ISSN 0031- 0204

Transactions and Proceedingsof thePalaeontological Society of Japan
New SeriesNo. 137

Pa laeontological Society of JapanA pri l 30, 1985

Co-Editors

Takashi HAMADA and Hisayoshi !GO

Officers for 1985-1986
President: Toshimasa TANAI
Honorary, President: Teiichi KOBAYASHI
Councillors;

Kiyotaka CHINZEI, Takashi HAMADA, Tetsuro HANAI, Yoshikazu HASEGAWA,

Itaru HAY AMI, Hisayoshi IGO, Junji ITOIGAWA, Tadao KAMEl, Tatsuaki KIMURA,
Tamio KOTAKA, Kei MORI, Ikuwo OBATA, Tsunemasa SAITO, Yokichi TAKAYANAGI,
Toshimasa TAN AI
Members of Standing Committee:

Kiyotaka CHINZEI (Membership), Takashi HAMADA (Co-

Editor of Transactions), Yoshikazu HASEGAWA (Foreign Affairs), Itaru HAY AMI(Planning), Hisayoshi IGO (Co-Editor of Transactions), Tatsuaki KIMURA (Finance),
Ikuwo OBATA (General Affairs), Yokichi TAKAY ANAGI (Editor of "Fossils"), Juichi
YANAGIDA (Editor of Special Papers)
Auditor: Yoshiaki MA TSUSHIMA

The fossil on the cover is Unuma (Spinunuma) echinatus ICHIKAWA and YAO, a
Middle Jurassic multisegmented radiolaria from Unuma, Gifu Prefecture, central
Japan (photo by A. YAO, X 260).

All communication relating to this journal should be addressed to the
PALAEO~TOLOGICAL SOCIETY OF JAPAN

c/o Business Center for Academic Societies,
Yayoi 2-4-16, Bunkyo-ku, Tokyo 113, Japan

Trans. Proc. Palaeont. Soc. Japan, N.S., No. 137, pp.I-18, pis. 1-3, April 30, 1985

790. THE BIVALVE FAUNA FROM THE MIYANOHARA FORMATION(LOWER CENOMANIAN) OF SAKAWA AREA, SHIKOKU*TOMOKO MATSUDA
Doshimaru 2·12·232, Wakamatsu-ku, Kitakyushu, 808

Abstract. This paper deals mainly with the description of the bivalve species
from the upper part of the Miyanohara Formation (Lower Cenomanian) of the
Sakawa area, Shikoku. They are 19 species of 15 genera, including 4 new species.
The occurrence of several trigoniids, Pterotrigonia (?Scabrotrigonia) pustu/osa, P.
(Ptilotrigonia) mifunensis and P. (Ptil.) amakusensis already described by Tashiro
and Matsuda (1983b) suggests that the fauna is referable to the upper Lower
Cenomanian. This conforms well with the previous age determination (K4a2) byammonites (Matsumoto, 1977). This bivalve fauna is closely similar to that of the
S-IV Formation (Tashiro and Matsuda, 1983a) of the Goshonoura Group in Shishijima island of Kyushu, that of the Middle part of the Nagase Formation (Tashiro
et aI., 1982) of Shikoku, and that of the Misakubo Formation of the Akaishi
Mountains.

tigraphical implications, including the correlation of the Miyanohara Formation with the
Cenomanian strata of Kyushu, Akaishi and
Hokkaido.
Repository :-The following abbreviations areused for the indication of the institutions where
the described specimens are kept.
KSG: Department of Geology, Faculty of
Science, Kochi University, Kochi
HPC: Hirata's Palaeontological Collections in
the Makino Botanical Garden, Godaisan of Kochi
Before going further, I wish to express mysincere thanks to Prof. Masayuki Tashiro of
Kochi University, for his continuous encouragement, valuable suggestions and kind supply of
the specimens from Hokkaido and Kyushu andto Prof. Emeritus Tatsuro Matsumoto of Kyushu
Univ., for his reading of the draft with instructive
suggestions. Thanks are also due to Dr. Itaru
Hayami of the Univ. of Tokyo, for his kindadvice, to Prof. Jiro Katto of Kochi Univ., for

Introduction
The Upper Cretaceous Miyanohara Formationis very narrowly distributed in the neighbourhood of Miyanohara (Sakawa district) in Shikoku(Text-fig. 1). This formation is composed of thelower part and the upper part in the latter ofwhich the described fossils occur. Several molluscan fossil localities are probably of the same
horizon. The specimens were mainly collected
at the easternmost locality (Text-fig. 1) where
those of Hirata's and Katto's collection werealso obtained. Al though - several bivalve fossils
from the Miyanohara Formation were describedby Amano (1956), more numerous bivalve
specimens have recently been collected fromthe upper part of the formation. In the present
paper I describe 19 species of 15 genera, including 4 new species, and discuss their biostra*Received November 28, 1983; read October
24,1982 in Tsu City.
1

Tomoko MATSUDA

2

"

OCHI

A

",

o----500m

KYUSHUText-fig. 1. Map showing the fossil localities of the Miyanohara Formation at Miyanohara in
Sakawa.
U: Upper member of the Miyanohara Formation; L: Lower member of the Miyanohara Formation;
A: Alluvium.
Below is the index map showing also relevant localities.
S: Shishijima island; G: Goshonoura island; N: Nagase.
his supply of some specimens from the Miyanohara Formation, to the staff of the Hirata's
Palaeontological Collections in the Makino
Botanical Garden, Godaisan of Kochi, for theinspection of several specimens which werecollected by the late Mr. Motome Hirata from
the Miyanohara and Nagase Formations.
Systematic description
Class Bivalvia
Subclass Palaeotaxodonta
Order Nuculoida

Superfamily Nuculacea Gray
Family Nuculidae Gray
Genus Nucula Lamarck, 1799
Subgenus Pectinucula Quenstedt, 1930

Nucula (Pectinucula) kochiensis
Tashiro et Matsuda
Plate 1, Figs. 1-8
1956. Nucula sp.; Amano, Kumamoto Jour.
Sci., sec. 1, (geol.), vol. 1, no. 1, p. 64,
pI. 1, fig. 9.
1982. Nucula (Pectinucula) kochiensis Tashiro
et Matsuda; Trans. Proc. Palaeont. Soc.

790. Bivalve Fauna from Miyanohara Formation
Japan, n.s., no. 127, p. 396, pI. 62, figs.
7,11-15, text-fig. 3.

Material:-KSG 3361, external mould of rightvalve; KSG 3360 and KSG 3362-KSG 3364,
internal mould of right and left valves; they arecollected from Miyanohara of Sakawa. Anotherspecimen, KSG 3365, external mould of rightvalve, from Yunokuchi at Shishijima.
Measurements (in mm):Specimen
KSG 3360 R. in. mould
KSG 3361 R. ex. mould
KSG 3362 L. in. mould
KSG 3363 R. in. mould
KSG 3364 L. in. mould
KSG 3365 R. ex. mould

Length Height Thickness
15.0
11.5
13.5
11.0
3.0
13.5
9.0
14.0
10.5
14.5
13.0
18.5
15.0
5.5

Remarks:-These specimens are undoubtedly
identified with Nucula (Pectinucula) kochiensis
Tashiro et Matsuda (1982), from the Fukigoshi
Formation of the Monobe area in Shikoku, judging from the radial ribs on the disk, trigonal
outline and features of the hinge structure. As
to Nucula sp. from the Miyanohara Formation
Amano (1956) did not describe the ornamentation on the disk, but it is probably identical withthis species in view of the hinge structure andshell outline.
Occurrence:-Medium- and fine-grained sandstone of the Miyanohara Formation at Miyanohara in Sakawa area. This species is known fromthe siltstone of the S-I and S-II1 Formationsof the Goshonoura Group at Hegushi and Yunokuchi of Shishijima.

Superfamily Nuculanacea Adams et Adams
Family Nuculanidae Adams et Adams
Genus Portlandia Morch, 1857
Portlandia (s. 1.) nagaseana Tashiro et Matsuda

Plate 1, Figs. 9, 10
1982. Portlandia (s. 1.) nagaseana Tashiro et
Matsuda; Trans. Proc. Palaeont. Soc.
Japan, n.s., no. 127, p. 399, pI. 62,
figs. 23-25, text-fig. 5.

Material:-KSG 3366 and KSG :3'367, internal

3moulds of left valves, from Miyanohara of
Sakawa.
Measurements (in mm):Specimen
KSG 3366 L. in. mould
KSG 3367 L. in. mould

Length Height
16.0
11.0
18.0
11.5

Remarks:-These specimens are referable toPortlandia (s. 1.) nagaseana Tashiro et Matsuda(1982), from the Fukigoshi Formation in Shikoku by the same features of the outline andhinge structure.
Occurrence:-Rarely found in medium-grainedsandstone of the Miyanohara Formation at
Miyanohara, Sakawa.

Subclass Pteriomorphia
Order Arcoida
Superfamily Arcacea Lamarck
Family Cucullaeidae Stewart
Genus Cucullaea Lamarck, 1801
Subgenus Idonearca Conrad, 1862
Cucullaea (Idonearca) ezoensis ezoensis
Yabe et Nagao
Plate 2, Figs. 11-16

1928. Cucullaea ezoensis Yabe et Nagao, Sci.
Rept. Tohoku Imp. Univ., ser. 2, vol. 9,
no. 3, p. 81, pI. 16, figs. 1-3.
1956. Cucullaea ezoensis var. amaxensis Matsumoto; Amano, Kumamoto Jour. Sci.,
sec. 1, (geol.), vol. 1, no. 1, p. 6.
1956. Cucullaea sp.; Amano, Ibid. vol. 1, no. 1,
p.68.
1975. Cucullaea (Idonearca) ezoensis ezoensis
Yabe et Nagao; Hayami, Univ. Mus.
Univ. Tokyo, Bull., no. 10, p. 31.
1982. Cucullaea (Idonearca) ezoensis ezoensis
Yabe et Nagao; Tashiro and Kozai,
Palaeont. Soc. Japan, Sp. Pap. no. 25,
p. 73, pI. 14, fig. 3.

Material:-KSG 3368 - KSG 3370, internalmoulds of the right valves, from Miyanohara,
Sakawa. KSG 3371, external mould of the rightvalve, from Kashiwaguri of Shishijima island.

Tomoko MATSUDA

4

Measurements (in mm):Specimen
KSG 3368 R. in. mould
KSG 3369 R. in. mould
KSG 3370 R. in. mould
KSG 3371 R. ex. mould

Length
38.0
32.0
18.0
18.5

Heightca 35.0ca 28.0
12.5
16.5

Thickness

8.0

Remarks:-Many specimens from the Goshonoura Group of the Shishijima island and theMiyanohara Formation are before me. They arecharacterized by the subquadrate outline, andtheir postero-ventral comer are not much projected towards posterior. Although the specimensfrom the Goshonoura Group of the Shishijima
island were identified with Cueullaea ezoensis
var. amaxensis Matsumoto by Amano (1956),
they are safely identified with Cueullaea (Idonearea) ezoensis ezoensis Yabe et Nagao, from
the Middle Yezo Group in Hokkaido, because of
their less projected postero-ventral comer. Likewise, the specimens from the Miyanohara Formation are undoubtedly identified with the same
subspecies.
Oeeurrenee:-Rare in the medium-grainedsandstone of the Miyanohara Formation at
Miyanohara, Shikoku, and the siltstone of the
S-I Formation at Hegushi of the Shishijima
island; also rare in fine-grained sandstone of the
S-V Formation of the Goshonoura Group at
Yunokuchi of the Shishijima island; common
in the medium-grained sandstone of the S-IV
Formation at Hegushi; abundant in the mediumgrained sandstone of the S-III Formation of the
Goshonoura Group at Kashiwaguri of the Shishijim a island.

Family Arcidae Lamarck
Genus Area Linne, 1758
Subgenus Eonavieula Arkell, 1929
Area (Eonavieula) tashiroi sp. nov.
Plate 2, Figs. 1-10; Text-fig. 2

1982. Area

(Eonavieula) sp.; Tashiro andTrans. Proe. Palaeont. Soc.
Japan, n.s., no. 127, p. 402, pI. 64, fig.
Matsuda,22.

O~_ _ _ _---,10MM

Text-fig. 2.

Area (Eonavieula) tashiroi sp.

nov.
A diagramatic sketch of the holotype. (T. Matsuda delin.)

Material:-Holotype, KSG 3372, externalmould of right valve, from Enokuchi of Goshonoura island; paratypes, KSG 3374 and KSG
3375, external and internal moulds, from Miyanohara of Sakawa; the other para types, KSG
3373, KSG 3376 and KSG 3377, external andinternal moulds from Kashigaguri of Shishijima
and Enokuchi of Goshonoura.
Diagnosis:-Shell medium to large for the
genus, elongately subquadrate, longer than high,very inflated; umbo prominent, orthogyrous,
located at about one third from front of thevalve; anterior margin a little convex, subverticalto the dorsal margin; ventral margin horizontal,
nearly straight but slightly concave at the middle
part; posterior margin nearly straight, obliquely
truncated; dorsal margin nearly straight; ashallow radial sulcus extends from the umbo tocenter of the ventral margin; posterior carinal
ridge not angulated but well elevated, especiallynear the umbo; dorsal carinal ridge weakly
elevated; hinge line straight with about 40
small diverging teeth; ligament area wide, triangular, provided with five or more chevronshaped ligament grooves; disk ornamented with
abundant fine radial ribs and numerous laminated concentric ribs; median part of the disknear the radial sulcus somewhat reticulated by
two sorts of the ribs; posterior area ornamented
with two sorts of the ribs as like as the disk;
the concentric ribs are usually waved near the790. Bivalve Fauna from Miyanohara Formation

posterior margin; inner margin smooth; bothlateral adductor scars weakly impressed.
Measurements (in mm):Specimen
KSG 3372 R. ex. mould
KSG 3373 R. in. mould
KSG 3374 R. ex. mould
KSG 3375 L. in. mould
KSG 3376 R. ex. mould
KSG 3377 L. in. mould

Length
30.0
27.5
21.5
24.0
28.5
15.5

5

Family Glycymerididae Newton
Genus Glyeymeris da Costa, 1778
Subgenus Hanaia Hayami, 1965

Height
12.5
14.0
9.0
12.5
15.0
ca 7.0Thickness
5.5
5.5
7.0

Observation:-This species is very variable in
the outline and the strength of the concentricribs. In mature specimens the concentric laminae
are more strongly marked than in the younger
specimens, and the secondary radial ribs frequently appear on the ventral part of the disk.
Comparison:-This species is discriminatedfrom Area (Eonavieula) prolata Amano (1957),
from the Hagino Formation in Shikoku by themore numerous radial ribs and strongly laminated concentric ribs. Area (Eonavieula) shinanoensis Yabe et Nagao (in Yabe, Nagao and Shimizu, 1926), from the Shiroi Formation in Central
Japan, is distinguishable from this species in its
less inflated and smaller valve. This species resembles Area sanetae-erucis Pictet et Campiche,
from the Lower Greensand of England (Woods,
1899), in the numerous laminated concentricribs on the surface, but differs in its distinct
chevron-shaped ligament grooves and less rounded anterior margin. Area earteroni d'Orbigny,from the Lower Greensand of England (Woods,
1899), is similar to this species in its numerous
laminated concentric ribs on the surface andseveral ligament chevrons, but differs in its
more elongated outline.
Oeeurrenee:-Medium- to fine-grained sandstone of the Miyanohara Formation at Miyanohara, Sakawa; siltstone of the Fukigoshi Formation of Odochi, Monobe area (see, Tashiro andMatsuda, 1982); siltstone of the S-I Formation
at Hegushi of Shishijima island. Fine-grainedsandstone of the S-IV Formation at Kashiwaguri of the same island; medium-grained sandstone of the lIb Formation (Matsumoto, 1938),of the Goshonoura Group at Enokuchi of Goshonoura.

Glyeymeris (Hanaia) goshonouraensis
Matsukuma
Plate 1, Figs. 11-15

1930. Glycymeris amakusensis var. solida Nagao;
Jour. Fac. Sci. Hokkaido Imp. Univ.,
ser. 4, vol. 1, no. 1, p. 16, pI. 3, figs. 13,
14.
1956. Glyceymeris aff. amakusensis Nagao;
Amano, Kumamoto Jour. Sci. ser. 1,(geol.), vol. 1, no. 1, p. 68, pI. 1, figs.

22-25.
1956. Glycymeris sp.; Amano, Ibid., vol. 1,
no. 1,p. 70.
1971. Glycymeris(Hanaia) solida Nagao;
Tashiro, Trans. Proc. Palaeont. Soc. Japan,
n.s., no. 84, p. 233, text-fig. 5, pI. 28,
figs. 1-8.
1975. Glycymeris (Glyeymerita) solida Nagao;
Hayami, Univ. Mus. Univ. Tokyo Bull.,no. 10, p. 34.
1979. Glycymeris goshonouraensis Matsukuma,
Venus (Jap. Jour. Malac.), vol. 38, no. 2,
p.98.

Materiai:-KSG 3379, internal mould of left
valve, and KSG 3380, left valve, both from
Miyanohara of Sakawa; KSG 3378, KSG 3381
and KSG 3382, internal and external moulds,
from Hegushi, Shishijima island.
Measurements (in mm):Specimen
KSG 3378 R. ex. mould
KSG 3379 L. in. mould
KSG 3380 L. valve
KSG 3381 R. in. mould
KSG 3382 R. in. mould

Length
24.0
11.0
16.5
22.5
ca 20.0

Height
23.0
9.5
15.0
ca 16.0ca 19.0

Thickness
9.5
6.0

Remarks:-Several specimens have been obtained from the Miyanohara Formation. On theother hand, many specimens occur from the
S-IV Formation of the Goshonoura Group of
the Shishijima island. They are characterized by
its asymmetrical hinge structure in the immature
stage, inflated valve, round-topped radial ribs on
the surface and fine radial ridges on the internal

Tomoko MATSUDA

6

surface. In these characters they are identified
with Glycymeris (Hanaia) solida Nagao (Tashiro,1971) from the Goshonoura Group of the
Goshonoura island.
Occurrence:-Rate in the medium- to finegrained sandstone of the Miyanohara Formation,
at Miyanohara, Sakawa; abundant in the finegrained sandstone of the S-IV Formation of the
Goshonoura Group at Hegushi of Shishijima
island; common in the fine-grained sandstone of
the S-I Formation of the Goshonoura Group at
Yunokuchi of the same island.

the Mifune Group of Central Kyushu.
Occurrence:-Common in hte medium- tocoarse-grained sandstone of the Miyanohara
Formation at Miyanohara, Sakawa.
Order Trigonioida
Superfamily Trigoniacea Lamarck
Family Trigoniidae Lamarck
Subfamily Pterotrigoniinae van Hoepen
Genus Pterotrigonia van Hoepen, 1929
Subgenus Scabrotrigonia Dietrich, 1933

Order Pterioida
Suborder Ostreina Ferussac
Superfamily Ostreacea Fafinesque
Family Ostreidae Rafinesque
Subfamily Ostreinae RafinesqueGenus Crassostrea Sacco, 1897
Crassostrea kawauchidensis Tamura

Plate 2, Fig. 18
1938. Ostrea sp. (sp. nov.); Matsumoto, Jour.
Geol. Soc. Japan, vol. 45, no. 532, p. 13,
text-figs. 1, 2.
1977. Crassostrea kawauchidensisTamura;Mem.
Fac. Educ. Kumamoto Univ., no. 26, nat.
sci., p. 114, pI. 2, figs. 1-5.
1982. Crassostrea aff. C. kawauchidensis Tamura; Tashiro and Kozai, Palaeont. Soc.
Japan, Sp. Pap. no. 25, p. 78.
1982. Crassostrea
kawauchidensis
Tamura;Tashiro and Matsuda, Trans. Proc. Palaeonto Soc. Japan, n.s., no. 127, p. 405, pI.
63, figs. 8,9,11.
Material:-KSG 3387, internal mould of theleft valve, from Miyanohara of Sakawa.
Remarks:-Although some specimens occur
from the Miyanohara Foramtion, they areimperfect or fragmentary. KSG 3387 is measured
34.0 mm in length and 55.0 mm or more inheight. This is characterized by its tall andinflated valve, and thick test. These specimens
are probably referable to Crassostrea kawauchidensis Tamura (1977), originally described from

Pterotrigonia (?Scabrotrigonia) pustulosa(Nagao)Synonymy, Material, Description and Occurrence:-See Tashiro and Matsuda, 1983b, pp.
25-27.

Subgenus Ptilotrigonia van Hoepen, 1929
Pterotrigonia (Ptilotrigonia) mifunensis(Tamura et Tashiro)
Synonymy, Material, Description and Occurrence:-See Tashiro and Matsuda, 1983b, pp.
42-45.
Pterotrigonia (Ptilotrigonia) amakusensis
Tashiro et Matsuda
Synonymy, Material, Description and Occurrence:-See Tashiro and Matsuda, 1983b, pp.
41-42.
Pterotirigonia (Ptilotrigonia) miyanoharensis
Tashiro et Matsuda
Material, Description and Occurrence:-See
Tashiro and Matsuda, 1983b, pp. 45, 46.

Subclass Heterodonta
Order Veneroida
Superfamily Lucinacea Fleming
Family Lucinidae Fleming
Subfamily Myrteinae Chavan

790. Bivalve Fauna from Miyanohara Formation

Genus Myrtea Turton, 1822
Su bgenus Myrtea Turton, 1822
Myrtea (Myrtea) amanoi sp. nov.
Plate 1, Figs. 16-21; Text-fig. 31956. Lucina (?) sp.; Amano, Kumamoto
Jour. Sci., sec. 1, (geol.), vol. 1, p. 77,
text-fig. 2.
1982. Myrtea (Myrtea) sp.; Tashiro and Matsuda, Trans. Proc. Palaeont. Soc. Japan,
n.s., no. 127, p. 408, pI. 65, fig. 23.

Material:-Holotype, KSG 3389, right valve,from the Fukigoshi Fonnation at Odochi of
Monobe area (see Tashiro and Matsuda, 1982);
paratype, KSG 3390, internal mould, from thesame locality of the holotype; KSG 3391 andKSG 3392, external moulds, from Miyanohara,
Sakawa; KSG 3393, external mould, from
Enokuchi, Goshonoura island.
Diagnosis:-Shell small, subovate in outline,
slightly longer than high, weakly inflated; umbo
small, located at a little posterior than midlength of the valve; anterior dorsal margin

7

oblong, nearly straight but weakly concave
near the umbo; posterior dorsal margin slightly
convex; anterior margin weakly arched, truncated, fonning an angle of about 1200 with thedorsal margin; ventral margin broadly arched;
posterior margin nearly straight or slightly
convex, vertically truncated from the dorsal
margin; apical angle about 1200 ; lunule narrow,elongated, distinctly separated from the disk bya narrowly angulated ridge, nearly smooth onlywith growth lines; escutcheon depressed very
narrow, smooth; the concentric ribs on thesurface roof-shaped, regularly spaced in general,narrower than their flat interspaces; posteriorcarina weakly extended from the umbo to thepostero-ventral comer; hinge plate long; hinge
fonnula is as follows:AlII 3a 3b/AIV All 24b
2 subvertical or slightly oblique; 3a small nearlyvertical; 3b strong, obliquely extended towards
postero-ventral comer; 4b large, elongated,strongly oblique; lateral teeth elongated; anterior adductor scar oblong, weakly impressed;
posterior adductor scar small; fine and numerous
radial striae appear on the internal surface;
inner margin smooth.
Measurements (in mm):Specimen
KSG 3389 R. ex. mould
KSG 3390 R. in. mould
KSG 3391 L. ex. mould
KSG 3392 R. ex. mould
KSG 3393 R. ex. mould

O;...._ _ _...5MM

Text-fig. 3.

Myrtea (Myrtea) ama-

noi sp. nov.
A diagramatic sketch of the holotype. (T.
Matsuda delin.)

Length
17.0
12.5
17.5
18.5
14.5

Height
16.0
11.5
15.0
17.0
13.5

Thickness
2.0
3.5
3.5
3.0

Observation:-The concentric ribs number
about 40, being more closely spaced near theumbo than on the ventral part in the adult specimens. Fine but distinct growth lines are discernible on the interspace of the ribs on theventral part of the disk.
Comparison:-This species is discriminatedfrom Myrtea (s. 1.) angularis Tashiro (1976),
from the Himenoura Group in Kyushu, in its
rounded outline and less numerous concentricribs on the disk. This species differs from Myrtea
ezoensis (Nagao) (1938), from the Upper Ezo
Group of Hokkaido, in its rounded outline andTomoko MATSUDA

8

numerous concentric ribs. This species resembles
Caullucina esbedensis Freneix (1976), from theHassi Oum-Esbed of France, in the subovate
outline, but differs in its small size and posterior
location of the umbo. Lucina mattiformis
Steph~nson (1941), from the Nacatoch Sandof U.S.A., is discriminated from this species,
by its rounded outline and angulated posteriorcarina.
Occurrence:-Siltstone of the Fukigoshi Formation in Monobe area (see Tashiro and Matsuda, 1982): medium- to fine-grained sandstone of
the Miyanohara Formation at Miyanohara of
Sakawa.

thick, was collected from the Miyanohara Formation. Although its hinge structure is not clear,other features are very well preserved. It is
certainly referable to Thetis japonica (Yabe et
Nagao), because of its well inflated valve, rounded outline and smooth surface except for fine
growth line.
Occurrence:-Very rare at the medium-grainedsandstone of the Miyanohara Formation of
Sakawa.

Family Mactromyidae Cox

Genus Pachythaerus Conrad, 1869

Genus Thetis Sowerby, 1826

Pachythaerus nagaoi (Matsumoto)

Thetis japonica (Yabe et Nagao)

Plate 1, Figs. 22-24

Plate 2, Fig. 17

1938. Crassatella (Pachythaerus) nagaoi Matsumoto, Jour. Geol. Soc. Japan, vol. 45, no.

1927. Thetironia affinis (Whiteaves) var. japonica Yabe et Nagao; in Yabe, Nagao andShimizu, Sci. Rep. Tohoku Imp. Univ.,

1928.

1975.

1976.

1981.

1982.

ser. 2, vol. 11, no. 1, pI. 5, figs. 7a-b.
(without description)
Thetironia affinis (Whiteaves) var. japo·
nica Yabe et Nagao; Yabe and Nagao,
Ibid., vol. 9, no. 3, p. 89, pI. 17, figs. 14a,
14b and 15a.
Thetis japonica (Yabe et Nagao); Hayami,
Univ. Mus. Univ. Tokyo, Bull., no. 10, p.
122.
Thetis affinis japonica (Yabe et Nagao);
Tamura and Tashiro, Atlas of JapaneseFossils, no. 43-258, pI. Cr.-24, figs. 17,
18.
Thetis japonica (Yabe et Nagao);Hayami
and Kase, Trans. Proc. Palaeont. Soc.
Japan, n.s., no. 121, pp. 37, 38, pI. 5,
figs. 2-4.
Thetis sp. aff. T. japonica (Yabe et
Nagao); Tashiro and Matsuda, Ibid.,
no. 127, p. 409, pI. 65, figs. 20-22.

Material:-KSG 3388, external mould of left
valve, from Miyanohara of Sakawa.
Remarks:-A single specimen, (KSG 3388),
27.5 mm long, 25.0 mm height and 11.5 mm

Superfamily Crassatellacea Ferussac
Family Crassatellidae Ferussac
Subfamily Crassatellinae Ferussac

532, p. 16, text-figs. 10, 11.

1956. Crassatellites nagaoi Matsumoto; Amano,
Kumamoto Jour. Sci., sec. 1, (geol.), vol.
1, no. 1, pp. 74, 75, pI. 1, figs. 16-20.

1975. Pachythaerus nagaoi (Matsumoto); Hayami, Univ. Mus. Univ. Tokyo, Bull., no.
10, p. 130.

Material:-KSG 3395 and KSG 3396, internaland external moulds, from Kashiwaguri of
Shishijima Island; KSG 3394, internal mould ofimperfect right valve, from Miyanohara of
Sakawa.
Measurements (in mm):Specimen
KSG 3394 R. in. mould
KSG 3395 R. in. mould
KSG 3396 R. ex. mould

Length
32.0
24.5
10.5

Heightca 25.0
20.0
9.5

Thickness

3.0

Remarks:-Although a specimen, KSG 3394,
from the Miyanohara Formation is an imperfectinternal mould, it is referable to Pachythaerus
nagaoi (Matsumoto), from the Goshonoura
Group of Central Kyushu, by its characteristic
hinge structure. The specimens from the Shishijima island are also referable to this species as790. Bivalve Fauna from Miyanohara Formation

already discussed by Amano (1956).
Occurrence:-Very rare in the medium grainedsandstone of the Miyanohara Formation at
Miyanohara, Sakawa; rate at the fine-grainedsandstone of the S-III and S-V Formations at
Hegushi and Yunokuchi of the Shishijima island;
abundant in the fine-grained sandstone of the
S-IV Formation at Kashiwaguri of the sameisland.
Genus Anthonya Gabb, 1864
Anthonya apicalis Nagao
Plate 1, Figs. 25-31

1938. Anthonya apicalis Nagao, Jour. Fac. Sci.
Hokkaido Imp. Univ., sec. 4, vol. 4, no.
1-2, p. 75, pI. 2, figs. 6-12.
1956. Anthonya apicalis shishijimensis Amano,
Kumamoto Jour. Sci., sec. 1, (geol.), vol.
1, no. 1, p. 76, pI. 2, figs. 6-12.
1972. Anthonya apicalis Nagao; Tamura andPackard, Mem. Fac. Educ. Kumamoto
Univ., vol. 20, no. 1, p. 27.
1972. Anthonya apicalis shishijimensis Amano;
Tamura and Packard, Ibid., vol. 20, no. 1,
p.27.
1975. Anthonya apicalis Nagao; Hayami, Univ.
Mus. Univ. Tokyo, Bull., no. 10, p. 131.
1975. Anthonya apicalis shishijimensis Amano;
Hayami, Ibid., no. 10, p. 131.
1981. Anthonya sp. cf. A. apicalis Nagao;
Hayami and Kase, Trans. Proc. Palaeont.
Soc. Japan, n.s., no. 121, p. 38, pI. 4, fig.
17.

Material:-KSG 3397 - KSG 3400, internaland external moulds, from Miyanohara, Sakawa;
KSG 3401 and KSG 3402, external moulds, from
Kashiwaguri and Yunokuchi of Shishijima island;
KSG 3403, internal mould, from Katsurazawa,
Mikasa.
Measurements (in mm):Specimen
KSG 3397 L. ex. mould
KSG 3398 L. ex. mould
KSG 3399 L. in. mould
KSG 3400 R. ex. mould
KSG 3401 L. ex. mould
KSG 3402 R. ex. mould
KSG 3403 L. in. mould

Length
30.0
27.5
23.0
42.0
21.0
23.5
33.0

Height
11.5
10.0
12.5
22.5
9.0
8.5
11.5

9

Remarks:-Amano (1956) distinguished thespecimens from Shishijima island and Miyanohara from Anthonya apicalis Nagao (1938) from
Hokkaido, as a subspecies, Anthonya apicalis
shishijimensis. It was said by him that the shell is
not so rapidly tapering in its posterior part, notso concave at the dorsal margin, and the anterior
margin is more produced. As far as I have observed, several specimens in my hand from theMiyanohara Formation are tapering in theposterior part like the specimens of A. apicalis
from Hokkaido (Nagao, 1938). Although thedorsal margin is nearly straight in the immature
specimens from Miyanohara and Shishijima, it
is usually concave in the adult specimens. Hayami (in Hayami and Kase, 1981) has noted thatthe specimens of A. apicalis from the sea bottom
off the coast of Kuji have not so prominent
umbo and not so regularly spaced ribs on thesurface as those from Miyanohara and Shishijima.
The adult specimens from the Miyanohara are,however, identical with A. apicalis apicalis in its
surface ornamentation and the shape of umbo.
To sum up, I am inclined to deny the subspecificdistinction within A. apicalis between the forms
from Hokkaido and Southwest Japan.
Occurrence:---Common in the medium-grainedsandstone of the Miyanohara Formation at Miyanohara, Sakawa; rare at the fine-grained sandstone and siltstone of the S-IV and S-III Formations at Hegushi and Yunokuchi of Shishijima.

Superfamily Veneracea Rafinesque
Family Veneridae Rafinesque
Subfamily Pitarinae Stewart
Genus Goshoraia Tamura, 1977
Goshoraia crenulata (Matsumoto)
Plate 3, Figs. 1-3

1938. "Callista" (Pseudamiantis) crenulatus Matsumoto, Jour. Geol. Soc. Japan, vol. 45,
no. 532, p. 19, text-figs. 12, 13, pI. 1, fig.

5.
1956. Pseudamiantis crenulatus (Matsumoto);
Amano, Kumamoto Jour. Sci., ser. B, sec.
1, vol. 2, no. 1, p. 78, pI. 1, fig. 26, pI. 2,
figs. 13-19.

Tomoko MATSUDA

10

1963. "Callista" (Pseudamiantis) crenulatus Matsumoto; Iwasaki, Trans. Proc. Palaeont.
Soc. Japan, n.s., no. 51, p. 94, pI. 15, figs.
4-7.
1975. Pseudamiantis? crenulata (Matsumoto);
Hayami. Univ. Mus. Univ. Tokyo, Bull.,no. 10,p. 144.
(Matsumoto );crenulata
1977. Goshoraia
Tamura, Mem. Fac. Educ. Kumamoto
Univ., no. 26, pp. 139-140, text-fig. 14,
pI. 9, figs. 9-16.
1981. Goshoraia crenulata (Matsumoto); Hayami and Kase, Trans. Proc. Palaeont. Soc.
Japan, n.s., no. 121, pp. 39-40, pI. 5.
1982. Goshoraia crenulata (Matsumoto); Tashiro and Matsuda, Ibid., no. 127, pp. 410411, pI. 65, figs. 12, 13.

Material:-KSG 3404 and KSG 3405, external
and internal moulds, from Miyanohara, Sakawa; .
KSG 3406, internal mould, from Hegushi of the
Shishijima island.
Measurements (in mm):Specimen
KSG 3404 R. ex. mould
KSG 3405 R. in. mould
KSG 3406 L. in. mould

Lengthca 35.0
31.5

Height
26.5
25.0
15.5

Thickness
6.5

Remarks:-These specimens are undoubtedly
conspecific with Goshoraia crenulata (Matsumoto), from the Goshonoura Group in Kyushu(Matsumoto, 1938; Tamura, 1977), because of
its fine subinternal radial ribs and numerous
irregular concentric striae on the disk, prominentand prosogyrate umbo, subovate outline, finely
crenulated inner margin and the same featuresof the hinge structure.
Occurrence:-Common in the medium-grained
sadstone of the Miyanohara Formation at Miyanohara, Sakawa; common in the medium-grainedsandstone of the S-I1I Formation of the Goshonoura Group at Kashiwaguri of the Shishijima
island; common in the fine-grained sandstone of
the S-IV and S-V Formation of the same Groupat Hegushi and Yunokuchi of the same island;common in the siltstone of the S-I Formation of
the same group at Hegushi and Katasoba of thesame island.

Subfamily Tapetinae Adams et Adams
Genus Legumen Conrad, 1858

?Legumen sp.
Plate 3, Fig. 7
Compare:1982. ?Legumen sp.; Tashiro and Matsuda,
Trans. Proc. Palaeont. Soc. Japan, n.s.,
no. 127, p. 411, pI. 65, figs. 8-10.

Material:-KSG 3407, left internal mould,
from Miyanohara.
Remarks:-A specimen, KSG 3407, is measured 15.0 mm in length and 9.5 mm in height.
This is similar to ?Legumen sp. (Tashiro and Matsuda, 1982) from the Fukigoshi Formation in
Shikoku, in having the same features of the outline and hinge structure.
Occurrence:-Very rare in the fine-grainedsandstone of the Miyanohara Formation at
Miyanohara of Sakawa.
Subclass Anomalodesmata Dall
Order Pholadomyoida Newell
Superfamily Pholadomyacea Gray
Family Pholadomyidae Gray
Genus Pholadomya Sowerby, 1823
Subgenus Pholadomya Sowerby, 1823

Pholadomya (Pholadomya) japonica Amano
Plate 3, Figs. 4-6
1956. Pholadomya japonica Amano, Kumamoto Jour. Sci., sec. 1, (geol.), vol. 1, no.
1, p. 80, pI. 2, figs. 1-5.
1975. Pholadomya (Pholadomya) japonica Amano; Hayami, Univ. Mus. Univ. Tokyo,
Bull., no. 10, p. 148.

Materiul:-KSG 3408, conjoined valves, from
Miyanohara; KSG 3409, imperfect, conjoined
valves, from Yunokuchi of the Shishijima island.
Measurements (in mm):Specimen
KSG 3408 valve
KSG 3409 valve

Length45.0
30.0

Height24.5
31.5

Thickness
13.5
9.0

790. Bivalve Fauna from Miyanohara Formation
Remarks:-This species was established by
Amano (1956) on the specimen from the Miya.
nohara Formation. The outline of this species isvariable from subquadrate to subovate.
Occurrence:-Rare in the medium·grainedsandstone of the Miyanohara Formation at
Miyanohara of Sakawa; very rare in the fine·grained sandstone of the S· V Formation of
the Goshonoura Group at Yunokuchi of the
Shishijima island.
Subgenus Bucardiomya Roilier, 1912

Pholadomya (Bucardiomya) hiratai sp. nov.
Plate 3, Figs. 8-13; Text·fig. 4

Material:-Holotype, KSG 3383, externalmould of right valve, from Miyanohara of Saka·wa; paratypes, KSG 3384 and KSG 3385, ex·
ternal moulds of right valves, from the same11

locality; another paratype, HPC 8517, externalmould of right valve, from Nagase, Monobe
area.
Diagnosis:-Shell medium in size, subtrape·
zoidal or subtriangular in outline, strongly ex·panded; umbo prominent, located at about two
fifths from front of the valve; anterior margin
nearly straight, obliquely truncated, forming anangle of about 120 0 with ventral margin; ventral
margin broadly arched; posterior margin narrow·
ly rounded; posterior dorsal margin elongated,weakly concave near the umbo; disk ornamented
with about 20 strong concentric ribs on its
anterior half, and with distinct radial ribs on
its posterior half; the concentric ribs narrower
than their interspaces; the radial ribs loosely
spaced with about 10 on the posterior marginal
part, but closely spaced on the central part ofthe disk; posterior area broad, nearly smooth
without fine growth lines; lunular area smooth.
Measurements (in ,mm):-

KSG 3383
KSG 3384
KSG 3385
HPC 8517......;;.20MM

loO_ _ _ _Text·fig.4. Pholadomya (Bucardio·mya) hiratai sp. nov.
A diagramatic sketch from synthetic
reconstruction. (T. Matsuda delin.)

Specimen
R. ex. mould
R. ex. mould
R. ex. mould
R. ex. mould

Length37.0
27.0

Heightca 25.0
ca 21.0

25.0

ca 25.0

Thick·
ness
ca 9.0ca 10.0

Observation:---,The outline of the valve issomewhat variable. The concentric ribs are some·times weakened near the ventral margin.
Comparison:-This species resembles Pholado·mya (Bucardiomya) miyamotoi Nagao (1943),
from the Aptian Hiraiga Formation of North·east Japan, in its outline and radial ribs on thedisk, but differs in the absence of granulations
on radial ribs and stronger concentric ribs on the

Explanation of Plate 1
Nucula (Pectinucula) kochiensis Tashiro et Matsuda

Fig.1. Lateral view of right valve, gum cast of external mould (KSG 3365), x 1.2, loco Yuno·
kuchi of Shishijima, Kagoshima Prefecture.
Fig. 2. Lateral view of the same specimen, x 1.2.
Fig. 3. Dorsal view of the same specimen, x 1.2.
Fig. 4. Lateral view of left valve, plaster cast of internal mould (KSG 3364), x 1.2, loco Miyano·hara of Sakawa, Kochi Prefecture.
Fig. 5. Lateral view of right valve, plaster cast of internal mould (KSG 3360), x 1.2, loco ditto.

TomokoMATSUDA

12
Fig. 6.
Fig. 7.
Fig. 8.

Lateral view of right valve, plaster cast of external mould (KSG 3361), x 1.2, loco ditto.
Lateral view of left valve, plaster cast of internal mould (KSG 3362), x 1.2, loco ditto.
Lateral view of right valve, plaster cast of internal mould (KSG 3363), x 1.2, loco ditto.

Portlandia (s.l.) nagaseana Tashiro et Matsuda
Fig. 9. Lateral view of left valve, plaster cast of internal mould (KSG 3367), x 1.2, loco Miyanohara.
Fig. 10. Lateral view of left valve, plaster cast of internal mould (KSG 3366), x 1.2, loco ditto.
Glycymeris (Hanaia) goshonouraensis Matsukuma
Fig. 11. Internal view of left valve, gum cast of internal mould (KSG 3379), x 1.5, loco Miyanohara.
Fig. 12. Internal view of right valve, gum cast of internal mould (KSG 3382), x 1.2, loco Hegushi
of Shishijima.
Fig. 13. Lateral view of left valve, gum cast of external mould (KSG 3380), x 1.2, loco Miyanohara.
Fig. 14. Internal view of right valve, gum cast of internal mould (KSG 3381), x 1.5, loco Hegushi.
Fig. 15. Lateral view of right valve, gum cast of external mould (KSG 3378), x 1.2, loco Yunokuchi of Shishijima.
Myrtea (Myrtea) amanoi sp. nov.
Fig. 16. Lateral view of right valve, plaster cast of external mould (KSG 3392), x 1.2, loco Miyanohara.
Fig. 17. Internal view of right valve, gum cast of internal mould (KSG 3390), x 1.5, loco Fukigoshi of Monobe area, Kochi Prefecture.
Fig. 18. Lateral view of left valve, gum cast of external mould (KSG 3391), xl, loco Miyanohara.
Fig. 19. Lateral view of right valve, gum cast of external mould (KSG 3393), x 1.5, loco Enokuchi
of Goshonourajima, Kumamoto Prefecture.
Fig. 20. Lateral view of right valve, gum cast of external mould (KSG 3389), x 1.5, loco Fukigoshi.
Fig. 21. Lateral view of right internal mould (same specimen with KSG 3389), x 1.5.
Pachy thaerus nagaoi (Matsumoto)Fig. 22. Lateral view of right valve, gum cast of external mould (KSG 3396), x 1.7, loco Kashiwaguri, Shishijima.
Fig. 23. Internal view of right valve, gum cast of internal mould (KSG 3394), x 1, loco Miyanohara.
Fig. 24. Internal view of right valve, gum cast of internal mould (KSG 3395), x 1.2, loco Kashiwaguri of Shishijima.
Anthonya apicalis Nagao
Fig. 25. Lateral view of left valve, gum cast of external mould (KSG 3401), x 1.2, loco Kushizaki,
Shishijima.
Fig. 26. Lateral view of left valve, plaster cast of external mould (KSG 3398), x 1.2, loco Miyanohara.
Fig. 27. Internal view of imperfect left valve, gum cast of internal mould (KSG 3399), xl, loco
Miyanohara.
Fig. 28. Internal view of left valve, gum cast of internal mould (KSG 3403), x 1.2, loco Katsurazawa of Mikasa area, Hokkaido.
Fig. 29. Lateral view of right valve, gum cast of external mould (KSG 3402), x 1.2, loco Yunokuchi.
Fig. 30. Lateral view of left valve, gum cast of external mould (KSG 3397), x 1.2, loco Miyanohara, collected by Late Mr. Hirata.
Fig. 31. Lateral view of right valve, gum cast of external mould (KSG 3400), x 1.2, loco ditto.

Plate 1

MA TS UDA: Bivalve Fauna from Miy anohara Formation

5
1

7

11
.. .
~

......... ... . ..

2

13

12

3

16

17

20

15

18

19

22

23

27

10

790. Bivalve Fauna from Miyanohara Formation

disk. It is distinguished from P. (B.) subpedelnalis
Nagao (1943), from the Hiraiga Formation inthat the latter has a trigonal outline. It is similar
to P. decussata (Mantell), from the Chalk Marlof England (Woods, 1909), in its ornament on
the disk, but differs in its elongated outline.
Occurrence:-Very rare in the medium-grainedsandstone of the Miyanohara Formation at
Miyanohara of Sakawa area; rare in the mediumgrained sandstone of the Nagase Formation of
the Monobe area.
Superfamily Pandoracea Rafinesque
Family Laternulidae Hedley
Genus Periplomya Conrad, 1870
Periplomya japonica sp. nov.
Plate 3, Figs. 14·-17

Material:-Holotype, KSG 3410, conjoined
valves, from Hegushi of Shishijima; paratype,
KSG 3411, conjoined valves from the same
locality; the other paratypes, KSG 3412 andKSG 3413, external moulds of the left and rightvalves, from Miyanohara, Sakawa.
Diagnosis:-Shell medium in size, elongatedly
ovate, weakly inflated; test very thin; umbo alittle prominent, nearly orthgyrous, pointed
at a little posterior than mid-length of the valves;anterior dorsal margin oblique, nearly straight;
anterior and posterior margins well rounded;
ventral margin broadly arched; posterior dorsal
margin nearly straight and horizontal, apicalangle about 120°; surface with irregular growth
striae; two narrow inner buttresses extend
radially from the umbo to the venter, of which
the anterior one, observable subvertically under
the umbo, short with about a ninth of the valve
height; the other poste.rior one stronger andmore elongated than the anterior, extended
towards but not reaches the postero-ventral
corner.
Measurements (in mm):Specimen
KSG 3410 valve
KSG 3411 valve

Length41.0
32.5

Height25.0
24.5

Thickness
4.0
3.5

KSG 3412 R. ex. mould
KSG 3413 L. ex. mould

13
22.0
21.0

13.0
14.0

4.0
2.5

Observation:-The H/L ratio of this species isvariable from 0.75 to 0.59. The growth striae on
the surface are very fine but well marked.
Comparison:-"Periploma sp." from the Misakubo Formation of the Akaishi Mountaines(Matsushima and Kitamura, 1981) are probably
conspecific with this species in showing the samefeatures of the valve. This species is similar to
Periplomya grandis Ichikawa et Maeda (1958),
from the Izumi Group, in the outline, but differs
in its smaller valve and weaker and narrower
buttresses. It is discriminated from P. nagaoi
brevis Ichikawa et Maeda (1958), from the Izumi
Group, in that the latter has a more rounded
outline. It is similar to "Thracia" robinaldina?
(d'Orbigny), from the Lower Greensand of
England (Woods, 1909), in its elongated outline,
but is characterized by less inflated valve thanthat of "T." robinaldina?
Occurrence:-Common in the siltstone of the
S-I Formation of the Goshonoura Group at
Hegushi of Shishijima, and of the s-m Formation of the same group at Yunokuchi of thesame island; very rare in the medium grainedsandstone of the Miyanohara Formation at
Miyanohara of Sakawa.

Concluding remarks
According to a biostratigraphic study of theCretaceous pterotrigonians in Japan by Tashiro
and Matsuda (1983a), the geological age of thefossiliferous bed of the Miyanohara Formation
was determined .to be as upper Lower Cenomanian. This is supported by an ammonite,
Sharpeiceras sp., which suggests the substage
K4a2, Le. upper Lower Cenomanian (Matsumoto, 1977, fig. 3; Matsumoto et al., 1982, fig.
2).
The middle part of the Nagase Formation(Tashiro et aI., 1982), which is characterized by
the occurrence of Mantelliceras japonicum
Matsumoto, Muramoto et Takahashi, an indicator of the upper Lower Cenomanian (K4a2), isundoubtedly correlated with the fossiliferous

14

Tomoko MATSUDA

bed of the Miyanohara Fonnation. This isevidenced by the occurrence of some common
bivalve species, i.e., Pholadomya (Bucardiomya)
hiratai, Pterotrigonia ('lScabrotrigonia) pustulosa(B fonn) and Cucullaea (Idonearca) ezoensis
ezoensis.
The bivalve fauna of the Misakubo Fonnation (Matsushima and Kitamura, 1981) is closely
similar to this Miyanohara fauna, but Neitheasp., Linotrigonia sp. and P. ('lS.) monobeana
are unknown in the latter.
Many species of the Miyanohara fauna, i.e.,
Cucullaea (Idonearca) ezoensis ezoensis, Arca
(Eonavicula) tashiroi, Glycymeris (Hanaia) solida,
P. ('lS.) pustulosa, P. (Ptil.) mifunensis, Pachythaerus nagaoi, Anthonya apicalis and Goshoraia

crenulata are known from S-IV Fonnation(Tashiro and Matsuda, 1983a) of the Goshonoura Group in Shishijima. In my opinion, theMiyanohara fauna is safely correlated withthe fauna of the S-IV Fonnation.
It can be said that the Miyanohara fauna
represents an intervening substage between thefauna of the Members lIb and lIe or S-I Fonnation of the Goshonoura Group (Uppennost
Albian to lower Lower Cenomanian on theevidence of associated ammonites) and that of
the Lower Fonnation of the Mifune Group or
the upper part of the Nagase Fomlation (Middle
Cenomanian). It is devoid of P. (Ptil.) ogawai, P.
(Ptil.) dilapsa, P. ('lS.) pustulosa (A form),
Nipponitrigonia spp., Cucullaea (Idonearca)

Explanation of Plate 2
Area (Eonavieula) tashirui sp. nov.
Fig.1. Internal view of right valve, gum cast of internal mould (KSG 3373), x 2, loc. Enokuchi
of Goshonourajima, Kumamoto Prefecture.
Fig. 2. Dorsal view of the same specimen, x 1.8.
Fig. 3. Lateral view of right valve, gum cast of external mould (KSG 3372), x 1.5, loc. ditto.
Fig. 4. Internal view of left valve, gum cast of internal mould (KSG 3377), x 1.5, loc. Kashiwagrui of Shishijima, Kagoshima Prefecture.
Fig. 5. Lateral view of right valve, plaster cast of external mould (KSG 3374), x 1.2, loc. Miyanohara of Sakawa area, Kochi Prefecture.
Fig. 6. Lateral view of imperfect left valve, gum cast of esternal mould, x 1.5, loc. Enokuchi.
Fig. 7. Lateral view of imperfect right falve, gum cast of external mould, x 1.5, loc. ditto.
Fig. 8. Lateral view of right valve, gum cast of external mould (KSG 3376), x 1.5, loc. Kashiwaguri.
Fig. 9. Dorsal view of internal mould (KSG 3375), x 1.5, loc. Miyanohara.
Fig. 10. Lateral view of the same specimen, x 1.5.
Cueullaea (ldonearca) ezoensis ezoensis Yabe et Nagao
Fig. 11. Lateral view of right internal mould (KSG 3370), x 1.5, loco Miyanohara.
Fig. 12. Dorsal view of the same specimen, x 1.5.
Fig. 13. Internal view of right valve, gum cast of internal mould (KSG 3369), x 1, loc. ditto.
Fig. 14. Internal view ofright valve, gum cast of internal mould (KSG 3368), x 1, loco ditto.
Fig. 15. Lateral view of right valve, gum cast of external mould, x 1.2, loco ditto, collected by
Late Mr. Hirata.
Fig. 16. Lateral view of right valve, gum cast of external mould (KSG 3371), x 1.2, loco Kashiwaguri.
Thetisjaponica (Yabe et Nagao)
Fig. 17. Lateral view of left valve, plaster cast of external mould (KSG 3388), x 1, loco Miyanohara.
Crassostrea kawauchidensis Tamura
Fig. 18. Lateral view of left internal mould (KSG 3387), x 1.2, loc. ditto.

MA TSUDA: Bivalve Fauna from Miyanohara Formation

Plate 2

4

5

6
2
7

8

9

10

13

16

790. Billalve Fauna from Miyanohara Formation

15

Table 1. List of bivalves from the Miyanohara Formation andtheir known distribution in their parts of JapanK\ushuShikokuIIb lIe IS-I Is-m IS-IV IS-V M IFu INa

Bivalves from the Miyanohara F.

0

Nucula (Pectinucula) kochiensis

0Portlandia (5. I.) nagaseana

Glycymeris (Hanaia) goshonourensis

666- 06- 0Crassostrea kawauchidensis

0

Cucul/ aea (Idonearca) ezoensis ezoensis
Arr~ (Eonavicula) tashiroi

0

0 0 0
0
0
0 0 0 00 0 0 0 0
0 0
6- 0 00
6- 0

Pferotrigonia (?Scabrotrigonia) pustulosa @P (Ptilotrigonia) mifunensis@
P (Ptil.) amakusensis
P (Pfil.) miyanoharensis
Myrtea (Myrtea) amanoi
Thetis japonica
Pachythaerus nagaoi
crenulata?Legumen sp.
Pholadomya (Pholadomya) japonica
Pholadomya (Bucardiomya) hiratai
Periplomya japonica
Geological

0 0
0
0
0
0
0
0
0 0
0
0
0
0 0

Mk

0

0
0

0 0

0

0 0 0
0 0
0 0 0 0 0 0 0 0 0
60
0 0
0 0

0 0
0 0
0

66-

age

K

0
0
0

@

Anthonya apicalis
Goshoraia

66-

A

UMA

0

0

0

LLC

ULC

rMC MC LLC ULC LC

LC MC

IIb, IIe: Goshonoura Group in the island of Goshonoura, 8-1, 8-III, 8-V: Goshonoura Group in 8hishijima, M: Lower Formation of the Mifune Group (after Tamura, 1977), Fu: Upper Member of the
Fukigoshi Formation (after Tashiro and Matsuda, 1982), Na: Middle Member of the Nagase Formation(after Tashiro and Kozai, 1982), A: Misakubo Formation (after Matsushima and Kitamura, 1981), K:
Cenomanian rock from the sea bottom off the coast of Kuji (after Hayami and Kase, 1981), Mk:
Mikasa Formation, UMA: uppermost Albian, LLC: lower Lower Cenomanian, LC: Lower Cenomanian,
ULC: upper Lower Cenomanian, MC: Middle Cenomanian. b..: very rare, 0: rare, @: abundant.

ezoensis amaxensis and Anthonya japonica,
characteristic elements of the former (Le. Uppermost Albian to lowest Cenomanian). On theother hand, P. (Ptil.) Mgoensis, Cymbophoraokadakensis, Glycymeris (Hanaia) hokkaidoana
and Anthonya mifunensis which are characteristic species of the latter (Le. Middle Cenomanian), have not yet been found in the Miyanohara fauna. In addition to these facts, the Miyanohara fauna contains many species which arecommon with the faunas of the Lower andMiddle Cenomanian strata in various areas ofJapan as shown in Text-fig. 5.
Through this study the detailed change ofthe bivalve fauna from the late Albian to the
Cenomanian has been made clear. This would
be a foundation for further careful comparison
between various areas within the Japaneseprovince.

Tomoko MATSUDA

16
References

Univ. Tokyo, Bull., no. 10, p. 1-249, 10 pIs.
and Kase, T. (1981): Cenomanian molluscs
in a sandstone block form the sea bottom
off the southern coast of Kuji, Northeast
Japan. Trans. Proc. Palaeont. Soc. Japan,
n.s., no. 121, p. 29-50, pIs. 4-5.
Ichikawa, K. and Maeda, Y. (1958): Late Cretaceous pelecypods from Izumi Group, Part
2, Orders Taxodontida, Priodontida, Dysodotida, Desmodontida and Adapedontida.
Jour. Inst. Poly tech. Osaka City Univ., ser.
G., p. 71-122, pIs. 3-7.
Iwasaki, Y. (1963): Pseudamiantis, a pelecypod
genus. Trans. Proc. Palaeont. Soc. Japan,
n.s., no. 51, p. 91-101, pIs. 14, 15.
Matsukuma, A. (1979): Glycymeridid bivalvesfrom Japan and adjacent areas, part 1.

Amano, M. (1956): Some Upper Cretaceous
fossils from Southwestern Japan (part 1).
Kumamoto Jour. Sci., sec. 1, (geol.), vol. 1,
no. 1, p. 63-86, pIs. 1-2.
--(1957): The Lower Cretaceous fauna from
Hagino in Southern Shikoku, Japan. Ibid.,
vol. 1, no. 2, p. 77-121, pIs. 1-2.
Freneix, S. (1976): Les Mollusques bivalvescretaces du Bassin cotier de Tafaya (Maroc
meridional). Le Bassin cOtier de Tafaya(Maroc meridional), tome III Paleontologie
Notes & M. Servo geol. Maroc, no. 228, p.
49-255.
Hayami, I. (1975): A systematic survey of the
Mesozoic bivalvia from Japan. Univ. Mus.

Explanation of Plate 3

Goshoraia crenulata (Matsumoto)Fig.1. Dorsal view of internal mould (KSG 3406), x 1.2, loc. Hegushi of Shishijima, Kagoshima
Prefecture.
Fig. 2. Lateral view of right valve, gum cast of external mould (KSG 3404), x 1, loc. Miyanohara
of Sakawa area, Kochi Prefecture.
Fig. 3. Internal view of right valve, gum cast of internal mould (KSG 3405), x 1, loc. ditto.
Pholadomya (Pholadomya)japonica Amano
Fig. 4. Lateral view of right valve, plaster cast of external mould, xl, loc. Miyanohara, collectedby Mr. Hirata.
Fig. 5. Lateral view of left external mould (KSG 3409), x 1, loc. Hegushi.
Fig. 6. Lateral view of left external mould (KSG 3408), x 1, loc. Miyanohara.
?Legumen sp.
Fig. 7. Internal view of left valve, gum cast of internal mould (KSG 3407), xl, loc. ditto.
Pholadomya (Bucardiomya) hiratai sp. nov.
Fig. 8. Lateral view of imperfect right valve, plaster cast of external mould (KSG 3384), x 1,
loc. ditto, collected by Prof. Katto.
Fig. 9. Lateral view of imperfect right valve, plaster cast of external mould (KSG 3385), x 1,
loc. ditto, collected by Prof. Katto.
Fig. 10. Lateral view of imperfect right valve, plaster cast of external mould (HPC 8517), x 1,
loc. Nagase, Monobe area, Kochi Prefecture, collected by Mr. Hirata.
Fig. 11. Lateral view of imperfect right valve, plaster cast of holotype (external mould) (KSG3383), x 1, loc. Miyanohara, collected by Mr. Hirata.
Fig. 12. Lateral view of the same specimen, x 1.
Fig. 13. Dorsal view of the same specimen, x 1.
Periplomya japonica sp. nov.
Fig. 14. Lateral view of left valve, plaster cast of external mould (KSG 3413), x 1.8, loco Miyanohara_
Fig. 15. Lateral view of right valve, plaster cast of external mould (KSG 3412), x 1.2, loc. ditto.
Fig. 16. Lateral view of right external mould (KSG 3411), xl, loc. Hegushi.
Fig. 17. Lateral view of left external mould (KSG 3410), x 1, loc. ditto.

Plate 3

MATSUDA: Bivalve Fauna from Miyanohara Formation

2

3

5
6

7

. . .......

1014

790. Bivalve Fauna from Miyanohara Formation
Venus (Jap. Jour. Malac.), vol. 38, no. 2,
p.95-128.
Matsushima, N. and Kitamura, K. (1981):
Bivalve fossils from the Lower Cretaceous
Misakubo Formation. Shimoina Educ. Com.
Nat. Sci., vol. 4, p. 99-112, 5 pis. (in Japanese).
Matsumoto, T. (1938): Preliminary notes onsome of the more important fossils among
the Goshonoura fauna. Jour. Geol. Soc.
Japan, vol. 45, no. 532, p. 13-26, pis. 1, 2.
--(1977): Zonal correlation of the Upper
Cretaceous of Japan. Palaeont. Soc. Japan,
Spec. Pap., no. 21, p. 63-74.
--and Tashiro, M. (1975): A record of Mortoniceras (Cretaceous ammonite) from Goshonoura Island, Kyushu. Trans. Proc.
Palaeont. Soc. Japan, n.s., no. 100, p. 230238, pI. 25.
- - , Obata, I., Tashiro, M., Ohta, Y., Tamura,M., Matsukawa, M. and Tanaka, H. (1982):
Correlation of marine and non-marine
formations in the Cretaceous of Japan.
Pal. Soc. Japan, Fossils, p.1-26 (in Japanese).
--and Tashiro, M. (1982, ed.): Multidisciplinary research in the Upper Cretaceousof the Monobe area, Shikoku. Palaeont.
Soc. Japan, Spec. Pap., no. 25, p. 1-123,
23 pis.
Nagao, T. (1930): On some Cretaceous fossils
from the island of Amakusa, Kyushu,
Japan. Jour. Fac. Sci. Hokkaido Imp. Univ.,
ser. 4, vol. 1, no. 1, p. 1-25, 3 pis.
- - (1938): Some molluscan fossils from theCretaceous deposits of Hokkaido andJapanese Saghalien, Part 1, Lamellibranchiata and Scaphopoda. Ibid., vol. 4, no. 2,
p. 117-142, pis. 14-16.
- - (1943): Pholadomya from Japan. Jour.
Geol. Soc. Japan, vol. 50, no. 596, p. 153160, pis. 12, 13.
Stephenson, L. W. (i941): The larger invertebrate fossils of the Navarro Group of Texas.
Texas Univ. Publ., no. 4101, p. 1-641,
pis. 1-95.
Tamura, M. (1977): Cenomanian bivalves from
the Mifune Group, Japan. Pt. 2. Mem.

17

Fac. Educ. Kumamoto Univ., vol. 26, sec.
1, p. 107-144, pis. 1-3.
-and Packard, E. L. (1972): The genotype
species of Anthonya Gabb. Ibid., vol. 20,
p. 22-30, pI. l.
and Tashiro, M. (1976): Mesozoic bivalvesof Japan. Atlas of Japanese fossils, no. 43258.
Tashiro, M. (1971): Upper Cretaceous glycymerids in Japan. Trans. Proc. Palaeont.
Soc. Japan, n.s., no. 84, p. 225-242, pis.
27,28.
(1976): Bivalve faunas of the Cretaceous
Himenoura Group in Kyushu. Palaeont.
Soc. Japan, Spec. Pap., no. 19, p. 1-102,
12 pis.
- - and Kozai, T. (1982): Bivalve fossils fromthe Upper Cretaceous of the Monobe area,
Shikoku. Ibid., no. 25, p. 69-92, pis. 1214.
and Matsuda, T. (1982): The bivalve fossils
from the Cretaceous Fukigoshi formationof the Monobe area, Shikoku. Trans. Proc.
Palaeont. Soc. Japan, n.s., no. 127, p. 393418, pis. 62-65.
and - - (1983a): The biostratigraphy of theCretaceous pterotrigonians in Japan. Res.
Rep. Kochi Univ., vol. 31, nat. sci., p. 2560, pis. I-II.
and (1983b): A study of the pterotrigoniae from Japan. (I) Taxonomy. Mem.
Fac. Sci. Kochi Un iv. , ser. E, Geol., vol. 4,
p. 13-52, pis. 1-13.
Woods, H. (1899-1913): A monograph of theCretaceous Lamellibranchia of England.
vol. 1 (1899-1903), xliii+227 pp., 42 pis.;
vol. 2 (1904-1913), 473 p., 62 pis. Palaeontogr. Soc. London.
Yabe, H. and Nagao, T. (1928): Cretaceous
fossils from Hokkaido; Annelida, Gastropoda and Lamellibranchiata. Sci. Rep.
Tohoku Imp. Univ., ser. 2, vol. 9, no. 9,
p. 77-96, pis. 16, 17.
, - - and Shimizu, S. (1926): Cretaceous
mollusca from the Sanchu graben in the
Kwanto Mountainland, Japan. Ibid., vol. 9,
No.2, p. 33-76, pis. 12-15.

Tomoko MATSUDA

18

Akaishi iJf;1'i, Enokuchi IT / r1, Fukigoshi nxM&, Godaisan 1i:fj-LlI, GoshDnoura ~iiJfil1i, Hagino
Hegushi !lWill, Himenoura M2 / lifj, Hiraiga :'¥;lH'i, Izumi tlI*, Kashiwaguri tl~~, Katasoba JHPJ], Katsurazawa tttR, Kochi if~?:fl, Hokkaido ~tifjjJt'i. Kyusyu JL'J+I, Mifune ~An, Mikasa .=::'1:, Misakubo *11\, Miyanohara "'f / Iii{, Monobe 41~;m, Nagase 7](iffj. Odochi )dJij,
Sakawa it)ll, Shikoku RB[,t Shiroi 1'3;11:, Shishijima lllili'ff;!j, Ezo :r.. '/, Yunokuchi i~/ n~H!'f,

RBI'Wi*i~m?'. (t.:JII.l1!!t.!!\tC1)'f.i / IJl{m (Lower Cenomanian) n'I?g€-tG=tJefJ.{I::15I':''0l,-e
Lt, Amano (1956) I':''\: I) f1:fiI!n;~CJllX~.h "(l'Gn', A,liJI.wrlfi~(sts~< (1)=&H{I::1'i~tTHi~-r:~t::.(1)-r:, ;t;;l?t::.Iib-e~G$J(:-rGo*{I::Il 77'7 71t, ::::1'1 n Pterotrigonia (?Scabrotrigollia) pustu/osa, P. (Ptilotrigonia) mijunensis, P. (Ptil.) amakusl!llsis. tt. I? rfl.:. 7:/ -'E: 7 1 r Shapeiceras sp. (1)J1IT
IHn>f:, upper Lower Cenomanian c !.!.'.hh Q 0*- 1:::., *il::.(177 ry 'nt, :h 1+1 (1)'f,1jJi'Ji'iJiilri) jlf, f711[li1(1)JkMifot/, m,IlJIHJ)!(C1)}j(ntfr1, ~tifii)n(l):c:i9:fo;ci tt. c- n *,.:.;t;ft G*J1!!(1) Lower Cenomanian (l)J1!!II'i)C1){1::71 7 7 '77 c f;Cl(.!;J. L -e.t~ I) ,fH.:.:iU·IHIliliTli:j (1)f,ljIi'Ji'rill1I1ltY', S-lV)<,',/C1)ir.T,7 7 '77 c (U <-f{-r G

0f'~Ul'fjJT

Trans. Proc. Palaeont. Soc. Japan, N.S., No. 137, pp. 19-24, pI. 4, April 30, 1985

791. MULTILAMINAR COLONIES OF BRYOZOANS FROM JAPAN. 1.
"ECTOPROCTALITH" OF ANTROPORA TINCTA (HASTINGS)*YASUO NISHIZAWA
Department of Earth Sciences, Faculty of Science, Chiba University, Chiba, 260

Abstract.
A massive, multilaminar colony of Antropora tincta (Hastings)
attached to a gastropod shell from the Jizodo Formation (Middle Pleistocene)and its hydrodynamic system is described. It has regularly spaced mounds likemonticules and shows a high degree of colonial integration. The zooids overgrownby subsequent zooid layers have thin and concave "frontal walls".

described and its hydrodynamics are discussed.
Before going further, I would like to express
my sincere thanks to Professor Sumio Sakagami
of Chiba University for his constant guidanceand his kindness in reading this manuscript,
and to Dr. Tomoko Hayami of Ehime University for her kind guidance and encouragement.
I am particularly indebted to Dr. Patricia L.
Cook of British Museum (Natural History) for
her kindness in critical reading this manuscript.
I am also indebted to Messrs. Shinji Arakawa
and Kiyoshi Ishii of Chiba University for theirkind advice and assistance_

Introduction
Nodular cheilostome colonies have beenreported from the Cenozoic age by Canu andBassler (1923), Hoffmeister et al. (1967),
and Banta (1972). Recently, Rider and Enrico(1979) described such colonies as ectoproctaliths
which are "highly spherical ectoproct colonies
that begin development on various kinds ofprimary substrates." The growth-form of ectoproctaliths can be included in the Celleporiform
morphotype (Canu and Bassler, 1920; Lagaaij
and Gautier, 1965; Schopf, 1969) because
they are composed of numerous, concentric
layers of zooids. Rider and Cowen (1977) subdivided the celleporiform into two categories,
namely, Celleporiform A ectoproctaliths composed of numerous zooid layers of anascan
species, and Celleporiform B ectoproctaliths
developed from the zooid columns of ascophorans. Banta (1972) studied frontal bud
formation in an ascophoran species: Schizoporella
unicorn is floridana Osburn.
In this article, a Celleporiform A ectoproctalith of Antropora Uncta (Hastings), from the
Jizodo Formation (Middle Pleistocene), is

Locality of Specimen
The Jizodo Formation (Mid. Pleistocene)
distributed in the central part of Chiba Prefecture, Japan consists of shallow marine sediments
and contains many kinds of fossils, such asbivalves, gastropods and bryozoans which havebeen reported by Ogose (1959), Aoki and Baba
(1980) and Sakakura (1935).
A single specimen of massive, nodular colonyof Antropora Uncta was collected from loose,cross-bedded, coarse sands of the Jizodo Formation at Oi, about one kilometer west of Nishiyatsu. The locality and the columnar section*Received November 29,1983; read January 23,
1983 at Tokyo
19

Yasuo NISHIZA WA

20

Ni'hiya..

10

o

20 km

I

I

I

Text-fig. 1.

Map showing the locality (x) of sample studied.

taken at the outcrops at Oi are shown in Textfig. 1 and 2, respectively.

A

B

Ectoproctalith of Antropora tineta (Hastings)~~J.!JC I111I1III111

o

~

X

5m

E
Text-fig. 2. Columnar section of
the Jizodo Formation at Oi and showing
the horizon collected bryozoan colonystudied. A: cross-bedded, medium sands,
B: highly bioturbated muds, C: crossbedded, coarse sands with gravels andshells, D: medium sands with gravels
and shell fragments, E: cross-bedded, fine
to medium sands.

According to Rider and Enrico (1979), theCelleporiform A ectoproctaliths are known tobe produced by only two genera, namely, Membranipora Blainville and Conopeum Gray. The
specimen from the Jizodo Formation is, however, produced by Antropora tineta (Hastings)(PI. 4, Figs. 1-3). Osburn (1950) reported multilaminar colonies of A. tineta, and Banta (1973)
and Buss (1979, 1981) described that A. tin eta
can overgrow a pre-existing layer. This is the firstfind of the nodular colony of the genus Antropora Norman.
In this specimen, the primary substratum isa gastropod shell surrounded by approximately
70 further zooid layers (PI. 4, Fig. 5). The colonyof A. tineta is similar to that of Membranipora
flabellata Canu in the mechanism of colonial
development (see Rider and Enrico, 1979), but
it differs in the smaller dimensions of subcolonies(PI. 4, Fig. 11). The primary substratum may
have been more easily overturned by wave and/or

791. Ectoproctalith (Bryozoa) from Japan

current action than flat substrata or rocks. The
stratum comprised this nodular colony is composed of cross-bedded, coarse sands, and it isconsidered that the sediments was depositedunder strong current and/or wave action as
mentioned by Arakawa (1983).
It is clear that the previous zooids have"frontal walls" which are continuous withvertical walls (PI. 4, Fig. 4). They are thin andconcave. By use of a needle, the "frontal walls"of pre-existing zooids can be easily separated
from the basal walls of overgrown zooids. This
separation suggests that the frontal membranes
became calcified as "frontal walls", before theovergrowth of the next layer of zooids. Thereis a semicircular area in the distal part of frontal
wall and it seems to be reflected by the shapeand size of an operculum. Thus it is possiblethat the overgrown zooids may first become
closed by calcification, although it is not certainly known when the closure occurred.
The present colony is encrusted by two othercheilostomes, Verminaria areolae Sakakura (PI.
4, Fig. 9) and Stephanosella vitrea Osburn (PI. 4,
Fig. 10).
Hydrodynamics
Most of marine bryozoans generate colonywide current patterns to gather food particles
and to remove fecal pellets and sediments. Since
Banta, McKinney and Zimmer (1974) pointed
out the significance of colony-wide current
patterns, they have also been studied by otherauthors (Cook, 1977, 1979; Cook and Chimonides, 1980; Winston, 1978, 1979; Lidgard,1981). Taylor (1975) reconstructed the water
current system of the fossil cyclostome Reptomultisparsa incrustans which produced regularly
spaced mounds like the monticules known intrepostomatous bryozoans.
In the nodular colony of Antropora Uncta
there are numerous raised areas spaced in arhombic pattern (PI. 4; Fig. 6). Distance between
the nearest mounds (center-to-center) is about
4.6 mm and it is comparable to the center-tocenter distance between the nearest chimneys

21(4.56 mm) in Membranipora villosa Hincks(Lidgard, 1981). The distance is, however, larger
than those in Membranipora sp. by Banta et al.
(1974) and also in Cleidochasma contractum(Waters), Schizoporella cornuta (Gabb andHorn), Hippoporina porosa (Verrill), Cryptosula
pallasiana (Moll) and Parasmittina nitida (Verrill)by Cook (1977), and it is smaller than that in
Membranipora membranacea (Linnaeus) by Cook
and Chimonides (1980). Cook and Chimonides(1980) mentioned that the difference in distance
between chimneys is directly related to the large
size of the zooids in the population they studiedof M. membranacea at least. Therefore, themounds may represent areas where excurrent
water flow is expelled, and it may be that thepolypides form fixed clusters enhanced by theregular patterning of the colonial skeleton.
Thus the nodular colony of A. tincta seems to
be a highly integrated colony (see Cook, 1979).
According to Winston (1979) who divided many
marine bryozoans from Florida and Panama
into seven groups based on the type of colonial
behaviour pattern, polypides in A. Uncta form
temporary clusters or permanent clusters enhanced by an irregular patterning of the zoarium.
The difference of the types of behaviour pattern
between fossil and recent specimens may becaused by the environmental difference, or thecolony may produce regularly spaced mounds
as zooid layers increase in number.
There are two kinds of zooids in A. Uncta:
the large and small (see Table 1). Mean length oflarge and small zooids are 0.453 mm and 0.350
mm, respectively. The raised areas containirregularly arranged large zooids (PI. 4, Figs. 7,8) and the intervening channels consist of small
zooids which are arranged closely in a quincunx
pattern. The mounds distributed allover the
Table l. Zooecial measurements (in mm).
Mean
zooid
lengthZooids at the mounds
Zoo ids at the channels

Mean
zooid
width

0.453

0.305

0.350

0.225

Yasuo NISHIZAWA

22

A

Text-fig. 3.

B

Diagrammatic reconstruCtion of the development of mounds.

surface of the zoarium are low or high. The
diagrammatic reconstruction of the developmentof raised areas is shown in Text-fig. 3. A) There
are two mounds and the distance between themis suitable to establish a current system. B) As
the distance becomes broader with accumulationof zooid layers, it becomes difficult to maintainfeeding efficiency. The mounds become higher
because the large zooids of new layer overgrow
the pre-existing one. C) A group of large zooids
occurs between two high mounds. D) Consequently a low mound is produced. Recently,

Cook and Chimonides (1980) described thatthe mean length of chimney zooids and otherautozooids are 0.95 mm and 0.72 mm, respectively, in Membranipora membranacea.
Most cheilostome zooids have been considered to be hermaphroditic. Marcus (1938)
reported that there are male, female and sterile
zooids in Hippothoa hyalina (Linnaeus).
Gordon (1968) found the male zooids in Hippopodinella adpressa (Busk), but it is impossible
to distinguish them from other zooids in deador fossil specimens. According to Cook (1968),

Explanation of Plate 4
Figs. 1-8, 11. Antropora tincta (Hastings)
1-3. Showing the three dimensional views of the ectoproctalith, natural size. 4. Autozooids
with "frontal wall", x20. 5. Inside of the zoarium, showing a gastropod shell and zooid
lamination, natural size. 6. Another side of the zoarial surface, showing the development of
the regularly spaced mounds, natural size. 7, 8; Enlarged part of the mounds, x20. II.
Zoarial surface showing pseudoancestrulae, sub colonies and boundaries between subcolonies,
xl0.
Figs. 9, 10.
Verminaria areolae Sakakura and Stephanosella vitrea Osburn. Specimens of twoother species of bryozoan encrusting the colony of Antropora tincta, xl0.

NISHIZA WA: Ectoproctalith (Bryozoa) from Japan

Plate 4

791. Eetoproetalith (Bryozoa) from Japan
there are two kinds of zooids in Hippoporidra
senegambiensis (Carter). One of them, "corticalzooids" are larger and have a small number oftentacles lacking cilia. Silen (1977) consideredthat these zooids may have a male function
though the spermatozoa were not found in living
or preserved specimens. The facts of the tentacles
lacking cilia and of the cortical zooids occurredat the centers of the protuberances suggest thatthese areas represent chimneys and that malezooids are in a suitable position for the releaseof spermatozoa (Banta et al., 1974; Cook, 1977).
Thus there seems to be a relationship between
mounds and reproduction (see Cook, 1977).
But such relationship is not known in Antropora
tine ta, and further research is necessary.

References
Aoki, N. and Baba, K. (1980): Pleistocene molluscan assemblages of the Boso Peninsula,
Central Japan. Sci. Rep., Inst. Geosci., Univ.
Tsukuba, Sec. B, vol. 1, p. 107-148.
Arakawa, S. (1983): Sedimentary facies of the
Jizodo Formation (Pleistocene), Boso Peninsula. Clastic Sediments (Jour. Clastic Sediments Research Group in Japan), no. 2, p.
8-15 (in Japanese).
Banta, W. C. (1972): The body wall of cheilostome Bryozoa, V. Frontal budding in
Schizoporella unicornis f/oridana. Mar. Bioi.,
vol. 14, p. 63-71.
--(1973): The significance of areolae in cheilostome Bryozoa. in Larwood, G. P. (ed.)
Living and Fossil Bryozoa, p. 209-219.
Academic Press, London.
- - , McKinney, F. K.and Zimmer, R. L. (1974):
Bryozoan monticules; excurrent water outlet? Science, vol. 185, p. 783-784.
Buss, L. W. (1979): Bryozoan overgrowth interactions - the interdependence of competition for space and food. Nature, vol. 281, p.
475-477.
--(1981): Mechanisms of competition between
Onychoce/la alula (Hastings) and Antropora
tincta (Hastings) on an eastern Pacific rocky
shoreline. in Larwood, G. P. and Nielsen, C.
(eds.) Recent and Fossil Bryozoa, p. 39-49.
Olsen and Olsen, Fredensborg.

23

Canu, F. and Bassler, R. S. (1920): North
American Early Tertiary Bryozoa. U.S.
Nat. Mus. Bull., vol. 106, p. 1-879, pIs. 1162.
--(1923): North American Later Tertiary and
Quaternary Bryozoa. Ibid., vol. 125, p. 1302, pIs. 1-47.
Cook, P. L. (1968): Observations on Living
Bryozoa. Atti. Soc. Ital. Sci. Nat., vol. 108,
p.155-160.
--(1977): Colony-wide water currents in living
Bryozoa. Cah. Bioi. Mar., p. 31-47.
--(1979): Some problems in interpretation ofheteromorphy and colony integration in
Bryozoa. in Larwood, G. P. and Rosen, B. R.
(eds.) Biology and Systematics of Colonial
Organisms, p. 193-210, Academic Press,
London.
--and Chimonides, P. J. (1980): Further
observations on water current patterns inliving Bryozoa. Cah. Bioi. Mar., p. 393-402.
Gordon, D. P. (1968): Zooidal Dimorphism in
the Polyzoan Hippopodine/la adpressa(Busk). Nature, vol. 219, p. 633-634.
Hoffmeister, J. E., Stockman, K. W. and Multer,
H. G. (1967): Miami Limestone of Florida
and its Recent Bahamian counterpart. Bull.
Geol. Soc. Amer., vol. 78, p. 175-190.
Lagaaii, R. and Gautier, Y. V. (1965): Bryozoan
assemblages from marine sediments of theRhone delta, France. Micropaleont., vol. 11,
no. 1, p. 39-58.
Lidgard, S. (1981): Water flow, feeding, andcolony form in an encrusting cheilostome.
in Larwood, G. P. and Nielsen, C. (eds.)
Recent and Fossil Bryozoa, p. 135-142,
Olsen and Olsen, Fredensborg.
Marcus, E. (1938): Bryozoarios marinhos brasileiros II, Bolm Fac. Filos. cienc. Univ. S.
Paulo Zool., vol. 2, p. 1-196.
Ogose, S. (1959): On the type of mixture ofmolluscan fossil-coenosis in the Zizodo
Sand at Atebi, Hukuta-mati, Kimitu-gun,Tiba Prefecture, South Kanto, Japan.
Jour. Geol. Soc. Japan, vol. 65, no. 760, p.
31-46.
Osburn, R. C. (1950): Bryozoa of the Pacific
Coast of America. Part I. CheilostomataAnasca. Allan Hancock Pacific Exped., vol.
14, p. 1-269, pIs. 1-29.
Rider, J. and Cowen, R. (1977): Adaptive archi-

24

Yasuo NISHIZA WA

tectural trends in encrusting ectoprocts.
Lethaia, vol. 10, p. 29-4l.
Rider, J. and Enrico, R. (1979): Structural andfunctional adaptations of mobile anascan
ectoproct colonies (ectoproctaliths). in
Larwood, G. P. and Abbott, M. D. (eds.)
Advances in Bryozoology, p. 297-319.
Academic Press, New York.
Sakakura, K. (1935): Pliocene and Pleistocene
Bryozoa from the Boso Peninsula (1). Imp.
Univ. Tokyo, Fac. Sci., Jour., Sec. II, vol.
4, p. 1-48, pIs. 1-7.
Schopf, T. J. M. (1969): Paleoecology of ectoprocts (bryozoans). Jour. Paleont., vol. 43,
p.234-244.

Silen, L. (1977): Polymorphism. in Woolacott,
R. M. and Zimmer, R. L. (eds.) Biology ofBryozoa, p. 184-232. Academic Press, NewYork.
Taylor, P. D. (1975): Monticules in a Jurassic
cyclostomatous bryozoan. Geol. Mag., vol.
112, no. 6, p. 601-606, 1 pI.
Winston, J. E. (1978): Polypide morphology andfeeding behavior in marine ectoprocts. Bull.
Mar. Sci., vol. 28, p. 1-3l.
- - (1979): Current-related morphology andbehaviour in some Pacific coast bryozoans.
in Larwood, G. P. and Abbott, M. D. (eds.)
Advances in Bryozoology, p. 247-268,
Academic Press, New York.

Jizodo jIQ;i:tt'i!::, Nishiyatsu gg;fr, Oi j;:1t-

A *i£-=- vt!i!.O)~~tl:llff*o :?CO) 10 Anlropora tincla (Hastings) 0) "Ectoproctalith":
Anlropora tincla (Hastings) O)Mf;J;:(Ectoproctalith) v':''':)\''-C, :?CO) j-'P¥;ilic7fciift>%tr" ~cJ!iXLt..::o ltH1>:krnH.:.(t, :JLE:ffJ; (mon·ticules) 1.:.1.Clt..::~~n;m.[\IJfl/]~:.[Ij~71j L -C:t; I), ;~I5tO)m ftn;ff:(£ Lt..:: -=- c tr"~ L -C \" 0 0 tJ!l1U~nt..::(I.\j!i!.f':'ftiW< -C < Ic£/vt.3. 1~!llJ n;.7,..Gn0 o
j1§~EJt'jj
l1.H;G't~£,j;rgI~~h~jlQiIl:!it.mn, j:-Ji£/±l L t..::J:ll!~x-C-~J\,W10)

Trans. Proc. Palaeont. Soc. Japan, N.S., No. 137, pp. 25-49, pIs. 5-7, April 30, 1985

792. LATE PERMIAN AMMONOIDS FROMTHE SOUTHERN KITAKAMI MASSIF, NORTHEAST JAPAN*
MASA YUKI ERIRO
Department of Earth Science, College of General Education, Tohoku University,
Sendai 980
and
YUJI BANDO**
Department of Geology, Faculty of Education, Kagawa University,
Takamatsu 760

Abstract.
Biostratigraphical correlation among the Upper Permian sectionsof the Southern Kitakami, Transcaucasia, Iran and South China is discussed basedon the ammonite fauna of the Upper Permian Toyoman Series distributed in the
Utatsu and Okago districts of the Southern Kitakami Massif. Thirteen species
belonging to nine genera are described. Among them, one new family, Paratirolitidae, and two new species, Medlicottia kitakamiensis and Prototocerasjaponicum,
are proposed.
The lowermost part of the Toyoman Series contains Dzhulfian ammonites,such as Araxoceras cf. A. rotoides and Pro to toceras japonicum sp. nov. The Lower
and Middle Toyoman are correlated to the Dzhulfian in Transcaucasia and Iran,and to the Wujapingian in South China, taking the occurrence of Araxoceras cf.
A. kiangsiense from the middle part (Murata and Bando, 1975) into consideration.
It is highly probable that the Upper Toyoman is correlated to the Dorashamian inTranscaucasia and Iran, and to the Changxingian in South China based on theoccurrence of Para tiro lites ? sp.

1969), Abadeh in Central Iran (Bando, 1979;
Iranian-Japanese Research Group, 1981) andSouth China (Chao, 1965; Zhao et al., 1978).
In the Japanese Islands, ammonoids havebeen scarcely reported from the Permian, particularly from the upper part. Up to date, only
seven specimens have been found and all arefrom the Southern Kitakami Massif, Northeast
Japan.
The Permian system in the Southern Kitakami Massif is divided into three Series, namely,
the Sakamotozawan, Kanokuran and Toyoman

Introduction
Ammonoid fossils, as well as fusulinids, havebeen considered to be useful in subdivision andworld-wide correlation of the Permian rocks.
They are of increasing use and value in Upper
Permian stratigraphy in Transcaucasia andNorthwestern Iran (Ruzhentsev and Sarycheva,
1965; Teichert et al., 1973; Stepanov et al.,*Received Feb. 20, 1984; read Oct. 23, 1983 at
Kumamoto.
**Deceased.
25

26

Masayuki EHIRO and Yuji BANDO

in ascending order (ex. Minato et at, 1978).
The Toyoma Formation, the type of the Toyoman Series, was proposed by Mabuti (1932,MS) for a thick shale formation exposed in
Toyoma-cho, Tome-gun, Miyagi Prefecture. The
Toyoma Formation and its correlatives are
distributed in the seven separated areas in thesouthern part of the Southern Kitakami Massif(Fig. 1). They are composed mainly of blackshale and contain some intercalation of sandstone and conglomerate, showing rather uniform
lithological facies. They had long been thought
to be almost barren of fossils, with the exception of few sporadic occurrence of molluscs,
conularids, trace fossils and plants. Therefore,
the Toyoman Series had tentatively been assigned to be Late Permian without any positive
fossil evidence.
Murata (1969) correlated the Toyoman
Series to Middle Ochoan of North America
and to Chideruan (Chhidruan) of Salt Rangeon the basis of similarity of Bellerophontacean
fossils. Further, it was biostratigraphic ally
divided into three zones, namely, Euphemitopsis
kitakamiensis-Astartella toyomensis zone, Palaeoneilo ogachiensis-Phestia kon 'noi zone andKitakamispira hanzawai-Nuculopsis mabutii zone
in ascending order by Murata (in Working Group,
1975; Murata and Bando, 1975).
Since 1975, several important fossils, such as
ammonites, smaller foraminifers and fusulinids,
were reported from the Upper Permian in theSouthern Kitakami Massif. These fossils are as
follows:
Araxoceras cf. A. kiangsiense Chao - from
Palaeoneilo ogachiensis-Phestia kon 'noizone at Hiraiso coast (Murata and Bando,
1975).
Eumedlicottia sp. and Artinskia sp. - fromthe middle and upper part of the Toyoman Series at Okago (Bando, 1975).
Colaniella parva fauna in association with
Palaeofusulina sp. - from the upper partof the Toyoman at Mt. Nabekoshi, northern part of Kesennuma (Tazawa, 1975;
Ishii et at, 1975) and at Tanoura, Utatsu(Murata and Shimoyama, 1979).

Stacheoceras cf. S. trimurti Diener - from
Euphemitopsis
kitakamiensis-Astartella
toyomensis zone at Toyoma (Working
Group, 1975).
Xenodiscus cf. X. carbonarius Waagen - fromthe lowermost Toyoman ? at Okago (Ehiro
and Bando, 1978).
Rotodiscoceras sp. - from the upper Toyoman at Senmatsu (Ehiro and Bando, 1980).
In addition, Propinacoceras aff. P. galilaei
Gemmellaro described by Hayasaka (1963) fromthe h Member of the Iwaizaki Limestone, inwhich Abadehella-Colaniella assemblage wasobtained (Ishii et al., 1975), may also be an
Upper Permian (Abadehian) ammonite. Detailed
stratigraphic horizon of Propinacoceras is after
Koizumi (1975).
Recently, many ammonite specimens belonging to 9 genera and 13 species were collectedfrom the Upper Permian in the Utatsu andOkago districts, Southern Kitakami Massif. The
purpose of this paper is to clarify the biostratigraphy of the Toyoman Series based on theammonite fauna and to attempt the correlationof the Upper Permian distributed in the Tethys
Province.

Stratigraphy and Marine Fauna of theUpper Permian in Utatsu and Okago
1) Utatsu District
The Permian strata in this district are distributed in the eastern peninsula of Utatsu-cho,Motoyoshi-gun, Miyagi Prefecture (Fig. 1).
They form a nearly homoclinal structure, dippingto the west in various degrees (Fig. 2). Slaty
cleavage is well developed. It strikes N-S anddips steeply toward E or W.
The Permian of this district was divided into
the Kanokura and Toyoma Formations (Murata
and Shimoyama, 1979). The latter was subdivided lithologically into the Lower, Middle
and Upper. However, present investigation has
revealed that it is difficult to divide the Permianlithologically into four units mentioned above.
It could be classified only into two units, theSuenosaki Formation below and the Tanoura

792. Late Permian Ammonoids from Kitakami

27

Low.
Cret.(vo[c.)Low.
Cretaceous

rrrrm
Mid.-Up.
Uli1JJ Jurassic

II

Low.
Jura ssi ct.(:;\lk:::l Up. Triassic
1:: :::....:··;.1

Mid: Triassic
Low. Triassic}:j~TOYOman.§r===:l K~~}:i ~I:::::::::::J Sakamotozawan ~0..

~ Carboniferous

[MJ

- -

Porphyrite~ Granitic rockso•Gabbroic rocks

Text-fig. 1. Compiled geologic map of the southern part of the Kitakami Massif. The studied
areas are shown in the squares.

28

Masayuki EHIRO and Yuji BANDO

Fonnation above (Fig. 3). The latter is roughly
corresponds to the Upper Member of the Toyorna Fonnation by Murata and Shim oyama(1979).
The Suenosaki Fonnation, which attains morethan 800 meters in thickness, is typically developed along the northern coast of the peninsula,from the northeastern cape (Suenosaki) to theeastern coast of Tanoura. The Fonnation ismainly composed of shale and sandy shale, frequently associated with sandstone laminas. It
contains also some beds of sandstone and conglomerate. The sandstones are mostly of calcareous and dominant in the lower part. They
are often involved in the slump structure andthin out laterally. The conglomerates or pebbly
shales occur in two horizons in the lower part.
They consist of well rounded pebbles to cobbles
of various kinds of rocks in shale matrix andthin out laterally. Besides them, two types ofthin bedded, lenticular or nodular calcareous
rocks are frequently intercalated. One of themis phosphorous shale and the other is limestone,
composed of fibrous sparite. The lower limitof the Fonnation is unknown, because it isbelow the sea level.
Murata and Shim oyama (1979) reported thefollowing fossils from the same stratigraphic
sequence:
Lepidolina kumaensis Kanmera and L. multiseptata (Deprat) - from the calcareous
sandstone of the lowennost part (Loc. 1,
Fig. 2).
Euphemitopsis kitakamiensis Murata, Pseudopermophorus uedai Nakazawa and Newell
and Astartella toyomensis Nakazawa andNewell - from shale matrix of the both
conglomerates (Loc. 4, 6-8).
Palaeoneilo ogachiensis Hayasaka, Nuculida
and Neocalamites sp. - from shale of the
middle part (Loc. 9).
In addition to this previous work, we collected some ammonites in association with
Euphemitopsis-Astartella fauna from shale andcalcareous nodules in the lower conglomeratic
beds (Loc. 2,3, 5). They are as follows:

Stacheoceras iwaizakiense Mabuti. . . . . . . . . . . . . . . Loc. 2, 3,5
Pseudogastrioceras sp. . . . . . .. Loc. 3
Araxoceras cf. A. rotoides Ruzhentsev. ........... Loc.3
Loc.3
A. sp.
Pro to toce ras japonicum
Bando and Ehiro sp. nov.
Loc.3
P. spp. . ...... _ . . . . . . . .. Loc. 3
The Tanoura Fonnation confonnably overlies
the Suenosaki Fonnation. It is typically distributed along the eastern and northwestern
coast of Tanoura, and attains more than 600
meters in thickness. The basal part of the formation is composed of alternation of sandstoneand shale, 50 to 70 meters thick. The mainpart consists of shale, often associated withsandstone laminas, and contains lenticular
sandstones, showing slump structure, in thelower part. Two types of calcareous rocks
found in the Suenosaki Fonnation also occur
in the fonnation. The uppennost part of the
Tanoura Fonnation is in fault contact withLower Triassic fonnations in many places,
but in some places, e.g. at the northwesternhill of Tanoura, it is covered by the Lower
Triassic Hiraiso Fonnation with unconfonnity.
The lower part of the Tanoura Fonnation(loc. 10, 11) yields the following fossils (Murata
and Shimoyama, 1979):
Colaniella aff. C. inflata (Wang), Palaeofusulina sp., Bellerophon (B.) yabei Murata,
Kitakamispira hanzawai Murata (MS) and
Nuculopsis mabutii Murata (MS).

2) Okago District
In this district the Pennian fonnations arewidely distributed. They are bordered by granitic
rocks, the Senmaya Mass at the north andcovered unconfonnably by the Lower Triassic
Hiraiso Fonnation at the eastern and southern
part. In the western half of the district thePennian strata are complexly folded and faulted,
and slaty cleavage is clearly recognized in finegrained rocks. While in the eastern part, they
dip gently eastward and show rather simple
geologic structure. Slaty cleavage become grad-

792. Late Permian Ammonoids from Kitakami

0

1 Km

0.5

~~

~ 2 ~3 ~4 ~5g...
EZJ B m D

em

9

10

[]] 11

6

29

1

W

7

12

Text-fig. 2. Geologic map of the northern part of the Utatsu District. 1. fossil localities, 2-4.
Suenosaki Formation (2. shale, 3. conglomerate, 4. sandstone), 5. lower part of the Tanoura Formation (alternation of sandstone and shale), 6-7. main part of the Tanoura Formation (6. shale, 7. sandstone), 8-11. Triassic formations (8. Hiraiso Formation, 9. Osawa Formation, 10. Fukkoshi Formation, 11. Isatomae Formation), 12. porphyrite.
ually indistinct toward the east.
The main part of the Permian formationsin this district had been referred to the Lower
and Middle Triassic formations by Bando (1956,
MS, quoted partially by Onuki, 1956) andOnuki and Bando (1959) on the basis of thelithological similarlity to the Triassic formations
and the occurrence of "Pe.cten ", Pseudomonotis,
Eumorphotis, Deltopecten, etc. at Senmatsu
and Episageceras at Okago. However, after
reexamination of these fossils, it became clearthat Pseudomonotis sp. and Deltopecten sp.
are both referred to Aviculopecten ? onukii
Murata (Murata, 1969) and Episageceras sp. to
Eumedlicottia sp. (Bando, 1975), both Permianin age. Moreover, Permian age of these formations was confirmed by the discovery of Permianammonites at Okago and Senmatsu by theauthors (Ehiro and Bando, 1978, 1980).
The Middle and Upper Permian in the Okago
district are divided into four formations; theHigashifukakaya, Shin den, Okago and Senmatsu
in ascending order (Ehiro, 1979; Ehiro andBando, 1980). All four are in conformablecontact.
The Higashifukakaya Formation occurs in thenorthern part of this district. It conformably
overlies the Nishikori Formation, which yields
Pseudoschwagerina (Robustoschwagerina) shellwieni Hanzawa. The thickness attains morethan 1000 meters. The formation is composedof massive and bedded shales. The latter isinterlaminated or very thinly interbedded withsandstones, some of which show graded bedding.

Masayuki EHIRO and Yuji BAND 030:iJColaniella aff. inflatap Palaeofusulina sp.

it 11 Bellerophon fB.) yabei
t 10

Kitakamispira hanzawai
Nuculopsis mabutii

t 9 - Fblaeoneilo ogachiensis

Euphemik~f~£~miensis
Pseudopermophorus uedai
Astartella toyomensis!

Stacheoceras iwaizakiense:·. ~;~:~frf!;!· t0'8 Pseudogastrioceras
Araxoceras
rotoidesPrototoceras japonicum
i L.Lepidolina
kumaensis
multiseptata•.•.;;::~:~.!.~:.t::.

2-

sp.

cf.

t 1

Text-fig. 3. Geologic columnar section of
the Upper Permian along the northern andeastern coast of Utatsu.

Upper part of the formation contains lenticularconglomerate and sandstone. The conglomerate
has well rounded pebbles to boulders of various
kinds of rocks, i.e., shale, sandstone, granitic
rocks, porphyrites, chert and limestone. Limestone lens in the conglomerate at Konakogi(Loc. 1, Fig. 4) yields Pseudofusulina sp. and
Lepidolina sp.
The Shinden Formation, 200 to 300 metersin thickness, is exposed in the northern part.

The formation is composed of sandstone, alternation of sandstone and shale, and bedded
shale interlaminated with sandstone. The sandstones are grey to dark grey and coarse to very
coarse grained wacke. Calcareous sandstones areintercalated in places. At the west of Fujisawa
and the upper reaches of Matsukozawa, east of
Yonekawa, !t is intercalated with lenticularconglomerate. This formation is barren offossils.
The Okago Formation is widely distributed.
The main part of the formation is approximately
800 to 1000 meters thick. It consists of bedded
shale interlaminated or very thinly interbeddedwith sandstones, most of which show gradedbedding, and occasionally contains thin beds ofsandstone. The shale often changes laterally
into thin alternation of shale and sandstone.
The lower middle part is intercalated withalternation of sandstone and shale, 50 to 70
meters thick. Uppermost part of the formationis composed of massive or nearly massive blackshale. The thickness ranges from 80 to 300
meters and thins toward the south.
The Okago Formation yields the following
fossils:
Xenodiscus cf. X. carbonarius Waagen - fromshale of the lowermost part at Yahagi,
Okago (Loc. 2, Fig. 4) (Ehiro and Bando,1978).
Euphemitopsis kitakamiensis Murata, Warthia
sp., Straparollus (Euomphalus) uedai Murata,
Mourlonia (M.) toyomensis Murata, Spiroscalasp., Limipecten bandoi Murata, Pseudopermophorus uedai Nakazawa and Newell
and Astartella toyomensis Nakazawa andNewell - from shale of the lower part at
Nagahata (Loc. 3) (Murata, 1969). Exact
horizon of these fossils in the column is
not known, because of the complicatedgeologic structure and lack of key bed.
Aviculopectin ? onukii Murata - from shaleof the middle part at Yamashita, Okago(Loc.4).
Eumedlicottia sp. - from shale of the uppermost part at Kobuchi, Okago (Loc. 5)(Bando, 1975).

792. Late Permian Ammonoids from Kitakami

W0 alliiJ2

31

~3eB6

.
~
~3d ~5~2km
Text·fig.4. Geologic map of the Okago District. 1. Higashifukakaya Formation (la. shale, lb.
conglomerate, lc. sandstone), 2. Shinden Formation (2a. sandstone and shale, 2b. conglomerate),
3. Okago Formation (3a. bedded shale of the main part, 3b. massive shale in the Yonekawa district,
3c. conglomerate, 3d. sandstone, 3e. massive shale of the uppermost part), 4. Senmatsu Formation(4a. bedded shale, 4b. sandstone, 4c. massive shale), 5-6. Triassic formations (5. Hiraiso Formation,
6. Osawa Formation), 7. porphyrite, 8. fossil localities.

Masayuki EHIRO and Yuji BANDO

32
lithology@

Medlicottia
kitakamiensis

::::>

~

«
~
z

rtinskia sp.
Eumedlicottia sp.
ekclolobus cf. walkeri( otodiscoceras sp.)Paratirolites ? sp.

w
Vl

z
«

~

0

>

sp.

0

I-

0

t!)

«
:.::

®

0

Xenodiscus
cf. carbonarius

z
«

a:

Lepidolina sp.

:J

:.::

~
~

•:::::::.

maSSive black shale
bedded shalethin alt. of sst. & shale,::.<~~/ _~~~g~~ma:;~t~f sst. & shale

Text-fig. 5. Compiled geologic columnar
section of the Middle and Upper Permian in
the Ok ago District.

Paraconularia sp., Spiroscala sp., Straparollus(Euomphalus) uedai Murata and Aviculopecten ? onukii Murata - from shale of theuppermost part at some localities (Loc.
6-S).
The uppermost formation of the Permian inthis district is the Senmatsu Formation. It occurs
in the eastern half of the district and the total
thickness exceeds 1100 meters. The lower partof the Formation, about 300 meters in thickness, is mainly composed of bedded shale inter-laminated or very thinly interbedded withsandstone, and contains alternation of sandstone and shale in the lower part. The latteris 100 meters in maximum thickness and thins
toward the north. The sandstones in the alternation are medium- to very coarse-grained andpartially contains plant fragments. The upper
part of the formation consists massive or nearlymassive black shale, about SOO meters thick,that grades downward into bedded shale of thelower part. Calcareous rocks mentioned in the
Utatsu district are also intercalated in the formation but in lesser amount. The formation iscovered unconformably by the Lower Triassic
Hiraiso Formation.
The Senmatsu Formation yields the following
fossils:
Straparollus (Euomphalus) sp., Spiroscala sp.,
Nuculopsis sp., Phestia sp. and Paracalamites
sp. - from the alternation in the lower partat north of Unazawa, Okago (Loc. 9).
Aviculopecten ? onukii Murata, Medlicottia
kitakamiensis Bando and Ehiro sp. nov., andParatirolites ? sp. - from shale of the upper
part of the lower part at Kiridoshi, Senmatsu (Loc. 10).
Rotodiscoceras sp. - from shale of the lowest part of the upper part at Kiridoshi(Loc. 11) (Ehiro and Bando, 19S0). This
specimen is under reexamination, so that
it is not discussed in this paper.
Paraconularia sp., Straparollus (Euomphalus)uedai Murata, Spiroscala sp., Palaeoneilo sp.,
Aviculopecten ? onukii Murata, Eumedlicottiasp., Medlicottia kitakamiensis Bando andEhiro sp. nov., Cyclolobus cf. C. walkeri
Diener and plant fragments - from shale orcalcareouS nodules in the lower part of theupper part at Iwanosawa, Senmatsu (Loc.
12).
Artinskia sp. - from shale of the upper partat the south of the Kuromori-toge (Loc.
13) (Bando, 1975).
Paraconularia siitai (Sugiyama), Straparollus(Euomphalus) uedai Murata, Spiroscala sp.,
Aviculopecten ? onukii Murata, Palaeoneiloogachiensis Hayasaka, Nuculopsis sp. and792. Late Permian Ammonoids from Kitakami
Paracalamites iwatensis Kon'no - from shaleof the upper part at several localities inSenmatsu (Murata, 1967, 1969; Murata
and Shimoyama, 1979; Kon 'no, 1973).
Medlicottia kitakamiensis Bando and Ehiro
sp. nov. - from shale of the upper and uppermost part near Nagasakiyama, Senmatsu
and uppermost part near Takizawa-toge,
southwest of Magome (Loc. 14-19).

Faunal Consideration and Correlation
Before going to the discussion of the present
fauna, the definition of the Toyoman Series
must be considered in some detail, because, up
to date, it has not been defined precisely, particularly on the basis of biostratigraphic criteria.
For instance, Minato et al. (1978) proposed abiostratigraphic scheme for the Permian in theSouthern Kitakami Massif based mainly on
fusulinids and devided the Permian into threeseries and six stages. They subdivided the Toyoman into the Maehaman and Nabekoshian
Stages. However, in the subdivision the base of
the Toyoman Series and the boundary between
the Maehaman and Nabekoshian Stages were
not defined dearly. Smaller foraminifers andfusulinids have only been known from a few
localities and horizons of the series, because of
the Toyoman Series consists mainly of blackshale. Further, the black shale facies often
extends to the lower horizons. Therefore, smaller
foraminifers and fusulinids are not effectual in
the biostratigraphic subdivision of the Upper
Permian in the Southern Kitakami Massif. At
present, we consider that the base of the Toyoman is defined as the base of Euphemitopsis
kitakamiensis-Astartella toyomensis zone by
Murata (in Working Group, 1975; Murata andBando, 1975).
Among the ammonite fauna from the lower
part of the Suenosaki Formation, Araxoceras
cf. A. rotoides, A. sp., Prototoceras japonicum
sp. nov. and P. spp. are of great importance.
Araxoceras and Prototoceras are characteristic
ammonoids of the Dzhulfian. The species of
Araxoceras have been known from Unit 3 (Beds33with Araxoceras) of the Dzhulfian in Transcaucasia (Ruzhentsev and Sarycheva, 1965),
the Lower Julfa bed in Julfa, northwestern Iran
(Stepanov et al., 1969), the Dzhulfian bed in
Abadeh, Central Iran (Bando, 1979), the Wujapingian in South China (Chao, 1965; Zhao etal., 1978) and the middle Toyoman in theSouthern Kitakami, Japan (Murata and Bando,
1975). Prototoceras have been known from Unit
3 and 4 (Beds with· Vedioceras) of the Dzhulfianin Transcaucasia (Ruzhentsev and Sarycheva,1965), the Dzhulfian and Dorashamian in
Abadeh (Bando, 1979) and the Wujapingian inSouth China (Chao, 1965; Zhao et al., 1978).
None of these ammonites known as Araxoceras
fauna has been reported pre-Dzhulfian formations.
The Lower Toyoman Series together withthe uppermost part of the underlying Kanokuran Series has been correlated to the
Abadehian by the fossils previously reported(Murata and Shimoyama, 1979; Iranian-Japanese
Research Group, 1981). In the Utatsu district,however, the Araxoceras fauna was obtained
from a horizon about 80 meters above thehorizon of Lepidolina kumaensis, in association
with Euphemitopsis kitakamiensis-Astartella
toyomensis fauna, and no molluscan fossils
characterized the Euphemitopsis-Astartella fauna
have been collected below this horizon. Therefore, this horizon is regarded to be the base of
the Toyoman Series, and the lowest part of the
Toyoman is correlated to the Dzhulfian, not
Abadehian. The Abadehian in the Kitakami
Massif may be limited to the uppermost partof the underlying Kanokuran Series, namely,
Lepidolina kumaensis Zone. From the middle
part of the Toyoman Series, Araxoceras cf.
A. kiangsiense was reported (Murata and Bando,
1975), accordingly the Lower and Middle Toyoman are correlated to the Dzhulfian (Wujapingian).
Xenodiscus cf. X. carbonarius was collectedfrom the lowermost part of the Okago Formation. Xenodiscus carbonarius was originallyreported from the Middle Productus Limestone(Kalabagh Member of the Wargal Formation)

34

Masayuki EHIRO and Yuji BANDOin Salt Range as Ceratites carbonarius by Waagen(1872). It is later described from the Chhidru
Formation, which conformably· overlies the
Wargal Formation, as Xenodiscus carbonarius(Waagen, 1879). It is now known from theKuling Shale in Central Himalayas, the Zewan
Formation in Kashmir and the Abadeh Formation in Iran (Spinosa et aI., 1975; Bando, 1979).
The Kalabagh-Chhidru, the Kuling and the
Zewan have been considered to be of equivalent
age by many authors. The Kalabagh-Lower
Chhidru and Upper Chhidru are correlated to
the Abadehian and Dzhulfian, respectively(Iranian-Japanese Research Group, 1981). Therefore, the stratigraphic range of Xenodiscus
carbonarius is considered to be from Abadehianto Dzhulfian.
Euphemitopsis kitakamiensis-Astartella toyomensis fauna was reported (Murata, 1969) fromthe lower part of the Okago Formation, above
the horizon of Xenodiscus. This fauna belongs
to Early Dzhulfian in age as discussed already.
Thus the boundary between the Abadehianand the Dzhulfian in the Okago district is probably located near the boundary between the
Shinden and Okago Formations, although theexact horizon is not determined.
Of the ammonite fauna from the Senmatsu
Formation, Paratirolites ? sp. and Cyclolobus
cf. C. walkeri are important for correlation.
On the other hand, Eumedlicottia sp. and Medlicottia kitakamiensis sp. nov. are less usefulcomparatively. The species of Eumedlicottia
are common throughout Middle and Upper
Permian and have long ranges. M. kitakamiensis
may be the first record of the genus Medlicottia
from the Upper Permian.
Paratirolites is a characteristic ammonite of
the Dorashamian (Rostovtsev and Azaryan,1973) in Transcaucasia and Iran (Ruzhentsev
and Sarycheva, 1965; Stepanov et al., 1969;
Teichert et aI., 1973; Bando, 1979). It is also
known from Madagascar (Tozer, 1969) andLower Changxingian in South China (Zhao etal., 1978). In addition, Tozer (1979) concluded
that Shizoloboceras described from the Upper
Changxingian (Zhao et aI., 1978) is probably a

synonym of Paratirolites. The Kitakami specimens are rather poorly preserved, but fromthe shell ornamentation and general characterof whorls they seem to belong to Paratirolites.
Accordingly, it is highly probable that the
Senmatsu Formation is correlated to the Dorashamian and Changxingian.
The occurrence of Cyclolobus cf. C. walkeri
just above the horizon of Paratirolites ? sp. isof interest. At present, Cyclolobus walkeri
is known from the Chitichum Limestone in
Tibet, Kuling Shale in Central Himalayas,
Chhidru Formation in Salt Range, Zewan Formation in Kashmir and Ambilobe Formationin Madagascar (Furnish and Glenister, 1970;
Furnish et al., 1973). The stratigraphic range ofgenus Cyclolobus has been considered to befrom Abadehian to Dzhulfian by many authors,although there is an opinion that the age of
Cyclolobus is Guadalupian (Zhao et al., 1978;
Zhao, 1980). Present specimens of Cyclolobus
were collected from the Senmatsu Formation,
which conformably overlies the Dzhulfian
Okago Formation. Therefore, it is evident thatthey are of Late Permian age. Moreover, present
data may indicate that Cyclolobus ranges up
in~o the Dorashamian (Changxingian), becauseof it is associated with Paratirolites ? sp.
The precise correlation of the Upper Permian
sequences between the Utatsu and Okago districts is difficult. However, coarse grained rocks
are dominant both in the lower part of the
Tanoura Formation and the lower part of theSenmatsu Formation. The lower part of the
Nabekoshiyama Formation in northern partof Kesennuma, which yields Palaeofusulina
sp. and Colaniella parva fauna (Ishii et al., 1975;
Tazawa, 1975), is also composed mainly ofsandstone. They may be correlated each otherbased on the lithologic similarity. Further biostratigraphic studies are needed on the boundary
between the Dzhulfian and the Dorashamianin the Southern Kitakami Massif.
Correlation of the Upper Permian formationsin the Southern Kitakami Massif and those in
the Tethys Province is given in Table 1.

792. Late Permian Ammonoids from Kitakami

35

Table 1. Correlation chart of the Upper Permian in the Southern Kitakami Massif, Northeast Japan,
South China, Salt Range, Iran and Transcaucasia .
• - horizon of ammonites, a - horizon of smaller foraminifers and fusulines.

~ MID. PERMIAN~GUADALUPIAN~ MAOKAUAN

UPPER PERMIAN
DZHULFIANABADEHIAN

CHANGXINGIAN
BAOQ. MEISH.
(Talung F.)

WUJAPINGIAN.0

Chhidru F.

~. KANOKURAN
(

SALT
RANGE

..,)

TOYOMAN

HigashifUkakaya Shinden
Form.
Form.

Senmatsu Form.

Okago Form.

•

•

o

•••

••

0

0

0

0

~ Iwaizaki Lst.
a

a

a

f-3
f-3

0

w

c:::
f-3
0
0-<:
0

.

.,)

•

~

~

::r:

"Toyoma" Form.
a

•

H

::0
~

•

0

"Toyoma" Form.

H
W

0
:;>;:
Nabekoshiyama ~
zt>:!
Form.
~ c:::w
0

Acknowledgments
The writers wish to thank Professor Kei
Morl of the Institute of Geology and Palaeontology, Faculty of Science, Tohoku University for his valuable discussion and reading thefirst draft of the manuscript. Thanks are also
due to Professor Masafumi Murata of the Department of Geology, Faculty of Science, Kumamoto
University, and Dr. Shoichi Shim oyama of the

~

0
0

~

•
Toyoma Form.

Yamazaki Cgl.

0

:;>;:

e:

Suenosaki Form. Tanoura Form.

~o

USSR
& IRAN
SOUTH
CHINA

I

(Lungtan F.)~Wargal F. ~bagh M.

~

DORASHAMIAN

~

~t>:!

I- ~zI

Department of Geology, Faculty of Science,
Kyushu University, for their valuable suggestions
on geological problems.
Systematic Description
by Yuji Bando and Masayuki Ehiro
Specimens here described are kept in the
Department of Geology, Faculty of Education,
Kagawa University.

36

Masayuki EHIRO and Yuji BANDOTable 2.

Measurements in mm [Stacheoceras iwaizakiense]

TY-8306
Mabuti's
type specimen(IGPS, 51723)
D: Diameter of shell,umbilicus.

D

H

W

U

H/D

W/H

UID

38

18

17

3

0.48

0.95

0.08

37.2

23

18.3

0.62

0.79

H: Height of whorl, W: Width of whorl, U: Diameter ofSuperfamily Cyclolobaceae Zittel, 1895
Family Vidrioceratidae Plummer and Scott, 1937
Genus Stacheoceras Gemmellaro, 1887
Type species:-Stacheoceras mediterraneum
Gemmellaro, 1887.
Stacheoceras iwaizakiense Mabuti
PI. 5, Figs. 3a-c, 4a-b; Text-fig. 6A

1935. Stacheoceras iwaizakiense Mabuti, p. 147,
pI. 14, figs. 1-7.

1975. Stacheoceras iwaizakiense, Koizumi, p.
68, pI. 15, figs. 4a-d.

Description:-Shell involute, subglobular to
subdiscoidal, with broadly rounded venter,closed umbilicus and rounded-convex sides.
Shell surface smooth and ventral shoulders
indistinct, because of globular form of conch.
Suture well preserved as shown in Fig. 6A.
The ventral lobe broad and bifid symmetrically.
The first lateral lobe also bifid, the second andthird trifid, and the fourth bifid. The umbilicallobe consists of small lobes to the umbilicus.
Remarks:-Two specimens were examined.
They are clearly identified with S. iwaizakiense
Mabuti (1935), which was reported from thebasal part of the Iwaizaki Limestone, in which
Monodiexodina matsubaishi occurred from thelower part, at Iwaizaki, Kitakami Massif, in theform of conch. The suture line of the present
specimens is also similar to that of the typespecies by Mabuti as illustrated in Fig. 6.

Text-fig. 6.

Suture lines of Stacheo-

ceras iwaizakiense Mabuti.
A. Present specimen (TY-8306),H=16mm.
B. Type specimen by Mabuti (1935, pI.
XIV, fig. 5), No. 51723 (Tohoku
Univ., Sendai), H=14 mm.

The outline of the siphonal saddle of thepresent specimens is slightly different from thatof the type species. However, the general outlineof suture is very similar between both specimens. Mabuti compared the present species
with S. arthaberi Smith from the Lower Permianof Bitauni in Timor (Smith, 1927, p. 50, pI. 13,
figs. 15-17). The present specimens from the
Suenosaki Formation occurred together with
Araxoceras cf. A. rotoides Ruzhentsev in thelocality at Ishihama. Therefore, the horizonof the present specimens belongs to the
Dzhulfian of the Upper Permian and the biostratigraphic horizon of S. iwaizakiense is considered to be extended upward from the Kungurian to the Dzhulfian.
Occurrence and geological horizon:-Lowerpart of the Suenosaki Formation (Lowermost
Toyoman) at the eastern coast of Ishihama,
Utatsu-cho, Motoyoshi-gun, Miyagi Prefecture.
The Dzhulfian of the Upper Permian. Reg. No.
GLKU-TY-8202, 8306. Coli. M. Ehiro, 1982,
1983.

792. Late Permian Ammonoids from Kitakami

Family Cyclolobidae Zittel, 1895

37

about 7-8 points. Auxiliary series badly injured
by weathering. General character of sutures
arrange in parabolic form and apex of external
saddle bi-partites.
Remarks:-Two specimens were examined.
In the general characters of conch, the present
specimens are clearly compared with Cyclolobus
walkeri Diener based on the characteristicfeatures of septa, especially in the form of siphonal saddle, the form of umbilicus and on thefine ornamentation of shell surface. The holotype of C. walkeri (Diener, 1903, pI. 1, fig. 3ad) was reported from the fine grained whitelimestone of Chitichum in Tibetan Himalays.
It is stored in the Museum of Geological Surveyof India in Culcatta. In Kashmir, Furnish et al.
(1973) reported C. walkeri from the upper partof the Zewan Formation at Guryul Ravine section. In 1970, Furnish and Glenister described
C. walkeri from the Chhidru Formation of theSalt Range and concluded that the genus Cyclolobus is an index fossil of post-Guadalupian of
the Upper Permian. Another locality of C.
walkeri is in Madagascar. According to Furnish
and Glenister (1970, p. 172), more than 150
specimens of C. walkeri have been collectedfrom nodules in argillaceous strata at Ankitohazo(Ankitokazo) near Ambilobe in northern Madagascar. One of the authors (Bando, 1979) also
described Cyclolobus sp. from the Abadeh Formation in Ku-e-Hambest, Abadeh region, inCentral Iran. The Iranian Cyclolobus resembles
C. walkeri in the general character of conch,but it is unable to observe their suture owing
to poor preservation (Bando, op. cit.).
Cyclolobus is here first described in Japan.
Occurrence and geological horizon:-Fromcalcareous nodules of the Senmatsu Formation(Upper Toyoman) at Iwanosawa, Senmatsu,

Genus Cyclolobus Waagen, 1879
Type species:-Phylloceras oldhami Waagen,
1872.
Cyclolobus cf. C. walkeri Diener
PI. 5, Figs. la--c, 2; Text-fig. 7

Compare:1903. Cyclolobus (Krafftoceras) walkeri Diener,
p. 12-14, 162, pI. 1, figs. 3a-d.
1903. Cyclolobus (Krafftoceras) kraffti Diener,
p. 165-167, pI. 6, figs. 9a--c.
1903. Cyclolobus (Krafftoceras) haydeni Diener,
p. 167-169, pI. 6, figs. 7a-b, 8a-b.
1921. Cyclolobus walkeri, Diener, p. 27.
1936. Cyclolobus walkeri, Besairie, p. 105, pI.
4, figs. 6-9.
1940. Cyclolobus walkeri, Miller and Furnish,p.45.
1970. Cyclolobus walkeri, Furnish and Glenister,p. 165-173, text·figs. 2A-D, pIs. 2, figs.
A-D, 3, figs. A-E, 4, figs. H-J.
1980. Cyclolobus walkeri, Zhao, pI. 1, figs.
6-7.

Description:-Shell involute, subglobose andsub discoidal conch, with rounded venter, convex
sides and small umbilicus. Surface ornamented
by fine growth lines which slightly bi-projectedfrom umbilical margin to venter. Outer whorl
embraced completely inner whorls. Suture
partly well preserved as illustrated in Fig. 7.
Ventral lobe deepest and divided by broad bibranched siphonal saddle, about 2/3 height ofventral lobe, into narrowly distinct lobes. Siphonal saddle also denticulated and at a portionof 1/3 height most denticulated compared withothers. External and lateral saddles simply
denticulated and lateral lobes also denticulated,

Table 3. Measurements in mm [Cyclolobus cf. C. walkeri]

TY-8003
TY-8004

D

H

W

U

HID

W/H

U/D

69

30

29

5?

0.43

0.96

0.16?

50?

16?

Masayuki EHIRO and Yuji BANDO

38

9, pI. 1, figs. 1-3, pI. 2, fig. 2, 2a, as Goniatites
striatus Martin; Moller, 1879, p. 239, as Goniatites abichianus von Moller; Stepanov et al.,1969, pI. 6, figs. la-b; Teichert et al., 1973, p.
401, pI. 4, figs. 2-4) in the general characterof the shell, although it is unable to determine
the species name because of missing the suturesin the present specimen.
Occurrence and geological horizon:-Lowerpart of the Suenosaki Formation (Lowermost
Toyoman) at the eastern coast of Ishihama,
Utatsu-cho, Motoyoshi-gun, Miyagi Prefecture.
Dzhulfian of the Upper Permian. Reg. No.
GLKU-TY-8303. ColI. M. Ehiro, 1983.

Fujisawa-cho, Higashiiwai-gun, Iwate Prefecture.
Upper Permian. Reg. No. GLKU-TY-8003,
8004. ColI. M. Ehiro, 1980.
Superfamily Goniatitaceae de Haan, 1825
Family Paragastrioceratidae Ruzhentsev, 1951
Genus Pseudogastrioceras Spath, 1930
Type species:-Goniatites
Moller, 1900. (in Arthaber)abichianus

vonPseudogastrioceras sp.

PI. 5, Fig. 5a-b
Remarks:-Only single specimen was examined. Characteristic concentric striae areobserved on the shell surface of the present
specimen. These concentric striae are considerably densely spaced and almost run parallel withoutline of the whorls. These striae are observedon the shell of Pseudogastrioceras, Agathiceras,
Adrianites and Retiogastrioceras. Of these
Permian ammonoid genera the present specimen
belongs to Pseudogastrioceras in the form ofumbilicus, that is narrow funnel-shaped with
distinct umbilical shoulders, and the featuresof whorl. The specimen resembles Pseudogastrioceras abichianus (von Moller) (Abich, 1878, p.

Superfamily Medlicottiaceae Karpinsky, 1889
Family Medlicottidae Karpinsky, 1889
Genus Medlicottia Waagen, 1880
Type species:-Goniatites orbignyana de Verneui!, 1845.
Remarks:-The genus Medlicottia was first
proposed by Waagen (1880) based on Goniatites
orbignyana de Verneuil from the Artinskian
beds of Ural. About ten species of the genus
Medlicottia have been reported from the Lower
and Middle Permian of the Ural, Salt Range,
Sicily, Timor and North America, up to date.
Medlicottia is closely related to Artinskia,
Eumedlicottia and Episagecera.~. The ancestralgenus of Medlicottia may be Propinacoceras
and the intermediate genus between Prop inacoceras and Medlicottia is Artinskia. Eumedlicottia is a little advanced form in comparison
with Medlicottia as shown in the suture which
is characterized by development of slight notches
in the side of the saddles (Spath, 1934; Bando,
1979). Medlicottia has some variabilities in theform of venter. The ventral shoulders of theconch are generally smooth. However, in somespecies, such as M. costellifera Miller and Furnish

Text-fig. 7. Suture line of Cye/olobus cf. C. walkeri Diener from the Senmatsu Formation (TY -8003). Bar seale is
10 mm.

Table 4. Measurements in mm [Pseudogastrioeeras sp.]

TY-8307

D

H

w

U

HID

W/H

U/D

34

17

10?

7

0.50

0.59?

0.21

792. Late Permian Ammonoids from Kitakami(1940, p. 57, pI. 7, figs. 2-4, pI. 8, fig. 4, pi. 9,
fig. 3), two rows of small ventral nodes, lateralextensions of which continue as ribs across theventral portion of the flanks, are prominent.
Artinskia and Propinacoceras have also two
distinct rows of ventral nodes, lateral extensionsof which are across the ventral part from theventral shoulders to the median part of theventer. These characters of the ventral nodes
are prominent in the genus Artinskia and Propinacoceras rather than those of Medlicottia.
In addition, the genus Medlicottia is clearly
distinguished from the genera Artinskia andPropinacoceras in the form of external saddle.
Miller and Furnish (1940, p. 40) stated that
Artinskia seems to have arisen from Uddenites
and the sutures of Propinacoceras are more orless intermediate between those of typicalUddenites and those of typical A rtinskia , andthe suture of Artinskia passes through a Prop inacoceras stage during their ontogenetic development. We think that the evolutional evidence
is suggested in the change of sutures of theexternal and lateral saddles from Uddenites
to Artinskia or Medlicottia, and those of
Eumedlicottia are higher stage of evolution
as well as those of Episageceras.
Occurrence and geological horizon:-Permian,especially A.rtinskian to Dzhulfian. Urals, Sicily,
Timor, North America and Japan.

39

Medlicottia kitakamiensis sp. nov.
PI. 6, Figs. 1-7, Text-figs. 8A-D

Description:-Shell involute, discoidal, laterally compressed, with closed umbilicus, slightly
convex sides, and narrowly concave venter with
two rows of prominent small ventral nodes
extending from ventral sides, about 4/5 height,
crossing venter, to median part of venter, like
Artinskia or Propinacoceras. Main part of shellsurface almost smooth except for nodes ornamentation of ventral sides. Suture typical typesof Me dlic 0 ttia , consisting of narrow ventral
lobe, high narrow denticulated external saddle,
a bifid lateral lobe, and of numeous auxiliary
lobes and saddles.
Remarks:-Eleven specimens were examined.
Shell ornamentation and sutures of the present
specimens are well preserved. But in somespecimens, ventral parts and umbilicus are
ill-preserved. The present new species has tworows of prominent small ventral nodes extending
from ventral sides as in Artinskia or Prop inacoceras but the suture of the present species
has a character of Medlicottia, especially inthose of external saddle. However the speciesof Medlicottia described up to date have no
distinct ventral nodes except for M. costellifera
Miller and Furnish (Miller and Furnish, 1940,
p. 57, pI. 7, figs. 2-4; pI. 8, fig. 4; pI. 9, fig. 3)
from the Leonard Formation in the Glass Mountain and Finlay Mountain, Texas in North

Table 5. Measurements in mm [Medlicottia kitakamiensis sp. nov.]
D

H

TY-8001(Holotype)40

TY-8002
TY-8101

W

U

HID

20?

2?

0.50?

0.05?

48

23?

3?

0.48?

0.06?

54

24?

TY-8102

49

21

TY-8103

69

35

TY-8105

49

23

TY-8107

32

18

W/H

U/D

0.44?
12?

2

0.43

5?

0.51

0.04
0.35?

0.07?

0.48
2?

0.56

0.06?

Masayuki EHIRO and Yuji BAND 040

and near Takizawa-toge, southwestern part ofMagome, Motoyoshi-cho, Motoyoshi-gun, Miyagi
Prefecture. Upper Permian. Reg. No. GLKU-TY8001 (Holotype), 8002, 8101-8109. ColI. M.
Ehiro, 1980, 1981.

A
(

B

c

\r0~~
~f2~

Genus Eumedlicottia Spath, 1934f

I 1--10 mm---l

D

E

1~~
GDJ)
.)\..[1../\[\/ . .J
f+--l0mm -1

Text-fig. 8. Suture lines of Medlicottia and Eumedlicottia.
A-D. Medlicottia kitakamiensis Bandoand Ehiro, A. TY-8001 (Holotype), H=19mm, B. TY-8107, H=18 mm, C. TY-8106,
H unknown, D. TY-8104, H=23 mm. E.
Eumedlicottia sp., TY-8005, H unknown.
America_ The ornamentation of small ventral
nodes of M. costellifera is more indistinct thanthat of the present new species and projected
forward in the ventral margin. Regarding thesuture line, the present new species has 6-7
denticulations in the external saddle, as inthose of M. costellifera and M. kingolum Miller
and Furnish (1940, p. 60, pI. 4, figs. 5-7),
while the species of Artinskia and Neogeoceras
have 5 denticulations in the external saddle.
Occurrence and geological horizon:-Fromshale of the middle and upper part of the Senmatsu Formation (Upper Toyoman). Kiridoshi,
Iwanosawa and Nagasakiyama in Senmatsu,
Fujisawa-cho, Higashiiwai-gun, Iwate Prefecture,

Type species:-Medlicottia
mellaro, 1887.

bifronsGem-

Eumedlicottia sp.
PI. 6, Fig. 8, Text-fig. 8E
Remarks:-Single specimen was examined.
The shell is a fragment of the outer whorl andshell ornamentation is missing. Only sutures
are well preserved. Inner whorl and their suturesare slightly preserved. Sutures clearly belong tothat of Eumedlicottia and consist of numerous
lateral saddles and are subdivided lateral lobes.
Lateral saddles bifurcate at half height of bothwings, but their bifurcation is not distinct inthe sutures of the inner whorls.
Judging from the suture, the present specimen is similar to Eumedlicottia primas(Waagen) from Timor, but it is difficult todetermine the specific name because of poor
preservation of the material.
Occurrence and geological horizon:-Fromshale of the middle part of the Senmatsu Formation (Upper Toyoman) at Iwanosawa, Senmatsu, Fujisawa-cho, Higashiiwai-gun, Iwate
Prefecture. Upper Permian. Reg. No. GLKUTY-8005. ColI. M. Ehiro, 1980.
Superfamily Otocerataceae Hyatt, 1900
Family Araxoceratidae Ruzhentsev, 1959
Genus Araxoceras Ruzhentsev, 1959
Type species:-Araxoceras latissimum Ruzhentsev,1959.
Araxoceras cf. A. rotoides Ruzhentsev
PI. 7, Figs. la-c

792. Late Permian Ammonoids from Kitakami

41

Table 6. Measurements in mm [Araxoceras cf. A. rotoides]

TY-8301

D

H

W

U

HID

W/H

U/D

43(24)

20(10)

15

10(8)

0.46

0.75

0.23

Compare:1963. Araxoceras rotoides Ruzhentsev, p. 57,
fig. la, pI. V, figs. la-b.
1965. Araxoceras rotoides, Shevyrev, in Ruzhentsev and Sarycheva, pI. XVIII, fig. 2.
1969. Araxoceras rotoides, Stepanov et aI.,
pI. IX, figs. 3a-b.
1979. Araxoceras rotoides, Bando, p. 119, pI.
I, figs. 2a-b, pI. II, figs. 2, 4, 5a-b.

lated to the Dzhulfian of Transcaucasia and Iran.
Occurrence and geological horizon:-Fromcalcareous nodule in the lower part of the Suenosaki Formation (Lowermost Toyoman) at theeastern coast of Ishihama, Utatsu-cho, Motoyoshi-gun, Miyagi Prefecture. The Dzhulfian of
the Upper Permian. Reg. No. GLKU-TY-8301.
ColI. M. Ehiro, 1983.

Description:-Shell rather involute, discoidal,
laterally compressed, with broadly tabulated
venter, but slightly convexed to median ridge?
on venter. Umbilicus width is about 1/4 of total
diameter of shell and umbilical rim likes ear-lobe.
Shell sides concave and ventral margin sharply
edged. Cross section of whorl high-trapezoidal
form. Maximum width at umbilical margin about
15 mm, and height of whorl about 20 mm inlast whorl. Shell surface ornamented with slightradial striations from umbilicus. Suture unknown.
Remarks:-Single specimen was examined.
The present material is slightly deformed laterally, but the general characters of the shell are
well-preserved.
The present specimen is compared with
Araxoceras rotoides Ruzhentsev (Ruzhentsev,
1963) in the shell form, although the suture is
missing in the former. A. rotoides has beenrecorded from the Dzhulfian beds of Transcaucasia and Iran (Ruzhentsev, 1963; Stepanov
et al., 1969). Recently, A. rotoides was described by Bando (1979) from the Araxoceras
tectum Zone of the Upper Dzulfian bed at Kuhe-Hambest in Abadeh, Central Iran. The related
species, "Prototoceras" longilobatum Zhao,
Liang et Zheng (Zhao et al., 1978, p. 96, pI. 5,
figs. 4-6) was reported from the Laoshan Shaleof the "Loping" Series in South China. In South
China araxoceratid ammonoids occur commonlyfrom the Wujapingian which is probably corre-

Araxoceras sp.
PI. 7, Fig. 2a-b

Description:-Shell rather involute, discoidal,
rather depressed, with slightly convexed tabulated venter. Sides concave from umbilicalmargin to ventral shoulders. Umbilical margin
sharply elevated. Ventral margin also sharply
edged and cross section of whorl showing lowtrapezoidal form. Diameter of shell about 18
mm, maximum width of shell about 14 mm atumbilical margin, height of whorl about 10 mm
and diameter of umbIlicus about 5 mm. Suture
unknown.
Remarks:-Single fragmental specimen was
examined. More than half of the whorl is missingin the present specimen, but the umbilicus,
ventral part and shell surface are all well-preserved. Judging from the general characters of
the shell the present specimen is similar to
Araxoceras tectum Ruzhentsev (1963, p. 38,
pI. V, fig. 2a-b; Shevyrev, 1965, pI. XVIII,
fig. 1a-b, in Ruzhentsev and Sarycheva),
which commonly occurs from the Dzhulfian
beds in Armenia and Iran, but it is difficult to
identify with the species mentioned above.
On the other hand, the described specimensof "Prototoceras" plicatum Chao et Liang(Zhao et al., 1978, p. 93, pI. 4, figs. 34-36)
resem ble the present specimen in the whorl
characters, but it is also difficult to compare
the latter with the formers because of the poor

Masayuki EHIRO and Yuji BAND 042

Table 7. Measurements in mm [Prototoceras japonicum sp. nov.]

TY-8201

D

H

W

U

HID

W/H

U/D

25?(18)

11(5)

7

6

0.56

0.63

0.24

state of preservation.
Occurrence and geological horizon:-Fromnodule in the lower part of the Suenosaki Formation (Lowermost Toyoman) at the eastern
coast of Ishihama, Utatsu-cho, Motoyoshi-gun,
Miyagi Prefecture. The Dzhulfian of the Upper
Permian. Reg. No. GLKU-TY-8302. CoIl. M.
Ehiro, 1983.
Family Otoceratidae Hyatt, 1900
Genus Prototoceras Spath, 1930
Type species:-Gerotites tropitus Abich, 1878.
Prototoceros japonicum sp. nov.

PI. 7, Fig. 3a-c, Text-fig. 9A
Description:-Shell involute, discoidal, laterally compressed, with tricarinate venter. Sides
flat or slightly concave from umbilical margin
to distinct ventral shoulders. Umbilicus funnelshaped and umbilical margin projected. Diameterof umbilicus about 1/5 of total diameter of shell.
Surface ornamented with falcoid striations onflanks. Suture ceratitic, consisting of entire
lateral saddles and !!lightly denticulated laterallobes. Ventral lobe rather shallow and divided
into two points by small entire median-saddle.
Remarks:-Single specimen was examined.
The present species from the Suenosaki Formation resembles Prototoceros acutum Ruzhentsev(1959, p. 63, 1 Z, 22) in the general charactersof shell, but it is clearly distinguished from thelatter in having wider umbilicus and shorter
umbilical lobe. The present species resembles
also P. trochoides (Abich) (= Cerotites trochoides
Abich, 1878, p. 14, pI. 1, fig. 6, 6a) from theDzhulfian beds in Armenia, but the detailed
comparison is difficult, because the ventral partof the Armenian form is not well preserved.
Occurrence and geological horizon:-Fromcalcareous nodule in the lower part of the
Suenosaki Formation (Lowermost Toyoman)at the eastern coast of Ishihama, Utatsu-cho,Motoyoshi-gun, Miyagi Prefecture. The Dzhulfianof the Upper Permian. Reg. No. GLKU-TY8201 (Holotype). CoIl. M. Ehiro, 1982.
Prototoceros sp. A

Pl. 7, Fig. 4a-b, Text-fig. 9B
Description:-Shell laterally compressed, discoidal, with slightly tricarinated venter andslightly projected umbilical rim. Sides concave
without ornamentation. Umbilicus funnel-shaped.
Maximum width at umbilical margin and diameter of umbilicus about 1/4 of total diameter ofshell. Diameter of shell about 18 mm, height ofwhorl 7 mm, width of whorl probably 7 mm anddiameter of umbilicus about 5 mm. Suture rather
goniatitic, consisting of large lateral saddles,
narrow lateral lobe and shallow umbilical series.
Ventral lobe considerably deep with small
arched-shape median-saddle.
Remarks:-Single specimen was examined.
The present specimen is poor in preservation,
but the general shape of the shell and the character of the suture line may indicate that thepresent specimen belongs to the genus Prototoceras, although the specimen at hand is verysmall compared with the species of Prototoceros
which have been described from the Dzhulfian
beds of Transcaucasia and Iran. The present
specimen more or less resembles P. tropitum(Abich) illustrated by Ruzhentsev (1959, p.
62, figs. 1-2) in the general character of theshell and suture.
Occurrence and geological horizon:-Lowerpart of the Suenosaki Formation (Lowermost
Toyoman) at Ishihama, Utatsu-cho, Motoyoshigun, Miyagi Prefecture. The Dzhulfian of theUpper Permian. Reg. No. GLKU-TY-8303.
CoIl. M. Ehiro, 1983.

792. Late Permian Ammonoids from Kitakami
Prototoceras sp. B
PI. 7, Fig. 5a-b

Description:-Shell laterally compressed, discoidal, with slightly rounded venter and flat orslightly concave sides. Umbilicus funnel-shaped
and umbilical margin slightly projected. Widthof umbilicus about 1/3 of total diameter of theshell_ Shell surface ornamented by fine growth
striae which projected on ventral shoulders anddiminished on venter. Suture unknown.
Remarks:-Single small specimen, half volution of outer whorl, was examined_ The present
specimen belongs to Prototoceras, judging fromthe shell feature and whorl shape, but it is difficult to determine the specific name, becauseof the poor state of preservation.
Occurrence and geological horizon:-At theeastern coast of Ishih am a, Utatsu-cho, Motoyoshi-gun, Miyagi Prefecture. From the calcareous nodule in the lower part of the Sue nosaki Formation (Lowermost Toyoman). The
Dzhulfian of the Upper Permian. Reg. No.
GLKU-TY-8304_ CoIl. M. Ehiro, 1983.
Prototoceras sp. C(Lowermost Toyoman) at Ishihama, Utatsucho, Motoyoshi-gun, Miyagi Prefecture. The
Dzhulfian of the Upper Permian. Reg. No.
GLKU-TY-8305. CoIl. M. Ehiro, 1983.
Superfamily Xenodiscaceae Frech, 1902
Family Xenodiscidae Frech, 1902
Genus Xenodiscus Waagen, 1879
Type species:-Xenodicus plicatus Waagen,
1879.
Xenodicus cf. X. carbonarius Waagen
PI. 7, Fig. 9, Text-fig. 9D

Compare:1872. Ceratites carbonarius Waagen, p. 355,
pI. 1, figs. 2-3.
1879. Xenodiscus carbonarius, Waagen, p. 35,

~

A

)l01,

B
)

PI. 7, Fig. 6a-b, Text-fig. 9C

Description:-Shell laterally compressed, discoidal, with tricarinated venter and slightly
concave flanks. Umbilicus not clear_ Suture
well preserved, consisting of entirely roundedbroad lateral saddles and narrowly denticulated
lateral lobes. Ventral lobe divided by broadly
rounded siphonal saddle_ Umbilical lobe considerably long without denticulation.
Remarks:-Single fragmentary specimen was
examined. The general features of the shell andsutures of the present specimen are included inthose of Prototoceras, but it is impossible todetermine the specific name, because of the poor
preservation. Only the element of suture issimilar to that of P. japonicum sp. nov. or P.
parallelum Ruzhentsev (1959, p. 63, figs. 1d-e,2d) from Armenia_
Occurrence and geological horizon.·-Fromthe lower part of the Suenosaki Formation

43

c

~

D

vIilJ1
t

E

!'\.~
I

Text-fig. 9.

Suturelines

ofPrototoceras, Xenodiscus and Paratirolites? A.Prototocerasjaponicum
Bando and Ehiro, TY-8201, H=9mm, B. P. sp. A, TY-8303, H=5mm, C. P. sp. C, TY-8305, H=7mm, D. Xenodiscus cf. X. carbonarius Waagen, TY-7701, H=7 mm,
E. Paratirolites ? sp., TY-8204, H=
12mm?

Masayuki EHIRO and Yuji BANDO

44

present specimen illustrated here was alreadyreported by us (Ehiro and Bando, 1978) fromthe lowermost part of the Okago Formation.
The general character of the shell is similar tothat of Xenodiscus carbonarius which was
originally described from the upper divisionof the Productus Limestone of Chhidru in theSalt Range, Pakistan (Waagen, 1879). The
horizon of X. carbonarius belongs to the uppermost part of the Wargal Formation (Kalabagh
Member) and to the Chhidru Formation in the
Salf Range (Furnish, 1966; Kummel, 1970;
Fatmi, 1973; Spinosa et al., 1975). In the
Abadeh Region, Central Iran, X. carbonarius
occurs from the basal part of the Abadeh Formation (Unit 4 by Taraz, 1974) (Ban do, 1979),
that is the type section of the Abadehian Stageof the Upper Permian.
Occurrence and geological horizon:-Fromshale of the lowermost part of the Okago Formation (Lowermost Toyoman ?) at Yahagi,Kami-okago, Fujisawa-cho, Higashiiwai-gun,
Iwate Prefecture. Upper Permian. Reg. No.
GLKU-TY-7701. CoIl. M. Ehiro, 1977.

pI. 2, figs. 2-5.

1970. Xenodiscus carbonarius, Kummel, p. 189,
pI. 2, figs. 4-9.

1978. Xenodicus cf. carbonarius Waagen, Ehiro
and Bando, p. 37-38, figs. 2 (1,2).

1979. Xenodiscus carbonarius, Bando, p. 131,
pI. V, fig. 7.

Description:-Shell evolute, laterally compressed, discoidal, with narrowly rounded
venter and wide umbilicus with abruptly roundedumbilical shoulders_ Shell surface ornamented
by slightly sigmoidal fine striations running fromumbilical margin to ventral margin, rather
slightly prominent on lower half height ofwhorl and half height of it becoming slightly
indistinct. Sutures primitive form of ceratitic,
consisting of slightly serrated lateral lobes (1stand 2nd) and entirely rounded external andlateral saddles. Ventral lobe missing and auxiliary
lobe simple. Denticulation in lateral lobes observed slightly 3-4 points at bottom, and firstlateral lobe widest and deepest than that ofsecond.
Remarks:-Single specimen was examined.
Only one side of the specimen is preserved. The

Table 8. Measurements in mm [Xenodiscus cf. X. carbonarius]

TY-7701

D

H

47?(38)13(12)W

U

HID

26(17)

0.28?(0.32)

W/H

U/D
0.05?(0.45)

Explanation of Plate 5
Figs. 1a-c, 2.
Cyclolobus cf. C. walkeri Diener . . . . . . . . . . . . . . . . . . . . . . . . . . . . . p. 37
1. GLKU-TY-8003, lateral (a), front (b) and ventral (c) views, x 0.9.
2. GLKU-TY-8004, lateral view of shell fragment, x 1.
The specimens illustrated in Figs. 1 and 2 were collected from the lower horizon of theupper part of the Senmatsu Formation at Iwanosawa, Senmatsu, Fujisawa-cho, Higashiiwai-gun,
Iwate Prefecture.
Figs. 3a-c, 4a, b. Stacheoceras iwaizakiense Mabuti . . . . . . . . . . . . . . . . . . . . . . . . . . p. 36
1. GLKU-TY-8306, lateral (a), front (b) and ventral (c) views, x 1.1.
2. GLKU-TY-8202, lateral view (a), x 1, and suture line on ventral part (b), x 1.5.
Figs. 5a, b. Pseudogastrioceras sp . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . p. 38
GLKU-TY-8307, lateral (a) and ventral (b) views, x 1.3.
The specimens illustrated in Figs. 3, 4 and 5 were collected from the lower part of the
Suenosaki Formation at eastern coast of Ishihama, Utatsu-cho, Motoyoshi-gun, Miyagi Prefecture.

EHIR O and BANDO: Lale Permian Ammo no ids from Kilalwmi

Plai e 54b792. Late Permian Ammonoids from Kitakami

Family Paratirolitidae nov.
Remarks:-The present new family is pro·
posed based on the following items: l)Dzhulfites
Shevyrev (in Ruzhentsev and Sarycheva, 1965,
type species: Dzhulfites spinosus Shevyrev) issynonymous with Paratirolites Stoyanow (1910)(Teichert and Kummel, in Teichert et al., 1973;
Bando, 1979; Tozer, 1981). Therefore, theFamily name "Dzhulfitidae" is preferable tochange into Paratirolitidae, 2) the genus Paratiro lites is more common than other genera inoccurrence and 3) the type species of Dzhulfites,
D. spinosus Shevyrev (in Ruzhentsev and Sarycheva, 1965, p. 173, pI. 21, fig. 9; pI. 22, fig. 1),
is very similar to Para tiro lites kittli Stoyanow.

Genus Paratirolites Stoyanow, 1910
Type species:-Paratirolites kittli Stoyanow,
1910.
Paratirolites ? sp.
PI. 7, Figs. 7, 8, Text-fig. 9E

Description:-Shell evolute, discoidal, withbroadly rounded venter and distinct umbilicalmargin. Sides are ornamented by considerably
widely spaced radial ribs which are distinct onshell surface from umbilical margin to halfheight of whorls, and each ribs diminish at
surface of half height of whorls. Suture slightly
preserved on shell, but ventral suture unknown.
Remarks:-Two specimens were examined.
The present specimens are rather poorly preserved, but the shell ornamentation and generalcharacter of whorls indicate that it may belong
to Paratirolites, although it is difficult to determine the species, because of missing their ventral
suture and precise whorl section due to lateral

45

deformation. Judging from the shell ornamentation, broadly rounded venter and the form ofumbilicus, forcibly to say, the present specimens resemble Paratirolites abichi (Shevyrev)(in Ruzhentsev and Sarycheva, 1965, p. 181,
pI. 26, fig. 4a-b, as Abichites).
Occurrence and geological horizon:-Fromshale of the upper part of the lower part of theSenmatsu Formation (Upper Toyoman) at
Kiridoshi, Senmatsu, Fujisawa-cho, Higashiiwai·
gun, Iwate Prefecture. Upper Permian. Reg.
No. GLKU-TY-8203, 8204. ColI. M. Ehiro,
1982.
References
Abich, H. W. (1878}: Geologische Forschungenin den kaukasischen Liinde rn. Th. 1, Eine
Bergkalkfauna aus der Araxesenge bei
Djoulfa in Armenien. 126 p. Alfred HOlder,
Wien.
Bando, Y. (1956): Geology of the Fujisawa
District, Higashiiwai gun, Iwate Prefecture(Graduation thesis, Tohoku Univ., MS,in Japanese).
- - (1975): On some Permian Medlicottidae
from the Toyoma Formation in the Kitakami Massif. Mem. Fac. Educ., Kagawa Univ.,
Pt. II, vol. 25, p. 67-81.
- - (1979): Upper Permian and Lower Triassic
ammonoids from Abadeh, Central Iran.
Ibid., vol. 29, p. 103-138.
Besairie, H. (1936): Recherches geologiques aMadagascar, Premiere suite; La geologie duNord-ouest, Chap. 3, Les fossiles. Acad.
Malgache Mem., fasc. 21, p. 105-207.
Chao, K. (1965): The Permian ammonoidbearing formations of South China. Scientia
Sinica, vol. 14, p. 1813-1825.
Diener, C. (1903): Permian fossils of the Central
Himalayas. Mem. Geol. Surv. India, Palae-

Table 9. Measurements in mm [Paratirolites ? sp.]

W/H

U/D

U

HID

16?

17

0.35?

0.37?

14?

14

0.35?

0.35?

D

H

TY-820446?

TY-8203

40?

W

46

Masayuki EHIRO and Yuji BANDa

onto Indica, ser. 15, vol. 1, pt. 5, p. 1-204.
__ (1921): Ammonoidea Permiana. Fossilium
Catalogus, I. Animalia, pars 14, 36 p.
Ehiro, M. (1979): Geology of Fujisawa-cho.
In the Editorial Committee for the historyof Fujisawa-cho, The History of Fujisawacho, vol. 1, p. 661-690. Fujisawa-cho,Higashiiwai-gun, Iwate Prefecture (in Japanese).
__ and Bando, Y. (1978): Discovery of Xenodiscus from the Permian Toyoma Formation of southern Kitakami Massif. Jour.
Geol. Soc. Japan, vol. 84, p. 37-38 (inJapanese).
and - - (1980): Discovery of Rotodiscoceras from the Upper Permian of southern
Kitakami Massif and its significance. Ibid.,
vol. 86, p. 484-486 (in Japanese).
Fatmi, A. N. (1973): Lithostratigraphic units of
the Kohat-Potwar Province, Indus Basin,
Pakistan. Mem. Geol. Surv. Pakistan, vol.
10, p. 1-80.
Furnish, W. M. (1966): Ammonoids of the Upper
Permian Cyclolobus-zone. Abhandl. N. Jahrb.
Geol. Plaont., vol. 125, p. 265-296.
--and Glenister, B. F. (1970): Permian ammonoid Cyclolobus from the Salt Range,
West Pakistan. In Kummel, B. and Teichert,
C. (eds.), Stratigraphic boundary problems:Permian and Triassic of West Pakistan.
Kansas Univ. Geol. Dept., Spec. Publ., 4, p.
153-175.
- - , Glenister, B. F., Nakazawa, K. and Kapoor,
H. M. (1973): Permian ammonoid Cyclolobus from the Zewan Formation, Guryul
Ravine, Kashmir. Science, vol. 180, p. 188-

190.
Hayasaka, I. (1963): Some Permian fossils fromSouthern. Kitakami. III. Proc. Japan Acad.,vol. 39, p. 594-599.
Iranian-Japanese Research Group (1981): The
Permian and the Lower Triassic Systems in
Abadeh Region, Central Iran. Mem. Fae.
Sci., Kyoto Univ., ser. Geol. Mineral., vol.
47, p. 61-133.
Ishii, K., Okimura, Y. and Nakazawa, K. (1975):
On the Genus Colaniella and its biostratigraphic significance. Jour. Geosci. Osaka
City Univ., vol. 19, p. 107-138.
Koizumi, H. (1975): Palaeozoic Cephalopods ofJapan. 149 p. Teiseki Bunko, Chiba (inJapanese).
Kon'no, E. (1973): New species of Pleuromeia
and Neocalamites from the Upper Scythian
Bed in the Kitakami Massif, Japan - with abrief note on some Equisetacean Plantsfrom the Upper Permian Bed in the Kitakami Massif. Sci. Rep. Tohoku Univ., ser.
2, vol. 43, p. 99-115.
Kummel, B. (1970): Ammonoids from the
Kathwai Member, Mianwali Formation,
Salt Range, West Pakistan. In Kummel, B.
and Teichert, C. (eds.), Stratigraphic boundary problems: Permian and Triassic of West
Pakistan. Kansas Univ. Geol. Dept., Spec.
Publ., 4, p. 177-192.
Mabuti, S. (1932): Stratigraphy of the Paleozoic
rocks of the Tabashine-yama Massif, southern part of the Kitakami Massif (Graduation
thesis, Tohoku Univ., MS, in Japanese).
- - (1935): On the occurrence of Stacheocerasin tht! Kitakami mountainland, Northeast

Explanation of Plate 6
Figs. 1-7. Medlicottia kitakamiensis Bando and Ehiro, sp. nov . . . . . . . . . . . . . . . . . . . p. 39
1. GLKU-TY-81 01 , x 1; 2. GLKU-TY-8102, x 1; 3. GLKU-TY-8105, xl; 4. GLKU-TY8001 (Holotype), xl; 5. GLKU-TY-8106, xl; 6. GLKU-TY-8103, x 0.8; 7. GLKU-TY8107, x 1.4.
Fig. 8.
Eumedlicottia sp . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . p. 40
GLKU-TY-8005, lateral view of shell fragment, x 1.8.
The illustrated specimens in Figs. 1, 2, 6 and 7 were collected from the-uppermost part of
the Senmatsu Formation near Nagasakiyama, Senmatsu, Fujisawa-cho, Higashiiwai-gun, Iwate
Prefecture. The specimens of Figs. 3 and 5 from the uppermost part of the Senmatsu Formationnear Takizawa-toge, southwestern part of Magome, Motoyoshi-cho, Motoyoshi-gun, Miyagi Prefecture. The specimens illustrated in Figs. 4 and 8 from the lower horizon of the upper part of theSenmatsu Formation at Iwanosawa, Senmatsu, Fujisawa-cho, Higashiiwai-gun, Iwate Prefecture.

EHIRO and BANDO: Late Permian Ammonoids from Kitakami

Plate 63

5

792. Late Permian Ammonoids from Kitakami
Honsyu, Japan. Saito Ho-on Kai Mus. Res.
Bull., no. 6, p. 143-149.
Miller, A. K. and Furnish, W. M. (1940): Permianammonoids of the Guadalupe Mountainregion and adjacent areas. Geol. Soc. America
Spec. Paper, no. 26,242 p.
Minato, M., Kato, M., Nakamura, K., Hasegawa,Y., Choi, D. R. and Tazawa, J. (1978):
Biostratigraphy and correlation of thePermian of Japan. Jour. Fac. Sci., Hokkaido
Univ., ser. 4, vol. 18, p. 11-47.
von Moller, V. (1879): Uever die bathrologishe
StellungdesJungerenpaliiozoischen
Schichtensystems von Djoulfa in Armenien.
Neues. Jb. Miner. Geol. Paliiont., p. 225243.
Murata, M. (1967): Some Permian Conulariidae
from the Kitakami Massif, Northeast Japan.
Saito Ho-on Kai Mus. Res. Bull., no. 36,
p.9-17.
- - (1969): Molluscan fauna of the Toyoma
Formation (Late Permian). Ibid., no. 38, p.
1-22.
--and Bando, Y. (1975): Discovery of Late
Permian Araxoceras from the Toyoma Formation in the Kitakami Massif, Northeast
Japan. Trans. Proc. Palaeont. Soc. Japan,
N. S., no. 97, p. 22-31.
and Shimoyama, S. (1979): Stratigraphynear the Permian-Triassic boundary and the
Pre-Triassic unconformity in the Kitakami
Massif, Northeast Japan. Kumamoto Jour.
Sci., Geol., vol. 11, p. 11-31 (in Japanesewith English abstract).
Onuki, Y. (1956): Geology of the Kitakami
Massif. In Iwate Prefecture (ed.), Explanatory text of geologic map (scale 1: 1 00,000)
of Iwate Prefecture. 189 p. Sasaki Print.
Publi. Co. Ltd., Sendai (in Japanese).
-and Bando, Y. (1959): On the Inai Group of
the Lower and Mi(idle Triassic System (Stratigraphical and Palaeontological studies of
the Triassic System in the Kitakami Massif,
northeastern Japan: 3). Contr. Inst. Geol.
Palaeont., Tohoku Univ., no. 50, p. 1-69
(in Japanese with English abstract).
Rostovtsev, K. O. and Azaryan, N. R. (1973):
The Permian-Triassic boundary in Transcaucasia. In Logan, A. and Hills, L. V.
(eds.), The Permain and Triassic Systems
and their mutual boundary. Mem. Canad.

47

Soc. Petrol. Geol., no. 2, p. 89-99.
Ruzhentsev, V. E. (1959): Classification of theSuperfamily Otocerataceae. Paleont. Zhurnal,
no. 2, p. 56-67 (in Russian).
(1963): New data about the Family Araxoceratidae. Ibid., no. 3, p. 56-64 (in Russian).
-and Sarycheva, T. G. (eds.) (1965): Development and change of marine organisms at
the Palaeozoic-Mesozoic boundary. Trudy
Paleont. Inst., Acad. Nauk SSSR, no. 108,
p. 1-312 (in Russian).
Smith, J. P. (1927): Permian ammonoids ofTimor. Jaarboek. v. h. Mijnwezen in Ned.Indiii, Verhandl. I, p. 1-58.
Spinosa, C., Furnish, W. M. and Glenister, B. F.
(1975): The Xenodiscidae, Permian ceratitoid ammonoids. Jour. Paleont., vo. 49, p.
239-283.
Spath, L. F. (1934): The Ammonoidea of theTrias (1); Catalogue of the Fossil Cephalopoda in the British Museum (Nat. Hist.),Pt. 4, p. 1-521.
Stepanov, D. L., Golshani, F. and Stocklin, J.
(1969): Upper Permian and Permian-Triassic
boundary in North Iran. Rept. Geol. Surv.
Iran, no. 12, p. 1-72.
Taraz, H. (1974): Geology of the Surmaq-Deh
Bid Area, Abadeh Region, Central Iran.
Ibid., no. 37, p. 1-148.
Tazawa, J. (1975): Uppermost Permian fossils
from the Southern Kitakami Mountains,Northeast Japan. Jour. Geol. Soc. Japan,
vol. 81, p. 629--640.
Teichert, C., Kummel, B. and Sweet, W. (1973):
Permian-Triassic Strata, Kuh-e-Ali Bashi,Northwestern Iran. Bull. Mus. Compo Zool.,
vol. 145, p. 359-472.
Tozer, E. T. (1969): Xenodiscacean ammonoids
and their bearing on the discrimination of
the Permo-Triassic boundary. Geol. Mag.,
vol. 106, p. 348-361.
--(1979): The significance of the ammonoids
Paratirolites and Otoceras in correlating thePermian-Triassic boundary beds of Iran and
the People's Republic China. Canad. Jour.
Earth Sci., vol. 16, p. 1524-1532.
--(1981): Triassic Ammonoidea: Classification, evolution and relationship with Permianand Jurassic forms. In House, M. R. and
Senior, J. R. (eds.), The Ammonoidea, p.

48

Masayuki EHIRO and Yuji BANDO

65-100. Academic Press, London.
Waagen, W. (1872): On the occurrence of Ammonites, associated with Ceratites, andGoniatites in the Carboniferous depositsof the Salt Range. Mem. Geol. Surv. India,
vol. 9, p. 351-358.
- - (1879-1880): Salt Range fossils: Productus
Limestone fossils. Mem. Geol. Surv. India,
Palaeont. Indica, ser. 13, vol. 1, pts. 1, 2;
p. 1-72,73-183.
Working Group on the Permian-Triassic Systems(1975): Stratigraphy near the PermianTriassic boundary in Japan and its correlation. Jour. Geol. Soc. Japan, vol. 81, p.
165-184 (in Japanese with English abstract).
Zhao, J. (1980): Origin, classification, evolution
and distribution of the Family Cyclolobidae.
Acta Palaeont. Sinica, vol. 19, p. 79--90(in Chinese with English summary).
__ , Liang, X. and Zheng, Z. (1978): Late
Permian Cephalopods of South China.
Palaeont. Sinica, no. 154,194 p. (in Chinesewith English summary).

Fujisawa I[#V\, Fukkoshi f.l\l,~, Higashifukakaya lh1X';'. Hiraiso T-~. Isatomae fJfl[!_Ijli. Ishihama liiV,. Iwaizaki ·i:-JI',11.t'. Iwanosawa 'r':-V')iR. K<lnokura nt-n-, Kesennuma )<\1llli{l. Kiridoshi
Ljj)il1.Kobuchi 'HI::I. Konakogi t)} jl\:~,. Kuromori ).I.\lj1~. Magome ,1Mrt1. Matsukozawa r.L: J-iR.
Motoy'oshi ~"I,--, Mt. Nabekoshi (N<lbekoshiyama) Jl,',\,I~IiI. Nagahala Jd:llI. Nagasakiyama Jil~.;fIii. Nishikori $lili'it Okago ),iifi, Osawa kv~. Sabmolozawa j-U~in, Senmatsu T-t:. Shinden%lilll. Suenosa,ki -1~V')I~,;f, Takizawa il~iI\. Tanoura 11IV')i1Il. Toyoma Y:U~. Unazawa :{ir,V{,
Utatsu ;lkift. Yahagi ;'J'F. Yamazaki lilill~f, Yamashita Jlff. Yonekawa *)11

Explanation of Plate 7
Figs. la--c.
Araxoceras cf. A. rotoides Ruzhentsev . . . . . . . . . . . . . . . . . . . . . . . . . . . p. 40
GLKU-TY-8301, lateral (a), ventral (b) and front (c) views, X 1.2.
Figs. 2a, b. Araxoceras sp . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . , . . . . . . . . . . . . p. 41
GLKU-TY-8302, lateral (a) and front (b) views, X 1.2.
Figs. 3a-c. Prototoceras japonicum Bando and Ehiro, sp. nov. .. . . . . . . . . . . . . . . .. p. 42
FLKU-TY-8201, lateral (a, b) and ventral (c) views, X 1.9.
Figs. 4a, b. Prototoceras sp. A . . . . . . . . . . . . . . , . . . .. . . . . . . . . . _ . . . . . . . . . p. 42
GLKU-TY-8303, lateral (a) and ventral (b) views, X 2.
Figs. 5a, b. Prototoceras sp. B .. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
. . p. 43
GLKU-TY-8304, lateral (a) and ventral (b) views, X 2.
Figs. 6a, b. Prototoceras sp. C . . . . . . . . . . . . , . , . . . . . . . . . . . . . . . . . . . . . . . . . p. 43
GLKU-TY-8305, lateral (a) and ventral (b) views, X 1.8.
The specimens illustrated in Figs. 1-6 were collected from the lower part of the Suenosaki
Formation at eastern coast of Ishihama, Utatsu-cho, Motoyoshi-gun, Miyagi Prefecture.
Figs. 7, 8. Paratirolites ? sp . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . p. 45
7. GLKU-TY-8203, external mold, X 1; 8. GLKU-TY-8204, external mold, X 0.8.
The specimens in Figs. 7 and 8 were collected from the upper horizon of the lower partof the Senmatsu Formation near Kiridoshi, Senmatsu, Fujisawa-cho, Higashiiwai-gun, Iwate
Prefecture.
Figs. 9.
Xenodiscus cf. X. carbonarius Waagen . . . . . . . . . . . . . . . . . . . . . . . . . . . . . p. 43
GLKU-TY-7701,lateral view, xL
The specimen in Fig. 9 from the lowermost part of the Okago Formation at Yahagi, Kamiokago, Fujisawa-cho, Higashiiwai-gun, Iwate Prefecture.

EHIRO and BANDO: Late Permian Ammonoids trom Kitakami

Plate 7

792. Late Permian Ammonoids from Kitakami
mffll~U:UIJilliliH&JW~ It.- j,~c 7 /' -r: -)-1

I· : rHffjl~tJ::ILIJillO)il!kr4t;f-,; J: cJ')-:ifgJMxl'::'7.r;(li-,J-

QJ::t;jl~/l- J.. *~a::¥:;J;ICO) 7 /' -r: T 1 I- 7 .~ - TI'::' <b c -::it:, rrHifl~tJ::, r '7/'7, :z -:h -/7,

1 '7 /';t.; J: U'11'Ili!miiBO)J::f,jl~/L- .!<,f"IRg:O)Mj:t'd:'~fiii Lt-:o 9 ),1l13M[0) 7 /' -T: T 1 I- 'd:'~cjr\l( L.
'CO) t~tvc 1 ~rl+ (ParatiroJiticiae) ;f-,; J: U' 2 ifrfiJl: (Medlicoltia kitalwmiensis ;t·o J: C)' Pro-

totoceras jajJonicum) 'd:'jJ~lIlJ L t-:oft::¥:mtdG:-rml(i Araxoceras d. A. roloides ;t.; J: U' Prololoceras japon/cum 0) J: 5 fc;( It.- 7 -r WI 7 /' -T: T 1 I- 'd:' j!i?:-t Q 0 1:11 {'IjIll , ~J 0) Araxoceras d. A. Iliangsiense (7) ~1:U (Murata and Bando, 1975) 'd:' iOh-itc 'J§'i:... Q c, lVK;J;ICrh11;f-,; J: U'11,f(flli, r '7 /'7-. :z -:h -/ 7-\"'1 '7 /' 0) ~·/t.- 7 71~r ;t.; J: U' rl'II~j.H{jjIO) Jl:I.~O"fJlWIC X;jJ:t ~ nQo 1VK;J;ICJ:.:f\jHi, Paralirolites '! sp. 0) i2iHL\I.::. J: I), r '7 /,7, :z - 7} -/7 -\",1 '7 /,0) I: '7 -/ i' j, 11J;\';t.; J: U'IIIIJiIIH j~jlO) K!Jfl
llM'vcX;jJ:t ~J1, Q "Jtjg1~:Il;i:t~\,7k}1\ IIJZ • .!fJU1H,jJ(~'049

Trans. Proc. Palaeont. Soc. Japan, N.S., No. 137, pp. 50-63, April 30, 1985

793. OSTRACODA FROM THE PLIOCENE ANANAI FORMATION,SHIKOKU, JAPAN - FAUNAL ANALYSES -*KUNIHIRO ISHIZAKI
Institute of Geology and Paleontology, Faculty of Science, Tohoku University,
Sendai980,JapanandYOSHIHIRO TANIMURA
Department of Paleontology, National Science Museum
Hyakunin-cho, Shinjuku-ku, Tokyo 160, Japan

Abstract.
In a previous study of 35 samples collected from the Pliocene
Ananai Formation which is distributed sporadically along the southeastern coastof Shikoku, Japan, 79 ostracode species coming under 42 genera were recognized(Ishizaki, 1983, Table 1). Q-mode principal components factor analysis performedon an initial data matrix in this table shows that ostracode faunas in the formation
are characterized fundamentally by four varimax assemblages representing open
shelf, Kuroshio, bay mouth, and coastal current habitants.
Principal components factor analysis on the frequency distribution of grain
size and the relative abundance of different kinds of grains in different size fractions, both of which resulted from the grain-size analysis of sediments, indicatesfour distinct factors; tranquil waters, preservation of the piled sediments, andsupplies of biogenic and terrestrial materials.
The correlation coefficients calculated among the factor loadings for the
sediment and ostracode data, species diversity, and equitability suggest that structural indices such as species diversity and equitability have hardly any significant
relation to sedimentological factors but are inherent in respective varimax assemblages.
The second varimax assemblage shows clear geographic differences in its
species diversity, equitability, and number of species, suggesting the existence ofa gradient in the effect of the then prevailing Kuroshio Current. The temporal
shift in the same parameters in the Ono section may also be equated to the secularvicissitudes of water conditions.

Introduction

uted sporadically in several isolated patches along
the southeastern coast of Shikoku in Southwest
Japan (Ishizaki, 1983, text-fig. 1). This formation yields various groups of fossils in abundance,
including foraminifers, which were studied by
Katto et ai. (1953) and Kurihara (1968) in order

The Pliocene Ananai Formation, one of thethree units of the Tonohama Group, is distrib*Received Feb. 25, ,1984; read June 19, 1983
at Utsunomiya.
50

793. Ostracode Analyses in the Ananai Formation

to deduce geographic variations in the depositional environments of the formation.
This formation also generally yields fossil
ostracodes in great abundance. These werestudied by Ishizaki (1983), who gave full descriptions of 11 previously unnamed species
together with a list showing the occurrence of
all the discriminated species by samples (Table1). The purpose of the present study is theanalysis of fossil ostracode faunas from those
30 samples which yielded 200-odd specimens
each by using principal components factor
analysis in order to discriminate feasible varimax
assemblages based on factor scores, and to
determine the distribution of respective assemblages in terms of factor loadings. By doing this
we hope to provide a better understanding of
secular and geographic variations in the depositional environments of the Ananai Formation.
The structure of the assemblages of various
groups has been examined by many authors inorder to set down clues to paleoenvironmental
analyses. Most of these authors have suggested
that the structure of assemblages tends to become more complex in a stable and consistentenvironment. Buzas and Gibson (1969) concurred with this opinion; however, in their later
report, Gibson and Buzas (1973) propoundeda different opinion based upon their study ofboth Recent foraminifers from the Arctic region
through to the Gulf of Mexico and fossil ones
from the Miocene. The time-stability hypotheses could not fully explain the species diversity
found in these samples. Alternatively, theysuggested that each environmental regime has its
own carrying capacity which seems to be attained relatively rapidly.
In this study, the structure of the ostracodeassemblages defined by varimax factor scores
higher than 1.28, which were obtained from theprincipal components factor analysis set forth
by Imbrie and Purdy (1962), was examined byusing the Shannon-Weaver's information function as somewhat expanded by Buzas and Gibson(1969). We also compared geographical andtemporal changes in the structure of the varimax
assemblages with lithologic data which may

51

indicate physical aspects of the depositional
environments.
Careful examination reveals that the recognition of relevant assemblages per se is a requisite
for applying faunal dynamics to fossil assemblages and for assessing environmental conditionsin the geologic past.
Faunal Analysis
In this study, 30 of the 35 samples in Table
1 of Ishizaki (1983) were studied. Each ofthese 30 samples yielded 200-odd ostracodespecimens. Additional information concerning
the samples is given in that article. The 74
ostracode species selected for this study, withthe exception of Ambocythere japonica Ishizaki, Buntonia parascorta Ishizaki, Echinocythereis? bradyformis Ishizaki, Hemicytherurakajiyamai Hanai, and Kobayashiina hyalinosa
Hanai from the same table, are those which
are represented by ten or more specimens amongthe 35 samples. The number of specimens refers
to the larger number of the two valves.
Analyses of the ostracode data set consistingof 30 columns and 74 rows were made for the
Q-mode technique by using the principal components factor analysis set down by Imbrie andTable 1.

Summary of principal components
factor analysis on the ostracode data.

Factor

Eigenvalue

Cum. perc.

1

21. 741

72.47

2

2.059

79.33

3

1.083

82.94

4

0.971

86.18

5

0.899

89.18

6

0.574

91.10

7

0.472

92.67

8

0.275

93.59

9

0.252

94.43

10

0.221

95.17

Kunihiro ]SHIZAKI and Yoshihiro TANIMURA

52

Table 2.

Varimax scores of the first four
factors for ostracode species.

Actinocythel'eis kisarazu.ensis
goujo>!iAl'giUoecia ho>!aii
AurHa cymba
Auri~a hataii
11urila l11unechi1ca.£
AurHa tosaensis
Aurila u.l'a'louchiensis
BairdoppHata sp,
Bicornucythere bisanensia

0.531 -0.059 0.011 -0.142
0.008 -0.218 -0.026 -0.352-0.069 -0.353 -0.355 0.086
0.683 -0.082 -1.106 -2.527
0.397 -0.448 1.594 0.275
0.310 0.907 3.936 -0.768
0,146 -0.136 0.367 -0.875
0.787 -0.196 1.013 -0.616-0.115 -0.023 -0.156 0.210-0.498 0.102 4.471 0.684
Brad~eya a~batrossia
0,824 -0.087 -0.161 0.116
Brad~eya nuda
2.226 -0.585 -1.122 -0.794
Buntonia honaii
1.182 -0.049 -0.352 0.147
Buntonia SCOl'ta
0.615 -0.167 -0.378 0.118
Bantonia u-carinaca
0.024 0.489 0.402 0.254
8ythoceratina dip~eura-0.237 -0.052 0.601 -0,078
Bythoceratina hanaii-0.221 0.076 0.529 0.060
Bythoceratina cf. m·ientGUs
0.017 -0.123 0.310 0.140
Ca~Ustocyth,,'e a~ata-0.381 -0.242 -0.173 -0.316
CaUistocytherc ana"aie"sis-0.357 -0.308 -1.165 0.208
CaUistocythere japonica-0.188 -0.09l -0.088 0.066
CaUiatocythere kattoi-0.147 1.377 -1.095 -0.610
CaUistocythere ovata
0.155 -0.048 0.193 0.016
CaUistocythere u>!data
0.222 -0.248 1.034 -0.073
CaUistocythere sp.
0.090 -0.071 -0.046 0.085
Coquimba iBhizakii
0.272 -0.067 0.396 0.125
Comu.coqu.imba tosae'lsis
1.207 0.340 -0.100 -0.270
Cythere ~utea omotenippo>!ica
0.182 -0.018 0.065 0.201
CythereUa japanica
0.665 -0.031 -0.240 0.194
CythereUoidea hanaii-0.072 0.131 1.119 0.476
CythereUoidea Babahebsis
0.762 -0.108 -0.443 -0.059
CythereUoidea d. yake>!ae>!sia -0.328 -0.527 0.030 0.082
Cytheropteron miurense
1.178 -0.135 1.551 -0.116
Cytheropteron rhombea-0.014 -0.481 -0.856 -0.903
Cytheropteron uchioi
6.015 -0.126 -1.655 0.720
Doratocythere tailJa>!ensia-0.045 -0.006 -0.249 -1.068
Hemicytherura cava
0.295 -0.073 -0.161 -0.260
Hemicytherura cuneata
0.622 -0.575 0.601 -0.412
Hemicytherura mdiata
0.025 -0.130 -0.077 -0.220
HirButocythere? ha'laii-0.057 -0.041 -0.356 0.075
JugoBocythereiB sp.
1.578 -0.128 -0.092 -0.615
Krithe honoii
0.041 -0.178 -0.126 0.484
Krithe producta
0.170 -0.090 -0.543 0.067
Lizouria nipponica
0.663 -0.197 -0.209 0.201
Lozoconcho hottorii-0.212 0.354 0.266 0.226
Lozoconcha japonica
0.125 -0.162 0.226 0.012
Lozoconcha kattoi
2.257 -0.154 0.578 -0.908
Lozoconcha optima-0.331 -0.276 0.749 -0.344
Lo:roconcha sinensis
0.819 2.593 1.328 0.907
Lozocornicu~um mutauense
0.060 -0.031 0.394 -0.432
Macrocypria decora
0.108 -0.071 -0.101 -0.342
MunseyeUa oborozukiyo
1.202 0.749 1.492 0.639
MmaeyeUa japonica
0.219 -0.043 0.176 -0.202
MutHua nodu~oBum-0.018 -0.009 -0.137 -0.415
Neonesidea viUosa-0.764 -1.469 1.506 -5.537
Nipponocythere bicarinata
0.291 -0.051 0.619 0.406
PaijenborcheUa iocosa
0.416 -0.091 -0.414 -0.182
PaijenborcheHa miu}tennis
0.964 -0.272 0.341 0.169
l'aijenborcheUa triangu~aris
0.043 0.104 0.890 -0.025
Paracytheridea cf. bosoensis
0.023 0.045 0.472 -0.154
Paracytheridea neo~ongica"data 0.616 -0.167 0.445 0.092
ParakritheZZa pseudadonta-0.092 0.320 0.737 0.059
I'o"tocythere japonica
0.300 7.563 -0.519 -1.906
Pontocythere miurellsis
0.072 -0.045 0.717 -0.048
Pseudoaul·ila japonica
0.196 0.001 0.358 -0.430
Pterygocythereis scalaris
0.899 -0.156 0.377 0.298
Schizocythere kiBhinouyei
2.378 -0.349 2.427 2.541
Semicytherl<ra hanaii
0.105 -0.089 0.097 0.033
Semicytherura henryhoIJei
0.214 -0.285 0.660 -0.682
Trachy~eberi. ~ungkengen.is1.879 -1.002 0.490 -3.417
Trachy~eberis? toaaonais
0.369 -0.314 0.460 -1.585
XeBto~oberis ha'laii
0.602 0.178 0.582 -0.689
Xe.to~eberis sagamiensis
0.458 -0.118 0.484 -0.876
Xesto~eberia sp.
0.062 0.003 0.323 -0.570

A~ocopocythere

Purdy (1962) for an analysis of modem Bahamian carbonate sediments. A summary of theresults obtained from the analysis shows thatthe first four factors account for more than
86% of the total variance (Table 1). Table 2
shows the calculated scores of the first four
factors for every ostracode species. Species
having factor scores of 1.28 or more are within
the first 10% of the standardized normal distribution in relation to their contributions to
the respective factors. Therefore, this value(1.28) may be regarded as a critical value ingrouping varimax assemblages, whose frequency
distributions may be equated to the distributiOIisof the factor loadings. By using this procedure,
the following varimax assemblages were discriminated:
The first varimax assemblage;
Bradleya nuda Benson
Cytheropteron uchioi Hanai
Jugosocythereis sp.
Loxoconcha kattoi Ishizaki
Schizocythere kishinouyei (Kajiyama)
Trachyleberis lungkangensis Hu and Chen,the second varimax assemblage;
Callistocythere kattoi Ishizaki
Loxoconcha sinensis Brady
Pontocythere japonica (Hanai)
the third varimax assemblage;
Aurila hataii Ishizaki
Aurila munechikai Ishizaki
Bicornucythere bisanensis (Okubo)
Cytheropteron miurense Hanai
Loxoconcha sinensis Brady
Munseyella oborozukiyo Yajima
Neonesidea villosa (Brady)
Schizocythere k'ishinouyei (Kajiyama), anda fourth varimax assemblage;
Schizocythere kishinouyei (Kajiyama).
The modem distributions of the first varimax
assemblage is as follows: Bradleya nuda is distributed in the northern section; Cytheropteronuchioi in the entire area of the studied shelf ofthe East China Sea, except for one station(Ishizaki, 1981); Loxoconcha kattoi only outside of Uranouchi Bay, Kochi Prefecture (Ishizaki, 1968); Schizocythere kishinouyei in the53793. Ostracode Analyses in the Ananai Formation

southern section, which is affected by southward-flowing countercurrents from the Yellow
Sea; and Trachyleberis lungkangensis in a wider
area than S. kishinouyei, extending further
north, in the East China Sea (Ishizaki, 1981).
An environmental regime common to these
species is likely to be an open shelf area.
Of the second varimax assemblage, the modem distribution of Callis to cy there kattoi is not
yet known because it was first recorded fromthe Ananai Formation (Ishizaki, 1983). Loxoconcha sinensis is distributed widely in the
shelf area of the East China Sea, increasing
toward the outer part where the effect of theKuroshio Current is stronger (Ishizaki, 1981).
On the other hand, Pontocythere japonica
does not significantly occur in the East China
Sea in terms of the terminology set down by
Ishizaki (1981); it does not occur at all in the
Nakanoumi Estuary, Shimane Prefecture (Ishizaki, 1969), nor in Aomori Bay (Ishizaki, 1971).
It does occur significantly, however, in thearea ranging from the outer half to the mouthof Uranouchi Bay, Kochi Prefecture (Ishizaki,1968), and has also been reported by Frydl(1982) to occur significantly in Tateyama Bay,
Chiba Prefecture. Judging from the known
modem distribution of the above two species,
this varimax assemblage may represent, to acertain extent, the effect of the Kuroshio Cur-rent.
Of the third varimax assemblage, Aurila
hataii and Aurila munechikai are both distributedin the area ranging from the bay mouth to outside Uranouchi Bay, Kochi Prefecture (Ishizaki,1968), and Bicornucythere bisanensis characteristically occurs in great abundance in the bay
area. Cytheropteron miurense has been reported
by Frydl (1982) to occur significantly in Tateyama Bay, Chiba Prefecture. Neonesidea villosa
occurs in abundance in the area which is affected, to a certain extent, by the Kuroshio
Current in the East China Sea (Ish izaki, 1981).
The modem distribution of the first four species
shows that this varimax assemblage is indicativeof the bay mouth regime.
The known distribution of Schizocythere
kishinouyei suggests that the fourth varimax
assemblage is an element which is, to a certain
extent, subject to the influence of a coastal
current.
It is generally assumed that an inspection of
the factor loadings in a cross-section reveals
the geographical and temporal distribution of
those varimax assemblages in the Ananai Formation.
To test the significance of the factor loadings
computed on 74 species, the value of a/aSE wasexamined if it is greater than 2.00 (the 5 percent
level in case of 2-sided test, Sokal and Sneath,

loki

Ono
L4

SempukuTonohama

L3

L2

HI
H2
H3
H4

K2 Open shelf
K3
K4

.5
K6

.7
K8
K9

GI
G2
G3
G4
G5
G6
G7
G8

KID

.,
Text-fig. 1. Geologic section of the Ananai Formation, with the distributions of significant
highest loadings of each of the first three factors (open shelf, bay mouth, and Kuroshio Currentrelated assemblages), and that of higher loadings of all the first three factors (mixed assemblage).

Kunihiro !SHIZAKI and Yoshihiro TANIMURA

54

Table 3.

1963, p. 313-315). Examination shows thata factor loading higher than 0.052 is significant
at that level. All the samples from the Ananai
Formation bear significant loadings of all thefirst three factors. Therefore, in this study, theloadings of each factor were classified into threeclasses; highest, higher, and significant, using
critical values of 0.052 (unity), 0.156 (threetimes unity), and 0.468 (nine times unity).
Four environmental categories were classified
in a section, which cuts through all five localities,
on the basis of the highest and higher loadingsof the first three factors (Text-fig. 1). These
categories are open shelf, bay mouth, Kuroshio
Current-affecting, and mixed faunas regimes.
The first three regimes were defined by thehighest loadings of any of the first three factors,
and the last one by the combination of thehigher loadings of all the first three factors.
The distributions of these regimes in the section(Text-fig. 1) delineate both the vertical andlateral features of the Ananai Formation in relation to the fossil ostracode faunas contained.
This figure clearly shows that the bay mouth
regime prevailed in the Ananai area in an earlier
period of the deposition time of the Ananai

Varimax loadings of the first four
factors calculated, from the ostracodedata.

Factors

4

3

2

1
Samples

P 1
P 2
P 3
L 4
L 3
L 2
L 1
M1
K1
K2
K3
K4
K5
K6
K7
K8
K9
KlO
Kll
H1
H2
H3
H4
I 1
J 1
G2
G3
G4
G5
G6

0.3478 0.4354
0.2942 0.2635
0.3289 0.1914
0.2085 0.8531
0.1215 0.9326
0.2368 0.6635
0.3277 0.3144
0.4122 0.3308
0.6352 0.2472
0.5351 0.2956
0.5573 0.3453
0.2512 0.1664
0.5286 0.2362
0.8324 0.1967
0.6660 0.1484
0.6855 0.1935
0.8697 0.2585
0.4348 0.2973
0.7952 0.2225
0.2907 0.5130
0.3442 0.4851
0.4380 0.4895
0.2782 0.5301
0.3733 0.7179
0.3625 0.6347
0.3314 0.4016
0.3573 0.2570
0.3676 0.3846
0.3184 0.4970
0.2514 0.3975

0.6543 0.0518
0.7664 -0.3300
0.7162 -0.4665
0.2634 -0.1066
0.0844 -0.1808
0.3064 -0.4000
0.4748 -0.3117
0.3843 -0.3255
0.2436 -0.4506
0.3279 -0.3922
0.2962 -0.5495
0.2147 -0.8582
0.2422 -0.5880
0.1481 -0.2928
0.2138 -0.3862
0.3871 -0.2827
0.2086 -0.1247
0.2919 -0.4193
0.2738 -0.0832
0.1285 -0.1682
0.2181 -0.3614
0.1097 -0.3656
0.3246 -0.2561
0.2824 -0.1574
0.2055 -0.2097
0.2967 -0.3215
0.2538 -0.4835
0.2812 -0.1979
0.1785 -0.1703
0.2539 -0.1932

Dry-weight percentage of the sediments in the range of coarser than 0 cp to 4.1 cp.
Numerals on the left margin correspond to those plotted in Text·fig. 2.

Table 4.

Sample
PI

P2

P3

L4

L3

L2

11

K1

K2

K3

K4

K5

K6

K7

K8

K9

K10

K11

Size
1)

-0.0.

.01

2)

-1.0.

.33

3)

-1.2.

.15

.11

4)

-1.4.

.20

5)

-1.6.

6)

-1. 8.

7)

-2.0.

8)
9)

.46

.20

.12
1.42

.16

.91

1.08

.16

.55

.16

.16

.25

.84

.13

.54

.19

.16

.24

1.33

.12

.15

.69

.24

.16

.22

2.10

.15

.18

.51,

.40

.41

.20

2.60

.08

.14

.23

.63

.42

.47

.17

2.1,5

.15

.11

.31,

.32

.71

.95

.77

.37

1,.07

.26

.33

.81,

.76

1.29

1.38

1.19

.55

1,.68

.70

.78

1.17

1.02

3.20

1.66

2.08

.82

5.69

1.97

1.1,l

2.33

3.51

2.81

5.92

3.22

3.76

1.96

7.11

7.03

4.64

3.99

6.80

7.91,

6.61

8.80

5.17

6.73

6.05

9.13

8.85

6.79

8.0810.6211.62 10.7511.73

7.98

9.3910.8810.61

.05

.69

.10

.38

.25

.38

.66

.07

.11

.03

.24

.14

.13

.79

.12

.22

.04

.16

.16

.05

.29

.19

.15

.62

.14

.11

.04

.50

.15

.15

.10

.44

.24

.20

.39

.03

.10

.04

.40

.28

.28

.11

.87

.30

.22

.44

.07

.10

.04

.56

.33

.33

.19

.68

.39

.28

.54

.35

.08

-2.2.

.90

1.20

1.20

.1,1,

1.30

1.70

.99

.96

.61

-2.1,.

1.26

1.56

1.56

.63

LSI,

2.52

1.58

1.25

.59

10)

-2.6.

2.10

2.71

2.71

1.04

2.95

1,.23

2.21

2.1,l

1.08

11)

-2.8.

3.50

4.82

1,.82

2.21

5.73

6 36

5.21,

4.20

12)

-3.0.

5.21

6.89

6.89

5.04

9.30

8.22

6.1,9

13)

-3.2.

6.86 10.62 10.62

9.16

11,)

-3.1,.

7.9611.96 11.96 10.81 11.8711.51

9.16 11.5311.02

8.8110.61.108.6511.61 13.0313.1612.2612.95

9.24 11.22 12.61 12.29
9.86 11.3812.6513.13

15)

-3.6.

9.10

9.95

9.9511.8011.92 11.32

7.2011.07

9.1,6 12.6013.3912.36 12.8013.12

16)

-3.8.

9.72

6.25

6.25 11.5010.6510.79

5.77 10.38

8.6212.86 12.02

9.1,211.8812.53

9.2511.1,1,

9.6813.1,7

17)-1,.0.

9.1,8

6.10

6.1010.33

9.5110.52

5.13 10.27

7.7512.32

9.59

6.86

9.1,211.1,6

8.1,211.15

7.7613."0

18)

-4.1.

1,.1,0

3.82

3.82

1,.28

3.35

3.26

3.85

2.80

3.90

3.80

3.07

1,.80

5.16

1,.70

5.35

5.1,0

5.20

6.37

793. Ostracode Analyses in the Ananai Formation
Fonnation and in the loki area near the middle
period. The open shelf regime prevailed in the
Tonohama area for almost the entire period oftime and the Kuroshio Current-affecting regime
in the Ono and Sempuku areas in the earlier
short period as well as in later periods in loki
and Ono areas. The mixed faunas regime dominated the loki area in the earliest period, theTonohama area in the middle period and the
Sempuku area over a long period of time. On theother hand, the coastal current-affecting regime,
represented by almost significant positive fourthfactor loadings, is detected only at P1 in the
Ananai area (Table 3).
Sedimentological Analysis
Of the 30 samples which yielded 200-odd
ostracode specimens, 27 have been kept incollections in the fonn of rock samples. An
analysis of the sedimentology of those samples
was conducted using the automatic grain-size
analyser described by Niitsuma (1971). This
analysis yielded two kinds of data sets; thegrain-size frequency distribution and the relative
frequency of the kinds of grains such as shellfragments, foraminiferal tests, quartz grains,rock fragments, and pellets. The fonner data

HI

H2

H3

H4

11

G2

G3

G4

G5

1)
2)

.21

.05

.25

.16

.07

.12

.01

.13

3)

.07

.04

.24

.45

.23

.01

.04

.10

4)

.10

.13

.28

.45

.18

.01

.04

.04

.17

5)

.17

.26

.23

.36

.20

.01

.08

.04

.16

6)

.22

.17

.27

.47

.24

.01

.07

.06

.15

7)

.53

.48

.37

.57

.46

.07

.08

.15

.12

8)

.44

.83

.36

.57

.79

.20

.26

.43

.16

9)

1.23

1. 84

.66

.80

1.93

.51

.46

1.09

.52

10)

2.79

3.08

1. 4 7

1.45

3.96

1.81

.97

3.06

1.19

11)

4.80

5.28

3.46

2.35

6.81

5.60

3.29

6.85

3.59

12)

7.99

6.79

5.21

3.25

9.13 10.70

13) 10.38

9.01

7.08

4.80 10.98 13.15 11.45

9.98

14) 11.33 10.18

8.57

6.90 11.30 12.96 12.48

10.07

15) 10.91 10.31

9.34

8.50 11.00 10.85 11.79

9.18

8.12 10.70

7.70

16)

9.49

9.10 10.41

9.46 10.11

8.72

9.87

7.51

17)

7.58

8.51 11.10

9.93

9.26

7.37

7.36

6.34

18)

3.04

3.74

5.05

4.18

3.10

3.00

2.55

5.35

55

set consists of the dry-weight percentage of thesediments in each of the 18 fractions ranging
from coarser than 0 ¢ to 4.1 ¢ (Table 4). The
latter data set is the relative frequency of thedifferent kinds of grains in different size fractions ranging from coarser than 0 ¢ to 4 ¢(Table 5).
A summary of the principal components
factor analysis on the grain-size frequency
distribution for the Q-mode technique showsthat the first two factors account for more than
98% of the total variance (Table 6). The plottedvarimax factor scores of the first two factors
demonstrate that the sediments in classes 3.43.6 ¢ (variable 15), 3.6-3.8 ¢ (16), 3.8-4.0 ¢(17), and coarser than 4.1 ¢ (18) are all morethan 1.28 and, being within the first 10%,contribute greatly to the first factor, and thatthe sediments of 2.8-3.0 ¢ (variable 12) and2.6-2.8 ¢ (11) to the second factor (Text-fig.
2). This means that the first factor is indicativeof low sediment-settling velocities or tranquilwater conditions, while the second factor may
possibly represent more cOJ;nplete preservationof the accumulating sediments because thecohesive sediments of such fractions are, in a
Hjulstrom effect, erosive and mobile at rather
lower current velocities than for both finer andcoarser sediments.
This analysis was conducted using 18 variates,
where factor loadings of more than 0.199 are
significant at a level of 5%. Two classes of thesignificant factor loadings may be detected bya value of 0.597, three times the critical valuesof significance. Table 7 gives calculated varimax
loadings of the first and second factors. Thisshows that, except for two (G2 and G4 in the
Sempuku area), all samples bear higher loadings
than 0.597, representing widespread tranquilwater conditions. The loadings of the second
factor are higher than 0.597 only at G4 in the
Sempuku area and lower, but still significant,at scattered horizons in all five areas, signifying
the spasmodically occurring entire preservationof the piled sediments.
A summary of the principal components
factor analysis on the relative frequency of

56

Kunihiro ISHIZAKI and Yoshihiro TANIMURA

Table 5.

"~~a"ple

The relative frequency of the kinds of grains in each of the five fractions in the range ofcoarser than 0 cp to 4 cp.
Numerals in parentheses correspond to those plotted in Text-figs. 3 and 4.
Pl

P2

P3

L4

L3

'L2

Ll

Grains26.70- 06 SF (10)
QZ(1)

16.70

_ 1¢ H(5)

11.70

Kl

K4

K3

K2

K5

K7

K6

62.50 12.50

Kll

100.0
33.00

16.67 40.00 20.00

33.33
5.00 50.00

40.00

37.50 37.50 54.95 66.67 60.00 35.00 95.00 50.00
71.70

KlO

100.0

25.00 45.05

SF(l1)
RF(J5)

K8

5.00

6.2564.52 40.00

50.0087.5026.8853.33 33.33

5.00

6.25

7.53

2.67 23.33
1.43 50.00

40.00 25.02 16.70 31.60 15.40 20.00

H(6)30.00 18.72 50.00 36.80 23.1028.0033.3343.0040.0041.6736.0838.46 76.4760.0061.22 27.78 35.71 18.75-2. PL(9)8.33 20.00 35.00

33.33

QZ(2)

10.00

3.30

3.06

25.0018.72 16.7015.8038.50 20.00 41.67 25.00 15.00 41.6751.5546'.15 17.65 io.oo 25.51 22.22 50.00 18.75

SF(12)RF(J6)

5.00 37.53

p.70

5.30

3.10 12.00

8.33

5.00

3.00

-

,

5.00

5.10 11.11

2.86

6.25

42.10 35.40 35.30 50.00 38.50 76.50 44.44 50.00 70.00 57.89 66.33 61.86 51.55 50.00 54.0040.40 55.56 63.16

QZ(3)_ 301 Fr(7)21.10

7.10 23.50 20.00 22.00

5.9022.22 20.0010.0015.79 15.31 10.31 30.39 20.00 15.00 20.20

SF(J J)

21.00

5.10 11.80 15.00 27.50

5.9022.22 10.00

35.40 23.50

3.50

RF(P)
QZ(~)

60.00

~0.00

_ 401 H(8)

10.00

5.00

SF(J4)

15.00 15.00

Table 6.

10.0010.00

5.26

2.00 25.00

5.30

3.0020.0010.50
1.10

5.40

7.0015.00

2.06

7.0010.0010.00

3.2310.0010.0010.0015.00
5.40

10.00

2.06 10.00

Eigenvalue

7.0015.0020.0025.00

5.0010.00

7.00

Summary of principal components
factor analysis on the grain-size
distribution of sediments.

Factor

1.02

10.10

5.56

75.00 35.00 63.20 80.65 70.0058.0071.0060.0070.00 75.00 57.00 55.00 40.00 70.00 60.61 72.16

25.00 10.00

RF(18)

5.50

5.56 10.53

5.0010.5315.31 15.46 10.31 15.00 20.00 10.10 11.11 21.05

1.00

2.00

2.02

5.0010.00 25.00

5.00

7.07 10.31

7.22

5.00

2.00

2.02

F2

4.0

12

Cum. perc.
3.0

125.433

94.20

2

1.090

98.24

3

0.332

99 .. 47

4

0.088

99.80

5

0.021

99.87

6

0.012

99.92

7

0.007

99.95

shell fragments, foraminiferal tests, rock fragments, quartz grains, and pellets for the Q-mode
technique reveals that the first four factors
account for more than 90% of the total variance(Table 8). The plotted varimax factor scoresof the first four factors show that relatively
coarse-grained shell fragments [0-1 cp (variable11) and 1-2 cp (12)] have varimax factor scoresof more than 1.28 and contribute highly to the

2.0
1.0

-1.0

I I

lIZ!

4.0 FlText-fig. 2. Plot of varimax scores of thefirst versus second factors for the grain-size
distribution. Numerals plotted correspond to
those on the left margin of Table 4.
first factor (Text-fig. 3), and that rock fragments
in classes 0-1 cp (variable 15),1-2 cp (16), and2-3 cp (17) contribute to the fourth factor(Text-fig. 4). This proves that these two factors
are indicative of the supply of biogenic material
consisting mainly of shell fragments and of
terrigenous material composed largely of rock

793. Ostracode Analyses in the Ananai Formation
Table 8.

HI

H2

H3

75.00

H4

II

G2

5.00
5.00 53.00

G4G5

40 .00l5.00 10.53

58.82 20.00

75.00 84.21

15.00 100.0

25.00 20.00 75.00

G3

29.41

5.00 20.00 42.37

57

Summary of principal components
factor analysis on the relative frequency of the kinds of grains.

Factor

Eigenvalue

Cum. perc.

120.45975.78

2

1. 623

81. 79

3

1.372

86.87

4

0.895

90.19

5

0.766

93.03

6

0.605

95.27

7

0.414

96.81

8

0.295

97.90

9

0.214

98.69

10

0.144

99.23

73.00 15.00 15.00 35.00 25.42 20.00 15.38 27.27 17.65
38.4627.27
10.00 15.00 70.00 20.00 U.86 26.00 38.46 36.36 70.59
2.00 10.00

10.00 11.86

4.00

23.00 63.00 45.00 48.00 60.00 63.16 63.16 77.32 72.16
35.00

5.00 20.00 20.00

7.00 10.53 10.53

7.22 10.31

25.00

7.00 25.00 10.00

7.00 10.53

8.42

5.15 10.31

2.U

3.09

10.00 15.00

15.00 10.00

2.U

2.06

63.00 68.00 40.00 74.00 -65.00 85.00 80.00 80.00 80.00
15.00

1.00

3.00

3.00

5.00

5.00

10.00 10.00 20.00

7.00 20.00

3.00'10.00

3.00

2.00

2.00

7.00

5.00

7.00 10.00

15.00

3.00

7.00

F2
3.0

Table 7.

Varimax loadings of the first two
factors calculated from the grain-size
frequency distribution.
Fac cars

'2
lIZ!

1

K1
K2
K3
K4
K5
K6
K7
K8
K9
KlO
Kl1
H1
H2
H3
H4
I 1
G2
G3
G4
G5

I I

5: 1

S::B-i\1

Samples
p 1
P 2
P 3
L 4
L 3
L 2
L 1

2.0

0.82690.5986
0.59840.79400.70070.73350.60210.77650.77950.83790.73120.62830.73790-.7466
0.77190.79070.67630.78290.67320.72580.84800.8942
0.69450.58760.65010.07690.6308o.17l40.22350.2236
0.06390.25460.25350.29820.19180.10460.00370.08850.16280.08990.21170.14280.15270.07570.25800.23580.23710.14120.08430.29630.28030.167l
0.98290.2301

-1. a

,

,

1.0

2.0

3. a

Fl

g
-1.0

3

12

-2.0
Lj
-3. a

Text-fig. 3. Plot of varimax scores of thefirst versus second factors for the relative frequency of the kinds of grains. Numerals plottedcorrespond to those in parentheses in Table 5.

fragments. The meaning of the second andthird factors remains to be interpreted.
Table 9 gives the calculated varimax loadingsof the first four factors. Except for two (P2and H4), all samples are characterized by significant loadings of the first factor at a level of
5% (higher than 0.199), which represents deposi-

Kunihiro !SHIZAKI and Yoshihiro TANIMURA

58
4.0

F4

IS:

2.0

16
17
18

9
-1.0

I I

1.0

2.0

F3

3.0

tional environments where biogenic material
consisting largely of shell fragments has almost
ubiquitously been brought in. In relation to thefourth factor, a significant higher loading is
detected at P2 (Ananai) and a significant lower
loading at P3 (Ananai), K2, K9, Kll (Tonohama) , H2 and 11 (Ono), which signifies thatthe supply of terrigenous material has notreached the entire area, having remained local
and intermittent.
Faunal Structure

Text-fig. 4, Plot of varimax scores of thethird versus fourth factors for the relative frequency of the kinds of grains. Numerals plottedcorrespond to those in parentheses in Table 5.
Table 9.

Varimax loadings of the first four
factors calculated from the relative
frequency of the kinds of grains.

1
P 1
P 2
P 3
L 4
L 3
L 2
L 1
K1
K2
K3
K4
K5
K6
K7
K8
K9
KI0
Kll
H1
H2
H3
H4
I 1
G2
G3
G4
G5

2

0.2306 -0.5298
0.1264 -0.1968
0.2050 -0.5764
0.4282 -0.0922
0.4791 -0.3464
0.5782 -0.2723
0.4103 -0.1791
0.6085 -0.2023
0.4102 -0.3415
0.8307 -0.2159
0.6039 -0.4089
0.3714 -0.7339
0.2831 -0.5284
0.5582 -0.2263
0.7953 -0.0963
0.3104 -0.2846
0.3640 -0.2133
0.3899 -0.3338
0.2767 -0.1834
0.3105 -0.4309
0.8231 -0.2267
0.1142 -0.3308
0.5521 -0.2245
0.3948 -0.5704
0.3339 -0.8056
0.7102 -0.4199
0.7731 -0.4043

3

4

0.3555 0.1736
0.2453 0.8773
0.3916 0.2373
0.7513 0.1127
0.3384 0.1837
0.2250 0.1452
0.2356 0.0673
0.5926 0.1437
0.4373 0.2070
0.2668 0.0764
0.5716 0.1062
0.2963 0.1612
0.3740 0.1225
0.6150 0.1355
0.2915 0.1108
0.7637 0.2129
0.3303 0.0988
0.2587 0.2897
0.8216 0.1112
0.3064 0.2189
0.2715 0.1293
0.8780 0.1819
0.2647 0.3382
0.5680 0.1161
0.2370 0.1302
0.3176 0.0836
0.2570 0.0941

Ostracode diversity and equitability are
expressed by Shannon-Weaver's information
function as somewhat revised by Buzas andGibson (1969). Those two parameters are givenin the following formulae:ef/(s)

H(s)=-p'lnp'zz, andE=-S'

where Pi stands for the proportion of the ith
species in a 'sample, and S the number of species.
The latter equation equals the formulation,
H(s) = In (S-E). By this formula, the relationships between the three parameters, diversity,
equitability, and number of species in a sample,
can be directly depicted in a graph. Text-fig. 5
shows that the first varimax assemblage is characterized by relatively high values of diversity,
equitability, and number of species, while theparameter values of the second varimax assemblage are all rather low. The third varimax
assemblage lies between the two assemblages
on the graph. It is particularly interesting thatthe mixed fauna of the first three varimax
assemblages is also in the intermediate range,
never showing the increases in number of species
or diversity which might be thought to havebeen caused by a mixing. Another point ofinterest is the recognition of three types ofchanging diversity values: 1) the second varimax
assemblage displays changes in diversity depending on both the number of species and equitability; 2) the first varimax assemblage denoteschanging diversity values following only the
number of species (This may represent an inter-793. Ostracode Analyses in the Ananai Formation

59(Equi tabU ity)..

Fl assemblage

Vlokl areav

Ono area"

Sempuku area

1.0
0.8
)

0.6
F2

0.4
0.3
0.2

0.1

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

10

20

30

40

50

60

Species number

Text·fig.5. Diagram showing three varimax assemblages and a mixed assemblage discriminatedin the Ananai Formation in relation to species diversity, equitability, and number of species.
Fl assemblage, first varimax assemblage; F2 assemblage, second varimax assemblage; F3 assemblage,
third varimax assemblage; Mixed, mixed assemblage defined by higher varimax scores all of thefirst three factors.

esting inquiry if it reflects the fact that equita·
bility generally remains between 0.7 and 0.8
at its maximum and does not increase becauseof biological relationships among the taxa
which have been in similar ecological situations);
3) the diversity of mixed fauna is particular inbeing almost constant, with equitability values
increasing as the number of species decreases
and decreasing as the number of species increases.
The geographic variation in assemblage
structures is not clear except in the second
varimax assemblage. In the loki area, this assemblage, which represents the effect of the thenprevailing Kuroshio Current, has structures
which are characterized by low values of diversity, equitability, and number of species (Text·
fig. 5). On the other hand, in the Sempuku area,

assemblage values are rather high for all threeparameters, while in the Ono area, all threeparameter values are in the intermediate range.
Such geographic variation in the second varimax
assemblage may be a result of the effect of theKuroshio Current which has been less intensive
westward from the Sempuku area via Ono to
the loki area.
The temporal variation in assemblage structures was also examined in the Tonohama andOno areas, where vertical sections display relatively complete successions of single varimax
assemblages. In the Tonohama area, the numberof species appreciably increases from the lowest
sample Kll to K6, but decreases abruptly at
K5, immediately below the mixed fauna (K4),showing a similar value to those of Kll and
KID (Text-fig. 6). Passing through the mixing

Kunihiro !SHlZAK/ and Yoshihiro TAN/MURA

60

~Kl-

K7

~.------::f~B ~Kll'1\S- 'K9------./--

o::-------.-.K4 ~

Kl0

i<6

,-

t __ K3 =:::='K2

c::---~

60

50
Species numb.., I

40

Text-fig. 6. Up-section variations Df assemblage structure in the TonDhama section. ArrDWheads stratigraphically upturned.

50
Species number

Text-fig. 7. Up-section variatiDns of assemblage structure in the Ono section. Arrowheads
stratigraphically upturned.

fauna, the number of species increases again
from K3 to Kl with slightly increasing diversity.
Such a variation may suggest that an environmental condition unfavorable to the open shelfassemblage prevailed at and around K4, as
indicated by the occurrence of the mixing
fauna, to have made assemblage structures
simple, meanwhile, even at the top, the environment has still been favorable, under which thestructure of the open shelf assemblage has

become more stable.
In contrast, in the Ono area, both the number of species and equitability increase withincreasing diversity, from lowest samples Jl11 to H4 (Text-fig. 7). Above H4, diversity is
apt to decrease with decreasing numbers ofspecies up to H2, and then abruptly decreases
between H2 and Hl. In comparison with thediversity in the Tonohama section, such a varia-

Table 10. CorrelatiDn coefficients among respective factor IDadings of Dstracode faunas and sediments, diversity, and equitability.
Gs 1, 2, loadings Df the first and secDnd factDrs calculated from the grain-size frequency
distributiDn; Kinds of grains 3-6, lDadings of the first to' fourth factDrs calculated from therelative frequency of the kinds Df grains; D 7, diversity; E 8, equitability; OstracDda 9-12,
loadings Df the first to' fourth factors calculated from the Dstracode data.

~

Gs
1

2

I

I

3

0.255

6

I
I

D

7

I
I

E

I

8

I

9

Ostracoda
10
11

12

1

1.000 -0.882

2-0.8821.000

0.165 -0.103 -0.200

3-0.081

0.165

1.000

4

0.255 -0.103

0.315

1.000

0.204

5

0.257 -0.200-0.3120.204

6-0.023-0.4290.103 -0.171

1.000

0.075

0.165 -0.062 -0.052

0.547

0.023 -0.078

0.057 -0.119 -0.084

0.075

1.000

0.949

0.620 -0.840

0.185 -0.369

8-0.067 -0.004-0.009 -0.094 -0.118

0.165

0.949

1.000

0.569 -0.834

0.240 -0.343

0.620

0.569

1.000 -0.623 -0.162

0.002-0.081

Kinds of grains
45

0.257 -0.023

0.023 -0.067

0.224

0.002 -9·078 -0.004 -0.158

0.315 -0.312 -0.429

0.078

0.033

0.256

0.057 -0.009

0.103

0.068 -0.415 -0.194

0.103 -0.119 -0.094

0.046

0.246 -0.042

0.228

1.000 -0.171 -0.084 -0.118

0.019

0.076 -0.218

0.109

9

0.224 -0.158

0.103

0.046

0.019 -0.062

10

0.077

0.078

0.068

0.246

0.076 -0.052 -0.840 -0.834 -0.623

11-0.1170.033-0.415 -0.042 -0.218

0.547

12

-0.0040.256-0.194

0.108 -0.369 -0.343

0.228

0.077 -0.117 -0.004

0.109

0.185

1.000 -0.265

0.240 -0.162 -0.265
0.045

0.449

0.108

0.045
0.449

1.000

0.061

0.061

1.000

793. Ostracode Analyses in the Ananai Formation
tion may suggest that the environment was
optimum at H4, and then became unfavorable
for the Kuroshio-related assemblage becauseof the decreasing effect of the Kuroshio Current,
as is shown in its geographic variation in theloki area (Text-fig. 5).
Correlations among Parameters
The next step in our study was the clarification of the relationships between the examined
respective factor loadings, diversity, and equitability of ostracode faunas and those of grainsize distribution and the kinds of grains throughcorrelation coefficients. Table 10 shows a summary of the analyses. The correlation coefficientswere computed on 27 samples, where those of
more than 0.136 are significant at a level of 5%.
Significant higher correlations were, as a matterof convenience, marked off by values of morethan 0.597, three times the critical values ofsignificance.
The third factor loadings of ostracode faunas
correlate positively and negatively with thefourth and first factor loadings of the kinds ofgrains, suggesting that the area which the bay
mouth assemblage inhabited has most likely
had a supply of terrigenous material consisting
mainly of rock fragments rather than biogenic
material including shell fragments.
Table 10 points out that community structure as defined by diversity and equitability
does not show a close relationship with sedimentological parameters, but does with faunalassemblages per se. For example, diversity has
a high positive correlation with the first factor
loadings and a high negative correlation withthe second factor loadings· of ostracode faunas,and equitability has a positive correlation withthe first factor loadings, and a negative correlation with the second factor loadings of ostracodefaunas. Through the analyses it seems likelythat these ostracode faunal parameters havenot been modified remarkably by the agents ofwater movement or reworking which might
have taken place.

61

Remarks
Katto et al. (1953) and Kurihara (1968)
studied fossil foraminifera from the Ananai
Formation and suggested that there were geographic variations in the depositional environments of the formation; shallower in the loki
area in the west and deeper in the Sempuku
area in the east. The present results reveal both
geographical and temporal vicissitudes in theenvironments by means of the distribution ofvarimax assemblages as well as by variations
in faunal structures. The Tonohama area wasclosely related to the open shelf element rather
than the remaining four areas. The Ananai andloki areas were related to the bay mouth element, and the environment of the Sempuku area
might have largely been intermediate.
In addition, this study delineates four important physical aspects of the Ananai sedimentation: The supply of biogenic material andtranquil water conditions were almost ubiquitous; meanwhile, the supply of terrigenous
material, particularly to the environments which
the bay mouth assemblage inhabited, and theentire preservation of accumulating sediments
were local and intermittent.
One of the results of this study has been
the delineation of the temporal changes in somevarimax assemblage structures. In general, thosestructures are much more complex than thoseof Recent ostracode assemblages (g.v. Ishizaki,
1979, fig. 4). The most likely cause of such a
difference is the differences in the history of
the habitats where. ostracode lived. The modem
shelf area has a relatively short history, only
about 18,000 years since the last glacial episode;on the other hand, the Ananai sedimentationof several million years ago (Pliocene) might
have taken place under a stable environment,
which presumably, continued for a much longer
period of time.
Opinions concerning species diversity havevaried. Fischer (1960) considered tropical areas
to have had a longer period of climatic stability
which allowed biotic rather than abiotic accommodation of species. Many subsequent

62

Kunihiro ISHIZAKI and Yoshihiro TANIMURA

researchers have held to the hypothesis that
under given stable conditions over a long periodof time biologic components became more
important than physical ones. These ideas
are an expansion of Fischer's climatic·stability
hypotheses (Margalef, 1963; Hessler and Sander,
1967; Buzas and Gibson, 1969). Meanwhile,
Gibson and Buzas (1973) studied modern sam·pies extending from the Arctic to the Gulf of
Mexico, in addition to samples from the Miocene
strata of the Atlantic Coastal Plain and conti·
nental shelf, and suggested that species diversity
and equitability have not increased during thelast 15 Ma; each environment has its own carrying capacity and this capacity is reached rather
quickly.
The intention of those reports has been,
primarily, the clarification of the relationshipbetween the species diversity of faunas andthe environmental conditions under which they
live in order to distinguish paleoenvironments
by means of species diversity of fossil faunas.
The examined assemblages in those studies
have been holistic ones consisting of various
groups in the deep sea (Hessler and Sanders,1967) or the total foraminiferal assemblages(Gibson and Buzas, 1973). The present study
has clarified the point that the structure ofassemblages is fundamentally inherent in respective varimax assemblages, and varies greatly
among and, to a certain extent, within varimax
assemblages due to environmental conditions
or increases in their complexity under stableconditions over a longer period of time. There·
fore, it is highly possible that, by a close inspec·tion of pertinent assemblages, changes in assemblage structure can be more closely related toparticular environmental conditions. In otherwords, a critical factor in applying faunal dy·
namics to fossil assemblages and in assessing
environmental conditions in the geologic pastis the recognition of relevant assemblages per se.
Acknowledgments
The writers are deeply indebted to Professor
Yokichi Takayanagi of the Institute of Geology

and Paleontology, Tohoku University, for hiskind provision of samples for this study, en·couragement, and reading of the manuscript.
Necessary computation was made throughNEAC-ACOS model 1000 computer in the
Tohoku University Computer Center.
The works on which this study is based werepartly supported by the Grant-in·Aids for Scientific Research of the Ministry of Education,
Science, and Culture of Japan (58540501).

References
Buzas, M. A. and Gibson, T. G. (1969): Species
diversity: Benthonic Foraminifera in western
North Atlantic. Science, vol. 163, p. 72-75.
Fischer, A. G. (1960): Latitudinal variations inorganic diversity. Evolution, vol. 14, p. 64-

8l.
Frydl, P. M. (1982): Holocene ostracods in thesouthern Boso Peninsula. In T. Hanai (ed.)
Studies of Japanese Ostracoda, Univ. Tokyo,
Univ. Museum, Bull., no. 20, p. 61-140.
Gibson, T. G. and Buzas, M. A. (1973): Species
diversity: patterns in modern and Miocene
Foraminifera of the eastern margin of North
America. Geol. Soc. Amer. Bull., vol. 84, p.
217-238.
Hessler, R. R. and Sander, H. L. (1967): Faunal
diversity in the deep sea. Deep-Sea Res.,
vol. 14, p. 65-78.
Imbrie, J. and Purdy, E. G. (1962): Classification of modern Bahamian carbonate sediments. In W. E. Ham (ed.) Classificationof Carbonate Rocks, Amer. Assoc. Petroleum Geologists Mem. 1, p. 253-272.
Ishizaki, K. (1968): Ostracodes from Uranouchi
Bay, Kochi Prefecture, Japan. Tohoku
Univ., Sci. Rep., 2nd ser. (Geol.), vol. 37,
p.131-163.
--(1969): Ostracode~ from Shinjiko andNakanoumi, Shimane Prefecture, western
Honshu, Japan. ibid., vol. 41, p. 197-224.
- - (1971): Ostacodes from Aomori Bay, Aomori Prefecture, northeast Honshu, Japan.
ibid., vol. 43, p. 59-97.
- - (1979): Study of Ostracoda from the
Pliocene Ananai Formation, Shikoku, Japan- a step toward distinguishing the sedi-

793. Ostracode Analyses in the Ananai Formation
mentary environments -. In Serbian Geol.
Soc. (ed.) Taxonomy, Biostratigraphy andDistribution of Ostracodes, Proc. VII Intern.
Symp. Ostracodes, p. 197-205. Serbian
Geol. Soc., Belgrade.
- - (1981): Ostracoda from the East China Sea.

Tohoku Uniu., Sci. Rep., 2nd ser. (Geol.),
vol. 51, p. 37-65.
--(1983): Ostracoda from the Pliocene Ananai
Formation, Shikoku, Japan - description-.

Trans. Proc. Palaeont. Soc. Japan, new ser.,no.131,p.135-158.
Katto, J., Nakamura, J. and Takayanagi, Y.
(1953): Stratigraphical and paleontologicalstudies of the Tonohama Group, Kochi
Prefecture, Japan. Kochi Uniu., Res. Rep.,

63

vol. 2, p. 1-15 (in Japanese with English
abstract ).
Kurihara, K. (1968): Notes on the benthonicForaminifera of the Tonohama Group,
Shikoku, Japan. Trans. Proc. Palaeont. Soc.
Japan, new ser., no. 70, p. 267-283.
Margalef, R. (1963): On certain unifying principles in ecology. Amer. Naturalist, vol. 97,
p.357-374.
Niitsuma, N. (1971): Automatic grain-size
analyser for sedimentological investigation.

TohokuUniu.,

Inst.

Geol. Pal.,

Contr.,

no. 72, p. 25-36 (in Japanese with English
abstract ).
Sokal, R. R. and Sneath, P. H. A. (1963): Principles of Numerical Taxonomy. 359 p.,
Freeman and Co., San Francisco.

mHfr$i'EJ\rl-JJi~ ([lqb!:~) I!) fl lI';;a -llf*~nfr--: ilYl~~ f~np: fifll!) ifJWI:.iiJ~) -C .~{E L -C 0';(flT;,s ffi.'f.1'lr,f;!t,\i*J r"Y).t I) f1}L 35 -tr ;.. /It- n· G 421~ 79 j\j\1!) It jf;.4; {tTl n;~,i'!:iE ~ h t.: (ishizaki, 1983,~ 1 L .:.. I!) 1f. ~ 11; 7' - !J -;' ~ ~, " 7-. t L -C , Q -f: - I: I:' l ;,sctlll1: 57" Ii~ T 5:Hfr ~ 11 ') t.: *ti if:

Ii. J\Il-ll,~tI!)H/f~.'UF.'fft;');, ),q,;(j~I:.'i, 4 -':)I!),: ~ -", "7,lrf'!H (~irli~#lIJlWf;R. f1.li*JJ:%r,rt1~. ~ Il E'tifH.; len;) )\\iJit:%f,( Us) i:'l~) -C ~fil'~0''f~);h;,s :. t 'd:'~T".ljj;ft(¥(J1!) /t 11['1:'.t ~. -c f~ G ht.: f:(lj~Jj;fjli7t;fJi:t~ .t v: PT I!) f1Hl[ I!) HIM J:U:.1j!;--j l •-c :1::I;\tn"
I7.H,7t fir 'd:' L U,,'ilf', l:t. 7YJ&I~J:ll1!) I/1IH't ~, it ft'U/7.!11!) (lUr:, II:, fuiii;\4'.!1'[!{ I!) (JUf11~ l v:Il'~VJM~'l'tI!)(Mf1~m;Jd-;,s Il~ T~ ;j;I!f,t-t;,s 0

JIHm~ t !ur; 1(1:' -':) l ,-C I!) 1'-1]'- fHij ffl:. f1jlO) ~I~n. J~J~N ill' Ie t'l!) IIiJ I!)i:fj!*l rH&1 i. Hil!)~UWI:. J:Jji/!jJ!:tlJ;JiUt'iCf:n~'!l!IJ~ c':: l:tll tic. c~rxJ(,f:-c. J: ~ -,' 'y " 7- Uo!:.l;';HifJ: ~ 1!)-C';Ji,;,sf,r:. t ~7J;I~T Z:."~ 2 ~: ~ "', "7-./ir ftl!)f'TiI!):HHI:. J:JWtiI[t, .flTi~':'liJiliJ#JWUNjJj~':.~26')G.h. ~IL'f1!),~,\i':;AI!)J.\' ))I!)Ill' (, l ,l!)jB1;l' 'd:' ixH!J( L -C l';,s ~ I!) t :J5';/~ r);lL;,s );~!Y.-t!l '/ ~ /' ':'1~ l' -C 7;. G J1
0;,s /I'frr~J(i':J¥£{t >b. I"j 1:$ t;oJd!~J~iJQI!)Hfft ~ ;J;I!f,t-j- ;,s t I!) t 15' *- G h;,s0

.fi~J(J1 R]!~ • ~H HiT:

Trans. Proc. Palaeont. Soc. Japan, N.S., No. 137, pp. 64-74, pIs. 8, 9, April 30, 1985

794. LARIX REMAINS FROM PLEISTOCENE STRATA OF NORTHEAST
JAPAN, WITH SPECIAL REFERENCE TO THE DISTRIBUTION OFLARIX IN THE LATTER HALF OF THE LAST GLACIAL AGE*
KEIJI SUZUKI
Laboratory of Earth Science, Faculty of Education, Fukushima University,
Matsukawa-machi, Fukushima, 960-12

Abstract.
The morphological characters of cone and long shoot remains of
the genus Larix which were obtained from the Pleistocene strata in the northeastern Japan are examined. They are referred to Larix kaempferi (Lamb.) Carr.,
L. kamtschatica (Rupr.) Carr. and L. cf. kaempferi (Lamb.) Carr. The former two
species were all obtained from strata of the Last Glacial age and the last species,
represented by only one specimen, was collected from the Middle or Early Pleistocene stratum. It is pointed out that the range of geographical distribution of L.
kamtschatica (Rupr.) Carr. and L. kaempferi (Lamb.) Carr. had come closer toeach other during the latter half of the Last Glacial than it is at present time.

Introduction

for a monographic treatment of the genus has
been evident for many years. Since it is not myintention to revise or add to the taxonomy of
the genus, I follow the opinion of Ohwi andKitagawa (1983) for the Japanese species andthat of Komarov (1968) for those species which
occur outside of Japan. Accordingly, a population of Larix distributed on high mountains ofCentral Honshu is referred to by the name of
L. kaempferi (Lamb.) Carr. L. leptolepis (Sieb.
and Zucc.) Gordon is regarded as a junior synonym of it. Furthermore, a population on thesouthern Kurile Islands, southern Sachaline andthe 01 'ga District in Ussuri Territory is treatedas L. kamtschatica (Rupr.) Carr., and bothL. gmelini Gordon and L. dahurica Turcz. var.
japonica Maxim. are regarded as its junior synonyms. The distributional range of L. kaempferi(Lamb.) Carr. is thus isolated from that of L.
kamtschatica (Rupr.) Carr.
The cone and long shoot remains which
form the basis of the present study were ob-

Larix is one of the genera among the family
Pinaceae, widely distributed in the cold latitudesof the northern hemisphere, and also one ofimportant plants to investigate minutely thegeohistorical changes of the flora and vegetation
during the Pleistocene epoch. Fossil cones andtwigs of the genus Larix have abundantly beenfound in Pleistocene strata of the JapaneseIslands (Miki, 1938, 1956, 1957; Sohma, 1959;
Suzuki and Sohma, 1965; Yano and Fujita,
1970; Yano et al., 1975; Yano et al., 1978).
Although these fossils have inadequately been
described in most cases by these previous workers, they have been reported under such varied
names as L. gmelini Gordon, L. dahurica Turcz.
var. japonica Maxim., L. kaempferi Sarg., andL. leptolepis Gordon.
The status of East Asiatic taxa of the genus
Larix has not fully been evaluated. The need
*Received May 10, 1984.
64

Larix remains from Pleistocene strata

tained from strata of the Last Glacial age, except
for one cone remain from an early Middle orlate Early Pleistocene stratum, all distributedin the northeastern Japan. After a careful examination of morphological characters of these
cone and long shoot remains, they are foundto belong to the following two species andpossibly a third one:1) Larix kaempferi (Lamb.) Carr.
2) Larix kamtschatica (Rupr.) Carr.
3) Larix cf. kaempferi (Lamb.) Carr.
Taking both stratigraphical and geographicaldistributions of these fossil specimens into
consideration, the following facts may be pointed out:
1) L. kamtschatica (Rupr.) carr. was distributed in the southwestern part of Hokkaido and in the northern part of Tohoku
District of Honshu, whereas L. kaempferi(Lamb.) Carr. had its distribution in thesouthern part of Tohoku District andKanto District both in Honshu, during thelatter half of the Last Glacial. Their age isyounger than a radiocarbon date of ca.
30,000 y. B.P. during the Last Glacial
period.
2) The range of geographical distribution of
L. kamtschatica (Rupr.) Carr. and L.
kaempferi (Lamb.) Carr. had come closer
to each other during the latter half of theLast Glacial than it is at the present time.
3) The single cone remain from the early
Middle or late Early Pleistocene stratum
is morphologically similar to the cones of
L. kaempferi (Lamb.) Carr.
Locality and Stratigraphical Horizon of the
Plant-bearing Bed
Those fossil cones and shoots of the genus
Larix which are described in the present study
are obtained by the present writer and his
collaborators from twenty-one beds at seventeen
localities as shown in Text-fig. 1 and Table 1.
Those fossil specimens identified as Larix
kamtschatica (Rupr.) Carr. are newly obtained
from peat beds intercalated with the terrace

65

deposits at Yosumizawa and the Jinya fluvial
terrace deposits at Higashiyama, both in the
Oshima Peninsula of southern Hokkaido (Yanoet al., 1978). Specimens of the same species
were also known under the name of L. dahurica
Turcz. var. japonica Maxim. from a peat bedof the Sambongi Formation at Ootai (Sohma,
1959; Takeuti, 1971). Kanto Loam ResearchGroup and Shinshu Loam Research Group(1962) also obtained specimens of the same
species from three beds of the Hanaizumi
Formation at Kanamori. These two localities
are in the northern part of Tohoku District.
Ages of these peat beds can be considered tobelong to the latter half of the Last Glacial
age on account of stratigraphical data or radiocarbon dates mentioned by these authors.
Those specimens identified as Larix kaempferi(Lamb.) Carr. are known from fourteen peator peaty beds at twelve localities distributedin the southern part of Tohoku District and the
Kanto District. All of these beds are of theLast Glacial age. Of these fourteen beds, thefollowing eleven may be thought to represent
the latter half of the Last Glacial based on
stratigraphical and radiocarbon data. These
are: a peat bed of the Fifth terrace deposits inthe coastal area of Fukushima Prefecture (Suzuki and Nakagawa, 1971), three peat beds occurring in the upper part of the Fujita Formationof the Fukushima Basin (Yoshida et al., 1969),
a peat bed in the lower part of the Ootsuki
Formation of the Koriyama Basin (Suzuki andSohma, 1965), peat beds in the upper part of
the Saru-uchi. II Formation of the Abukuma
Mountainland (Yoshida et aI., 1981), a peaty
bed of the Sunagawa Formation of the Inawashiro Basin (Yoshida and Suzuki, 1981), a peat
bed overlain by Holocene gravel and sand strata
in the western part of the Aizu Basin (Suzuki
et aI., 1977; Suzuki, MS), a silt bed overlying
the Kuboma pumice flow bed at Minamikaruizawa of Nagano Prefecture (Unozawa andSakamoto, 1972), and a peat bed in the Ekoda
Formation at Ozaki in Tokyo (Oosawa, 1982,
personal communication).
The remaining three of the fourteen beds

Keiji SUZUKI

66

142°

42°

36°

Text-fig. 1. Map showing localities from which fossil specimens of the genus Larix were recovered.
Locality numbers correspond to those shown in Table 1. All localities except for 6b, 8, 9 and 17
represent strata accumulated during a time of ca. 30,000-13,000 years B.P. in the latter half of
the Last Glacial. Localities 6b, 8 and 9 belong to the middle or early part of the Last Glacial (before
32,200 years B.P.) and 17 to an early Middle or late Early Pleistocene (Takada Formation).

Larix remains from Pleistocene strata
Table 1.
Loe.

No.
1

2

3

List of localities yielding fossil Larix, radiocarbon dates (years B.P.) and associated planttaxa, in Pleistocene strata of Northeast Japan.

Locality(Altitude m)
YosumlzawB. Assabumacht, Htyama-gun,
Hokkaldo. (70)
Hlgashlyama, Esashlmachi, Hlyama-gun I
Hokkaldo. (65)
Ootal, Nanga-mura,
Sannohe-gun. Aomori
Pre f. (205)

Formation or
Bed

7a

7b

8

9

10

11

12

13

14

15

16

17

Negishi. Kori-machi,Date-gun. Fukushima
Pref.-041
South of Koristation, Kori-machi.
Date-gun. Fukushima
Pre f. (78)South of Ko ristation. Kori-machl,
Date-gun, Fukushima
Pref.-(76)Wakamiya-machi,
Nihonmatsu-City,
Fukushima Pre f.
(200)
500m north of
Kamiza, Hotomiyamachi, Adachi-gun,
Fukushima Pref. (256)
Ha ra, Katabiramachi, Koriyama
City, Fukushima(262)
Pre f.
Loc. I, Sa ru-uchi,
Takine-machi,
Tamura-gun,
Fukushima Pref. (466)Sunagawa,Inawashiromachi. Yams-gun,
Fukushima Pref. (525)Nakano-iri, Konanmachi, Koriyama
City, Fukushima(560)
Pre f.
Ookawa-River, Bangerna ch i. Kawan uma-gun,
Fukushima Pref. (172)kamt:schatica

Associated species

Picea glehni(Rup r. ) Carr.

Reference
Vane and al. ,1978

L. kamtschatica Picea jezoensis, p.
(Rupr.) Carr.
glehni

Ditto

Sambonp,tFormation

L. kamtschatica Picea glehni, Abies(Rup r. ) Carr.
sachal inensis, Tsuga
sp.,Pinus koraiensis,

Sohma, 1959;
Takeuti, 1971

Kanamori, Hanaizumimachi, Nishiiwaigun, lwate Pre f.
(32 )Kanamori, Hanaizumimachi, Nishiiwaigun, Iwate Pre f.
(31. 5)
Ogawa, Shinchi-mura,
Sohma-gun,
Fukushima Pre f . (12)Negishi. Kori-machi.
Date-gun. Fukushima
Pre f. (67)6b

L.

Jinya terrace 27, 86O :t 2 ,67(
deposits(Gak-7214)

4b

6aSpecies of Lari x

named)

Kanamori, Hanalzumi- Second peatmachi, Nishiiwalof Hanaizumi
gun, Iwate Pret.
Formation(33)

5

14C date

River terrace 15,070:t490
deposits(un(Gak-7701)

4a

4c

67

26 600+ 1 ,75C,
-l,50C(Gak-2845)

Hen.Jl.....an thestrifoliata

L. kamtschatica Pieea glehni, Taxus(Rupr.) Carr.
euspidata, Pinus
koraiensis, Pieea sp.

Third peatof Hanaizumi
Formation

21,430:t800

Fourth peatof Hanaizumi
Formation

L. kamtseha ti ea Pieea jezoensis~ p.
28 070+ 1 ,100
(Rupr.) Carr.
bieolor, p. s p. ,'-1,250L. kamtsehatiea Pieea glehni, p.
(Rupr.) Carr.
bieolor~P. sp. ~Kanta LoamRes. Group an d
Shinshu LoamRes. Group,
1962
Ditto

Pinus kora i en sis

Ditto

Pinus koraiensis

Fif th terrace 28, 05O:t l ,550 L. kaempferi
deposits(Gak-145l)(Lamb. ) Carr.
Lower part of )40,350
Fujita(Gak-7330)
Formation

L. kaempferi(Lamb. ) Ca r r.

Upper part of 18,750:t500
Fujita(Gak-1452)
Formation
Upper part of 21, 66O:t l ,190
Fujita(Gak-6053)
Formation
24,2 30:t1, 380(Gak-6054)
Upper part of 22,OOO:t l ,140
(Gak-6055)
FujitaFormation
25, 4OO:t l ,150
(Gak-209))32,200
Nihonmatsu(Gak-517)
Formiltion

L.

kaempferi(Lamb.)

Ca rr.

L. kaempferi(Lamb.) Ca rr.

L. kaempferi(Lamb.) Carr.

L.

kaempferi(Lamb.)

Carr.

Pieea bieolor va r.
reflexa, Pinus
koraiensis
Pieea maximowiezii,
Abies sp. , Tsuga sp.
Thujopsis dolabrata~
Betula platyphylla
Pieea jezoensis, P.
bieolor, pi n us
koraiensis
Pieea maximowiezii,
Phellodendron
amu rense,
Prun us salieina
Pieea maximowiezii,
Abies veitehii~ Tsuga
sp. , Thujopsis
dolabrata
Pieea bieolor, Pinus
koraiensis~

Suzuki an dNakagawa, 1971
Yoshida andal .• 1969 ;Suzuki, MS
Ditto

Ditto

Ditto

Ditto

Tsuga

diversifolia

Lower part of )32,380
Ootsuki(Gak-9815)
Formartion

L. kaempferi(Lamb.) Ca rr.

Lower part of 29, lOO :t2 ,OOO L. kaempferi(Gak-495)(Lamb.) Ca rr.
OotsukiFormation
Upper part of 17,570+400(Gak-6846)
Saru-uchi I I
Formation
19,320:t420(Gak-6845)
Sunagawa
p,720:t980
Formation(Gak-6849)
Kanan
Formation

P2,880~:~~L.

kaempferi(Lamb. ) Ca rr.

L. kaempferi(Lamb.) Carr.
L. kaempferi(Lamb. ) Ca rr.

Pieea maximowiezii,
Pinus koraiensis~
Tsuga diversifolia,
Prunus salieina
Pieea koyama i ~ P.
bieolorSuzuki andal. I 1967 ;Suzuki. MS

Pieea
Tsuga

sp.,Abies s p. ,sp. ,Menyanthes
trifoliata

Yoshida anda 1. , 1981

Pieea .maximowiezii,
jezoensis,
Pinus koraiensis
Picea s p. , Abies sp. I
Tsuga diversifolia

Yoshida andSuzuki, 1981

Pieea maxlmowiezii,
Menyanthes trifoliata

Suzuki anda1. , 1977;
Suzuki, MS

Pieea maximowiczii,

Unozawa an d
Sakamoto, 1972P.

S u z uk i

Sohma ,

and1965

S uz uk i andal .• 1982

(TH-753)

Peat bed
overlaid by
Holoceneravel
Cli f f of Kumoba
Sl1 t bed over- 19,400:tSOO(Gak-2656)
lying Kumoba
Ri ve r, HinamikaruiO,200:t700
zawa , Karuizawa City, pumice flow
(Gak-2655)
Nagano Pre f. (930 )Peaty bed of
3,600:tllO
Ozaki, Egota,(N-3754)
Ekoda
Nerlma-ku, Tokyo(30)
Formation
3,700:t160
Pre f.
(N-3755)
TakadaTakatori, Nakano,
Formation
Fuk ush ima City,
Fukushima Pref. (150)L.

kaempferi(Lamb.) Carr.

L. kaempferi(Lamb.) Ca r r.

P. shirasawae, Abies
sp. , Tsuga sp. ,Menyanthes trifoliata
Pieea maxlmowiczi~~
Pinus koraiensis,
Ostrya japoniea, Alnus
sp. , Prunus ~.
cf. kaempferi Pieea maximowiezii~(Lamb. ) Ca rr.
Alnus .p.

L. kaempferi(Lamb.) Ca r r.

Personal
communication
by Osawa, 1982
S u z uk i an d
Yoshida, 1972

Keiji SUZUKI

68

may be assigned to the early half of the Last
Glacial, an interval older than ca. 30,000 y. B.P.,
on account of their radiocarbon dates as well
as stratigraphical data. These are: a peaty mudin the lower part of the Fujita Formation of
the Fukushima Basin (Yoshida et al., 1969),
a peat bed in the Nihonmatsu Formation whichforms a terrace in the lowland area along the
Abukuma River (Yoshida et al., 1969), and apeat bed at the base of the Ootsuki Formationof the Koriyama Basin (Suzuki, MS), all inFukushima Prefecture.
A cone remain identified as Larix cf. kaempferi (Lamb.) Carr. comes from a peaty mudin the upper part of the Takada Formation at
the northwestern margin of Fukushima Basin.
(Suzuki and Yoshida, 1972). The Takada Formation may be thought to be of early Middle
or late Early Pleistocene age based on stratigraphical data and palaeobotanical evidences.
Description of Fossil Specimens
Larix kamtschatica (Rupr.) Carr.

Plate 8, Figs. 1a-j, 2a-f, 3a-i, 4alt,
5a~, 6a-o, 7a-j, 8a-r
kamtschatica (Rupr.) Carr., Komarov,
1968, p. 123-124.
Larix gmelini Gordon, Miki, 1957 (part), p.
232-233, pI. 1, figs. Aa and B (not Ab, Ac
and Ad).
Larix dahurica Turcz. var. japonica Maxim.,
Sohma, 1959, figs. B-1 and B-2.

Larix

Description:-Cones oblongly to ellipticallycylindrical, rarely oblongly ovate, 1.0-1.7 cm
in length, 0.6-1.0 cm in width, maximum widthsituated at middle or lower part of its entire
length, bearing 15-25 cone-scales and thickcone-stalk. Cone apex truncate or obtusely acute.
Cone-scales orbicular to widely ovate, upper
margin truncated or emerginated, and notrecurving downwards, and each cone scale 0.51.0 cm long. Bracts long and rectangular, withneedle-like apex.
Long shoot with many short shoots, andintervals between the points where short shootsattached to the long shoot generally narrow.
Remarks and comparison:-Most of the cone
specimens are well preserved, whereas somefrom Ootai (Figs. 3c~), Higashiyama (Figs.
2d-f) and Hanaizumi (Figs. 6b, n, 0; Bl-q)
localities are somewhat incomplete. furthermore, some of the specimens from Yosumizawa(Figs. 1h-j) , Higashiyama (Figs. 2b, c) andOotai (Figs. 3a, b, d) are remarkably flattened,and such specimens having an oblongly ovate
shape as those from Hanaizumi (Figs. 6m-o)
are somewhat worn away at the outer part ofthe cone.
These cone specimens are generally small insize and comprise two types, one having acylindrical and the other having an oblongly
ovate form. The former may be an Ildult stateof opening cone, and the latter appears to
represent a younger stage.
Those cone specimens from Yosumizawa,
Higashiyama and Ootai are specifically identified
as the cone of L. kamtschatica (Rupr.) Carr.
in having a cylindrical form, a fewer numberof cone-scales and ovate~to-obvate-shaped conescales with an emerginated or truncated upper
margin. Most of the cone specimens from those
three peat beds of the Hanaizumi Formation
are also identified as those of L. kamtschatica(Rupr.) Carr. because they exhibit similar morphological characteristics. However, some cone
specimens (Figs. 6g, h, k-o) from the third
peat bed of the Hanaizumi Formation are somewhat different in having an oblongly ovate form.
At a first glance, they appear to be somewhat
similar to those of L. kaempferi (Lamb.) Carr.
but differ in having a fewer number of conescales. This feature may be seen in a younger
stage of development in the cone of L. kamtschatica (Rupr.) Carr. Therefore, none of theabundantly occurring cone specimens from thethird peat bed of the Hanaizumi Formation
exhibits the typical characters of L. kaempferi(Lamb.) Carr.
The long shoots obtained from the peat bedof Jinya terrace deposits are identified as thoseof L. kamtschatica (Rupr.) Carr. by taking into
account the close interval between short shoots

Larix remains from Pleistocene strata

on the long shoot.
Locality and stratigraphic horizon:-As shownin Table 1, specimens identifiable with the present
species are obtained from four localities; twoin the Oshima Peninsula, one in Aomori Prefecture, and one in Iwate Prefecture. In Iwate
Prefecture, three beds are recognized as thefossil-bearing bed. Those three have been called
the second, the third, and the fourth peat bed of
the Hanaizumi Formation; respectively. The
fossil-bearing beds at these four localities arethought to belong to the latter half of the Last
Glacial age (about 15,000-30,000 y B.P. inradiocarbon dates).
Repository:-Stored in the Laboratory of
Earth Science, Faculty of Education, Fukushima
University.
Other occurrences in Japan:-Fossil female
cones have been reported from Pleistocene
strata of Hokkaido under the name of L. gmelini
Gordon. Among them, specimens from theHiroshima Formation (Yano and Fujita, 1970)
in Hiroshima-cho, Sapporo-gun, and from theOshamanbe terrace deposits (Yano et al., 1975)
in Oshamanbe-machi, Yamagoe-gun, are identicalwith the present materials identified with L.
kamtschatica (Rupr.) Carr., and these strata areassignable to the latter half of the Last Glacialage. Furthermore, there are fossil records ofcones and long shoots described under thename of Larix gmelini Gordon from the Larix
bed at Manchidani in Nishinomiya City (Miki,
1957, p. 232-233, pI. 1, Ac, Ad), Yozawa in
Itsukaichi-town (Miki, 1957, p. 232-233, pI.
1, Ab) and a Pleistocene bed in Higashikushiro(Miki, 1957, p. 232-233, pI. 1, B). The cone
specimens from the former two localities resemble those from young trees of the extant
species, L. kaempferi (Lamb.) Carr. Further
revision may be needed for these fossil specimens.
Larix kaempferi (Lamb.) Carr.
Plate 9, Figs. 1a""""1:, 2a""""1:, 3, 4a-c, 5a-c,
6a-c,7,8a""""1:,9a,b,10a-e,11a,b,12,13

Larix kaempferi (Lamb.) Carr., Ohwi anq Kita.

69

gawa, 1983, p. 60
Larix kaempferi Sargent, Miki, 1938, p. 229,
pI. 3, figs. A-C.
Larix /epto/epis Murr., Miki, 1956, p. 450,
pI. 13, fig. H.
Larix kaempferi Sargent, Miki, 1957, p. 233,

pI. 1, C.
Description:-,Cones elliptical to ovate, rarely
globularly 'ovate, 1.6..,-2.5 cm in length, 1.01.5cm in width, maximum width situated below.
the half way in its entire length, with 25..,.35
cone-scales, rarely with about 20 cone.scales,
and with thick cone-stalk. Cone apex round to
obtuse;' Cone·axis stout, with stiff hairs .. Conescales orbicularly fan-shaped, upper· margin
generally round or recurving downwards, ca.
0.5-0.8 cm long. Bracts short and rectangular,
with a needle-like apex. Long shoots having
many short shoots, and interval between shortshoots on the long shoot generally wide.
Remarks and comparison::-Most of the fossil
cone specimens are preserved in' somewhat
flattened state and some are" incomplete. The
cone obtained at the Bange locality lacks theupper portion (Fig. 7) and the one from Nakanoiri is missing the lower portion (Fig. 6). However,most of the specimens are well preserved. 'Many cone remains are from elliptical toovate in shape and bear a large number of conescales of which upper margin recurves down.
wards. These characteristics as seeri in the fossil
cones are identical to those of the extant' species,
Larix kaempferi (Lamh.) Carr., although 'manyof the fossil cones are somewhat smaller thanthe Recent cones.
The shape of some fossil coneS ranges fromovate to globular ovate. These fossil cones are
somewhat small in size and have cone-scales ofwhich upper margin recurves, less distinctly
downwards (Figs. 1, 10e, 13). These features
are also fOlind commonly on the cones of young
trees of extant Larix kaempferi (Lamb.) Carr.,as shown in Plate 9, Fig. 15 .
. .Some 'long shoots obtained from the upper
part of the Saru-uchi II Formation and the upper
part of the Fujita Formation could be identified
as those' of· L.kaempferi (Lamb.)' Carr. on:

Keiji SUZUKI

70

account of the wider intervals between shortshoots on the long shoot.
Locality and stratigraphic horizon:-As shownin Table 1, the fossil specimens are obtained
from twelve localities of which ten are in thesouthern part of Tohoku District (Fukushima
Prefecture), one in the District of Tokyo, andone in Karuisawa City of Nagano Prefecture.
Among these ten fossil localities in Fukushima
Prefecture, two fossil-bearing beds having astratigraphical interval of 7 m and 2 m occur at
Negishi and south of the Kori Station, respectively.
Among these twelve localities mentioned
above, fossil-bearing beds at three localities
belong to the first half of the Last Glacial age
older than 32,000 y. B.P. based on radiocarbon
dates. These are the lower part of the Fujita
Formation, the Nihonmatsu Formation andthe lower part of the Ootsuki Formation. Elevenfossil-bearing beds at the remaining ten localities
belong to the latter half of the Last Glacial
spanning a period from ca. 30,000 y. B.P. to
13,000 y. B.P. radiocarbon dates. These are:peat beds of the Fifth terrace deposits in the
coastal area of Fukushima Prefecture, upper
part of the Fujita Formation, lower part of the
Ootsuki Formation, upper part of the Saru-uchi
II Formation, the Sunagawa Formation and the
Konan Formation, and a peat bed in Bange, asilt bed overlying the Kumoba pumice flow anda peaty bed of the Ekoda Formation.
Repository:-Stored in the Laboratory of
Earth Science, Faculty of Education, Fukushima University.
Other occurrence:-The cone remains referredto those species discussed in this study werereported from the conifer bed at Ekoda in Tokyo(Miki, 1957, p. 233, pI. 1, C).
Larix cf. kaempferi (Lamb.) Carr.

Plate 9, Figs. 14a-c
Remarks and comparison:-A somewhat poorly preserved cone remain was obtained from theupper part of the Takada Formation assignable
to a late Early or early Middle Pleistocene age.

This specimen with numerous cone-scales (morethan 30) is small in size (1.4 cm long) and has
an ovate shape. The upper margin of these conescales is somewhat recurved downwards, thoughsome of their outer structures are ragged.
This cone specimen resembles cones of an
extant species L. kaempferi (Lamb.) Carr., but
is distinct in having a large number of conescales despite of its small size. Therefore, thepresent writer is withholding specific identification of this specimen.
Repository:-Stored in the Laboratory of
Earth Science, Faculty of Education, Fukushima
University .
Geographical Distribution in the Northeast
Japan during the Latter Half of theLast Glacial Age
From the preceding chapters, it becomes
clear that both Larix kamtschatica (Rupr.)
Carr. and L. kaempferi (Lamb.) Carr. were
distributed somewhere in the southwestern
Hokkaido, Tohoku and Kanto Districts ofnortheastern Japan during the latter half of theLast Glacial. However, there is no locality where
the specimens of both species occurred together.
During that time, L. kamtschatica (Rupr.) Carr.
had its distribution in the southwestern partof Hokkaido and in the northern part of '1'0hoku District. On the other hand, L. kaempferi(Lamb.) Carr. had been distributed mostly inthe southern part of Tohoku District and Kanto
District, though its distribution might havebeen more restricted in time and space in Kanto
District. In other words, fossil remain identifiablewith L. kamtschatica (Rupr.) Carr. has neverbeen found in the southern part of Tohoku
District and Kanto District, although remainsof the genus Larix were obtained from manysites. On the other hand, no remain identifiablewith L. kaempferi (Lamb.) Carr. has been foundin the southwestern part of Hokkaido and in
the northern part of Tohoku District, althoughremains of the genus Larix were abundant atfour sites. This observation may indicate thatgeographical ranges of both species had roughlyLarix remains from Pleistocene strata

been divided in the middle part of Tohoku
District on the eastern side of Ohu Backbone
Range. However, it is not clear as to whether
these two species had been isolated from eachother or occurred together in the vicinity ofthe boundary. In any case, geographical rangesof these two species had been close to each otherfar more than they are at the present time.
It is noteworthy that the northern geographical limit of L. kaempferi (Lamb.) Carr. during
the latter half of the Last Glacial was not greatly
different from that at the present time, whereas
the southern geographical limit of L. kamtschatica (Rupr.) Carr. during that time wasgreatly shifted from its present distribution.
Furthermore, it must also be pointed out thatthese two species were representatives of lowland floras of northeastern Japan during thelatter half of the Last Glacial as evidenced bytheir presence in the fossil-bearing beds ateach locality.
Fossil remains of Picea bicolor (Maxim.)
Mayr, P. maximowiczii Regel and Abies veitchii
Lindl. occur commonly in association withthose of Larix kaempferi (Lamb.) Carr. as
shown in Table 1. All of these are, however,not found in beds yielding remains of L. kamtschatica (Rupr.) Carr. Fossils of Picea glehni(Fr. Schm.) Masters and Abies sachalinensis(Fr. Schm.) Masters are common in beds bearing
those of Larix kamtschatica (Rupr.) Carr.,
whereas they are absent in beds containing
remains of Larix kaempferi (Lamb.) Carr. Suchspecies as Pinus koraiensis Sieb. and Zucco andPicea jezoensis (Sieb. and Zucc.) Carr. havebeen found in beds bearing remains of Larix
kaempferi (Lamb.) Carr. or L. kamtschatica(Rupr.) Carr. in the Tohoku District, and fossil
specimens of Picea jezoensis (Sieb. and Zucc.)
Carr. have been recovered also in beds yielding
remains of Larix kamtschatica (Rupr.) Carr.
in the southwestern part of Hokkaido. Fromthese observations, it may be suggested that theboundary between the geographical ranges of
Larix kaempferi (Lamb.) Carr. and L. kamtschatica (Rupr.) Carr. had nearly coincided withthe respective floral and vegetational boundaries

71

in the northeastern Japan during the latter
half of the Last Glacial age.
Acknowledgments
I wish to express my sincere thanks to Prof.
Kankichi Sohma, Tohoku University, for hiskind advice and giving permission to examine
the specimens in his collections, and Prof.
Tsunemasa Saito, Yamagata University, forreading the manuscript and his helpful critisism.
My thanks are also due to Mr. Makio Yano,
Historical Museum of Hokkaido, Mr. Susumu
Osawa, Wako-gaku-en High School, and themembers of Kanto Loam Research Group andShinshu Loam Research Group, for their kindassistances. Furthermore, my thanks are extended to Mr. Toshio Watanabe, Fukushima
University, for his kind assistance in photographying.
References
Kanto Loam Research Group and Shinshu Loam
Research Group (1962): On the GeologicalAge and Sedimentary Environment of the
Hanaizumi Bed. Earth Science (Chikyukagaku), vol. 16, no. 62, p. 1-10; no. 63, p. 1018 (in Japanese).
Komarov, L. V. (1968): The Genus Larix. in
Flora of the U.S.S.R. I, p. 120-124. Jerusalem (translated from Russian edition,
1934, Leningrad).
Miki, S. (1938): On the change of flora ofJapan since the upper Pliocene and thefloral composition at the Present. Jap.
Journ. Bot. vol. 9, p. 214-25l.
--(1956): Remains of Pinus koraiensis S. et
Z. and associated remains in Japan. Bot.
Mag. Tokyo, vol. 69, p. 447-454.
--(1957): Pinaceae of Japan, with specialreference to its remains. Journ. Inst. Polytech. Osaka City Univ., vol. 8, ser. D, p.
221-272, pIs. 1-10.
Ohwi, J. and Kitagawa, M. (1983): The Genus
Larix. in New Flora of Japan, p. 60. Shibundo, Tokyo (in Japanese).
Sohma, K. (1959): On woody remains from a
Pleistocene peaty lignite at Otai, Aomori

Keiji SUZUKI

72

Prefecture. Ecol. Rev., vol. 15, no. 2, p.
67-70.
Suzuki, K., Manabe, K. and Yoshida, T. (1977):
The Late Cenozoic stratigraphy and geo·
logic development of the Aizu Basin, Fukushima Prefecture, Japan. Mem. Oeol. Soc.
Japan, no. 14, p. 17-44 (in Japanese withEnglish abstract).
--and Nakagawa, H. (1971): Late Pleistocene
flora from the Pacific coast of Fukushima
Prefecture, Japan. Sci. Rep. Tohoku Univ.,
Sec. ser. (Oeol.), vol. 42, no. 2, p. 187198, pis. 27-30.
--and Sohma, K. (1965): The Late Pleistocene
stratigraphy and Palaeobotany of the Koriyama Basin. Sci. Rep. Tohoku Univ., 4thser. (Bioi.), vol. 31, no. 3, p. 217-242,
pis. 1-3.
- - , Takeuti, S. and Seino, A. (1982): Terrace
deposits in the southern part of the Inawashiro Basin. Ann. Rep. Synthetic Study,
Fukushima Univ., The Nature of Lake Inawashiro, no. 3, p. 13-20 (in Japanese withEnglish abstract).
--and Yoshida, T. (1972): The geohistory of

the formation of the Fukushima Basin in thesouthern part of the Tohoku District, Japan.
Mem. Oeol. Soc. Japan, no. 7, p. 285-295(in Japanese with English abstract).
Takeuti, S. (1971): 14C Age of the Sambongi
Formation at Otai, Aomori Prefecture.
Earth Science (Chikyukagaku), vol. 25, no.
4, p. 186-187 (in Japanese).
Unozawa, A. and Sakamoto, T. (1972): Recent
history of Minami-Karuizawa, Nagano Prefecture, Central Japan. Journ. Oeol. Soc.
Japan, vol. 78, no. 9, p. 489-494 (in Japanese with English abstract).
Yano, M. and Ishikari Teichitai Research Group(1969): On the remains of Larix gmelinii
from the Quaternary deposits in the Ishikari Plain, Hokkaido. The Quaternary Research, vol. 8, no. 2, p. 44-48 (in Japanesewith English abstract).
__ and Fujita, I. (1970): 14C Age of the Larix
bearing peat bed in the Ishikari Plain, Hokkaido. Earth Science (Chikyukagaku), vol.
24, no. 3, p. 110-111 (in Japanese).
- - , Mino, N., Yamada, G., Fuzita, I. andOnoe, H. (1975): On the plant fossils from

Explanation of Plate 8
Fossil remains of Larix kamtschatica (Rupr.) Carr.
Cones, x1.5; Loc. no. 1, Yosumizawa, Assabu-machi, Hiyama-gun, Hokkaido, Riverterrace deposits; e-j show flattened cones.
2a-f. a_ cones, f long shoot with a cone and short shoots, x1.5; Loc. no. 2, Higashiyama,
Esashi-machi, Hiyama-gun, Hokkaido, Jinya terrace deposits; outer parts of cones
somewhat destroyed, e and f lacking upper part of cone.
3a-i. a_ cones, x1.0, f-i cone-scales x 1.5; Loc. no. 3, Ootai, Nango-mura, Sannohe-gun,
Aomori Prefecture, Sambongi Formation; a somewhat flattened, b-d somewhat
destroyed in upper parts, band d opening cones.
4a-g. Cones, x1.5; Loc. no. 4b, Kanamori, Hanaizumi-machi, Nishi-iwai-gun, Iwate Prefecture, Third peat of Hanaizumi Formation.
5a_. Cone-scales x1.5; Loc. no. 4b, Kanamori, Hanaizumi-machi, Nishi-iwai-gun, Iwate
Prefecture, Third peat of Hanaizumi Formation.
6a-o. Cones with various shapes, x1.0; Loc. no. 4b, Kanamori, Hanaizumi-machi, Nishiiwai-gun, Iwate Prefecture, Third peat of Hanaizumi Formation; g, k-o outer parts
somewhat destroyed.
7a-j. Cones, a-g x1.0, h-j x 1.5; Loc. no. 4c, Kanamori, Hanaizumi-machi, Nishi-iwaigun, Iwate Prefecture, Fourth peat of Hanaizumi Formation; h-j enlarged figures off, band a.
8a-r. Cones, a-k x1.0, I-r x1.5; Loc. no. 4a, Kanamori, Hanaizumi-machi, Nishi-iwaigun, Iwate Prefecture, Second peat of Hanaizumi Formation; j shows transversed
section, 1-0 somewhat destoyed in outer parts, b lacking upper part.

Figs. 1-8.
1a-j.

Plate 8

SUZUKI: Larix remains from Pleistocene strata

3

6,"0,::•~-#Il..:,. .'I

hJ ,, -.

. ,r

Larix remains from Pleistocene strata
Quaternary deposits in the Oshima Peninsula, Hokkaido. Mem. Hist. Mus. Hokkaido,
no. 9, p. 15-21 (in Japanese with English
abstract).
- - , Mino, N., Yamada, G. and Nakata, M.
(1978): On the plant fossils from Quaternary deposits in Oshima Peninsula, Hokkaido, II. Ann. Rep. Hist. Mus. Hokkaido,
no. 6, p. 13-20 (in Japanese with English
abstract).
Yoshida, T., Ito, S. and Suzuki, K. (1969):
Quaternary chronology along the middle
and lower courses of the Abukuma Riverin the southern part of the Tohoku District,Japan. Monogr. Assoc. Geol. Col/abo Japan,
no. 15, p. 99-125 (in Japanese with English
abstract).

73--and Suzuki, K. (1981): On the Quaternarystrata in the southern piedomont area of
Mt. Bandai, Fukushima Prefecture, Japan.
Ann. Rep. Synthetic Study, Fukushima
Uniu., The Nature of Lake Ina wash iro, no.
2, p. 15-26 (in Japanese with English
abstract).
- - , Ito, S., Shirase, M., Hori-uchi, T., Manabe,K., Suzuki, K., Takeuti, S., Nonaka, T.,
Nirei, Y. and Nirei, N. (1981): On the
Quaternary strata and plant fossil assemblages in the central Abukuma Mountains,with special reference to changes of vegetation in the southern Tohoku District during
the Last Glacial Age. The Quaternary Research, vol. 20, no. 3, p. 143-163 (in Japanese with English abstract).

w..

Hara
Higashiyama ·JfW~. Kanamori ~:Jiti, Kamiza Mlm. Kori ~.Jrr. Kumoba ~~, Nakanoiri 1"1' /:1\, Negishi trU1, Ogawa IJ\J/I. Ookawa *111. Ootai *>Jl, Ozaki ffillir;f, Saru-uchi m~,
Sunagawa jiyJ/l, Takatori i%1&, Wakamiya ~Y,cf, Yosumizawa ~~'Ilif{cc

JfUt fI *O)~~mflf.: Larix BHtTi- <Ic.l&ttf-*Wlft:~<·I;::~''1 Q Larix ~O)7t*J: *~t
fl *O)~mf.JEi.J\I?PE U.:: Larix ~O):&&~ JHxO) ft:fi 0) ]f~~liv!/'t1'!i'i~d9l:JH. . t.::o .:cJI. I? U:. 200)m':Efm (Larix kaempjeri (Lamb.) Carr.
L. kamlschatica (Rupr.) Carr.)L.
d. kaempjeri (Lamb.) Carr. f;::IIilAt;l;Q~"llt!f!Q'HI.Qo 200)cfi1H;::"i1J.i.!~nt.::ft:fi'1-t'""-c.tili:*~).k1YJO)J1EI\1'ii.J'I?1.'}I?Jtt.::o t.::t':' 100) L. d. kaempjeri (Lamb.) Carr. (;::.ltr,c~J1Q
ftllb~il1T Wlt.'> Q ~ \fi'f' JDJO) J!:mtltO)jillf,'ili'l? ~ I? -C ~'Q 0 L. kamlschatica (Rupr.) Carr.
e!:: L. kaempjeri (Lanib.) Carr. O)J1El!I[(j~7t;(li~IlIHi. ~:(£J: I) ~ i&~7.kJtij1&~O)~1!1H;:::t;~'-C'1, t.::i.J~H':'J: 1)4~i[[L-C~,t.::,:ci.J\tliiji~~nQo
J1;:;f;: IiZYil

c

n

c

74

Keiji SUZUKI

Explanation of Plate 9
Figs. 1-13. Fossil remains of Larix kaempferi (Lamb.) Carr.
1a-c. Cone, xl.O; Loc. no. 5, Ogawa, Shinchi-mura, Sohma-gun, Fukushima Prefecture,
Fifth terrace deposits; a oblique view, b lateral view, c apical part.
2a-c. Cone, xl.O; Loc. no. 6b, Negishi, Kori-machi, Date-gun, Fukushima Prefecture,
Upper Part of Fujita Formation; a-c lateral views from different angles.
3.
Cone, xl.O; Loc. no. 6a, Negishi, Kori-machi, Date-gun, Fukushima Prefecture,
Lower part of Fujita Formation.
4a-c. a, b lateral views of cone, c long shoot, xl.O; Loc. no. 7a, South of Kori Station,
Kori-machi, Date-gun, Fukushima Prefecture, Upper part of Fujita Formation.
5a-c. a, b lateral views of cone (Outer part of cone somewhat destroyed), c cone-axis,
xl.O; Loc. no. 12, Sunagawa, Inawashiro-machi, Yama-gun, Fukushima Prefecture,
Sunagawa Formation.
6a-c. a-c lateral views of cones (Outer part of cones more or less destroyed), xl.O; Loc.
no. 13, Nakano-iri, Konan-machi, Koriyama-City, Fukushima Prefecture, Konan
Formation.
7.
Cone lacking apical part, x2.0; Loc. no. 14, Ookawa Ri:ver, Bange-machi, Kawanuma-gun, Fukushima Prefecture, Peat bed overlaid by Holocene gravel.
8a-c. Long shoots with short shoots, xl.O; Loc. no. 11, Saru-uchi, Takine-machi, Tamuragun, Fukushima Prefecture, Upper part of Saru-uchi II Formation.
9a, b. Cones, xl.O; Loc. no. 10, Hara, Katabira-machi, Koriyama City, Fukushima Prefecture, Lower part of Ootsuki Formation.
10a-e. Cones, a-c xl.O, d, e x1.5; Loc. No.9, 500 m north of Kamiza, Motomiya-machi,
Adachi-gun, Fukushima Prefecture, Lower part of Ootsuki Formation.
11a, b. Cone-scales, xl.O; Loc. no. 9, 500 m north of Kamiza, Motomiya-machi, Adachigun, Fukushima Prefecture, Lower part of Ootsuki Formation; a outer side, b inner
side.
12.
Cones, xl.O; Loc. no. 15, Cliff of Kuboma River, Minamikaruizawa, Karuizawa
City, Nagano Prefecture, Silt bed overlying Kumoba punice flow; middle one lacking
apical and basal parts.
13.
Cones, xl.O; Loc. no. 16, Ozaki, Egota, Nerima-ku, Tokyo Prefecture, Ekota Formation; middle one lacking apical part.
Figs. 14a-c. Cone remain of Larix cf. kaempferi (Lamb.) Carr. a xl.O, b, c enlarged figures,
lateral views from different angles, x2.0; Loc. no. 17, Takatori, Nakano, Fukushima
City, Fukushima Prefecture, Takada Formation.
Figs. 15, 18. Larix kaempferi (Lamb.) Carr. (extant) for comparison.
15.
Cones and long shoot with cones attached to young tree cultivated in ground of
Fukushima University, Matsukawa-machi, Fukushima City; x1.0.
18.
Long shoots with cone and short shoots attached to tree growing wild in Mt. Yatsugadake, Nagano Prefecture; xl.O.
Figs. 16, 17. Larix kamtschatica (Rupr.) Carr. (extant) for comparison.
16.
Cones attached to tree cultivated in Nopporo Park, Sappro City; xl.O.
17.
Long shoots with cone and short shoots attached to tree cultivated in Nopporo Park,
Sap pro City; xl.O.

Plate 9" from Pleistocene strata
SUZU KI "" Larix remains

a

6

• b

"

24

75

PROCEEDINGS OF THE PALAEONTOLOGICALSOCIETY OF J AP AN

B *i5"~!ffIJ~~iIJ.ti: 50 f.i.I~~2~:rt!ll! • *RH~@.A.~;~

A*~~.~~M~W~~~~~A~lUmn~Mm~a~~O)rem~m-M~~.~.~-~/J~ 1985 if. 2 JJ 1 A t.::.Il":V:.fi~~IW-~J.lJln-e lilJlm ~ il-

t.:.o
1)

rm~O)li'F

2)~.N:~ii''f· ............. 1IIIIY.i*i\i~· ~mjFH~i'fJ • *~ fM-t......... .

~tiifjili;tR 1':1 ifHe JEft1 i 0) f,l'f;a HM}3) *11{rR8¥· ....................... j1!jIJji'flx· ji!jHl

4):f,~t~:N:~W

5)fll] \[/I.ft1*0):ft~t.::.¥m:~;JAP.Mti1
mjljiillil'i~ r.m~~*t.::. i '?h~RjjJ fE:WPi"f!~6)7)

IH.f;J'i-rfl~O)iW

il21tm~'i~

B *i5"~!ffIJ~~ 1985 ~~ • t€~
A *rl;~E~{}~:ft {f.~ • r.€~/J; 1985 ~ 2 Jj 2 n,
38~~ftM.~.m~lU~~k.R.$~~W

c. L.-cfj~Hm~11t.:. @~:?';. 279 :f,).

'I'~t trilh1ii,

1(,CAf.,·Ul!!J~.~~~fu~~.:V:E~~D~~~~~A 19~,
'I ':7It.-) ...•.... *~:;j"JYlJTj· ~m~1fi:I:

m6Ii1)ri"~/{~ / P~-~Ji(i8.26-9.1,7}1t.-7l~-)(VI I·P·C)(19~,............ ,:·~mli'l

1Jr12 F1Jr<t~iiM~4.~~ (2nd I·O·P·C) (l9~,8.18-26, 7}1t.--}f ~ - • .x. I: -'E' ~ ~ ~) ......
...... #lIHJ:~mt.· *Hi.rf!Jl • itlifl1i't1)(v:iIJ.13f,
3rd Latinoamerican Palaeontological Congress(1984, 10.14-22 ;< 9'- ~ :z) ........ ;j'.Ni.f1lfJ

tij; }3IJ~;~

Cythere ~ (fl'1f~$) O)j'IH.fiJ!CI<.J7};{li C. Hl~}{t ..

.................................. itIrfr1111Z~t:;t'f-n *i1!ifi!,jF~i'fM~ 0) mj!t]J\;~E1{JLrtHrn i0)

millt7t:fli ........................ 1i<.J.lMU!Jt!

Ar.~

c. {tTl .......................... 'H1Hjf\n~50 f.i.I~i2~tt: &~;~
IJ' ~ t.(/J\ ~ tdtTl .................... ~iff.?lnE:A:~tdM~~IUjC;-t~:ItH~~lllii~.............. JHtJII~f11;)./ci'''III.'f{"\';O) fI
fUiHl'fi:kI:i/J.

* ......

liIIG

Dipteridaceae from the Upper Triassic Mine
Group in Yamaguchi Prefecture, Japan (4).................................. Naito, G.
~fQ,fl"'!it',ii'flH.iff!J.',iY-iJ;jWI, (cl~~f (Baegunsa) ~l I) Lobatannularia I:l:/J'=-.fi:*'CJlttr:M¥tJO)~Q . ................... *HJ.ttJij. ~ ~~~$JH-f.1itl1 Cfffllr:=Jim*) /J·GJ2iII.f:l Lt.:. Cheirolepidiaceous conifer ....................... .
· ., .. .. .. .. ... Jj;:Hj.rf!Jl· T.lf*lf- • )1'UJ:m y.
fJH"N'jf,f Cffflls]ffi*) /J·Gi1f.:UI Lt.:. NilssolliaMO)l{IHW)ll ........... . )..:~{*~X • *ttJ!f!Ji
f&JVJ1Jr:'E f\:0){t:rijji'i~4llf, i- 0) 2 •;.~~~1fr~~I:l:It.tfIH§·

10.8-11,· ................... IJ\,liHll%. Barnes, G. L.
X (,l1o.1:yloll O)ni(Jj.f:{:m~O),fffiJlllliltl'::' '?t '-c ....

.............. JH~iN/l& • i'fl1<J &J T

~t F1 *O)i~'m~*e 7':T·H (Fagaceae) {t{i~O)]l}19tH .............................. j/jijjj:hU~.... i1tr.-ll- 'JJ

jj(i~{}*;f:fti\iIUf;:~ft ~ r.a:ml~l;: '?t '-C)./[7 ~

7(7)",,, A ~ ~ 7 A *2r!i1:~J.I !tl!.I!I!/.::. /MIT

~ 2 • 3 O)rm~.................. mJllj')lf-J'!~

Cretaceous Corbulidae from Japan. Part II,
Caes/ocorbula and Nippollicorbula . . Kozai, T.
Two new species of the Lower Cretaceous
corbiculoid in Shikoku ...... , ......... , .. .
· ., .. " ......... TashirJ, M. and Onishi, T.
On the Plica/ounio (Cretaceous nonmarine
bivalvia) from Korea .............. 5i'i j~*
A note on an inoceramid species (Bivalvia)
from the Lower Coniacian (Cretaceous) of
Hokkaido ...... Matsumoto, T. and Noda, M.
A new species of Inoceramus (Cordiceramus)(Bivalvia) from the Upper Cretaceous of
Hokkaido ........................ Noda, M.
~tifijJtl+:;f • :k7'1k~t~J::$Silli*O) {tfi~rr· .. .. .. .. .. ... 111;jj:1!JI A • :'Y:P.Y.'ll,)tl • t'l:*JtJ'l~~~iliJ.t~~~O)~$S~*~~Gh~~~~4WJlIf~~ Urmm.................... ,)lImn,';'!!

76~~~7~~~1~.ftffi~&~M.~~~~~lf?; .................... ~r'J~inf;· jJjIJnfl-);X;

7 '7~~~::t A ~ '7 :1 - jl -t:-~ 1-1:J!!,~f9f!':;Ii .::.lJJH:.trllJt2thkalJfw,c 7 ~~7'1 H'lI: ....

~~*~~1:=~fl.~m~~1:.~-~m~
fnJJJlt~$*'2:'{llj L -C - -t:-~ 1, 1:t'l.:}.; J: V:· . . . . . . . . . . . . . . . . . . . . . .. ~iHto'(;' H ('!.!'Barremian ammonites from the Ishido Forma·tion, Japan .................. Matsukawa, M.
Some gaudryceratid ammonites from the Cam·panian and Maastrichtian of Hokkaido ....
· . . . . . . . . . . . . . . . . . . . . . . . . . .. Matsumoto, T.
E~'h\'~~7~-'E:7'11' Nipponiles ~J'I!,1U;@..................................

j,\';j*I;;r.

Akiyoshiceras, a new Carboniferous goniatitefrom the Akiyoshi Limestone Group ..... .
· ............... Kyuma, Y. and Nishida, T.
Morphologic analysis of Nautillis pompilills
from the Fiji Islands ................... .
· ..... Tanabe, K., Hayasaka, S. and Oki, K.
Radiolarian assemblages and their relationshipto the oceanic conditions in the Northeast
Pacific ...................... Yamaguchi, M.
Nassellaria (}/di,;:!i~) ~1J..Jtmt,\};~!':5HJH:'0"-C.................................. VrHT'/ITJ

rl *~ y "- '7 ;,y,1j!<n,;:~1t1i5HH: ............. .

&Jf;~~M f*...................... :t$:frJli1;c

J!ll'!z~Bl~5J'::ffi!.:iIE;IK ................... .

.......... .... ,jJ]~l'ff)-)i1i:'

rn.Jl:: --t:-~ 2,i1i* ~. ~EB ~711ff CIlxJH.iRAiJ> G:J;..t:: -7 T/:

71' -1 (Coecella chinen sis) !.:;Ii;li' ~ 71' 1 (Pha.
cosoma japollicum) ~1: ffl!iXffl& .. , ... ~8:l ~ifv;I*1I!.!J¥.o Cyclina sinensis ~J!~!z1:i£'~Jif:Jt:ljlm%'€ ................................ TU-In:;Ii~~&.~!.:~~~A~~f*........• 5.~=~J'lml:9-'~tli~M!l/~31- /~icll:5Ci't; .. j('l'fWt:ic
F:I *iIE Volachlamys ~:i}fJi bf!W:. ('f-~n ....

. ............................... -. Ji7lc til

0'ti'~*iff&i:ILIllJf\iIE~~':::*fl::.fil:''-C .. - ...
· ............. ;;-'m.:::a~· m* ] I . it ~Jl~.~~, W~&J!i$~~~~~M~m~ M~.~
Wi' iF.MIJl..r-& ~ Wi' Ij:.f~ ::: (rJ !1~ II: 1"1 .......... 5 W&1t fJ}
T;jt.'j~~ :wi'~':::*iMTjJI"I'I'~ '7 .::.I:'J: 7.> 1=J.R11:
E ..................... · LLIJ:J7!fz' ~iR~tIsocrinidae ('7 ~ ;:L y) ~Jf1!L~!.: 7J\'::ffi~.tlli9.:R'J~

11: ................................ j;j-oll\i'E· .. .. .. .. .. .. .. .. .. .. ... 1i~IIi;j X{)· Nt 11[1JiU)dlll fdl njIUIfJJ!i~ 1*j,CIiLt I) iIE-j 7.>y.~~K71~-t7.>~~M:.fiJj}(~#~~~~'7'7"- '7 w,c Ii!< 1t,;:!U ............ J8' III 1m !J) • .!bl: jIIilSt-.
Paleocene Radiol:lria at Site 384, DSDP (j·r.tn.... j(M~.·tt .~·j(M-~·W*~~-1 -/~ ~ :1--tl'1t'2:' ffl' ,t:: llU:i'F~ 1t<:MtIJ:1R~i#k,f[
iMiJtt .......... H:il#~IHt • £t:lj:fID:~ • 'J,5{t--:.
-1 -/ -It ~ :1' l1·m ~ 7J; -t t,7J\11i1L 11: r::J 1'i: f= • Hi'! i~ .::'H"1:IlJ(ifllhErjufl~J'I:'I:~{I:-fi!.: TiJj}('b- ....... .
.. .. .. .. .. .... 'Hlj i~= .,!jl, )fir-V-' J.mifn-)'( fI• i~';JLLI~lIr{ • :Jl'I=l!'U= • fj'it:flllp, • :.fiMllif7\• f'l' =-.~I\(:tiJ' KI-184- I &.:JIDtiiiB!!Jlfi:t,·
F:I *Fnlill~ibiIJIji[ril9<t\idI:1-1 ......... ,1H!Ej!t,:=:YrEJ';j(li,'fill']oI:.;'5';UL7.> rhodoliths ~*!i'ij~I:'0"-C.................................. jH~r,H)(mow.............................. Nishimura, A.
Fusulinacean biostratigraphy of the Akasaka
Limestone, Central Japan ............... .
· ................. Kawai, K. and Ozawa, T.
Gradual evolul ion in some neoschwagerinid
lineages from the Akasaka Limestone ....
· ................. Ozawa, T. and Kawai, K.
WifRTi&<{';'~ Parafusulilla ;ir::~;)JJj'~!3~I:''-C· ....................... {:tlll~ay.· flli?J,~'H'
Tethys and peri-Gondwana faunal provincesof smaller Foraminifera in the Late Permian· ................. Okimura, Y. and Ishii, K.

0't)J} ;j,lj,m!t1uJ f.:kLUJII.I::iJiU:,:}.;(rJ 7.> -fiJj}('/U: I) &T7.>.:::,\'Hc:1/ F'~ H:'0,'-C .......... ..
......................

t£1I$!~ldJiJ' 'j'~(!f-r;tx

I~JitJJ/JmIWiril, imIW,~MJ: I) 3t1i1 U.: =1'Hc:1/ f ~ I, .............. 1'If~'I5~m· ~[J~-nI5
Miocene ostracoda from Mizunami, central
Japan. . . . . . . . . . . .. . . . . . . . . . . . .. Yajima, M.
Plio·Pleistocene ostracoda from the Tsugaru
Basin, North Honshu ............ Tabuki, R.
/\f~ilij;jtirllt:'71:;(ff-t 7.> Jur;:~ .......... 't;·Iw.f~Jn
Recent marine ostracodes from Korea ..... .

. .. .. .. .. .. .. .. .. ,~ ....... " ....... -lli ttf..j;~ 7WYU'¥f~I:.~-t 7.>#Ji~*:I-............... .

fMortality of a Pleistocene solitary coral,
Fungiacyathus kikaiensis (Yabe and Eguchi). ................................. Mori, K.
'1'1lfi[ll:~{1:7i-lt / ~@\ ..................... .
· ... l"l[Jf~A' :5I~/l'mm) • i~I33~ffi:± • 'f'Il!~ciN>'ll.M[jJliiI!;~ml~:;ufi(t-lt / :1-}Jj~lffl;l~.jili ",,)r. ,;';Jm.iiaI5 • *'.§5C1l,1........................ · _.
............ UlrJf,fZ' ~tH~t:~· t~~~Jlj'i:· .. .. .. .. .. ... rl';f':1~

m~ ~ :1'"(18'1.:?

.A.tlliK~(rJ7.>A/.~Jj}(W~~ffi:}';J:~~5-l1.H:'0"-C ........................ 1"l''l'fj~;;1;

Notes on the genera Labechiella and Labe·chiellata (Stromatoporoidea) ............. .
· . . . . . . . . . . . . . . . . . .. Mori, K. and Kato, M.
Heterocora/lia from the Akiyoshi Limestone,

77Southwest Japan. Part 2. Biostratigraphy
and correlation ................ Sugiyamll. T.
A new tremllnotiform bellerophontllcelln fromthe Devonian Fukuji Formation ......... .
· .. .. .. .. .. .. .. ... Nishida. T. and Niko. S.
Mode of life of an open coiling gastropod
St'mitubina sllkoi. n. sp. from the Silurianof Shikoku. Japan .................. Kase. T.
fYj lff~~tl :i1IJt!!1l) JH';'m /:"ic'r,jiJ~m Clwristites . ...
· .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. ... IIIV'~i:ijj-Jlt~"iJtl!f{;jJllill){iE;~*clJ9ilh!.m Sirialijera. Ci·
ganloproduclus .......... nIiI~*ltl- • fJIII!¥- :ill(
A new Siluro-Devonian brachiopod fauna from
Fukuji. Gifu Prefecture. Central Japan ....
· .. .. .. .. .. .. .. ... Ohno. T. and Hoe. G. D.
7. 1:.' 'Y -;/ "" It- IT /' IJi Il)"" It- ,l, ;.y,rl' \.::..7,.. GJ1 t.: 1T~ilPlf~rt.lJl Il)tl1:.tl.~............... .rI'tHJI::

M~mW~ffi&~.Il)~~fim*Rffm~m~%!I~.......... ifHR*l{li • tKii*-ttl: • IHj~ Ii~tjU+l ;~·rf-.F;')llftJ·~.J 9tJi!.~J1t.: ~im<(!rff.('I.~j7::lP

7 1'7 7, Il) iiJ{',HU jI.::. '0l ' -C.......... ..

• .. .. .. . • .. .. .. .. .. ... Wr]I~.i)- Jdt • JHt!ll iH11
hr.;iwil!kO)itjtNI!TiIJ~-!JjtH.::. '0l '-C Ar~mz' iilY',~\'Jl\

Correlation of mammalian fossil bearing deposits. southeastern Arizona. U. S. A. . ...
................................ Tomida. Y.
m; J\'ij ,...·1 ttl' ~fl.~ ,'ldt:{ i I'::' '0l ' -C .......... if.: If(~
rJei';-~9tHf:{il'::' '0l '-C..................... .

............ !IlF);lj'~1~· J~fiJJI;t,;:f11 • 1,(;llfll i1Ji
Ichthyoliths from deep-sea sediments of
Penrhyn Basin. Southwestern Pacific Ocean...... _....................... Nishimura. A.
-f{fllflf1!.lr~tr('#1l) 'rhf.n~l('1 'I'::' ~~ ({ ~ J"L -C l ' t.:Osteocyte Il)fUi ........ ~"I"iik • i'iMfJ)j"f:tt":l't:'I!£WJ1','m fTlJ'(illi n 9r',II'!J: I) P~IH Lt.: ftli'l'j'
el'll) Osteocyte 1'::''0l'-C .. ~IU"iik· Mif1IJ.i~l:~~MU±-=-:r. /' ,;";" Il) lli'nll/fnx tJ·G.7,..t.: 1'H~J1:1l)
Iliff\; 1rft c (;M Il),HlHt I'::' '0l ' -C ...... ,NI1l ~tn'
JL1+1(J!j;lJirnIJ.~:1 7Il)MHJr. ;ell) 1. nt/l:-fjIL!1~.................................. ~tjH n
IIU:. ;ell) 2. Para/ia su/cata 1l)'l:)--11i c ),j:iiLl;j'-i *-Il) ii1l J~ ........................ {;tHY- 1"1"
fill 1: . .7c ll) 3. E[1(fI-r /' / 7") /' '7 r /' ....
· ........ " .. .. .. .. .. .. .. .. .. .. ... ),UllfIJi

fiIll:. ;ell) 4. Jjl(llt~ .............. i1'~~H):-=::f!/lIfill: • .:'ell) 5. i¥-.iQ£i'f:tf{L!I~}.; J: U tI"Uillij(:Y:{1It ................................ )cJi';J.!.\;n[] *iW (rr~.JttJjt) :1 71l)Mi(j:Jr. ;ell) 1. 1TIL!1~}.; J: U.fiIR.'f{-r /' / 7 '7 /' Y r /' _.........
· . . . . . . . . . . . . . . . . . . . . . .. JJ"}UCt!lM1~' ,r:j Ii 1f&:I1{{/fijJ:. ;ell) 2. ~)(. !I;Ji~=.II~jf\:;ll)ilJ.HMWlMi(j:Jr.................................. 'j'* t'1'l-f~tY!il; ~t~Ir.f,1l) W[~'::*Ii".i:rt; c 'I,J!:JjrlrifrjjUt~ftfilir~~ .... 11/1.11.12 • tHR ,*. (Jt~{l-tl=.
fl~f;tiM~sr'::'J: Q ~t®:kiJZi:r.~.f.ifrlittJ1fkll) rlil~m~]I~ .. - ........................... 'h'R f~

An evolutionary trend of Rl'licll/ojl'llestra
and its related taxa based on biometrical
data ..... : ...... Nishida. S. and Taguchi. K.
m~~1A/7{-=-~A.Y~-~(Il) 18 WILIl) Jf~J1~ c 7 IJ ~ ~ - -)-•• n~•••..• t).;/ii'i] ~1t:

Nannofossils from some marine mangaese
nodules. especially on their age and growthrate ............ Yahagi. H. and Nishida. S.
k.~~·m~~~~mllfll)~~~R~Ilf~..
. ............. Jl-\ii#rWIT·IUIIJ.fZ·~tm. n:'!('JZM"ifrtfL::::;f,if&ftfil'."ili4':1l) lJU,fJ. ;ell) 1.
~j~i"ttfIL.!1!.'l-}'Il::I'::'J: Q IHJlli• ~:jliLmr.tll)~
THrYtjti WHIr ............... --....... i{;* t~Irij I: • .7c ll) 2.

'l,jtjl'I'W[/lt.ljtfirir.ij~MIl)t11IJjf-f~.................................. i{;* 1;
A standard Late Cenozoic microbiostratigraphy
in sOllthern Okinawa-jima. Part 1. Calcareous nannoplankton zones and their correlation to the planktonic foraminiferal
zones ............. Tanaka. Y. and Ujiie. H.

.f:m,H,',rll) ti1:::::*~I;;11l) tfIL!1Htfll'::''0l '-C ('1'#1) ................................ IT /il,nf.ltI
H ,,j,:;Jf,: Elphidid fl-u"('I:tjIL.'1U'::''0l'-C .. !f!rHfiU
lftH'U:if."'J1l) JJ.'('J=.tj;SL!1~ /If ~~-.7c Il) 2. f,4j'I'tJ-!;tifl• •• •. •. •. .. •. .• .. •. .• •• . . •• •. .• ••. )...:. ~-:;:.L.~ jfg
Inner structure of some species of C/obigerinll
and its phylogenic meaning ........ Ikeda. T .
n@)tl!i".i~'n::I'::' '1')~,-fQ JlX./l:.111L!1Ulf:!H 1.::..7,..GJ1 Q ~l!(I'~ 'l'Ti-.!:l1. !~!f'::' '0l ' -C ........ ~t!:Jl. to(;f1!jjj$iiti';-1l) Lepidocyclina W[i!EJlli ......... " .
. .. .. .. .. .. .. . . .. .. .. ... rX~;:~fl-':l: [~:1:fl,:i,Jf*-I.J'GIl))..:~HjlL.<1H':'0l........................

,-c ......... .

t:l::AI"~l'l!\' *ft~,t;iElWHltJli1; Il) 1iIL.1!,'I-=.II'1!f. .............. 1').; :J.t~~ l'!l~n111::jlljfMjlH.::. 'l:)--;(lii" Q (jllE*1l) ?£(1tTi.fn c Vt

til ................................ I,im!~

Geologic events across the Cretaceous/Tertiaryboundary and recognition of the boundary
in eastern Hokkaido. Japan ........ Saito. T .•Kaiho. K.• Yamanoi. T. and Okada. H.
Foraminifera from the Cretaceous/Tertiaryboundary interval in the Mokawaruppu River
section in eastern Hokkaido, Japan .. Kaiho. K.

78";f;=~" O)S@~~ (~ra"J\.~)
Ut~;IiA ('t(i1.¥iJ.j ~ • 111JlIlllj'i"fi •1WJi'ffln1J E • t~ f]J fU (::)
1!tRtA~W;tQ J: Uili'9::t ~ illVJJ]""" A ~ "7 ::1 - ~q.::. J: ~ ·iJ;~t.ff},,¥= ........ ~11fmlJg1B
Cladistic analysis -t'9~i:;JIH9IJ-fffff~iJJ!I'?J~f71jcc L..-C ................................. .
. . .. fill ~. 7-.*iHz • -=:tXlf:il=- • I1Ulfl;A*~~Jf~rJli:'9~.IlI!.:c 7" IH;:'''?\' '-C ........ j1ij1IlN;t!1-~~rf}"¥=I;:.;tQ~~.:c7"/t.- {tl;:'''?\''-C -j!UJI*c
L..-C'9~~"¥=A9tl~~- .... 1lJ)nj$;);;. ~BHU(::
k${tifi~6U

New members approved by the Council Meeting held on June 23,1984
Ordinary Members
Arai, Tsuneko; Hayakawa, Hiroshi; Hayano, Hisamitu; Itoh, Hideki; Kim, Jong Heon;
Kojima, Fumitoshi; Komori, Kazuo; Manabe, Makoto; Nakagawa, Tohru; Nikaido, Akinobu; Ohkura, Mitsuko; Okada, Daiji; Saegusa, Haruo; Shibuya, Masamichi; Shiraishi,
Tateo; Takayasu, Katsumi; Tanaka, Noriko
New members approved by the Council Meeting held on January 31, 1985
Ordinary Members
Endo, Kazuyoshi; Ezaki, Yoichi; Horiuchi, Tadashi; Kawaguchi, Shiro; Katsuta, Tsuyoshi;
Kishida, Youjirou; Kikuchi, Hitosi; Kurimoto, Chikao; Suzuki, Akihiko; Takagi, Kyo;
Takizawa, Kanemitsu; Tasaka, Kuniko; Tokumoto, Tadashi
Withdrawing Members
Akai, Kozue; Ito, Tomio; Kawakami, Toru; Kushima, Yasuo; Nakamichi, Osamu; Naruse,
Takehiko; Ogose, Sunao; Shibata, Toyokichi; Shimakura, Misaburo; Shiraki, Takayoshi;
Shuzui, Haruo; Takenaga, Shigeo; Tsuruta, Sayuri; Uchida, Nobuo; Yokoyama, Michiaki
Deceased Members
Hisamitsu, Masao; Nishida, Shoichi
Fellows
Eto, Tetsuto; Harada, Kenichi; Koike, Hiroko; Matsuda, Tetsuo; Mori, Shinobu; Okami,
Kazuyoshi; Okazaki, Yoshihiko; Okazaki, Yoshio; Okumura, Yoshitsugu; Ohmura, Kazuo;
Ohno, Terufumi; Samata, Tetsuro; Takeuti, Sadako

~fl

fm

1m

l1!!

fll(

~ilir$.i6~I7J

A

f71j~

*11!i(jTi.V:*~

1985:9=- 6 Yl15. 16 B

1985i:p 4 Yl15 B. 7C.: 113:m:~t*'+ • (tl!

1986i:p1 Yl31 fl-2Yl2 A

1985i:p11Yl30 13~134@l198611'-

i:p:*.~~~1'4'@!$.i6*h(ffI)JthOR~~J;~E 2-4-16

O~ 134IuIWIJ~-CI;t,;..-;/;f. ~ ,;, AFl *~~ffnJ5-1:: ;/ jl -El *il1=.¥.()~~

6"=11=1*

r1t.fi }jXI~x!l:!.Q)5tM • 1=.~rr- • i~·~-E~~&!1I!.--J1ifj[[Q)IiIf5'l:1IX: ~ J: I) J tJ;::-f:<E~n "n'~.

LfltftJ· G1tfM~ Jl.:}.; J: ~~f:l5~ Jl. Q)~*IJ7t:l!!tJl**bH.::.~I!I.::.t.c I) t U': o ~f:l5Q)Flrlt~!tJl-t ~ t.:lJb. 1985M~.Q)**~~Q) • • ~~ffla~KEL~:}.;~t-tQ)-CJ:~L< • • ~T~t~
O*.Q)tL-.i6->:}.;~ IJ L n'~~.i6ffl,j!l\;-CI3*,,¥=*$a-l::;/ jl-

O*.I.::.M-t~rMr-lt-->*H1*: *ttjlf!ij (**"¥=~*"¥=~"¥=fl:~)011\'f~~ Jl.*",Q)J!I!.-Rlt-->I(f;f~1*: 'h~1i~1:. (IE.'iLH~tf¥!.Jug7t~{)
O~~~~·A~.$.i6->I3*"¥=.*a-l::;/jl-~I3*il1=.¥!.J,,¥=.
O.5e.",Q)&.-~~~<~M~-cI3*"¥=• • a-l::;/'-~I3*il1=.~"¥=.~.1*(~.Q)~~~~l$.!:t5!:ftii:h- r~jif)!·ttt.:IUIj~L~T~t'o &.I.::.;i;t.:")~I;t~.fI:lJljiiJIi.*9 (No. 121) .!:JJi(ftiif'FJlltJ:Q):}.;JM\"~$!VA L ~T ~ \, ' 0 m5~c1~1.::.~-t~rR'1,-1t· ;jj):ftii:h -O*.~i:li.Q)l~iml!l~Q)r.~f'l'-It-->J3i:7.Kr'Q)~* (,J:~I.::.:}.;JMt' L t-tJ

:f'I1 OIU?:*"¥=!11!."¥=tmjl!!,ll{,,¥=t!c~)(No. 120 1'::'7f-[f;I~1:Q) n~.!:fljm~~H&txL~;i; I) i-tJ

O~~~KM-t~~ft-lt·~A$.i6-->~~~~.~ • • : .ffi~-(ftffi*"¥=!11!.• • ~."¥=fl:~) ~~~ffm/lfiJSir.I:j*illifJH~: 1-1/~ 12172; PR~ tf-;\r.'Gi 19014)
O"1tE" I.::.~-t ~rn'{j'-It • ~)Z.fth • /~ .,. ? -;J-;/ /~ - ...., 1tEf:iiamtm: jnjWPii'G· E~f1<I~ OU~t:k"¥=!1I!.,,¥=$!mrt "¥= t.' 't ¥!.J"¥= ¥J(7jO
04HQjQ)'!tI.::.j)ij-t ~ rn'{\--It • Hf~I!,lHtRf(-->jtQ)~ • • ~* J3i:7.K :f'I1 (1985 {J'.Jir Q).7;,.):f:l*-~''i:..~,*~

1985'4'-4 Jj25FI
19851f·4Yl30f]
ISSN

~[J

jjjlj

jC

fj

:X. he g ~]\ 1=. 2-4-16
13*"¥=.*f~-I::*;/jl-P-l*)(~~ lJ Pc¥.
he 84780('itt ill; 0 3 - 8 1 5 - 1 9 0 3)0031-0204

B *il1:.¥J.I"¥=:*m.g;.·~c$
XfrA'.f;137~-

2.5 0 0 fIl

f-Il

API]

:1;-

* ffI) ** .m !R
Jj1;~fit.f[~ilijJjjjljf..j(A~tt
('itt

~rli

~ :Ii ~t 2 / 13

ruiW,
0 3 - 9 9 1 - 3 7 54)
1.\

Transactions and Proceepings of the PalaeontologicalSociety of Japan
New Series No. 137

April 30, 1985

CONTENTS
TRANSACTIONS
790. MATSUDA, Tomoko: Bivalve fauna from the Miyanohara Formation (Lower Cenomanian) of Sakawa. Area, Shikoku. . . . . . . . . . . . . . . . . . . . . . . . . . . . ..
1791. NISHIZAWA, Yasuo: Multilaminar colonies of bryozoans from Japan. I. "Ectoproctalith" of Antropora Uncta (Hastings) . . . . . . . . . . . . . . . . . . . . . . . .. 19792. EHIRO, Masayuki and BANDO, Yuji: Late Permian ammonoids from the southern
Kitakami Massif, Northeast Japan . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 25
793. ISHIZAKI, Kunihiro: Ostracoda from the Pliocene Ananai Formation, Shikoku,
Japan -Faunal analyses- . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 50
794. SUZUKI, Keiji: Larix remains from Pleistocene strata of Northeast Japan, withspecial reference to the distribution of Larix in the latter half of the Last
Glacial age . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 64