a -lt"~i.~~~~.:k· ;~tTransactions and Proceedingsof thePalaeontological Society of Japan
New Series

No. 65

Palaeontological Society of Japan
April lOth, 1967

CONTENTS
TRANSACTIONS
516.

517.

\IASUDA, K6ichir6. l\lolluscan Fauna of the Higashi-Innai Formation of
Noto Peninsula, Japan-III; Description of New Species and Remarks
on Some Species ................................... .
I-IA:--!ZAWA, Shoshiro. Three New Tertiary Foraminiferal Genera from
Florida. Saipan and Guam . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .

518.

BuRTON, C. K.

1

19

Graptolite and Tentaculite Correlations and Palaeogeo-

graphy of the Silurian and Devonian in the Yunnan-1\Ialaya Geosyncline..

27

SHORT NOTE
13.

HJGUCIII, Yu.

Eponides

Hit;UCHI, Preoccupied

bo~oen~is

New

Name

for

Eponidesasanoi. . . . . . . . . . . .. . . . . . . . . . . . . . . . . . . . . . . . . . . . .. . . . . . . . .

26

PROCEEDINGS .. . . . . . . .. .. .. . . . . .. .. .. . .. . .. .. .. .. . . . . .. .. . . . .. .. .. .. .. .. .. ..

47

Honorary President ; Hisakatsu Y ABEPresident: Kiyoshi ASANO
Councillors:

Kiyoshi AsANO (Editor of Fossils), Tetsuro I-lANAI (Editor of Transac-

tions and Proceedings), Wataru HASHIMOTO (Treasurer), Kotora I-lATA!, Koichiro ICHIKAWA, Taro KANAYA, Kametoshi KANMERA, Teiichi KOBAYASHI,
Tamio KOTAKA, Tatsuro l\IATSUMOTU (Editor of Special Papers), tvlasaol\IJNATO. Hiroshi OzAKI (Planning), Tokio SHIKAMA (rvlembership), Tsugio
SHUTO, Fuyuji TAKA! (Chairman of Executive Councillor's Committee)
Secretaries:

Takashi llAMADA, ltaru HAY AMI, Yasuhide IWASAKI, Yokichi TAKA·YANAGIThe fossil on the front page is Kueic/wuphyllum yahagiense MINATO 1955.

All Communications relating to this Journal should be addressed to the
PALAEONTOLOGICAL SOCIETY OF JAPAN
Geological Institute, Faculty of Science, University of Tokyo, Japan

Tran:;. Proc. Palacont. Soc. Japan, N. S .. No. 65, pp. 1-18. pls. 1. 2, Apr. 10. 1967

516.

:MOLLUSCAN FAUNA OF THE HIGASHI-INNAI FORJ\IATIOI\OF NOTO PENINSULA, JAPAN-III : DESCRIPTION OF NEW
SPECIES AND REMARKS ON SOl\IE SPECIESKOICHIRO 1IASUDA
Department of Geology, Miyagi University of Education. Sendai

iiErt~l"!li'lltf.ll!"ll\'iiO)iliJ:!•I'lfiiJ'j7j"J(tT:i!tr--III; j#f.JlO)ll~if&:h J: (Ff',FFO)t\t~UfillO)-JS·~i: :<ji:~-::.':1~~ 16 ;flff•T!:>2~~il& Lt.: fl!!. r..:Ciill•fi 4 'f«<O):!/!l~ :::.·::>1.- ·-c flJI;i;~i-~f'Jt;. ·:d..:,!\'1 ffl*-)!!f,f)imensions (in mm} :-Family Potamididae

HeightDiameter

Genus Cerithidea SwAINSON, 18:10

11. 0*
4. 1

ca. 7. 6
2. 6

ca. 6. 0
2. 8

ca. 4. 0
2.0*-holotype

Ceritlzidea ohiroi l'v!ASUDA, n. sp.

Remarks .·-Cerilhidea
tokunariensis
p. 162, pl. 26. figs. 6. 7)
from the Higashi-lnnai Formation at
Loc. No. 12 resembles the present new
species, but is distinguishable from thepresent one by its low. narro\v, fewer
longitudinal ribs. fewer and faint spiralthreads and less rounded whorls.
Type locality :-Loc. No. 30.
Occurrence:- Type loc.-C; Loc. No.
3-R: Loc. No. 24-F: Loc. No. 32-R:
Loc. No. 39-F.

Pl. 1. figs. 5a-b, 6a-b

!VIASUDA (1956,

Holotrpe :-DGS. Reg. No. 4577.
Description .-Shell small, moderatelv
thick, turreted, with nine whorls . tw~to three younger whorls lacking; spiralangle about 30'. \Vhorls moderately
inflated, separated by rather distinct,
impressed sutures: surface \Vith elevated,rounded, granulated longitudinal ribs
and numerous. rather distinct spiralthreads: longitudinal ribs subvertical.
nearly equal to their interspaces. about
14 on penultimate whorl and 16 on bodv
w·horl. sculptured with spiral threads.;
spiral threads of distinct, fine threads
and fine intercalary threads broader
than their interspaces. Base of whorlwith two rather distinct sutural bands
and fine, unequal revolving threads.
Aperture subovate; outer lip notchedposteriorly; inner lip indistinctly defined:columella subvertical; canal short.

Genus Vicaryella YABE and1-!ATAI. 1938

Vicaryella ishiiana (YOKOY.-niA), 1926
Pl. 1. fig:;. la-b. 2a-b

1925. Cerithium baculum YoKOYA:\1.-\, jour.
Coli. Sci., Imp. Univ. Tokyo. Vol. ·15.
Art. 5, p. 12, pl. 2. fig. 6 (non YoKO·
YAMA. 1924).
1926. Cerithium ishiianum YoKOYA~lA. ]0111'.
Fac. Sci.. lmp. Univ. Tokyo. Sec. 2.

* Received February 23, 1966; read September 25. 1965 at Nagasaki.
1

2

Koichiro lvfASUDA

Vol. 1, Pt. 7, p. 218, pl. 28, figs. 11. 12.
1935. Cerithium (Proc/ava) otukai NOMURA,
Saito Ho-on Kai Mus .. Res. Bull., No.
6, p. 227. pl.l7. fig. 17
1938. "Vicaryella" ishiicma (YotWYA~tA),
YAllE and IlATAI. Sci. Rep., Tohoku
Imp. Univ., Ser. 2. Vol. 19, No. 2, p.
169.
19,14. Vicaryellaishiiana(YotWYA~IA).
0YA~IA
andSAKA.
Shigenkagaku
Kenkyusho, Bull., Vol. 1.. No. 2. p. 139,
pl. 14. figs. 5. 6a. b, 7a. b. Sa. b.
1960. l'icaryel/aishiiana(YOKOYAMA).
KAMADA. Sci. Rep .. Tohoku Univ., Ser.
2, Spec. Vol. No. 4, p. 28-1, pl. 31. figs.
·la, b, 8. 9.
1962. Vicaryella ishiiana (YoKOYA:O.tA), KA·:\!ADA.
Palaeonl. Soc. japan, Spec.
Papers. No. 8. p. 152, pl. 18. figs. 15. 16.

Syntype :-Geological Survey of Japan.
Remarks:- Vicaryella ishiiana (YOKO·
YAl'IIA) was described from the Miocene
Mizunami Group, Gifu Prefecture under
the genus Cerithium. Subsequently it
was reported from the Miocene Nakayama Formation, Fukushima Prefecture
in association with Vicarya yokoyamai
T AKEY AMA and also from the Miocene
Ajiri Formation. Miyagi Prefecture
together with Vicarya yokoyamai TAKE·YAMA (KAMADA. 1960).
On the other hand, Vicaryella notoensisl\1ASUDA was first described from theHigashi-Innai Formation at Loc. No. 12(MASUDA. 1956). It was subsequently
recorded from the Kunimi Formation,
Fukui Prefecture (KASENO, 1956), Orito
Formation, Niigata Prefecture (KAMADA.
1960) and Kurosedani Formation, Toyama
Prefecture (TSUDA. 1960).
In 1960
KAMADA pointed out the associatedoccurrence of this species with Vicaryacallosa japonica YABE and I-IATAI,
Vicarya yatuoensis YARE and HATAT or
Vicarya yokoyamai TAKEY All! A in the
Hokuriku District.
From the occurrence of Vicaryella in

the present field it is inferred that the
species of the genus when associatedwith Vicarya callosa japonica YABE and
HATAt always is Vicarye!la notoensis
MASUDA, but the species when not associated with Vicarya is liicaryellaishiiana (YOKOYAMA). From the different
occurrences ofVicarrella notoensis
iVlASUDA and Vicaryella .ishiiana (YOKO·
YAMA) it is suggested that they lived
in different environmental conditions,that is to say, Vicaryella notoensis
MASUDA and Vicaryella ishiiana (YOKO·
YA:O.IA) are very closely related with eachother and they are probably allopatricforms of the same stock. This consideration is supported by that the younger
stage of ishiiana is indistinguishable
from that of notoensis but with growththey can be easily distinguished fromeach other.
Type locality .-Matsubara, Hitoichiba,l\'lizunami City, Gifu Prefecture.
Occurrence :-Loc. No. 23-A; Loc· No.
39-C.
Genus Batil!aria BENSO]';, 1842

Batillaria toshioi MASUDA, n. sp.
Pl. l. figs. 7a-b, Sa-b. 9

Holotype .·-DGS, Reg. No. 4580.
Description :-Shell of medium size,
rather thick, turreted, with about 12
whorls, two younger whorls lacking:spiral angle a little less than 30•.
Vl/horls separated by distinct, impressed,
uneven sutures: surface with elevated,broad, nodose longitudinal ribs andnumerous distinct spiral threads: longitudinal ribs subvertical, nine on bodywhorl, narrower than their interspaces,
sculptured with distinct spiral threads;
spiral threads of three conspicuous
spiral threads and subordinate, fine but

516.

Mollt!scan Fauna of the Higash:i-Inna.i

distinct, unequal spiral threads among
main spiral threads; subordinate spirals
tend to decrease their number upwards.
Base of body whorl with three conspicu-ous revolving threads and several, fine3

subequal threads among main threads.
Aperture subovate; outer lip thin; inner
lip with thin callus; colmella somewhat
curved ; canal short, nearly straight.

Dimensions (in mm) :Height
Diameter•-holotype

30.0*
11. 0

ca. 38.0

1-LO

ca. 36.0
12.0

ca. 34
11. 5

29.0
10.0

Remark.~:- Batillaria yamanarii lVIAKI·

Pl. 1. figs. lOa-b. lla-b. 12a-b. 13a-b, 17a-b

p. 148, pl. 13, fig. 4) fromthe !\liocene Heirokudo Formation, North
Korea resembles the present species but
is distinguishable from toshioi by its
subcentrally angulated
whorls andsubequal, fine spiral threads. Batillaria
minoensis ITOIGAWA (1960, p. 280 pl. 4.
figs. 4a-b) from the 1\liocene !\lizunami
Group, Gi fu Prefecture and lJatiflm·ia sitoi NO:\IUI~A and ZINBO (1936. p. 343,
pl. 20, fig. 5) from the Yanaga\va 1\>lioceneof Fukushima Prefecture resemble thepresent species. But the present species
is distinguishable from the former inhaving larger shell. fewer longitudinalribs which are narrower than theirinterspaces and unequal spiral threads.
and from the latter by the larger shell,larger spiral angle, strong. elevatedlongitudinal ribs and unequal spiralthreads.
The present new name is given to thename of my son. Toshio YIASUDA.
Type locality :-Loc. No. 23.
Occurrence·-Type loc.-A; Loc. No.
21-C; Loc. No. 39-A.

1929. Potamides ancisus YoKOYAMA. Jour.
Fac. Sci., Imp. Uni1•. Tokyo, Sec. 2. Vol.
2. Pt. 8. p. 367. pl. 70. tig. 2.
1956. Cerithium ancisum (YOJ<OYA~tA). ITotGAWA. Mem. Coil. Sci .. U11i1:. Kyoto,
Ser. B. Vol. 22. Art. 2, pl. 2. fig. 7.

Y AMA (1926.

Family Cerithiidae
Genus Cerithium BRUGUIERE, 1792
Subgenus l'roclava THIELE, 1929
Cerilhium (Proclava) ancisum(YOKOYAJ\TA), 1929

Holotype :-GT. Reg. No. •1895.
Remarks :-The following description
is based upon abundant specimens newly
collected: Shell of medium size. moder·ately thick. turreted ; Len whorls preseryed ; spiral angle 25" -30". Whorls
slightly rounded, shouldered, separated
by distinctly impressed sutures; shoulders with numerous. somewhat elevatedtubercles; surface with three, unequal.
rather distinct, somewhat granulated
spiral threads and two. subordinate,fine spiral threads. Base of body whorlwith several. unequal, fine revolving
threads. Aperture subovate. somewhat
angulated posteriorly; outer lip rather
thick. denticulated within; inner lip
sharply defined by very thick, somewhat
protruded callus; columella subvertical.
smooth; canal short. rather deep, narrow.
somewhat bent back.
This species was first described by
YOKOYA:'>IA (1929) as Potamides from the
11iocene Togane Formation, Shimane
Prefecture based upon a single specimenof the last two whorls. Subsequently
it was illustrated by OTIJJ<A {1938. p. ·12,

Koichini MASUDA

4

pl. 4. fig. 36) from the lVIiocene Shobara
Formation, Okayama Prefecture as Cf!rithium. At that time 0TUKA considered
Batillaria atukoae 0TUKA once describedby him (1934. p. 623, pl. 49. figs. 69, 70)
from the !vliocene Shiratori ~!ember ofthe Kadonosawa Formation, lwate Prefecture .to be a synonym of ancisa, andthat Batillaria atukoae 0TUKA illustrated
by NOMUI~A (1935. p. 282, pl. 17. fig. 23)
from the !vliocene Ajiri Format ion,l\liyagi Prefecture is conspecific with thepresent species. Further, OTUKA statedthat since the specimen collected fromthe Lower Kadonosawa Series has acolumellar fold in the whorls it may belong to Proclm:a. OY Alii A and SAKA
(19-14) presented a key to the species of
the genus llicaryella and included into
it the present species. Lately KAMADA(1959) reported on llicarya and llicaryellain Japan and referred the present
species to Vicaryella as done previously
by OYA\IA and SAKA.
To clarify the characters of thisspecies and its relationship with related
species. observations were made on
YOKOY A:'\! A's and 0TUKA's type specimens (Reg. No. 10024) preserved in the

Geological Institute of the Tokyo University. As the result, it was found that
YoKOYAMA'S holotype specimen has nocolumellar fold but OTUKA'S specimens
have. Thus OTUKA's ancisum from the
Shobara and Shiratori tvliocene are different from YOKOYA:\TA's ancisus. though
their surface characters are similar to.
one another. Therefore OTUKA's ancisumshould be referred to another species.
Consequently, OTUKA's ancisum from the
Shobara and Shiratori Miocene andNOMURA's atukoae from the Ajiri can bereferred to Cerithidea sirakii (MAKIYAMA)(1936. p. 221. pl. 5, figs. 10.15) from theLower Bank6d6 l\liocene, North Korea.
Cerithium (Proclaua) meisense MAKIY AI\! A (1936, p. 220, pl. 5, fig. 20) fromthe !vliocene Heirokud6 Formation, North
Korea also resembles the present species.
Cerithizmz (Proclava) meisense differsfrom ancisum in having a larger spiralangle, more prominent beaded spiralthreads and a columellar fold. Meisense
is distinguishable from Cerithidea sirakii(MAKIYAMA) by its larger spiral angle
and more conspicuous beaded spiralthreads.

Dimensions (in mm) :Height
Diameter

33.0
13. 1

ca. 33.0

14. 5Type locality :-Senjyojiki, Togane-ura.
Kokubu-mura, Naga-gun. Shimane Prefecture.
Occurrence :-Loc. No. 3-F; Loc. No.
10-C; Loc. No. 23-C; Loc. No. 24-C:
Loc. No. 30-C: Loc. No. 32-F.
Family Epitoniidae
Genus Nodiscala BOURY, 1890

Nodiscala suzuensis l\IASUDA. n. sp.

ca. 31. 0
10. 5

27.5
10.0

27.0
10.0

Pl. 1. figs. 19a-b

Holotype :-DGS, Reg. No. 4588.
Description :-Shell very small, moderately thick, turreted, rounded at base;
five whorls preserved ; spiral angle about
20,.
Whorls rounded. separated by
distinct. impressed sutures: surface withconspicuous, rounded. rather smoothlongitudinal ribs and fine spiral threads;
longitudinal ribs somewat oblique, nearly equal to their interspaces, about 15

516.

Molluscan Fau.na of the Higashi-Inna.i

on body whorl. sculptured with fine·spiral threads: a few longitudinal ribs
especially thick. elevated like varices;spiral threads rather faint. nearly equal.
rather regularly spaced. Aperture subcircular; outer lip makes thick, roundedvarix sculptured with faint. fine spiralthreads; inner lip sharply defined bycallus; not umbilicated.
Dimensions (in mm) :-Height 5.0. diameter 2.0 (holotype).
Nemarks :-This species is distinguished from Nodi.~cala rissoinaeformis(YOKOYA:\IA) (1927, p. 418, pl. ·17, fig. 4)
from the Pleistocene Tokyo Formation,
Tokyo :\letropolis by its small shell andmore conspicuous longitudinal ribs which
are nearly equal to their interspaces.
Type locality :-Loc. No. 30.
Occurre11ce :-Type loc.-R.

Family Eulimidae
Genus Eulima Risso. 1826

/iulima hataii !VIASUDA, n. sp.
Pl. 1. 6gs. 21a-b

1/olotyfJc :-DGS, Reg. No. 4590.
Description .-Shell very small. thin.
subulate, with about eight whorls, one
and half whorls are nuclear whorls;
spiral angle about 25°. Whorls smooth,polished, very slightly inflated, separated
by rather indistinct sutures: nuclear
whorls smooth.
Aperture elongated,posteriorly angulated. more or lessrounded at base; outer lip thin. simple;
inner lip rather sharply defined.
Dimensio11s (in mm) :-Height 6.5, diameter 2.0 (holotype).
Nemarl•.~ :-This
species is distinguishedfrom Eulima osawanoensts
TSUDA (1959. p. 85, pl. 4. fig. 5) fromthe Kurosedani i'vliocene of Toyama Pre-

fecture by its small shell, indistinct
sutures and larger aperture which isangulated above and rounded below.
Type locality :-Loc. No. 35.
Ocwrrence :-Type loc.-R.

Family Naticidae
Genus :Yeverita Risso. 1826

Neverita coticazae (\IAKIYA:\IA), 1926
Pl. 1, figs. 25a-b. 26a-b
1926. Polinices (.Veverita) colicazae 1\·IAKIYA~JA. Mem. Coil. Sci .. /(ytJ/o Imp. Univ ..
Ser. n. Vol. 2, No. 3. Art. 8. p. 150. pl.
12, fig. 8.
1939. Polinices (Nel'erito) rolicazoe MAKIYA:\IA. No:-.JURA. ]o11r. Ceo/. Soc. jopo11.
Vol. 46, No. 5,18, p. 255, pl. 3, figs. 13a-b.
l4a-b.

Holotype ·-Geological Survey of Korea.
Reg. O'Jo. 75.
Nemarlzs :-This species was t1rst described by MAI<IY Al\IA from the i\liocene
Bank6d6 Formation at Kinshod6, 1\orthKorea, illustrated by NoMtmA from the
Miocene Kozai Formation, !\liyagi Prefecture. reported from the Mizunami\Eocene of Gifu Prefecture ((TOIGAW A,
1960) and also from the Kurosadani:\liocene of Toyama Prefecture (TSUDA.
1960).
The present species was described to
be characterized by its slightly elevatedspire, wide umbilicus and very thickcallus filling the posterior angle of theaperture. The longitudinal profile shownin fig. 25b of Plate 1. is the morphological character by which it can be easily
distinguished from its related ones.
That the specimens from the lligashilnnai Formation are generally small insize compared with the holotype andtopotype specimens from the Bankod6

1{6-ic:hin) MtlSUDA

Formation of North Korea suggests thatthey may be young or dwarfted shells.
In other words, the environmental conditions may not have been favourable

to them. This view is supported bythat the fauna with small sized shellsof coticazae in this field includes somebrackish water species.

Dimensions (in mrn) : Height
Diameter

12.5

12.0

J.l. 513.0Type locality :-Kinsh6d6. 1\Ieisen District, North Korea.
Occurrence :-Loc. No. 1-R: Loc. No.
3-C: Loc. No. 4-F; Loc. No. 7-R: Loc.
No. 23-C; Loc. No. 24-C; Loc. No. 32F; Loc. No. 35-F: Loc. No. 39-F.
Family Cypraeidae
Genus Cypraea LI:"<::\AEUS, 1758

10.0
11. 5

10.0
11.0

10.0
10.0

Pl. 1. Jigs. 28a-b. 29

Holotype -DGS. Reg. No. 4598.
Description :-Shell of medium size,
moderate in thickness, swollen, cypraeiform. narrowed towards both ends.
\Vhorls smooth. polished. Aperture long,narrow: outer lip with about 25. rather
distinct. fine transverse teeth; inner lip
a little swollen, finely denticulated atinner margin : canal short.

Cvpraea ohiroi l\lASUOA. n. sp.

Dimensions (in mm) :32
26. 4*Height24. 5**
17.0
22.0
16.4
18.0
Lateral diameter
13.8
17.0
15.0
Dorso-ventral diam.
13.5*-holotype: **-specimen from lwaki. Osawano-machi. Toyama Prefecture(Kurosedani l\Iiocene)

Remarks:- The present species re·sembles Cyjnaea nomurai HATAI andNISIYAMA (1952. p. 197) which was illu·
strated by Nm·IURA (1940. p. 38, pl. 3.
figs. 4-6) as Cypraea sp. from the Moniwa!Vliocene. Miyagi Prefecture. But olziroi
is distinguished from nmnurai by its
rather long shell, larger number of distinct, fine teeth at the outer lip andrather swollen shelL Panda carneola(LINNAEUS) (REEVE, 1846, pl. 6, fig. 19),
a Recent, Pleistocene and Pliocene
species of Southern japan, resembles thepresent one but differs by its larger
shell and transverse teeth on the innerpart of outer lip.

C.t·praea sp. illustrated by KAN:-:o (1960,
p. 359, pl. 47, fig. 20) from the :vliocene
Hiranita Formation, Saitama Prefecture
may probably be the present species.
but further materials are necessary tosettle this problem.
A single specimen preserved in the
Department of Geology, Faculty of
Education. Tohoku University. collectedfrom the Kurosedani l\1iocene of Toyama
Prefecture, can be identified with thepresent species. The specimen from
Toyama shows faint longitudinal stri·ations on the surface.
Type locality :-Loc. No. 30.
Occurrence :-Type loc.-F.

Molluscan Fauna of the Hiyashi-Innai.51(1.

Family Pyrenidae
Genus Alitrella RISSO, 1825

Mitrel/a noloensis I'.lASUDA, n. sp.
Pl. 2. Jigs. 3a-b, 4a-b. 5a-b

Holotype :-DGS, Reg. No. 4603.
Description :-Shell small. rather thick,fusiform, with about seven whorls. one
or two nuclear whorls lacking: spiral
Dimension.~

7

angle about 35". Whorls somewhat
rounded, gradually growing below,
separated by distinct, slightly impressed
sutures; surface smooth except for afew, faint spiral threads on basal partof body whorl. Aperture elongate oval,
narrow. with acute posterior angle:
outer lip thin, very feebly denticulated
within; inner lip with thin callus: columella a little curved ; canal short andopen.

tin mm) :-HeightDiameter

6.8•
3.0

ca. 10.0
3·9

7.0
3.1

7.0
3.0

5.0
2.4

4.5
2.0

•-holotype

Remarh :- Mitrella minoensis lTOI(1960, p. 286. pl. 5, figs. 7a-b)
from the J\lizunami Miocene of Gifu
Prefecture can be distinguished fromthe present one by its shorter shell,spiral striae on surface, wide apertureand expanded body whorl. i\fitrellaz·arians DtJt\KER (1860, p. 231. sp. 7), a
common l~ecent species of japan. also
can be distinguished from notoensis by
its larger and inflated shell and larger
aperture.
Type locality :-Loc. No. 30.
Occurrence :-Type loc.-C; Loc. No.
1-C: Loc. No. 3-R; Loc. No. 10-F;
Loc. No. 23-C ; Loc. No. 21-C : Loc.
No. 35-C.

Phos notoerz.~is IvlASllllA, n. sp.

GA \VA

Family Buccinidae
Genus t>hos MoNTFORT, 1810

Pl. 2, figs. 6a -b

Holotype :-DGS, Reg. No. t\605.
Description :-Shell of medium size,
moderate in thickness, fusiform, withseven whorls, of which two are nuclear,spiral angle about :15°. Whorls moderately rounded, separated by distinct,
impressed sutures:
nuclear whorls
smooth, rounded: surface with conspicuous, rounded. longitudinal ribs and low.
regular. smooth spiral threads; longitudinal ribs narrower than their interspaces, about 18 on penultimate whorl.
sculptured with spiral threads; interspaces with spiral threads broader thantheir interspaces. Aperture oblongly
ovate. angulated posteriorly; outer lip
thin, finely denticulated within; inner
lip sharply defined by thin callus, concave; canal short.

Dimensions (in mm) :Height
Diameter*-holotype

ca. 13. 5"
6.5

ca. 14.5
7. I)

ca. 11. 5
5.5

ca. 10 ·5
5.0

9.0
4.2

8

Koichiro MASUDA

Remarks:- This species is distinguished from Phos minoensis ITOIGAWA(1960, p. 289, pl. 6. figs. 2a-b, 3) fromthe i\lizunami Jvliocene of Gifu Prefecture by its low spire, moderately
rounded whorls. fewer longitudinal ribs
and low. regular. smooth spiral threads.
Type locality .-Loc. No. 23.
Occurrence:- Type loc.-C; Loc. No.
4-F: Loc. No. 7-R.

Family Nassariidae
Genus :Vassarius DU'\If.:RILL, 1806
Subgenus Zeu:ris H. and A.
ADA:\IS. 1853

_Vassarius (Zeuxis) minoensis

lTO!GAWA. 1960
Pl. 2. figs. 7a-b, 8a-b
1960. Nassarius(Zeuxis) minoensis lTOIEarth Sci., Nagoya Unit• ..
Vol. 8. No. 2. p. 289, pl. 6. figs. la-c.

GAWA. four.

Holotype :-Institute of Earth Science.
Nagoya University, Reg. No. 20079.
Remarks :-Nassarius (Zeuxis) minoensis lTOIGAWA was described from the
C\liocene Mizunami Group, Gifu Prefecture. It is characterized by its small
shell and flat-topped longitudinal ribs
slightly wider than interspaces.
Nassarius simizui OTUKA (1934. p. 631.
pl. 50. figs. 85-87) from the Shi ralori:Miocene of Iwate Prefecture is related
to the present species and Nassarius
notoensis ?\IASUDA from the HigashiInnai Formation (1\IASUDA. 1956. p. 164.
pl. 26, figs. 13. 14). But minoensi.~ andnotoensis can be distinguished fromsimizui by their small shell and fewer
longitudinal ribs.
Nassarius notoensis l\lASUDA
wascollected at Loc. Nos. 10. 12. 23 and 24.

whereas Nassarius minoensis ITOIGAW A
was found at Loc. Nos. 1, 3. 24, 30 and
32. The specimens from the upper partof Loc. No. 24 consist of a well preserved
minoensis and some, small, fragmental
individuals of notoensis. ,votoensis isfound in associated with Vicarya.
Vicaryella. etc. but minoensis does notoccur with such an association. The
different geographical distribution of
the species mentioned probably depends
upon the environmental conditions andthe co-occurrence of minoensis and notoensis in the upper part of Loc. No. 24
is probably that the small. fragmental
individuals of notoensis were transported
from another area. However. they may
be allopatric forms.
Type locality :-Shukubora. ~Hzunami
City, Gifu Prefecture.
Occurrence :-Loc. No. 1-R: Loc. No.
3-F: Loc. No. 4-R; Loc. No. 10-R;
Loc. No. 24-F; Loc. No. 30-F; Loc.
No. 32-F.

Family Mitridae
Genus Mitra :tvlARTY:\, 1781
Mitra ishidae i\IASUDA. n. sp.
Pl. 2. figs. 11, 12a-b

HolofJPe :-DGS, Reg. No. 4609.
Description .·-Shell small. moderately
thick. fusiform. with seven whorls;
spiral angle about 40". \Vhorls slightly
rounded. separated by shallow. uneyen.
rather distinct sutures: two younger
whorls smooth, rounded: surface rathersmooth but sculptured with four, unequal. fine, more or less channeled spiralthreads on upper part and very fineincremental lines; spiral threads unequally spaced. much less than theirinterspaces in breadth; middle two more.516.

Jfollu::;can F'altJin of the lligashi-lnna.i

distinct than others.
Body whorl
rounded. slightly contracted below,
sculptured with two, line spiral threads
on upper part, with seyeral, rather
distinct revolving threads at extreme
end. Aperture rather narrow. elongated,with acute posterior angle: outer lip
simple; columellar folds three, upper one
stronger than others and middle onestronger than lower ; canal short.
Dimensions (in mm) :-Height 9.6, di·ameter '1.3 (holotype) : height ca. 7.0, diameter 3.6; height 15.0. diameter 6.5(paratype).
Remarks :-This species resembles
Milra lwkusimana No~IURA and ZINBO(1936, p. 174, pl. 15. figs. 29. 29b) fromthe Yanagawa Miocene of Fukushima
Prefecture. but differs by its longer
shell, smaller spiral angle, smooth surface and four columellar folds.
TyfJe locality .-Loc. No. 30.
Occurrence:-Type loc.-F: Loc. !'Jo.
24-R.

threads near base. Aperture narrow.
elongated, angulated posteriorly: outer
lip thick, simple; inner lip thin, rather
faint; columellar folds four, upper threerather distinct, lo,ver one very faint;
canal long, wide and open.
Dimensions (in mm) :Hcighl
Diameter*-holotype

8. 8*
3. 5

8.9
3.3

7.8
2.9

6.5

2.6

Remarks:- Vexillum sangui suga (LI:>:·(TRYO:-\. 1882, p. 165, pl. 48, figs.
393-39.7), a Recent species of Southern
japan, can be distinguished from thepresent new species by its larger shelland longitudinal ribs which are narrower
than their interspaces.
The new name is given to the nameof my wife, Setsuko MASUDA who helped
me in various ways.
Type locality :-Loc. No. 30.
Occurrence:- Type loc.-F: Loc. No.

~AEUS)

24-1~.

Genus Vexillum Ri:iDIC\G, 1798
Genus Strigatella Sw AI"SON, 1840
F exillum set sukoae 1\IASUDA, n. sp.
S/rigatella notoensis MASUDA, n. sp.
Pl. 2. ligs. 21a -b. 22a-b
Pl. 2. figs. 20a-b

Holotype :-DGS, Reg. No. 4617.
Descriptioll :-Shell small, rather thick,elongated fusiform. with six whorls.
one or two nuclear whorls lacking:spiral angle about 30•. 'Whorls moderately rounded, separated by rather distinct, impressed sutures, sculptured withconspicuous. fine longitudinal ribs andfine spiral threads: longitudinal ribs
subvertical, rather low, about 12 on bodywhorl. broader than their interspaces
and tend to become obsolete below :spiral threads numerous but become
fewer upwards. Body whorl contracted
below, . with rather distinct revolving

Holotvpe :-DGS. Reg. l\o. 4616.
Description :-Shell rather large. thick,fusiform. with six whorls. two to three
younger whorls lacking: spiral angle
about 40'. Whorls slightly rounded,separated by distinct, channeled sutures:
surface smooth, with one or two, very
faint. fine spiral threads and line incremental lines.
Body whorl smooth.
slightly contracted below, with several,
faint, fine revolving threads near base.
Aperture rather nar'row, long, subverti·
cal, angulated ·above. truncated below;
outer lip vertical. simple, subparallelKoi.chiro MASUDA

10

with columella; inner lip thin. rather
narrow, rather distinctly defined; columellar folds four. decreasing in sizeand strength below; upper three folds
prominent, lowest one very faint andfine: canal short.
Dimensions (in mm) :-Height 32·0, diameter 12.2 (holotype) : height 17.0, diameter 7.0 tparatype).
Remarks:-This new species is distinguished from Strigatella dainiliensis
l'v1AKIY .t\:VIA t1927, p. 114. pl. 5. figs. 15.
16) from the Pliocene Dainichi Formation. Shizuoka Prefecture by its distinct sutures, long aperture and surface
sculpture.
Type locality :-Loc. No. 24.
Occurrence:-Type loc.-F.

Family Cancellariidae
Genus Sydap!zera IREDALE. 1929
Svdaphera horii MASUDA, n. sp.
Pl. 2. figs. 16a-b. 17a-b. 18a-b. 19

Holotype :-DGS. Reg. No. 4613.
Description :-Shell rather small, rather
thin. ovate-fusiform. with seven whorls,
two and a half nuclear whorls; spiralangle about '10'. Whorls shouldered.
moderately convex, separated by distinct
sutures: nuclear whorls low, smooth,rounded: surface sculptured with distinct. eleYated, spirally sculptured longitudinal threads and numerous, distinct,
round-topped spiral threads and fineintercalary threads: longitudinal ribs
somewhat narrower than their interspaces, about 13 on penultimate whorl :interspaces with distinct spiral threads
and intercalary threads. Aperture obliquely ovate. rounded above; outer lip
rather thick, denticulated within: inner
lip defined by thin callus: columella

nearly straight, with three distinct folds,
upper tvm much stronger than lo\ver
one; canal short.
Dimensions (in mm) :Height
11. 0*
Diameter
5. 5*-holotype

ca.l5. 0
8.0

12.0
6.5

7.0
4.2

Remarks:-The present species resembles Cancellaria hukusimana NO:\IURA
and HATAI (1936b, p. 134, pl. 17, figs.
6a-b) from the Tanagura Miocene. Fukushima Prefecture. but horii is distinguishable therefrom by its oblong shell, more
longitudinal ribs and spiral threads.
Sydaphera sp. illustrated by ITOIGAW A(1960, p. 290. pl. 6, fig. 4) from thel'v1izunami Miocene of Gifu Prefecture
may be included into the present species, but the naming is withheld until
better materials accumulate.
This species is named in honor of
Mr. llisanao llORI of the Kanaza wa
Technical High School who was myformer teacher during the t\,liddle Schooldays and who helped me in various
ways.
Type Locality :-Loc. No. 32.
Occurrence:-Type loc.-R: Loc. No.
4-R: Loc. No. 7-R; Loc. No. 35-R.

Family Turridae
Genus Inquisitor HEDLEY, 1918
Inquisitor slzibanoi MASUDA, n. sp.
Pl. 2. figs. 23a-b, 24a-b. 25a-b, 26a-b

Holotype .-DGS. Reg. No· 4619.
Description :-Shell of medium size,
rather thick, turreted, with about ten
whorls, two to three nuclear whorls;
spiral angle about 40". Whorls separated
by rather distinct, uneven sutures: sur-516.

.~.llolluscan

Fauna. of the Hiyaski-Innai

face with elevated, smooth longitudinalribs and somewhat granulated subsutural cords; longitudinal ribs oblique, 13
on penultimate whorl and 15 on bodywhorl. somewhat narrower than theirinterspaces, angulated at uppermost
part: nuclear whorls smooth, rounded.
Base of body whorl somewhat contracted. with a few, faint, fine revolving
threads. Aperture oblique, rather narrow. elongated, narrowly channeledposteriorly: outer lip thin. with rather
deep sinus; inner lip sharply defined,with thin callus; canal short and open.
Dimensions (in mm) :-Height H.O.
diameter 5.0 (holotype) : height ca. 13.0.
diameter 4.0; height 6.4. diameter 2.9(paratype·.
Remarks :-The present new species
can be distinguished from Inquisitor
mizunamiensi.~ ITOTGAWA (1960. p. 291.
pl. 6. figs. 8a-b) from the Mizunami
Miocene of Gifu Prefecture by its larger
number of longitudinal ribs and angulated subsutural bands. and from [nqui·sitor osazcanoensis TsUDA (1960. p. 97,
pl. 6. figs. 4. 5) from the Kurosedani't\Iiocene of Toyama Prefecture by its
larger spiral angle and more longitudinal ribs.
This species is named in honor of I'vlr.
Shoichi SHIBANO of the Yanaida Agri·cultural High School who helped me in
the field.
Type locality .·-Loc. No. 30.
Occurrence :-Type loc.-R; Loc. No.
4-R: Loc. No. 23-R; Loc. No. 24-F;
Loc. :--.lo. 35-R.
Family Pyramidellidae
Genus Synwla A. Ao.uts, 1860
Synwla notoensis l-.IASUDA. n. sp.
Pl. 2. rigs. 31a. b

11Holotype .-DGS. Reg. No. 4627.
Description :-Shell rather large. thin.
turreted. rounded at base. six whorls
preserved ; spiral angle about 20·.
Whorls tlattish to slightly rounded.
separated by distinct. shallowly channeled sutures: surface smooth but withnarrow. colored band a little above
sutures. very faint. fine spiral threads
and very faint. fine incremental lines.
Aperture subovate, posteriorly angulated
but anteriorly rounded; outer lip thin.
smooth: columella short, with a fold.
Dimensions (in mm) :-Height 7.2,
diameter 3.0 (holotype) : height ca. 8.5,
diameter 3.6 (paratype).
Remarks:- The present species was
described based upon a well preserved
specimen lacking the upper whorls andsome unfavourably preserved specimens.
This new species can be distinguishedfrom Synzola cinctella !\.
ADA:O.IS(NO:\IURA, 1937. p. n. pl. 9. figs. 47a-b!.
a Recent and Pleistocene species of japan. by its larger shell and rather weakfold.
Type locality .·-Loc. No. 23.
Occurrence:- Type loc.-R; Loc. :-\o.
39-F.

Genus Turbonilla Risso. 1827
Turbonilla ishidae MASUDA. n. sp.
Pl. 2, figs. 34a. b. 35/Iolotype :-DGS, Reg. No. 4632.
Description :-Shell small. thin. elongate-conical. with six whorls. nuclear
whorls lacking; spiral angle about 35'.
Whorls somewhat rounded. separated byconstricted sutures: surface with ele·
vated. slightly oblique. fine longitudinalribs much narrower than their inter·spaces, about 18 on body whorl. Baseof body whorl somewhat contracted.

Koichiro .MASUDA

12

slightly concave. with three. faint. finespiral threads. Aperture subquadrate,with acute posterior angle; outer lip
thick : columella nearly straight.
Dimensions (in mm) :-Height 4.3, di·ameter 2,2 (holotype): height 2.2. di·ameter 1.3 (paratype).
Remarks:- This new species distin·
guishable from Turbonilla tayaensis
NOMURA and HAT AI (1938b, p. 61, figs.
5a-b) from the !vliocene Taya Formation, Akita Prefecture by its rather
small, low shell, larger number ofwhorls and rounded base.
Type locality .·-Loc. No. 24.
Occurrence:- Type loc.-R; Loc. No.
10-R.
Genus Tiberia 1\IO;\TEROSATO, 1875
Tiberia lwnamiensis ~viASUDA, n. sp.
Pl. 2. figs. 32a. b

Holotype :-DGS, Reg. No. 4630.
Description :-Shell small, thin, umbi·
licated, regularly turreted, with nine
whorls, younger two to three whorls
lacking; spiral angle about 30'. Whorls
flattish, gradually growing, separated byrather distinct sutures; surface smooth
but with very faint, fine incremental
lines.
Body whorl flattish above,rounded at periphery, convex at base.
Aperture subovate, with acute posterior
angle: outer lip thin. simple; inner lip
with thin callus; columella straight,
with three unequal folds, upper foldstrong. conspicuous and lower two
much less conspicuous.
Dimensions (in mm) :-Height 9.0. di·ameter 4.5 {holotype).
Remarks:-The present new species
can be distinguished from Pyramidellalzataii ~lASUDA (1956. p. 164. pl. 26, figs.

15a-b) from the Higashi-lnnai Formation
at Loc. No. 12 by its larger spiral angle,
not channeled sutures and upper con·spicuous columellar fold and two, lower'veak columellar folds.
Type locality .-Loc. No. 35.
Occurrence:- Type loc.-K
Family Scaphanderidae
Genus Adamnestia IREDALE, 1936
Adamnestia onukii 1-IASlJDA, n. sp.
Pl. 2, figs. 36a, b/-lo/otype :-DGS. Reg. No. 4634.
Description .·-Shell small, solid. elon·
gated, cylindrical, rounded at lower end:
convolute; vertex shallowly depressed,with a small pit at bottom. Body whorl
equal to length of shell; surface smooth
but with very faint, fine growth Jines
and a few. very faint, fine spiral threads
at uppermost part. Aperture linear,
narrow, dilated at lower part: outer lip·thin, nearly straight: inner lip coveredby callus; umbilicus very shallow, slit·
like.
Dimensions (in mm)-Height 7.2. di·ameter 3.0 (holotype); height 5.7, eli·ameter 2.4 (paratype).
Remarks .·-Adamnestia japonica (A.
ADAliiS) (BABE. 1961, p. 91. pl. 43, fig. 15).
a Recent species of japan, can be dis·tinguised from the present one by its
smaller shell and surface sculpture.
This new species is named in honorof Professor ·Yoshio ONUKI of the Depart·
ment of Geology, Faculty of Education,
Tohoku University.
Type locality :-Loc. No. 24.
Occurrence:- Type loc.-R: Loc. No.
23-R.

51li.

illolluscrm Fazow of the IJz.ya.shi.-lwnai

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teXt·fi!{., pis. 2-8.

516.

.Molluscan Fannn of the Higashi-Inna.i- - (1935b) : Miocene Mollusca from Siogama, :\orthcast Honsyfi. Japan. Ibid.,
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- - (1937): Additional Pyramidellidae from
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1\lolluscan Fossils from theTatunokuti Shell Bed Exposed at Goroku
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Sci. Rep .. Tohoku Imp. Unh· .. 2nd Ser.,
Vol. 19. ~o. 2. pp. 235-275, pis. 33-36.
- - (1939): Miocene Mollusca from Yarnaguti. Kozai-mura. lgu-gun, Miyagi-ken,
Northeast llonsyfi. Japan. jour. Ceo/. Soc.
japan, Vol. •16, No. 548, pp. 253-257, pl. 13.
- - (1940) : Molluscan Fauna of the Moniwa
Shell Beds Exposed along the Natori-gawain the Vicinity of Sendai, Miyagi Prefecture. Sci. Nep., Tohoku Imp. Univ .. 2nd
Ser .. Vol. 21. No . .1. pp. 1-·16, pls. 1-3.
- - and HATJ\1. K. (1936): Fossils from the
Tanagura Beds in the Vicinity of the
Town Tanagura. I-Iukusima-ken, Northeast Honsyii. Japan. Saito Ho-on I<aiMus., Nes. /Ju/1., No. 10, pp. 109-155. pis.
13-17.
- - and - - (1938a): Fossil Mollusca fromthe Neogene of Izumo. japan. jour. Ceo/.
Ceogr .. Vol. 16, Nos. 1-2. pp. 1-9, pl. 1.
- - and - - (1938b) : On Some Fossils from
Akita Prefecture. Northeast Honsyil..
Japan. Ibid .. Vol. 16, Nos. 1-2. pp. 39-64.
text-figs. 1-5.
- - and Zr:--;uo, N. (1935): Mollusca fromthe Yanagawa Shell-Beds in the Hukusima Basin. Xortheast Honsyu. Japan.
Saito llo·OII Kai Mus.. Res. Bull., Xo. 6.
pp. 151-192, pl. 15.
OINO~IIKADO, T. (1938) : Neogene Shells fromthe Vicinity of the City of Takasaki.
Gumma-ken. japan. jour. Ceo/. Soc. japan,
Vol. 45. No. 539, pp. 671-676, pl. 20.
0TuKA, Y. (1934): Tertiary Structure of theNorthwestern End of the Kitakami
Mountainland, Iwate Prefecture. Japan.
Bull .. Earthq. Res. Inst., Imp. Univ. Tokyo.
Vol. 12. Pt. 3. pp. 566-638, 1 map, pls. 4451.

15- - (1937) : The Geologic Age of the Tertiary Formation near Hamada, Simane
Prefecture, Japan. japan. Jour. Ceol.
Geogr .. Vol. 14. Nos. 1-2. pp. 23-32. 1
text-Jig .. 1 table. pl. 33.
- - (1938a): Neogene Fossils of the lhara
District. Sizuoka Prefecture. Japan. jour.
Fac. Sci .. Imp. Univ. Tokyo. Sec. 2. Vol.
5, Pt. 1. pp. 1-19, text-figs. 1-2, 3 tables.
pis. 1-2.
- - (1938b) : Mollusca from the Mioceneof Tyugoku. Japan. Ibid .. Vol. 5. Pt. 2.
pp. 21-45. text-Jigs. 1-·1, pls. l-·1.
- - (1941) : Fossil Mollusca from Tazima.
Hyogo Prefecture. Japan. japan. jour.
Ceo/. Ceogr., Vol. 18. Nos. 1-2. pp. 21-45.
OY .... MA, K. (1950): Studies of Fossil Molluscan Biocoenosis, No. 1. BiocoenologicalStudies on the Mangrove Swamps, with
Descriptions of New Species from Yatuo
Group. Ceo/. Surv. Japan. Rep .. No. 132.
pp. 1-15 . 1 text-fig .. pls. 1-3.
- - (1961) : Revision of Cenozoic Fossil Mollusca from Japan (1). Ibid .. Bull., Vol.
21. No. 5. pp. 75-85 (in Japanese).
- - (19:53):
Fossil Communities of the
Oceanic ·water (No. 1). Misc. Nc•p .. Res.
Ins/. Nat. Res .. No. 32, pp. 23-29 (inJapanese).
- - (1954) : Fossil Communities of the
Oceanic Water (Xo. 2). Ibid .. No. 34. pp.
89-100 (in Japanese).
--and SAKA. K. (1944) : Fossilicnmollusken
der
Tukiyosi-Formation(1).
Bull ..
Sigenkagaku Kenkyusho. Vol. I. Xo. 2,
pp. 137-l-14. pis. 14-15 (in japanese).
PIIIL!PPI, R. A. (1845):
Abbildungen undBeschreibungen neuer order wenig gekannter Conchylien, unter Mithiilfe mehrerer
deutscher Conchyliologen. Vol. I. pp. 1204.
PrLSBRY, H. A. (1904): New Japanese !\Iarine
Mollusca: Pelecypoda. Proc ..·lead. Nat.
Sci. Plrila .. Vol. 56. pp. 550-561, pls. 39-41.
REE\'E. L.A. (1843-1887) : Conchologia Iconica.
figures and descriptions of the shells ofmolluscs; with remarks on their aflinities,
synonymy. and geographical distribution.
Vols. 1-17, 18-20 (continued by G. B.
SOWERHY).

Hi

Koichfro MASUDA

SHuTo. T. (1957): Fossil Paphia from theMiyaznki Group. japan. jour. Geol. Geogr.,Vol. 28, Nos. 1-3. pp. 1:39-160, text-figs.
1-9. 6 tables, pl. 12.
- - (1961) : Palaeontological Study of the
Miyazaki Group.-A General Account of
the Faunas. Mem. Fac. Sci.. Kyushu
Unit· .. Ser. D. Vol. 10. No. 2. pp. 73-206.
text-figs. 1-23. 5 tables, pis. 11-13.
So\\'ERIIY. G. B.. (1842-1887):
Thesaurus
Conchyliorum. Vols. 1-5.
TRYO:-.:, G. W .. (1878-1898) : Manual of Conchology. Vols. 1-9: 10-16 (continued by

H. A. Pll.SflRY) : 17 (by H. A. Pu.sHY and
B. SHAI~P).

Tst.:DA, K.. (1955) : On the Sedimentary
Environments of the Yatsuo Group.-A
Study of the Sedimentary Environmentof the Miocene Deposit~ in the so-called"Green Tuff" Region-(Part 1). jour.
Geol. Sac. japan, Vol. 61, No. 722, pp.
532-542. text-figs. 1-4, 2 tables (in Japanese).
- - (1956) : Faunas and Facies of Some
Middle Miocene Deposits in japan. jour.
Paleant., Vol. 30, No. ·1. pp. 9H-980, text·

Explanation of Plate(All figures in natural size. unless otherwise stated)
Figs. la-b. 2a-b. Vicaryella ishiiana (YOKOYA!\IA). la-b. DGS, Reg. No. 4573: Loc. No. 23.
2a-b. DGS. Reg. No. --1574: Loc. No. 39............................................... p. 1
Fig. 3. Vic(lryella no/oensis MASUDA. DGS, Reg. No. 4575: Loc. No. 24.
Fig. 4. Cerithidea k(/npokuensis MAKIYAMA. DGS. Reg. No. 4576: Loc. No. 2•1.
Figs. Sa-b. 6a-b. Cerithidea ohirai l'vlASUDA, n. sp. 5a-b. paratype, DGS, Reg. No. 4578:
Loc. No. 30. x 5. 6a-b, holotype. DGS. Reg. No. 4577: Loc. No. 24. x 2. . ......... p. 1
Figs. 7a-b. Sa-b. 9. Bali/l(lria toshioi MASUDA. n. sp. 7a-b. holotype, DGS. Reg. No. 4580:
Loc. No. 23. Sa-b. para type. DGS. Reg. No. 4582: Loc. No. 38. 9, para type, DGS. Reg.
No. •1581 : Loc. No. 23 ............................................................... p. 2
Figs. lOa-b. lla-b. 12a-b. 13a-b. 17a-b. Cerithium (Proclava) (lltcisum (YOKOY'\~!A). lOab. 12a-b, DGS. Reg. No. 4583: Loc. No. 30. lla-b, DGS. Reg. No. 4579: Loc. No. 2-1.
x2. 13a-b, 17a-b. DGS. Reg. No. 4584: Loc. No. 23 ................................. p. 3
Figs. !<la-b, 15a-b. Cerithidea sirakii (MAKIYAMA). 14a-b. DGS. Reg. No. 4585: Loc. No.
35. 15a-b. DGS. Reg. No. 4646; Loc. No. 35.
Figs. 16a-b. Cerithium meise11se MAKIYA~IA. DGS. Reg. No. 4586; Loc. No. 7.
Figs. !Sa-b. Bittium sp. DGS. Reg. No. ·1587; Loc. No. 24. X 5.
Figs. 19a-b. Nodisc(l[a suzue11sis !\1.-\Sl'DA, n. sp. Holotype. DGS. Reg. No. 4588: Loc. 1'\o.
30. x5....................................... · · · · · · · · · · · · · · · · · · · · · · · · · · · · · · · · · · · ·· .p. ·1
Figs. 20a-b. Turriscala sp. DGS. Reg. No. 4589: Loc. :\'o. 3. x2.
Figs. 2la-b. Eulima hataii MASl:DA. n. sp. Holotype. DGS. Reg. No. 4590: Loc. :\'o. 35. x2 .
. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. .. . p. 5
Figs. 22a-b. Pachycrammium japonicum KA;-.;:-.:o. DGS. Reg. No. 4593; Loc. No. 24.
Figs. 23a-b. Si11u111 i11eptum (YoKOYA~!A). DGS. Reg. No. -159-l: Loc. No. 23.
Figs. 24a-b. Polillics meisensis MAKIYAMA. DGS. Reg. No. 4595; Loc. No. 23.
Figs. 25a-b. 26a-b. Neverita coticazae (MAKIYA!\IA). 25a-b, topotypc, IGPS. coli. cat. no.
6•1773: Loc. Kinshodo. Meiscn District, North Korea (Bankodo Formation). 26a-b.
DGS. Reg. No. ,1596: Loc. No. 24. . . . . . . . . . . . . . . . . .
.. .. .. .. .. ..
. ...... p. 5
Figs. 27a-b. Pro/erato (Sulcerato) minoensis lTOIGAWA. DGS. Reg. No. ·1597: Loc. No. 30.
x5.
Figs. 28a-b, 29. Cypraea ohlroi MASUDA. n. sp. 28a-.b. holotype, DGS. Reg. No. 4598: Loc.
No. 30. 29. para type. DGS. Reg. No. 4599: Loc. No. 30. . ........................... p. 6

Plate 1

.S16.

figs. 1-(i.
- - (1959): New Miocene !\·lolluscs fromthe Kurosedani Formation in Toyama
Prefecture. Japan. jour. Fac. Sci., Niigata
Unil' .. Ser. 2. Vol. 3, No. 2, pp. 67-110, l
text-fig., 1-7.
- - (1960): Palco-Ecology of the Kurosedani
Fauna. Ibid .. Vol. 3, No. -1. pp. 171-203.
text-figs. 1-27, 1 table.
Uo:w~u. S.. (1962):
Xeogene ~Iolluscan
Faunas in llokkaido (Part 1). Sequenceand Distribution of Neogene Molluscan
Faunas). jour. Fac. Sci .. Hokkaido Univ.,
Ser . .J. Vol. 11. No. 3. pp. 507-544, textfigs. 1-11. 3 tables.
VRcDE:'\IlFIH~. E.. (1928) :Descriptions of
Mollusca from the Post-Eocene TertiaryFormation of Northwestern India. Mem.
Geol. Sun·. India. Vol. 50, Pt. 2. pp. 351•162. pis. 1-l-33.
YAnA, H. and IIATAI. K .. (1938): On the Japanese Species of l'icarya. Sci. Rep.,
Tohoku Imp. Uni~· .. 2nd Ser., Vol. 19.
No. 2. pp. 1·19-172. pl. 12.
- - and - - (19<11):
The Cenozoic Formations and Fossils of Xortheast Honsyu.

AkagamiDoguchiFujio
Hizumewaki
InomoteKanagura
Kobunayama
Konosuyama
Matsunagi
Mukaiyama
Najimi
Nishi-lnnai
Sakaishiyama
Suzu City
Tokunari
WanizakiYanaida-mura

17

Molluscan Fauna of the Iliua.shi.-lnncti

JJ;
±

t$

8i

~

n
~
"" iiD

(] H'

11'
~

iii
+81t U1

iBii!tl llr
fE... 1}

Iii)

~
Ill

iYi ;t: J!
Jl!ir.t 1*1:lJl fi Ill£1~ iffl rfl
1!I'J

ffZ

r,;

itt

m IU ft

Japan. Ibid .. Vol. 22. No. 1. I>Jl. 1-86, pis.
1-4.
YoKOY.-UJA, M .. (1920) : Fossils from theMiura Peninsula and Its Immediate
North. four. Coli. Sci .. Imp. Univ. Tokyo.
VoL 39. AJt. 6, pp. 1-193. pls. 1-20.
- - (1923) : Tertiary Fossils from Kii. japan. jour. Geol. Geogr .. Vol. 2. Ko. 3, pp.
47-58, pis. 6-7.
- - (1925) : Molluscan Remains from theUppermost Part of the Jo-Ban Coal-Field.
jour. Coli. Sci .. Imp. Unil'. Tokyo. VoL
45. Art. 5. pp. 1-35. pis. 1-6.
- - (1926a) : Molluscan Fossils from the
Tertiary of Mino. jour. Fac. Sci .. Imp.
Unit•. Tokyo, Sec. 2. Vol. 1. Pt. 7. pp. 213227, pl. 28.
- - (1926b) : Fossil Shells from the Atsumi
Peninsula, Mikawa. Ibid .. Vol. l, Pt. 9.
pp. 369-375. pl. 43.
- - (1927) :Mollusca from the Upper
Musashino of Tokyo and its Suburbs.
Ibid .. Vol. 1, Pt. 10, pp. 391-437. pis. •16-50.
- - (1929) :Neogene Shell8 from Some
Pro,·inces of Chugoku. Ibid .. Vol. 2, Pt.
8. pp. 363-368, pl. 70.

AwaguraFugeshi-gun
Higashi-Innai
IizukaKakumaKendaradakc
K6nami
Kuden
Maura
Munehiro
Nekogatakc
Orito
SarugabaTannoji
Wajima City
Wasumi
Yoshiro~119. -~~iimlR r:n I~
.ti
ll!i
ffJ

r.n

J! I]~ ffi
~

iJ.t

9-.

fll

l4
iili
.,r,
ll\
Jlli 7 Iii
F
.fiT
~

m

?- JJJ-6 ~!f Jt!!

,;u h,) 'iii
HI

11:

-:1:

~~~

Ll

18

Koichiro kiASUDA

Explanation of Plate 2(All figures in natural size, unless otherwise stated)
Figs. la-b. Apollon osawanoensis Tst:DA. DGS, Reg. No. 4601 ; Loc. No. 24.
Figs. 2a-b. Siphonalia nisiyamai IL"-TAI and KoTAKA. DGS. Reg. No. 4602; Loc. No. 30.
Figs. 3a-b. -ia-b, 5a-b. Mitrella notoensis ~L-\SUDA, n. sp. 3a-b, holotype, DGS, Reg. No.
4603; Loc. No. 30. x 2. 4a-b, 5a-b. paratype, DGS, Reg. No. 4604; Loc. No. 24. x 2.
. .. . . . . . . . . . . . . . . . . .. . . . . . . . . . . . . . . . . .. .. . . . . . . .. .. . . .. . . .. . . .. . . .. .. .. .. . . .. .. . . . . . p. 7
Figs. Ga-b. Phos notoensis MASUDA, n. sp. Holotype, DGS, Reg. No. 4605; Loc. No. 23.
x2 ................................................................................. p. 7
Figs. 7a-b, Ba-b. Nassarius (Zeuxis) minoensis lTOIGAWA. 7a-b, DGS, Reg. No. ·1606; Loc.
No. 32. Ba-b, DGS, Reg. No. 4607; Loc. No. 3....................................... p. 8
Figs. 9a-b, lOa-b. Mitra hukusimana NOMURA and ZII'\HO. DGS, Heg. No. 4608; Loc. No.
30. x2.
Figs. 11, 12a-b. Mitra ishidae MASUDA, n. sp. 11. paratype, DGS, Reg. No. ·ltlOl; Loc. No.
30. x2. 12a-b, holotype. DGS, Reg. No. 4609; Loc. No. 30. x2 ..................... p. 8
Figs. 13a-b, 14a-b. Oliva osawanoensis TsUDA. DGS. Reg. No. •1611; Loc. No. 2•1.
Figs. 15a-b. Pusia sp. DGS, Reg. No. 4612; Loc. No. 35. x 2.
Figs. 16a-b, 17a-b, 18a-b. 19. Sydaphera horii MAsUDA. n, sp. 16a-b, 19, paratype, DGS.
Reg. No. •1614; Loc. No. 23. x2. 17a-b, holotype. DGS. Reg. No. •1613; Loc. No. 32.
x2. lBa-b. para type, DGS, Reg. No. 4615: Loc. No. 7. x2 ......................... p. 10
Figs. 20a-b. Strigatella notoensis MAsUDA. n. sp. Holotype, DGS, Reg. No. ·1616: Loc. No.
2·1. .................................................................................. p. 9
Figs. 21a-b, 22a-b. Verillum setsukoae MASUDA, n. sp. 2la-b, holotype, DGS, Reg. No. 4617:
Loc. No. 30. x 5. 22a-b, para type, DGS, Reg. No. ·1618; Loc. No. 2·1. x 5........... p. 9
Figs. 23a-b. 2·1a-b, 25a-b, 26a-b. Inquisitor shibanoi MAsUDA, n. sp. 23a-b, holotype, DGS.
Reg. No. ·1619; Loc. No. 30. x2. 24a-b. 25a-b, 26a-b, paratype, DGS. Reg. No. 4620:
Loc. No. 24.. x2. . ................................................................. p. 10
Figs. 27a-b. Philbertin sp. DGS, Reg. No. 4622: Loc. No. 30. x 5.
Figs. 28a-b. Cythara sp. DGS, Reg. No. 4624: Loc. No. 30. x 5.
Figs. 29a-b, 30a-b. Conus tokunagai 0TUKA. DGS. Reg. No. 4626; Loc. No. 23.
Figs. 31a-b. Syrnola notoensis .MASUDA, n. sp. Holotype. DGS, Reg. No. 4627: Loc. No. 23.
x2 ................................................................................. p. 11
Figs. 32a-b. Tiberia konamiensis MASUDA. n. sp. Ilolotype. DGS, Reg. No. •1630; Loc. No.
35. x2 ............................................................................. p. 12
Figs. 33a-b. Ringicula minoensis TAKEYA~JA. DGS, Reg. No. 4631; Loc. No. 23. x 5.
Figs. 34a-b, 35. Turbonilla ishidae MASuDA. n. sp. 34a-b, holotype, DGS, Reg. No. 4632;
Loc. No. 24. x 5. 35, paratype. DGS, Reg. No. •1633; Loc. No. 10. x 5. . ........... p. 11
Figs. 36a-b. Adamnestia onukii i\LI\SUDA, n. sp. Ho1otype, DGS, Reg. No. 463·1; Loc. No.
2·1. x2 ............................................................................. p. 12
Figs. 37a-b. Acteon osawanoensis TsuDA. DGS, Reg. No. ·1635; Loc. No. 23.
Figs. 38a-b. Menestlw sp. DGS, Reg. No. 4636: Loc. No. 30. x5.
Figs. 39a-b. J!olvulella tokiensis lTO!GA\\'A. DGS, Reg. No. 4637; Loc. No. 30. x5.

Plate 2
MASUDA:

Molluscan F aun:r of the Hi gashi- Tnnai

30a

30b

31a

38a
'$7a

37b

39b

Trans. Proc. Palacont. Soc. Japan. N. S .. No. 65. pp. 19-25. pis. 3. -!. Apr. 10. 1967

517.

THREE NEW TERTIARY FORA'JIINIFERAL GENERAFROI\I FLORIDA, SAIP AN AND GUAM*SHOSHIRO !lANZAW A
Institute of Geology and Paleontology, Tohoku University. Sendai~t,*7 :o: 1J ;i · 4/"1,; :/ if:J · 1/T L.,\'}j'l[;o:J?f':::=:fi!·f'ffL!l!OJifr~J;: -;• ~=' ~ frf.l)~fttfri!Jii?i£
Borelis gunteri CoLE, 19-11 11 multi-tiered chambers 7k.u" continuous septa ~lf L-.
!flrfr~JJ;I:'t.l!JJOJ illueolinella DouVILLF' :::;!i:U.:lL. single storied chambers 0) Bore/is
EBRE:"\BERG fJ· .;.\KJ)I] L.f,;: :t:h::ff.;: !;,;",;:'. 'o:l-:'fti~ Q11asiborelis ~tJ~~ :. _ f:_, -1!-1 ~; J'};fJ
Aquitanian M£•!'E Gypsina marianensis IIA:-:ZA wA. 1957 ;J:tJitii!ft"ni:. 3 ~ i::7ift. t.,, .:COJ•I•OJ!fli'!o:J chambers ::::! 4 stolons ~.f1.X. "(~<':>. Gypsina CARTER ::.!;l:.;:O)j.)tt.>.~;'ft'l:~if.J:'. ·OJ·c:.Mif!ii Gypsina ;?>J?[J(jjiJi:"~o::51iT~:bo:Jc L-tli~ Tayomaia ~J.l.l%&L-t.:, !17.:\,\',~!f.~~ Ali fan :fiEkE-~"7' Rotalia atjehtmsis VA:-; DER VLERK. 1924: CoLF.. 19630)-tfi):;J: plano-convex -::•,'f.l.!i£:! Calcarina D'0RBIG;o.;Y Q) t o:Jf"]t;l! 2 m:::tJ: ·:> "( ;f;; IJ tlliiil
J: Bae~~logypsinoides YABE and liA~ZAWA ::U;J.-r~~:n~-r;:.:~~l-'11:".: spinose structure ~J(~lfrl/l1 Quasirotalia C. L- 'CIK.IJIJ~~1.;,;,,
o'f: iR lE 11!1 f~li

Introduction and Acknowledgement!{eview of the previous works on the
Tertiary larger Foraminifera from theGulf of \lexico and Pacific regions has
1ed the writer to establish three newgenera, Quasiborelis from the lower
Eocene of Florida. Tayamaia from the
Aquitanian of Saipan and Quasirotalia
from the Pliocene of Guam. For (.juasiro·./alia, the writer is much indebted to Dr.
Arthur CooPER of the U.S. National
Museum and Dr. joshua I. TRACEY. jr.
of the U.S. Geological Survey, Washington, D. C. who kindly loaned to the writer
limestone sections of the Alifan andBonya limestones from Guam containing
the afro-mentioned Foraminifera andhelped the writer's investigation.

Systematic Descriptions
Family Alveolinidae EHRE:\'BERG• Received May 8. 1966; Read June. 20. 1966.

All the foraminiferal genera whichwere grouped up into a single family
Alveolinidae EHRE:\'BEIH~ by REICHE!.
(Treaties on Invertebrate Paleontology.
C2, vol. 1. p. C503-C510) vary fromspherical. subspherical, o\·oidal, ellipsoidal. fusiform. cylindrical. to nautiloidal
in external form. Their wall structure
and mode of growth are similar. Theirshell walls are solid and porcellaneous,consisting of a number of whorls coiling
p\anispirally around a juyenarium. The
whorls of all the genera of this family
consists of a single sheet of the spirallamella. excepting for Multispira REI·CHEI., which consists of a composite
whorl of a number of successively superposed spiral lamellae. The whorls of all
the genera are divide into multitudes ofchambers by radial septa extending frompole to pole of the test. The chambers
are S!.!bdi\'ided into many chamberlets
by the septula normal to the septa.
The alveolinids range stratigraphyica\ly from the upper Albian to Recent. In20

Shoshiru 11 ANZA Wtl

boLh the Mesozoic and Cenozoic genera,
two different modes are detected in thedisposition of the septula, either continuous or alternating.
The continuous
septula are aligned in the next succeeding chambers. whereas the alter·
nating ones are arranged alternatingly
in succeeding chambers. Most of thervlesozoic genera are equipped With COil·tinuous septula, whereas some Cenozoic
forms have continuous septura and theremainder have alternating ones. The
arrangement of the septula may furnish
some clue to the phylogenetic relations
among the genera.
The ontogeny of J'abeina DEPRAT, a
Permian fusuliuid clearly illustrates thephylogenetic succession of this genus(HANZAWA and MuRATA, 1965. 1-L\NZA·
WA. 1965, p. 241). Namely its enclothyroid juvenarium is immediately followedby some whorls of the Cance/lina-structure. which is in turn succeeded byseveral whorls of the A'eoschzcagerina·
structure before the final ontogenetic
stage of Yabeina proper begins. However. most of the alveolinid genera do
not appear to show such a differential
ontogenetic development as shown in
Yabeina. In all the alveolinid genera,
all the post-juvenarium whorls showstheir own generic characteristics. The
earliest whorls of Alveolinella DOUVILJ.E
have two-tired chambers. while the later
whorls are subdivided into three or moretiers. But Flosculinella ScHUBERT, which
has the characteristic two-tired chambers
is difficult to consider representing theearliest ontogenetic stage of Alveolinella
DouviLL~ because the septula of theformer are of the alternating type andthe latter is equipped with continuous
septula.
Oual!!eolina REICHEL and Praealveolina
REICHEL occur in the same geologic ages
and their internal structures are alike.

But the apertural features of the former
are sorne\vhat simpler than those of thelatter. The former may be regarded as
the predecessor of the latter.
Si m palveoli na (Praeah'eo/ina) REICHEL
may haye been derived from Praeah,eolina s. s. REICHEL. The former made its
first appearance later than the latter.
The unique form, Multispira REICHEL
may be considered to have originatedfrom Praealveolina REICHEL by the proliferation of the sheets of whorls.
Cisalveolina REICHEL, which is characterized by a single slit-like apertureand the alternating septura may be considered to have been derived from Praeall'eolina REICHEL, or from anothermiliolid ancestor independent from thelast-named genus. Subalueolina REICHEl.
also may be regarded to have originatedfrom this independent ancestral stockof the miliolids or from Praealueolina
REICHEL. Its septula have no definite
arrangement.
Fa~cioliles
PARKI!'\SON (=Alveolina
D'0RlliG!'\Y) and Glama/veolina HOTTINGER are surely independent from theMesozoic alveolinids in phylogeny. The
youngest l\lesozoic genus, Subalveolina
REICHEL became extinct in the Campanian and the oldest Cenozoic one,
Fasciolites PARKIJSSO~. made its first appearance in the Paleocene. Therefore,
a stratigraphic interval, from the baseof the ~Iaastrichtian to the top of theDanian Stage, exists bet\veen the twogenera. Paleontologically, it is incrediblethat the above Cenozoic form is heritablefrom the above-named l'vlesozoic one.
The Cretaceous forms now in question
should be excluded from the Alveolinidae
EHRE!'\BERG as the isomorphs of the
Cenozoic alveolinids and allocated into a
new independent family.
Both Bullalveolina REICHEL and Flosculinella SCHUBERT are also character-New Tertial'y Foramimfcral Ge1wra
ized by alternating septula. There is thepossiblity that they are phylogeneticallycontinuous with Fasciolites PARKINSON.
considering the structural similarities
and stratigraphic distribution of thethree forms.
Bore/is EHRENBERG which is characterized by continuous septula may be phylogenetically independent from Fasciolites
PARKINSO'-: which has alternating septula.
The former ranges from the lower Eo·
cene to Recent, and the latter from the
Paleocene to the lower Upper Eocene(Bartonian).
All'eolinella DoUVILI.f' with continuous
septula may be phylogenetically independent from Floswlinella in spite of thestructural resemblance of both forms.

2
Figs. l. 2. Quasibore/is gzmte1·i (COLE)
Schematic drawings of eqatorial (Fig. 1)
and axial (Fig. 2) sections. x26.8(Original: C<>I.E, HJ-1 I. I> I. 2. figs. 2. 3).
1REICiiEI.)

and Bore/is pygmaeus (HA:->Floswhnella bontangensis (RUTTE!\) is fusiform, whereas
Flosculinella globulosa RUTTE~ is spherical. But nobody has ever tried to distinguish generically JJorelis melo from
Bore/is sclzlumbergeri or from Bore/is
pygmaeus, similarly Flosculinel/a bontangensis from Flosculinella glolmlosa.
Bore/is gunteri CoLE is nautiliform,
whereas Alz·eo/inella quoyi o'ORBIGNY is
fusiform. Both are common in having
the same internal structural constituents.
They differ from each other by theirexternal form and the latter is much
more delicate than the former in internal structure. Considering the interrelation between !Jorelis melo and Bore/is
sclzlumbergeri or that between Flosculinella bontangensis and Flosculinella
g!obulosa, Bore/is gunteri may not be
rationally distinguished from Ah•eolinella
quoyi generically because of having thesame structural constituents. But Bore/is
gunteri is found in the lower Eocene of
Florida and Alt>eolinella quoyi ranges
from Miocene? to Recent. It is easily
considered that both the forms are notin any close phylogenetic relation. A
ZA \VA) are fusiform.

Genus Quasiborelis, nov.
Type-species: JJm·elis gu11teri CoLE (19·11,
p. 34, pl. 3. figs. 1-3: pl. 18. figs. 5, 6) fromthe lower Eocene of Florida.

Bore/is gunteri COLE may not be congeneric with Bore/is mdo -;FICHTEL and~lou.:.
The former is similar to thelatter in almost every respect. Especially, the former is characterized by thecontinuous septula ·:CoLE, 1941, pl. 2.
fig. 3J as the latter. But the chambersof the former are subdivided into twoor several tiers by one or five horizontal
septa, whereas those of Bore/is melo
(FICHTEL and !\loLL) are undivided.
COLE'S illustration of Bore/is gunteri
COLE 1941, pl. 2, fig. l1 shows that thisform of Foraminifera is equipped \Vithseveral rows of apertules. However, theabove description shows that this form
is indistinguishable from Alt·eolinella
DouviLLE in the fundamental internal
structure.
Bore/is melo ·FICHTEL and MOLL 1 isspherical, whereas B01·elis schlumbergeri

21

Shoshiro HANZA W.4

22

new genus name Quasibore/is is proposed
for Bore/is gunteri COLE. Quasiborelis,gen. nov. is supposed to have arisen
from Bore/is EHRE:-<BERG in the lower
Eocene.
Family Planorbulinidae ScEW AGER

irregular in transyerse and horizontal
sections respectively. The ventral layers
consists of chambers, which are arcuate
in transverse section and irregular inhorizontal section. All the chambers
cited above are common in having solid
vertical walls and finely cribrated roofs

Genus Tayamaia, nov.
Type-species: Gypsina marianensis I-lANZA·
WA (1957, 66, 67, pf. 31, fig. 8: pl. 27)
from the Aquitanian Stage of Saipan,
Mariana ls.-Coi.E, 1957. p. 337, pl. 103,
figs. 1-4.

The characteristic features of GyjJsina
marianensis are as follows:
The test is helmet-shaped and is differentiated into three sets of layers ofdifferent-shaped chambers, viz., a dome·
shaped median layer, some tiers of superjacent dorsal layers and those of subjacent ventral ones. The median layer
consists of spherical proloculus and annularly disposed chambers, which are oftruncated-arcuate type, equipped withfour stolons (refer to HAr-.:ZAW A. 1957,
pl. 27. fig. 3)· The dorsal layers consistsof chambers which are quadrangular andFig. 3.
Tayamaia mariaensis (IIA:"·
Schematic drawing of transverse
section. x 26. 5.
zAWA)and floors.
LOEBLICH and TAI'l'AN 1196,1, Treatiseon Invertebrate Paleontology, C2, vol. 2,
p. 696) pointed out that the type speciesof Gypsina CARTER is Gypsina mastelensis
BuRSCH. not Orbito/ina concat•a yar. vesicularis PARKER and jONES. The characteristic features of the chambers ofGypsina mastelensis BuRSCH are quite thesame as those of Gypsina t·esicularis

Explanation of Plate 3(Juasirotalia guameusis, gen. nO\'. and sp. nov.
Figs. 1 (Holotypc), 2, 8. Transverse sections.
1. 2. 8. Locality Ts 16-14. Guam, l\-Iariana Is. USGS col!.
Figs. 3. 4. Equatorial sections.
3. Locality Ts 16-14. Guam, Mariana Is. USGS coli.
4. Locality Ts 16-12, Guam. Mariana Is. USGS col!.
Figs. 5-7. Tangential sections.
5, 6. Near ventral sides of tests.
5. Locality. Ts 1.6-1, Guam, Mariana Is. USGS coli.
6. Locality. Ts 16-14, Guam, :Mariana Is. USGS coiL
7. Near dorsal side of test.
Locality. Ts 16-14, Guam. Mariana Is. USGS coli.
Fig. 9. Transverse section of microspheric form?
Locality. Ts 16-5. Guam. Mariana Is. USGS.
All figures thirty times naturl saize

HANZA WA:

New Tertiary Foraminiferal Genera

1

K uMAGA I

photo.

Plate 3

.~.Vezc

Tert·iary Foram1:niferal Genera(PARKER and JONES) and c;ypsina plana'.CARTER:. The chambers of these species
are destitute of stolon passages in theirchamber-walls.
Gypsina marianensis is like Gypsina
vesticularis (PARKER and joKES), one of
the typical Gypsina CARTER in major
structure (refer to HANZAW A. 1957, pl. 21.
fig. 9l. But the internal structure of
Gypsina t•esicularis is not differentiatedinto any sets of layers as that of Gypsina
marianensis. _\Ioreover, the whole surface of all the chambers of Gypsina z·esicularis is cribrated and devoid of any
stolen passage. Thus Gypsina marianensis may be distinguished from Gypsina
z.esicularia in having arcuate medianchambers with four stolons. Therefore,
it must be assigned to a different genus.
A new genus name. Tayamaia is proposed for Gyp.~ina marianensis HANZAWA,
dedicated to the late Dr. Risaburo T AYAMA who made valuable contributions
to the geology of Micronesia.
Tayamaia, gen. nov. is considered toto be more rationally referred to thefamily Planorbulinidae ScHwAGER than
to the Acervulinidae SCHULTZE because
its median chambers are characterizedin having solid vertical walls withstolons.
Geologic horizon and locality: Aquitanian Tagpochau limestone, S88, R.
TA y Al\IA. Kanat Fahan Lichan, Saipan,
Mariana Is.
Family Calcarinidae ScHWAGER
Genus Quasirotalia. nov.
The test is lenticular or plano-con vex
and may be structurally distinguishedinto a rotaloid juvenarium and a maturitas consisting of two or three layers ofchambers added on the periphery andyentral side of the juvenarium, andalmost spirally disposed. The test walls
are double in structure like those of
Calcarina o'ORBIGNY. The type-species
is Qzwsirotalia guamensis sp. nov.

Fig. 4. (Juasirolalia guamensis.
nov. Schematic drawing of transverse section. x 13.3.

Remarks: This new genus is moreadvanced than Rotalia LAMARCK in
structure and is distinguished from it
in having layers of chambers on theventral side and periphery of the test,
and double walls with thick and densely
crowded ventral canals. It resembles
BaculogypsiHoides YABE and l-IANZAWA,
but lacks the spinose structure of thelatter Pliocene.

Quasirotalia guamensis, nov.
Pl. 3: Pl. 4, Figs. 1--8
Rotalia atjelzensis VAN DER VLERK.-Cou:.
part. 1953, p. E20, pl. 5, figs. 1. 3. 9, notfigs. 3. 4.

The test is biconvex or plano-convex,
the dorsal side is flat or slightly vaulted,
whereas the ventral side is broadly
rounded. It is small, 2 mm across and1.5 mm thick. The proloculus is spherical, 120-220t..t in diameter and surrounded by a thin walls, 20-40,u thick and it isfollowed by 7 trochispiral nepionic chambers of the juvenarium \Vhich is 760800~t acrqss ~nd 420~t thick. The juvenarium is succeeded by the trochispiralsecond and third and sometimes fourth24

Shoshiro H ANZA IVA

whorls of the maturitas; the size ofchambers of the first, second, and third
whorls is usually smaller, 100f1 X 100,uand that of the fourth whorl is larger,
160,u x300f1. The walls of the chambers
are usually composed of double layers.
the inner one is thin, 20-60tL in thickness, whereas the outer one is thick, 300p
in thickness, and piereced by numerous
thick vertical canals, 20-40t1 across.
Pliocene Alifan
Geologic horizon:
Limestone.
Localities: Ts 16 and Gj9, northern andsouthern Guam. rvlariana Is. respectively.
Remarks on COLE's Rotalia atjehensis VAN llER VLERK: Rotalia atjehensis{COLE, 1963, p. E20, pl. 5, figs. 1-4, 8, 9)
comprises two forms of Foraminifera,
which are distinguishable generically aswell as specifically from each other inthis writer's view. One of them was
depicted by CotE in figures 1, 2, 9 justcited and is dealt with in this paper as
Quasirotalia guamensis. gen. nov. andsp. nov., and occurs in localities Ts 16
and Gj 9, northern and southern Guam,
Jvlariana Is. respectively. whereas theother illustrated by COLE in figures 3. 4

(Plate 4, figs. U, 15) occurs in locality
Ih 5, central Guam. Referring to the
Geological l\lap and Locality !\lap ofGuam (TRACEY. et al., 1964, pis. 1, 2)
should be noted that localities Ts 16 and
Gj 9 are located in the area of Tal,
Alifan Limestone, whereas locality Ih 5
is in the area of Tb Bonya Limestone.
Under the microscope, the limestone with
Rotalia atjelzensis appears to be moreadvanced in recrystallization than thatwith Quasirotalia guamensis, and these
two forms are never associated with eachother in the same limestone from thelocalities just cited. CoLE (1963, loc. cit.)
identified all the forms mentioned above
with Rotalia becarii (LlNNEAliS) var.
atjehensis VAN DER VLERK from Atjeh.
North Sumatra (VAN DER VLERK, 192<1.
p. 25. 26, pl. 5, figs. 21-24) and with I-lA:\·ZAW A's Rot alia schroeteriana PARKERand }ONES (HANZAWA, 1931, p. 157. pl.
26, figs. 6-8) (Plate 2. figs. 9-13) fromthe lower l'vliocene Misaka Formation ofJapan. associated with Nephro/epidina
japonica YABE and :\liogypsina kotoi
HANZAWA. As shown in Plate 4. figures
9-15 in this paper. the form are lenti·

Explanation of Plate 4
Figs. 1-8. Quasirotalia guamensis, gen. nov. and sp. nov.
1-3. Equatorial sections.
-1. Tangential section near ventral side.
Locality. Ts 16-10, Guam, Mariana Is. USNM. 625565.
5-7. Transverse sections.
Locality. Ts 16-10, Guam, Mariana Is. USNM. 625565.
8. Transverse section of microspheric form?
Locality. Ts 16-10, Guam, Mariana Is. USNM. 625565.
Figs. 9-13. Rotalia sp.
Locality. The mountain creek at the east of IIisari, Kwanto Massif, Japan.
9, 10. Transverse sections.
11-13. Equatorial sections.
Figs. 14. 15. Rotalia sp. (Rotalia atjehensis VAN DEn VLERK. CoJ.E, 1963, pl. 5. figs. 3. 4)·
Locality. lh 5-:{, Guam, Mariana Is. USNM. 625567.
All figures thirty times natural size

HANZAWA :KuMAGAIN ew Tertiary Foraminiferal Genera

photo.

Plate 4

25

New Tertiary Foraminiferal Genera
cular with a broadly rounded peripheryand lack the accessory chambers on
the periphery and ventral side of thetest unlike the form referred to ()uasirota/ia guamensis. The statistics cited
below show that the forms from thelocality lh 5, Guam and llisari, japan
are alike, but they are not quite identicalwith the type of Rot alia atjehensis V AI':
DI·:R VLERK. which periphery is rather
acuminated and with Rolalia schroeteriana PARKER and ]Ol':ES.

ComJlarison of the statistic of Rotalia atjehensis VAN DER VLERK
and Rotalia sp. from Guam and .Japan

DiameterThickness
Xumber of chambers in
the whorls
1st whorl
2nd whorl
3rd whorl
Number of chambersin the last-fo•·med whorl

SumatraGuam (Ih 5)

Japan

I. 00 mm

1. 77 mmJ. 00 mm

2.00mm
1. 00 mm

2. 5-:~

2.5-3

7
13
14?

7

16?

14-16?

0. 50 rnr-1

15-18

References cited
CoLE. W. S. (1941): Stratigraphic and Paleontologic Studies of Wells in Florida.
Florida Geol. Sun• .. Geol. Bull .. no. 19,
p. 1-91, pis. l-18.
- - (1957): Larger Foraminifera (Geology
of Saipan, Mariana Islands, pt. 3. Paleont.).
U.S. Geol. Surv., Prof. Papar 280, p. 321:~60, pis. 5·1-ll8.
- - (1963) : Tertiary Larger Foraminiferafrom Guam. Ibid., 403-E. p. 1-23, pis. 11.
HA:"ZAWA, S. (1931): Notes on Tertiary
Foraminiferous Rocks from the Kwanto
Mountainland. Japan. Tohoku Univ .. Sci.
Rep .. 2nd Ser. (Geol.). v. 12, no. 2A, p.
141-157, pis. 24-26.
- - (1957): Cenozoic Foraminifera of Micro·
nesia. Geol. Soc. Amer., _\/em. 66. p. 1111. pis. 1-H. 5 tab.
- - (1965): The Ontogeny and the Evolution

ll-13
14?

of Larger Foraminifera. Tohoku Unit.•.,Sci. Rep .. 2nd Ser. (Geol.). \'. 36. no. 2.
p. 239-256, 1 tab. pis. 30···'10.
- - and MllRATA . .tvl. (1963): The Paleontologic and Stratigraphic Considerations on
the Neoschwagerininae and Vcrbcekininae.
with the Descriptions of Some Fusulinid
Foraminifera. Ibid., v. 35, no. 1. p. 1-31,
pis. 1-20.
LoEBLICH. J.. A. R. and Helen TAPPAX,(1964): Treatise on ln\·ertebrate Paleontology. pt. C, Protista. 2, Sarcodina. v.
1. p. 1-510. fig~. 1-399: \'. 2. p. 511-900.
figs. 400·-653.
TRACF.Y.].I.. ScBLAXGER,S.O .. STARK. J.T.,
DoAl". D. B. and MAY. H. G. (196-1):
General Geology of Guam. U.S. Geol.
Sun1., Prof. Paper. 403-A. p. Al-A104,
pis. 1-3, text-figs. 1-53.
V!.ERK. I. }.I. VA:-1 DER, (1924): Foraminiferen
uit het Tertiair van java. I. Dienst. Mijnb.
Wetensch. Meded .. no. l. p. 1-13, pis. 3-5.

Trans. Proc. Palaeonl. Soc. Japan. N. S., No. 65, p. 26, Apr. 10. 1967

SHORT NOTE
Vt

1.<-'PONIDE'S BOSOENSISNEW NAME FOREPONI/JES ASANOI HIGUCHI. PREOCCUPIED*YU HIGUCHI
Suncoh Consultants Co., Ltd.

Richard CHARJ\IA TZ, American !\1useumof Natural History, for his kind advice
about the preoccupied species.

While carrying out a study of Foraminifera from the gas field in Chiba
Prefecture, it was discovered that Eponides asanoi HIGUCHI (Trans. Proc.
Palaeont. Soc. japan, N. S., ~o. 60, pp.
178-181, pl. 21, Dec. 20, 1965) from theboring well at Kujukuri-machi. Sanbugun, Chiba Pref. is preoccupied by
Eponides asanoi YOSIIIDA, 1958 (Hokkaido
Gakugei Univ., jour., vol. 9, No. 1, p.
257. pl. 2. figs. la-c) from the Cretaceousof Hokkaido.
The new name Eponides bosoensis is
proposed for Eponides osanoi HIGUCHI.
1965.
Acknowledgement is paid to \-1r.

References
HJGUCtll, Y. (1965). On the some new species
of fossil foraminifera from the boringcores in the gas field in Chiba Prefecture,
Japan. Trans. Proc. Palaeont. Soc. Japan,
N. S .. No. 60, pp. 178-181. pl. 1, 1 table,
1 text-fig.
YosHIDA, S. (1958). The foraminiferal faunaof the upper Cretaceous llamanaka andKiritappu formations of eastern Hokkaido.
Japan. jour. Hokkaido Gakugei Unit• ..
Vol. 9, No. 1. pp. 250-264, pis. 1-3, 1
table, 2 text-figs.

• Received July 28. 1966

26

Trans. Proc. Palacont. Soc. Japan, N. S .. !\o. 65, pp. 27-46, April 10, 1961

518. GRAPTOLITE AND TENTA.CULITE CORRELATIONS AND
PALAEOGEOGRAPHY OF THE SILURIAN AND DEVONIAN
IN THE YUNNAN-l\IALAYA GEOSYNCLINE*
C.K. BURTON
Department of Geology. Faculty of Science, Chulalongkorn University
Bangkok, Thailand

ditN--. 5i -( .l~li·J~'lll.) :/ '"''"' .

r rf Y'f{,ll.)~:fi c tentaculites r: J: 15 ~Ht d: •'illl!i]l: l!!:~j'.;jti§..,. ~H iJ·G~~Cl):lifi-~ tentaculites ;';'-jEQ~t,. "(I. . .::,, 'f\.-l.i0.7~;1!>7J;,t Llandovery

Wl0 {.0-:'-;ll\ Wenlock lw.n:a, ~" Tentaculites i;l:!IJJ Go~ ·U=pTM-T ,f. Y*ll) {, (7)·::a, <;,,•=

~tt:nll~ t JJ'IH:) G·fr.ti ?f<;ti'f;t~::w.,. -co<. 16 @:!11!.·:: ;;tfUI-ft'lJimiJ:::f'f-:>-:: 'lit!\ t..
-: 1• • ;:,, *<.oGht.:rJ~;k'.!:-m!f.;t..:rH~ t..t:Wf-~11 >t.:.:. 2: :;;. • ..::.llJJ;? to:::,.-,~.-T:r.
Y~ tentaculites O))tf·f,!:v'?~·ijllf~1£~)(Lt. ~U4""'71ii·0J.t1(1Eii1!i. ~~~-;")ff~li7J:'"-·C~l¥ill§ffii;:.Q: ftl!rlil~l!t!!'li\'-e::~:.:: 'l'r ;ru:::..1"-.>.:.. n:-:' ~ -.:,, ..:. Cl);; ? 7"..: -:1 .; - -:rt~JiJttr:i.
-)eyl'f-Jt.:l\'iili:tk"ll)f.t* L. "Cf'f.iffi~E~1.1:J1HJlftl!·!l\':i·J?iM'~ L-. t;ltv ·-OW'Ji!l!,~t.l:m:ucJ 1.... t:a,f:::.;!Jtl.Jil''J!Ililn:g . , t:iMt~"t' <0 !> .!:~ ;t 1?~ 1. -i:,. ;:,Cl.)iJ~H\':!flWJO).i1l!(nl¥'Ht. ~i*it.l· l?:ltltr'"'*c'1£E c

<
c.

<

c

c

<

<

I:&:Pil'J!:0U:. k:h~J· G:B ~:, L;t 3 - 1=1 ::> .- ~ c )!f.~n:<~;-? t:..:. :!: '2 ;1;-rv · -?t·Cl.)iltE~~:;lJ, .:;:, ,.: clJ~iN-"' 7 1 !l!![liJ*f:;t. -:!:f.:, ~ -...- 7 '"\'ftl!ll.IU: {,JI!j'k }!I!·.> '"Cv ·t:, l~i1J""C'j"i. Kalimantan(1 Y r ft::/70):f.•t.-t.;;t-) ~-1?.::. :>.-"f.::.7''J Irian Barat '.!:-"-"":'m;;t-7-. ~ 7 ~ 7::1lJu'< '· •t: WJflEi'£1.1:a, t.,, I~f\':O)~Q :/ '"' ,~.-~c iii: 11 ~ rf :.-- *C tentaculites c :?>mf'l' ., -c I!Ul',T ~.:-::. ;;~:, Victoria ·c:f> \J10h "( '. • ~,C. K. BcRTo;o.;r" .... I can well recall the thrill of delight and astonishment with which 1 recognised. in
the first fossiliferous piece of rock that I broke off, a fragment of a graptolite .... "LA ToL'CllE, "The Geology of the Northern Shan States"
Introduction

Graptolites and tentaculites are now
known from several areas disposed in anarrow zone extending from west Yunnan through east Burma and west Thairand into northwest Malaya.
The first discovery of graptolites inthis region was made by LA Touci-IE in
1899 in the Northern Shan States 'of
Burma. Continued investigations by
this pioneer yielded more graptolites,with numerous other fossils. including
tentaculites (LA ToucHE, 1913: REED,* Received Apr. 9, 1966: Read Jan. 22. 1967.

1906. 1915).
Graptolites of Silurian age were next
found in the Chinese province of Yun·nan by BROWN (BROW:\. 1913; REED.
1917) and the faunal census here has
been continuously augmented. by later
workers (YIN & Lu. 1937: Sui\, 19,15:
SU~ & SZETU, 1947 etc.).
BROWN and
SoNDHI (1933a. b) then extended the re·cord of graptolites and tentaculites to
the Southern Shan States, their collections being described· by ELLES and by
REED (REED, 1932, 1936).

Later. tentaculites were also proved inwest Yunnan (by WAl\GI and the geo-

28

C. K. BURTON

synclinal nature of the tract between
this area and the Northern Shan States
was recognised and named the SinoBurmese geosyncline (SuN. 19-15).
Tentaculites were found in Thailand
in 1950 (BROW:-\ et al., 1953i and graptolites were encountered in Malaya. close
to the Thai border in 1956 (JONES, 1959).
KOBA y ASIII (1960) now realised that thegeosynclinal belt extended to this vicinityfrom Burma. He subsequently termed
this the Burmese-\lalayan geosyncline.
at the same time reporting graptolites
from two localities in Thailand (KOBA·Y ASHT, 1964).
Recent work by the writer and hisformer colleagues in the Geological Survey of !vlalaysia (\lalaya) has shownthat there is a considerable expanse of
Silurian to Devonian graptolite- andtentaculite-bearing strata in northwest
r.Ialaya, and we have further been able
to demonstrate (BmnoN, in the press. b)that the mid-Palaeozoic geosyncline extended through the country for some
300 miles from the Thailand frontier tothe western seaboard in !vlalacca state.
For convenience the term "Yunnanl'vlalaya geosyncline " is used here to
designate the whole geosynclinal tractfrom west Yunnan to south l'vlalaya (see(Fig. 1). The informal nature of thisusage is emphasized since it is not yet
fully established that the entire belt
constituted an uninterrupted basin ofdeposition at any one time and sinceextensions may exist beyond Malaya
and Yunnan (see below). Until thesequestions are resolved, "Yunnan-.Malaya
geosyncline" may be used concurrently
with such conceptual terms as SinoBurmese geosyncline, Burmese-!vlalayan
geosyncline. \lalayan geosyncline etc.

Details of graptolites and tentaculite
occurrences in the YunnanMalaya geosynclinea) l\Ialaya
The beginning of a new era in l\lalayan geological research was signalized
in 1956 by jONES's discovery of graptolites on the Langkawi Islands in thenorthwest (Lat. 6"25'N; Long. 99.55'E).
Tentaculites were later found in thisvicinity, although their identity was notappreciated at the time (Jo:-ms, 1959.
1961).
Subsequent work has shown that theoccurrence on the Langkawi Islands isbut the outpost of an extensive development of Silurian to Devonian graptoliteand tentaculite-bearing rocks located 60
miles to the southeast in the states of
Kedah. Perak and Penang. As presently
known. the bulk of these rocks (some600 square miles of outcrop) lies between
S"17' and 5'56'N and between 100'21'
and 101"04'E. In all. 103 graptolite localities and 45 tentaculite localities havebeen recorded in northwestern Malaya(of which 87 and 36 respectively were
found by the writer and his assistants
during the past three years, 1962-65).
The majority of these fossils occur inthe euxinic ~vlahang Formation 186 graptolite and 40 tentaculite localities) andnearly all the remainder are containedin black shale members of the contemporaneous limestone-rich "Baling Formation "* (or Group) to the east (13 graptolite and 4 tentaculite occurrences)and the" Setul Formation" of the Langkawi Islands in the northwest \2 incid* Throughout this communication theconvention is followed of placing informal
stratigraphic names between inverted commas.

519.

Graptolites and Tentaculites tn tlte Yunnan-Malaya Geosyncline

29

H UP Et

TIBET

kantiruo

SZECHUAN,•
EPA~ [.'', ... ,

TungtzuI

KUEICHOW

INDIA'

KIANGSI
HUNAN

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Sh•lf Faco•s Recorded/

Oasin Axis Obser•ed/

Basin Axi,. InferredGeanticllnal Axis

Mi.IOO0.~
Kmro:>

100-100

Fig. 1. Map of South East Asia showing the location of the Yunnan-Malaya Geosyncline
and the disposition therein of some Mid-Palaeozoic features and localities of significance.

C.!{. BUNTON

30

ences of graptolites and one of tenta·
culites).
Farther south, in the centre of Perakstate, two other discoveries of graptolites have been made. So far. tenta·
culites have not been found in this area.
Study of Malayan graptolites is still
Locality

Locationat an early stage. Ten collections fromthe i\1ahang Formation have been examined in detail by STRACHA:'\ andjONES (COURTIER, in manuscript) andin five of these specific determinations
were possible, viz.,

Fossil identifications

Age

KKF8

5"21 '22''N:
100•-14'51"E
Map 21/ll-182641

Monograptus gregarius LAP.
Monograptus cf. inopinus TOR:'\'.
Monograptus sp.
Glyptograptus cf. sinnua/us NicH.
Diplograptus modes/us LAP.
Climacograptus rectangularis M'Coy

lower ]\riddle
Llandoyery

KKF9

5"20'57"::\ :100"45'25''E
Map 21/12493633J-lonograptus aff. concinnus LAP.
Diplograptus modestus LAP.
Orthograptus sp.
Climacograptus sp.

lower Middle
Llandovery

KKFlO

5'22'10"N:
100'·13'0l"E
l\1ap 21/11,159658.\lonograptus decipiens TOR:'\'.
Monograptus sp.
G/yptograptus sinnuatus NICIJ.
Climacograptus cf. rectangularis l\f'COY

upper Jl,liddlc
Llandovery

KKF2-1

5' 19'02"N:
100'45'0-!''E
l\Iap 21/12-18759-1'vfo11ograptus decipiens UoRN.
Monograptus convolutus His.
MonografJtus sp.
Cephalograptus tubulariformis );IcH.
DiplograjJtus sp.
Climacograptus hughesi NICII.

upper Middle
Llandovery

KKF18

5"21'·16"N:
100'2·1'03''E.Map 21/11·173649

Monograptus aff. ga/aensis LAY.

middle Upper
Llanrlo\·cry

These fossils span a rather limited
time range. from graptolite zone 19(Monograptus ~regarius) to zone 22(,\Ionogratus turriculatus) or 23 (.Hono·
graptus crispus). The remaining collec·
tions of l\lahang graptolites have been
examined only briefly as yet. but thebulk of them are clearly Llandovery inage (JoNES. personal communication).
Orthograptus aff. resiculosus and ;\/ouo·
graptus cyphus are the oldest forms reported, respectively zone fossils of graptolite zone 17 and 18, \Vhilst in a very

recent (personal) communication _TO:\'ES
records the presence of the Wenlock

Cyrtograptus.
Graptolites of the "Baling Formation"
have not yet been studied. but it isevident that they also comprise diplograptids in association with mongraptids.
indicative of a Llandovery date. Twoargillite horizons occur amidst the lime·stone of the "Setul Formation" in Langkawi (see Table 1). Both contain graptolites.
From the "Lower Detrital
Band", STRACIIA:'\ (in KOBAYASHI et a/.,518.

Graptolites and Tentacn/.ites in the }:'unnan-Malaya. Geosyncline

1964a) determined :Monograptus (?) 2 spp.
Dimorphograptus sp.
Climacograptus rectangularis
Climacograptus sp.
Orthograptus sp.
G!yptograptus sp.
The horizon yielding Dimorplwgraptus
was said to approximate to the Lower
Llandovery zone of Orthograptus r-·esi·
culosus (17). Some 400 to 650 feet higher
in the succession. the " Upper Detrital
Band.. carries the Middle Llandovery
species Monograptus clingani. identified
by BALL and STRACHAN (KOBAYASHI elal., 1964a).
Southwards (along the strike) of theMahang outcrop, in the Sungei Siput·
lpoh area of central Perak. the proportion of limestone is again high. Asso·
cia ted shale near Kanthan (c 4' 46'N:
101 •06'E) contains graptolites, deter·
mined by BALL as diplograptids with
faint indications of being of the (Middle
Ordovician to Lower Silurian) ortho·
graptid type (INGHAM and BI{ADFORD.
1960. p. 20). Another locality at Chemor.
ll miles to the south was found to carry
Orthograptus sp. (BALL, written communication).
Finally. an isolated discovery of mono·
graptids has been made by Inche jA'AFAR
BI:\ AHMAD in the Foothills Formation
at Karak, Pahang state. central Malaya
rjONES. personal communication).
The Malayan tentaculite discoveries
have recently been announced and preliminary descriptions giyen (BURT0:-1, in
the press. a). Subsequently systematic
examination has been carried out byProfessor BoucEK.
His findings are
summarized below. These fossils are
small, less than 10 mm in length, thinshelled forms manifestly belonging to
FISHER's (1962) Order Dacryoconarida.
although they usually do not possess a:ndrop-like embryonal bulb, but rather amore primitive tubular projection. As
is common elsewhere. ringed and un·ringed types of similar proportions occur
together and it seems conceivable to thepresent writer that this may represent
some kind of dimorphism.
BOUCEI< (personal communication\ saysthat the l'vlalayan ringed tentaculites
commonly prove to be close to the Lower
Devonian Nowakia acuaria.
In the'vlahang Formation he has distinguishedanother form with scantier rings, similar
to some Eifelian or even Givetian speciesof Nowakia (e. g.. locality KKF14.
5'21'51"N; 100'43'04"£: Survey Dept. of:Malaya map 21/11 445651).
BoUCEK
likewise considers that there may be
two species of smooth tentaculite in the
Mahang. The larger individuals (as at
locality Khl3. 5· 43'07''N; loo·36'29''E;
map 21/7 313080) belong to the group of
Sty/io/ina fissurc!//a HALL. mostly of
1\tiddle Devonian (Eifelian-Givetian) datein Europe, although possibly somewhat
earlier elsewhere. Smaller shells. if they
are not Slyliolina fissurella too. may becompared with similar forms which
occur together with Nou·akia acuaria in
Europe.
Tentaculites from one locality in the" Baling Formation " have been seen by
BOUCEK, who observes:.. In Joe. rl (Upper Perak), together with
Sty/iolina is .... (a form) .... very close to
Nowakia acuaria (smaller forms) and I
think it is possible to correlate the beds
with Lower Emsian (middle part of Lower
Devonian)"

We have also identified Striatostylio·
linids (Lower to i\liddle Devonian) at
this locality (I.3URTOJ\, in the press. a).
The •· Upper Detrital Band .. of the"Setul Formation .. bears tentaculites at
one point. These comprise Styliolina cf.
fissurella again. with a ~owakiid.

32

C. K. BURTON

13oucEK considers this horizon Middle
Devonian (Eife\ian, or more likely Givetian).
Thus, in northwest Malaya. the graptolites are Lower to l'vliddle Silurian inage, whilst the tentaculites are Lower
to l\hddle Devonian. No fossils of Ludlow age have been proven in the area.
It is surprising to find that at 16 localities graptolites and tentaculites occur
together on the same bedding planes.
15 such localities lie in the l\lahang For·mation where the graptolites accompany·
ing the tentaculites are often poorly
preserved and have so far proved speci·
fically identifiable in only two cases.
Both of these are referred to the midUpper Llandoverian Monograptus ga/aensis. Associated tentaculites appear tocomprise both Lower and Middle Devonian forms.
Whilst no admixture of graptolites
and tentaculites has been found in the"Baling Formation", a comparable situation exists therein for the Lower Emsian
tentaculites detailed above are intermixed with Ordovician graptolites, including the agnostic! genus Trinodus(identified by KOBAYASHI. personal communication). Similarly. in the '' Setul
Formation" the Middle Llandovery
Monograptus clingani and Middle Devonian tentaculi.tes are intimately associated together in the " Upper Detrital
Band".
b) Thailand
In Thailand, where a time-stratigraphic
rather than a rock-stratigraphic classification has been adopted (BRow:-: et a/.,1953) the Kanchanaburi Series extends
from the Silurian to the Carboniferous.
Information is at present limited, butthree graptolite andjor tentaculite localities are known herein.
At Ban ~a. northeast of Thung Song,in peninsular Thailand (see Fig. 1),
poorly preserved specimens of Climacograptus and Dip!ograptus from a thin
shale band in a limestone succession indicate an Upper Ordovician to Lower
Silurian age (KoBAYASHI, 1964, p. 6;
KOBAYASHI et a/., 1964b, p. 49-50).
A little over 400 miles north-northwestof Ban Na and about 150 miles westnorthwest from Bangkok is Na Suan, inKing Amphur Si Sawat. where tentaculites of Mahang type occur in pinkish
sandy shale. DuNCAN (in BROWN et al.,1953, p. 33) has likened these to forms
referred to Styliolina clavula and Tentaculites -elegans by PATTE and REED in
Indochina
and Burma respectively.
"Styliolina clavula " is a synonym for
Styliolina fissurella HALL (usually of
Middle Devonian age) whilst BARRANDE's" Tentaculites elegans " is now regarded
as comprising several (Lower to Middle
Devonian) species of Nowallia (BoucEK,] 96-t, p. 59. 80).
Some 350 miles farther north. justsouth of Fang in the extreme northwestof the country are black argillites. partly
siliceous and associated with chert.
KonA YASHI (1964, p. 6) reports that thesestrata contain the Lower Llandoverian
Monograptus cyphus, which is also known
from the lithologically similar Mahang
Formation of Malaya. Other graptolites
at Fang may be Llandeilian or Lower
Caradocian.
Colonel Samak BURAVAS, who discovered these graptolites. informs thewriter (personal communicalion) thattentaculites also occur close by.
c) Burma
In the Northern Shan States. graptolite- and tentaculite-bearing rocks are
known from the early work of LA
ToucHE (1913). The succession he elucidated. with suggested correlations by.S18.

Grnptol.ites and Tentaculites in the Yunnan-1lfalaya Geosyncline

the present writer. is set out in Table
1. The Upper Ordovician \\'ith. according to SuN (Su:-; & SzETU. 1947). thelowest Silurian. comprises limestones
and shales with shelly fossils. This isfollowed by a discontinuous horizon ofwhile shale !black at one locality) which
outcrops in the vicinity of Panghsa-pye(c22'47'i\: 97'16'E), some 90 miles north·east of Ivlandalay. It carries the follow·
ing graptolites:Orthograptus vesiculosus.\fesograptus modes/us
G/yptograptus cf. persculptus
Climacograptus medius
C/imacograptus tornquist i
Climacograptus rectangu/aris
Monograptus tenuis
Monograptus gregarius
Monograptus cyp/ws
Monograptus concinnus
Rastrites peregrinus

(M)
(M)

(:\I)

(M)
(l\1)

Forms marked t~vl) are known in i\lalaya,where much systematic work remains
to be done. The Panghsa-pye gratolites
listed above are rather early in the
Llandovery. pertaining to the zones of
Ortlwgraptus !'esicu/osus (17). Monogra·
plus cyphus {18) and Monograptus gre·garius (19). In addition to these. :\lono·
graptus priodon and Cyrtograptus. pos·sibly indicating the base of the Wenlock.
were found at one locality whose strati·
graphic position appears to correspondto that of the Panghsa-pye band (LATOUCHE, 1913. p. 129).
The succeeding Namhsim Stage com·prises coarse clastics with a \\'enlockian
shelly fauna. but graptolites reappear in
the Zebingyi Stage (limestone and shale)in the form of Monograptus cf. riccar·
tonensis and MonograjJius dubius. The
former is a \\'enlock zone l27J fossil andthe latter is Wenlock to Ludlow in age.
Together with these graptolites areother apparently Wenlockian fossils(Meres/ina. }/odiolopsis etc.) plus someof Devonian aspect. including numerous
tentaculites and Orthoceras aff. commutatum and / 1/wcops (Dalmanites) swin·
lwei. This faunal admixture is recorded
at five places. between 20 and 30 miles
east and southeast of ~landalay. Tenta·
culites are present at all five localities.
usually in great proliferation.
Theywere identified by REED (1906) as Ten·taculi/es eleg011s and Stylio/ina cf. laevis.
but BouCEK {196<1. p. 81) believes theformer to be, in fact. the Middle De·
vonian .Vowakia cancellata and has
further shown that " Styliolina /ae!'is "is another synonym of Stvliolina ]issur·
ella. usually I\liddle Devonian also. al·though similar forms may be somewhat
earlier. The associated Orthoceras com·mutatum is of Lower Devonian age inthe Harz and Phacops (Dalmanites) steinlwei is closely allied to south European
Lower Devonian forms. Subsequent to
LA ToucHE's work a wholly Lower De·
vonian shelly fauna was recorded fromthe Zebingyi on the Lashio·I\long·pyenroad (PASCOE. 1959. p. 650).
REEll (1906, 1915) and LA TOUCHE(1913) regarded the Zebingyi Stage as
Upper Silurian or transitional SilurianDevonian and later than the Namhsims.
It is contended here that this syncretism
is not valid. The two dates indicatedby the Zebingyi fauna are too well defined and too far apart for this to be achronologically homogeneous assemblage.
In particular, the exclusively Lower
Wenlock
Monograptus
riccartonensis
could not ha\·e been a contemporary of
the Middle Devonian Nozrakia cancel/ala
with which it is associated in LA
TOUCHE's locality ·!4. Pyintha (21"51'30"N:
96'24'30"E). It is therefore postulated
that, as in :\lalaya, two faunules of differing ages are mixed together in the
Zebingyi of the North Shan States. As

C. K. BURTON

34

Table 1.
,---

"fAHAIII_§ BASil'/t\1.~ /tfALAY.&i 1

Mid-Palaeozoic Correlations in theIs.

LAN~K,qWJ
N W. f1ALAYR 2

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1 From BURTO!' (in the press, b).
2 Modified after ]ONES (1961) and KOBAYASHI et a[. (1964a, b).
3 Modified after BRow:-~ et a/. (1953) and KoBAYASHI (1964).

in northwest Malaya the older component
is Wenlockian and the younger is Lower
to Middle Devonian. The Wenlockian
portion of the Zebingyi may be, in part,the lateral equivalent of the Namhsim
stage.
Geological survey in Burma was extended to the Southern Shan States by
BROWN and SONDHI (1933a, b) and theirfossil collections were examined by
ELI.ES and by REED (REED, 1932, 1936).
The mid-Palaeozoic sedimentary succession here is included in Table 1.

Limestone, argillaceous limestone andshale with shelly faunas constitute theUpper Ordovician. The Llandovery isagain represented by black and bleachedgraptolite-bearing shales, apparently
more extensive here than in the North·ern Shan States. They appear at threemajor localities (Wabya Taung, tviebyataung and Panghkawkwo) and one or
two minor ones. lying in a zone some
60 miles from east to west between
Kalaw and Loilem (see Fig. 1). A composite list of all the graptolite species

518.

Graptolites and Tentaculites in the Yunna.n-Malaya Geosyncl·ine

85

Yunnan-Malaya Geosyncline.

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·l Modified after BRow;-; and So:->Dtll (1933a, b) and REED (1936).
5 Modified after LA ToucHE (1913).
6 Modified after SuN and SzETU (1947).

recorded is given below. Those accom·
panied by an (N} also occur in North·shan and those with an (I'd) are present.in Malaya.
Monograptus circularis
concinnus
co11volutus
cyphusdecipiens
difformis
distans
fimbriatus
gemmatus
gregarius(~l\1)(M)(Nl\1)( l\1)(Nl\1)

incommodus
jaculumlobijerus
mille pod aregularis
Diplograptus (.\lesograptus) magnus.:
Orthograptus mutabi/ist·esiculosussp.
Climacograplus innotatus
mediusrectangularis
scalar is
tonrquisti

(NM)

(N)
(NM.)
(~)

C. K RURTON
sp.
Glyp/ograplus tamariscus
serratus
Retiolites sp.
Monograptus Hl"O[utussandersoni· ·sedgwicki
tenuiszwdulatus(:'\)

Due largely to a rather confusedstatement by REED 11936. p. 103J, PAscoE's (1959. p. 654; summary of the
Llandovery graptolite beds of the Southern Shan States contains a number of
errors. He says.
"The lo\vest zone is that of Monograptus
cyphus. the highest that of M. sedgzt"icki,
and above this comes the zone containing
M. lobijerus, which is also present in thePanghsa-pye area of the Northern Shan
States. These three zones are all represented in the 'Vabya Taung exposure.
The, zone of M. sedgwicki has not beenfound in the country between Kalaw andTaung-gyi, nor has it been recognised in
the Northern Shan States···.

The actual position is as follows. Thezone of Monograptu.~ cyphus (18) is
known only at Wabya Taung, in thewest lc.23'53'N: 96'32'E). The MonograjJtus sedgwicki (21) zone is not provenhere but apparently occurs at ivlebyataung 120'26'N; 97'47'30"E) and at Panghkawkwo, near Loilem. in the east. In
conflict with PASCOE's statement. theformer locality lies between Kalaw andTaung·gyi. The range of Monograptus/obiferus is normally from zone 19 to 21.
but it is perhaps most often found inzone 20 and possibly occupies this horizon in the Southern Shan States. for inboth of its appearances there. at Wabya
Taung and Panghkawkwo, it is accompanied by the zone fossil Monograptus
convolutus. This zone may conceivably
be represented at Mebyataung too. but
this is not yet established. It is notknown in the Northern Shan States.
The Llandoverian graptolite beds are
succeeded by the Loilem Stage, comprising sandstones. limestones and sandy·shales and bearing a poorly preserved
brachiopod fauna plus Monograptus cf.
z:u/garis. suggestive of a Salopian date.
The Loilem Stage is probably to be correlated with the Namhsim Stage of
1\orth Shan (PASCOE, 1959. p. 651}.
Limestone and shale of the Zebingyi
Stage re-appear in South Shan. once
again with an asynchronous faunal association. In a mauve mudstone southeast of Taung-ni (20'3'1'N: 96°49'E) andnot far from 1\lebyataung. SO:-IDHI discovered the Wenlock graptolite Monograptus lJomerinus, along \Vith tentaculites referred by REED (1936) to Tentaculites elegans and Styliolina clavula.
d) Yunnan
Farther north. graptolites and tentaculites are known in the Paoshan regionof west Yunnan. southwest China(BRowN. 1913: REED. 1917; Yil'\ & Lu.
1937; Su:-<, 1945; Su:--; & SZETU. 19-t/
etC.J.
According to the last-named
authors. the Paoshan succession is very
similar to that of the Northern Shan
States (see Table 1). The Upper OrdoYician and lowest Silurian again constitutes limestone and shale with a shelly
fauna and the Llandovery (Lower Jenhochiao Series) includes black shales
with abundant graptolites. -15 species
recorded here are set out in Table 2 beside lists of Llandovery graptolites fromthe areas discussed above. In Yunnan
all Llandovery zones from that of Orthograptus vesiculosus ~no. 17; to that of.\Jrmograptus crispus (no. 23) are recorded. a range corresponding to that indicated in i\lalaya and which O\'erlaps
those of Burma.
As in Burma and t·"lalaya. Wenlock

518.

Graptolites and TentacHlites in the 1-ltnnan-Jllalaya Geosyncline

graptolites are known from west Yunnan. zones 28 and 29 being represented
in the Upper Jenhochiao Series (Su:-.r and
SZETU, 1947). Exceptionally. however.
Ludlow graptolites (zones 32 and 35) arealso reported here (YIN and Lu. 1937).
Furthermore, in common with othergraptolite-bearing areas in the Yunnan/11!a!aya geosyncline. tentaculites are en·countered in the Paoshan region andare again referred to the superceded
Tentaculites elegans (SU:--i, 19-l5L Sun
regarded the tentaculite beds as younger
than the jenhochiao and named them
the Washih (\Vasehj Formation. corresponding to the Burmese Zebingyi Stage.
On the other hand. WANG. the discovererof these tentaculites. believed the containing rocks to be the lateral equivalents of the Upper .fenhochiao <Su;.; andSzETU, 1947. p. 8). This would seem tobe the correct interpretation since theWenlock ,\lonograptus t•omerinus wascollected immediately above the .. Tentawlites e/egaus .. horizon. Nevertheless.
Su:--;·s correlation of the \\"ashih \Viththe Zebingyi still holds good.
Graptolite and tentaculite correlations
within the Yunnun-Malaya
Geosyncline
From the foregoing survey it emergesthat the anomalous association of Silurian graptolites and De\·onian tentaculites recorded in l'vlalaya (BPino;-.;. in thepress. a, b) also occurs in the Northern
Shan States. the Southern Shan States
and west Yunnan. The close proximityof graptolites and tentaculites at Fangin northwest Thailand implies that thesame faunal admixture may feature
there (see Table ]J·
It might be contended that this anomaly is only apparent and that either:37

the graptolites involved are DeYonian inage. or that the tentaculites are Silurian
forms. However, the Silurian dating of
the graptolites is attested by the renowned graptolite experts ELJ.ES (for13urma) and STRACHA:-J (for !'vlalaya). In
addition. Boul:EK (1961) has stated that.
"The first representatives of the pelagic
nowakia-Jike tentaculites ...... appeared
only at the end of the Silunan .. and thesame authority has personally testified
to the Devonian age of the :'vlalayan
and one at the Burmese tantaculites.
Complimentary to this mingling offaunas is a palaeontological hiatus andpossibly a sedimentation hiatus also.
The time inten·a! between the two admixed faunules is not represented in
the local fossil record (except. partially.
in Yunnan) and rocks of this age, it
they exist. cannot therefore be recognised.
There is some variation in the ages of
the component faunulcs. particularly theearlier one, and hence the fossil gap is
not eyerywhere of the same duration,
viz.,\Nest Yunnan:
Wenlock-Devonia n:'\orthcm Shan :L. Wenlock-1..-M. Devonian
Southern Shan :'\Ven lock- Devon ian
Northwest Thailand :L. Llandovery-Dcvonian
Northwest Malayaa) West (Langkawi):
M. Llandovery-~!. De\·onianb) Central (Mahang):"Wcnlock-L.-M. Devonianc) East (Baling) :Ordovician-L. Devonian

Further work may well modify this picture. :\t present the ~lalayan evidence
suggests that the dating of the interval
depends, to some extent at least, on
position in the depositional zone.

C. K. BURTON

38
Table 2.

Llando\·err Graptolite Correlations in the Yunnan.Malaya Geosyncline.

----

c,

I
01

Spccicst:-;:.2:

I

I

~

o:l

-=. >.

<=II$.!!:0:
lm2'1;:: 0:cl·-5:;,0:1
QJ!$~ ~~ ·~275 z~

1x ·-~-~~--· Monograptus -run-ct-.n-a~-;"\fonograptus atavuslx
sande1·soni!Jecki-I
X
X
sedgwicki
circular isXilxX
spit·a/isclingani
X
X
tenuisX
concinnusX
I X I X
X
turriculatus
X
X
cont•olulus
X-I
I X
tmdulatus
XX
cyplzus
X I X
I----1-,-·-decipiens
I X
X lx
Rastrites equidistans
x ,I dextrosus
jX
linnaei
I x I I difjormis
X
ma:dmus
1 x
idislansi X
peregrinus, x : x !- ' .timbriatusXI- - - - - - --~-'-1-.---Ceplzalograptus tubulalijormis , - , - 1 x
flagellar is- - --·-- - - - - - - -- '--l--·--f-I
galaensisx Climacograptus lzuglresi
I X
I
1 -/ gemma/us
X'
innotatus
1 I- 1 x
gregarius
X I
mediusxx
Xlzal/i
rectangularisx x x' x
I X
hybrid us
seal aris
X 1-l X 1incommodus: X - I x
tiirnquisti
X 1 X I X Iinopinus,
X ~ -------- ------·-----DiPlograptus
I I , I
intermedius! x I(Mesograptus) modes/us, x , x x
i1wo/utus
X
I
Afesograptus magnus
I x
I x
jaculum
X
X
I_[X l-1Gladiograptus periatus/eptotlzeca I X
lobiferus
I X
x
Glyptograptus--incer~ - - - '--;-1--.=--,1- - m'coyiXpersculptusx
millipoda
X
serratusX:xnodijerXsinnuatus
X
nudus
X
tamariscusx
1
planus--------X
Orthograptus vesiculosus
I - I X I X 'I X
priodonX, X
mutabilis
I X
regular is
X
j

-1

I-

-

j

i

i-

1

-

1

1

1

-----------

rtwo/utusX--1-,-~-

Petalograptus minor
pa/meus- - - - --------

I
i

x

I

X

-

I
-~-

I

-

All specific references are listed here, including the comparative .. aff."." cf." and"?" identifications.
2 Taken from REED (1917). YIN and Lu (1937) and Sc:-.; and SZETti (1917).
3 Taken from LA TovcHE (1913).
4 Taken from BROWN and SONDHI (1933b) and REED (1932, 1936).
5 Taken from CouRTIER (in manuscript). KoBAYASHI et a!. (1964a) and Jo;-;Es (personal communications) N.B. Numerous collections made in this area have not yet been examined in detail.
6 Monograptus priodon occurs here in beds assigned to the Wenlock by LA ToucHE (1913,p. 129).
7 This form is referred to Climacograptus prerectangularis in BR0\1'1\ and Sor-:DHI (1933b. p.
213) but to Cl. rectangularis in REED (1936. p. 10·1-6).

.518.

Graptolites a.nd Tentaculites in the Yunnan-Malaya Geosyncline

Llandovery graptolites occur in all the
documented fossiliferous areas in the
Yunnan-l\lalaya geosyncline except for
Na Suan in central western Thailand,and possibly Ban Na in south Thailand.
The species reported from the four best·
known regions are listed in Table 2.
which shows that close correlation exists
in the lower half of the Llandovery.
Monograptus gregarius, Monograptus
concinnus and Climacograptus rectan·
gularis are present in all four regions.
Furthermore, Monograptus cyplws. whilst
not known in Yunnan. occurs at Fangin northwest Thailand as well as inl'vlalaya and in the Northern and South·ern Shan States. Seven other species of
Llandovery graptolites appear at threeout of the four main fossiliferous areas.
It is likely that further work on the
Malayan collections will buttress these
correlations and additional discoveries
will almost certainly be made in Thai·
land.
Wenlock graptolites have recently
been proven in northwest Malaya. but
full details are not yet available. The
Zebingyi Stage of the North Shan area
contains the Wenlockian Monograptus
cf.
riccartonensis and ,\lonograptus
dubius together with tentaculites and in
the same stage in South Shan the \\/en·lockian .Honograptus vomerinus accom·
panies tentaculites. In the equiYalent
Washih Formation of Yunnan. Monograptus z;omerinus enters into a similar
association. This species and Alono·
graptus dubius also occur in the Upper
Jenhochiao Series (Su:-.: and SzETU. 1917).
thought here to be contemporaneouswith the \Vashih.
A small ringed tentaculite. e\·erywherereferred to BARRA:\DE's Tentaculites
elegans is recorded at Na Suan. Thai·land. in North and South Shan and inwest Yunnan. The original discovery:39

from the Northern Shan States has, as
observed above, now been re-designatedas the Middle Devonian Nowakia cancel/ata (BoucEK. 1964, p. 81). The otherthree occurrences have all been compar·
ed with the Northern Shan forms (REED,
1936; BROWK et al.. 1953; SUK and
SzETU. 19,17) and it therefore seems
probable that these are Nowakia cancel·
lata also, or a closely related species.
Additionally. BoucEK has reported aJ\liddle Devonian Nowakia from tvlalaya
as well as the common Lower Devonian
Nowakia acuaria.
In !vlalaya, Thailand and the Shan
States, the Nowakiids are accompaniedby smooth-shelled tentaculites, all ofwhich appear to correspond to Styliolina.rissurella HALL. So far as the writer isaware. this form has not yet been foundin China.
Palaeogeography
The Mahang Formation. which con·tains the bulk of the Malayan graptolites
and tentaculites. is comprised to the extent of more than 90% of carbonaceous.
more or less siliceous. argillites and isconsidered to have been generated in abarred or restricted basin of deposition.
East of the basin facies. in the contem·
poraneous .. Baling Formation " (orgroup). similar black argillites are repeatedly intercalated with limestone.
apparently expressing intermittantly
shallower and better-aerated conditions
on the flank of a mobile geanticline.
To the northwest. the Ordovician-Silu·
rian "Setul Formation " of the Langkawi
Islands consists of limestone with only
two thin bands of shale (JONES. 1961 ).
This rock unit oyerlies coarse arenites,
is affected by earth movements to only
a limited degree compared with thebasin and appears to represent a shelf

40

C. K. BURTON

facies (BuHTON, in the press. b).
The anomalous admixture of Silurian
graptolites and Devonian tentaculites in~1alaya is ascribed to temporarr isola·tion of the depositional zone and very
slow sedimentation, or even non-deposi·tion. together with orogenic disturbancewhen external contacts were reestablished. It seems that the initial geosynclinal
dowmvarp (?Ordovician) in northwest
l\lalaya was compensated by a geanticlinal
upwarp to eastward which. as it rose.
came to restrict the natural circulationof the seawater. This promoted anaerobic conditions at depth and the generation of black shales, mainly in the\1ahang basin, but at times on the shelfand geanticlinal flank too. Life wasthus confined to the surface waters andthere flourished here. in the Lower Silurian. a graptolitic planklon which probably originated in the adjacent Palaeozoic Ocean, just as RuEDEiiiA);N (193·'1. p.
63) has proposed in North America.
In the northwest l'vlalayan region l'vliddle Silurian graptolites seem to be rather
restricted in number and in Upper Silurian times pelagic plankton \vas apparently entirely excluded from the areaby the emergence of the geanticlinal
barrier above sea-level. Communication
with the ocean is thought to have beensubsequently restored by the collapse of
the geanticline in a chain of islands inthe Lower Devonian, whereupon a tentaculite plankton invaded the northw-est!\lalayan area. Associated earth movements would have agitated both thesediments and the waters in the depositional zone.
Disturbed toxic bottom
water would then have stilled the tentaculites whose shells would have sunk tothe bottom in large numbers to join aminority of displaced graptolite (andtrilobite) remains dating from 20 to 30
million years earlier. This process ofannihilation and faunal mixing was probably repeated several times in theLower to :\Iiddle Devonian.
The anomalous faunal associations inThailand, Burma and China all lie on asimilar strike to those of i\lalaya. allspan an apparent hiatus at a similar
time and all involve similar faunas. both
before and after the hiatus. It does notseem unreasonable, therefore. to propose
the same explanation for all the midPalaeozoic mixed faunas in the geosynclinal tract from Malaya to '{unnan.
The emergence of the geanticline.
which is of critical importance to ourthesis, could have been accomplished byabsolute marine regression. said to havebeen widespread in the Wenlock (PASCOE,
1959, p. 658). However, since the period
of isolation seems to have begun earlier
in the south than in the north. orogenic
uplift is perhaps indicated. KOOP:\.IA:-.s
il965} has postulated a late Silurian to
Devonian " Langkawi folding phase··in northwest tvlalaya, and it is conceivable that these moyements upraised thebarrier. Alternatively, the rise of thegeanticline may be a normal feature of(ortho) geosynclinal evolution. as impliedby ]A\IES (1954. p. 279) and PETTUOII);.
(1957. p. 626, 637). and effected by slow,
progressive uplift. The "Langkawi folding phase" might then mark the subsequent breakdown of the geanticlinal
ridge.
Although Silurian to Devonian rocks
are known at intervals in the Yunnan~vlalaya geosynclinal tract. owing to thesparsity of information. it is uncertain
whether there were several distinct midPalaeozoic basins. or whether a continuous trough occupied the wholestretch from north\vest 1\lalaya to southwest China.
The Mahang Formation of Malaya isof euxinic facies and the rocks at Fang

:118.

(,'raptohtes and Tentaculites 1n the 1·11111W11-Malaya Geo8yncli'lte

m northwest Thailand are almost inentical in lithology. In the I Iuronian of}dichigan. U.S.A .. jA~lES (}9;).ol. p. 280i
has suggested that restricted (euxinic)basins may have been about 500 miles
long by 100 miles wide. On the other
hand, the Mahang Formation has an almost wholly planktonic fauna rBURTOl'\.
in the press, b) and corresponds to what
RuEDD!A:-;'\ l1934. 1935) has called trueor pure graptolitic shale, which in eastern North America is distributed
throughout the 1800 miles length of asingle trough.
The writer has recently had the opportunity of visiting the Fang area. andwas impressed by the very close similarity of the geology here to that ofnorthwest Malaya. The black. siliceous.
graptolitic shale of Fang duplicates the~ilahang Formation and is associated inplace with pale gray shales and greywackes indistinguishable from the Middle Devonian to Lower Carboniferous"Kampong Sena Formation" which succeeds the ~vlahang in the type area. In
both Thailand and Malaya this succession is followed by massive, white. Permian limestone. That three consecutive
rock units should maintain their character and mutual relationships in theset\VO areas. 1000 miles apart, is perhaps
best explained by postulating a single
elongate and persistent basin of deposition.
Possibly then, there was a continuous
trough from northwest .Malaya to west
Yunnan. at least at times of marinetransgression. When- external contacts
were interrupted, this geosynclinal belt
may ha\·e broken down into a numberof sub-basins, each with a slightly different history (witness the limited development of Ludlovian in west '{unnan).
It has been established that a basin
existed in the Silurian and Devonian in41

the northwestern coastal lowlands of!vlalaya with, to the west, a shelf or
platform (possibly marginal to the Gondwana continent) and a geanticline to theeast I see Fig. l '·Ban Na in south Thailand exhibits an
Ordovician-Silurian succession, ,-ery likethat of Langka\\·i. 170 miles to the south.
It appears likely that the shelf lay acrossthe peninsula in this latitude .c.9' nonh 1
whilst the contemporary basin was sitednear or within the present Gulf of Thailand (Fig. 1). The basin facies re<~ppears
at Fang in northwest Thailand.
In the Shan States the Llandovery
often comprises black shale. but thedominance of limestones and arenites in
the preceding and succeeding strata.
together with their situation to the westof the l'vlahang-Fang (basin1 axis. indi·cates that these areas were mostly near
the shelf. This accords with the Yiewof LA ToucHE (1913. p. 347l who be·lieved that the Palaeozoic rocks of ~orthShan were laid down along the eastern
shore of Gondwanaland. Apparently theeuxinic basin facies encroached westwards onto the continental shelf in
Llandovery times. The rocks at the )Ia
Suan locality in central west Thailand
have been likened to those of the contemporary Zebingyi Stage of Burma·'BRow:-: et a/., 1953. p. 331 and presumably reflect similar shelf-like conditions.
West Yunnan is situated close to the:\tahang-Fang axis. but its mid-Palaeozoic succession is not that of a typicaleuxinic basin facies. Black shale isagain present in the Llandovery, buthere it is admixed with sandstone andlimestone.
It seems likely that thecharacter of the Yunnan-:\lalaya geosyncline is somewhat different in this area.
Whilst throughout l'vlalaya and Thailand
it constitutes an orthogeosyncline. thesuccession discussed aboye occupying

42

C. K. BURTON

the miogeosynclinal zone, in west Yunnan MISCH (1945. p. 4!-s) has classified it
as a parageosyncline (intracratonic) and
SuN (1945. p. 61 has located its eastern
shore in this vicinity.
Similarly. although the mid-Palaeozoic
geosynclinal belt continues southwards
throughout !\lalaya. its history elsewhere
manifestly diverges from that indicatedin the northwest. South of the l'vlahangbasin. around Sungei Siput and I poh incentral Perak, the succession from Upper
Carboniferous is mainly limestone, withsubsidiary shale (in the ratio 4: 1 according to lNGilAM and BRADFORD, 1960). It
appears that this area subsided more
slowly and/or a geanticlinal barrier was
not well-developed here. At some stage
in the Upper Ordovician to Lower Silurian, however. a euxinic environment
temporarily obtained. when the graptolitic shales of Kanthan and Chemor wereformed. Oe\'Onian conodonts are reported in central Perak. but no fossil material of ~diddle to Upper Silurian datehas been found and it is therefore conceivable that this area experienced theperiod of isolation recognised to thenorth. Near Kuala Lumpur in the stateof Selangor. this interval is spanned bylimestone with Jvliddle to Upper Silurian
corals (TJIO:.JAS. 1963) and Ludlow brachiopods iBoucoT. ]Oil)\SO:x and ]mms.
1966). The limestone does not persist
southwards from south Selangor, but
associated clastics and chert extend to
the sea coast in l'vlalacca state.
The foregoing areas all lie on thewestern side of the contemporary geanticline. The l'vlalacca outcrop, howe\·er, is physically continuous with theFoothills Formation (RICHARDSON, 19,16)
on the eastern Hank of this feature(whose site is now occupied by the Main
Range granite batholith). A recent discovery of monograptids from the Foot-hills Formation, confirms its inferred
mid-Palaeozoic date. This formation,with its included ultrabasic bodies andsituation to sea\vard of the former geanticline (island arc) seems to represent
deposition in a deep marginal trough or
geotectocline (I-lESS. 1938. p. 79).
Further graptolite and tentaculite
correlations beyond the Yunnanl\lalaya geosyncline

A mid-Palaeozoic geosynclinal tract
has now been traced for some 1600 miles
from Yunnan to southern Malaya. It is
possible that further extensions exist.
In the north, SU)I; (19·16, p. 6) andPASCOE (1959, p. 658) believed that theNorth Shan-Yunnan sector was connected with the Himalayan geosyncline in
Silurian times. On the other hand. aslong ago as 1913, LA TOUCHE (p. 349-50)
had pointed out ...... the marked discrepancy that exists. until we arrive at the
Permo-Carboniferous epoch. between thefaunas of the Himalayas and of the
Shan States .... ·· and he had postulated
an ··unsurmountable barrier" between
the Shan and Himalayan areas.
In part, LA ToucHE's hypothesis rested on the apparent absence of graptolites from the whole of the Himalayan
tract.
Recent discoveries, however,necessitate a re-assessment. GuPTA has
found graptolites in the Kashmir Himalayas (SAHNI and GUPTA, 1964a, 1964b).
identified by Stubblefield as:Monograptus cf. vulgaris
1Honograptus cf. colonus
Monograptus cf. dubius

apparently indicative of a Lower Ludlow age. It will be recalled that Monograptus cf. vulgaris occurs in the Loilem
Stage of the Southern Shan States, whilst
Monograptus dubius is known from the.'518.

Graptol-ites and Tentaculites in the Ywnna.n-Malaya Geosyncline

Zebingyi Stage, Northern Shan and theUpper jenhochiao of west Yunnan.
Graptolites have now also been reported from the Himalaya of ~epa\.
SnACHAN et at. (1964) list:Climacograptus cf. medius
Orthograptus sp.
Dimorphograptus extenuatus
Glyptograptus sp.
Diplograptus s. str. sp.
.\/onograptus lobiferus
Monograptus aff. tenuis
Rastrites sp. (cf. hybridus)

This assemblage is clearly Llandovery
in age.
Whilst !Jimorphograptus ex·
tenuatus and Rastrites hybridus are notknown in the Yunnan-Malaya geosyn·
cline. the other three species identified
in Nepal. MonograjJ!us lobiferu.~. Mono·
graptus tenuis and Climacograptus medius
are all recorded from both Yunnan andSouth Shan and the two latter are also
found in North Shan (Table 2).
In the light of this new evidence it
appears that the proposed barrier be·
tween the Himalayan and Shan areas
was in fact surmounted, or more probably circunwented. in lower Silurian
and in tvliddle-Upper Silurian times.
Nevertheless. there remains a consider·able body of faunistic eYidence to sup·port LA ToucHE's thesis and probably
the connection between the two geosyn·
clinal zones was neither direct nor sus·
tained.
T'A\' (1937), in reconstructing
thepalaeogeography of west China shows.
in his plate ll·figure 2. the Silurian sea
as swinging northeastwards from north
Yunnan and expanding to cover muchof Szechuan, plus west llupei, southeast
Kansu, north Kueichow and south Shensi.
He does not give details of the litho·
facies and fauna. but graptolitic Fuchih
Shale of Llandovery age occurs at three
localities in Hupei according to SoN

4•J·:>(]931) and is also known in the Szechuan(StH\ and WAi\G, HH6. p. 92). YrN andl\lu (1945) have further described Lower
Silurian graptolites from the Tungtzu
area on the SzechuanjKueichow border.
:tvloreover. the ECAFE "Geological Map
of Asia and the Far East" (1959) port·rays a discontinuous belt of Silurian
rocks extending from west Yunnan
north-northeast to Kanting (Tatsienlul
and thence northeast wards towords Sian.
A northeastward extension of the
Yunnan-Malaya geosyncline thus seems
to be better established than a westward
connection with the Himalayan geosyn·
cline.
LA Tot5CIIE \1913. p. 3491 remarked
on the European afl1nities of the Palaeozoic fossils from the Shan States and inparticular he drew attention lp. 179) tothe Bohemian or Hercynian facies of the
Zebingyi fauna. lie inferred therefrom
some sort of contemporary communica·tion between Europe and Southeast Asia.
Similarly. whilst SUN and SZETU (19·17)
believed that the Palaeozoic faunas of
Yunnan were essentially of oriental
origin. they awr (p. 12) that " .... connection with Europe is quite certain due
to the occurrence of cosmopolitan gra·
ptolites ''.
It is noteworthy, therefore. that GA\'S·
SER's map of the Himalayan region (196-1.
plate 1-bl depicts two arms of Palaeozoic strata leading westwards fromsouthern China to Fcrghana, one via the
Kun Lun Shan and the other by way of
the Tsingling Shan, the Nan Shan andthe Tien Shan. MUIR- WooD 11948. p. 19)
considers that the latter. rather thanthe Himalayan geosyncline. seryed as aconnection between Europe and r.;lalaya
in Visean time and BULMAN's (196,1. p.
4731 distribution map of :\lonograptus
turriculatus suggests a similar routefrom Europe to Yunnan in the Llando·

4-1

C. 1\. BURTON

Yery.
At its southern end the ·yunnan:Vlalaya geosynclinal tract passes beneaththe Straits of ~Ialacca and is therefore
difficult to trace farther. In a discussionof structural belts in the East Indies,
WESTERVELn 11952! assigned peninsularThailand and ~Ialaya to the ·· :"Aalaya
Orogen " which stretches southwards to
Singkep and Bangka. \Vhence it bends
east-northeast through Belitung 1Bi!!iton)
to continue into west and central Kalimantan (Indonesian Borneo). Whilst no
pre-Carboniferous rocks have been foundin the Riau and Lingga Archipelagoes!Fig. 1) or in the "tin islands", the disco\·ery of the Lower Devonian Clathro·
dicton and Heliolites in central Kalimantan (VAN BE:\L\IELEN. 1949. p. 3661 maymean that the mid-Palaeozoic geosyncline extended throughout the length ofthe " i\lalaya Orogen ...
Some 1200 miles farther east. Silurian
rocks are known at the western end of
Irian Barat (Indonesian New Guinea)\Vhere ButMAl\ (1964. p. 473) has indicated an occurrence of Monograptus iurriculatus.
These tenuous correlations to southand east of :vlalaya are enhanced byevidence from the Tasman geosynclineof eastern Australia.
Association ofgraptolites with tentaculites. a distinctive and characteristic feature of themid-Palaeozoic in the Yunnan-Malaya
geosyncline. recurs in Victoria where
SKEATS (1928. p. 229) reported the concurrence of Monograptus and Styliola.
GILL (19-11) later showed that this ··Sly·/iota ·· is apparently to be referred to
Slyliolina fissure/In and is frequently
accompanied by ·· Tentaculites matlocki('11Sis ". The l::1tter seems to be. in fact.
Nozmkia acuaria 1Bol:cr:K. 19641 andhence the Victorian tentaculites correspond to the t\VO most common forms

in i\talaya.
The Monograptus found with tentaculites in Victoria has not been specifically determined. but Monograptus dubius
occurs close by (SKEATS, 1928.1 and thesame stratigraphic unit. the l\lelbournian.
contains Jlfonograplus romerillll-' iGILL,
19·ll. p. 159).
Monograptus dubius is
known from the mixed fauna of theNorthern Shan States and is also re·ported in west Yunnan (and Kashmir).
Monograptus vomerinus similarly participates in the graptolite-tentaculite admixture in the Southern Shan States
and Yunnan. It is evident that thegraptolite member of the Australianfaunal association is also similar incharacter to that of the Yunnan- ~lalaya
geosyncline.
These graptolite and tenlacu!ite correlations engender the suggestion that
the Yunnan-!vlalayan and the Tasman
geosynclines were formerly contluent.
Their present separation is perhaps
largely a result of continental drift,
particularly the oft-postulated eastward
migration of Australia.

Acnowledgements
The author wishes to express here his
gratitute to Professor Bedlich RoucEKof the Czechoslovak Academy of Sciences
who has examined the .\lalayan tentaculites and given us permission to quote
his findings. Acknowledgement is also
due to Mr. C. R. jo:sES who has informed us of his preliminary determinationsof the Malayan graptolites.
We would further like to take thisopportunity to thank l'vlr. \Vattanachai
BooNYAKJART and his colleagues in theThai Department of r..lineral Resources
who conducted us to the important Fang
locality in northwest Thailand.

518.

Graptoli.tes andTentoculite.~ in

Dr. K CHI:\ZEI verr kindly prepared
the Japanese abstract of this article.
References
BDI>Il·:LE::-;. R. \V. van (19·19) : The Geology
of Indonesia, Volume lA, General Geology
of Indonesia and Adjacent Archipelagoe~:
The Hague, Martinus Nijhoff. i32 p., 3i8
figs.
Bm.:cEI;. B. (1964) : The Tentaculites ofBohemia: Their Morphology, Taxonomy,
Phylogeny and Biostratigraphy: Prague.
PuMislzing House of Czech Academy of
Sciences. 215 p., 40 pl.. 36 figs.
Bm·coT, A.] .. .]OIIl\'so:-~,]. G. and Jo:x"s, C. R.
(l966): Silurian Brachiopods from Malaya: jour. Palaeontology, 1·ol. 40. p. 102731.

BR0\1·;-.;, J. C. (1913): Contributions to the
Geology of the Province of Yunnan inWestern China. Ill. Notes on the Stratigraphy of the Ordodcian and Silurian
Beds of \Vestern Yunnan : Rec. Geol.
Surr·. India. vol. ·l:l. p. 327-34.
BRow:-;,]. C. and So:-;DIII, V. P. (1933a): Geological Reconnaissance in the Southern
Shan States: Ibid .. Vol. 67, p. 134-65(1934).
and - - (1933b) : The Geology of theCountry bctween Kalaw and Taunggyi,
Southern Shan States: Ibid .. vol. 6i. p.
166-248 (1934).
BRO\\X G. F. et a/. (1953): Geologic Reconnaissance of the :Mineral Deposits ofThailand: Ceo/. Suru. Mem. 1. Ba11gkok.
Royal Dept. Mines, 183 p., 38 figs., 20 pl.
lkL,tA::-;, 0. ~1. B. (1964): Lower Palaeozoic
Plankton: Ceo/. Soc. London Quart. jour ..
vol. 120, p. -155-76.
Ht:RTO:", C.K. (in press. a): Dacryoconarid
Tentaculites from the Euxinic Facies ofthe Malayan Geosyncline. jour. Paleoutology.
- - (in the press. b). The :Vlahang Forma.
tion : A Mid-Palaeozoic Euxinic Facies
from .\lalaya. with !\otes on its Conditionsof Deposition and Palaeogeogt·aphy. Geologie en J!ijnbouu·.
EC.\FE (1959): Geological ~lap of Asia andthf' Yunnan-Jfalaya. Geo.<;yndine

45

the Far East. 1: 5,000.000: Bangkok.
EC:IFE. United Naliolls Secretarial.
FISHER. D. W. (1962): Small Conoidal Shellsof Uncertain Affinities: in Treatise on
Invertebrate Palaeontology-Dir. & Ed.
R. C. MooRE. Part W. p. 98-1-13. Ceo/.
Soc. Am. and Univ. of Kansas Press.
G.\N'ssER. A. (196·1): Geology of the Himalayas: ['w"ew l'ork. ]. Wiley, 289 p .. 4 pl.
GILL. E. D. {19-11) : The Place of the Genus
Styliolina in the Palaeozoic Palaeontology
and Stratigraphy of Victoria: Proc. Roy.
Soc. Victoria, \"OI. 53. N. S .. p. 145-16,1.
HEss. H. H. (1938) : Gravity Anomalies andIsland Arc Structure with Particular Reference to the West Indies: ;lm. Phil.
Soc .. Proc .. YOI. 79, p. 71-96.
1:--;<~H ..UI. F. T. and BRADFORD. E. F. (1960) :The Geology and l\·1ineral Resources of
the Kinta Valley, Perak: Fed. of Malaya
Ceo/. Sun·ey. :\!em. No. 8: Kuala Lum·pur. G01•t. Press, 347 p .. 20 figs., 18 pl..:!
maps.
].\~IES. H. L. (195·1): Sedimentary Facies of[ron-Formation: Econ. Ceo/., ,·ol. ·19. p.
236-93.
Jo:-.-Es, C. R (1959) : Graptolites Recorded
from Malaya: Natu1·e. vol. 183, p. 232 only.
- - (1961): A Re\·ision of· the Stratigraphical Sequence of the Langkawi Islands.
Federal ion of Malaya: 9th Pacific Sci.
Congr., 1957, Proc .. vol. 12. p. 287-300.
KoBAYASHI. T. (1960): ~otes on the Geologic History of Thailand and AdjacentTerritories: japan. jour. Geol. Geogr.
vol. 31. p. 129-··18.
- - (1964): Geology of Thailand: Geology
and Palaeontology of Southeast Asia, Vol.
l : Tokyo, Uni\', of Tokyo Pre5s, p. 1-15.
- - , jo::-;Es, C. R. and IL\~IADA. T. (1964a) :On the Lower Silurian Shelly Fauna in
the Langkawi lslands.!\orthwest Malaya:japan. Jour. Ceo/. Geogr .. vol. 35, p.,i5-80.
- - et a/. (1964b): Report on the Stratigraphical and Palaeontological Reconnais~ance in Thailand and lVIalaysia. 19631964: Tokyo. Ove1·seas Technical Co·
operatioll Agency. 72 p., 10 figs.
Kooi''IA:-:5, B.:;\. (Hl65) : Structural E\·idence
for the Pre:>ence of a Palaeozoic Orogeny

C. K. BURTON
in North West Malaya: Ceol. Mag., vol.
102, p. 501-20.
LA ToucHE. T. II. D. (1913) : Geology of theNorthern Shan States: A/em. Ceol. Sun•.
India. vol. 39, 379 p .. 27 pl.. 3 coloured
maps.
~I1scH, P. (1945): Remarks on the Tectonic
History of Yunnan with Special Reference
to its Relations to the Type of the Young
Orogenic Deformation: Ceol. Soc. China,
Dull.. vol. 25, p. 47-15•1 (1946).
~IUIR-Wooo, H. ~I. (1948): Malayan Lower
Carboniferous Fossils and their Bearing
on the Visean Palaeogeography of Asia:
British Museum, 118 p .. 3 figs .. 17 pl.
PAscoE. Sir E. II. (1959) : A Manual of theGeology of India and Burma. Vol. 2(1960): Calcutta, Covt. of India Press. p.
485-1344.
PETTIJOH:-<. F. j. (1957): Sedimentary Rocks(2nd Ed.): New York. Harper Bros .. 718
p., 173 figs .. 119 tables.
REED, F. R. C. (1906) : The Lower Palaeozoic
Fossils of the Northern Shan States.
Burma: Mem. Ceo/. Surv. India. Pal. Indica. N. S. vol. 2, Mem. No. 3, 154 p., 8 pl.
- - (1915) : Supplementary 1\•lcmoir on );few
Ordovician and Silurian Fossils from theNorthern Shan States: Ibid., vol. 6, Mern.
No. l. 123p., 12 pl.
- - (1917) : Ordovician and Silurian Fossils
from Yunnan: Ibid., vol. 6, l\lem. No. 3.
85 p .. 8 pl.
- - (1932) : Notes of some Lower Palaeozoic Fossils from the Southern Shan
States: Rec. Ceo/. Sun•. India, vol. 66. p.
181-211 (1933).
- - (1936) : The Lower Palaeozoic Fossilsof the Southern Shan States: .\!em. Ceo/.
Sun•. India. Pal. l11dica, N. S. vol. 21,
Mem. No. 3, 130 p .. 18 pl.
l~ICHARoso:-.;, j. A. (1946): The Stratigraphy
and Structure of the Main Range Foot·hills. F. M.S.: Ceo/. Mag., vol. 83, p. 217-29.
RuEDE'ooiANJ'\, R. (193,1): Palaeozoic Plankton
of !\orth America: Ceo/. Soc. America.
.\/em. No. 2, 1<11 p .. 6 figs .. 26 pl.
- - (1935) : Ecology of Black Mud Shalesof Eastern New York: ]our. Palaeont.,
vol. 9, p. 79-91.
SAHJ'\1, M. R. and Gt:PTA. V. ]. (1964a) : Gra.

ptolites on the Indian Sub-Continent:
Nature. vol. 201, p. 385-6.
- - and - - (1964b) : Graptolites from the
Kashmir Himalayas, also a Xote on the
Discovary of Fossils in the Muth Quart.
zite: Nature, vol. 204, p. 1081-2.
SKEATS. E. W. (1928): Stratigraphical and
Structural Relations of Silurian Rocks ofWalhalla-Woods Point District. Victoria,
in Relation to the "Tanji\ian" Series:
Rep. of the Hobart Meeting, 1928. Aust·
ralasian Assoc. for Adv. of Sci., p. 219-30.
STRACHAN. 1.. BoDENHAUsEN, ]. '\V. A.,
BooY. T. and EGELER, C. G. (1964) : Graptolites in the "Tibetan zone" of the
Nepalese Himalayas: Ceo/. en Mijnb.,
vol. 43. p. 380-82.
SuN. Y. C. (1931): Graptolite-bearing Strata
of China: Ceo/. Soc. Chirw, Bull., vol. 10,
p. 291-99.
- - (Hl,l5) : The Sino-Burmese Geosynclineof Early Palaeozoic Time with Special
Reference to its Extent and Character:
Ibid., vol. 25, p. 1-8 (1946).
SL·:-.;, Y. C. and SzETt:. S. S. (1947): Prelimin·
ary Notes on the Stratigraphy and Structure of the Paoshan Region, ",.· Yunnan:
Contr. Ceo/. Ins/., Nat. Uni~·. Peking, No.
32, 26 p., 7 figs., maps, sections.
SDN. Y. C. and WANG, H. C. (1946): Silurian
Stratigraphy of the Malung and Kutsing
Districts, Eastern Yunnan: Ceo/. Soc.
China. I1ul/., \'Of. 26, p. 83-99.
T'AX, H. C. (1937): A Summary of the Geo.
logic History of Szechuan and Sikang:
Ibid., Bull.. vol. 16, p. 389-.U6.
T11o~IAS. H. D. (1963) : Silurian Corals from
Selangor, Federation of Malaya: Overseas
Geology and .\fin. Resc., vol. 9, p. 39-46.
W ESTEKVEI.D, ] . (1952) : Phases of Moun.
tain Building and Mineral Pro\·inces inthe East Indies: Internal. Ceo/. Congr.,
18th, Ct. Britain, 19·18. Proc. Section M.
p. 245-55.
Yll'\, T. ll. and Lu. C. H. (1937): On theOrdovician and Silurian of Shihtien,'Vestern Yunnan: Ceo!. Soc. China, Bull.,vol. 16. p. 41-56.
YIN, T. H. and Mu. A. T. (1945) : Lower
Silurian Graptolites from Tungtzu: Ibid.,
vol. 25, p. 211-20 (1946).

o"47
PROCEEDINGS OF THE PALAEONTOLOGICAL SOCIETY
OF JAPAN

A:$:i!l±1iJJ¥~~ 95 [<i]f>'J~;i, 1966 ~ 11 FJ 26

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.. .. · ...... · · ........... JlfrEBI'!H!'!I: · Jll111~i!XSpecies and subspecies concept in paleonto.
logy .................... Takayasu UcHJO~"-'~~:ff · fl§!A~~iiitt.J:ib I), ~~f!I::~T Lt:,

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.................................. ~111*1!!1>
On the genus Pseudofusulinella, with de·scription of a new species from Japan ..
. . . . . . . .. . . . . . . . . . . .. . . . . . Tomoo OzAwA
Fusulinids of the Millerella zone of the
Taishaku Limestone. (Studies of thestratigraphy and the microfossil faunasof the Carboniferous and Permian Taishaku Limestone in West japan, No. 1)(f-\::AA:) .................... Kimiyoshi SADA
Fusulinids of the Projusulinella zone of the
Taishaku Limestone. (Ditto, No. 2) (f\::ihc) ...................... Kimiyoshi SADA
Fusulinids of the Fusulinella zone of the
Taishaku Limestone. (Ditto, No. 3) (ft~) ...................... Kimiyoshi SADA............ ' .................... ' ·f'l·;;f:if!!lg
On the Triassic Myophoriidae and Trigoni·
idae in the Asio-Pacific at·ea ......... .
. . Teiichi KoBAYASHI & Minoru TAMURA
Claraia from North Pahang. Malaya ..... .
. . . . . . . . . . . . . . . . . . . . . . . . Minoru TAl\IURA
Some lower Cretaceous biv;tlvcs from the
Shimantogawa Group of South Shikoku. ..... Itaru JIAYANI & Kcizo KA\\'ASAWA
Paleoecology of shallow sea molluscan
faunae in the Neogene deposits of North·cast Honshu, Japan ................... .
.. Kiyotaka CHINZEI & Yasuhide IwASAKI
Dosinia tatunokutiensis No~IL'R,\ ':-.J•, ·"( ..
................................ J:l~[I!#;-~;
Fulgoraria Xfi(l)ifllfl: ........ · · ...... f,lj!F.flPJf~
Carboniferous ammonoids from Akiyoshi.
(Molluscan paleontology of the Akiyoshi
Limestone Group. Pt. 3) ........ Tamio
NISHIDA, l\lasamichi 0TA & K. HASHIMOTO
Occurrence of Metoicoceras in Trichinopoly
Cretaceous ........................... .
M. V. A. SASTRY & Tatsuro iVIATSUl\IOTO
Lower Cretaceous ammonites from the
Miyako Group. Pt. 2: Some Silesitids

48
from the .Miyako Group .... Ikuwo 0BAT.\
Graptolite and Tentaculite correlations andpaleogeography of the Silurian and
Devonian in the Yunnan-C\lalaya Geosyncline (ftroV ............ C. K. BVRTO:"
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Pleistocene monkey and human remains
from Ojikado Cave of Hiraodai Karst
Plateau. northern Kyushu ............. .
. .. . . .. . . .. . . .. .. .. . Yoshikazu HASEGAWA
On two new species of Cervidae from theKuchinotsu Group of West 1a pan ..... .

0........................ Hiroyuki 0Tsl'KA
Ordo\·ician and Silurian Conodonts from
Langkawi. Malaya. (supplement) ...... .
.......... Hisayoshi IGo & Toshio KOIKE
Carboniferous Conodonts from Kuantau,
Malaya .. Hisayoshi !Go & Toshio KoiKE

I:F.~.!:HII~Hflt:lll:i:..l-=515~!i:O)~~-t0)-~IJ....

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............................ Kazuo AsA:O.JA

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