similar species (seeText-fig_ 4). P. mutabilis SHENG has-

smaller shell than P. prisca and P.
pseudoprisca. JUdging from the numberof volutions, statistics of the size of
proloculus and width of each volution,
P. mutabilis may be immature formsof P. prisca and P. pseudoprisca. P.
pseudoprisca and P. mutabilis are entirely
conspecific, and they are synonyms of P.
prisca DEPRAT.
SHENG (1963) pointed out the similarity
between P. simplicata SHENG and P.
fusiformis SHENG. However, the former
has weaker and more irregular septal
fluting and smaller proloculus than thelatter. P. fusiformis with small proloculus (SHENG, 1963, pI. 10, fig. 8)
indicates that the species is of the
microspheric generation. Also, SHENG(1963) emphasized the close relationshipbetween P. laxa and P. mutabilis in
general shape of shell and number ofvolutions, but no common characteristics
are recognized between size of proloculus,
expansion of shell or septal fluting of thetwo species. In my opinion, however, P.

Fumio KOBAY ASH!

224
(mm~

P. prisco

2.0

1.5

p. ellipsoidal Is

1.0

0.5

P.slmplex

OL.....-~--=-2---=----:4~--!-5-~6-(VOI.1

Text·fig. 4. Growth curve of six
species of Palaeofusulina; measurements
based on SHENG'S (1955, 1963) and SHENG
and CHANG'S (1958).

laxa SHENG and P. simplicata SHENG have
many common characteristics, such as
minute proloculus, tightly coiled inner
volutions, rapid expansion of shell inouter volutions and rather weak andirregular septal fluting.
These two
species are conspecific, but they differ
from P. nana and P. prisca.
According to SHENG (1963), P. elli.
psoidalis SHENG, P. pulla SHENG and P.
compacta SHENG have close similarities,
but there are slight differences in thenumber of volutions, coiling pattern ofshell and size of shell. However, theabove mentioned three species have many
common characteristics in elongate elli·

psoidal shell, strongly and rather regularly
fluted septa, tightly coiled inner volutions,slowly and almost constantly expanded
shell in outer volutions and a large
numbers of volutions for the size ofshell. Accordingly, these three species
are distinguished from P. nana, P. prisca
and P. laxa, but, P. pulla and P. compacta
are synonyms of P. ellipsoidalis.
P. minima SHENG and CHANG has
minute inflated shell, less numbers ofvolutions and very tightly coiled first
volution, and it resembles closely P.
ellipsoidalis. There are some possibilities
that P. minima represents the immatureform of P. ellipsoidalis. According to
the statistics, however, P. minima hasmore tightly coiled first volution and lessnumber of volutions than P. ellipsoidalis.
Both species have very similar growth
curve (Text· fig. 4) and P. minima occupies
slightly lower stratigraphic position thanP. ellipsoidalis in South China. From thementioned evidence, I treated tentatively
P. minima:and P. ellipsoidalis are inde·
pendent species and the former represents
an ancestor of the latter species.
P. simplex SHENG and CHANG is thesimplest form among the previously
proposed species of Palaeofusulina.
SHENG (1963) stated that this species was
the smallest andmostprimitive
palaeofusulines.
In addition to the above mentioned
Palaeofusulina, P. weberi (SCHUBERT) andP. pamirica LEVEN were described. The
former was originally described by
SCHUBERT (1915) as Fusulina weberi
SCHUBERT from east of Pualaca, Portuguse
Timor. Later, THOMPSON (1949) revised
SCHUBERT'S specimen as Palaeofusulina
weberi (SCHUBERT) to Palaeofusulina
prisca DEPRAT based on the similar spi·rothecal structure and the other features.
P. weberi has ellipsoidal shell and rather
irregular inner volutions and is associated655.

Palaeofusulina-Reiohelina faunawith the Lower Permian species of
Schwagerina, S. granum-avenae (ROEMER).
Therefore, this species probably belongs
to Boultonia or Paraboultonia.
P.
pamirica was described by LEVEN (1967)
from Darvas. It has tightly coiled andrather irregular juvenile volutions, small
proloculus and strongly fluted septa,
Associated fusulinids are Reichelina
pulchra K. M. MACLAY, Staffella zisongzhensis (SHENG), Codonofusiella lui SHENG
and C. curtekensis LEVEN. Therefore,
LEVEN'S Palaeofusulina pamirica may bealso revised to Dunbarula or Paradunbarula.
In conclusion, based upon the above
discussed morphological considerations,stratigraphicaldistribution
intheChangshing Limestone in South China,
and geographical distribution of the225

previously described eighteen species of
Palaeofusulina, the following six species
are valid.
1. Palaeofusulina prisca DEPRAT
2. P. nana LIKAREV
3. P. laxa SHENG
4. P. ellipsoidalis SHENG
5. P. minima SHENG and CHANG
6. P. simplex SHENG and CHANG

Genus Reichelina ERK, 1941
Reichelina cribroseptata ERK
PI. 23, Figs. 1-20
1941. Reichelina cribroseptata ERK, Ecol.
Ceol. Herv., Vol. 34, No.2, p. 250, pI.
14, figs. 17-21.
195,1. Reichelina cribroseptata ERK; K. M.

P.nanaP. prisca

P. simplex

P. minima

P. I axa

P. ell ipsoidalis
O.5mm.
Text.fig. 6. Six species of Palaeo/usulina.

Fumio KOBAY ASH!

226

MACLAY, Gosgeolizdat, p. 71, pI. 14,
figs. 1-2, 4.
1963. Reichelina cribroseptata ERK; SHENG,
Acta Palaeontologica Sinica, N. S. B,
pp. 148-149, pI. 1, figs. 13-16.

Septa
lower and upper tectoria.
numerous, plane and unfluted throughout
the shell. Weak secondary deposits ofcalcite recognized in axial region.
Chomata low and indistinct.
Tunnellow and narrow.
Remarks.'
This species resembles
closely Reichelina media K. M. MACLAY
in many respects. However, importantdissimilarities are recognized between
two species in the length of axis, form
ratio of shell and the height of volutions.
Compared with the Chinese materials
described by SHENG (1963), the present
specimens have a horn-like prolongation,
while the Chinese ones have a tail-likeand shorter prolongation than the present
ones. ERK's original specimens havesomewhat less developed prolongation.
Reg. nos. .' 27028-27047.
Statistical values of R eichelina cribroseptata ERK are given below in mm.

Shell small, lenticular to sub discoidal
in shape with almost straight axis ofcoiling, straight lateral sides and protruding or slight umbilical poles. Inner
two volutions sub discoidal with narrowly
pointed periphery; the third and fourth
volutions with pointed periphery, straightlateral sides and protruding or slightumbilical poles; last half or last volution
vaulted protruding a long, horn-likeprolongation of shell. Mature shells
have 4.5 to 5 volutions, 0.28 to 0.33 mm
in axial length and 0.78 to 1.58 mm inmedian width, giving form ratio 1: 0.2
to 1: 004. Proloculus minute, sphericaland its external diameter 0.05 to 0.06 mm.
Spirotheca thin, composed of tectum,

Half Length
L

W

2

3

4

5

1

8
8
0.04 0.07
0.03 0.05. O. 03 0.06
0.01 0.01

8
0.12
0.08
0.09
0.01

7
0.14
0.12
0.13
0.01

3
0.17
0.15
0.16
0.01

8
0.08
0.05
0.06
0.01

1
N
Max.
Min.

X
s

6
0.33
0.28
0.30
0.02

7

8
0.06
0.78 0.05
1. 16 0.05
0.27 0.01
1. 58

Radius Vector

P
2

3

4

5

8
8
8
3
0.14 0.24 0.64 1. 25
0.09 0.13 0.27 0.73
0.10 0.18 0.34 0.91
0.02 0.03 0.13 0.29
(to be continued)

Explanation of Plate 23
Figs. 1-20. Reichelina cribroseptata ERK
1-9, 12-16. Axial sections; 10, 17-18, 20. Tangential sections; 11, 19. Sagittal sections,
1-4, 15-16 x 40, 5~14, 17-20 x 50, Reg. nos. 27028-27047.
Figs. 22-29. Palaeofusulina nana LIKAREV (See also Plate 24)
22-28. Axial sections; 29. Nearly centered tangential section, 22-29 x 30, Reg. nos.
27001-27008.
Fig. 21. Staffella sp. (See also Plate 24)
Oblique section x 30; Reg. no. 27009.

KOBAYASHI:

Palaeofusulina-Reic helina fauna

Plate 23~\'~m~: ' '~~

\~
r, ~

,

tal ~' -\. ~;_ _~' . I'. ~~19 'rj

'

20

655.

227

Palaeofusulina-Reichelina fauna

Width of Volution

N

Max.
Min.

X
s

1

2

3

4

5

8
0.13

8
0.24

8
0.42

8
0.90

0.09

0.15

0.25

0.49

6
1. 58
O. 78

0.11
0.02

O. 19

0.32

0.58

0.03

0.06

0.14

~ j~'
~.

1. 16
0.27

2·

'" a

~.

c

a

a

0

,.

>

Cfr. 1954. Reichelina
tenuissima
K. M.
MACLAY, Gosgeolizdat, p. 73, pl. 14

.

~

.:'

PI. 24, Figs. 20-24

0

...

!~

t~

a

",.

t, f~

+~

f~

a

fig. 3.
Cfr. 1963. Reichelina~.

tenuissima
K. M.
MACLAY; SHENG, Acta Palaeont%gica
Sinica, pp. 149-150, pI. 1, figs. 19-22.

0

~.

0

a
!.
a

",.

Shell minute, lenticular to subdiscoidal
in shape with straight axis of coiling,
convex lateral sides, umbilically shallow
depressed poles, and bluntly pointed toarched periphery. Mature shell with 4.5
to 5 volutions, 0.20 mm in axial lengthand 0.53 mm in median width giving form
ratio 1 : 0.4. Half length of the first to
fifth volutions 0.02, 0.03, 0.05, 0.08 and0.10 mm; radius vectors 0.04, 0.07, 0.10,
0.18 and 0.28 mm; width of the first to
fifth volutions 0.08, 0.13, 0.19, 0.33 and0.50 mm, respectively. Spirotheca very
thin, composed of distinct tectum andlower and upper layers. Septa plane andunfluted. Septal counts from the first to
third volutions 8, 13 and 18, respectively.
Axial filling developed in polar regions.
Remarks: The present materials arecomparable to SHENG'S form from the
Changsing and Wuchiaping Limestonesof South China in minute shell, shape of
periphery, slight umbilical poles, thinspirotheca and others. However, uncoiled
prolongation starts from the fourth

f'

j~'

Reichelina dr. tenuissima
K.M. MACLAY

r'

",.

a
0",

fi

g:.

a

~.

f~

a

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+~

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~.
a

~

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_N

a

.

."

~

:;:

a

.-

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~.

a

:'i
a

-

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a
o·
a

t~ t~ Ht~ t~ +~

d

+~

.~

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+i +~

<1l
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(J)

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~

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u

a

+~

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tJ

~

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~

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~
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228

Fumio KOBAYASHI

volution in the Chinese materials, whilesome of the present specimens, shell coils
even at the fifth volution. More numerous
specimens are necessary to make adetailed discussion.
.Reg. nos.: 27049-27053.
Genus Staffella OZAWA, 1925
Staffella sp.
PI. 23, Fig. 30; PI. 24, Fig. 19

Remarlls:
Mineralized shell withstaffelloid shape, arched periphery, convex
lateral sides and umbilical poles is referredto the genus Staffella. Axial length 0.64
to 0.65 mm, median width 0.90 to 1.01 mm
and form ratio 1: 0.6 to 1: 0.7. External
diameter of proloculus 0.05 mm. Dense
secondary mineralization obliterates thedetails of spirotheca as well as inner
structure of shell. Specific identificationis postponed until more specimens
accumulate in the future.
Reg. nos.: 27009, 27048.

References
ERK, A. S. (1941): Sur la presence du genre
Codonofusiella DUNBAR et SKINNER dans
Ie Permian de Bursa (Turquie). Eeal.
Ceol. Herv., Vol. 34, pp. 243-253, pIs. 1214.
FUJIMOTO, H. (1932): Stratigraphical studyof the southern part of the Kwanto
Mountainland. (in Japanese) Jour. Ceol.
Soc. Japan, Vol. 39, No. 466, pp. 430-457.
LEVEN, E. Y. (1967):
Stratigraphy andfusulinids of the Pamir Permian deposits.
(in Russian) Acad. Sci. U. S. S. R., Ceol .
Inst., Transact., Vol. 167, pp. 5-215, pIs.
1-39.
LIKAREV, B. (1926): Palaeofusulina nana sp.
nov. des depots anthracolithiques duCaucase septentrional.
Comm. Ceol.
Leningrad, Bull., Vol. 45, pp. 59-66, pI. 2.
MACLAY, K. M. (1954): The Foraminiferaof the Upper Permian deposits of theNorthern Caucasus. (in Russian) Trudy
Vses. Nauchnoissled. Ceol. Inst., pp. 1163, pIs. 1-19.
SAJ(AGAMI, S. (1956): Fusulinids from thelimestone conglomerate in the. Yagooki
Valley,Tamanouchi,
Hinode·mura,Nishitama-gun, Tokyo-to; Japan. Trans.
Proc. Palaeont. Soc. Japan, N. S., No. 24,
pp. 259-265, pI. 37.
- - (1958): Conglomerates in the Upper
Permian System of the northern part of
Itsukaichi, Tokyo-to, Japan. (in Japanese)
Jubilee Publication, Prof. FUJIMOTO H.,
pp. 91-97.
._- (1972): Discovery of the Early Carboniferous Visean fauna from the Kwanto
Massif. (in Japanese) Jour. Ceol. Soc.
Japan, Vol. 78, No.4, p. 216.
SCHUBERT, R. (1915): Die Foraminiferen
des jiingeren PaHiozikums von Timor.
Paliiontologie von Timor, Lief. 2, pp. 4759, pIs. 39-41.
SHENG, J. C. (1955): Some fusulinids from
Changhsing Limestone. Acta Palaeont.

Explanation of Plate 24
Figs. 1-18. Palaeofusulina nana LIKAREV (See also Plate 23)
1-2, 5-7, 9, 12, 15-18. Axial sections; 3-4, 8, 11, 13-14. Sagittal sections; 10. Pararell
section, 1-18 x30, Reg. nos. 27010-27027.
Fig. 19. Staffella sp. (See also Plate 23)
Axial sectio n x 30, Reg. no. 27048.
Figs. 20-24. Reichelina cfr. tenuissima M. MACLAY
2b, 24. Sagittal sections, 21-23. Axial sections, 20, 22-23 x 50, 21, 24 x 40, Reg. nos_
27049-27053.

KOBAY ASH!:

Palaeofusulina-Reichelina fauna

Plate 24

:1' •.· ..i ~

.

',

~.:

. ,,r""~iC::.':~ "'i~

}\ :.

': ..

"

.':'~.' .

"': ~,.

..

.

·f····

,

."' ~

,'.

.:;;' . ".",''.

'... ..•.

r"

...

~'.:

'.

.,:.

"

....
~ .'

"':'.

.

-..

;."

.. j

..'

.,
.

"

'. '"":'

· 655.

Palaeofusulina-Reichelind fauna

Sinica, Vol. 3, No.4, pp.287-308, pIs. 14.
- - (1963): Permian fusulinids of Kwangsi,
Kueichow and Szechuan. Ibid., N. S. B,
No. 10, pp. 1-247, pIs. 1-36.
- - and CHANG, L. H. (1958): Fusulinids

Okutama
Itsukaichi
Nishinoiri
Yasuba229

from the type-locality of the Changhsing
Limestone. Ibid., Vol. 6, No.2, pp. 205214, pI. l.
THOMPSON, M. L. (1949):
The Permian
fusulinids of Timor. Jour. Palaeont.,
Vol. 23, No.2, pp. 182-192, pIs. 34-36.

Hirai-gawa
KanyhoMusashi-itsukaichi

Trans. Proc. Palaeont. Soc. Japan, N. S., No. 100, pp. 230-238, pl. 25, Dec. 25, 1975

656. A RECORD OF MORTONICERAS (CRETACEOUS AMMONITE)FROM GOSHONOURA ISLAND, KYUSHUTATSURO MATSUMOTO
Department of Geology, Faculty of Science, Kyushu University, Fukuoka

and
MASA YUKI TASHIRO
Shokei High School, Kumamoto;I1}IHltllmUll~.i¥:~ Iv r .::. -I! '7 AO)aa~: )W,*J!j!,mImUll~tLJ:l le:to\, ''L, mImUllRlff9='t5Ilo)
IIb t5IlRlil'1?7Y~7-f ril~.i¥:i±lL.t..:O)<::aatl1;·¥IH!j·i'"Go .:..nft{:Emil~{JiI:ff~.n, ~;ff0)i!t
J:l~~i±l (rostrum) tft~<::~GH'I!*<::~Go *~0)J:t5Il7Ivt::"7Y J:t5Il.i¥:O) Mortoniceras (M ortoniceras) rostratum lel!iMtli'" Gil~, ~~t.(~<::~~il~~ Go /i'fJ:ffiO)~~il~+7tJ:<:bil'-:>'L\"t.(\',m:!*<::ft, .:.O){t15~ M. (M.) sp. aft. M. (M.) rostratum cJ:
A, <:::to <0 .:. 0) .i¥:i±l Ie J: IJ IIb t5IlRlltJ:t5Il7 Iv t::" 7 Y C !i'~~ L, i'"<::le ~ I?,nt..: IIe ft,
Graysonites O).i¥:i±lte J: IJ rt5ll-l! / ,,"'::' 7 Y<::~ Gil' I?, J:. ra!ll!*o)~ft IIb-IIe rdlO)':'il'te~ G':' c c t.( G 0 ft!!O)ilikf;f>j}J!f'kI{t15il t .:. O)ra'<:: cO) J: ? t.(~{t~ff-i'"il'il~4-~O)~J8!ct.(Go t.(:to.:. 0) 7 Y~7-f HU::>\,''L, :j,IUtUI~~~1:.m~~te~i'"GIDfUii!~ll>\.lj.Go:t~*~a~· EBfI;;lEz.

cand gastropoda of shallow sea facies
and partly those of brackish water or
non-marine facies. Hence it used to becalled the Trigonia Sandstone (e. g. YEHARA, 1923). Ammonites are rather rare
and limited to particular beds.
Among previously reported ammonites,
Graysonites sp. cf. G. fountaini YOUNG,
from Member lIe, is the most important,because it indicates the lower part ofLower Cenomanian (MATSUMOTO, 1960).
Fortunately we have recently acquired
another good age indicator, an ammonite
referable to Mortoniceras, from a bed ofdifferent horizon. In this paper we givea palaeontological description of thisammonite, discuss the age of the Goshonoura Group and attempt to consider thepalaeoecology and palaeoenvironment.
Before going further we thank Mr.

Introduction

Goshonoura Island of Kumamoto Prefecture (Fig. 1) is well known for theabundant occurrence of Cretaceous molluscan fossils. As was described in detail by one of us (MATSUMOTO, 1938),
the island is geologically made up of the"Middle" Cretaceous Goshonoura Groupin the main part, the Senonian Himenoura Group in the northwestern coastal
belt, and a faulted block of basement
granite cropping out at the northeastern
corner. The Goshonoura Group consists
primarily of sandstones of various gradesof coarseness with some red beds. Its
molluscan fossils are primarily bivalvia* Received June 17, 1975; read June 14,1975 at Morioka.
230

656.

Fig. 1.

Mortoniceras from Goshonoura

231

Outline geological map of Goshonoura island, showing the locality of

Mortoniceras with a solid circle (.).
Outcrop of Member lIb is indicated with ruled areas; boundary of memberswith dotted line; that of formation with fine broken line. I, II, III: Lower, Middle and Upper Formations of the Goshonoura Group; H: Himenoura Group; G:
Granite.
Inset is a map of Kyushu (upper left corner), indicating with a solid circle
the location of Goshonoura Island (Go).
(Adapted from MATSUMOTO, 1938, with revision)

Sanemi KOMATSU, teacher of Kameba(Hondo) Primary School (formerly teacherof Amura Primary School), who cooperated with one of us (M. T.) in collecting
fossiliferous rocks. Miss Mutsuko HAY ASHIDA has assisted us in preparing themanuscript. This work is one of thecontributions to the rGCP Mid-Cretaceous
Events.
Palaeontological description

Superfamily Acanthocerataceae

Family Brancoceratidae
Subfamily Mortoniceratinae
SPATH, 1925
Genus Mortoniceras MEEK, 1876

Type-species.- Ammonites vespertinus
MORTON, 1834.
Remarks.- One of us (T. M.) had opportunities to study the syntypes (ANSP.
4783) of MORTON (1834, p. 40, pl. 17, fig.
1) at the Academy of Natural Sciences,

232

Tatsuro MATSUMOTO and Masayuki TASHIRO

Philadelphia, and other good examples
from the Duck Creek Limestone in thecollection of U. S. Geological Survey,
Denver, by courtesy of Dr. W.A. COBBAN,
gave a brief note on them (MATSUMOTO,
1960, p. 37, fig. 1), and as a result, agreeed WRIGHT'S (1957, p. L406) definitionof the genus and also the subgenus
Mortoniceras (s. s.), rejecting YOUNG'S(1957, p. 3) concept in which the characters of the type-species were ignored.

M ortoniceras (Mortoniceras)

sp. aff. M. (M.)
rostratum 0. SOWER BY)
PI. 25, Fig. 1; Text-fig. 2Compare:1932. Mortoniceras (Pervinquieria) rostratum(1. SOWERBY, 1817), SPATH, Ammonoidea of the Gault, part 9, p. 400 (withfull synonymy list).

Material: KE. 2241, collection of M.
TASHIRO, from Enokuchi, Goshonoura
island, Amakusa-gun, Kumamoto Prefecture. It is represented by an externalmould in the sandstone and partly by aninternal mould, but the shell material isdissolved away. A plaster cast of thisspecimen, GK. H5738, is preserved at
Kyushu University.
Description: This single specimen issecondarily modified to an elliptical outline, owing probably to a tectonic deformation. It is about 155mm in thelongest diameter of the deformed shapeand the width of the umbilicus is measured at 39 percent of the diameter. The
ratio of whorl-breadth to height cannot
be precisely measured, but the whorl
seems to be somewhat higher than broad.
Despite the secondary deformation theliving chamber is almost wholly pre. served. It occupies a .little more than ahalf (200·) of the outer whorl and therostrum at its apertural margin shows arecurved shape, although the very apexof the rostum is not preserved.
The main part of this adult living
chamber is ornamented with fairly distant, coarse, strong, equally long ribs,
each of which has a bullate umbilical,
nodate mediolateral, prominent inner
ventrolateral and clavate outer ventrolateral tubercles. The last two tend tobe approximated as the shell grows, resulting in a doubled appearance. They
are finally amalgamated into a large
ventrolateral tubercle at the stage anteriorly about 90· from the last suture.
On the last part (about 30·) of the living
chamber the ribs gradually become lessdistant, by which the tubercles tend to
be absorbed, and finally the ribs remainon the inner half and branched to ribletsand lirae on the outer part which extends to the rostrum.
The keel, which is partly preserved, isfairly sharp on the internal mould but
moderately thick on the external mould.
The septate whorl is ornamented with
densely spaced ribs which consist of
primaries and inserted or branchedsecondaries. The umbilical tubercles arebullate; the mid-lateral tubercules are atfirst indiscernible, then becoming more
distinct on the later part, although not
so strong as those on the living chamber.
The last suture, which is preserved at
the posterior end of the fragmentaryinternal mould, shows the broad, massive, bipartite saddle between E and L
and the widely open L.
Comparisons: If the deformed shape
be restored, this specimen closely resembles the holotype of Mortoniceras (Mortoniceras) rostratum 0. SOWERBY), from
the Malmstone of Oxfordshire, England(see SPATH, 1932, text-fig. 136). The two
specimens show the same recurved shape

656.

233

lVIortonice?"as from GoshonOU1"a
Q

b

"

a
F ig. 2. Mo rton iceras ( Morto niceras) sp. aff. M. (M .) rostratU11! (J. SO WE RB Y) .
Intern a l mould of t he posterior part of the li ving chamber (part of KE. 2241) ,w it h t he last septum at its end . Side v iew (a ) , restored w horl-section (b) at Q,
and t he last suture ( partl y resto red fro m that of t he other si de) ( c) . See PI. 25,
Fig. 1d fo r the ventra l v iew .

of the rostrum . In another t ypical specimen of 1\IJ. (M.) rostratum from theMalmstone, illustrated by SPATH (1931,
pI. 36, fig. 6), the lateral tubercles seemto appear earlier and are more distinct
on the inner whorl than in the present
specimen but as strong as ours on theouter whorl; they are situated closer tothe ventrolateral tubercles than in ours.
In the same character and in the narrower ribs as well as broader whorls,
M . (M .) stoliczlwi SP ATH, 1921, from
India (STOLICZKA, 1865), Angola (SPATH,
1925) and Madagascar (COLLI GNON, 1963),
is distin g uished from ours, but its ribbing on the inner w horl is as densel yspaced as ours.
In the mode of r ibbing and tuberculation on the outer whorl the Goshonoura
form is similar to M. (M .) vespertinum(MORTON), but the latter has distinctly
coarser ribs on the inner whorl and a
depressed section and larger size of theadult whorl. · The apertural margin is
not known in this Gulf Coast species.
Despite the well known specific na mes,
the true extent of variation and therelationships of the three species mentioned above are not necessarily clear.
Therefore it is hardly decided whether
or not the above described differences
are great enough fo r specific or subspecific distinction. Moreover , our material itself is insufficien t. For the time
being the describ ed specimen from Goshonoura is called Mortoniceras (Mortonicera s) sp. aff. M. (M. ) ro stratu m 0.
SOWERBY).
Occurren ce : The described ammonite
was collected from one of the fallen
blocks of sandstone at Enokuchi, southeastern coast of Goshonoura isl and . It
was associated with Gly cymeris (Ha naia )solida, A canthotrigonia oga wai, . Cra ssatellites (Pachy thaeru s) nagaoi, "Cal/ista"
crenulata , etc. The block was undoubted ly derived from Member IIb, middle
fo rmation of the Goshonoura Group.
Age of 't h e Goshonoura GroupThe Goshonoura Group is lithostrati graphically divided as follows . in ascending ,order . (MATSUlVlOTO, 1938; OKADA,

234

Tatsuro MATSUMOTO and Masayuki TASHIRO

1961):
I. Lower Formation, 200m.
Ia. Coarse-grained, feldspathic arenite, sometimes conglomeratic, crosslaminated, massive or thick bedded,
with lenticular red beds, almost barren of fossils.
lb. Feldspathic wacke of various
grades of coarseness, bedded, withthin coaly seams, mudstone andseveral prolific fossiliferous layersof shallow sea to brackish water
facies.
II. Middle Formation, about 550m. Sandstones (mainly feldspathic wacke andpartly feldspathic and quartz-feldspathic wacke and partly feldspathic
and quartz-feldspathic arenite) containing molluscan fossils of generally
shallow sea environments (the socalled Trigonia Sandstone). This is
subdivided into five members, Ila toIle in ascending order. Members
Ilb (180m) and Ile (150m) consist of
massive well-sorted, medium- to finegrained sandstones, containing abundantly molluscan fossils (trigonians,
Cucullaea, Anthonya, "Callista" etc.)of shallow open sea facies in lenticular beds and calcareous nodules.
Ammonites are occasionally associated with them. Members IIa (100m)
and IIc (70m) are ill-sorted, coarsegrained, sometimes conglomeratic,
feldspathic wacke, containing trigonians and other mollusca. Member lId (50m) consists of conglomerate and sandstone with some red
beds and brackish-water mollusca.
III. Upper Formation, 200 m or less.
Sandstones of various grades ofcoarseness, conglomerate (sometimes
boulder-bearing), mudstone and red
beds, with fossiliferous layers ofbrackish to fresh water facies. Sandstones are mainly of lithic wacke.

This formation may be subdivisible
into several members in accordancewith the predominant rock assemblage among the above, but there islateral change in the details of facies.
One of us (MATSUMOTO, 1938) once
stated that the Goshonoura Group is
mid-Cretaceous, that its main part isapproximately referable to Cenomanian[Gyliakian] and that its lower part possibly ranges down to Albian [Upper
Monobegawa]. This conclusion was arough estimation on the basis of theprovisional study of the molluscan fauna
as well as the stratigraphic sequence,but it is now confirmed on more reliable
evidence.
Mortoniceras (Mortoniceras) rostratum
occurs, according to SPATH (1932, p. 405),
in the Zone of Stoliczkaia dispar, upper
part of Upper Albian in England andFrance. M. (M.) stoliczkai occurs fromthe Upper Albian of southern India,
Madagascar and Angola. M. (M.) vespertinum probably came from the Duck
Creek Limestone (ADKINS, 1928), whichis assigned to the lower part of Upper
Albian (STEPHENSON et aI., 1942).
How far the zonal sequence establishedin western Europe can be maintained inJapan, which was much distant and belonged to a different biogeographicalprovince, may be a question. This isespecially questionable when the species
are not quite identical.
So far as the better studied material
is concerned, most of the species belonging to the Acanthocerataceae do notshow discrepancy in the biostratigraphic
succession at substage level between
Europe and Japan, if identical or closely
allied species are taken into consideration (e. g. MATSUMOTO, 1975). Of course
there can be local difference in the subzonal succession. Consequently we arereasonably led to regard the age of656.

Mortoniceras from Goshonoura

Member lIb as Upper Albian, if not convinced of the upper Upper Albian. To
determine whether it is upper Upper
Albian or otherwise, we should complete
the list of associated ammonites.
It has already been concluded (AMANO
et at. in MATSUMOTO, 1960) that Member lIe is most probably assigned tolower Lower Cenomanian on account ofGraysonites cf. fountaini YOUNG and
Desmoceras kossmati MATSUMOTO obtained from it. In Texas G. fountaini
occurs in the Zone of Graysonites adkinsi,
which is in the lower, but not basal, partof Lower Cenomanian, since the Zone of
Plesioturrilites brazoensis is allocated at
the base of the Cenomanian (YOUNG,
1958). Should this succession be maintained in Japan, there would be someroom below Member lIe for the basal
Cenomanian. In other words Member
lId may still be within Lower Cenomanian. As the fossils contained in lId
are mostly of endemic species, direct
evidence for the correlation with theinternational scale is not available forlId.
To sum up, the Albian-Cenomanianboundary would be either at the base of
IId or at the base of IIc; or could besomewhere within Member IIc. Sinceammonites could scarcely be expectedfrom lId and IIc in view of their facies,
further search for more ammonites from
Members lIb and lIe would give evidence
to decide one of the alternatives.
Another problem to be settled in the
future is whether and how other molluscan fossils, such as species of the
Trigoniidae and Glycymeridae, are changed or unchanged across the AlbianCenomanian boundary in the Goshonoura
and other sequences in Japan.
Incidentally the Upper Formation of
the Goshonoura Group is most probably
correlated with the lower part of the235

Mifune Group, southwest of Kumamoto,on account of common occurrence ofsuch diagnostic species as Matsumotoa
japonica OKADA, M. unisulcata (AMANO),
Acanthotrigonia yeharai (NAKANO andNUMANO) and Crassostrea sp., as clearly
discussed by TAMURA et al. (1968). Recently Eucalycoceras sp. cf. E. spathi(COLLIGNON) and Inoceramus concentricus
costatus NAGAO and MATSUMOTO havebeen discovered from a part of theLower Mifune, which indicate Middle toUpper Cenomanian (TAMURA et at. 1974).
Therefore, the Goshonoura Group is not
likely to extend to Turonian in age andthere should be an unconformity or hiatus
between the Goshonoura Group and theSenonian Himenoura Group.

Further remarks(Tatsuro MATSUMOTO*)
It should be noted that the adult living chamber is preserved in the specimen of Mortoniceras from Member lIb
as in the case of Graysonites from Member lIe. This implies that the sedimentary condition was rather quiet during
the deposition of lIb and lIe. The petrographical characters of the sandstones(well sorted, medium to fine-grained
wacke with muddy matrix) support thisas investigated by OKADA (1960).
The bottom sediments where adultshells of Mortoniceras were embedded
are not always of the same kind. For
instance, Malmstone (fine-grained glauconitic sandstone) in the case of Oxfordshire examples, and limestone in the caseof Duck Creek ones, and medium to finegrained sandstone with muddy matrix
in our case. They are all sediments* T. MATSUMOTO alone is responsible forthis article.

236

Tatsuro MATSUMOTO and Masayuki TASHIRO

under calm shallow sea, although theabsolute depth is hardly estimated withthe available data.
As can be judged from the differencein the characters of ribbing and tuberculation between the adult and immatureshells, the animals of Mortoniceras may
have changed to some (if not great)extent their mode of living during theirlife history. Especially the rostrum at
the apertural end of the shell suggests
a particular mode of life of the adultanimal. The function of the rostrum,
especially a recurved one as in M.
rostra tum, has not yet been sufficiently
investigated, although the morphology
itself was noticed long ago (e. g. STIELER,
1922).
Presumably the animal of Mortoniceras
must not have been a rapid swimmer.
The rectiradiate, strong ribs with fairly
strong tubercles and the sub quadrate
whorl section would be shell characters
against the stream. The adult animal
may have moved up and down in thesea-waters to some extent, controllingthe buoyancy of air-chambers, and also
could have swimmed slowly backward.
The raised or recurved rostrum may
have served as a kind of anchor when
she settled herself on the bottom sediments under the sea water. A moderately long and broad living chamber
occupied by the animal would make theentire shell less buoyant.
The above is a working hypothesis
which should be examined further bysome model experiment or by theoretical
calculation. Another, more serious probblem is about the funnel. In Nautilus
and most of Paleozoic Ammonoidea(Goniatitida defined by MATSUMOTO,
1974) the hyponomic sinus is distinctly
present on the ventral (i. e. external) sideof the shell. In most of the Mesozoic
Ammonoidea (Ceratitida and Ammonitida,

except some Lytoceratina), there is nohyponomic sinus on the ventral side but
instead the external part of the shell ismore or less projected. This is extreme
in the case of Mortoniceras which bears
rostrum. I dare propose an idea as aworking hypothesis that the funnel inmany Mesozoic ammonoids may havedoubled openings or have been in pair,being produced somewhere at the ventrolateral part. HOEPEN (1951) described a
distinct sinus at the ventrolateral part(or outer lateral part) of "Pervinquieria"
scobina. This sinus may correspond tothe hyponomic sinus (one of the pair).
Many other Mesozoic ammonites (e. g.
Ho/cophylloceras, Harpoceras, Desmocerasetc.) show a more or less sinuous apertural margin which has a pair of outer
lateral (or ventrolateral) and inner lateralor umbilical) sinuses. The former ispresumably one of a paired hyponomic
sinuses, while the latter is certainly
an ocular sinus.
How to prove or
disprove this working hypothesis afuture problem.

References cited
ADKINS, W. S. (1928). Handbook of Texas
Cretaceous fossils. Univ. Texas Bull.,no. 2838, 303p., 37 pis.
COLLIGNON, M. (1963). Atlas des fossiles
caracteristiques de Madagascar (Ammonites), fasc. 10 (Albien), xv+18p., pis.
241-317, Servo Geol., Tananarive.
HOE PEN, E.C.N. VAN (1951). Die gekielde
Ammoniete van die Suid-Afrikaanse
Gault. 6. The so-called old mouth-edgesof the ammonite shell. Paleont. Navors.
Nas. Mus. Bloemfontein, vol. 1, no. 8,273-284.
MATSUMOTO, T. (1938). The geology of
Goshonoura Island, Amakusa. (Withspecial reference to the Cretaceous
stratigraphy). Jour. Ceol. Soc. Japan, vol.
45, p. 1-47, pis. 1-4 [in Japanese with

656. Mortoniceras from Goshonoura
Engl. palaeont. descrip.].. (1960a). On some type ammonites fromthe Gulf Coast Cretaceous. Sci. Rep.
Dept. Geol., Kyushu Univ., vol. 5, no. 1,
p. 36-49 [in Japanese with Engl. abo
stract].
- - (1960b). Graysonites (Cretaceous Am·
monites) from Kyushu. With notes on
stratigraphy by AMANO, M., MATSU·
MOTO, T., OKADA, H. and OGURI, H.
Mem. Fac. Sci., Kyushu Univ., ser. D,
vol. 10, no. 1, p. 41-58, pIs. 6-8.
- - (1974). Cephalopoda [Tosoku.rui]. In
MATSUMOTO, T. (ed.) Palaeontology[Koseibutsu.gaku] vol. 2, p. 62-160. Asa·kura Book Co., Tokyo [in Japanese].
- - (1975). Additional acanthoceratids from
Hokkaido. Mem. Fac. Sci., Kyushu Univ.,
ser. D, vol. 22, no. 2, p. 99-163, pIs. 11-23.
MORTON, S. G. (1834). Synopsis of the organic
remains of the Cretaceous group of theUnited States. 88 p., 19 pis., Philadelphia.
OKADA, H. (1961). Cretaceous sandstonesof the Goshonoura Group. Mem. Fac.
Sci., Kyushu Univ., ser. D, vol. 11, no.
1, p. 1-48, pIs. 1-2.
SPATH, L. F. (1922). On Cretaceous Cephalo·
poda from Zululand. Ann. South AfricanMus., vol. 10, no. 3, p. 113-147, pIs. 5-9.
- - (1925).
On Cretaceous Ammonoidea
from Angola, collected by Professor J.W.
GREGORY, D. Sc., F. R. S. Trans. Roy. Soc.
Edinb., vol. 53, pt. 1, p. 91-160, pis. 1-4.
- - (1931). Amonograph of the Ammono.
idea of the Gault. Part 8. Palaeontogr.
Soc. (London), 1929, p. 313-378, pis. 31-36.
- - (1932). A monograph of the Ammono·idea of the Gault. Part 9. Ibid., 1930, p.
-

237

379-410, pis. 37-42.
STIELER, C. (1922). Anomale Miindungenbei Inflaticeraten. Unter Beriicksichtung
derselben Erscheinung bei anderen Mol·lusken. Neues jahrb. Min. Geol. Palaont.,
Beil. Bd., 47, p. 295-346.
STEPHENSON, L. W., KING, P. B., MONROE,
W. H. and R. W. IMLAY (1942). Correia·
tion of the outcropping Cretaceous for·mations of the Atlantic and Gulf Coastal
Plain and Trans·Pecos, Texas. Bull.
Geol. Soc. Amer., vol. 53, p. 435-448,
pI. 1.
TAMURA, M., TASHIRO, M. and MOTOJlMA,
T. (1968). The correlation of the Mi·
fune Group with the upper formationof the Goshonoura Group, with descrip.
tion of some important pelecypods fromthe strata. Mem. Fac. Educ .. Kumamoto
Univ., no. 16, sec. 1, p. 28-43.
TAMURA, M. and MATSUMURA, M. (1974).
On the age of the Mifune Group, with adescription of ammonite from the groupby T. MATSUMOTO. Ibid., no. 23, sec. 1,
p. 47-56, pI. 1.
WRIGHT, C. W. (1957).
In MOORE, R. C.
(ed.): Treatise on Invertebrate Paleonto·
logy. Part L, p. L119-L232, L362-L437,
Geol. Soc. Amer., Univ. Kansas Press.
YEHARA, S. (1923).
Cretaceous Trigonia
from Southwest Japan. japan. jour. Geol.
Geogr., vol. 2, no. 3, p. 59-84, pIs. 8-13.
YOUNG, K. (1957). Upper Albian (Cretaceous)Ammonoidea from Texas. jour. Paleont.,
vol. 31, p. 1-33, pis. 1-10.
_ . (1958). Graysonites, a Cretaceous am·
monite in Texas. Ibid., vol. 32, p. 171182, pis. 27-29.

Explanation of Plate 25
Fig. 1. Mortoniceras (Mortoniceras) sp. aff. M. (M.) rostratum (1. SOWERBY). Specimen from
Goshonoura island, KE. 2241. Lateral view (a), the other side of a part of the rostrum(b), the other side (c) of the plaster cast; ventral view of the internal mould of theposterior part of the living chamber (d) (see Text.fig. 2 for the same internal mould).
All figures of natural size. Repository: Department of Geology, Faculty of Education,
Kumamoto University, Kumamoto 860.

238

Tatsuro MATSUMOTO and Masayuki TASHIRO
Amakusa
Amura
EnokuchiGoshonoura
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239

PROCEEDINGS OF THE PALAEONTOLOGICAL SOCIETY
OF JAPAN

E *ti~E.''I'!Q~~~ 116 @)f1lj~lt, 1975 ~ 9 }j 23
E ('k) . 24E (71<.) t;::~tR::k~3:l!l~$t;:::to\',-clmfl€

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(ftWi:) ........................... ·~m*:f!I!t;::":)\,,-C .............. 1ll~~;Jc. tt;*J.ijtz;jfl1£ItH[ Syringopora Q)~:iH£I;f\'4'~t;::":)\,,-C ......

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chia·type Q)!t~fift;::":)\,'-C) ........ t'~Ji€JI§~
New discovery of the Tetori·type Florafrom the Tokura Formation, Gumma
Prefecture, Japan ..................... .
......... . T. KIMURA, S. SAITO & T. ToJO
The new occurrence of some dipteridaceous
ferns from the Daedong Group, Korea ..
· . . . . . . . . . . . . . . . . . .. T. KIMURA & B. KIM~tR m~71-Q)::k~~ '/J' I? ~I±I L. t.: !I Iv ~ ~*t;::":) \, '-C (ftWi:) .. ·.·.·········.·.····::k:ft-;Jc

Discovery of Palaeofusulina from the To·
yoma Formation in the Kitakami Massif,
Northeast Japan (f'CWi:) ................. .
.................. M. MURATA & K. ISHII
Upper Carboniferous fusulinacean from theOmi Limestone ............ K. WATANABE
Ij'32:.llj(~!1I;£l:!1I;H[ Discocyclinidae (Larger
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242

List of Contributors
to the TPPSJ, New Series, Nos. 1-100(n: single author, n: co.author, n: presidential address, n: short note etc.)A
AKAGI, Saburo 43
AKIY AMA, Masahiko 25, 31
AKUTSU, Jun 21
AMANO, Masahisa 17
AOKI, Naoaki 39,41,53,54,62,67,70,71,74
AOKI, Shigeru 22
ARAKI, Yoshio 33, 36
ASANO, Kiyoshi 10,11
B
BANDO, Yuji 50,56,78,79,93,94,97
BURCKLE, Lloyd, H. 82,96
BURTON, C. K. 65

HATAI, Kotora 23,23,27,42,42,43,45,46,
49,57,57,60,72,81,83,86,87,88,95,
100
HAYAMI, Itaru 26,28,29,30,34,34,35,35,38,
43,43,59,60,66,73,73
HAYAMI, Tomoko 79,82,84
HAYASAKA, Ichiro 7,10,12,15,16,21,23,
52,75
HAYASAKA, Shozo 10,38,47,57,60
HIGUCHI, Yu 60,65
HIRANO, Hiromichi 89, 90
HIRATA, Motome 74,76
HIRAYAMA, Katsumi 31
Hu, Chung-Hung 51,52,78,82,85,95,97
HUANG, Tunyow 60,62,68
HUZIOKA, Kazuo 3,13,14,16,19,41,77,89
I

c
CHINZEI, Kiyotaka 67,90
CHOI, Dong Ryong 86
D

DANNER, W. R. 90,91,93
DOMNING, D. P. 80
E
ENDO, Riuii 4,5,8,31,74
ENDO, Seido 1,50,52,61

F
FUJI, Norio 73,74,76,86
Fu JIMOTO, Haruyoshi 18, 21
H

HADA, Shigeki 62
HAMADA, Takashi 58,100
HANAI, Tetsuro 44
HANZAWA, Shoshiro 5,65,68
HASE, Akira 42
HASE, Kotaro 58
HASEGAWA, Yoshikazu 45,69
HASHIMOTO, Wataru 12,32,40,55

ICHIKAWA, Koichiro 1,2,17
ICHIKAWA, Takeo 19,60
IcHIKAWA, Wataru 4,27,31
IcHIKURA, Masaki 91
IGo, Hisaharu 92
IGo, Hisayoshi 18,22,34,43,53,53,54,59,96
IMAIZUMI, Rikizo 6,7,25,27,32,57
INoMA, Akitoshi 87
INOUE, Eiji 46
ISHIBASHI, Takeshi 77,88,96
ISHII, Ken-ichi 44,44
ISHIKAWA, Hideo 62
ISHIZAKI, Kunihiro 50,51
ITOIGAWA, Junji 25,29
IWAI, Takehiko 37,41
IWAMOTO, Hisaichi 45
IWAsA, Saburo 16
IWASAKI, Yasuhide 51,67,77,99
K
KAMADA, Yasuhiko 6, 15, 17
KAMBE, Nobukazu 2
KANIE, Yasumitu 49
KANMERA, Kametoshi 24
KA:"1NO, Saburo 18,19,24,25,32,33,42

243
KANUMA, Mosaburo 26
KAPOOR, Hari Mohan 93
KASENO, Yoshio 2
KATAOKA, lun 28
KATO, Makoto 26,28,28,29,33,72,81
KA WANO, Michihiro 36
KAWASAWA, Keizo 66
KIKUCHI, Yoshiki 16
KIM, Bong Kyun 93
KIMURA, Tatsuaki 29,41,84,86,98
KIRII, Yoshihiro 24
KOBOYASHI, Fumio 92,96,100
KOBAYASHI, Manabu 23
KOBAYASHI, Teiichi 1,3,4,5,6,8,12,17,19,

20,23,24,26,27,28,30,31,37,41,58,77
KOIKE, Toshio 53,59,96
KOIZUMI, Itaru 86,91
KOMURA, Seiichi 99
KONISHI, Kenji 5,7,12,35,40
KON'NO, Enzo 40
KOTAKA, Tamio 10,42,43,45,47,49,81
KOTOH, liro 22,25
KURIHARA, Kenji 70,83
KURODA, Hidetaka 55
KUWANO, Tadashi 97

M
MAEDA, Shiro 4,36,46,47,48,49,51,56
MAIY A, Seijuro 91
MAKIY AMA, liro 5
MASATANI, Kiyoshi 17
MASUDA, Koichiro 8,12, 13,14, 15,20,21,21,

22, 23, 24, 30, 31, 32, 33, 33,34,35,38,39,46,
49,52,63,64,65,72,75,83,84,86,95
MATOBA, Yasumochi 55
MATSUI, Masaru 30
MATSUMARU, Kuniteru 64,72,84
MATSUMOTO, Tatsuro 1, 12, 18, 22, 23, 27,
53, 56, 61, 62,63,64,71 ,76,87,89,97,97,
100,100
MATSUNAGA, Takashi 15,18
MATSUO, Hidekuni 14,40,55,66,71,80
MA TSUOKA, Kazumi 94
MI);ATO, Masao 1,11,16,18,21,21,25,26,
28,29,72
MIZUNO, Atsuyuki 6, 9
MORI, Kei 50,56
MORI, Ryuji 74
MORIKA\rA, Rokuro 3,41
MORISIlITA, Akira 9,11,13,20,58

MeLLER, Klaus]. 55
MURAMOTO, Tatsuo 87
MURATA, Masafumi 54,57,82,97
MCRA T A, Shigeo 3

N
NAGAO, Sutekazu 55
NAGASAWA, loji 42,43,47,51,59,61,66
NAITO, Gentaro 40
NAKAI, Isao 59,62
NAKAMURA, Koji 21,35
NAKANO, Mitsuo 42,43,44,48,68
NAKAZAWA, Keiji 17,25,30
NATORI, Hiro'o 55
NEMOTO, Mamoru 57
NISI-IIDA, Shiro 71,75,80,83
NISHIDA, Tamio 69,69,70
NISHIMIYA, Katsuhiko 89
NODA, Hiroshi
59,69,72,75,77,78,81,83,
86,87,88,88,93,95,100
NODA, Masayuki 64,71,88,93,100
NOGAMI, Yasuo 44
NUMANO, Kyoichiro 43o
OBATA, Ikuo 46,56,58,66,67,76
OGASAWARA, Kenshiro 87
OGASAWARA, Kenzo 7
OGURA, Yuzuru 4,8,19,44
OHTA (=OTA), Yoshihisa 33,34,34,79,98
OKAFUJI, Goro 69
OKA!v!OTO, Kazuo 48,68,95
OKIMURA, Yuji 87
OK UNO, Haruo 13,14,19,21,31,36
OMATA, Toshikazu 34
OYlURA, Kazuo
71
OSHITE, Kei 24
OYAMA, Katura 46
OYAMA, Toshiji 55
OZAKI, Hiroshi 64
OZA WA, Tomowo 68, 73sSADA, Kimiyoshi 63,67,75,87,90,91,93
SAITO, Minoru 78
SAITO, Rinji 22
SAITO, Tsunemasa 45,48, 91
SAITO, Yasuji 56
SAKA, Yukiyasu 85
SAKAGAMI, Sumio 24, 26, 34, 39, 43,46,48,

244
49,52,56,57,85,90
SAKAGUCHI, Shigeo 49
SATO, Tadashi 20,49,85,96
SATO, Teruo 56
SEKIDO, Shinji 84,86
SHIBATA, Matsutaro 23,25,39,40,42
SHIKAMA, Tokio 1,9,24,44,45,64,69,80
SHIMIZU, Daikichiro 17
SmMOY AM A, Shoichi 94
SHUTO, Tsugio 20,31,37,55
SUGl, Tomomitsu 39
SUGITA, Munentitsu 47
SUZUKI, Keiji 14,29
SUZUKI, Nobuo 52T
TADA, Motohiko 69
TAKAHASHI, Eitaro 89
TAKAHASHI, Kiyoshi 30,46,51,54,73,78,81
TAKAI, Fuyuji 41
TAKAOKA, Yoshinari 41
TAKAYAMA, Toshiaki 87
TAKAYANAGI, Yokichi 3,45
TAMURA, Minoru 33,34,35,36,37,38,39,44
TAN, Li-Lin 82
TANABE, Kazushige 92,99
TANAI, Toshimasa 7,8,9,37,52,66
TANAKA, Keisaku 42,59
TASHIRO, Masayuki 84,86,100
TAZAWA, Jun-ichi 94
TERACHI, Masami 95

TODD, Alayne 96
TOKUYAMA, Akira 27,32,35,44
TOMIZA WA, Tsuneo 33
TORIY AMA, Ryuzo 15uVcmo, Takayasu 2,7,67
VEDA, Yoshiro 50
VJIIE, Hiroshi 60,61,91
VOZUMI, Satoru 15,19,47
VRATA, Hideo 55

w
WATANABE, Kozo

95,99

Y
YABE, Hisakatsu 33
YABE, Yukio 17
YAMAGIWA, Nobuo 23,44,44,49,85,89
YAMAKUCHI, Shiro 62
YAMAUCHI, Hiroshi 69
YANAGIDA, Juichi 72,74,90
YANAGISAWA, Ichiro 57
YANG, Seong-Young 95, 100
Y AO, Akira 73
YOKOYAMA, Tsuruo 38,63
YOON, Sun 93
YOSHIDA, Saburo 26
YOSHIDA, Shinji 44
YOSHIDA, Takashi 28

245
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19771j::l!£Q)Jtl'lBtC?Xflm~llbnlt~~ $~ L, 19771j:: 11 .R ;:: 0 1±l!ltiiQ)7~-e~ Q
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Transactions and Proceedings of the PalaeontologicalSociety of Japan

New Series No. 100

December 25, 1975

CONTENTSEDITORIAL . . ... . . . .. . . .. .. . ..... . . .......... . . . .. .. ............ . . . .. .. ...... . . 175
TRANSACTIONS

652. YA NG, Seong-Young: On a new non-marine pelecypod genus from the Upper
Mesozoic Gyeongsang Group of Korea ..... ... . .. . . . . ..... . ........ . .. 177

653. MATSUMOTO, Tatsuro and NODA, Masayuki:

Notes on Ino ceramus labia/u s(Cretaceous Bivalvia) from Hokkaido . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 188654. HATAI, Kotora and NODA, Hiroshi: An armored worm from the Miocene
Yoko-o Formation, Nagano Prefecture, Japan .. .... ............. .. ..... 209

655.

KOBAYASHI, Fumio:

Palaeofu sulina-Reichelina fauna contained in the peb-bles of intraformational conglomerate distributed in the Okutama district, West Tokyo .. . . . ..... . . . .. . . ... . .. . .. . . . . .. . ...... . " .. . ... . ... 220

656. MATSUMOTO, Tatsuro and T AS HIRO, Masayuki: A record of Mortoniceras(Cretaceous ammonite) from Goshonoura Island, Kyushu . . . . .... . ..... 230
PROCEEDINGS .. ... . . ....... . ..... ... . ..... ....... . .. . . .. . . . ... . . . . .. . . . . . .... 239
LIST OF CONTRIBUTORS (New Series Nos. 1- 100) .. .. .... . . . ..... . . ........ .. 242