a -lt"~i.~~~•t·ic.iJ
Transactions and Proceedingsof thePalaeontological Society of Japan
New Series

No. 61

Palaeontological Society of japan
April 20th, 1966

CONTENTS
TRANSACTIONS
Page

500.

A new species of a whale tympanic bone from Taiwan, China ........... .
. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . Tunyow HUANG 183

501.

On the genus Tilia from the !Voodwardia zone of Hokkaido, with descrip·

502.

Shell structure503.

Notes on Ammonites bourgeoisi o'ORBIGNY from the upper Cretaceous oftion of two new species .................................... Seido ENDO 188
of japanese smaller foraminifera Part 2.

Pararotalia

nipponica (ASANO, 1936) ................................... Hiroshi UJIIE 191
France ............................................ Tatsuro lVIATSUMOTO 201

50-1. The significance of the magnesium and calcium ratios of fossil shells ofUmbonium costatum (KIENER) from the deposits since the Pliocene in
the southern Kanto region, japan ...................... Joji NAGASAWA 207
Proceedings of the Palaeontological Society of japan .......................... 214

President:

Kiyoshi ASANO

Councillors:

Kiyoshi AsA~o (Editor of " Fossils"). Haruyoshi Fun~IOTO, Tetsuro

HANAI (Editor of Transactions and Proceedings), \Vataru HASHIMOTO (Treasurer), Kotora liATAI, lchiro HA"iASAKA, Koichiro ICHIKAWA, Taro KANAYA,
Teiichi KOBAYASHI, Tatsuro rviATSUI\IOTO (Editor for Special Papers). l'vlasao
1VIINATO, Hiroshi OZAKI (Planning), Tokio SHIKAI\IA (l'vlembership), Fuyuji
TAKA! (Chairman of Executive Councillors' Committee), Ryuzo TORIYAMA
Secretaries: Takashi HA:'IIAOA, Hisayoshi IGo, Yokichi TAKAYANAGIAssistant Secretary:

Takeo ICIIIKAWA

All Communicalions relating to this journal should be addressed to the
PALAEONTOLOGICAL SOCIETY OF JAPAN
Geological Institute, Faculty of Science, University of Tokyo, japan

Trans. Proc. Palaeont. Soc. Japan, N. S., No. 61, pp. 183-187, pl. 22, April 10, 1965

500.

A NEW SPECIES OF A WHALE TYMPANIC BONE
FRO.M TAIWAN. CHINA*TUNYOW HUANG**
Institute of Geology and Paleontologr Faculty of Science,
Tohoku UniYersitr

Introductionof its increasing the value of such fossils in correlation of geographically isolated geological formations, interprcta·tion of the depositional environmentand other problems as once mentioned
by Kotora HATAI, et al. (1963).

As already summarized by lchiro(1942), mammalian fossils
are frequently found in the Toul<oshan
Foramation (Tokazan beds) of western
Taiwan and about 11 species have beenreported. However, fossil pelagic mammals (whale) have never been foundfrom the geologic column of Taiwan.
Therefore, the find of fossil tympanies
is worthy of record.
In the summer of 1961. a tympanic
bone \vas collected by !\lr. Chao-Yi
MENG, Chief Geologist of the Chinese
Petroleum Corporation and Mr. Yu-Lai
FAN, Geological Assistant of the same
Corporation, in association with otherfossil bones, shark-teeth (Pl. 22, figs. 1022) ..Mollusca, Foraminifera, crab (Galene
granulifera Lil\), and miscellrneous plantremains from the lower part of the
Cholan (Takuran) Formation in the
Chutong Oil Field. near Hsinchu Citv.
The tympanic bone is well preserved.
and thus its taxonomic position can be
determined. The record of occurrenceof the tympanic is important because
IIA Y ASAKA

Acknow Jedgements

The writer thanl<s Professor Kotora
HATAI of the Institute of Geology andPaleontology, Faculty of Science. Tohoku
University for his kindness with regard
to this study and for reading the manuscript. lie also expresses his sincere
thanks to Mr. Chao· Yi !VI ENG, Chief
Geologist of the Chinese Petroleum Cor·
poration for the opportunity to study
the specimen and for the permition to
publish this paper. Thanks are due to
Mr. Kimiji KUl\IAGAI for his pho agraphic works.
Systematics
Order Cetacea
Family Balaenidae• Received June 20, 1965: read June 20.
1965 at Kanazawa.
•• Chinese Petroleum Corporation.

Genus Balaenoptera LACEPEDE, 1804
Based upon YAMADA's (1953) de~crip-

183

Tnnyow HUANG

184

tion and comparative mophology of the
tympanic bon~ of Balaenoj>lera physalus(LINNAEliS) (IGPS. Coli. Cat. No. 85968)
labelled as from the Antarctic Ocean,
and a gift from Miss Yoko SuZUKI, 1964,
the fossil one from Shantahu can bereferred to Balaenoptera without doubt.
Further, its size, proportions and a thedetails suggest its intimate relation with
the Recent species of Balaenoptera.
From comparative mophology withthe known species of the genus now
available to the writer, it is evident
that the present tympanic is so different
that it should be treated as a distinct
species and a new specific name is proposed to distinguish it from that of
Balaenoptera physalus (L~NAEUS).

~)
Balaenoptera taiwanica, new species0!.

Pl. 22, figs.

1~3

Type :-A single well preserved righttympanic bone, now deposited in Paleontolongical Laboratory, Geological Department, Chinese Petroleum Corporation. ~vliaoli, Taiwan.
Type locality:- The specimen was
found at Shantabu in the Chutung Oil
Field 3.6 kilometers south of Chutung·Chen, Hsinchu-Hsien, Taiwan !Fig. 1).
Horizon:- The specimen \Vas discovered and excavated by Yi·Lai FA!\,
geological assistant of lhe Chinese Pet·
roleum Corporation in the summer of
1961. It was dug out from a bluishgray mudstone bed situated at about
100 meters above the Chinshui (Kinsui)
Shale and making the small hill near
Shantahu in the Chutung Oil Field.
The lithology of the exposed formationsin the area are shown in Fig. 2. The
lower part of Cholan Formation is composed chiefly of beds of loose, yellowish
brown sandstone with bluish gray mud-soo<000 ...1{liYUAJNTUNGTZU •Fig. 1.

l: "••

Map showing the fossil locality(after ME"'G. 1961).

stone. The stratigraphic position of
the Cholan Formation is shown in Fig.
2. from which it may be noticed that itlies with conformity upon the Chinshui
Shale. On the basis of the fossil Foraminifera and Mollusca the age of the
Cholan Formation is early Pliocene.
Description of the tympanic:- The
tympanic bone (Pl. 22. figs. 1-3) was
found in association with many large
whalerib bones, marine molluscs, shark's

500.

Whale ty1npanic bone from Taiwan

sww~Jffjtf( iJ§ >'?;NEE~} CHOLAN

FORMATION

~

SHALE

@]
Fig. 2.

CHINSHUI

Geologicsection near the fossil locality (after ME~G. 1961).

teeth, crabs, and foraminifers. In thisrespect the occurrence of 13alaenoptera
taiwanica is quite similar to some of
the tympanic bones from the Tatsunokuchi Formotion (IIATAI. et a!.. 1963).

Measurements of the tympanic honeGreatest longth of bulla ........ 11.5 em
Greatest width of bulla ........ 7.8 em
Greatest thickness of bulla ...... 6.6 em
Distance from antero-internal endof tympanic to anterior end of
involucrum .................... 1.5 em
This right tympanic shows the formof the tympanic cavity which is boundedby the overarching outer lip, and thesize as given in the table and the direction of its anterior outlet or tympanic
aperture of the eustachian canal arequite characteristic.
Nemarks :-This specimen resembles
Balaenoptera physalus (LI~NAEUS) (Pl.
22, figs. "l-6) in the relative thickness ofthe convex and the concave portions of
the involucrum, in the outline of theeustachian end of the cavity. in theposition of the posterior conical apophysis, and in the general outlines of
the tympanic as a whole. However, thepresent one is distinguishable from thatspecies by that the shape is rather renal
and of courie-shall form with narrow
tympanic cavity. The thick convex

involuted portion of the tympanic. orinvolucrum, is unequally depressed on theoverarching outerlip (Pl. 22. fig. 3).
A narrow and gentle depression (Pl.
22. fig. 1) extend a long the columella
from the anterior part to the posterior
portion and near the inner lip.
The dorsal surface of the involucrum
is almost smooth an gently convex (Pl.
22, fig. 2), and maintains more uniform
breadth from the anterior to the posterior end (Pl. 22, fig. 1).
The surface of the middle part of theinner lip is gently concave and withmany very weak grooves, all coverging
towards the cavity.
The anterior process of the righttympanic, which unites with the periotic,
is broken at the level of the outer lip.
The anterior portion shows abruptly
the limbation of the superior face. The
next furrow is a distinct deep groove
between the processus sigoideus and theso-called posterior conical apophysis.
The posterior conical apophysis is not
so well developed as in Ba/aenoptera
plzysa/us (LIK::>:AEUS) but is roundedslightly above the superior face of theinvolucrum.
The posterior part projects mainly
from the involucrum, although the outerlip posterior to the conical apophysis
contributes to the thin edged outermargin.
The tympanic cavity is continued

186

Tunyow HUASG

forward to the anterior end of that bone
and the outlet is relatively narrower
than in Balaenoptera physalus (LIN1'\AEUS).

Although the specimen is similar to
the ear bone of Balaenoptera physalus(LI~:\AEUS). figured and described by
YAMADA (1953) and with the Recent
specimen from the Antarctic Ocean(IGPS, CoiL Cat. No. 85968), the present
one differs from that species in theabrupt limbation and distinct deep furrow on the superior surface of the involucrum, gen tie de presion and very
weak· grooves on the middle part of theinner lip. and narrow tympanic cavity.
As KELLOGG (1924) said. the charactersderivable from the tympanic bone aresufficiently diagnostic to be used as a
guide in the determination of species.
The peculiar features of the tympanic
described above are sufficiently marked
to justify its being named as distinct
species.
References Cited
AGASSIZ, Louis (1833-•13) :Recherches sur

Jes Poissons Fossiles. Tome III. Neuchatel, en Suisse.
HATAI, K., HAYASAKA, S. and MASUDA, K.
(1963) : Some Fossil Tympanies from
the Mizuho Period of Northern Japan.
Saito Ilo-on Kai Mus .. Res. Bull .. No. 32,
p. 5-17, pis. 1-2. table 1.
HAYASAKA. Ichiro (1942): On the Occurrence of Mammalian Remains in Taiwan.
A Preliminary Summary. Taiwan Tigaku
Kizi, vol. 13. no. 4. p. 55-109. pls. V-VIL
Hu.-\:\G. Tunyow (1960). Preliminary Noteon the Microfaunas from the Paohsan
Area. Southeast of Hsinchu. (Unpublished
Report. Oct 1960, CPC file. in Chinese).
IcHIKAWA. Y. (1931) : Explanatory Text of
the Geological Map of Taiwan. Tikuto
Sheet: Bureau of Productive Industries,
Goverment-General of Taiwan, Pub. No.
582 (in Japanese)_bHIWARA, Y. (1921): On Some Fossil SharkTeeth from the Neogene of Jnpan. Tohoku Imp. Univ .. Sci. Rep .. ser. 2, Geology,
Vol. 5 ..1\lo. 3. p. 61-74. pls. 10-12.
KELLOGG. R. (1924) : Description of A New
Genus and Species of Whalebone ·whalefrom the Calvert Clifs. Maryland. U.S.
Nat. Mus .. Proc .. Vol. 63, Art. 15, No.
2483. p. 1-14. pls. 1-6.
MENG, C. Y. (1961) : The Well Preserved
Fossil Bones First Discovered from Tai-

Explanation of Plate 22
Figs. 1-3. Right side of the tympanic bone of Balaenoptera taiwanica. new species, Holotype,x2f3, from Shantahu. Chutung-Chen, Hsinchu-1-Isien. Taiwan. I, Superiorvew. notice
the longitudinal groove: 2. External view, notice the abrupt limbation at the anterior
portion. deep groove and the so-called posterior conical apophysis: 3. Interior view,notice the narrow tympanic cavity.
Figs. 4-6. Left side of the tympanic-periotic bone of Balaeuoptera Physalus (LIN:-;AEt:S) _IGPS, Coli. Cat. No. 85968. x 2/3. from Antarctic Ocean. Recent.
Figs. 7-9. Digit bone probably of Balaenoptera taiu,anica. new species, x 1/2. from same locality as holotype.
Figs. 10-11. Galeocerdo aduncus AGASSIZ. (lower lateral teeth). x 1. from same locality as
holotype. 10, Anterior view: 11, Posterior view.
Figs. 12-14. lsurus hastalis (AGASSIZ). (lower lateral tooth). x 1. from same locality as holotyye. 12. Anterior view: 13. Side view: 14. Posterior view.
Figs. 15-22. Carcharhinus gangeticus (l\hiLLER and HE:-:LE). x 1. from same local it~' as bolotype. 16, 18. 20, 21. Anterior views: 15. 17. 19. 22. Posterior views.

H u A NG :K uMAGA I

Whale tympanic bone from Taiwan

pho ta .

Plate 22

500.

Whale tympanic bone from Taiwan

wan. Shih Yu Tu11g Hsin, No. 220. p.
2-4. figs. 1-7, (in Chinese).
NAKAMUR;\, M. (1937) : On the Fossil Foraminifera from the Byoritu Beds in the
Northern Oil Fields of Taiwan. Geol.
Soc. japall, jour., \lol . .J4, No. 526, p.
672-685 (in japanese).
ToRII, K. and YosHIDA, H. (1931) : Report

Chihshui Shale
Jlil*-J'l~
Cholan Formation .!ji.rii.Jt!'i
Chutung-Chen'lt-*:J\

187

of the Geological Survey of the Byoritu
and Tikuto Oil Fiel<l~; Bureau of Productive Industries, Goverment-Generalof Taiwan, fub. No. 585 (in japanese).
Y.-\:.tAD.-\. M. (1953): Contribution to theAnatomy of the Organ of Hearing ofWhales. Whales Res. Insl.. Sci. Rep., No.
8, p. 1-/9, 29 text-figs.

Hsinchu-Hsien.ii'ITM
Shantahu
J:.j,;tlij
Toukoahan Formation ifJt~h.IJ.Jf'l

Trans. Proc. Palaeont. Soc. Japan, N. S., 6l, pp. 188-190. pl. 23, April 10, 1966

501.

ON THE GENUS TILIA FROI\1 THE WOODWARDJAZONE OF HOKKAIDO. WITH DESCRIPTION OF
T\\10 NEW SPECIES~SEIDO ENDO

Tilia jji!C I!, .!Jl~E.f!l! t {!:::[iN[!: fr-tt"'C 52 fi!li;! 7J ·I)~ o, -'2 (i) ·) i?}ji ~ fij!;;l..: c C ~ (:1t.f.EJ(0lnl.{ff::p.l-[0i.l"t' f.t}{;, 1!::Eil!li~$c 22 fm:3'>7.>o 8!!Uih'>·<? li~~f.; ~0Jii~0tL
L'Pt,:~ 'f.>:. rfi'Ef~l:t;t~ii?JL:".~~tJ-J?!;i:*'g 10 .f<li, jl~.?.*G~J.;tl..qfW.ll~IJ.:!mtl1:ii•0(;!: 12 {ifiidJ 0 f.l L' ~ ' (, ,""7!i!li;!:{Sfifl!O)b0J Tilia eojaponica E;.;oo crJ•jTtlt0t0 Ti/ia protojaponica E:-;ooc~~C.~T¢c ifui1!\'iiW:~!Efil! Tilia japonica S1~1o:--:K :i)tft:Ji';lt'!cJll?tt~ {:,01:ci)¢ •<.

.it§~~The genus Ti!za comprises 52 species,of which 22 occur as fossils (LA:\IOTTE,
1952. pp. 342-343) and 30 as living species(LEE, 1935, pp. 807-818, pis. 226, 227).
Occurrence of living species is limited
to the temperate regions of the northernhemisphere. including about 20 species
and several varieties known in China.
As to the geologic age of the fossil
species, 10 species belong to Paleogene
and 12 to Neogene and Pleistocene, although some doubtful species are foundin Cretaceous sediments (HoLLICK, 1930.
p. 106, pl. 82, fig. 3).
The genus Tilia is identified by its
leaves which are heart-shaped with one
side developed better at the base. Margin of the leaves is usually serrated
and strongly glandular-tipped. Flowers
are arranged in a nearly radial cluster(cyme) on a long common stalk which
is provided with a characteristic longand narrow leafy bract.

The present paper describes two new
species, Tilia eojaponica ENoo of Eocene
and Ti!ia protojaponica ENDO of Miocene,both being regarded as ancestral formsof a living Tilia japonica SIMO:-IK.
Ti lia eojaponica E!\oo, n. sp.
Pl. 23, Figs. 1 and 2

Description :-Leaves simple, nearly
orbicular in shape: tip prolonged acu·
minate: base deeply cordate, margins
denticulate with glandular tip; length±6 em: width ±6 em: petiole slender
1.5 em preserved ; palmately nerved witha strong midrib and usually 2 pairs oflateral primt?ries. The midrib stoutest ;from it diverge 4 pairs of alternate or
subopposite secondaries at angle ofabout 40°. runing directly to the margin
or arching slightly toward the tip. The
first pair of lateral primaries is weaker
than that of the first pair: tertiary
venations and areolation are obscure;texture firm.

* Received Julr 9. 1965: read Jan. 2,1. 1965
at Tokyo.
188

50 l.

Tilia front Hokkaido

Remarks:- The present species isquite similar to the existing Tilia japonica SniK. in shape and nervation of
the leaves. The former is less serrate
than the latter. The primary nervationsof the genus Tilia are generally slenderand stout. The characteristic nervations
are easily distinguishable from othergenera. The genus Tilia includes 52
species, (22 species occur as fossils and
30 as living species). The present
species was collected from the troodwardaia zone of the Shin-yubari colliery,
Yubari city. It is probably a remoteancestor of existing japanese Tilia ja-

ponica SIMK.

18!)

and nervation of the leaves. The latteris less serrate than the former. The .
nervations of the genus Tilia are generally slender and stout. The characters.
are easily distinguishable from othersimilar genera in shape and nenrationof the leaves. Tilia includes 52 species(22 as fossils and 30 as living species);
and the .present fossil is more likely toexisting Tilia japonica, and this species
must be an ancestor of Tilia japonica
SIMK.

The material was collected by T. Y AGI(ex-professor of Tohoku University)from l'vlinase-mura, Okatsu·gun. Akita
Prefecture. Northern Japan. tsee Fig. 1,
pl. 27 in "leones of Fossil Plants fromJapanese Islands" by S. E:'\DO. 1955.)

Tilia protojaponica ENDO, n. sp.
Pl. 23, Fig. 3

Ti/ia japonica SIMO:\K

Seido El'DO: 1955 leones of fossil plantsfrom Japanese Islands, pl. 27, fig. l.

Pl. 23. Figs. 4 and 5

Description :-Leaves nearly orbicular
in shape: tip not preserved (probably
prolonged slender tip); base deeply
cordate: length ±5 em; width 6 to 6.5
em ; petiole slender :1: 4 em ; margin
denticulate with glandular tip. Palmatelyner\'ed with a stout midrib and usually
3 pairs of lateral primaries: the midrib
stoutest; from it diverge about 3 pairsof alternate or subopposite secondaries
at angles of about 35'. running directly
lo the margin or arching slightly toward the tips; the first pair of lateral
primaries give off several (usually 4)
abaxial secondaries; the second pair oflateral primaries is weaker and thinnerthan the first pair ; tertiaries and arealations are obscure ; texture firm.
Remarks:- The present material isquite similar to the existing Tilia japonica. This is more closer to Tilia
japonica than Tilia eojaponica in shape

Seido E.'< DO: 19·10 1\ Pleistocene Flora from
Shiobara. Japan. The Science Report,
Tohoku Imp. Univ. Second Series Vol.
XXI, No. I. p. 68. pl. 1. fig. 1: pl. 5, figs.
7. 19.

Description :-Leaves cordate or orbicular-cordate, lamina somewhat inequilateral. apex caudate-acuminate. Length
and width 5 to 9 em. i\largins denticulate with strongly glandular tip.
Petiole slender. 3 to 5 em long. Texture
firm. Palmately 5 or 7 nen'ed, acordrome; secondary nerves of middle primary in 5 to 7 alternate or subopposite
pairs and diverging from the primary
at angle -of 110 ±degrees. those of otherprimaries 3 or 4 in number issuing fromthe lower side of the primaries, camptodrome; tertiary nerves somewhat
regularly arranged, straight or curved
outwards. and connect the secondaries ;areolation obscure. Bract entire. oblanceolate or oblong-oblaoceolate ; reti-

Seido P..'NDO

190·culately nerved: 4 to 7 em long with ashort (l em long) peltate stalk.
Remarks: - The present material-agrees quite well with the existing
species. This species which now flourishes in the japanese Islands and China.
grow luxuriantly at the altitudes of-about 800 to 1.300 meters above sea.level in central Hondo. According to
K. MIYAHE and Y. KUDO (1929, p. 32),
"its distribution in Hokkaido is limited
to its main-island and the islet of Oku·shiri; it grows usually on soils rich inmoisture. associated with other decidu·ous tree such as [(alopana:r: septen/obum
Komz.. (.)uercus crispula BL., Fagus-crenata BL., Ascer pictum THUMB., Cer·
cidiphyllum japonicum SJEH. et Zucc ..
etc.
References
E;-~oo, S ..

Shiobara. Japan. Toltoku UnirJ .. Sci. Rep.,
Ser.2. Vo/.21. No.1. pp.68,69, pls.l. 5.
- - (1955) : leones of fossil plants fromjapanese Islands. Sang_yo Toslw, Tokyo.
HoLLICK, A., (1930): The Upper Cretaceous
Flora3 of Alaska. U.S. G. S. Prof. Paper,
15.9, pp. 106. pl. 82, fig. 3.
Hu. H. II. and CHA:"F:Y. R. W. (1938) : A
Miocene Flora from Shantung Province .
China. Carnegie Ins/. Washington Pub/.
No. 507. pp. 68-70. pl. 33, fig. 3. pl. 44,
figs. 1. 2, pl. 45, figs. 3. 7. 8, 1, 2. 4. pl.
50. fig. I.
LA:\IOTTE, R. S. (1935) : The Miocene Tiliasof Western America.
Carnegie Ins/.
TVasltingto11 Pub/. No. 455. pp. 41-48. pis.
1-3.
- - (1952) : Catalogue of the Cenozoic
Plants of North America through 1950.
Ceo/. Soc. llmer. Mem. 51. pp. 3·12-343.
LEE, S.C. (1935) : Forest Botany of China.
Commercial Press. Shanghai, pp. 807-818.
pis. 226, 227.

(1.940) : A Pleistocene Flora from

Shin-Yubari
Okatsu-gun
Uryu-gun~~1*

ifEJmlllli¥i1llHlll

Minase-mura ~ifjft
Numata-mura mmtt
Shiobara Spa jj,i!ljt~Jji

Explanation of Plate 23
Fig. 1. Tillia eojaponica E:-;oo x 1.
Locality: Shin-Yubari, Yubari city. Hokkaido (IVoodwardia zone, :\fiddle Eocene).
Fig. 2. Tilia eojaponica E:--:oo x ca. I.
Locality: Same as Fig. 1.
Fig. 3. Tilia protojaponica E:-.~oo xI.
Locality: Minase-mura, Okatsu-gun, Akita Prefecture (Uppe1· Miocene).
Fig. 4. Titia japonica SI~lO:XK x 1.
Locality: Shiobara Spa, Tochigi Prefecture (Lower Pleistocene).
Fig. 5. Tilia japonica Sr:-.1o:"K x 1.
Living leaf. for comparison.
Lo.:ality: Numata-mura, Uryu-gun, Hokkaido.

E NDO :Tilia from Hokkaido

Plate 23

Trans. Proc. Palaeont. Soc. Japan, N. S .. ~o. 61, pp. 191-200. pis. 24. 25, April 10, 1966

502.

SHELL STRUCTURE OF JAPANESE .SMALLER FORAl\UNIF.ERA
PART 2.

PilRAROTALTA. NIPPONICA (ASANO. 19:3(i)*HIROSIII UJIIE

Department of Paleontology, 1\ational Science Museum. Tokyo. Et:1;:~,H\'l:fHL.!.h1£iO)l'8H/til!f; ~0) 2. Pararotalia nipponica (AsA1'\0, 1936): Rotalia
mppomca AsA:->o O)J'i!l!Hiti'li'i: h [.., §ctlL.. -tniJ> Pararota/ia fll;:;...~ c ~t.:o ;J;t.:. -tO)ttf.JUc.:>z::mJ:~1)~IM' J:: !J. ~~"'!:~ ~n.r., lltf.Ef;t. ~!c fjH!ic -c O)ll'lJi.ll8\SO)iit)JW,lc~
IL:-::>P'"C. :kPI:~JE"t«~.~>£-~1±1 Lt.:, 7l~. Rota/ia ozawai AsA:--;o, 1951, t.Jt;$:N!O)<<

x/J,H1/Ir-t~t~~' c.. c b, i'ri~~-?lJltlt!ft#t%J9'0)£~tJ- ~lltibt.:o:\laterials and Occurrence.Il;* '1i:.

different from " /?." nipprmica; e. g.
rounded transverse periphery of test,
Ammonia-type aperture. no. large internal
tooth-plate, etc.
Rotalia ozawai ASANO, 1951, describedfirst from the Pliocene Sawane Formation in Niigata Prefecture, has beenreported from various locali lies extending from Honshu to the seas of South
China and the Philippine Islands. As
fossil it occurs mostly from the Pliocene
and later deposits as \veil as in theshallow water sediments.
From the writer's experience, the two
species mentioned above are always
found in association in the same sample
of sediments. Such a co·existence in
specimens from Taiwan was noticed by
HUAJS'G (196!) between Pararotalia ozawai (=Rota/ia ozawai ASANO) and Pararotalia taiwanica (NAKA:\IURA), which isreally "Rotalia" nipponica according to
the writer's opinion. On the other hand,the figure of HUANG's Ammonia nipponica
evidently shows that it may belong toa distinct genus. HUANG attributed thisco-existence to a phylogenetic intergradation of morphology between " Para-

Since No/alia llipjJo11ica ASANO. 1936,
was described from the Pliocene. Tomioka Formation in Kanagawa Prefecture,it has been found to be a species common in the Neogene to Quaternarystrata or in the Recent shallow water
sediments of the japanese Islands andtheir adjacent areas. Its geographic
distribution seems to be restricted to
the region south of Honshu, althoughYosmnA (1958) reported it from the
Miocene Okawa and lkushima Formations of western Hokkaido. llis figure
shows clearly many different charactersfrom those of the true .. Rotalia " nipponica. So far as the writer knows, itsgeologic occurrence appears to be limited to the strata younger than the late
Pliocene. AsANO (1951) regarded Rotalia
ikebei INOUE and NAKASEKO, 1951, fromthe :\1iocene Sakuma Formation of Chiba
Prefecture, to be an aberrant form of
this species. The present !vliocene"Rotalia ··, however, has many features~ Received Oct. 4. 1965: read jan. 21. 1965
.at Tokyo.

lHl

192

Hiroshi UJ 1/ i:rotalia ozawai" and " Pararotalia taiwanica ". In the writer's observations
on the co-existence of those two species
from Japan. the coarser fractions of
sediments contain many specimens of
Lhe so-called " Rotalia " nipponica but
none of the so-called "Rotalia ·· ozawai.
whereas the latter .. species" is exclusively found in the finer fractions of
the same sediments. Unfortunately sucha relation between the test-size and theparticle-size of the sediments had nol
been recognized in any published reportson these " species •·. An exceptionalcase is TAKA YANAGI's investigation(1955) on the distribution of the foraminifera in the inlet of l'v1atsukawa-ura
and its adjacent sea. judging from thelist of the foraminifers and their distribution shown by him and the data of
mechanical analysis of the same sediments made by Mil (1955). it is evident
that .. Rotalia nipponiw .. and " R. ozawai ·· occur very commonly and always
in association in the Isobe facies, namely
off-shore facies of Matsukawa-ura. andless commonly in the .Nlatsukawa-minato
subfacies, namely the entrance area of:Vlatsukawa-ura. Within the latter area.
·· R. ozawai" is found only in areas of
medium- to fine-grained sands, while theoccurrences of " R. nipponica .. \Vithout" R. ozawai .. are restricted to areas of
medium· to coarse-grained sands. At
Loc. L-3 of coarse-grained sands, there
is reported an abundant occurrence of.. R. nipponica ... amounting to 2.7 percent of the total specimens of foraminifera.
The above-mentioned field-evidence
that " Rotalia ozawai .. is merely a young
form of .. Rotalia nipptJnica "is supported by the detailed investigation on the
test-morphology and its internal structure as stated in later paragraphs.
Many specimens of both " species" inthe same sediment-sample from the sea
coast of Katase in Kanagawa Prefecture
w·ere dissected or sectioned. The results
were re,examined by observations on
many topotypic materials of "R. nipponica " and on the holotype of " R.
ozau·ai" through the courtesy of Prof.
K. ASANO.
The detailed re-examination not only
clarifies the true generic position ofthese .. Rolalia " but also suggests thenecessity for a re-consideration of thegeneric definition of Pararotalia, to\\'hich both " species" belong.
Description
Family Rotaliidae EHRENBERG. 1839
Genus Pararolalia LE CALVEZ. 1949

Pararolalia nipponica (ASANO, 1939)(Text-figs. 1-3: Pl. 24. figs. 1-7:
Pl. 25. figs. 1-5)
Rota/ia nipponica AsA:"o. 1936, p. 614. pl. 31.
figs. 2a-c. -AsAl"O. 1951. p. 15. text-figs.
112-114. -TAKAY.\!\'AGI, 1955, pl. 2, fig. 14.
-M.\TSt!:"c\CA. 1963. pl. 45. figs. 9a-c.
Not Rotalia nipponica AsA:-:o. -YosHIDA.
1958. p. 270. pl. 3. figs. 6a-c.
Not Ammonia nipponica {AsA:-.~o). -HUA:"G,
19&!, p. 54. pl. 2. fig. 1.
Rotalia ozarmi AsAKo, 1951. p. 15. text-figs.
115-117 -'fAKAYA:\ACI. 1955, pl. 2. fig. 17.
.. Rotalia.. ozawai AsANO. -GRAIIA~t andl\ltLITANTF., 1959, p. 100. pl. 15, figs. 6-8.
Neorotalia ozawai (AsA"'O). -POLSKI. !955,
p. 576. -WALLER. 1960. p. 1180.
Pararotalia ozawai (AsANo). -HuANG. 1964,
p. 56. pi 1. figs. 14a-c.
Cf. Rotalia ozau·ai AsAJ\'0, -MATSUJ\'AGA.
1963. pl. 46. figs. 9a-c.
J>ararotalia taiwanica (NAKA~WRA). -HlJA:"G,
19&L pp. 56-58. pl. 2, figs. 2a-c.
Cf. Rotalia taiwanica NAKA~tuRA. 1937. p. 141.
pl. 12, figs. 6a-c.

Description:

Test free, biconvex to-502.

Structure of Pararotalia nipronica.

plano·convex, low trochospiral coil ofthree volutions; periphery weakly keel·ed, peripheral outline slig(ftly lobulate
or smooth in adult, but with a shortand solid spine on each chamber inmany young specimens; spiral sulUres
limbate and flush on surface, sometimes
remaining spinate protrusions encrustedwith secondary deposition of shell rna·terials in earlier parts; chambers num·erous, increase \Vith shell·growth fromsix or seven up to nine and half per
one volution ; intercameral sutures lim·bate and flush on spiral side, deeply de·pressed on umbilical side. forming open
ventral fissures: intercameral septum
imperforate, secondarily double. leaving
open space on umbilical side. but per·fectly closed on spiral side, towards
which anterior lamella thins out: spiro·
thecal wall distinctly perforate. of radi·
ally fibrous calcite: spiral surface smooth
but umbilical one sometimes with secondary deposition of clear shell materials in form of very small buttons: umbilicus \Vith open umbilical-ventral fis·sures along intercameral sutures andlarge central plug throughout. umbilicalplug extending inward to proloculus.
forming a single clear and imperforate
pillar of shell meterial without canal;
aperture interiomarginal-basal arch onumbilical side, its spiral end slightly
extending towards shell-periphery. withweakly indented and distinct rim along
its distal (dorso-peripheral) margin: in·tercameral foramen areal, comma-shaped.
converted from aperture by attachmentof tooth plate at its proximal margin.
remaining rim intact ; tooth plate imper·
forate. extending from proximal marginof last intercameral foramen to distal(peripheral) margin of aperture, adher·
ing its basal (umbilical) margin on pro·ximal margin of spirothecal wall of lastchamber throughout whole chamber·

193

length, developing its upper (dorsal)
free part broadly but very thinly inform of spatula with concaye face turn·ed to axial side and its upper anterior
margin bent inwardly: narrow slit open
between central plug and perforate pro·ximal margin of last chamber (not "umbilical lip'") in many specimens, com·municating with. chamber-lumen througha narrow passage between spatula·shap·
ed tooth plate and extra-umbilical wallof previous volution ; umbilical slit closedwith secondary deposition of shell substance in penultimate and preceding
chambers of most specimens. dissolved
spatula-shaped part of tooth plate at
the same time.
I-lypotypes: Reg. Nos. 5887 to 5903, Nat.
Sci. i'vlus. from the sea coast of 1\atase.
near the boundary of Kamakura Cityand Fujisawa City. Kanagawa Prefecture (Lat. 35"18'N: Long. 139'29.5'£).
Remarks: In 1943, lSHIZAKI pointed
out that the "aperture" (really lastintercameral foramen) of Rotalia niP·
ponlca ASAI'\0 is areal comma-shape justthe same as those of Calcarina calcaro"ORBIGNY.

Calcarlna venus/a (BRADY),

and Calcarina taiwanica (NAKA!vll1l{A).
which are now regarded as representa·
tives of Pararotalia. He followed FI:S:·
LAY's definition of the genus Calcarina.
Namely, FTI'\LAY (1939) accepted GALLO·
WAY's opinion (1933) that Nautilus spengleri GiVIELI~. 1788, which was designatedsubsequently as the type species ofCalcarina D'0RRJG.:\Y. 1826, by PARKER
and ]ONES, 1859, should be included in
the genus Tlnoporus Mo~TFORT. 1808.
and recognized Calcari na calcar D"OR·mG-.;Y, 1826, as the type species bytautonymy. Differing from GALLOWAY's
opinion, however. the validation of thegenus Tinoporus was doubted by CuSH·
i\!AN (1921) and suppressed by LoEBLICH
and TAPPAN (1962). The latter authors

194

Hiroshi UJIIE

Text-fig. 1. Specimen dissected at spiral part of
spirothecal wall of the last chamber, to show a verythin internal tooth plate of spatula form; a: aperture,
f: last intercam eral foramen, r': its rim, t: upper andanterior margin flared inward ly of tooth plate; Reg. No.
5890.

T ex t-fig. 2. Spiral-apertural view of specimen dissected at spiral-anterior part of the last chamber-wall,
to show the situation of the tooth plate. Thick arrow
line indicates the connection between the inside andthe outside of the t est; a: aperture, r: its rim, f: last
i ntercameral forame n , r': its rim ;. Reg. No. 5891.

concluded that the type species of Calcarina is Nau tilus
spengleri GM£LIN, because
Calcarina calcar was "included in the Modeles, but neither
described nor figured, hence a
nomen nudum, and in spite of
the tautonymous name cannot
be the type species." If it validated later, Calcarina calcar
may belong to Pararotalia aGsuggested by REISS and MERLING (1958) and HOFKER (1960).
According to the writer'~>observation on the holotyp ·~of Rotalia ozawai ASANO, 1951,
this specimen shows somewhat chalky appearance sothat the sutures on its spiralside are obscure as seen in
the original fig ure.
This
situation was a lso reported by
POLSKI (1959) and by WALLH(1960) in many specimensfrom off China. If it is due
to preservation during fossilization as POLSKI believed, thisspecies has the same characters as Rotalia nipponica ASANO, 1936, except for the smaller size of test and the peripheral spines of the former
species. As stated already,the smaller and spinate ozawai
occurs almost always together
with the larger and non-~pin­ate nipponica , if t here was nosorting effect which separated
those specimens into these
two "species" after death, although the smaller but nonspinate f orms are found exceptionally (for example, Pl.
1, fig. 3; GRAHAM and MILTTANTE, 1959, Pl. 15, fig. 6).
When the adult specimen of502.

Structure o.f Vararotalia nim;onica

195

Rotalia nipponica as Rotalia taiwanica.
It seems to be necessary to re-study the
topotypic materials of the latter species
in the light of modern taxonomy.

Text-fig. 3b.

Text-fig. 3a.

Text-fig. 3. Schematic figure showing
morphology of the tooth plate and its relation with the aperture and the intercameral foramen ; 3a: same view as Textfig. 2; 3h: view from proximal (axial)
side; u: umbilical slit between umbilicalend of chamber wall (or umbilical marginof tooth plate) and spirothecal wall of theprevious volution: other abbreviation~same as in Text-fig. 2.

nipponica-type is immersed in glycerinor sectioned near at the spiral surface.
some peripheral spines are observed to
be preserved in the earlier parts. Suchan ontogenetic degeneration of the peripheral spines as seen in Pararotalia
nipponica (ASA:SO) seems to be the reverse to what LOEBLICII and TAPPA:\(1957) supposed in the phylogenetic development of spines in their lineage
from Pararotalia macneili LOEBLTCH and
TAPPAN to Pararolalia armata (o'ORIWiNY). This argument may be not soimportant, because the spines of thisgenus are caused only by the chambershape.
NAKAMURA (1937) described Rota!ia
taiwanica NAKAl\IURA from the Upper
Byoritsu beds (Pliocene) of West Taiwan
and remarked as follows: " This species
closely resembles R. nipponica AsA:SO,
but differs from it in lobulated peripheryand fewer chambers." They may beconspecific judging from his obscure
figure and description and from the "reexamination" by HUANG (196:1). who
appears to have misidentified the true

Comments on the GenericDefinition of Pararotalia
This genus was restudied in detailby LOEBJ.JCH and T APPA:S (1957) using
several species including the type species. In the following year (1958). REISS
and MERLING published their work on
this genus from the view-point of internal structure and pointed out some discrepancies from LOEBLICH and TAPPA~'s
emendation. Two important different
features are concerned with the composition of the intercameral septal walland the tooth plate.
What the intercameral septal wall issecondarily double was reyealed by
REISS and l'viERLTNG and also by IIOFI<ER(1960) who, however, denied it later(1962). This feature seems to have been
accepted in a synthetic text-book by
LOEBLICH and TAPPAN (1964). because
they place this genus in the subfamily
Rotaliinae, a procedure different fromtheir previous view. It is better. thewriter thinks. that this character should
be more clearly stated in the genericdescription of Pararotalia. although thetwo lamellae of the septal wall sometimes adhere to each other so closelythat the open space between them oreven their boundary can not be recognized, especially near the spiral surfaceof the test.
Concerning the tooth plate and its
adjacent parts. REISS and MERLI:SG(1958) criticized LOEBLICII and TAPPA:S's
description ( 1957) as follows: " 'What
they have described as secondary umbilical plates in Pararotalia refers to196

Hiroshi U!IIE

actual chamber w·alls: the internal
septum described in' the latter genus
by those authors is formed by the toothplate.- The toolhplates are primarily
formed structures and no secondary
umbilical plates are formed in Pararo.talia." At least parts of the present
discussion seem to be adopted in the
text-book by LOEBLICH and TAPPA?\{1964). although the diagnosis of the
tooth plate is too simple.
These authors. however. retained apart of the previous description (1957)
as "-, umbilical region of each chamber partially covered by secondary umbilical plates " and this was changedslightly as follows: "-. umbilical regionof each chamber partially covered byumbilical flap; -." REISS and 1\IERI.ING(1958) rated this umbilical " plate·· asmerely a part of the chamber wall but
such a treatment may be superficial.
According to the writer's observation
on Pararolalia nipponica, the secondary
deposition of shell materials occurs likeplaster over an umbilical slit bet\veen
the spirothecal wall of the previous
volution and the proximal (axial) end
of each chamber wall of the following
volution. It is not a mere chamber walland its remnant, as evidenced after
the dissection of the wall, may be
shaped like " plate " or " flap". Thisfilling-up is already seen at the penultimate chamber in many cases andrarely even at the last chamber, although the umbilical slit of the lastor often the penultimate chamber isusually open.
REISS and MERI.I?\G \1958) seem tooverlook the presence of this kind ofumbilical slit ("umbilical labial aperture"), which can not be seen in thedissected specimen shown by theseauthors (Pl. 5. figs. 17-20). because it isscreened from view by the tooth plate(probably its basal part, strictly speaking).
The basal (umbilical) margin of the
tooth plate adheres to the proximal(axial) and of the spirothecal wall of
the last chamber and the upper (dorsal)
margin develops highly so that there isdeveloped an internal partition within
the last chamber. Although LoEBLICH
and TAPPAN (1957) recogniied such arole of the tooth plate calling it internal
septum. they overlooked its porelessstructure. which is characteristic in thetrue tooth plate and, besides. an important discontinuity between the pro·ximal margin of chamber wall and theumbilical margin of the tooth plate{1957. Pl. 1. fig. 2; 1964, Fig. 486-2). In
the same figure of the type species(Rotalia iuermis TERQUEM). both authors
showed the mode of tooth plate whichruns from the proximal margin of thelast intercameral foramen towards theanterior side within the last chamber
but is cut off at a half distance of thechamber-length and never reaches theaperture. Previously the writer (1963)
also reported a similar sittiation of the
tooth plate of Pararotalia murrayi(HERON-ALLEN and EARLAND). The
mode might be caused by the breakdown of the anterior half of the whole
tooth plate at the time of dissection.
On the other hand, REISS and MERLING(1958) figured the tooth plate of Pararotalia inermis (TERQUE:.ll running fromthe preceding foramen to the apertureand restricted in its height to be very
low. This condition suggests that it
might have been made by the partial
disolution of the upper free part of an
originally higher tooth plate.
There is seen a large difference between LOEBLICII and TAPPAN's opinion
and REISS and l'viERT.TNG's one concerning the shape of the tooth plate of the.502.

Structure of Pararotalia nipponica

same species. Paratotalia i11ermis. If it
is supposed that the observations' ofboth authors are actual figures but only
a partial remnant of 'the same shaped
tooth plate owing to slightly rough dis·section, the true shape of the toothplate of this type species would be very
similar to that of Pararotalia nippollica:
namely. a very thin tooth plate v,ihich
starts from the proximal (axial) marginof the last intercameral foramen near
the · spirothecal wall of the previous
volution, then intersects the wholechamber-length attaching its basal (Um·bilical) margin on the proximal marginof the chamber and its upper (dorsal)
part developing broadly in form of a
spatula. and reaches to the distal (peripheral) margin of the aperture. The
writer believes that many species ofPararotalia including the type species
should be re-examined with very careful
dissection of the chamber wall of the
spiral side and with skillful techniqueof sectioning. Concerning Pararotalia
tuberculifera (REISS). HoFKER 119601
stated .. the toothplate is formed at firstat the sutural part of the aperture. thenruns over its dorsal part. and flares off
at the distal part of the aperture. thus.
as REISS believes. forming the porelesspart of the double septum in case thata next chamber is formed.'' Really the
tooth plate and REISS's sepal flap arequite different as stated by REISS and!viERLI~G (1958).
The .. tooth plate··shown by HoFKER in four figures attaches on the distal margin of the foramen and extends within the chamberlumen tow·ards the anterior side considerably. It resembles REISs's rim or
LOEBLICH and TAPPAN's lip. except for
its extreme development and. thererore.
it may not be a true tooth plate. "l~im''on the anterior side of the foramennever continues to the previous tooth197

plate attached on the posterior side of
the same foramen as revealed in thepreceding description (see also Pl. 25,
figs. 2 and 3).
Taxonomic Position of theGenus Pararotalia
In a monographic work on Pararotalia,
LOEBLICII and TAPPAN (1957) stated:.. It [Pararotalia] does not have radial
canals or fissures. nor does it haYe in·traseptal and subsutural canals andthus does not belong to the Rotaliidae ··but probably to the Discorbidae. This
opinion. however. was denied by REISS
and MERLIXG (1958) who presented several photographs of sectioned tests ofPararotalia showing clearly the doubleintercameral septa.
Later, LOEBLICII
and TAPI'AN (1964) recognized this feature and re-assigned the genus Pm·aro·/alia as a member of the family Rotaliidae in their new system of foramini·feral classification. l\.leanwhile. HoFKER\1960) also reported the presence of adouble septal wall but later (1962) expressed the opposite viev,; as follows:.. the septa between the chambers inPararotalia are simple. and a complicatedtooth plate, as is found in Rotalia tro·
chidaeformi:; LA~1ARCK and in Streblus
beccarii (LINNE). does not occur in Pararotalia. - So it must be qui tc uncertainthat Pararotalia has anything to do with
the Rotaliidae." Instead he stressed on
the close relationship between this genus
and Globorolalia since 1957 and suggested its derivation from the Ia tter genus.
REISS (1963) criticised the present viewand said that Globorotalia has bilamel!idwall differing from Pararota/ia.
Following SJ\WUT's suggestion (1955).
REISS and 1\IER LING (1957) emphasizedon the close relationship between Pararota lia and some members of the !viis-

198

Jliros}u: UJIIE

cellaneidae and. most recently. REISS(1963) established a new subfamily
Pararotaliinae as one of the two subdivisions of the family ~v1iscellaneidae
SIGAL, 1952, separating it from thefamily Rotaliidae. Such a treatment
appears to depend upon the original
definition of the l'vliscellaneidae: namely.
.. Le caractere essentiel est !'absence decorde marginate et done de tout systeme
canaliculaire longitudinal: il n'y a quedes canaux intraseptaux et verticaux(ou radiaux). le plus souvent tres cteveloppes." In his definition of the family
Miscellaneidae, REISS (1963) stated " Intraseptal passages communicate withtubular vertical. radial and sutural canals, which may be divergent and opening in double rows. or through canals
and fissures with grooves (marginal.
lateral or divergent (chevron shaped)
sutural). or with intramural. lateral andfor marginal cavities which is turn lead
into canals." According to REISS andMERLING (1958). "Intraseptal spaces between a previous distal chamber-walland subsequently built septal flap are

not true canals." In Pararotalia, therefore. there is no true canal and its intraseptal spaces always remains open
towards the outside of the test. The
system of intraseptal passages resembles
rather that of Ammonia. the main member of the Rotaliidae. On the otherhand. " two genera of the subfamily
Pararotaliinae" (Cuvilherina and La_ffiteina) have well developed and complic·
ate canal-system and. besides. different
major construction of test. If Pararo·
talia is considered as a probable but
direct ancester of the two genera as
REISS thought. therefore. some transitional forms should be supposed between
them. These three genera. moreover,possess some considerable differencesfrom the proper subfamily of the Miscellaneiclae (i.e. lVIiscellaneinae) andseem to belong to the other family as
treated by many authors.
Acknowledgements
The writer was given an oppotunity
to examine the type specimens of Ro·

Explanation of Plate 24
Fig. 1. Full-grown specimen with smooth peripheral outline: i.e. nipponica-type, a: spiralside, b: umbilical side. c: apertural side, x 70; Reg. No. 5887.
Fig. 2. Young specimen with distinctly spinate peripheral outline: i.e. ozawai-type, a: spiralside, b: umbilical side, c: a pert ural side. x 70; Reg. No. 5888
Fig. 3. Rare young specimen with rather smooth peripheral outline: spiral side, x70; Reg.
No. 5889.
Fig. 4. Vertical section of a young specimen, showing the last intercameral foramen with
distinct trace of rim (r) and of tooth plate (t). x 150: Reg. No. 5899.
Fig. 5. Vertical section of an adult specimen. in particular, showing the aperture and its
adjacent area, where the umbilical spirothecal wall of the _last chamber was damaged.
x 150; Reg. No. 5898.
Fig. 6. Vertical section of an adult specimen, in particular, showing a partial trace of avery thin and curved tooth plate (t) within the last chamber-lumen and an open umbilical slit (u). x200; Reg. No. 5897.
Fig. 7. Enlarged photograph of the apertural area of the specimen shown in Fig. 5. showing
distinct rim (r). no trace of tooth plate. and open umbilical side of aperture, x 750.

UJIIE;

Structure of Pararotalia nipponica

Plate 24

502.

Structure of Pamrotalia nipponica/alia nipponica and Rotalia ozau.1ai by
the courtesy of Professor Kiyoshi AsANo of the Tohoku University.
He isalso indebted to Professor Kotora HATAIof the same University for his readingof the manuscript and to Dr. Hiroshi
OZAKI of the National Science Museum
for his encouragements during thisserial work.

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Muraoka-mura, Kamakura-g6ri, Kanagawa Prefecture. Ceo/. Soc. japan. jour ..
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- - (1951): Illustrated catalogue of Japanese Tertiarr smaller Foraminifera, Pt.
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IIoFKER. J. (1960): Foraminifera from theCretaceous of South-Limburg, Netherlands. Pt. 50: The aperture of Pararotalia
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andblad Limburg, vol. 4.9. nos. 7-8. p. 7983. 2 pis.
- - (1961) : Ditto. Pt. 54: Some smaller

199

rotaliids in the lower Paleocene above
the Md in the Quarry Curfs. ncar I-Iouthem. South-Limburg. Ibid .. vo/. 50. nos ..
7-8. p. 85-87.
- - (1963) : Ditto, Pt. 66: Once again Pararotalia tuberculifera (REt.:ss). !bid., vol.
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- - and - - (1962) : The status and type.
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- - and - - (196,1): Treatise on invertebrate paleontology. Pt. C. Protista 2, vol.
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MATSUKAGA, T. (1963): Benthonic smaller
Foraminifera from the oil fields of north·ern Japan. TOhoku Unil• .. Sci. Rep., ser.
2, val. 35. 110. 2. p. 67-122. pis. 21-52.
M11. H. (1955): Marine sediments of Matsukawa-ura and its vicinity. TOhoku U11iv.,
Contr. Ins/. Ceo/. Pal.. 110. -15. pp. 5-17
(In Japanese).
NAKA:\!t.:RA, M. (1937) : ~ew species of fossil Foraminifera from the Broritu bedsof the oil fields of northern Taiwan(Formosa), Japan. ]ap. jour. Ceo/. Geogr.,
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POLSKI. W. (1959): Foraminiferal biofacies
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REISS. z. (1963) : Reclassification of perforate Foraminifera. Israel Ceo/. Surv.,
Bull .. no . .15. 111 p., 8 pis.
- - and P. MERLII"G (1958): Structure ofsome Rotaliidea. Ibid .. no. 21, 19 pp., 5
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SteAL, J. (1952) : Ordre de Foraminifera: inthe Traite de Paleontologic. cd. Piveteau,].. tome 1. Masson et Cie. i>aris. p. 133-

Hiroshi UJ ll E

200

301.
TAKAYA:-.'.-\GI. Y. (1955): Recent Foramini.
fera from :Matsukawa·ura and its vicinity. Tohoku Univ., Contr. Jnst. Geol. Pal.,
no. 45, pp. 18-52, pis. 1-2, 1 table (Injapanese).
UJIIR. H. (1963): Foraminifera from theIsobe facies
Katase~tlllmfi·~

Yurakucho Formation (Holocene), Tokyo
City. Tokyo Kyoiku Daigaku. Sci. Rep ..
Sec. C. vol. 8, 110. 79, pp. 229-243. 3 pis.
WALLER. H. 0. (1960):
Foraminiferal bio·
facies off the South China coast. jour.
Pal., val. 34, no. 6, p. 1164-1182.

Matsukawa.minato.:\Iatsukawa.ura~lllif~.I}JIIilli

Explanation of Plate 25(X 150)Fig. 1. Horizontal section cut near the spiral surface of an adult specimen with smooth
peripheral outline, in particular, showing the earlier peripheral spines (s) encrusted bysecondary shell substance. It seems that most intercameral septa are composed of asingle lamella at a glance, because of the compact adhering of two lamellae and of the
upward thinning-out of an anterior lamella; Reg. No. 5892.
Fig. 2. Horizontal section cut at the more umbilical side than Fig. 1. in particular, showing
rim (r) and proxial (axial) trace of tooth plate (t) ; Reg. No. 5893.
Fig. 3. Horizontal section cut at slightly more umbilical side than Fig. 2, in particular. show·
ing proximal and distal traces of tooth plate (t). In this figure, there are recognized
the open spaces between the last four chambers. The earlier volutions of this figure,as well as Fig. 2, include the closed spaces (c) between the adjacent chambers andbetween chambers and central plug; Reg. No. 5894.
Fig. 4. Horizontal section cut near the spiral surface of a spinate young specimen, in particular, showing solid spines without any internal canal; Reg. No. 5895.
Fig. 5. Horizontal section cut near the spiral surface of a rare young specimen with smooth
peripheral outline: Reg. ~o. 5896.

UJIIE:

Structure of Pararotalia nipponica

Plate 25

Trans. Proc. Palaeont. Soc. Japan, N. S.. No. 61. pp. 201-206, pl. 26. April 10, 1966

50:3.

NOTES ON AMMOiVITES BOURGEOIS! D'ORBIGNY FROMTHE UPPER CRETACEOUS OF FRANCE*TATSURO l'.lATSUl\IOTO
Department of Geology. Kyushu University

7 7;.; 7.0.:>.1:$13!lli~sl¥. Ammonites bourgeoisi o·or~BIG;>;Y ::-?t 'L:-c.

;~:l\l!OJb;{iji!t

-c. <

<

'£-~M L
6 f!l!O)~~~~i:<F c~ 1 -?i-i&~il::~*i:~}i:: l. ..::- O~~;;J:;;r_:b L ~r.
~ l t:., ltl!LD~* ~:: :11. ~ ~--.~~.:: '-' t,;. ~t::. iJ'';. :J O.:>ifd£JI!())~~:r:ff:-t, GRossot;vRE(1894) (})jf(..l.,t:.li-*ii D'0RBIG:-.IY J:. 1) fi0 ::1 v 7 Y , ;.; i.:.JM-t 'i>i:J~. J:Jev"Jj&~J:\t'l{-j;:

ICJ:

n7.>

<~}.t.:: t,;,OJfp.;, f!t~i-ff:Tftl!(}).tiH;::{JJ.t: !.) 0)~ l: j;) ;~,, ;tlf.:::t Protexallites MATst:-!fJ55 O)~~:ftj!l;'j){)iJ{, 4,-i[!IO)fi(.}tf!::.J:: ::J,c.ti.-?t.::,l\IOTO,liiJ0:\0YI\ifi·Nll&/.!::O)~j;f>(i--t- -j!!IJ!lm
t.~: :1~;ij! fll)chacune pres du dos de trois ou quatre
tubercules externes; une carcne munie
de sillons lateraux. Villedieu (Loir-etCher). Saint-Frimbault (Sarthe)." His
description was shown as item no. 16
under the Senonian species. Althoughno specimens were illustrated in his
original book, six specimens are nO\\.available in the Collection of o'ORBIG::\Yat the Museum National d'Histoire Na·
turelle, Paris. By courtesy of Dr. ]. P.
LEH~IA~ and Dr. jacques SORNAY I
have had recently an opportunity of
studying them. This paper presents a
result of the study.
The six syntypes differ to a considerable extent one from another. One ofthem which rather shows mean characters. is selected here as the lectotype,as defined below. The others seem toshow the extent of variation of thesame species. The syntypes have beenregistered at the Museum with the same
number 1'\o. 7181: \\!ith suffix A for thefive specimens from Saint·Frimbault(Sarthe) and without A for the one from
Villedieu (Loir-et-Cher). For convenience'

Introduction

When I discussed the origin of Texanites and the evolution of the subfamily
Texanitinae, I established genus Protexanites designating Ammonites bourgeoisi n'ORBIG!\Y, from the Coniacian ofFrance, as the type-species. As regards
this French species DE GROSSOUVRE{189-1. p. 73, pl. 13. fig. 2 ; pl. H figs. 2-5)
described in detail and gave fine illustration under the generic name of Mor·
toniceras. I myself depended on GROS·SOUVRE to understand the diagnosis of
the species.
For some reason GROSSOUVRE did notillustrate o'ORBJG~Y·s original specimens
but showed the pictures of the specimens of LE rviESLE's subsequent collection. D'ORBIGNY's definition of Ammonite.~ Bourgeoisianus was very brief. as
quoted here from his original descri p·tion (n'ORBIGNY. 1850, p. 212): .. Helleespece yoisine de l'Ammonites 1:arians.
mais pourvue de cotes simples, ornees• Received Nov. 6, 1965: read Nov. 7. 1965
at Chiba.

201

202

Tatsm·o MATSUM01'0

sake I temporarily call them No. 7181A1 to No. 7181A-5 and No. 7181-6.

Lectotype of Ammonites

bourgeoisi D'0RBIGNY
Before going further I acknowledge
here my heartfelt thanks to the Director.
Dr. ]. P. LEHMAN. and Dr. jacques
SoRNA Y who gave me every facility forthe study at the Institut de Paleontologie. tvluseum National d'Histoire Naturelle. Paris.
The published photographs have been provided there.

DiameterUmbilicusu.;o.

Pl. 26. Fig. la. b; Text-fig. la, b

The lectotype, here designated. is
No. 7181A-l of n'ORRIGNY's collection in
the l'vluscum. Paris (illustrated in thispaper, Pl. 26, Figs. la. b; Text-fig. la,b). It is wholly septate and, accordingly,
the full-grown whorl must have been
considerably large.
The measurements follow:
Heightcostal119.0-1/6 vol. 110.0-2/3 vol.

52.4
45.0

0.44
0.41

As is shown by the above figures. theumbilicus is fairly wide, occupyingslightly over 40 percent of the shell
diameter. Only the ventral part. outside the ventrolateral tubercles. of theinner whorl is overlapped by the outer.
The whorl is subquadrate in cross section. nearly as high as broad in costal
section, slightly higher than broad inintercostal section, and broadest above
the umbilical shoulder; the umbilicalwall is vertical, the flanks are slightly
convergent, and the ventrolateral shoul-

-16.2
39.0
26.0

c.45.538.5
27.5

Breadthintercostal

c.

i. c.

34
23

0.98
0.98
1. 05

0.87
0.88

B.;n.

der is sloping.
The ribs are all simple, as far as theobservable parts are concerned. They
are slightly prorsiradiate; some arenearly straight, others are slightly flexuous or concave. They are moderately
strong and separated by wider interspaces. On the whorl of 120 mm. indiameter there are 24 ribs. of which 20
have umbilical bullae and 4 are slightly
shorter and have no bullae. The umbilical bullae are highest somewhat
above the shoulder. They are moder-

U3 U2

L

llj
E

;\
I

I

I

I

I
I
I

I

1

I
I

•

I

I:

1omm.
L--.......1abFig. 1. Lebtotype of Prote::canites bourgeoisi (o'ORDIG:-;Y).
Whorl-section (a) along a rib at the stage about 1/3 \·olution behind the anterior end,
with an approximate outline of intercostal section (dotted line) immediately behintl
the rib.

503.

ately strong but may be weak on someribs. Each rib has a rounded, moder·ately strong tubercle at the ventrolateralshoulder and an elevated clavus at its
ventral end. The median ventral keel
·On the internal mould is somewhat lower
than the top of the ventral clavi. It isslightly wavy, for it is slightly moreelevated at the position corresponding
to the ventral clavi. The ventral clavus
is closer to the ventral keel than to theventrolateral tubercle.
The suture is of normal collignoniceratid type. The saddle between E
and L is broad, subquadrate in roughoutline and divided. The first laterallobe (L) is situated at about the middle
Specimen

DiameterNo. 7181A-2 max.l20
112.0
No. 7181A-3
107.0
~o.

7181A-·lmax.

70

No. 7181A-5 max. 80.. (-1;2vol.).. (-3;2vol.)No. 7181-6
74.0

~03

A.mmonites bourgeoisi from Franceof the flank. somewhat deeper and nar·rower than the ventral lobe (E), andindistinctly bipartite. The second laterallobe (U2) is much smaller than L. Its
inner margin is approximately situatedat the umbilical shoulder. The subdivisions of U3 are small and not numerous.

Other Syntypes of Ammonites

bourgeoisi
The rest of the available syntypes
exhibits essentially the same characteras the lectotype but shows a consider·able variability in detail. The measure·ments come at first.

u.;o.

Height42.0·16. 0

0.375
0. 43

37
37
34.5

30.5

0. ·135

Umbilicus

31. 5

27.0

The specimen No. 7181A-2 agrees inmany respects with the lectotype, but
it has a narro\ver umbilicus.
The specimen No. 7181A-3 is as widely
umbilicate as the lectotype. Its whorl
is broader and squarish in section; its
ribs are slightly more distant, about 21
per whorl, all equally long and provided
with umbilical bullae. without shorter
intercalated ones. The umbilical bullae
are prorsiradiate and highest at somedistance from the umbilical margin.
The ribs on the main part of the flankare less prorsiradiate than those of thelectotype, and especially so on the lastpart of the whorl. The tubercles are

Breadthcostal

32.8

0.97
1. 08
0.95

21.6

1. 22
1. 09

36

c 40

21.3
19.8

26

19.8
8.3
28.8

21.5
8.4
26. ·I

B./II.

intcrc.

0. 39

0.36

1. 08
1. 01
0.91

also somewhat stronger.
The specimen No. 7181A-4 has thestrongest ornament. The ribs are all
simple, rigid and distant. The tubercles
are also prominent. The costal whorlsection is. accordingly, rather polygonal.
being broadest between the umbilicaltubercles. In the intercostal section thewhorl is subrounded with whorl-heightnot much different from the breadth.
On the inner whorl of this specimen\Vith diameters below 15 mm. the urn·
bilical tubercles are not yet well developed, but the ventrolateral tubercles
are very prominent. The ventral clavi
are narrow and close to the keel in the204

Tatsuro MATSUMOTO

r

J
I
\

5

6

4

'\
\

'

\ I
~I
',!

I
I

I
I

\I
II

I

I
I

fI
/I
_.f/

i
I
\

\

'
2
Fig~.

2-6. Protexaniles bourgeoisi D'(ORBIGJ\"Y).
Whorl-sections of the syntypes. :\o. 7181A-2 to 718\A-5 and No. 7181-6.
A restored part is drawn with a broken line.

young stage. but they are prominent
and aligned at some distance from thekeel on the outer whorl. The keel isfaintly undulated on the outer whorl of
this and preceding specimens as in thelectotype. In this specimen the saddle
between E and L is divided by a comparatively deeper lobule. Otherwise thesuture is essentially of the same pat ternas that of the lectotype.
The specimen No. 7181A-5. which isless perfectly preserved than others.
shows similar whorl-section and ornamentation as the specimen No. 7181A-3.
but has a slightly narrower umbilicus.
The specimen No. 7181-6 has a morecompressed whorl, more flattened flanks
and a narrower umbilicus than the lectotype. The ribs are comparatively
numerous, 'lJ on the outer whorl. lessdistant, and more prorsiradiate, withmore intercalated or branched shorterribs. The tubercles are weaker thanthose of the lectotype and other specimens. The highest point of the umbilical tubercle is closer to the umbilicalmargin.
Remarks
The lectotype of Ammonites bourgeoisi
and illustrated inthis paper, agrees in many respects withthe largest illustrated specimen of Mortoniceras bourgeoisi (o'ORBIGNY) of GROSSOUVRE ( 1894. p. 73, pl. 13. fig. 2, Coli.
11'0RBIGNY. described

LE l\lESLEJ.
GROSSOUVRE (1894) described at length
the change of characters with growth
and also a certain extent of variation.

503.

Ammonites bourgeoisi from France

The same is true for D'ORBIG~XY's original syntypes. As in other well studied
species of Texanitinae. such as Submortonicera s chicoense (TRASK) (MA TSUMOTO. 1959, p. 126, pl. 32. fig. 1 ; pl. 33,
fig. 1 ; pl. 3,1. figs. 1-3 ; figs. 1. 2), there
seem to be a considerable extent ofvariation in the relative size of umbilicus, proportion of whorl-breadth toheight. mode of ribbing, such as strength,
distance and inclination, and strengthof tubercles. It would be reasonable
and natural to regard all the above described syntypes of D'ORBIG:SY as wellas the hypotypes of DE GROSSOUYRE as
representing one. fairly Yariable species,
Protexanites /Jourgeoisi (o'ORHIGNY).
The specimen No. 7181-6 is fairly
similar to the holotype of Protexanites
bontanli DE GROSSOUVRE (1894, p. 77, pl.
17, fig. 2), but is still distinguished by
its wider umbilicus, less compressed
whorl. less flexuous and less crowded
ribs, of which branched or intercalated
ones are fewer, and stronger and morerounded ventrolateral tubercles. In P.
bon/anti the umbilical tubercles are mostelevated at the margin and the umbilicalThis character iswall is overhung.
never seen in any example of P. bourgeOis!. Therefore I would regard thespecimen No. 7181-6 as an example of
P. bourgeoisi, although it may be an
extreme variant.
Through the study of the original
specimens it is noticed that Protexaniles
bourgeoisi (o'ORBIG.:\Yl considerably resembles Subprionocyclus branneri (ANDERSON, 1902) [=Prionotropis cristatum
BILLINGHURST, 1927] (see ]'vlATSUMOTO.
1959. p. 109: rv!ATSUMOTO, 1965, p. 50).
from the Upper Turonian of Englandand probably corresponding stage ofCalifornia and japan, in the whorl-shape,mode of coiling, ribbing and tubercula-

205

tion, as well as in the pattern of suture.
The distinctive difference is in that the
keel is strongly serrate in Subprionocyclus branneri while it is almost entire
in Prolexaniles bourgeoisi. The faintundulation on the keel cf some specimens of the latter may be reminiscentof the strong serration of the former.
In S. branneri the whorl is somewhat
more compressed and the outer and inner ventrolateral tubercles are closer toeach other than in P. bourgeoisi. In thelatter the outer ventrolateral tubercles
are shifted outward. elongated longitudinally, and, thus. can be called theventral clavi. This and the smooth keel
are the characteristic features common
to the members of the Texanitinae.
Anyhow. on the grounds of stratigraphic
occurrence and the morphological resemblance, Protexanites bourgeoisi is judged
to have been derived probably from sucha species as Subprionocyclus branneri.
The lectotype, over 120 mm. in diameter. and DE GROSSOUVRE's largest
specimen. about 150 mm. in diameter,are still septate. Therefore we do notknow exactly the characters of the adultbody-whorl. It is, however. observed inthese and other specimens that the ventrolateral tubercles are relatively more
prominent on the inner whorl of an
earlier growth-stage. In other words it
is little likely that the hypernodosity
occurs on the outer whorl of the present
species.
The faint serration which may beseen on the keel of some specimens of
P. bourgeoisi corresponds to each rib asin the species of Subpnonocyclus. On
the other hand Prionocyclus and Prionocycloceras have minute serrations on
the ,-entral keel which are more num·erous than the ribs.
The serrations
may be apparently obscured on someinternal moulds of outer whorls. A con-Ta suro M.4.TSUMOTO"206-rusion which might occur in such a caseshould not make a reason to unite Pro.texanites. a member of Texanitinae, with
Prionocycloceras, that of Collignoniceratinae (see )V(ATSUMOTO, 1965).
GROSSOUVRE (189-i) mentioned at length
the similarity and distinction between
the present species and Ammonites serratomarginatus REDTE:'\BACHER (1873, p.
llO, pl. 25, fig. 2; GROSSOUVRE, 1894. p.
-69, pl. 16, fig. 1). The latter has twoventrolateral tubercles in addition to
the ventral ones and is the type-species·of Parabevahites COLLIGNON, 1948. The
two species may be parallel derivatives
from a common or closely allied an·cestor.
Heferences Cited
ANDERso:x. F. !VI. (1902): Cretaceous depositsof the Pnciftc Coast. Proc. Calif. Acad.
Sci., [3]. 2. (1), 1-15-!, pis. 1-12.
Bll.l.INGIIURST, S. A. (1927) : On some new
Ammonoidea from the Chalk Rock. Geol.
Mag., 44, 511-513. pl. 16.
-GoLLIGNO~.
:'vlaurice (1948):
Ammonites

neocretad!es du Menabe (Madagascar).
I.-Les Texanitidae. Ann. Geol. Serv.
Mines, Madagascar, 13. •19-107 [1-62]. pis .
7-20 [1-l·IJ; 14, 7-60 [63-116]: 99-101[118-120], pls. 1-18 [1.5-32].
GiwssouvRE, Albert de (189·1): Recherches
sur Ia Craie supericure. 11 Palcontologie.
Les ammonites de Ia Craie superieure.
A/em. Carte Geol. Del. France [1893]. 264
p., 39 pis.
MATSU:>.IoTo, Tatsuro (1955): Evolution of
Peroniceratidae. Trans. Proc. Palaeont.
Soc. japan, [N. S), (18), 37-4-1.
- - (1959): Upper Cretaceous ammonites
of California. Part II. Mem. Fac. Sci ..
Kyushu Univ., I..D:. Geol .. Special Vol. I,
1-172. pis. 1-41.
(1965) : A monograph of the Collignoniceratidae from Hokkaido. Part L
Mem. Fac. Sci., Kyushu Unit' .. [D]. Geol ..
16. (1), 1--80, pis. 1-18.
ORBIGNY, Alcide D' (1850): Prodrome dePateontologie Stratigraphique Universel/edes Animaux Mol/uscues el Rayonnes, 2.
REDTENBACHER, Anton (1873): Die Cephalopodenfauna der Gosauschichtcn in den
nordostlichen AI pen. Abhandl. Ceo/. Reichsanst .. 5. 91-149, pls. 22-30.

Explanation of Plate 26-Fig. 1. Protexa11ites bourgeoisi (o'ORBIG;\!Y).
Lectotype, from Sain~-Frimbault (Sarthc). France, o'ORBJG~Y's Collection No. 7181-A,
M•.1seum National d•Histoire Naturellc, Paris.
Lateral (a) and ventral (b) views.
natural size.

Trans. Proc. Palacont. Soc. japan, ~- S., ~o. 61. pp. 207-214, April 10, 1966

504. THE SIGNIFICANCE OF THE l\IAGNESIU:\1 AND CALCIUMRATIOS OF FOSSIL SHELLS OF UMBONIUM COSTATUM(KIENER) FROM THE DEPOSITS SINCE THE PLIOCENE
IN THE SOUTHERN KANTO REGION. JAPAN*
JOJI NAGASAWA
Institute of Earth Science, Tokyo Gakugei University~~~~D~MW~®~~~~E0U~~®~?*Y~A~~~y~~*~~0-~:<

1962i(O, ~~~~.i£!l~!i:]ff.jl1b!IJ.Ilm~iil>~!lWlliH'Bl~v)3'- CJJ.Itt!M':f:ti:l· ~~.!.IS Ld.: ft;fiCD;r. / ~ ...-Pr fi 1 CD }~i'CM..P ICft-.{4 ~ ~t ·n' Z, -" ':1 t- Y ~A 2. jJ Jv Y ~ ~~JJJFfll{CJJlt (%) ~?ftll~i:: L 1':,..COJ1tflL1ff\':OJji L, \ t,a, IC"?~t.ii'!i.k l /.:$~~i!i-L t.:tJ:, ~[U]~~:!rti~.\I!OJ!i'f'i'TMVJ*~
MOJ-Pr-+t ~0)~11:\tt:"?~ '1': J:f,co)lt~UJJU:::5j-tlfiftgJi:: L t.:*<S!f;:.t ~ (l.:.tt~tal¥:-£-Wt.:$~ c.
~ r:m*-t o c;ttic~trJrc:~~L t.:.ltt!f!";':_tlfl!Jlf:ilSZ>$:;1!rrtt~'-cOJta1-\r~~:lfCD.>t!Wc~m*-lt;lt~ Lt.:.

I.

~~ ff~ (j'(The results of the chemical analys;3of the shells are shown in Table I. fromwhich can be noticed the fluctuations of
the magnesium and calcium ratio during
the Quaternary period in the south
Kanto region. japan.
This fact seems to have some significant relations \Vith the problem of the
Quaternary thermal changes of the sea
water in japan.

Introduction

In 1963-1964, by the chelate-titration
method, the values of the ratios ofmagnesium and calcium, namely theatomic percent ratios between magnesium and calcium, calculated in terms.of the number of atoms were determined in the Recent and fossil shells ofUmbonium cos/alum (KIENER), a gastropod now living at a depth ranging frombelow low tide to 10m in the south
Kanto region of japan.
In this paper are presented the rela·tionships between the magnesium andcalcium ratios, geological horizons. thewater temperatures in which the animal
lived and the importance of the chemical
method for determining or correlating
the horizon or age of the geologicalformation which yielded the univalve
animal.

II.

Acknowledgements

The writer wishes to express his
thanks to Dr. Tatsuo :'vhTSUHASHI, Pro·
fessor of chemistry of the Tokyo Gakugei University for kind guidance in theanalysis of the shells by means of thechelate-titration method and for his encouragement during the course of thisstudy.
He also expresses his thanks to thefollowing persons of the same university,-:\liss Setsuko E:-;oo. Assistant of chemis·• Received November, 9, 1965: read November 7, 1965. at Chiba.

207

.loji N4G.4S.·l TVA

208try. Dr. jisuke SEKI. Professor of chemis·
try, Dr. Ryutaro NAGAI. Professor ofphysics and Dr. Takashi ToRII. Professorof agricultural chemistry. for their kind
helps during the course of this work.
He is also indebted to Professor Dr.
Kotara HATAI of the Institute of Geo·logy and Paleontology. Tohoku Univer·sity for his kindness in reading theoriginal manuscript.
Ill.

Historical Review

In 1922. F. W. CLARKE and W. C.
w·HEELER called attention to that the
proportion of magnesium carbonate in
the shells of crinoids and alcyonarians
is dependent upon temperature.
In 1935. by the analytical invest_iga·tions of shells of the fresh water gastro·
pod Semisulcospira libertina (GOULD). T.
OuYE and T. KATO reported that theiron content in the shells shows local
variations. but it is greater in the waterwith abundant iron than in that with aless amount of it.
In 1952 . .J. L. KULP. K. TUREKIAN and
D. W. BoYD concluded that the primaryfactor determining the SrjCa ratio in ashell is the Sr/Ca ratio of the water inwhich deposition take place.
The second influence upon the ratiois the type of crystal lattice of the cal·cium carbonate.
In 1954, K. E. CHAVE showed by aseries of analysis that the magnesium
content in the calcite skeleton of numerous invertebrates yaries with the tern·
perature of the water in which theanimal lived.
In 1955, from the result of analyticalim·estigations of the shells of the fresh
water gastropod Bulimus manchouricus
iaponicus (PIJ.SBRY) and the marine
gastropod lfaliotis gigantea GMELil'\. T.
MITSUHASHJ presumed that the magne·

sium-calcium ratio in the shells is influ·
enced by the ratio of magnesium ion to
calcium ion in the water habitat.
In 1956. by H.]. M. BOWEN. stated thatthe range of the calcium and magnesium
ratio in Cambrian to Ordovician lime·stone was from 1.6 to 270 and that inyounger carbonate rocks from 3 to 3.6.
In 1956, G. V. CHJLJNGER reported thatthe fossil coral reefs had lower strontium
content than the Recent coral reefs.
In 1962. T. l'viJTSUIIASHI reported asfollows: "The magnesium-calcium ratios
in the shells belonging to Glycymeris yessoensis. from the Pleistocene to Recentof the Boso Peninsula in japan gradually
decrease with ascending age. The de·creasing rate of the ratios are 0.13-0.28
per one hundred thousand years calculated in terms of the number of atoms.
It may therefore be supposed that theratio of magnesium ion to calcium ion
in sea-water became smaller with ascend·
ing age during the above period.
The quantities of conchiolin and pig·
ment extant in fossil shells also decrease
with ascending age.''
These results may provide a methodfor deciding the age of the deposits
yielding the fossil shells and also ofimportance in stratigraphy.
IV.

Water temperature and magnesiumand calcium ratios in the shells of the
Recent marine molluscs, their interrelationships
Considering from the analytical resultsof Dr. T. MJTSUHASHI (1955). the differ·ences of magnesium and calcium ratio
between the shell of Flaliotis gigantea
G:>.tELI:"' (ear-shell) from the San·riku
coast in northeastern japan and the one
from Hachijo Island at about 33'N. lat.,
far south of Tokyo, is 0.1 and the an·.504.

The Signi.ficance of the Magnesium a.nd Calciu·m Ratios

nual mean w·ater temperature between
the above two localities is about s·c.
and further. from the result of thewriter, the difference of magnesium andcalcium ratio between the shell of Umbonium costatum (KIE:-\ERI from the vicinity of Ilakodate, Hokkaido in northern
Japan, and the one from Shibushi Bay.
Kagoshima Prefecture in southern japan
is 0.3 and the annual mean water temperature between the two localities isabout 8' to 9T, which is near to theannual mean water temperature between
the coast of northeastern japan andHachijo Island as mentioned above.
In other words. the value of the difference of the magnesium and calcium
ratio corresponds to the difference of
the annual mean \Vater temperature,that is about 8'C for temperature and0.3 for the ratio in the case of the shellof Umbonium costatum.
This value is rather small. but is still
smaller in the case of Haliotis gigantC'a(0.1).

V.

Outline of the Paleogeography of

the Kanto Region since the Pliocene
To progress the discussions it seems
necessary to give outline of the Paleogeography of the Kanto Region since
the Pliocene.
During the Pliocene. the sea extended
over the eastern part of Kanagawa Prefecture and the larger part of Chiba Prefecture except for some parts of theMiura and Boso Peninsulas. which remained as land.
During the Pleistocene, Paleo-Tokyo
Bay extended oyer the area. from Tokyo
City, the eastern parts of Saitama andKanagawa Prefectures and the southernpart of Ibaragi Prefecture to the northern half of Chiba Prefecture.

209

In the older Holocene, the new shallow
sea covered the area over the marginsof the Boso and Miura Peninsulas andTokyo City to the eastern part of Saitama Prefecture. This is called the Prehistoric-Tokyo Bay.
From the sediments deposited in theseseas, abundant fossil shells have beencollected and among them Umbonium
costatum (KIE?\ER) is dealt with in thispaper.
The interrelation between the geological ages, formations and the magnesium and calcium ratios of Recent
and fossil Umbonium coslatum fromthe south Kanto region, Japan\'1.

The interrelation between the geological ages. formations and the magnesium and nlcium ratio5 of the Recent
and fossil Umbonium CO'itatum \KIENER)
collected from Tokyo Bay and the fossil
sediments in the Boso, lVIiura Peninsulas
and its adjacent area, are shown in
Table I.
Although the values of the magnesiumand calcium ratio of U. costatum measured by the writer and those of Glycymeris yessoensis and others by T. JvlrTSU·
HASH! (1962) from the same shell bed
are slightly different from one another,
this is thought to be due to the differences in the specific characters and toother features.
However, a similar phenomenon isfound between Umbonium and Glyc:ymeris as shown in Table II, in the fluctuations of their magnesium and calcium
ratios during the Quaternary period.
The shell beds listed in Table I arearranged in the order of younger toolder in downward succession.
The Yamamoto shell bed at Yamamoto,_
Takikawa, Tateno-mura, Awa-gun, Chiba

Joji NrlGASA H:4

210

Table I.
Boso Peninsula
GeologicalAge

MgfCa (%).
Localities & Formations I atomic
ratiosI

Hirasaura
Iwai
Tateyama

Recent~Iatsudo

Holocene
'

I

I

I

I
Upper
Part

Pleistocene

I

Omori
Shell Bed
Boyatsu
Shell Bed
Oyaru
Shell Bed
Banba
Shell Bed

I
I

I

1.8

Mg/Ca (%).

I atomic ratios
i
I
i

I

I
I

1.2

II

1.2

I
I

I

I

I
I

I

1.2
1.5

II
I

I

KikunaShell Bed

I
I

1.2

I

I
I

Kiyokawa
Shell Bed
Atebi
Shell Bed
Nishiyatsu Up.
Shell Bed

I

0.8
0.9
0.9

Sanuki Silt
Villafranchian
to Pliocene

Localities &Formations

1.5
1.4
2.3

I

---

Lower
Part

I

!\!iura Peninsula andits adjacent area

1.0-

Yamamoto
Shell Bed

Prefecture may be correlated with the
middle Pliocene and the limuro shell
bed at lnada-noborito. Kawasaki City,
with the Villafranchian or the upper
Pliocene.
The sample from Matsudo was collected at the entrance of the ~Iatsudo
Shrine, that from Kiyokawa, at a cliff
150m southeast of the Kiyokawa Station,that from \Vada, at Wada, Shimomiyata,
Miura City, and those from Omori, at acliff of Omori, lnzei-machi, Chiba-gun,Chiba Prefecture.
Banba is thought to belong to thesame horizon as that of Semata-no-seki.
The Naganuma shell bed belongs to
the so-called Naganuma fourth zone.

Wad a
Shell Bed
Naganuma
Shell Bed

0.9
0.9
-

-

1.2

IimuroShell BedI

1.2

The values of the above ratios wereobtained from one or two specimens
per one fossil bed. In Table II. themolluscan shells subjected to analyses
comprised the following species.
1. Glycymeris vestita (DUNKER) fromthe coast of Kuju-kuri, Chiba Prefecture,
a warm water form now living at thedepth of 10-·10 m in japan.
2. Saxidomus purpura/us (SOWERBY)
from Urayasu-machi. Chiba Prefecture.
It is now living at a depth of about
5 m in japan.
3. Glycymeris yessoensis (SOWERI3Y)
from the vicinity of the Shizu Railway
Station. The shell bed at Shizu is
considered to be equivalent to that of

504.

The Siunificance of the .Ma{Jnesium and Ca.lciurn Ratios

211

Table II. Correlative values of the magnesium and calcium ratios from analysesof shells of different species by MITSUHASIII (1962) and NAGASAWA (1964).
Geological
Age

Localities & Formations- -Recent
Holocene

---

- - -

- -

Cppcr
Part
- -

!

I

i

I Lower

I

I

Part

I

l\Ig/Ca (%), ratiosof Glycymeris.
by MITSUHASHI

1. 4-2.3

2.21

--

- -

Chiba Prefecture-------

Mg/Ca (%). ratiosof U. costa/lllll,
by NAGASAWA-- - -

Chiba Prefecture- - -Pleistocene

I

:

1.2

'

1.2

I

2. o~

- -

Omori Shell Bed
Boyatsu Shell Bed
Oyaru Shell Bed
Banba Shell Bed

I

1.2

I
I

1.2

1. 93
2.0•
1. 9•

1.5

1. 9•

I

i
Ki~•okawa!

Shell Bed
Atebi Shell Bed
I
Nishiyatsu Upper
Shell Bed
Sanuki Silt

Omori.
4. Glycymeris rotunda (DU:\KER: fromthe jizodo Shell Bed. Chibe Prefecture,
which is about equivalent to that ofAtebi. This species inhabits a depth of
40-200 m along the Pacific coast of lionshu, japan.
* Glycymeris yessoensis. This species
inhabits a depth of 40-200 m in northern
japan and is a cold water one.

0.8
0. 9
0.9

1.0

I
I

I
I
I

1. 1*

0. 74

-.

1.1

0. 7•

1.3 from the l'vlatsudo shell bed, respectively. All of these localities are distributed in the area east of Tokyo City.
The relations of the distances between
each of the fossil localities are as follows: Omori, about 13km north of Shizu;
Izumi. about 2.5 km southwest of Omori ;and Matsudo, about 22 km southwest of
Omori.

VIII. The horizon of theVII. The magnesium and calcium ratiosof Fmbonium costalum from the shell
beds of the same geological horizon
The values of the magnesium andcalcium ratios of the fossil Umbo11ium
costatum from various shell beds which
are judged to belong to the same geological horizon in the upper part of the
Narita Formation deposited in the fossil
basin of Paleo-Tokyo Bay show about
the same value, being 1.2 for the Omori
shell bed. 1.2 from the Izumi shell bed,

Kikuna shell bed
The value of the magnesium and calcium ratio of the shells from the Kikuna
shell bed, situated southwest of Tokyo
City, can be correlated with the ones
from the upper part of the Narita Formation in the Boso Peninsula by othermethods. present the same \'alue of 1.3
as already obtained for the shells fromthe eastern localities above mentioned.
Therefore, the horizon of the Kikuna
shell bed must belong to the upper partof the Narita Formation.

]oji iVAGASAWA

212
IX.

The magnesium and calcium ratiosof Fmbonium costatum from thelower part of the Pleistocene formations in the 1\liura and Boso Peninsulas

The values of the magnesium and calcium ratios for the shells from the shell
beds correlated to the lower part of the
Pleistocene formations by both paleontological and stratigraphic data are about
0.9. respectively as known from thatvalues from the shells of the Naganuma
shell bed at Naganuma-machi, Yokohama
City. in the northern border of theMiura Peninsula. from the \Vada shell
bed at Shimomiyata in the southernpart of the l'vliura Peninsula and fromthe shell beds at Kiyokawa, Atebi. Nishi·
yatsu and Sanuki in the Boso Peninsula
as shown in Table I.
Among the above named shell beds,
the Naganuma shell bed has been considered geologically to have been deposited in an independent bay: the PaleoSagami Bay, which was separated fromthe Paleo-Tokyo Bay during the older
stage of the Pleistocene.
The writer is confident that the results
described above give us important evidence for the application of the magnesium and calcium ratio method to thecorrelation of geological formations.
X.

On the fossil shell bedsof unknown horizons

Considering from the results mentioned
above, the Tako shell bed at Watta,
Tako-machi, Chiba Prefecture and theHashirimizu shell bed at a cliff. near
the temple, Enshoji, llashirimizu in theMiura Peninsula. are uncertain as totheir exact horizons.
However, they
may be correlated with any bed or
norizon in the upper part of the Pleisto·

cene formations by reason of their magnesium and calcium ratios. The saidratios of the shells from Tako and Hashirimizu, measured by the writer. were
1.2. 1.2 respectively.
XI.

The existence of an unconformity

is expected from the abrupt change
in the value of the magnesium andcalcium ratio

From Table I. distinct changes can berecognized in the values of the magnesium and calcium ratios between the
Holocene beds, the upper part of the
Pleistocene formations and the lower
part of them. corresponding to the actual
existence of the unconformities between
these three formations as already known
from field evidence.
From the above fact. we may expect
in general the existence of an unconformity by the abrupt change of value ofthat ratio.
XII.

The change of the water temper-

ature during the Pleistocene in thesouth Kanto region assumed from themagnesium and calcium ratio

As already mentioned in earlier lines,
the magnesium and calcium ratio of theshells is considered to be determined not
only by the composition of the water
habitat but also by the temperature.
The ratios of magnesium and calcium
presented by the writer shows that thevalue increased with descending age asshown in Table I.
.\s the magnesium content of the shells
is considered to be proportional, approximately, to the water temperature, if
we assume that in these shells the calcium content (%) was constant, but the504.

The Significance of the .Maynesiutn and Calcium Ratios

magnesium content varied only with thewater temperature since the Pliocene.
then we may conclude, from Table I,
that the water temperature of the Pleistocene must have been lower than that of
the Holocene and Recent and attained
the lowest temperature indicated by 0.8
in the magnesium and calcium ratio
during the depositional period of theYabu Formation and increased graduallywith descending age during the whole
period, but a distinct thermal change
had taken place bet\veen the Holocene
and Pleistocene.

XIII.

Conclusions

1. In order to foreknow or correlate
the horizon and the unconformity within
a single area or a comparatively limitedarea, the application of the magnesiumand calcium method for fossil shells isproved to be effective.
2. By the application of the magnesium and calcium method to fossil shells,
to determine the water temperatures andthe magnesium and calcium contents inthe sea waters during the geologicalperiods seems to be in need of further
considerations and investigations.

213

Literature Cited
CHA\'E, K. E. (195-la): Aspects of the biogeochemistry of magnesium. 1. Calcareous marine organisms. jour. Ceo/ .. vol.
62, pp. 266-283.
- - (1954b) : Aspects of the biogeochcmist ry of magnesium. 2. Calcareous sediments and rocks. jour. Geol., ~·ol. 62,
pp. 587-599.
GoLDBERG. E. D. (1957) : Biogeochemistry of
trace metals. in HEDGPETH, j.W., Treatise
oil Marine Ecology and J'aleontology. vo/.
1, Ecology, Ceo/. Soc. A mer. Mem. 67,
pp. 3-15-358. 1 fig.
:\IJTSL'HASHJ. T. (1955): Chemical components of the shell of llaliotis gigantea
GMELIN. (in japanese). null. Tokyo Gakugei l.init•., t•ol. VI. Ser.: Chemistry & Biology, pp. 125-132.
- - (1962) : The relation between magnesium-calcium ratios in shell fossils andgeologic age. (in Japanese). jour. japan.
Chem. Soc., 110/. 83. no. 2, pp. 123-127.
Ov\'", T. and IC\To. T. (1935): Local variation in the quantity of iron in the shellof Semisulcospira tiber/ina (GouLD). (inJapanese). japan. jour. Mal .. The \'enus.
1'01. v. 110. 5, pp. 278-284.
RE\'ELLE. R. and FAIRBHIDGE, R (1957): Carbonates and carbon dioxide, in HEDGPETH.
]. W., Treatise on .\Jarine Ecology andPaleontolog)'· vo/. 1. Ecology, Ceo/. Soc.
Amer .. •Hem. 67. pp. 239-296. 8 figs.

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El~
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lnzei-machi
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lwai
Kanto Region
KawasakiKagoshima
Kanagawa
KikunaKiyokawa
MatsudoMiura Peninsula
Narila Formation
Naganuma
Nishiyatsu

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Semata-no-scl< iShibushi Bay
Shizu
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Shinagawa

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PROCEEDINGS OF THE PALAEONTOLOGICAL SOCIETY
OF JAPAN

n*tJ'=E%l'¥:~~9l@lfftJitt>J::i:J r»rr~7:/7Jk.O:t~•ilf:JI.!O)J!i~:t!!Jcl11!~J 1:::~-t 7.> y Y lf.;:; r; A

li 1965 if 11 fJ 6-7 El (±. R) =f-~:k~{:Y,:Jil!·'J:$t> .~:. a'&l¥lf.$1::to ~ ''LmH!ll¢ ;i1. 1"91~:f't1JillitJ,.;O)t(9jct~jtfp~.t\IJICJ:: !J !flH~t!l!l<::~7 Lt.: (~.1JJ1~<~~n~~NAE· ~?77-e~mO)~~•
rc:-:>P'L .... :u:tt~- ~m~~ · rfJJJiil!f-~79 45) 0·

On some interesting Mesozoic plant remains
from the lloshiro Subgroup ........... .
. .. .. .. .. ..
. ........ Tatsuaki KI~lt:RA;ltttuitt:O~*It~fi'i!f1JJ{t:O 2 jff!l!l:: "? ~ '"'[ ..... .

.................................. !Jltlff.~if!
f·.~~lj!..ti 7-lllO);f'iJLSJ, {t :6 :J:fl........ Yasuo NoGA'-11 and Ken'ichi Ism!J -1 Jl.rJ~ 7 .y-O)J:$t'i~l:.tt~!Hm .... .!fiJ:ri!7<:
Some younger Mesozoic plants from Malaya. . . . . . . . . . . . . . . . . . . . . . . . . . . . Enzo KoNNO~ v- Y 1 0) Kelantan, Pahang ffil:il L ~c ~O)rnJJlli.s\lC-:>~''L · · · · · ·· · · · · · · · · · · · · · ·.. · · · · .tiffitJ !tShell structure of Japanese smaller Foraminifera. Pt. 4 .............. Hiroshi UJIIE;ltJ:Ilt.ll!!ffl$~fJlJii'SJiiliff.i!I 0) .tti~.!P.{t1:i IC"?~''L . · · · · · · · · · · · · · · .. · · · · -lll!ilWlit · =f-.!filitZ.
Upper Permian Fusulinids from Taishaku
Limestone Plateau, West Japan (1"\~f,;). , Kimiyoshi SADA and Tsuruo YoKoYAl\IA
Ordovician and Silurian conodonts from
Malaya .. Ilisayoshi leo and Toshio KoiKE
Discovery of Upper Triassic conodontsfrom Malaya.................... .

Notes on the 1\Iyophorian Sandstones in
Malaya ............................... .
Teiichi KoBAYASIII and Minoru TA~lURA
Some Myophorella from the Tetori Groupin the Arimine District. Central japan. ... Shiro MAEDA and Tetsuya KAWABE
R~IJ,~ 9lf<-:W!il;itf'iflll!i;~~::k~ :t- ' 7 W1t:Gc

JilffrJ ft:ti .......................... ;kiR~~~~WO)Uifm~M0~~~0)~8~0)~?*Y •7 A C ;fJ ;t-y '7 A-;'):;ff!tO)A~:'* · · · ·7kiR~lX

Notes on Ammonites bourgeoisi o'0RBIG!'\Y
from the Upper Cretaceous of France(ft~'1't) .............. Tatsuro MATSli'-IOTO
Yabeiceras t.:.{l;I."Cil~tJ:7.>7/-r-T1 1- (f\:~)........................... ·· ·· · · -f'~*iiM
An Acanthoceratid ammonite from Sakha·
lin ................................... .
Tatsuro .MATSU.\IOTO and Ikuwo 0DATA-r 7. -r A <f-;v;7.1£iO)if!Ut .............. 1Jl1rdl~7<:215(://:f,y~A)

rJiiWiY ::/ 7' lk.G~<plll:JltCI)o1 i'lJ1JJc.tllHl!J~ EJ-+:oooJ/Il!Jl ....................... t~alllf

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li1;Q)Jt!!~IC:-:::>t,-c ..

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........ t'}tfi'/.-· · 1..\Wil-~J... . {.\Wil-9']

J 111<1""- _,....,. -:f :.-- 0)=1ll:*Dh!:i!JWit:?'iWaagcnophyllid corals from Thailand ....
... ·...................... Rucha Ingavat
Rat Buri :OK1"l0UiM.!Rft:fiJ,jl' ('H!D ..... .
.. · .. · · · · · · · .~LlJJ:itC::. · WJ*!!t fHII(,; · !~PHI;tf­~··~~~K~~~/-'f-7~0)~~-ft...

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1 /' ~-" :.t·o/7"0):tJiflli*i11:cii'i.~~1t .. 1"lt£=:.1l!S:11 7 ::-' 7JIIHHC:bP"LJ:flt0i!ctJ~;{J'.JL!h{t:0.............................. Jd~~f'~f!jlji,. A., ~-" A0~tm --tui:J:t~=. n*r.'IJ. ~t~~mi%
J 1 · ""'7 ""'iJ>i? EL<J;:i L'0f8tiiii111Vf~Q)Nfjf·,r."]]:~~'.L4m"¥:~.t~.~-JlHiffo/t! .............. ·H%~1::1*15"1:!JW"¥'* 1966

if:IJH~'* .t.; ~ vx '.Jo ~ :;~. Hl66'.J: 1 FJ 24-25 R (~. !1<) W:~t:k'-J:Jll!·:f:fffHtll~~~i''i:¥JJ·.:r=rr~~~.iit~ !c :S t,
flli ~ft. IJ.\1 ~~ nii'iitJ. i?
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On the Hamamclidaceae from the Paleogene of Hokkaido, Japan (ftiO't) ........
........................ Toshimasa T ANAl
¥1fo1JIIJ:ili(.m7i'tiC~HiiLt.: Taeniopteris IC:-:::>ryz:- · · · .... · · ........ -t.U~~n · ;A::ft-;ktlJ(/!j~L'ft5t~Ht.:li:k Sphenophyllum IC-:::>
PL: . .. . . . . .. .. .. .. ..
. ... ·l:lWH-!t.!
JIJ~-*'lth I:.~I«Jllfltn·i~ltJ· i? (}):fifl!R ftE:ll:fiC-:Jt'L:' · .......................... -~;;f;:jj'Uf(jLepidolina fl~lli'iflllil'! .................. j;;$_N:R;
illlk~Af'J.i1 :1i .=. Geryon itb ....... -4-~J.J~
Triassic insect fossils from Omine, Japan. ....................... Ienori FUJIYAMA
l\otc on Apiotrigonia from the Futaba
Formation in the Joban district, North
Japan .................... Shiro 1-.lAEDA,
Haruo TAzvt..:E and Tetsuya KAWABE
On some Pterotrigonia from the Todai
Formation in the Akaishi Mountains,
Central Japan ......................... .
. . Shiro MAEDA and Tatcharu KtTAJI.IURA
l'aldedorse/la from the Miyako Group(Studies of the Cretaceous ammonites
from the Miyako Group. Pt. 1) ....... .
· · · · · · · · · · · · · · · · · · · · · ....... lkuwo 0BATA
Notes on Ammonites flaccidicosta Ro!'>IER
from the Cretaceous of Texas ....... .
· · · ·. · · · · · ..... · .... Tatsuro MATSUMOTO
A Mesozoic ammonite from Amami-Oshima.................... Tatsuro MATSMOTO,
Hidco bl!IKAWA and Shiro YAMAGUCIII

216
News
@

!n 231fil International Geological Congress 111968 ~ 8 rl 19 8 .t!) 28 Ll ~ -r. Prague cffiHlii~~t~, ilf~O.) First Circular KJ:::hlilti~F.!Ii!JIC~M':it t. -1! -7 ;,- u :/ IC(;!:;?.:O.),t ") t.£. b O)fJIGI; ~ oGenesis and classification of sedimentary rocks: Stratigraphy of Central European Lower
Palaeozoic and its correlation with other area; Tertiary/Quaternary boundary; Originof coal and problems of its deposition.
~~~.:~-rz. !m B--tt9G ~ l:i

The Secretary-General. x::III Session, International Geological Congress
Ustfedni ustav geologicky, Malostranske nam. 19, Prague 1. Czechoslovakia
IJl_ib]j.!;!: 1966 !f<l }';} 30 fl ic. t,:~. First Circular l:i"f:~!~~~c;fi-FOJ~mtJtGI;7.><D<:::ffl'ii!~lico@::V..~.$i6L.:.
13*W~~:1J$J~!::"?~'-riliilf!.IC~IIJJ Lt.:"':/ 7 v ·y 1- ;!)\~fi;.HLt.:" :ffl){H''flirtl~IU~tj6,Yyi;[A.f-<:~ {) 0*Jj(-~ff':IB!K1Jl!IB-·Ym 1 (J) I

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International Sedimentological Congress tl: 1967 {I: 8);! 11 LJJ:IJ 15 l.lit:*(;!iJO.)
Reading .&w~ Edinburgh t:IJIHi~;:t ~t7.> o~.iiKI}.!l"t 7.> f.tlo't-it:lt 3 li
Secretariat, VII International Sedimentological Congress, Sedimentary Research Laboratory. Department of Geology, The University. Whiteknights Park. Reading, England.
~ 6 [!i] International Congress of Carboniferous Stratigraphy and Geology (;t 1967 ~ 9
11 1-J .t IJ 16 0 i c~Q<IOJ Sheffield <:!JWrffi;5 ;11 ~ oFirst Circular IC.tZ, c;;$:~,1lfL'Ii::ti/:R*COJ)fllfl£?: · i.li 1l!J'fu·:[: · ;f5:fio!f:cl1Hvi# · ttl!ft"f: · !t.Jtl.lt!!
W~tJ ciJ!;il-it 01.t Bristol-Mendip area, Southwest England. J¥j., .X.- Jv A Pennines. ;;r.. ::1 '7
t- 7:/ reD Midland Valley tJ c<Dfil.:k-*OJ~f{R;Oi,lhllii¢~t-c~'t>o ill!*'l':1t~lir~Cc;jjJ.io
The Secretary-General. 6th International Congress of Carboniferous Stratigraphy andGeological Survey of Great Britain. Ring Road Halton. Leeds 15, England.
*~~3tlliill!li!lm~ lli5' P~ilJ~~:a 1:1 .1>:lkvi!IlfljJ/f.O)ifTj1Jtl!i!l.!J~.JJn jl;O) 1 (Palaeontological Societyof Japan. Special Papers, no. 11. The Echinoid Fauna from Japan and Adjacent Regions,
Part 1) iJ: 2 J] 20 EllCillmi ~ Ht:. 2'!.7 J,'i 18 !'!l!ll!li"l?~Hili (J2StH: ~t;) i! 5000 flJ (lEI 1_,;-f..:'.Jo'fJ!<::Ii!g)rJ~il)7.>o~@~H.Ei::*'Rt.tl;t;$:'r~ 2 J:J _l·.'n.JJ:!)~

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