Transactions and Proceedingsof thePalaeontological Society of Japan
New Series

No. 87

Palaeontological Society of Japan
September 30, 1972

Editor: Takashi HAMADA
Associate editor: Yasuhide IWASAKI

Officers for 1971 -1972
President: · Tokio SHIKAMA
Councillors (* Executives):

Kiyoshi ASANO*, Kiyotaka CHINZEI*, Takashi HAMADA*,

Tetsuro HANAI*, Kotora HATAI, Itaru HAYAMI, Koichiro IcHIKAWA, Taro
KANAYA, Kametoshi KANMERA, Tamio KOTAKA, Tatsuro MATSUMOTO*, Hiroshi
OZAKI*, Tokio SHIKAMA *, Fuyuji TAKA!*, Yokichi TAKA YANAGISecretaries:

W ataru HASHIMOTO, Saburo KANNOExecutive Committee
General Affairs:
Membership:
Finance:

Tetsuro HANAI, Naoaki AOKI

Kiyotaka CHINZEI, Toshio KOIKE

Fuyuji T AKAI, Hisayoshi !GoPlanning : Hiroshi OZAKI, Kazuo ASAMA
Publications
Transactions : Takashi HAMADA, Y asuhide IwASAKISpecial Papers:" Fossils":

Tatsuro MATSUMOTO, Tomowo OzAWA

Kiyoshi ASANO, Toshiaki TAKAYAMA

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Trans. Proc. Palaeont. Soc. Japan; N.S., No. 87, pp. 377-394, pl. 47, September 30, 1972

601.

TWO SMALL DESMOCERATID AMMONITES FROM HOKKAIDO(STUDIES OF THE CRETACEOUS AMMONITES FROM HOKKAIDOAND SAGHALIEN-XXIV)*TATSURO MATSUMOTO!), TATSUO MURAMOT0 2>
and AKITOSHI INOMN>~l::.ffljitffti:-T:A.:c-e 7 :Af31.'H~~7 :..-'.:C-;1-1 ~ 2 f!fi:~-t'O) 1 fi~~}]IJ!I!!)JJ3.!1E.;'f-O)r$-e /=- 7 :..-'0) Mantelliceras japonicum 1\'.'17• t?:>iit L. t: "b 0)'"(', Wfr~Wfrm! C. VC:::.. :::.lr.ilcl!lXT .Qo:::.. hvinl<:f*~O)fE:Q~ 2 em JE.l?:>fO)'J''!!'t',.Qo~~ilfilr.li~am77~f'I C. k

C.?J:v'o

JLI:l~v'ijWiWTrilfi~ "b t:,, mi»EEIB~Jl!:Q~y L. fh LV'~~lifT U~v' < v~~'Li7~mltt,gl]".)lr.lJ.gU.) l?:>~'L.Q o ~-8-~.~lii7'tJ: f) lJ!*-4ifl:: L. LV' .Q:Q~, fimf*~~i3"JICiJi! .Q C. 7':7. .:C -e 7 :A O)~!j't"C:· £> .Q o :!9J~fi-:l: .Q:::..
"'o ;:.0)~? tJ:!I;t~~~~ff-T'l'J!!O)tO)fi 7 :..-'.:C-;1-1 ~ 0))1fdl::'ii:'.J:v'ov'~:dJ::f.;J.fc.iE)J!i7'!?:> -t":tLf.:,HJ':t1( C. L. L~glib t?:>tL.Q o fl!!f1UC. Fol~iJ~-t'O)iJ1iJZ!~iLU~ .iE1i1iHciJi!tLf, Ji!Jif J:::r:i!!!m
~I%:Ji!.v't.:~~'LLv'.Qo ;::O)"bO)fitcfi!Ji0)7:A.:C-e7:Aill!:fJI.O) .;( /'/~-lr.li::.A:L, £>-:1: fJi!
9E'l:"tJ:v'1:.ffitJtr.\':~"b"" Lv'f.:O)'t'vitl:v'i7'ctiH~~tL.Qo
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l'illC. l..Lilc!ll\1-t'.Qo 7"Y"Y7.i!E.f-'Hcli ;kJ!!O)"bO):Q~~ < ~nl?:>:tLLv'.Qi7~. U'LiiJil<:f*~O)jj[f~;>7~fli7> 3 em ij!J.!t't'.:li;,.Q C. C. "biC, -t'O)~Q*~ICj!jj~tJ:Jfii;£>.Q:::.. C.:Q;~~'"(:"Ji;,.Qo -t'O):*Jil<:~~li K. (N.) ishikawai 0)-t'~'LC.~f.C),i'.Q:Qt, JfO)~~O)iJjj;!~ii;T't'lr.~~.lOI?:>h, JiX:
f*~'l:"liAJHi.lr.~tJ: .Qo :::.nlr.~iili L. L, '/"" 7 ~ 7 :..-'.:C-;1- 1 ~ 't'llftllii£~~0)~{7~ UHR~
hLv' .Qt~-fr C. O);f:DW:>7t:5(tfj·:Q,~'L.Q OYt". 7"v'"Y7!llil'-'HC.t;lt .Q llf:!Hi~~O) RJfiEiif:.lc '? ~­r.G~~iL.t::Qt, ~litl'L.0~~13"J't'£>.Qo Jls:!llif-'[0)7 /'.:C-;1-1 r li, -%"i0)~0)~-fr~-~~"b-::>Lv'.Qnt, ;k~~. ~O)~ftffiC.<Ir.{±EJ:}O)~ft[fj, ~I=!O)j1~tJ:ciC.Bv'L, i.PtJ:fJO)M;n
f1~~To *fll!li-t" :j L.f.:rJ11::~/iO)-J'ijffi~ff,T~{?IjC.7;1.fJ:~~1,Qo~*;~f.!r;.mra,AJ1f:il::for one of them, belonging to the subfamily Desmoceratinae, is T. MATSUMOTO and T. MURAMOTO and that forthe other, belonging to the subfamily
Puzosiinae, is T. MATSUMOTO and A.
!NOMA.
Before going further we thank Dr.
Itaru HAYAMI, Miss Yuko WADA andMiss Seiko HAY AKA w A in their kindassistance in preparing the plates andtypescript. For the study of the second
species we thank the Japan Petroleum
Exploration Company and Professor Wataru HASHIMOTO for their kind support.

Introduction

In this paper descriptions and remarks
are given on two small, peculiar ammonite species which are assignable to thefamily Desmoceratidae. The authorship* Received Jan. 23, 1972; read Jan. 20, 1972
at Chiba.
1) Department of Geology, Kyushu University, Fukuoka 812.
2) Yayoi, Mikasa, Hokkaido 068-22.
3) Japan Petroleum Exploration Co., Otemachi, Tokyo 100.

377

378

Tatsuro MATSUMOTO, Tatsuo MURAMOTO & Akitoshi !NOMA
Systematic description

Family Desmoceratidae
Subfamily Desmoceratinae*
Several years ago when we were concentrated in a field work to obtain fossils
from the Cenomanian of the Ikushumbets area, central Hokkaido, one of us(T. MURAMOTO) was successful to find
four small, peculiar ammonite specimens.
They show very distinctive characters of
one and the same species, which requires
a new genus in the Desmoceratinae.
Genus llficrodesmoceras MATSUMOTO
and MURAMOTO, nov.
Type-species.- Microdesmoceras tetragonum sp. nov., to be described below.
Generic diagnosis.- A small desmoceratid, with somewhat simplified pattern ofsutural elements, showing a broad andtrifid lateral lobe (L) and somewhat phylloid terminals of saddles aligned on adescending line.
Coiling of moderate involution; slightly deviated from normal spire in thelast whorl. The body-whorl and thepreceding part of the late, septate whorl
characterized by somewhat tetragonal
outline in cross-section. The surface ofthe shell nearly smooth, only with flexuous weak lirae, which show a moderately projected ct~rve on the venter andanother on the middle part of the flank.
Gently sigmoid, periodic constrictions
marked on the internal mould of latewhorls, but not accompanied with aperceptible elevation on the surface ofthe shell.
Remarks.-This genus is at present
represented by only a single species* The authorship of the description undersubfamily Desmoceratinae is Tatsuro MATsuMOTO and Tatsuo MURAMOTO.

from the Lower Cenomanian of Hokkaido. Its comparisons· and affinities withother genera are to be given after thedescription of the species.
Microdesmoceras tetragonum MATSUMOTO and MURAMOTO, sp. nov.
Pl. 47, Figs. 1-4; Text-figs. 1-4

Material.-Holotype, GK. H5653, fromloc. Ik 1101, Kami-Katsurazawa, Ikushumbets. Three paratypes, of which one
from loc. Ik 1101 and another from Ik
1051b are preserved in the MuRAMOTO
Museum and the last from loc. Ik 1067bp
is in Kyushu University (GK.) with register number H5650. The last one has
been cut into two main parts and a few
minute pieces (of the first whorl) to examine the characters of the inner whorls.
Specific characters.-The shell is small.
The holotype, which is regarded as representing an adult stage, is 18 mm inc

Text-fig. 1. Microdesmoceras tetragonum
sp. nov. Diagrammatic sketch of the halotype in two lateral and an apertural views(above). A part of the !irate surface (left)
and constriction on the internal mould(center) are shown. The external part ofthe second last suture (below) exposed ats. u.s. =umbilical seam; u.sh. =umbilicalshoulder.
·(T. MAT. delin.)

601.

E

c

U2

Two small desmocemtid ammonites

U3

U.Jh.

379

U4= 5

t.!.S',

Text-fig. 2. Microdesmoceras tetragonum
sp. nov. Diagrammatic sketch of a para·
type, from Joe. Ik 1101, in lateral andapertural views (above) and the suture
exposed at s.
(T. MAT. delin.)diameter. The involution is moderate
and the umbilicus is of moderate width,about 34(±1) percent of the shell diameter. The mode of coiling of the adultwhorl, as seen in the holotype, is slightly
deviated from the normal spire, i.e.
slightly scaphitoid.
The body-whorl occupies about threequarters of the last volution. It is· nearlyas high as broad and approximately
tetragonal in cross-section, having flatand parallel flanks, a broadly arched
venter and vertical umbilical walls. The
preceding septate part of at least a half
volution has also flat and parallel flanks
but is somewhat broader than high. Still
inner whorls are much broader than highand rounded to reniform in cross-section.
They are more evolute than the outerwhorls. The above mentioned change ofshell-form with growth may be illus·
trated by a cross-section (Text-fig. 4).
The surface of the shell looks nearlysmooth, having only weak lirae. As far
as the observed outer whorls (of 10 to
20 mm in diameter) are concerned, thelirae show a sigmoid curvature, running
fairly strongly forward from the umbilical edge to the mid-flank, curved somewhat backward on the outer half of the

Text-fig. 3. Microdesmoceras tetragonum
sp. nov. Diagrammatic sketch of a paratype, from Joe. Ik 105lb, in lateral andapertural views (above) and the externalpart of the last suture exposed at s.
(T. MAT. delin.)flank and then recurved at the ventrolateral part passing to a moderate ventral projection. The lateral and theventral projections are rounded. The
outline of the apertural margin is notprecisely known.
There are three or four constrictions
per whorl in the late growth-stages.
They are roughly sigmoid on the flankbut not so much projected as the liraeon the venter. They are impressed only
on the internal mould and the corn~s­
ponding elevations on the test are
hardly discernible. The constrictions of
the body-whorl is very faint on theflanks but better marked on the venter.
Generally speaking the suture is ofdesmoceratid type, but is particular inits more simple pattern as comparedwith those of the nearly contemporary
Desmoceras (Pseudouhligella) and Puzosia.
The external suture of the last whorl(at the whorl height of 4 or 5 mm) is
characterized by a somewhat narrowed
stem of the external lobe, asymmetricallydivided first lateral saddle, broad andtrifid first lateral lobe (L), which is situated on the ventrolateral shoulder, much

380

Tatsuro MATSUMOTO, Tatsuo MURAMOTO & Akitoshi !NOMA

Measurements.Specimen

DiameterUmbilicus

HeightBreadthB./H.

GK. H5653
Paratype from
Ik 1101
Paratype from
Ik 1051b
GK. H5650

18. 0(1)9. 8(1)

6. 2(. 34)
3. 3(. 33)

6. 0(. 33)
4. 0(. 41)

6. 0(. 33)
4. 0(. 41)

1.0
1.0

11. 2(1)

3. 8(. 34)

4. 2(. 37)

4. 2(. 37)

1.0

12. 5(1)4. 4(. 35)

4. 8(. 38)

5.1(. 41)

1.0

smaller and narrower second lateral lobe
(U2) and gradually descending auxiliaries. Minor incisions are less numerous
and shallower than in the typical Desmoceras or Puzosia and each of the saddles
and folioles show a rather entire outline,
resulting in a· somewhat phylloid aspectin the sutural pattern.
The development of the suture withgrowth has not been completely traced,because of unfavourable state of preservation. So far as the observation on theavailable material is concerned, the formula is probably E, L, U2 , U3 , U4 =S,
ulV• uld, I, but could be interpreted
otherwise. The saddle between E and
L is bipartite in early stages (from acertain stage of the second whorl) andthen modified in late stages, normally bysubdivision of the larger dorsal branch.
The protoconch is comparatively large
as in other examined examples of thedesmoceratids.
Remarks.-The holotype and the thirdparatype (GK. H5650) are regarded as
representing an adult shell, because thelast two septa are approximated andbecause the last whorl presents a particular shape as compared with earlier
whorls.
The variation in shell-form between
individuals seems to be little, as is indicated by the above measurements, but
the number of the examined specimens
is by no means· enough to lead a conclusion. There is some extent of differ-ence in the details of the suture, suchas the mode of subdivision of the firstlateral saddle, even among the four specimens, although the fundamental pattern of the suture is the same.
Comparison.-At first sight this species
looks like a certain species of Tetragonites
in shell-form, but it is not related with
the Tetragonitidae, because its suture isfundamentally different from those of
the Tetragonitidae. In the latter the firstlateral saddle is tripartite, the laterallobes [L and U 2] are bipartite and theinternal lobe forms a septal lobe [Is].
In its simplicity of suture (or betterto say simplified suture), small size andsmooth shell the present species reminds
us of such species as Flickia simplex
PERVINQUIERE, 1907, but it differs fromthem by its rather desmoceratid basic
pattern of sutures, different shell-form
and the existence of constrictions. Certainly it has no affinity with the Flickiidae which, in turn, are apparently related. to Mojsisoviczia or Falloticeras of
the Brancoceratidae (see WRIGHT, 1957,
p. L409), hence provisionally placed in
the Acanthocerataceae.
On account of its phylloid aspect ofsutures, smooth shell with sigmoid lirae ·and more or less evolute whorls, thisspecies is apparently similar to certain
early representatives of the Phyllocerataceae, such as Eopsilocems planorboides(GUMBEL) (see WIEDMANN, . 1970) andW opji.ngites krystyni WIEDMANN, 1970,

601.

Two small desmoceratid ammonites

381,/,...--- .....

II

' \

I

I

I

I

)

\

pr.

5

O.Smm
....---...<

30

U3

U2

L

E

.~2°
u.s.
O.Smm

,.····-I

Ul

U2

E

Text-fig. 4. Microdesmoceras tetragonum MATSUMOTO and MuRAMOTO, sp. nov.
Diagrammatic illustration of a paratype, GK. H5650, showing growth of whorls incross-section and lateral view (above) and also that of sutures (below). pr= protoconch, !•=the first whorl, z·=the second whorl, 3•=the third whorl, 4•=the fourth
whorl, b=early part of the body-whorl [living-chamber]- s=the last second suture.
A concealed but presumed part of a suture is drawn with a broken line, with theaid of the observed feature in cross-section.
(T. MAT. delin.)from the Upper Triassic of Europe. The
similarity is regarded again as homeomorphy, because it has no lituid internallobe of the phylloceratacean type andbecause its geological age is much sepa·
rated from them.
This species is somewhat allied toDesmoceras (Pseudouhligella) japonicum

382

Tatsuro MATSUMOTO, Tatsuo MURAMOTO & Akitoshi !NOMAY ABE (see MATSUMOTO, 1954a), from the
Cenomanian of the northern Pacific region, in the flattened flanks, perpendicular walls and sigmoidal constrictions ofan adult shell, although the shell of thelatter species is more compressed, much
more involute and about six times aslarge as the former in diameter. The
suture of the former resembles that of
an immature shell of the latter (seeMATSUMOTO, 1954, text-fig. 6 [52]), in
the general pattern and probably also inthe mode of development with growth,
although much broader L and more simple, phylloid outline of the saddles arecharacteristic of the former. D. (P.) japonicum and other species of Desmoceras
have more finely and deeply incised,complex sutures in late growth-stages.
The present species resembles certain
species of Puzosia [e.g. P. mayoriana(n'ORBIGNY)] in the degree of involution,
width of umbilicus and sigmoid constrictions. The suture of immature Puzosia
or its allies (see SCHINDEWOLF, 1966,
text-figs. 373-377) is fairly similar to thatof the present species, but the former ismore incised and the auxiliaries arestrongly descending* even if the shellsof the same size are compared. Speciesof Puzosia have generally more distinctly
marked constriction and numerous ribs.
They are evidently larger than the present species in the adult stage.
Occurrence.- The holotype and a paratype came from Joe. Ik 1101 and anotherparatype from Joe. Ik 1051b on the northern wall of the V -shaped valley of thelkushumbets (see MATSUMOTO et al.,1969, text-fig. 9). They were containedin calcareous nodules from the lower
part of unit lib, Mikasa Formation. The* This character is not well shown in
SctiiNDE\\'OLF's text-figs. See MATSUMOTO,
1954b, text-figs. 2-4 for this point.

bed belongs to the zone of Mantelliceras
japonicum, Lower. Cenomanian. The thirdparatype was found in a rolled calcareous nodule collected at Joe. lk 1067bp,
which was probably derived from thesame zone exposed on the southern wallof the Shimo-ichino-sawa [locally called
Tori-sawa], a tributary of the Ikushumbetsu near an electric power station,
because Zelandites injiatus, Hypoturilites
sp. and Eogunnarites sp., among manyother mollusks, were found in the same
nodule.
Discussions.-On the basis of the preceding description it can be concluded
that the genus 1\1icrodesmoceras, as represented by M. tetragonum, should be
ascribed to the family Desmoceratidae.
M. tetragonum is, however, so peculiarthat it is not directly connected withany known species of the Desmoceratidae. In other words the origin of thespecies is obscure.
Microdesmoceras is not so closely connected with main representatives of the
Desmoceratinae or those of the Puzosiinae that it could possibly be accomodated
in a new subfamily. However, we still
hesitate to propose a new subfamily
name, because we have not yet discovered any descendants or relatives which
could be closely grouped with Microdesmoceras under the same subfamily. It
is indeed a particular offshoot of the
Desmoceratidae, in view of its small size,
simplified suture, less prominent constrictions and tetragonal, smooth, slightly scaphitoid outer whorl. For the time
being we have to assign it to either the
subfamily Puzosiinae or to the subfamily
Desmoceratinae. Someone might prefer
the former assignement on account of
its less involute coiling, but we are rather
inclined to the latter assignement, thoughprovisionally, on the grounds of the pattern of its suture.

.(iO 1.

Two small desmoceratid ammonites

It is interesting to see the appearanceof peculiar micromorphic offshoots in theevolutional history of various branchesof the Ammonoidea. The Upper Albian
to Cenomanian Flickiidae, which are provisionally ascribed to the Acanthocerataceae (see WRIGHT, 1957, p. L409), aregood examples. Lower Cenomanian genus
Neosaynoceras, which is included at present in the family Acanthoceratidae may
be another minor example which considerably deviates from the principal generaof the family in many characters. Microdesmoceras can be taken as another example of a special, dwarfish derivative
which appeared in the course of theevolutional history of the Cretaceous
great family Desmoceratidae.
Aside from the Cretaceous examples,
Cymbites and Paracymbites in the Arietitidae, Protocymbites in the Psiloceratidae
and Metacymbites in the Liparoceratidae,
Primelites and Diaphorites, provisional
members of the Eoderoceratidae, andOecoptychius and Protophites in the Stephanocerataceae are examples of peculiar
dwarfs or degenerated, simplified (orspecialized) derivatives in several families or superfamilies of Jurassic ammonites (see ARKELL, 1957, p. L240, L248,
L296).
The origin of this kind of ammonites
is more or less obscure and they areoften called cryptogenic. In other words
the peculiar character appeared seemingly suddenly, with little evidence ofintermediate forms. Why this is so is
one of the problems of evolution inpalaeontology. How were the habitats
or ecological conditions of these ammonites may be another problem to beworked out in the future. We generally
presume that they may have been lessaggressive animals.

383

Subfamily Puzosiinae*
The subfamily Puzosiinae include many
species which have a large shell. A giant
example, which is more than a meter inshell-diameter, was reported by MILLER
and YouNGQUIST (1946) from the Senonian of Montana under the specific nameof Parapuzosia bradyi. A specimen of
Pachydesmoceras denisoni (STOLICZKA)(1865, pl. 66a), GSI. No. 208, which one ofus (T.M.) examined in the Museum of theGeological Survey of India, Calcutta, isnearly as large as 100 em in diameter at
the middle of the coarsely ribbed bodywhorl. The holotype of Lytodiscoides
conduciaensis (CHOFFAT, 1903) and thatof L. [ =" Achileoceras "] erasmusi (vAN
HOEPEN, 1951), which have magnificently
ornate body-whorl, are likewise large.
In the Cretaceous deposits of Hokkaido
and Saghalien large ammonites are notinfrequently found at various stratigraphic levels. Some of them certainly
belong to the subfamily Puzosiinae. Thus
an example of Mesopuzosia sp., whichcame from the Upper Turonian (upper
most part of the Mikasa Sandstone) of
the Yubari area, now exhibited in the
National Science Museum, and two otherexamples of Pachydesmoceras cf. pachydiscoide MATSUMOTO, from the Turonian
Saku Formation of the Saku area, oneof which was presented to the Akiyoshidai Science Museum (from T.M.) and theother in the possession of Kyushu University (T.M. Coll.), are about 70 to 80 em
in diameter. They are, however, nearly
wholly septate and, accordingly rriust
have exceeded a meter, if their bodywhorls were completely preserved. Asidefrom these giant examples, we see more

* The authorship of the description under
the subfamily Puzosiinae is Tatsuro MATSUMOTO and Akitoshi !NOMA.

384

Tatsuro MATSUMOTO, Tatsuo MURAMOTO & Akitoshi [NOMAfrequently pu:~;osiine arnmop.ites of about
30 to 40 em in diameter.
In contrast to the above mentioned
large ammonites of the Puzosiinae there
are very small specimens which represent a species of the !)ame family. They
were collected by one of us (A.I.) fromthe Upper Cretaceous of the Haboro area,
northwest Hokkaido, preliminarily studied by A. !NOMA, then sent to T. MATSUMOTO of Kyushu University for further study and now preserved in the
Type-Specimen Room, Department of
Geology, Kyu::;hu University. They are
assigned to a new species of Kitchinites
described below, with some discussions.
Genus Kitchinites SPATH, 1922
Subgenus Neopuzosia MATSUMOTO, 1954
Type-species.-Kitchinites (Neopuzosia)
japonicus SPATH, 1922.
Remarks.-Neopuzosia was proposed as
an independent genus, because the clistinction between the type-species of Neopuzosia and that of Kitchinites [K. pondicherryanus] was very clear. There are,however, certain species which show
apparently intermediate or even mixed
characters (see MATSUMOTO, 1954b, p. 89;
HOWARTH, 1965, p. 387). At present wewould agree with WRIGHT (1957) andHowARTH (1965) in admitting Neopuzosia
as a subgenus of Kitchinites.
Species of Kitchinites, including thoseof the subgenera Neopuzosia and Kitchinites (s.s.), have a shell of moderate tosmall size even at the mature stage,
being generally smaller than many otherspecies of the Puzosiinae. This point
was mentioned by MATSUMOTO (1954b, p.
90) and has been ascertained by subsequent descriptions of HOWARTH (1965)
and HENDERSON (1970). The species tobe described below may exemplify thesmallest form.
Kitchinites (Neopuzosia) haboroensis

MATSUMOTO and INOMA, sp. nov.
Pl. 47, Figs. 5-6; Text-figs. 5-9

Material.-Holotype, GK. H5654, fromJoe. IA-1564. Paratypes, GK. H5655, fromJoe. IA-1562; GK. H5656; from Joe. IA1561; GK. H5657, from Joe. IA-1599; GK.
H5660, from Joe. IA-1557; GK. H5661,
from Joe. IA-1570; GK. H5658, from Joe.
IA-1577, Haboro area. Probably referable specimens, GK. H5659, from Joe.
IA-1536, Haboro area; IGPS. 57746, lkushumbets area.
Specific characters.-Shell is small,about or slightly less than 30 mm indiameter at the adult stage. It is moderately evolute, about a half of the inner whorl being embraced by the outerone. Its umbilicus is also fairly wide,
occupying about 34-38 percent of a diameter in the holotype and measurable
paratype. The umbilicus is shallow andencircled by a very low but nearly vertical or steeply inclined wall.
The outer whorl is compressed, showing about 0.7 to 0.8 in the proportion ofbreadth to height. Its flanks are, however, gently convex, passing to a rather
narrowly arched venter. Its cross-sectionis, therefore, subelliptical. The inner
whorls are less compressed and subrounded ; the innermost one is depressed.
Constrictions are well marked (i.e. deep
and moderately broad on the internalmould) and fairly frequent, about five to
six per whorl. They are gently sigmoidon the flank and projected on the venter.
On the body-whorl the linguiform ventral projection is remarkable, being accompanied with the notable elevation
behind the constriction.
The inner whorls are nearly smoothish.

601.

Two small desmoceratid ammonites

385

a

Smm
L--J

Text-fig. 5. Kitchinites (Neopuzosia) haboroensis MATSUMOTO and !NOMA, sp.
nov. Diagrammatic sketch of the holotype, GK. H5655, in lateral view and its front
view, with body-whorl cut at Q (above); external part of the second last suture at
S (below). m =internal mould; t =test preserved; a= line of demarcation showing
the apertural margin at an earlier growth-stage; u.s. =umbilical seam, u.sh. =umbilical shoulder.
(T. MAT. delin.)

The septate part of the outer whorl has
fine and weak, sigmoidal ribs. The bodywhorl has more distinct, but fairly fineand dense, ribs, which are more or lesssigmoidal on the flank and projected on
the venter. The ribs which are situatedat some distance in front of the constriction are normally more sigmoid thanthe others, although there may be avariation in the details.
Near the apertural margin of the adultshell there are two approximated con·strictions which show a very strong ven-

tral projection. Aside from the elevations which are accompanied with thetwo constrictions, ribs are very faint,
whereas fine, sigmoid lirae are discernible on the shell-surface of the interval
between these two· constrictions. In frontof the last constriction there are elongated lappets which are situated at about
the inner one third of the flank. The
ventral part of the peristrome is moderately projected.
A distinct line of demarcation which
probably marks the apertural margin of386

Tatsuro MATSUMOTO, Tatsuo MURAMOTO & Akitoshi !NOMA

St

U.!;,

Text-fig. 6. Kitchinites (Neopuzosia) haboroensis MATSUMOTO and !NOMA, sp.
nov. Diagrammatic sketch of an immature shell, paratype no. 5, GK. H5658, inlateral and frontal view (above); the other side, in part (center); internal suture,with adjacent portion of external suture, at S2; external suture at Sl (below).
symbols m, t, a, and u.s. same as in Text-fig. 5, j =injured part of the apertural
margin at an early growth-stage.
(T. MAT. delin.)

the immature shell is sometimes preserved at some distance in front of theconstriction, showing a moderate flexuosity on the flank and a ventral projection.
Its convexity on the lower part of theflank is somewhat stronger than the ribs
or lirae on the adjacent parts (Text-figs.
5-7).

Sutures are of Puzosia pattern. Thosein the late part of the septate whorl
have a somewhat asymmetrically tripartite first lateral lobe (L) which is deeper
than the external lobe (E). The auxiliary elements beyond the second laterallobe (U 2 ) are aligned on a strongly_:ctescending line.

601. . Two small desmoceratid ammonites

387

Measw-ements.Specimen

DiameterUmbilicus

HeightBreadthGK. H5654

29. 0(1)

11. 2(. 38)

11. 5(. 40)" ( -180°)
GK. H5655
GK. H5656
GK. H5658

28. 0(1)
29. 5(1)
14. 3(1)

10. 4(. 37)
10. 2(. 34)
4. 3(. 30)

7.2
11. 2(. 40)
12. 2(. 41)
5. 5(. 38)

8. 9(. 31) (c)778. 7 (. 29) (ic)6.2
86
7. 3(sec. compr.)
8. 7(. 29).71
5. 5(. 38)
1.0

B./H.
0

0

·~--·-~The saddles are bipartite and theirstems tend to be narrowed by deep incision of the branches of the lobes. The
sutural formula is probably E, L, U2 , U3 ,U4 =S, U,v, U,d, I, but could be interpreted
otherwise [E, L, U2 , U 3 =S, U1 , I, as oneof us (T.M., 1954b, text-fig. 3) thought soon K. (N.) ishikawai] (see also ScHINDEWOLF, 1966, text-fig. 377).
Remarks.-There is some extent ofvariation in the relative width of umbilicus and the proportion between breadthand height of the whorl, even if theshells of corresponding size are compared. The details in the rib curvature
may also vary as shown in the illustration.
Comparison.-The shell of this species
closely resembles the small immature
one of Kitchinites (Neopuzosia) ishikawai(JIMBO, 1894) (see also MATSUMOTO, 1954b).
In fact the two species are apparently
indistinguishable up to the shell diameter of about 20 mm, if we ignore theminor variation. One point which may
serve as a distinction even in this immature shell is that a remarkably sigmoidal line of demarcation, probably theperistome of the immature shell, is distinct at some distance ahead of the constriction on a well preserved shell of K.
(N.) haboroensis. A similar line may bediscernible in front of the constriction
on some well preserved inner whorl ofK. (N.) ishikawai, but its curvature seems
to be more gentle, with a less pronounced

lateral projection.
The distinction in the succeeding later
whorls of the two species is unmistakable. The adult shell of K. (N.) habaroensis is much smaller and more widely
umbilicate than that of K. (N.) ishikawai
and ends at the peristome which is characterized by pronounced lateral lappets~
The mode of curvature of the ribs on
the body-whorl of K. (N.) haboroensis is
more sigmoid than those of K. (N.) ishikawai. The ribs are remarkably strongon the ventral part of the adult bodywhorl of K. (N.) ishikawai, except for
the faintly ribbed apertural part. Sucha sudden increase in the rib-intensity
does not occur in K. (N.) haboroensis,
although the ribs gradually become distinct on its outer whorl. The probably
adult shell of K. (N.) ishikawai has atleast two more whorls, attaining to about
120 or 130 mm in diameter, as represented by GK. H5663 (Y. UEDA Coli.) fromthe generally same Haboro-Chikubetsu
area (UEDA et al., 1962). Its very apertural margin is not completely preserved,
but there are two, fairly approximatedconstrictions which are prorsiradiate andvery gently sigmoid on the flank andstrongly projected on the venter. The
weak ribs and lirae on the interval of
the two constrictions and immediately infront of the last one show a similar
curvature. Although the very margin
is not completely preserved, judging
from the curvature of the lirae in the388

Tatsuro MAL-UMOTO, Tatsuo MURAMOTO & Akitoshi !NOMA

Text-fig. 7. Kitchinites (Neopuzosia) haboroensis MATSCMOTO and !NOMA, sp. nov.
Diagrammatic sketch of a part of an immature shell, paratype no. 6, GK. H5661,
in, Jateral view (test preserved).
(T. MAT. de/in.)preserved last part, it does not seem tohave long lateral lappets.
K. (N.) haboroensis is somewhat similar
to Yokoyamaoceras jimboi MATSUMOTO(1955, pl. 9, figs. 4, 5 ; text-fig. 13) in thesmall size, presence of lateral lappetsand other general appearance. The
latter has ventrolateral tubercles ona limited part of the body-whorl andprorsiradiate constrictions which cut obliquely numerous ribs behind them. The
suture of the former species is of puzosiine type, with remarkably descending
auxiliaries, whereas that of the latter isof Kossmaticeras type.
Kitchinites (Kitchinites) angolaensis
HOWARTH, 1965 (p. 386, pl. 11, figs. 4-6),
from the Campanian of Angola, is considerably small. Its probably adult shell,
as represented by the holotype, is 64 mm
in diameter. Therefore it is twice aslarge as K. (N.) haboroensis. K. (K.) angolaensis has somewhat less flexuous ribs
and more involute and more compressed
whorls than K. (N.) ishikawai and K. (N.)
haboroensis, if the shells are comparedat corresponding size. Rather rapid
strentghening of the ribs on the ventral
part of the probably adult whorl is evident in K. (K.) angolaensis, whereas con-strictions are stronger in K. (N.) haboroensis.
Unfortunately the peristome of theadult shell has not been clearly describedin K. (K.) angolaensis nor in K. (K.) pondicherryanus (KOSSMAT), the type-species
from India. The neotype of K. (K.) angustus (MARSHALL), proposed by HENDERSON (1970, p. 34, pl. 14, fig. 1), from theCampanian of New Zealand, shows dense
lirae at the preserved last part (diameter about 130 mm), which show a very
gently sinuous curvature on the flankand are considerably projected on theventer as in the above mentioned specimen of K. (N,) ishikawai. However, it
is not certain whether or not the lastpart of that New Zealand species marks
the very apertural margin.
In view of the gentle inflation of the::flanks and the gradual strengthening of
the ribs in the adult shell, this species
could be referred to Mesopuzosia, but
we are inclined to assign it to Kitchinites (Neopuzosia) because of its small
size and its close resemblance to K. (N.)
ishikawai in immature stages.
Occurrence.- The type-locality is Joe.
IA-1564, in unit B (siltstone) of the Santonian sequence exposed in the area ofthe Haboro dome, Rumoi district, Teshio
provine, northwest Hokkaido. Paratypes
came from Joe. IA-1599, Deto-Futamata,a tributary of the Haboro, upper partof unit A (siltstone), and rolled or fallen
nodules obtained at Joe. lA -1557, lA-1561,
lA-1562, lA-1577 (Haboro dome), IA-1570(Sakasa-gawa), and IA-1536 (Ainu-sawa).
The possible sources of the rolled orfallen nodules are from unit A to Dwithin the Santonian sequence (zone of
Inoceramus naumanni) of the Haboro
area (Text-fig. 8). They are all from
calcareous nodules in siltstone and often
associated with Inoceramus naumanni.
Thus in the Haboro area, which repre-

601.

Two small desmoceratid ammonites

389

N

+

0

Text-fig. 8. Geological map of the upper reaches of the Haboro. A-F= Upper
Cretaceous (Santonian) sequence in ascending order, A: dark grey siltstone, with
tuffaceous sandstone at the top (indicated by black band), B: dark grey siltstone,
C: glauconitic sandstone (coarsely dotted), D: dark grey siltstone, E: green sandstone, F: black mudstone. T=Tertiary (Miocene) conglomerate, sandstone, shale
and tuff (finely dotted). x =Locality where the described ammonites were obtained(in situ) ; + Ditto (in fallen or rolled nodules).
(Geol. Surv. by A. !NOMA)

sents a northwestern part of the Yezo
geosyncline and probably belongs to aless off-shore facies, the species seems
to occur not uncommonly. In other areas
the occurrence of the species has notbeen well ascertained, except for a rareoccurrence of a probable example fromthe Santonian of Kikume-zawa, lkushum-

bets area, central Hokkaido.
Discussions.-The fact that Kitchinites(Neopuzosia) haboroensis shows almost
the same stratigraphical range as K. (N.)
ishikawai (JIMBO) and that the former isclosely similar to the latter in the immature stages but much smaller in themature stage, having a particular type390

Tatsuro MATSUMOTO, Tatsuo MURAMOTO & Akitoshi !NOMAof peristome, recalls us of the possibility·· of sexual dimorphism between the two"nominal species". The situation apparently seems to be analogous with thecases in certain Jurassic ammonites as
exemplified by Cosmoceras spinosum(SOWERBY) and Quenstedtoceras mariae(D'ORBIGNY), which were discussed by
MAKOWSKI (1962), and by Creniceras
renggeri (OPPEL), Distichoceras bicostatum (STAHL), and ? Hecticoceras brightii(PRATT), which were ontogenetically examined by P ALFRAMAN (1966, 67, 69).
We do appreciate these and other authors who took into consideration the
problem of sexual dimorphism in the
study of ammonites, but it seems to us
fairly difficult to present the necessary
and sufficient evidence for concludingthat A is the female and B is the maleof one and the same species.
Aside from the Jurassic ammonites,with which we are not well acquainted,
let us consider the problem in the caseof the Puzosiinae. Although numerous
species of the subfamily have been
monographed by various authors, little
has been mentioned about the peristomeof mature shells. In our experience offield work we observe that the smoothish body-whorl of a large shell of Puzosia,
Mesopuzosia or Pachydesmoceras is oftensquashed probably because of its weakercondition as compared with the septate
whorls.
One of a few examples in which theapertural margin was described is avery large specimen of " Ammonites
planulatus " in STOLICZKA (1865, p. 134,
pl. 68). One of us (T.M.) fortunately
had an opportunity to examine this specimen in the museum of the Geological
Survey of India, Calcutta. There is abroad, deep, concave constriction near
the preserved last part of the shell (about
805 mm in diameter). The body-whorl

is smoothish and unusually inflated behind the last constriction, with thebreadth of 225 mm (about 0.98 of theheight). The shell in front of the last
constriction is not completely preserved;
the ventral linguiform projection is present but the presence or absence of latera! lappets is not know. If we assume
that there were no lateral lappets, thisspecimen could possibly be regarded as
representing a female form of Puzosia
sp. by analogy with the cases of Jurassic ammonites. However, the evidence
to conclude so is by no means sufficientand no corresponding male form (somewhat smaller one with lateral lappets)
has been confirmed to occur in the sameformation.
In the recent collection of one of us(T.M.) there is an interesting specimen,
GK. H5665 (Text-fig. 9), from Joe. T 1021p
of the Turonian Saku formation, in
which the peristome is almost completely
preserved. Based on the general characters of the shell it is probably referable to Mesopuzosia pacifica MATSUMOTO,
1954. It is of moderate size, only somewhat larger than the holotype. On thelast part of its body-whorl the ribs aremuch weakened between two, rather approximated, strong constrictions (elevations on the shell), which are very gently
sigmoidal on the flank and projected on
the venter. In front of the last constriction there is a remarkable ventral
rostrum, which approximately continues
the spiral line of coiling, and remarkable lateral lappets, which are as long as
the rostrum but somewhat bent inward
at their terminal portion. The lirae are
gently sigmoidal on the part immediately in front of the last constriction but
become more and more strongly flexuous so as to follow the outline of thevery apertural margin. Whether every
shell of Mesopuzosia pacifica has always

601.

Two small clesmoce?'"atid ammonites

39 1

Tex t-fig. 9. M esopuzosia sp. cfr. M. pacifica M ATSUMO T O . GK . H5665, from Joe.
Tl02lp2, Saku Formation, x 0.9. Note the w ill preserved apertural margin and a marked
contribution behind it.
(I.H . jJhotos)

this kind of peristome in the matureshell or not is not clear. One of theparatypes of this species, GK. I-!1571 (seeMATSUMOTO, 1954b, pl. 15, fig. 2) has alarger outer whorl than the holot ype andthe above specimen (GK. H5665), but its
outer whorl is so incompletel y preservedthat its apertural margin is not shown.
Thus we cannot yet settle the problem
of sexual dimorphism in this speci es.
Be that as it may, it is interesting tosee a similarity between the well pre·served peristome of the above mentioned
iVIesopuzosia jJacifica and that of Kitchinites (Neopuzosia) haboroensis. On thesegrounds it can be stated that at least
some, if not all, of the Puzosiinae havean apertural margin which is character·ized by a rostrum and lateral lappets.
We would not completely deny thepossibility that Kitchinites (Neopuzosia )haboroensis might represent the maleform of K (N.) ishilwwai. So far as
the available material is concerned, weshould regard them as two different

species, inasmuch as we obser ve a dif·
terence even in the immature stage (seedescription under the heading of com·
parison). The said difference, howev er,
should be examined more precisely bytreating more specimens with respect toontogeny and variation.
Another point which is unfavorable
for concluding the sex ual dimorphismin this case is the occurrence. Although
there would be some collection failure,
the specimens of K. (N.) haboroensis havebeen kno wn onl y in a limited area of aparticular facies and are not always as·sociated with K. (N.) ishilwwai, which, inturn, is more widely distributed. We
rather consider that smaller ammonites
which possess lappets at the peristomeof the shell should have particular habi·tats and mode of life which are different
from larger ammonites without lappets.
Presumably the former may have beenless active and less rapidly locomotive
than the latter and have taken different
kinds of food. Too much difference in392

Tatsuro MATSUMOTO, Tatsuo MURAMOTO & Akitoshi [NOMAthese respects between male and female
seems to be unnatural, if not impossible.
In other words, the difference in size andapertural character of the adult shell
may not imply sexual dimorphism but
may be concerned with taxonomic difference or morphological diversity inevolution, which in turn, is connectedwith diversity in habitats and mode oflife. It is, furthermore, noted that themegaform is about two whorls larger
and has much more numerous septa thanthe compared microform. This implies
a considerable gap in age between thetwo forms.
In spite of a large number of specimens which have been monographed
under the subfamily Puzosiinae, examples which have lappets are very few.
Smaller shells with lappets should occur
more frequently in association withnumerous, larger shells, if such sexual
dimorphism as analogous to that statedin Jurassic ammonites existed in the
Puzosiinae. We would rather expect a
different type of sexual dimorphism in
the Puzosiinae, such as more inflation of
the adult body-whorl or broader aper·
ture and somewhat (but not extremely)
larger size of the male shell than thefemale, as suggested by the· living species of Nautilus, or difference in finenessor intensity of the ornamentation of theadult shell as suggested by REYMENT(1971) for dimorphic pairs of Cretaceous
Benueites species.
To sum up, we have considered apossibility of sexual dimorphism in the
Puzosiinae but are rather inclined tothink that the available evidence is yet
insufficient to support it, leaving the
problem in the future. In this paper
we describe Kitchinites (Neopuzosia) haboroensis as a new species of the Puzosiinae which is characterized by a verysmall size and a particular type of shell-

aperture, stressing that the Puzosiinae
include various species from a gigantic
size to a very small one. It is notedthat the Puzosiinae show a considerable
diversity in the character of the adultbody-whorl. There would be some diversity in the character of its apertural
margin in the same subfamily, although
the actual features have not yet beenthoroughly known on account of the unfavourable preservation. The species
described in this paper presents a rare
but good example.

References cited
ARKELL, ].W. (1957) : In MooRE, R.C. (ed.) :Treatise on Invertebrate Paleontology,
Part L (Mollusca 4, Cephalopoda, Ammonoidea) L1-L490, Geol. Soc. Amer. &Univ. Kansas Press.
CHOFFAT, P. (1903) : Contributions Ia connaissance geol. des colonies portugaisesd'Afrique. I. Le Cretacique de Conducia,
pp. 1-29, 7 pis., 1 folded pl., Cornmiss. SeriJ.
Geol. Portugal.
HENDERSON, R.A. (1970) : Ammonoidea from
the Mata series (Santonian-Maastrichtian)of New Zealand. Special Papers in Palaeontology, (6), pp. 1-82, pis. 1-15.
HoEPEN, Ir. E.C.N. VAN (1951) : A remarkable desmoceratid from the South African
Albian. Paleont. Navor. Nas. Mus. Bloemfontein, D!. 1, St. 10, pp. 345-349.
HowARTH, M.K. (1965) : Cretaceous ammonites and nautiloids from Angola. Bull.
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KossMAT, Frantz (1895) : Untersuchungeniiber die Siidindische Kreide-formation, I.
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MATSUMOTO, Tatsuro (1954a) : Selected Cretaceous leading ammonites in Hokkaido

a

601.

Two small desmooerat_id ammonites

and Saghalien. In MATSUMOTO, T. (ed.) :The Cretaceous System in the japaneseIslands, Appendix, pp. 243-313, pis. 17[1]-36 [20].
- - (1954b) : Family Puzosiidae from Hokkaido and Saghalien. Mem. Fac. Sci.,
Kyushu Univ., Ser. D, Ceol., Vol. 5, No.
2, pp. 69-118, pis. 9-23.
- - (1955) : Family Kossmaticeratidae from
Hokkaido and Saghalien. japan. jour. Ceo/.
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8-10.
- - , Tatsuo MuRAMOTO and Takemi TAKA·
HASH! (1969) : Selected acanthoceratidsfrom Hokkaido. Mem. Fac. Sci., Kyushu
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251-296, pis. 25-38.
MILLER, A.K. and YouNGQUIST, Walter(1946) : A giant ammonite from the Cretaceous of Montana. jour. Paleont., Vol.
20, no. 5, pp. 479-484, pis. 73-75.
PALFRAMAN, D.F.B. (1966): Variation andontogeny of some Oxfordian ammonites;
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- - (1967) : Variation and ontogeny of some
Oxford Clay ammonites: Distichoceras
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Vol. 10, pt. 1, pp. 60-94, pis. 9-13.
- - (1969) : Taxonomy of sexual dimorphism
in ammonites: morphogenetic evidence in
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WEsTER:VIANN (Ed.). Sexual dimorphism
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393

No. 1, pp. 126-154, pis. 6-8.
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REYMENT, R.A. (1971) : Vermuteter Dimorphismus bei der Ammonitengattung Benueites. Bull. Ceol. Inst. Univ. Uppsala,[N.S.], Vol. 3, art. 1, pp. 1-18, pis. 1-10.
ScHINDEWOLF, O.H. (1966) : Studien zur
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etc. In BLANFORD, M.F. and STOLICZKA,
F., 1861-66. The fossil Cephalopoda of
the Cretaceous rocks of southern India.
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pis. 81-94, 1866].
UEDA, Yoshiro, Tatsuro MATSUMOTO and Ken
AKATSU (1962) : The Cretaceous deposits
in the Chikubetsu area, Hokkaido. Sci.
Rept. Dept. Ceo!. Kyushu Univ., Vol. 6,
no. 1, pp. 15-32, with 3 folded chart andmaps [in Japanese with English abstract].
WIEDMANN, Jost (1970) : Ober den Ursprung
der Neoammonoideen-Das Problem einer
Typogenese. Eclogae Ceologicae Helvetiae, Vol. 63, no. 3, pp. 923-1020, pis. 1-10.
WRIGHT, C.W. (1957) : In MooRE, R.C.
[Editor]: Treatise on Invertebrate Paleontology, Part L, Mollusca, Cephalopoda,
Ammonoidea, L1-L490, Geol. Soc. Amer.
& Univ. Kansas Press.

-----------------------------------------Ainu-sawa
Chikubetsu
Deto-Futamata
Ikushumbets
Kikume-zawa
Haboro~ ffJ.

iR* r =!Ysl
)Jlj

---f'

~;,ff}}lj%J 00 iR~~~1)\\

Mikasa
j;.l]
Rumoi
Ell
Sakasa-gawa
)!E
Jll
Saku
{:ti
!A
Shimo-ichino-sawa T-O)iR
Tori-sawa
.~
tR

394

Tatsuro MATSUMOTO, Tatsuo MURAMOTO & Akitoshi [NOMAExplanation of Plate 47
Figs. 1-4. Microdesmoceras tetragonum MATsUMOTO and MURAMOTO, sp. nov ....... Page 378
1. Holotype, GK. H5653, from Joe. Ik 1101, zone of Mantelliceras japonicum, Ikushumbets area. Two lateral (a, b), apertural (c) and external (d) views, approximately
x2.
2. Paratype no. 2, immature specimen, from Joe. lk 1051b, MuRAMOTO Museum coli.
Lateral (a) and external (b) views, approximately x 2.
3. Paratype no. 1, immature specimen, from Joe. Ik 1101, MuRAMOTO Museum coli.
Two lateral (a, b) and external (c) views, x 2.
4. A half of paratype no. 3, GK. H5650, from Joe. Ik 1067bp. Two lateral (a, b) andsectional (c) views, x 2.
Figs. 5-6. Kitchinites (Neopuzosia) haboroensis MATsUMOTO and !NOMA, sp. nov .... Page 384
5. Holotype, GK. H5654, from Joe. IA-1564, unit B of the Santonian sequence, Haboro
area. Two lateral (a, b-e) and external (d) views, xl.5. To show the ribbing andother features b and c are taken under the light of somewhat different orientation.
6. Para type no. 1, GK. H5655, from Joe. IA-1562. Two lateral view (a. b), x 1.5.
Kyushu University [I. HAYAMI] photos, with whitening.

•MATSUMOTO, MURAMONO & !NOMA:

Two small desrnocemticls

Plate 47

ld

lc

3c
2b

4b

3b

Trans. Proc. Palaeont. Soc. Japan, N.S., No. 87, pp. 395-408, pis. 48, 49, September 30, 1972

602.

SWIFTOPECTEN OF THE NORTHERN PACIFIC·~
KOICHIRO MASUDA

Department of Geology, Miyagi University of Education, Sendai~t.i:>fi.'Ni!!ll..)i(O) Swiftopecten: Swiftopecten fi, ~t.ll Jj(ip Gricif&~ ht.:3}1.j:_O) Pecten
swijtii BERNARDI 1!: {l,"i:t\:filU: !..- "(, HERTLEIN (1935) fC J:: -:> L"tJ!':III§ ~ ll.J.: ob 0)'"(· Ji:, 0 0:7ff;l:l:'Jj]iy, B::;j\:OJ1tT:i:t-'J:: lf331.1:0J Pecten swijtii fc-::n,,-cfi]fl\:L-. -'tOJ:li!!'W:~I'I'{E.i:¥'li:fC"?
v'-c;;-~~HTfJ:-:> t.: (MASUDA, 1959, 1960) o -'COJ[ifi~, *:'tHi~t.T ;< 0 ;t.J ®ifiJ!¥OJ'fi[r1:!fi!.i.i•
G\illf!r~h'Lv'0, v'bfiJ:>0 Swiftopecten c B::;j\:OJ Swiftopecten 1!:'J:Ut!.<:tJ!F.i-t0·.1Z·~ii~Ji:>
0 c. c 1!: Hitiii L-t.: o4'@1, ~11Hi;[t.T ;< 0 hiii:iifiJW=ii,G¥11'15~ht.:-jA:-cOJ Swiftopecten fC"?v''Lt'!\!il•J-L-t.:
t!f:!if!:, T 7 A t.J ii' GF.c![\1( ~ ht.: Pecten (Chlamys) kindlei DALL, Chlamys (Swiftopecten)
donmi lleri MAcNEIL :ts J:: lf, ~t. :iJ 0 7 ;t 1v =- T i.i' G ARNOLD (1906) il;\iR'ff L-t.: Pecten(Chlamys) parmeleei DALL fi, swijtii c :// =- J, -r· &.:> 0 C. c iJ;Q)l GiPfC tJ:-:> t.:iii.l', J:j:l
11~-m~~h 0 7;tlv=-TiPGioGh'Lv'0 parmeleei ii swiftii OJill.!tlc;;-.:Z0-"2:<::·&.:>0:::.cil~ft)JGiPfCfJ:-:>f.:o l-7.1'!..-, J1§iiiJi¥fC:Gft0C.hGL:H~OJ<bOJfi, Swiftopecten cfi5)1]*

OJ'~-~~AhGh0-"~~&.:>0c;;-.:ZGh~o

C. OJt!f:'if!:, Swiftopecten fiJ;Ii[T :/TiP G~t.Hi1;t:, -t; .f... 7- -t ., :iJ 1!:'{fJ:-c T 7 A :iJ, ~ G fC
T!l:iiliiwfci'fh'Lfyj:iJ 0 7 ;t ;L--=- T'iL:·5f;(fil..-'Lv't.:::. c fCfJ:0o B*<::·fj: swiftii OJliltfJJOJ/1',
JJHi Middle Miocene -r· ;!>:, 0 ii;, T 7 A ;/J '"(·f;l: Late Miocene fC l:I:',JJ!. L-, Early Pliocene
fU'i~t. :iJ 0 7 ;t '"' =- T 'i ~57'1!1 !..- t.:, :fit, ::lt.)JfCfP-:> -c Middle Pleistocene fC*i'\im1 L- 'Lv' 0,- ) j swijtii iPG~1tL-t.:c;;-.:ZGh6 parmeleei fi, Middle Pliocene fCJ:f:l-i'i~fi~:iJ 0
7 ;t 1t--=- TfC/1\JJ\l 1..-t.:ii;, -'tOJ;;!ZJiJHUi*~i~L- -c L-'i-:> t:c~.:ZGh6,
Swiftopecten 0) C. 0) J:: ? t~Ji!!l'JllO"J · J:I!!'W:~fi'J5-};(fifi, ::lt.i:-'fi't.J:I!!r~fc:Git 6 tJ'J:I!!J'.illO) ~i!c$i~tJ:~f~'{dc&.:>6:::.cfillflGi.I'<::·Ji:>6,
f\lliil -~- Jl!B

Among the Northern Pacific Recent
and fossil pectinids Swiftopecten is of interest because of its characters, extensive geographical distribution and rather
short geological range, as discussed in
the following pages.
From the study of the Tertiary Pectinidae of Japan the writer doubted whether Swijtopecten of the West Coast of
North America is identical with the true
Swijtopecten of Japan. To clarify thisproblem MASUDA (1959a, 1960) examined
numerous fossil specimens of Swiftopecten
swiftii (BERNARDI) collected from the
Neogene and Pleistocene formations inNorthern Japan and Recent speci~ens

Introduction
Pecten swijtii, a common Recent scallop of Northern Japan, was first describedby BERNARDI (1858), and subsequently it
and its varieties were recorded from theseas of Northern Japan and also from the
Neogene and Pleistocene deposits of Japan, the West Coast of North America
and eastern Soviet Russia. In 1935 HERTLEIN proposed Swijtopecten for the present species as a subgenus of the genus
Pecten.

* Received January 22, 1972; read January
23, 1972 at Chiba.

395

Koichiro MASUDA

396

from the Northern Pacific and Japan Sea.
At that time he supposed that the North
American Pecten kindlei DALL and Pecten
parmeleei DALL might be descendants ofswijtii, and that they migrated from
East Asia to the West Coast of North
America. MASUDA also pointed out thatthe interrelationship between the Japanese fossil and Recent Swiftopecten andthe so-called North American Swift apecten
should be studied comparatively.
Many specimens of Swiftopecten fromthe West Coast of North America werestudied in connection with the problems
mentioned above. The specimens studied
are now in the collections of the Department of Geology, Stanford University,
U.S. Geological Survey in Menlo Park,
Museum of Paleontology, University ofCalifornia in Berkeley, California Academy of Sciences in San Francisco, Smithsonian Institution in Washington, D.C.,
and County Museum of Natural History
in Los Angeles.
The examination of those specimens
revealed that Pecten kindlei DALL fromthe Pleistocene of Alaska, some of Pecten
panneleei DALL from the Pliocene ofnorthern California and Chlamys (Swiftopecten) donmilleri MACNEIL from the
Miocene of Alaska are synonyms of
Swiftopecten swiftii (BERNARDI), and thatseveral western North American species
or subspecies referred to Swiftopecten
differ from the true Swiftopecten.
In the present article the morphologicalcharacters of Swiftopecten are described
and the paleontological significances ofthe so-called Swiftopecten of the West
Coast of North America are discussed.

Acknowledgments
The writer expresses his deep gratitude to Dr. A. Myra KEEN, Professor
Emeritus of the Department of Geology,

Stanford University, Professor J. Wyatt
DURHAM of the Department of Paleontology, University of California at Berkeley and late Dr. Leo G. HERTLEIN of the
California Academy of Sciences in San
Francisco, for their continuous encouragement and help in various ways during
the course of the present work. Acknowledgments are due to Professor Kotora
HATAI of the Institute of Geology andPaleontology, Faculty of Science, Tohoku
University, for reading the manuscript.
The writer received support from thefollowing persons during the course of
the present work, and takes this opportunity to express his deep gratitude tothem : Drs. David M. HOPKINS, George
PLAFKER and Warren 0. ADDICOTT of
the U.S. Geological Survey, Menlo Park,Mr. Joseph H. PECK of the Departmentof Paleontology, University of California,
Berkeley, Dr. James H. McLEAN of theCounty Museum of Natural History in
Los Angeles, and Drs. Wendell P. WooDRING, Harald A. REHDER and Thomas R.
WALLER of the Smithsonian Institutionin Washington, D.C., Mr. Kenji SAKAMOTO of the U.S. Geological Survey in Menlo
Park prepared most of the photographic
work.
Thanks are due to the Department of
Geology, Stanford University, Museumof Paleontology, University of California,
Berkeley, U.S. Geological Survey, Menlo
Park, Smithsonian Institution, California
Academy of Sciences and Los Angeles
County Museum of Natural History, for
permission to study their collections.
Acknowledgments are also made to the
Ministry of Education of the Japanese
Government, for the scholarship of study
abroad.

Historical review of Swiftopecten
In the West Coast of North America

602.

Swiftopecten

the species or subspecies hitherto beenreferred to Swiftopecten or described asa variety of swiftii are: Pecten (Chlamys)parmeleei DALL, 1898, Pecten etchegoini
ANDERSON, 1905, Pecten (Chlamys) nutteri ARNOLD, 1906, Pecten (Chlamys) wattsi ARNOLD, 1906, Pecten (Chlamys) wattsi morani ARNOLD, 1906, Pecten (Chlamys) kindlei DALL, 1920, Chlamys (Swiftopecten) donmilleri MACNEIL, 1967, Chlamys (Swiftopecten) sp., MACNEIL, (1967),
Swiftopecten sp., ADEGOKE, (1967), Swiftopecten adekunbiana ADEGOKE, 1969 andChlamys (Swiftopecten) leohertleini MACNEIL, 1970. However, no Recent speciesof Swiftopecten is known from the West
Coast of North America.
Pecten (Chlamys) panneleei first described by DALL (1898) from the Pliocene
formation at San Diego, Southern California, was distinguished from swiftii. In
1906 ARNOLD illustrated parmeleei fromthe Pliocene formation at Pacific Beachnear San Diego and also from the Plioeene formation at Crescent City in Northern California. ELDRIDGE and ARNOLD(1907) also reported the species from the
Pliocene Fernando Formation at Elsemare Canyon, Southern California. Subsequently GRANT and GALE (1931) considered parmeleei a synonym of swiftii
with the statement that the morphological characteristics pointed by DALL are
the same as those of swiftii. WOODRING
and BRAMLETTE (1950) illustrated parmeleei from the Pliocene Careaga Sandstoneof the Santa Maria district, Southern
California.
In 1920 DALL described Pecten (Chlamys)
kindlei based upon the specimens fromthe Pleistocene deposits of Center Creek
Mines near Nome, Alaska. GRANT and
GALE (1931) included kindlei, nutteri andetchegoini into the variety of swiftii ofthe subgenus Pallium, and wattsi, wattsi
morani and cosibensis were included into

397

etchegoini and heteroglyptus into nutteri.
Among the species treated by them both
Pecten cosibensis YoKOYAMA, 1911 and P.
heteroglyptus YOKOYAMA, 1926 had been
described from the Pliocene formationsin Japan.
MACNEIL (1943) described Pecten kindlei
DALL under the subgenus Manupecten
from the Intermediate Beach, Center
Creek near Nome in Alaska, but subsequently from the same locality he (MACNEIL, 1967) recorded kindlei as a subspecies of swiftii under the subgenus Swiftopecten. At the same time he described
Chlamys (Swiftopecten) donmilleri, n. sp.
from the Miocene Yakataga Formation,
Yakataga district, Alaska, and Chlamys(Swiftopecten) cf. donmilleri and Chlamys(Swiftopecten) sp. from the Unga Conglomerate at Alaska Peninsula. Furthermore, very lately he also described
Chlamys (Swiftopecten) leohertleini, n. sp.,from the Pliocene Tachilni Formation
at the western end of Alaska Peninsula(MACNEIL, 1970).
In 1956 GLEN illustrated Pecten (Pallium)
swiftii var. etchegoini and swiftii var.
nutteri from the Pliocene "Merced" Formation near San Francisco, California.
F AUSTMAN (1964) recorded Pecten (Swiftopecten) etchegoini wattsi and Pecten(Swiftopecten) sp. from the " Wildcat"
Formation in Northern California.
Recently ADEGOKE (1967) described
Swiftopecten sp. from the Miocene Santa
Margarita Formation, California and discussed its paleontological significance,and he also (ADEGOKE, 1969) describedfrom the same formation, Swiftopecten
adekunbiana, n. sp. and Swiftopecten n.
sp. and included etchegoini, wattsi andnutteri from the Pliocene Etchegoin and
San Juaquin Formation, California, in thegenus Swiftopecten.
On the other hand, in Soviet Russia,
KHOMENKO (1934) recorded swiftii under398

KOichiro MASUDA

the subgenus Pallium from the Pliocene
formation of Schmidt Peninsula, Northern Sakhalin. Subsequently SLODKEWITSCH (1938) illustrated Pecten (Pallium)
swiftii from the Pliocene Pomyr Seriesof Sakhalin and considered nutteri, etchegoini, heteroglyptus and pilutukensis
as varieties of swiftii. Lately IL YINA
(1963) figured etchegoini as a variety ofswiftii under the genus Swiftopecten
from the Pliocene of Kamchatka and
KRISHTOFOVICH (1964) illustrated swiftii,
nutteri and pilutukensis as varieties ofswiftii under the subgenus Swiftopectenof the genus Chlamys from the Plioceneof Sakhalin.
Since the historical review of theswiftii group in Japan by the writer(MASUDA, 19o9a, 1960, 1962a), SAWADA(1962), IWAI (1965) and UOZUMI, FUJIE
and MATSUI (1966) figured swiftii under
the genus Swiftopecten from the Pliocene
formations in Northern Japan and also
KASENO and MATSUURA (1965) figured
swiftii under the genus Chlamys fromthe Pliocene of Ishikawa Prefecture.
As mentioned already HERTLEIN (1935)
proposed Swiftopecten as a subgenus of
the genus Pecten and designated switii
BERNARDI as the type species, but gave
no diagnosis of his new subgenus.
Although swijtii had been describedunder the genus Pecten, the genus orsubgenus Chlamys or as the subgenus
Pallium, HABE (1958) first used Swiftopecten as a subgenus of the genus Chlamys in Japan. The writer referredswiftii to the subgenus Swiftopecten of
the genus Chlamys (MASUDA, 1959a). But
because of its distinct morphologicalcharacters the writer raised Swiftopecten
to generic rank (MASUDA, 1960).
On the other hand, on the West Coastof North America this species and its
varieties had been referred to the subgenus Pallium or Manupecten of thegenus Pecten (GRANT and GALE, 1931,
MACNEIL, 1943) and to the subgenus
Swiftopecten of the genus Pecten, but
subsequently MACNEIL (1967) referredthem to the subgenus Swiftopecten of
the genus Chlamys and ADEGOKE (1967)
raised Swiftopecten to generic rank. In
eastern Soviet Russia swiftii and its
varieties were referred to the subgenus
Pallium of the genus Pecten (SLODKEWITSCH, 1938), but IL YINA (1963) raised
Swiftopecten to generic rank and KRISHTOFOVICH (1964) considered Swiftopecten as a subgenus of the genus Chlamys.
From the remarks given above the
Swiftopecten group is a confusing one in
the Northern Pacific area. Therefore,
to clarify the confusion the writer describes the type species from Japan andpresents discussions concerning it.
Description

Family Pectinidae
Subfamily Chlamyinae V. TEPPNER, 1918
Genus Swiftopecten HERTLEIN, 1935
Swiftopecten HERTLEIN, 1935, p. 319.
Type-species :~Pecten swiftii BERNARDI, 1858.
Recent, Northern Japan.

Geological and geographical distributions :-Middle Miocene to Recent. North
Pacific.
Remarks :-As pointed out on the earlier lines the Swiftopecten group has
been considered a subgenus Pallium or
Manupecten. However, Pallium (SCHUMACHER, 1817, fide GRANT and GALE,
1931) is distinguishable from Swiftopecten
by its small shell, nearly equal auricles
and well-marked cardinal crura, andManupecten (MONTEROSATO, 1889, fide
COSSMAN and PEYROT, 1914) differs from
Swiftopecten by its right valve being

602.

Swiftopecten

nearly equal to the left one in convexity,
both valves having equal sctJlpture, radialribs which are nearly equal to their interspaces in width, and by the left valve
with np constricted radial ribs. Manupecten is considered to be closely relatedwith Swiftopecten as pointed out by
PHILIPPI (1900), GRANT and GALE (1931)
and MACNEIL (1967). Therefore, further
studies are necessary to settle the relationship between them.

Swiftopecten swiftii (BERNARDI, 1858)
Pl. 48, figs. 1-5, Pl. 49, figs. 1-5
1858. Pecten swijtii BERNARDI, jour. de Conch., Vol. 7, 2nd Ser. Tome 3, p. 90, pl.
1, fig. 1, pl. 2, fig. 2.
1867. Pecten swijtii BERNARDI: SCHRENCK,
Moll. Amurl. Nordjap. Meeres, p. 487,
pl. 21, figs. 1-3.
1882. Pecten swijtii BERNARDI : KOCHIBE,
Rika Kai-shi, Tokyo Univ. Press, No. 4,
p. 75, pl. 5, fig. 2.
1888. Pecten swijtii BERNARDI: KOsTER und
KOBEL T in MARTINI und CHEMNITZ,
Syst. Conch. Cab., Vol. 7, pt. 2, p. 142,
pl. 40, fig. 3.
1902. Pecten swijtii BERNARDI: YOSHIWARA,
Zool. Mag. Tokyo, Vol. 14, no. 162, p.
144, pl. 2, figs. 6a-b.
1906. Pecten (Chlamys) parmeleei DALL: ARNOLD, U.S. Geol. Surv. Prof. Paper No.
47, p. 119, pl. 41, figs. 5, 5a.
1920. Pecten (Chlamys) kindlei DALL, U.S.
Geol. Surv. Prof. Paper 125-C, p. 30, pl.
6, figs. 2, 7.
1925. Pecten swijtii BERNARDI: YoKOYAMA,
jour. Colt. Sci., Imp. Univ. Tokyo, Vol.
45, art. 5, p. 27, pl. 2, fig. 1.
1926. Pecten swiftii BERNARDI: YoKOYAMA,
jour. Fac. Sci., Imp. Univ. Tokyo, Vol.
1, pt. 8, p. 303, pl. 37, figs. 5, 6.
1931. Pecten (Pallium) swijtii BERNARDI:
GRANT and GALE, Mem. San Diego Soc.
Nat. Hist., Vol. 1, p. 171, pl. 10, figs.
la-b, 4a-b.
Hi31. Pecten (Pallium) swiftii kindlei DALL:

399

GRANT and GALE, Ibid., p. 174, pl. 10,
fig. 7.
1934. Chlamys swijtii (BERNARDI) : KINOSHITA and IsAHAYA, Rept. Fish. Surv. Hokkaido Fish. Exp. Stat., No. 33, p. 14, pl.
10, fig. 74.
1934. Pecten swijtii BERNARDI: KHOMENKO,
Trans. Geol. Oil Inst., Ser. A, Fasc. 40,
p. 31, pl. 2, figs. 3, 4, pl. 3, figs. 2, 3.
1935. Pecten (Pallium) swijtii BERNARDI:
NoMURA and HATAI, Saito Ho-on Kai
Mus., Res. Bull., No. 6, p. 98, pl. 9, fig.
8, pl. 10, figs. 3, 4, pl. 11, fig. 8, pl. 13.
fig. 3.
1938. Pecten (Pallium) swijtii BERNARDI:
SLODKEWITSCH, Acad. Sci. USSR, Paleont. Inst. Paleont. USSR, Vol. 10, pt.
3, fasc. 18, p. 169, pi 22, fig. 2, pl. 23,
figs. 1, 1a, 2, 3.
1943. Pecten (Manupecten) kindlei DALL:
MAcNEIL in MAcNEIL, MERTlE andPILSBRY, jour. Paleont., Vol. 17, no. 1,
p. 87, pl. 12, figs. 7, 8.
1950. Chlamys islandicus var. swiftii (BERNARDI): KuBOTA, Cenozoic Res., No. 6,
p. 12, pl. 9, figs. 66, 67.
1955. Chlamys swijti (BERNARDI) : HABE,
Pub!. Akkeshi Mar. Biol. Stat., No. 4,
p. 6, pl. 2, fig. 7.
1958. Chlamys (Swiftopecten) swifti (BERNARDI) : HABE, Publ. Seta Mar. Biol.
Lab., Vol. 6,.no. 3, p. 263, pl. 12, fig. 18.
1958. Chlamys (Swiftopecten) swijti (BERNARDI) : YAMAMOTO and flAB!', Mar.
Biol. Stat. Asamushi, Tohoku Univ.,
Bull., No. 9, pt. 1, p. 15, pl. 3, fig. 4,
pl. 5, figs. 4, 7.
1958. Chlamys swiftii (BERNARDI) : ToMIZAWA in T. and K. YAGI, Geol. KamiMinochi, p. 326, pl. 3, figs. 5a-b.
1958. Chlamys swifti (BERI\:ARDI) : FUJIE,
Cenozoic Res., No. 28, p. 668, pl. 27,
figs. 29, 30.
1959. Chlamys (Swiftopecten) swiftii (BERNARDI) : MAsUDA, Trans. Proc. Palaeont. Soc. japan, N.S., No. 34, p. 87, pl.
9, figs. 1-7.
1959. Chlamys swiftii (BERNARDI): OYAMA,
Sci. Photogr. Club, Tokyo, II, Chlamys(5) , figs. 6-8.

400

Koichiro MASUDA

1960. Swiftopecten swiftii (BERNARDI) : MASUDA, Sci. Rept., Tohoku Univ., 2nd Ser.
(Geol.), Spec. Vol. No. 4, p. 380, pl. 39,
figs. 9, 10.
l 960. Chlamys (Swiftopecten) swifti (BER·i'>ARDI) : HABE, Shirikishinai Mar. Bioi.
Inst., Hokkaido Gakugei Univ., Pub!.,
No. 2, p. 4, pl. 1, fig. 16, pl. 5, figs.
7, 8.
1962. Swiftopecten swiftii (BERNARDI) : MASUDA, Sci. Rept., Tohoku Univ., 2ndSer. (Geol.), Vol. 33, no. 3, p. 196.
1962. Swiftopecten swiftii (BERNARDI) : SAWADA, Mem. Muroran Inst. Techno/.,Vol. 4, no. 1, p. 73, pl. 1, fig. 3, pl. 2,
fig. 3, pl. 3, fig. 4.
1964. Chlamys (Swiftopecten) swiftii (BER·
NARDI) : KRISHTOFOVICH, Soviet Petrol.
Sci.-Res. Geol., Expl. Inst., 232, p. 143,
pl. 20, figs. 1, 2.
1965. Swiftopecten swiftii (BERNARDI) : l\\"AI,
Bull. Educ. Fac., Hirosaki Univ., No. 5,
p. 29, pl. 15, figs. 9, 10.
1966. Swiftopecten swiftii (BERNARDI) : UoZUMI, FUJIE and MATSUI, jour. Fac.
Sci., Hokkaido Univ., Ser. 4 (Geol.
Mineral.), Vol. 13, no. 2, p. 175, pl. 14,
fig. 2.
1967. Chlamys (Swiftopecten) donmilleri MAcNEIL, U.S. Geol. Surv. Prof. Paper 553,
p. 12, pl. 3, figs. 1, 4, 6.
1967. Chlamys (Swiftopecten) swiftii kindlei(DALL) : MAcNEIL, Ibid., p. 13, pl. 3,
figs. 5, 7-9.

Remarks:- The original description isquoted below for the sake of persons towhom the original work is inaccessible.
"Testa maxima, utrinque convexa, solidiuscula, nitida, elongata, valva superore costis nodosis, majoribus 5, munita;
nodis distantibus concentrice dispositis;
interstiis longitudinaliter radiatis, minutissime granularis, costis concentricis 5
graditim dispositis; valva inferiore vix
nodosa, regulariter radiatum sulcata;
auriculis valde inaequilateralibus; supra
nodosis, infra sulcatis."
The present species is characterized byits large and thick, posteriorly contorted
shell which forms an angle of about 70•
at apex and is much higher than long,four prominent round-topped radial ribs
with several, fine radial threads, twosubordinate radial ribs near submargins,
fine intercalary threads. rather conspi·
cuous concentric constrictions, very large
triangular anterior auricle and flat hinge
plate in the right valve. The left valve
is characterized by its five prominent,
round-topped radial ribs which are usually nodose and by its young shell which
is nearly flat or rarely a little concave
upwards.
By the re-examination of the type spe·cimen (U.S. Nat!. Mus., No. 499058) andnumerous topotype specimens, it is considered that Pecten (Chlamys) kindlei DALL
is a synonym of swiftii, because the con·vexity of the valves, low radial ribs andconcentric constrictions observed in kindlei are quite similar with those of swijtii.
Similarly the hypotype specimen (U.S.
Nat!. Mus., No. 164842) and the specimens
labelled as parmeleei (Dept. Geol., Stan·
ford Univ., No. 4838) from the" Wildcat"
Formation in the vicinity of Crescent
City, Northern California, are synonymsof swijtii.
Chlamys (Swijtopecten) donmilleri wasdescribed by MACNEIL (1967) from the
Miocene Yakataga Formation, Alaska,
based upon rubber casts. The morpho·
logical characters of the type specimens(U.S. Nat!. Mus., No. 644882, 644883,
644884) as observed by the writer coincide with those of Swiftopecten swijtii,
therefore, MACNEIL's donmilleri is a syno·
nym of Swiftopecten swiftii. But Chlamys(Swijtopecten) cf. donmilleri described by
MACNEIL (1967) from the Miocene Unga
Conglomerate, Alaska Peninsula can not
be identified with swijtii but with Chlamys cosibensis (YOKOYAMA) which is
known from the Miocene to Pliocene

602.

Swiftopecten

formations in Japan. For the Chlamys
cosibensis group another paper is expected to be written.
Swijtopecten swijtii resembles Chlamys
cosibensis (YOKOYAMA) and has been confused with it (MASUDA, 1959b). Also Chlamys etchegoini (ANDERSON), Chlamys nutteri (ARNOLD), Chlamys wattsi (ARNOLD)
and Chlamys wattsi morani (ARNOLD) described from the Pliocene deposits ofCalifornia resemble swiftii, which can be
distinguished from those species and cosibensis by its large, higher, posteriorly
contorted shell, smaller apical angle, triangular large anterior auricle and nearlyflat left valve in younger stage.
Type locality :-Northern Japan. Recent.
Geographical distribution :-Living inNorthern Japan, Sea of Okhotsk andalong East Korea.
Geological distribution:- Middle Miocene to Recent in Japan, Pliocene to
Recent in Sakhalin and Kamchatka, andMiddle (?) to Late Miocene to Middle
Pleistocene along the West Coast of
North .America.
Swiftopecten swiftii parmeleei(DALL, 1898)
Pl. 48, figs. 6, 7, Pl. 49, figs. 6-8.
1898. Pecten (Chlamys) parmeleei DALL, Trans.
Wagner Free Inst. Sci., Philadelphia,
Vol. 3, pt. 4, p. 708, pl. 37, figs. 14, a.
1906. Pecten (Chlamys) parmeleei DALL: ARNOLD, U.S. Geol. Surv. Prof. Paper, No.
47, p. 119, pl. 41, figs. 1, 1a.
1907. Pecten (Chlamys) parmeleei DALL: ELD·RIDGE and ARNOLD, U.S. Geo[. Surv.,
Bull., No. 309, p. 25, pl. 36, fig. 7.
1959. Pecten (Pallium) swiftii etchegoini ANDERSON: GLEN, Univ. Calif. Publ., Geol.
Sci., Vol. 36, no. 2, p. 167, pl. 15, fig. 6.
1959. Chlamys (Swiftopecten) swiftii parmeleei(DALL) : MAsUDA, Trans. Proc. Palae-

401

ont. Soc. japan, N.S., No. 34, p. 93.

Remarks:-The original description is" This species is close to P. Swiftii BER·
NARDI of Japan (J. de Conchyl., vii, plates
1 and 2, 1858) but smaller, and differs
by the smooth top surface of the ribs,
which in P. Swiftii are more or lessstriated or coarsely threaded, and by
the not alternated radial riblets on theright posterior ear; also, especially, by
the profuse coalescent microscopicallycheckered squamation, which makes acomplete external coating to the valve.
Alt. 45, lat. 38 mm ".
Parmeleei is characterized by its small
shell which is contorted posteriorly inthe younger stage but tends to becomerounded with growth, four prominent
but rather low, round-topped radial ribs
which are broader than their interspaces
with several, fine radial threads, twosubordinate radial ribs near submargins,rather conspicuous concentric constrictions, very large triangular auricle in
the right valve, and by the left valve
having five round-topped radial ribs.
Parmeleei differs from the closely related Swiftopecten swiftii in having smaller shell which tends to become roundedwith growth and somewhat larger apicalangle. Thus, morphologically, parmeleei
may have descended from swiftii and isconsidered a subspecies of swiftii.
From Chlamys cosibensis (YOKOYAMA)
parmeleei differs by its higher shell whichis posteriorly contorted in the younger
stage and triangular anterior auricle.
GRANT and GALE (1931) figured parmeleei from the Middle Pliocene deposits
at Holser Canyon, Los Angeles, California,
but their specimens should be identified
probably with Chlamys species. In 1950
WOODRING and BRAMLETTE illustrated
Chlamys parmeleei from the Pliocene
Careaga Sandstone, Santa Maria district,Koichiro MASUDA

402

California. However, according to thewriter's study of the hypotype specimen(U.S. Nat!. Mus., No. 560101) their parmeleei should be identified with Chlamys
etchegoini (ANDERSON). GLEN (1959) described Pecten (Pallium) swijtii etchegoinifrom the "Merced" Formation, San Mateo,
California, but the writer considers that
GLEN's specimen (Mus. Paleont., Univ.
Calif. Berkeley, No. 37614) should be
identified with parmeleei. In 1966 STANTON recorded parmeleei from the Late
Miocene Castaic Formation, Los Angeles,
California, but STANTON's specimen has
not been authenticated.
Type locality:- Pacific Beach, San Diego,
California.
Distribution:- Middle to Southern California. Middle Pliocene.
Remarks

As already pointed several species orsubspecies of the West Coast of North
America have been referred to Swiftopecten. However, among those species
the true Swijtopecten is represented onlyby the so-called kindlei and donmilleri
from Alaska, some of the so-called parmeleei from northern California, and parmeleei from middle to southern California, whereas the other species hitherto
referred to Swiftopecten should be referred to Chlamys or some other genera.
According to the writer's study of thetype specimen (Mus. Paleont., Univ. Calif.
Berkeley, No. 36639) of Swijtopecten adekunbiana ADEGOKE, 1969 which was firstdescribed as Swiftopecten sp. (ADEGOKE,
1967) and subsequently named adekunbiana, n. sp. from the Miocene Santa
Margarita Formation, California is different from Swiftopecten, because its
hinge area is characteristic to the genus
Lyropecten.
Also several species have been de-scribed as the varieties of swijtii fromthe Pliocene deposits of Sakhalin andKamchatka but considering from theirdescriptions and figures Swijtopecten in
Sakhalin and Kamchatka is represented
only by swijtii (s.s.).
As already pointed out (MASUDA, 1959a)some morphological differences such asconcentric constrictions or natures of theradial ribs of the left valve are observedin the specimens living in the northernareas and those living in more southernareas. These morphological features
may suggest that the specimens livingin the northern areas are somewhat lessinfluenced by the water temperaturethan those living in more southern areas.
And, the morphological differences observed between the fossil specimens andRecent ones may be the reflection of theenvironmental conditions such as thermal conditions. Such inference may beinterpreted that the so-called kindlei represents the northern type of swiftii andthat some of the so-called parmeleei from
northern California the rather southern
type of swijtii. Also the so-called donmilleri may represent the southern typeof swiftii.
As known at present the oldest occurrence of swiftii is the Middle Miocene
Otsutsumi Formation in the environs of
Sendai, Northeast Honshu, Japan, where
it is rather rare, and its associated molluscan fauna mainly consists of what we
now call temperate water elements, suchas Miyagipecten matsumoriensis MASUDA,
Chlamys kaneharai (YOKOYAMA), Dosinia
lwneharai YOKOYAMA, Mercenaria chitaniana (YOKOYAMA), Spisula voyi GABB,
etc. But with the progress of geological age swijtii gradually increased its
dominancy in association with the increase of cooler water molluscs, bryozoans, barnacles, foraminifers, etc. from
the Miocene through Pliocene to Recent.

602.

Swiftopecten

From the morphological differences observed between the Recent and fossil
specimens it is inferred that Swiftopecten
swiftii acquired its stability as a species
during the Middle Miocene and survived
to the Recent with little morphologicalvariation (MASUDA, 1959a, 1960).
On the other hand, the first appearance of Swiftopecten along the West
Coast of North America is the Miocene
Yakataga Formation in Alaska, whichyielded donmilleri; it is believed to be
Middle to Late Miocene in American
chronology (MACNEIL, 1967). As themorphological characteristics of donmilleri can be interpreted to represent thesouthern type of swiftii (MASUDA, 1959a),
it is inferred that the Yakataga Formation may have been deposited under the
influence of moderate to rather coolwater environmental conditions. Thisview is also supported by the associatedfauna (ADDICOTT et al., 1971).
It is thought that the occurrence of
Swiftopecten along the West Coast of
North America is a result of its migration from East Asia to North America.
Therefore, the writer considers that theYakataga Formation is at least not older
than the Otsutsumi Formation in Japan.
The changes of the environmental conditions from the Miocene to Recent(DURHAM, 1950, MASUDA, 1962b) probably
have greatly influenced the marine fauna.
As swiftii had acquired its stability asa species in the Middle Miocene (MASUDA, 1959a), it could survive to the Recent
in the northwestern Pacific region but
in the northeastern Pacific region it became extinct in the Middle Pleistocene.
As the results of the gradual changing
environmental conditions, it is inferredthat Swiftopecten parmeleei branched offfrom the Swiftopecten swiftii stock as aresult of its southward migration followed by localization and adaptation in the403

Middle Pliocene and it became extinct
at the end of Middle Pliocene. On theother hand, Swiftopecten swiftii extended
its distribution to northern California in
the Early Pliocene but ~ith the progressof geological age it retreated· to Alaska
and became extinct in the Middle Pleistocene. Therefore, it is expected thatswiftii will be found from the Plioceneor Pleistocene formations of the northern part of the West Coast of North
America and also from the Pliocene ofKamchatka. The geographical distribution of swiftii and parmeleei is shown in
Text-fig. 1.
MACNEIL (1943, 1967) reported Fortipecten from Alaska and the writer and
ADDICOTT (MASUDA and ADDICOTT, 1970)
recorded Yabepecten from the Early Pliocene Montesano Formation in Washington, and from the same formation thewriter described Mizuhopecten warreni,n. sp. (MASUDA, 1971). Therefore, theoccurrences of Swiftopecten, Fortipecten,
Yabepecten and Mizuhopecten in theW est
Coast of North America may be significant for interregional correlation between
Asia and North America. Those genera
are all known from the Cenozoic formation of Japan.
The occurrence of Swiftopecten swiftii
from the Middle Miocene formation in
Alaska suggests that the first Bering landbridge connecting North America andAsia was in the Middle Miocene. On
the other hand, MACNEIL (1967) considered that the Unga Conglomerate yielding Chlamys (Swiftopecten) cf. donmilleri
in the Alaska Peninsula represents theMiddle Miocene in American chronology,
but according to the writer's study MACNEIL's cf. donmilleri is a synonym ofChlamys cosibensis (YOKOYAMA) and ismorphologically a Pliocene type of cosibensis. Therefore, the geological age of
the Yakataga Formation is open toques-K8ichir6 MASUDA

404

Pacific Ocean

\.

150E

150W

Text-fig. 1.

Geographical distribution of Recent and fossil Swiftopecten.
e--Swiftopecten swiftii (BERNARDI) (Recent)0--Swiftopecten swiftii (BERNARDI) (Fossil)x --Swiftopecten swiftii panneleei (DALL)

tion. Although further studies on thestratigraphy and paleontology of theYakataga Formation are necessary tosettle this problem, the writer is inclined
to consider that a part of the formation
with donmilleri may represent the Late
Miocene or Early Pliocene. Consideringfrom the occurrences of Y abepecten, Mizuhopecten and Fortipecten from the Early
Pliocene formations of the northern West
Coast of North America, it may be thatthe Bering strait was closed by a landbridge during the Late Miocene or very
Early Pliocene.
References
ADEGOKE, O.S. (1967) : California Late Miocene records of Swiftopecten HERTLEIN,
1935. Veliger, Vol. 9, no. 3, pp. 337-339,
pl. 47.
- - (1969) : Stratigraphy and paleontologyof the marine Neogene formations of the
Coalinga region, California. Univ. Calif.
Pub!., Ceo!. Sci., Vol. 80, pp. 1-241, pis.
1-13, 6 text-figs., 3 maps.
ADDICOTT, W.O., KANNO, S., SAKAMOTO, K.
and MILLER, D.]. (1971) : CLARK's Tertiary molluscan types from the Yakataga
district, Gulf of Alaska. U.S. Ceol. Surv.

"'

'"'

12cfw

Prof. Paper 750-C, pp. Cl.8-C33, figs. 1-6.
ANDERSON, F.M. (1.905) : A stratigraphic
study of the Mount Diablo Range of California. Proc. Calif. Acad. Sci., Ser. 3,
Vol. 2, pp. 155-248, pis. 1.3-35.
ARNOLD, R. (1906) : Tertiary and Quaternary pectens of California. U.S. Ceo!.
Surv. Prof. Paper 47, pp. 7-146, pis. 1-53.
BERNARDI, M. (1858) : Description d'especes
nouvelles. jour. de Conch., Vol. 7, 2ndSer., T. 3, pp. 90-94, pis. 1-2.
CossMAN, M. and PEYROT, A. (1914) : ConchologieNeogenique deL'Aquitaine. TomeII, Pelecypodes. Act. Soc. Linn. Bord.,
pp. 1-496, pis. 1-26.
DALL, W.H. (1898) : Contributions to the
Tertiary fauna of Tampa and the Pliocene beds of the Caloosahahatchie River.
Trans. Wagner Free Inst. Sci., Philadelphia, Vol. 3, pt. 4, pp. 571-947, pis. 26-37.
- - (1920) : Pliocene and Pleistocene fossils
from the Arctic Coast of Alaska and the
Auriferous Beaches of N orne, Norton
Sound, Alaska. U.S. Ceo/. Surv. Prof.
Paper 125-C, pp. 23-37, pis. 4-5.
DuRHAM, J.W. (1950) : Cenozoic marine climate of the Pacific coast. Bull. Ceo!.
Soc. Amer., Vol. 61, pp. 1243-1264, 3 textfigs.
- - (1961) : Palaeogeographic conclusions inlight of biological data. "Symposium,
Pacific basin biogeography". 1Oth Pacific602.

Swiftopecten

Congress, pp. 355-365, 4 text-figs.
- - and MAcNEIL, F.S. (1967) : Cenozoic migrations of marine invertebrates throughthe· Bering Strait region, in HOPKINs,
D.M., The Bering land bridge, pp. 326-349,.
4 tables, Stanford Univ. Press.
·ELDRIDGE, G.H. and ARNOLD, R. (1907) : The
Santa Clara Valley, Puente Hills and Los
Angeles Oil districts, southern California.
Bull. U.S. Geol. Surv., No. 309, pp. 1-266,
pis. 1-41, 17 text-figs.
FAUSTMAN, W.F. (1964) : Paleontology of the
Wildcat Group at Scotia and Centerville
Beach, California. Univ. Calif. Publ., Geol.
Sci., Vol. 41, pp. 97-151, pis. 1-3, 7 textfigs.
FUJIE, T. (1958) : Pleistocene molluscan fossils (Pelecypoda) from the Shikonai Formation, Hokkaido. Cenozoic Res., No. 28,
pp. 663-679, pis. 27-28.
GLEN, W. (1959) : Pliocene and Lower Pleistocene of the western part of the San
Francisco Peninsula. Univ. Calif. Publ.,
Geol. Sci., Vol. 36, no. 2, pp. 147-198, pis.
15-17, 5 text-figs.
GRANT, U.S., IV, and GALE, H. (1931) : Catalogue of the marine Pliocene and Pleistocene Mollusca of California and adjacentregions. Mem. San Diego Soc., Nat. Hist.,Vol. 1, pp. 1-1036, pis. 1-32, 15 text-figs.
HABE, T. (1955) : Fauna of Akkeshi Bay, 21,
Pelecypoda and Scaphopoda. Pub!. Akkeshi Mar. Bioi. Stat., No. 4, pp. 1-31, pis.
1-7.
- - (1958) : Report on the Mollusca chiefly
collected by the S.S. Soyo-maru of theImperial Fisheries Experimental Stationon the continental shelf bordering Japan
during the years 1922-1930. Part 3. Lamellibranchia (1). Pub!. Seto Mar. Bioi. Lab.,
Vol. 6, no. 3, pp. 241-279, pis. 11-13.
- - (1960) : Fauna of shell-bearing mollusksof the sea around Shirikishinai, Hokkaido. 1. Pelecypoda. Fauna and flora of thesea around the Shirikishinai Marine Station. Shirikishinai Mar. Stat. Bioi. lnstr.,
Hokkaido Gakugei Univ., No. 4, pp. 1-10,
pis. 1-5.
HERTLEIN, L.G. (1935) : The Templeton
Crocker Expedition of the California

405

Academy of Sciences, 1932. Proc. Calif.
Acad. Sci., Ser. 4, Vol. 21, no. 25, pp.
301-328, pis. 18-19.
ILYINA, A.P. (1963): Mollusks in the Neogene of Kamchatka. Soviet Petrol. Sci.Res. Geol. Expl. lnst., 202, pp. 1-242, pis.
1-54.
IWAI, T. (1965) : The geological and paleontological studies in the marginal areaof the Tsugaru Basin, Aomori Prefecture,
Japan. Bull. Educ. Fac., Hirosaki Univ.,
No. 15, pp. 1-68; pis. 12-20, 3 text-figs.,
10 tables.
.
KASENO, Y. and MATSUURA, N. (1965) : Pliocene shells from the Omma. Formation
around Kanazawa City, Japan. Sci. Rept.
Kanazawa Univ., Vol. 10, no. 1, pp. 27-62,
pis. 1-20, 3 text-figs., 5 tables.
KEEN, A.M. and BENTSON, H. (1944) : Checklist of California Tertiary marine Mollusca. Geol. Soc. Amer., Spec. Paper, No.
56, pp. 1-280, 4 text-figs.
KHOMENKO, l.P. (1934) : The stratigraphy of
the Tertiary beds of the south-western
coast of the Schmidt Peninsula (Northern
Sakhalin). Trans. Geol. Oil Inst., Ser. A,
Fasc. 40, pp. 12-86, pis. 1-19.
KINOSHITA, T. and IsAHAYA, T. (1934): Catalogue of marine Mollusca from Hokkaido.
Rept. Fish. Surv. Hokkaido Fish. Exp. Stat.,No. 33, pp. 1-19, pis. 1-15.
KocHIBE, T. (1882) : Johoku Chishitsu Hen(Geology of Northern Hitachi), Rika Kaishi, Tokyo Univ. Press, No. 4, pp. 1-153,
pis. 1-9.
KRISHTOFOVICH, L.V. (1964) : Mollusks in
the Tertiary sediments of Sakhalin .. Soviet
Petrol. Sci.-Res. Geol. Expl. lnst., 232, pp.
1-343, pis. 1-55.
KuLJOTA, K. (1950) : Explanation of Cenozoic
fossils from northern Japan, 9. Fossil
Pectinidae from the Setana Series. Cenozoic Res., No. 6, pp. 12-18, pis. 8-9.
KUsTER, H.C. and KoBELT, W. (1882): Die
Gattungen Spondylus und Pecten in MARTINI und CHEMNITZ, Syst. Conch. Cab.,
Vol. 7, pt. 2, pp. 1-296, 72 pis.
MAcNEIL, F.S. (1967) : . Cenozoic pectinids of
Alaska, Iceland and other northern regions. U.S. Geol. Surv. Prof. Paper 553,

406

Koichiro MASUDA

pp. 1-57, pis. 1-25.
- - (1970) : New Pliocene Chlamys (Swiftopecten) and Beringius from the Alaska
Peninsula. Nautilus, Vol. 84, no. 2, pp.
69-74, 1 pl.
- - , MERTlE, ].B. Jr. and PILSBRY, H.A.
(1943) : Marine invertebrate faunas of
the buried beaches near Nome, Alaska.
jour. Paleont., Vol. 17, no. 1, pp. 69-96,
pis. 10-16.
- - , WoLFE, ].A., MILLER, D.]. and HoPKINS, D.M. (1961) : Correlation of Tertiary formations of Alaska. Bull. Amer.
Assoc. Petrol. Geol., Vol. 45, no. ll, pp.
1801-1809, 2 text-figs.
MASUDA, K. (1959a) : On the Miocene Pectinidae from the environs of Sendai: Part
14, On Pecten swiftii BERNARDI. Trans.
Proc. Palaeont. Soc. japan, N.S., No. 34,
pp. 101-111, pl. 9, 1 text-fig.
- - (1959b) : On the Miocene Pectinidae fromthe environs of Sendai : Part 15, Pecten
cosibensis YoKOYAMA and its related species. Ibid., No. 35, pp. 130-141, pl. 13, 1
text-fig.

--------- - (1960) : On morphogenesis of Nanaochlamys. Sci. Rept., Tohoku Univ., 2ndSer. (Geol.), Spec. Vol. No. 4, pp. 371383, pl. 39, 10 text-figs.
- - (1962a) : Tertiary Pectinidae of Japan.
Ibid., Vol. 33, no. 2, pp. 117-238, pis. 1827, 11 text-figs.
- - (1962b) : Note on the Tertiary Pectinidae of Japan. Ibid., Spec. Vol. No.5, pp.
159-193, 9 text-figs., 9 tables.
- - (1971a) : On some PatinDpecten from
North America. Trans. Proc. Palaeont.
Soc: japan, N.S., No. 83, pp. 166-178, pis.
19-21, 2 text-figs.
- - (1971b) : Amussiopecten from North America and northern South America. Ibid.,
No. 84, pp. 205-223, pis. 25-26, 4 text-figs.
- - and ADDICOTT, W.O. (1970) : On Pecten(Amusium) condoni HERTLEIN from theWest Coast of North America. Veliger,
Vol. 13, no. 2, pp. 153-156, 1 pl.
NoMLAND, ].C. (1917) : The Etchegoin Pliocene of Middle California. Univ. Calif.
Pub!., Geol. Sci., Vol. 10, no. 14, pp. 109254, pis. 1-12, 2 text-figs.

···-~------------------------------------

Explanation of Plate 48(Natural size)
Right valve
Figs. 1-5. Swiftopecten swijtii (BERNARDI).
1, Dept. Geol., Stanford Univ., No. 4846. Loc.: Intermediate Beach, Nome, Alaska. Middle
Pleistocene.
2, IGPS*, coli. cat. no. 90593. Loc.: About 300m NW of Kurosawa, Akita City, Akita
Prefecture. Sasaoka Pliocene.
3, 4, Saito Ho-on Kai Mus., Reg. no. 21266. Loc.: Tayazawa, Wakimoto-machi, Oga City,
Akita Prefecture. Shibikawa Pliocene.
5, Dept. Geol. Stanford Univ., No. 4838. Loc.: Crescent City wharf, Del Monte County,
California. "Wildcat" Pliocene.
Figs. 6, 7. Swiftopecten swiftii parmeleei (DALL).
6, Dept. Geol., Stanford Univ., No. 47210. Loc.: East of Capitola, Santa Cruz County,
California. Purisima Pliocene.
7, Los Angeles County Museum. Loc. : South central part of San Diego County, California.
San Diego Pliocene.
*-Institute of Geology and Paleontology, Tohoku University, Sendai, Japan.

MASUDA:

Sw1}'topecten
Plate 487

602.

Swijtopecten

NOMURA, S. and HATAI, K. (1935) : Pliocene
Mollusca from the Daishaka shell beds inthe vicinity of Daishaka, Aomori-ken,
Northeast Honshu, Japan. Saito Ho-on
Kai Mus., Res. Bull., No. 6, pp. 83-137,
pis. 9-13.
OYAMA, K. (1959) : The molluscan shells, II,
Chlamys (5). Sci. Photogr. Club, Tokyo.
PHILIPPI, H.A. (1900) : Beitrage zur Morphologie und Phylogenie der Lamellibranchier. II. Zur Stammesgeschichte der Pectiniden. Zeit. Deutsch. Ceo/. Cesellsch.,
Bd. 52, pp. 64-117, 24 text-figs.
SAWADA, Y. (1962): The geology and paleontology of the Setana and Kuromatsunai
areas in southwest Hokkaido, Japan. Mem.
Muroran lnst. Techno!., Vol. 4, no. 1, pp.
1-110, pis. 1-8, 9 text-figs., 13 tables.
SCHRENCK, L. (1867) : Mollusken des AmurIandes und des nordjapanischen Meeres.
Reisen und Forshung Amurlande in dem
1854-1856. Vol. 2, pt. 3, pp. 259-976, pis.
12-28, 1 map.
SLODKEWITSCH, W.S. (1938) : Tertiary Pelecypoda from the Far East. Pts. 1 & 2.
USSR Acad. Sci., Paleont. Inst., Paleont.
of USSR, Vol. 10, pt. 2, fasc. 19, pp. 1275, pis. 1-106.
STANTON, R.J. (1966) : Megafauna of theUpper Miocene Castaic Formation, Los
Angeles County, California. jour. Paleont.,
Vol. 40, no. 1, pp. 21-40, pis. 5-7, 2 textfigs.

Akita
Kaidateno-sawa
Kurosawa
Oga
Otsutsumi
Sa do-gun
Sasaoka~LI:f:kfl Jr. iR

lJ3

iR
UE

-j(

~

!R.

t!r.
i/Jf. 'lf~,..,,.
·w:
fliU

407

ToMIZAWA, T. (1958) : Studies on fossils
from the Kami-Minochi district, Nagano
Prefecture, in T. and K. YAGI, Geologyof Kami-Minochi-gun, Nagano Prefecture.
pp. 317-347, pis. 1-14, 5 text-figs., 2 tables.
UozuMI, S., FuJIE, T. and MATSUI, M. (1966) :Neogene molluscan fauna in Hokkaido.
Part 3, Description of the Ainonai fauna
associated with Desmostylus cf. minor
NAGAO, from Kitami district, East Hokkaido. jour. Fac. Sci., Hokkaido Univ.,
Ser. 4 (Ceo/. Mineral.), Vol. 13, no. 2,
pp. 119-183, pis. 14-15, 3 text-figs.
WooDRING, W.P. and BRAMLETTE, M.N.
(1950) : Geology and paleontology of the
Santa Maria district, California. U.S.
Ceo/. Surv. Prof. Paper 222, pp. 1-185, pis.
1-23, 9 text- figs.
YAMA:v!OTO, G. and HABE, T. (1959) : Faunaof shell-bearing mollusks in Mutsu Bay.
Lamellibranchiata (1). Mar. Biol. Station
Asamushi, Tohoku Univ., Bull., Vol. 9, no.
1, pp. 1-20, pis. 1-5.
YoKOYAMA, M. (1911) : Pectens from Koshiba Neogene. Ceo!. Soc. Tokyo, jour., Vol.
18, no. 208, pp. 1-5, pl. 1.
- - (1926) : Fossil shells from Sado. jour.
Fac. Sci., Imp. Univ. Tokyo, Vol. 1, pt. 8,
pp. 249-312, pis. 32-37.
YosiiiWARA, S. (1902) : Japanese shells. Zoo/.
Mag. Tokyo, Vol. 14, n0. 162, pp. 141-145,
pis. 1-5.

Sawada-machi
Sa waneShibikawaTayazawa
Tomizawa
Wakimoto-machi

iH~IliiBJ

iR

tR

Jll
fi.ffl
III :t:l- iR

rniRn.;pt: IBJ

408

K6ichiro MASUDA

Explanation of Plate 49(Natural size)
Left valve
Figs. 1-5. Swiftopecten swiftii (BERNARDI).
1, Dept. Geol., Stanford Univ., No. 4846. Loc.: Intermediate Beach, Center Creek, Nome,
Alaska.
2, Saito Ho-on Kai Mus., Reg. no. 16827. Loc.: Tomizawa, Wakimoto-machi, Oga City,
Akita Prefecture. Shibikawa Pliocene.
3, 4, Dept. Geol., Stanford Univ., No. 4838. Loc. : Crescent City wharf, Del Monte County,
California. "Wildcat" Pliocene.
5, IGPS, coli. cat. no. 90597. Loc. : Kaidate-no-sawa, Sawada-machi, Sado-gun, Niigata
Prefecture. Sawane Pliocene.
Figs. 6-8. · Swiftopecten swiftii parmeleei (DALL).
6, 8, Los Angeles County Museum. Loc.: 305 A. South central part of San Diego County,
California. San Diego Pliocene.
7, IGPS, coli. cat. no. 92043. Loc. : Tijuana River south western San Diego County,
California. San Diego Pliocene.

MASUDA:

Swijtopecten

Plate 49

Trans. Proc. Palaeont. Soc. Japan, N.S., No. 87, pp. 409-413, September 30, 1972603.

SCAPHOPODA-LIKE FOSSILS FROM THE UDO FORMATION(MIOCENE) OF MIYAZAKI PREFECTURE, JAPAN*
KOTORA HAT AI, HIROSHI NODA
and KENSHIRO OGASAHARA
Institute o~ Geology and Paleontology, Faculty of Science,
Tohoku University, Sendai, Japan'E'(~eyl!,~ 9=JW!illl:!l\~Ff 1'.'1 iiU1~1JEJ'Ltoldl::t:dc -:>v' -c : 'll~f.i y;uc a:; <3Ei~T <S 'liiw~/l'ill¥'0) ,·r,~jfrl
Cf¥it\!ltil!Ji!X) J!,tTrtllf'J: SHuTo (1961) vu: 'JAA~Phio))(JT:Jitll/\'lcrrn15~h-cv'<S, 4-IITI. 7-Xli
rflll\1)0) '/IV H':· J: f)- J~. JF:ilJEL"l. t:flC Dentalium lCJ:Ji(J;J,-j <511::1-i~~~t*~ L, C.ft.~f"(l1NU:,!'!11<~10)

Dentalium, Terebrellina <b<Sv'v'J:, Makiyama ~~lH!Z~~tLf-::i.J~. ;:.;h,G cf'J:, ~~Jdl::,:fiO)',iJ!:1!l, -tt1 7-:,

~illJO)f.'W'f,

jl!ijil;/,i;'HIO)!j"#f~&.

:JI,tii1filld5"t1J,

e-:>-?%iC:·JPtt.~: fJ,

tr L 0,Ditrupa lC~Jift( L, J::)!tO) ~~N&f'J: 7-.Xllfillf~fflifif!i.J> Ditrupa vcl,li;-9 <S.::. c ~iftTt0)<: &:> <S, Lh · L Ditrupa O)P;t1~filHc f'J:~X=GniiMilliO)f,"Jd.~:t"fi~~ t--::> {, O)n>t.~: <, Ditrupa
miyazakiensis, n. sp. c L -c IKlllJ ~ ht-=:o~fll :Ji: ;J, J}i'. • rrrf ill 15 QJ • 1h '1E J)l"( )/§. l!LI R!>

sociate Professors Takehiko Iw AI, Birosaki University, Taisuke TAKAY ASU, Akita University, Tamio KOTAKA, Tohoku
University, Saburo KANNO, Tokyo University of Education, Hiroyuki OTSUKA,
Kagoshima University; Junji ITOIGAWA,
Nagoya University, Kiyotaka CHINZEI,Tokyo University, and Sakae OHARA,
Chiba University, Drs. Yasuhide IWASAKI, Tokyo University, Kazuo OKAMOTO,
Hiroshima University, and Mr. Kimihiko
OKI, Kagoshima University.

Introduction and acknowledgements

During the excursion for observations,discussions and collection of the invertebrate marine fossils of different stratigraphic units of Mizuho age distributedin Miyazaki Prefecture, Kyushu, Japanin the latter part of October, 1971, abundant scaphopod-like fossils were collected
and brought back to the laboratory forstudy. These form the subject of thepresent article.
Here the writers express their deep
appreciation to the undermentioned persons for their kind cooperation in thefield and talks during the evening, namely ; Professors Tokio SHIKAMA, Yokohama
National University, Koichiro MASUDA,
Miyagi College of Education, and Shozo
HAYASAKA, Kagoshima University; As-

Fossil locality and stratigraphic
position

The abundant scaphopod or Dentaliumlike specimens were collected from asiltstone of a road cliff south of Uzutsumi near the Kagamisu-toge (pass) on
the road leading from Nagayama to Kogochi, south of Kiyotake, Kiyotake-cho,* Received Jan. 23, 1972; read June 3, 1972
at Utsunomiya.

409

410

Kotora HATAI, Hiroshi NODA and Kenshiro OGAS'AHARA

Miyazaki-gun, Miyazaki Prefecture. The
siltstone is a part of the Boroishi Member of the Udo Formation (Miocene) andalso of the Aoshima facies of the Miyazaki Group of SHUTO (1961).
The fossil locality of the scaphopod
or Dentalium-like fossils nearly corresponds to locality no. 12 or 13 of SHUTO(1961). SHUTO (op. cit.) recorded fromthe locality (no. 12 and no. 13) such fossil molluscs as, Acila (Acila) submirabilis
MAKIY AMA, Saccella confusa kongiensis
OTUKA, Yoldia (Tepidoleda) naganumana(OTUKA), n. subsp., Paliolum (Delecto~
pecten) peckhami (GABB), Amussiopecten
iitomiensis (OTUKA), ]oanisiella cumingii(HANLEY), Laevicardium pigmaea SHUTO,
V epricardium kyushuense SHUTO, V entricoloidea foveolata miyazakiensis (SHUTO), Pitar sp., Paphia (Paphia) exilis takaokaensis SHUTO, Clementia (Clementia)
papyracea (GRAY).
These fossils, all marine in origin,
were considered to be Miocene in age
by SHUTO (op. cit.) and to characterize
the Boroishi Member, the lowest part of
the Udo Formation. The scaphopod-likefossils, although from most probably thesame cliff from where SHUTO recorded
the fossil molluscs mentioned above, did
not occur in association with the molluscs. Although from the same lithofacies as the molluscs, the scaphopodlike fossils were found forming a close
assemblage separated from the nearest
molluscan fossil both vertically and laterally by a distance of more than several ten centimeters.
The stratigraphic subdivision of the
Miyazaki Group according to SHUTO(1961) is reproduced in Table 1, for thesake of the readers.
The scaphopod-like fossils
The scaphopod-like fossils were foundin the siltstone facies of the Boroishi
Member of the Udo Formation. The
tubular fossils were found in a position
almost parallel with the bedding planeof the stratum preserving them. Noneof the calcareous tubular structures were
found to be either vertical or oblique tothe bedding plane at least where they

Table 1. Stratigraphic subdivision of the Miyazaki Groupaccording to SHUTo (1961).
Tozakibana M.

Kibana

Togo
·M.
I
I
I

I

.---'t---1..----.....L--..,L::------\-- .......: ..L- -~'"4"o:',---

Gonobaru""1,. ' ' l\L+.';. __~

603 .

Scaphopod-like fossils

411

Text-figs. 1, 2. Ditrupa miyazakiensis HATAI, No DA and 0 GASA HARA. Na tural size.
Tex t-fig. 1- weathered specimens . Tex t-fig. 2- well preserve d specimen showing annu lar
growth, other showing irregular growth.

could be determined as buried in their
original position, which is parallel withthe sea bottom on which they li ved, andon which they crawled over. In thisrespect they may be of value in determination of the inclination and top or
bottom of the strata in which they occur.
The non-association of the scaphopodlike or annelid tubes with other kindsof invertebrate fossils may be d ue tothat the larvae of molluscs, foraminifers
and other kinds of marine life form apart of their food chain.
The tubular specimens showed randomorientation of their shells, but all that
could be observed were preserved horizontall y throughout a thickness of about
ten to fifteen centimeters of siltstone,
the state of preservation was different
according to whether exposed or embedded , none were seen lying across one another a lthough many were in close position, none so far as observed exceeded
25 mm in length, andn one were found inassociation with fossils of bivalves, gastropods or scaphopods or other inve rtebrates. A ll of the tubular structures areshort, measuring up to about 20- 25 mm
in length and about 1- 1.3 mm in diame-ter, gently curved , both ends open, thesurface rather smooth, irregulary wrinkled or more or less annular, all brownish
colored, consistin g of calcium carbonate,
and none were found to be straight or
entirel y smooth throughout their length .
In genera l curvature the present specimens resemble D entalium (L aevidenta lium ) C01"USCU1n PILSBRY, described andillustrated by KURODA and KIKUCHI (1933,
p. 10, pl. 1, fig. 1) from Toyama Bay,
Toyama Prefecture, but the curvature isstronger and the shell is more strongly
polished in coruscum compared with thepresent fossil. The fossi l a lso resembles
Dentalium ( L aevidentalium) toyamense
KUROD A and KIKUCHI (1933, p. 11, pl. 1,
figs. 5, 6) from To yam a Bay, but the she ll
is smaller, more strongly curve d and thegrowth is more irregular than the Recent
species of KURODA and KIKUCHI.
In general size and shape, the present
fossi l resembles Den taliwn ophiodon DALL(HE NDERSON, 1920, p. 84, pl. 14, fig. 2) but
differs in having stronger and less oblique annu lation s on the shell.
The Miyazaki specimen also resembles the worm tube from Proctor Creek,
Snohomish County, Washington, illus-

412

Kotora HATAI, Hiroshi NODA and Kenshiro OGASAHARA

trated by DANNER (1955, fig. 3), but ismore strongly curved and shorter inlength. It is also similar to Tereb1·ellina
shikokuensis KA TTO (1960, p. 328, pl. 34,
figs. 1, 3, pl. 35, fig. 7) from the Eocene
Naharigawa Formation at Kannoura,Toyo-cho, Aki-gun, Kochi Prefecture, andalso the same species (KA TTO, op. cit.)from the Eocene Muroto Formation at
Nabae, Muroto City, Kochi Prefecture,
but differs from them in the smaller size,
Jess curvature of the tube and more
prominent external sculptu•re of the shell.
Hyalinoecia tubicola illustrated by HERSEY (1967, p. 239, figs. 22-23, p. 240, figs.
22-24) from Dalaware Bay in 450 m depth(former) and from Chesapeak Bay in 365
m depth (latter), also resembles the present fossil specimens but the Recent
species· is longer and straighter than thefossil one.
The genus Ditrupa BERKELEY, 1835,
figured by HOWELL (1962, p. W156, fig.
97-4) is very closely similar to the present fossil, which has stronger concentric wrinkles or annulations on the surface. The type species of Ditrupa, D.
cornea (LINNE) is stated to come fromthe Pliocene of Italy (HOWELL, op. cit.)
and to contain Dentalium corneaum LINNE
and Dentalium subulatum DESHA YES as
its synonyms. The characters distinguishing the present fossil from Ditrupa
cornea (LINNE) illustrated by HOWELL(op. cit.) are considered sufficient for the
proposal of a news pecies, which is here
named miyazakiensis, after the geographic name of its occurrence. Miyazakiensis can be distinguished from the different kinds of fossils mentioned above
which show resemblance with it by thefeatures already mentioned. There seems
to be little chance for the present fossils
being mistaken from detached parts ofthe sponge known as Makiyama chitanii(MAKIYAMA) (=Sagarites) (DELAUBEN-

FELS, 1955, p. E39; MAKIY AMA, 1931, p.
5, figs. 1, 2). Makiyama is widely dis·tributed in the Miocene and Pliocene
marine deposits of Japan, and wherever,it occurs, it is always found as isolated,
sporadic rods with squarely rounded terminals, generally more or Jess flattened
and often creased longitudinally along
its middle part. The terminal parts of
the Makiyama short rods never taper
towards one end, never consist of calcareous material, and usually do notoccur in clusters, although the rods areusually found in a position parallel withthe bedding plane of the strata in which
they occur. Under the microscope Makiyama is spiculate. The just mentioned
characters serve to easily distinguish
Ditrupa miyazakiensis from Makiyama
chitanii. Also since the genus Dentalium
or Siphonodentalium consists of shells
made of aragonite (SHROCK and TWENHOFEL, 1953, p. 362), they will not be
misidentified for the shells of an annelid
tube, which consist of calcium carbonate.

References cited
DANNER, W.R. (1955) : Some fossil worm tubes
of western Washington. Rocks and Minerals, pp. 451-457, 7 figs.
DELAUBENFELs, M. W. (1955) : Treatise on
invertebrate paleontology, Edited by R.C.
MooRE, Geol. Soc. America and Univ.
Kansas Press, Part E, Archaeocyatha andPorifera, pp. 1-122, 89 figs.
HENDERSON, J.B. (1920) : A monograph of
the East American scaphopod mollusks.
U.S. Nat. Mus., Bull., no. 111, pp. 1-177,
pis. 1-20.
HERSEY, }.B. (1967) : Deep sea photography.
johns Hopkins Press, 310 pp.
HowELL, B.F. (1962) : Treatise on invertebrate paleontology, Edited by R.C. MooRE,
Geol. Soc. America and Univ. Kansas Press,
Part W, Worms, pp. 144-177, figs. 85-108.
KATTO, J. (1960) : Some Problematica from603.

the so-called unknown Mesozoic strata of
the southern part of Shikoku, Japan. Sci.

Repts., Tohoku Univ., 2nd Ser., Geol.,Spec. Vol., no. 4, pp. 323-334, pis. 34-35.
KuRODA, T. and KIKUCHI, K. (1933) : Studies
on the molluscan fauna of Toyama Bay(1). Venus (Japan. jour. Malac.), vol. 4,
no. 1, pp. 1-14, pl. 1. (in Japanese withEnglish Resume).
MAKIYAMA, J. (1931) : Stratigraphy of the
Kakegawa Pliocene in Totomi. Mem.,

Aki-gun
Aoshima
BoroishiKannoura
Kagamisu-toge
Kiyotake
Kogochi*- IIhnil
1;;

l'l

)l)(

:fi

Ffl

iill

~ iJ« lhii

iflt

J1t

,J, iiiJ r"J

413

Scaphopod-like fossils

Colt. Sci., Kyoto Imp. Univ., Ser. B, vol.
1, art. 1, pp. 1-53, pis. 1-3, figs. 1-4.
SHROCK, R.R. and TwENHOFEL, W.H. (1953) :Principles of invertebrate paleontology.
MacGraw-Hill Book. Co. Inc., New York,
Toronto, London, pp. 1-816.
SHUTO, T. (1961) : Palaeontological study of
the Miyazaki Group-A general accountof the faunas-. Mem. Fac. Sci., Kyushu
Univ., Ser. D, Geol., vol. 10, no. 2, pp.
73-206, figs. 1-23, tabs. 1-5, pis. 11-13.

MurotoNabae
Nagayama
Naharigawa
Toyo-cho
Udo

:4?:

p

;w~

1:.
iJJ

7k

*~ifljJII

Jti:illliT~[=iTr_ans. Proc. Palaeont. Soc. Japan, N.S., No. 87, pp. 414-428, pis. 50, 51, September 30, 1972

604.

PERMO-CARBONIFEROUS ENDOTHYRACEANS FROM JAPAN*
PART 1. BISERIAMMINIDAEYU JI OKIMURA
Institute of Geology and Mineralogy, Hiroshima University:;1s:#'i)r1R Endothyraceans O)jiJB'E : Endothyracean foraminifera Vi l.l HiP G ts. IJ,
tlj:,f-tf&!\IJO) m'}l:.fs_7];iflft1"1 c ~ ~v-c "' .Q ;?;, I;' ':l: t.:l::: :;js:;!'J;::::.:t;:t .Q.f:O)J'5~~l'i1f c;;, ['Joll?;Jl,"t'i;'fS.v'o Jf,;:'}.[);?>GO) biseriamminids O)f,[{f!ffir'i tl/)"t'"(:·(li;,IJ,

i:O)f4-0)~;icil&!ID:a:­lf:Hli L- "t' itTl!fiFP¥:s'{'®~R :a:-41H*1F.;!, Lt.:o =E c L- "t' rN~JJ:t!r1;0)::l::W:EEk:EJii'i (lliiJ~·. ·,'i'i~R • 'f:ki'O iP G, ~lobivalvulina 1:::/,'il-t .Q (ftl!.O) 21m Biseriammina, Olympina f;J:*§£ 5',!) 7f!ll;
G. kamenszs, G. granulosa compressa, G. mosquensis, G. sp. cf. G. kantharensis, G.
sp. cf. G. gracea, G. regularis n. sp., G. sp. A, G. sp. B l2~~llix L- "(', ;tjs:;/'[)O)J_:. Ttff>
E~*O)!JE:3'\'-, ;: c f:::_i:.~II:W!R*Tl~llf:::.:t;lt 0 itE~Ji"·"NI''Jts.Mf.RHR G;?,f;:: L- t.:o ':l: t.:,r~lfl±'ri\"i tjfL;fo' J: Lf1:11Jd':-O)~~i1'1: U'U.l\~JU.Jtf;:: "?I;'"(' 1(, li}f)'E Lt.:ojrp .H ift=

the Biseriamminidae from Japan treating mainly the Carboniferous specimensfrom the thick limestones of Taishaku
Akiyoshi, Atetsu and Koyama of th~
Chugoku Region, the Kakisako formation of the Kuma Massif, Kyushu Region,and the Nagaiwa formation of the Kitakami Massif, Tohoku Region. The Permian specimens are also examined fromthe Taishaku and Atetsu limestones inorder to compare with Carboniferous
ones morphologically and to make clear
the stratigraphic distribution.
All the specimens from the above limestones belong to Globivalvulina, a genusof the Biseriamminidae. As is shown by
RAUSER-CHERNOUSSOVA and REITLINGER(1957), Globivalvulina appears in the upper
Lower Carboniferous and becomes extinct
in the Upper Permian, thriving extremelyin the lower Upper Carboniferous. Accordingly the frequency of globivalvulinid foraminifera may offer some important data to the boundary problem
between the Lower and Upper Carboni-

Introduction

It is well known that some of theendothyracean foraminifera have been
accepted valuable index fossil in the latePaleozoic. According to Treatise on
Invertebrate Paleontology (Edit. MOORE,
1964, pp. 329-358), the superfamily Endothyracea is organized by eleven families;
Nodosinellidae, Colaniellidae, Ptychocladiidae, Palaeotextulariidae, Semitestulariidae, Tetrataxidae, Biseriamminidae,
Tournayellidae, Endothyridae, Archaediscidae and Lasiodiscidae. Among them,
the biostratigraphical significance ofEndothyridae and Palaeotextulariidae
has been passably established on thebasis of their paleontological study.
However, the study of the other families
may be said to be insufficient, especiallyin Japan.
This report is the first description of* Received Jan. 24, 1972; read Jan. 23, 1972
at Chiba.

414

604.

Permo-Carboniferous endothyraceans

ferous of Japan.
Acknowledgements:-The writer wishes
to express his sincere thanks to Professor Akira HASE of Hiroshima University
who constructively advised him andkindly revised the manuscript. Thanks
are due to the research members ofstratigraphy and paleontology of thesame university for their helpful dis·cussions. Financial aids for this study
were partly granted by the Ministry of
Education.
Repository:- All the specimens described and figured in this paper are
kept in the Institute of Geology andMineralogy, Hiroshima University, Japan.
Their register numbers are indicatedwithin the brackets in the explanationof plates.

Paleontological and biostratigraphicalnotes on the family Biseriamminidae
and the genus Globivalvulina

The family Biseriamminidae was first
proposed by CHERNYSHEVA (1941) withthe type-genus Globivalvulina, but hisclassification is not always followed after
that. For instance, PLUMMER (1948) studied in detail the morphology of Globivalvulina, and said that it would beplaced in the family Cassiduliniidae by
the nature of a biserial arrangement ofchambers in a planispiral coiling, eventhough the aperture of this Paleozoic
form is not harmonious with those of
the rest of the family. CusHMAN and]ONES (1950) followed BRADY's classification (1876) which placed this genus in
the Trochamminidae characterized witha trochospiral coiling. REITLINGER (1950)
newly established the subfamily Globivalvulinae, and included it in the family
Tetrataxidae by the characteristics ofbiserial chamber arrangement, trocho-

415

spiral shell and two-layered wall. According to Osnovy Paleontologii (Edit.
RAUSER-CHERNOUSSOV A and FURSENKO,
1959) Globivalvulina is again attached to
the Biseriamminidae.
Such confusion on the taxonomy ofGlobivalvulina is chiefly caused by somedifference of worker's subjective ·view
with regard to the coiling form and wall
structure; that is to say, it is a question
whether the test is planispiral or trochospiral, and whether the wall is agglutinate or undifferentiated microgranularor layered. In this paper the writer
follows the classification of Treatise on
Invertebrate Paleontology. According toit, the diagnosis of Biseriamminidae(synonymous with Globivalvulinae REITLINGER, 1950; and Globivalvulininae
PoKORNY, 1958) is as follows: Test enrolled planispirally to slightly trochospirally, chambers biserially arranged,
involute, aperture opens. at inner borderof septal face.
The family Biseriamminidae consistsof three genera; Biseriammina from the
middle Tournaisian of South Ural (CHERNYSHEVA, 1941), Olympina from the Permian of Cyprus (REICHEL, 1945) and thetype-genus Globivalvulina. The first andthe second are monotypic, and there isnothing to be mentioned on their biostratigraphical significance.
SCHUBERT (1921) proposed Globivalvulina for the " Globigerina-like" Paleozoic
foraminifera, designating briefly V alvulina bulloides BRADY as the type-species,
but he did not defined it in detail. According to the emended definition ofTreatise on Invertebrate Paleontology, thebasic characters of the genus are summarized as follows: Subglobular to hemispherical test, planispirally to slightly
trochospirally coiled ; biserially arranged
chambers; microgranular calcareous wallwith some inner fibrous layers ; aperture416

Yuji OKIMURA
Table 1.

Stratigraphic distribution of the species ofGlobivalvulina previously described.
Up. Carbon.

Low
Car b.

G. biserialis CusH. & WATERS
G. bristolensis REITLINGER
G. bulloides (BRADY)*G. cora HARLTON

low.

up.

mid.

I Perm.
I

I

:

X
X

x?

X

!

X

G. cyprica REICHEL
G. donbassica POTIEVSKAYA
G. eogranulosa REITLINGER*G. gaptankensis HARL TON

I
X

:
:

X

I
i

X

X

I

X
:

G. gracea REICHEL
G. granulosa REITLINGER
G. granulosa complicata REIT.
G. granulosa compressa REIT.

x?

X

X

X
:

X
:

X

I

X

G. granulosa multiseptata REIT.
G. kamensis REITLINGER
G. kantharensis REICHEL
G. minima REITLINGER

X
X
X
X
;

G. moderata REITLINGER
G. mosquensis REITLINGER*•G. ovaia CusHMAN & WATERS
G. parva CHERNYSHEVA
G. pulchra REITLINGER
G. rauserae REITLINGER
G. scaphoides MoRozovA+G. shikhanensis MoRozovA+G. spiralis MoROZOVA
G. syzranica REITLINGER
G. vonderschmitti REICHEL+G. vulgaris MOROZOV A

X

X
:

X
X

X

I
;

X
X
X

X

X
X
X

I
X

I
I

X

x?

* Described only by the external characters of free specimens; + described by line
drawing without microphotograph; • identified with G. biserialis by thin section
study.

interiomarginal, opens into vestibule near
middle of apertural face.
Twenty-eight species of Globivalvulina
have been previously described ; twofrom the upper Lower Carboniferous,
twenty-one from the Upper Carboniferous and five from the Permian (see Table
1). Generally the species from the Lower

604.

A

Permo-Carboniferous endothyraceans

B

c

D

417

E

Text-fig. 1. Various sections of Globivalvulina (partly figured after REICHEL, 1964).
A, sagittal section; B, nearly sagittal section; C, apertural section ; D, parallel section;
E, external view. Lines under capital letters A, B, C and D correspond sectional lines
shown in E.

Carboniferous are small in size (0.25 mm
more or less in maximum length ofsagittal section) and subspherical inshape, while the Permian species arecharacterized with larger size (more than
0.6 mm) and rapidly expanding chambers
in adult stage. The Upper Carboniferous species are commonly 0.3 mm to 0.6
mm in size and intermediate in shell
shape between the Lower Carboniferous
and Permian types.
The re-examination is required withthree species which have been only studied by the external appearance without
taking notice of the inner microstructure by thin section. St. ]EAN (1957, p.
36) regards both species of Globivalvulina biserialis and G. ovata as the sameone from the common characteristics of
the inner structure. Three species whichwere defined with the vague figures byline drawing are also insufficient in order
to compare exactly with other species.
With regard to the orientation of thinsection in this genus, the terms of transverse and longitudinal sections have
hitherto been mainly used, but there issuch disorder that REITLINGER's transverse section (1950) is the same as St.
]EAN's longitudinal one (1957). In any
case, it admits of no doubt that thesection carrying the helicoid axis ofbiseriality (in other words perpendicular
to the coiling axis) and passing throughthe proloc!J.lus best reveals internal features of the shell, as is known from themorphological study of REICHEL (1946,
text-figure 36) and PLUMMER (1948). The
present writer makes use of the termof sagittal section to this orientation.
The apertural section, which is sliced
with the face of lobata opening, is indispensable for the purpose of observing
the feature of aperture, for it can not
be seen in sagittal section. Such others
as axial, parallel and nearly saggital
sections are also necessary to investigate
in. detail the characteristics of test (Textfig. 1).
Systematic description

Family Biseriamminidae
CHERNYSHEV A, 1941
Genus Globivalvulina SCHUBERT, 1921
Type-species:- Valvulina bulloides BRADY,
1876, Palaeont. Soc., London, Monograph, vol.
30, p. 89, pl. 4, figs. 12-15.

It was reported from the upper Pennsylvanian of Iowa, U.S.A., but according418

Yuji OKIMURA

to PLUMMER (1948, p. 169), the exact geographic position of the type-locality forthe species is questionable.
Diagnosis:- Test small, sub globular tohemispherical, planispirally to slightly
trochospirally coiled, comprises a biserial
succession of chambers arranged along
an axis of biseriality that draws an open
helicoid curve. Apertural face (ventralside) more or less concave. Wall calcareous, microgranular, may have an
inner fibrous or porous layer particularly
well developed along septa. Aperture
single, lobate, and opens into near thecenter of a little flattened part of somewhat concave apertural face, with avalvular projection.
Remarks:- This genus is clearly distinguished from the others of Endothyracea by a lobate aperture and chambers
biserially arranged along the helicoid
axis of biseriality. In parallel section,
the chamber arrangement closely resembles that of palaeotextulariids seen in
0/co/co section, but the shell of Globivaluulina is not tapering, being obtusetriangular in shape. The apertural character can be defined in detail only by
the external observation of isolated specimens, though examined partly in apertural section.
Geological age:- The upper Lower Carboniferous to the upper Permian; mainly
the lower Upper Carboniferous. Occurrences of the upper Lower Carboniferous and Permian species are geographically restricted. That is to say, only
two Visean species have been recorded
from the central part of Bashkiria,
U.S.S.R., and Permian ones, except G.
donbassica from Donbass region, from
Chatzimanoli, Ile de Chio, Greece andCyprus. All the other species occur
from the Pennsylvanian of the U.S.A.
and European Russia.

Globivalvulina kamensis REITLINGER
Pl. 50, figs. 1-8
1950. Globivalvulina kamensis REITLINGER,
Akad. Nauk. USSR, Inst. Geol. Nauk,
Trudy, Moscow, fasc. 126 (Ceo!. Ser.
no. 47), p. 78, pl. 16, figs. 5-6.
1962. G. kamensis: BocusH and }uFEREV,
Akad. Nauk, USSR, Dep. Siberian Inst.
Ceo!. Geogr., p. 197, pl. 8, fig. 14.

Types :-So far as the type-specimens
photomicrographed by REITLINGER areconcerned, they are not good enough todescribe the species definitely, because
the one is a nearly apertural section(fig. 5) and the other (holotype) a nearlysagittal, slightly oblique section (fig. 6).
They were obtained from the Kashiraformation (lower Moscovian), southernpart of the region around the Timan
Upland, Komi, U.S.S.R.
Material.·-Five sections almost perpendicular to the coiling axis, threeparallel to the plane of ventral side oftest, and seven others were examined.
The majority came from the Millerella
sp. ArvPseudostaffella antiqua zones of
the Akiyoshi and Taishaku limestonegroups.
Description:- Test moderate in size,hemi-ellipsoid, slightly trochospiral witha very weakly curved helicoid axis ofbiseriality, consisting usually of one to
one and a half volutions with biserial
chambers. Chambers six to seven in
number in each row, fairly overlapped;
the last two rapidly expanding, occupying about two-thirds of the total outerwhorl, and especially the last chamberhighly inflated ; inner half of the whorl
consists. of small chambers tightly coiled. The last chamber has a valvular
projection on the floor, which takes
about a half of the chamber height andgenerally parallels the " antetheca of604.

Permo-Carboniferous endothyraceans

Fusulinacea". Wall relatively thin, calcareous and microgranular, partiallywith inner fibrous layer. Aperture lobate, opening at the central part ofsomewhat flattened apertural face; itstrue character is indistinct, though observed as dark part in Pl. 50, fig. 8(nearly a pert ural section).
Dimensions:- The longest diameter
0.34 mm in the figured sagittal section(Pl. 50, fig. 1), and the maximum width
0.25 mm in the figured parallel section
with apertural face (Pl. 50, fig. 7).
Remarks:- The last chamber of thisspecieJ is more inflated than in any
other species of Globivalvulina. It also
differs from others except for G. gracea
REICHEL in its long valvular projection.
This projection is apparently short in
the photomicrograph of the holotype,for it is a slightly oblique section. G.
liamensis closely resembles G. granulosa
REITLINGER including its three subspecies, but the former is distinguishedfrom the latter in its plane or veryslightly arcuate apertural face.
Horizon:- The present species was
obtained from the Millerella sp. A""
Pseudostatfella antiqua zones of the Akiyoshi limestone, the Millerella sp. A
zone of the Taishaku and the Koyama
limestone, and the upper part of the
Kakisako formation (Millerella zone) of
the Kuma Massif.

Globivalvulina mosquensis REITLINGER
Pl. 50, figs. 9-12
1950. Globivalvulina mosquensis REITLII\GER,
Akad. Nauk, USSR, Inst. Geol. Nauk,
Trudy, Moscow, fasc. 126 (Geol. Ser.
no. 47), p. 79, pl. 16, figs. 1-4.

Types :-This species was first foundfrom the middle Upper Carboniferous
Podolsk formation in the eastern part419

of the Moscow Basin, U.S.S.R. The
holotype (fig. 1) is described as transverse section, but it may be a slightly
oblique, nearly sagittal section, and theparatype (fig. 2) is a parallel one. Therefore, the apertural feature and the valvular projection are unable to be seen
in detail in these figures.
Material:- The writer obtained fourteen specimens in all, but there is no
precisely sagittal section. Three nearlysagittal sections slightly oblique to thecoiling axis, two sections parallel to theapertural face, and nine other were examined. The occurrence is limited to
the Profusulinella"" Fusulinella zones of
the Akiyoshi and Atetsu limestones andthe Nagaiwa formation (Profusulinellazone) of the Kitakami Massif.
Description:- Test moderate in size,
subglobular, slightly trochospiral, andslightly compressed laterally; apertural
face very weakly concave. Number ofwhorls not more than one and a half.
Chambers increasing gradually in size,
especially slowly in juvenile stage, hiseriality that describes an open helicoid
curve, but the last chamber swerves
from the axis; seven chambers in eachrow interlocked very shallowly. The
valvular projection may be present on
the floor of the last chamber, as shownin Pl. 50, fig. 10 (slightly oblique, nearlysagittal section); the identical hookshaped projection is also recognized onfloors of the last three chambers in the
figure of the holotype. Wall relatively
thin, microgranular, calcareous, with inner fibrous layer partially. Apertureprobably lobate, opening on some what
concave apertural face; but its precise
character obscure because of a lack ofapertural section.
Dimension:- The longest diameter 0.38
mm in the nearly sagittal section (Pl.
50, fig. 10), and the maximum width 0.35

Yuji OKIMURA

420

mm in the parallel section with apertural face (Pl. 50, fig. 12).
Remarks :-Such characters as low
spire and inner fibrous layer describedon the type-specimens are not always
special ones of this species. The present species resembles more closely G.
bulloides (BRADY) than any other species,· but differs in its small size andregularly expanding chambers throughthe growth stage. It is also distinguished from G. lwmensis REITLINGER
in its more deeply concave apertural
face.
Horizon:- Although this species was
originally recorded from the upper Moscovian, it may range down to the lower
Moscovian or Bashkirian by reason of
occurring from the Profusulinella beppensis zone of the Akiyoshi limestone
and its equivalents.

Globivalvulina granulosa compressa
REITLINGER
PI. 51, figs. 1-6
1950. Clobivalvulina granulosa REITLII\GER
var. compressa REITLINGER, Akad.
Nauk, USSR, Inst. Ceo!. Nauk, Trudy,
Moscow, fasc. 126 (Ceo!. Ser. no. 47),
p. 81, pl. 16, figs. 10-ll.

Types:- The holotype specimen (fig.
10) is not a transverse section but anearly sagittal one, and also the paratype specimen (fig. 11) is a nearly apertural section (not a longitudinal one).
They were described from the lowermost
Moscovian V ereia formation, southernpart of the region around the Timan
Upland, Komi, U.S.S.R.
Material.·-Nine specimens were examined. They consists of four nearlysagittal, a just apertural and four othersections from the Millerella sp. A"'
Pseudostaffella antiqua zone of the Aki-

yoshi limestone and the Millerella""Profusulinella zones of the Taishaku limestone. There is no section precisely
perpendicular to the coiling axis andpassing through the proloculus.
Description:- Test moderate in size,
hemispherical, fairly concave in apertural face, composed of one to one anda quarter whorls with six or sevenchambers biserially arranged. almost
planispiral, but its helicoid axis weakly
curved in later stage. Chambers deeply
overlapped, rapidly expanding except
those in juvenile stage which are tightly coiled ; the last chamber relatively
inflated, slightly swerving from the helicoid axis of biseriality. Valvular projection indistinct owing to a lack ofsagittal section, but a small hook-shaped
projection may be present on the floorof the last chamber. Wall thin, microgranular, calcareous, inner fibrous layer
poorly developed. Aperture lobate, fairly large, opening at the central part ofconcave apertural face; there are fivelobations, among which one is acute andthe rest are obtuse.
Dimension:- The longest diameter 0.39mm and the maximum width 0.26 mm
in the nearly sagittal section (Pl. 51, fig.
2). The length along the axis of biseriality 0.34 mm and the maximum width
0.32 mm in the apertural section (Pl. 51,
fig. 5).
Remarks:- The present species is allied
to G. mosquensis REITLINGER in respectthat the last chamber swerves from thehelicoid axis of biseriality, but the former is clearly distinguished from the latterby its strongly concave apertural face.
This species closely resembles G. bulloides (BRADY), but it differs in its apertural feature with five lobations andcurved helicoid axis of biseriality.
Horizon:-Although the type-speciesof this species were originally described604.

Permo-Carboniferous endothyraceansfrom the lowermost Moscovian, its range
should be set down to the Bashkirian
owing to the occurrence from the Millerella zone.
Globivalvulina sp. cf. G. kantharensis

REICHELPl. 50, figs. 13-14
Compare:1946. Clobivalvulina kantharensis REICHEL,
Eclogae Ceo!. Helv., Lausanne, vol. 38,
no. 2, pp. 554-555, text.figs. 40a-d.

Types :-G. kantharensis was describedfrom the lower Permian of Cyprus. The
holotype (text-fig. 40b) is a sagittal sectiion and the paratype? (text-fig. 40c) is
a section nearly parallel to the coilingaxis and apertural face. Other two specimens are oblique. Therefore, the apertural feature is unknown even throughout all figured specimens.
Material:- Two nearly sagittal sections from the lower part of the Pseudoschwagerina zone of the Taishaku limestone.
Description:- Test small, sub globular,
comprising a compact biserial successionof gradually enlarging chambers, almost
planispirally coiled with an axis of hiseriality that describes an open helicoid
curve. Apertural side strongly concaved.
Valvular projection is present on thefloor of the last chamber, fairly long,
hook-shaped; Its length attains to halfof the chamber height. In sagittal section, a single aperture is recognized asa low slit-like opening. Wall thin, microgranular, calcareous; inner fibrouslayer very poorly developed.
Dimension:- The maximum length 0.32mm and the maximum width 0.23 mm
in the nearly sagittal section figured
with Pl. 50, fig. 13.
Comparison :-In many important char-421

acters the material here dealt with iscomparable with C. kantharensis REICHEL,
though the writer avoids the exact identification owing to insufficiency of thematerial. The species is closely allied
to C. bulloides (BRADY) and G. granulosa
compressa REITLINGER, but it can be
distinguished in its strongly depressedventral side and gradually expandedchambers.
Horizon:-In Cyprus G. kantharensis
was accompanied by Pseudoschwagerinasp., and in Taishaku, too, occurred only
from the lower Pseudoschwagerina zone.
Very recently, Mr. TAKEDA, who isengaging in studying the geology of thesouthwestern Atetsu limestone plateau,found three specimens belonging to thisspecies from the Pseudoschwagerina zone.
Therefore, the species may be effective
as a horizon marker.

Globivalvulina sp. cf. G. gracea

REICHELPl. 51, figs. 7-10
Compare1946. Clobivalvulina gracea REICHEL, Eclogae
Ceo/. Helv., Lausanne, vol. 38, no. 2, p.
550, pl. 19, figs. 15-17, text-figs. 36A-F
and 38a-f.
1970. Clobivalvulina gracea: KociiANSKY-DEVIDE, Ceo!. Razpr. Por., vol. 38, p. 185,
pl. 9, fig. 6, pl. 18, figs. 1-2.

Types :-REICHEL established G. gracea
from the Permian of Chio Island, Greece.
The holotype photomicrographed withpl. 19, fig. 15 is a nearly sagittal section.
The test-figs. 36A-F given as "cotype"(paratype ?) are the most important
figures requisite for thin section studyof the genus Globivalvulina.
Material:- Three nearly sagittal, aparallel and two oblique specimens were
examined from the Fusulinella and Para-

422Yu}i OKIMURA

fusulina zones of the Taishaku limestone.
Description:-Test relatively large,
subglobular, weakly depressed on apertural side, consisting of one and a half
whorls with eight chambers biseriallyarranged through the growth stage.
Chambers gradually enlarging, but thelast and penultimate ones fairly inflated.
A valvular projection is present on thefloor of the last chamber, long, tapering,and parallels the "antetheca of Fusuli- ·nacea ". Wall relatively thick, composedof outer microgranular and inner fibrouslayers. In sagittal section the apertureis recognized as a slit-like opening.
Dimension:-The maximum length 0.59mm and the maximum width 0.39 mm
in the sagittal section (Pl. 51, fig. 9). The
length along the axis of biserity 0.52 mm
and the maximum width 0.39 mm in theparallel section (Pl. 51, fig. 10).
Comparison :-Almost all charactersstated above are comparable with thoseof G. gracea, though the apertural nature
is indistinct because of lack of apertural
section. This species and G. kantharensis
REICHEL are closely alike in their subglobular shell, but the former is distinguished from the latter in its larger
size and more depressed ventral side.
The species is also distinguished fromG. mosquensis REITLINGER by that thelast chamber of the latter swerves outof the axis of biseriality.
Horizon :-According to the originaldescription of G. gracea from Chio Island,
the species coexists with such Permian
foraminifers as Agathammina pusilla(GEINITZ), Hemigordius aff. schlunbergi(SCHUBERT) and Geinitzina postcarbonica
SPANDEL, but there is no evidence on
the precise age. The specimens dealt
with in this paper occurred from the
Moscovian and Middle Permian parts of
the Taishaku limestone.

Globivalvulina regularis sp. nov.
Pl. 50, figs. 15-19

iVIaterial :-A sagittal section (holotype,
YONG6-15), a nearly apertural section(paratype, YONG6-14), two parallel sections with apertural face, two nearlysagittal sections and others were examined. The majority came from the Nagaiwa formation of the Kitakami Massif.
Description:- Test relatively large,
subglobular, planispiral, weakly depressed on both lateral sides of the boundary
between the juvenile and the adult, consisting of one volution with seven chambers of adult stage fairly inflated ascompared with four small, gradually enlarging and tightly coiled chambers of
the juvenile. On each floor of the adultchambers there is a hook-shaped projection, while the axial part of early stage
filled with calcareous microgranular secondary deposits. Wall composed of outer
thick microgranular and inner thin defective fibrous layers. Aperture lobate,with five shallow lobations, opening on
the concave apertural side.
Dimension:-The maximum length 0.48
mm and the maximum width 0.38 mm
in the holotype (sagittal section) figured
with Pl. 50, fig. 19. The maximum length
0.42 mm and the maximum width 0.41
mm in the paratype (apertural section)
figured with Pl. 51, fig. 18.
Remarks:-This new species can be
distinguished from other species of Globivalvulina in its depression on both lateral sides of test that is caused byabrupt expanding of chambers in adultstage.
Horizon:- Almost all specimens wereobtained from the Ng-6 horizon (ONUKI,
1955) of the Nagaiwa formation (Profusulinella zone), Kitakami Massif. A few
came from the Millerella sp. A zone of604.

Permo-Carboniferous endothyraceans

the Akiyoshi limestone and from thesame zone of the Kobatake limestone,
Jinseki-gun, to the south of Taishaku
district, Hiroshima Prefecture.

423

Hor·izon :-The occurrence of the present species is limited to the Millerella
sp. A zone of the Akiyoshi limestone.
Some specimens comparable with thisspecies were found from the same zoneof the Taishaku limestone.

Globivalvulina sp. A
Pl. 50, figs. 20-22

Material :-Six specimens were examined; a nearly sagittal, a parallel, anearly apertural and other sections fromthe lower Upper Carboniferous part of
the Akiyoshi and Taishaku limestones.
Description:- Test moderate in size,
subglobular, very slightly trochospiral.
Number of whorls not over one and ahalf. Commonly seven chambers biserially arranged ; chambers of an innerhalf whorl small and tightly coiled, while
those of later stage increase in size
rapidly but not uniformly, and the lastchamber fairly swerves from the helicoid axis of biseriality. Secondary deposits remarkably developed on floorsof the chambers. Wall relatively thin,consisting of outer microgranular andinner fibrous layers. Aperture lobate,with two or more acuate lobations, opening at the central part of apertural face.
Dimensions:- The maximum length
0.27 mm and the maximum width 0.21
mm in the sagittal section (Pl. 50, fig.
22). The length along the axis of hiseriality 0.31 mm and the maximum
width 0.33 mm in the nearly apertural
section (PI. 50, fig. 21).
Remarks:- This species is remarkably
characterized with secondary deposits,
inflated chambers of the adult stage, anda considerable swerve of the last chamber. Accordingly, it may be a new species, but the writer hesitates to conclude
so, because there is no sagittal section
enough to designate as the type-specimen.

Globivalvulina sp. B
Pl. 51, figs. 11-13

Material:-Two nearly sagittal andother oblique sections were examinedfrom the Upper Permian of Taishaku.
Descriptive remarks:- Test large, hemiellipsoid, planispiral, composed of one
and a half whorls with nine or ten
chambers biserially arranged along thehelicoid axis of biseriality. The helicoid
axis becomes very loosely coiled or uncoiled in later stage, and this is themost important character of the .species.
Chambers deeply overlapped as those ofpalaeotextulariids. The characters of
valvular projection and aperture are indistinct because of an absence of availably oriented section. Owing to the insufficiency of the material, the definite
designation is postponed.
Dimension:-The maximum length 0.57
mm and the maximum width 0.33 mm
in the sagittal section figured with Pl.
51, fig. 11.
Horizon:- All the specimens referable
to this species were obtained only fromthe locality TKSH-1, Yabeina zone of
the Taishaku limestone.

Notes on the occurrenceof Globivalvulina

In this chapter, the biostratigraphicalsignificance of Globivalvulina is noted,
and the frequency of it is related withthe petrographical character of lime-424
stone. The writer (1966) has alreadydivided the Carboniferous limestones of
the Chugoku Region into the following
zones in descending order.

than fusulinaceans in frequency. Especially speaking, the occurrence of three
species of G. kamensis REITLINGER, G.
granulosa compressa REITLINGER and G.
sp. A is limited to this zone. Moreover,
the writer did not find any species ofGlobivalvulina from the underlying zones.
Such being the case, it may be concluded that Globivalvulina is an important faunal element of the Eostaffella
sp. A-Millerella sp. A zone of the Chugoku Region, and that the frequency of
it offers an available datum to the problem concerning the boundary between
the Lower and Upper Carboniferous in
Japan. RAUSER-CHERNOUSSOVA and REITLINGER (1957, p. 113) has already statedthat the age of prosperity of the genus
is in the lower Upper Carboniferous.
Table 3 shows the distribution of Globivalvulina with regard to the lithologic
types of limestone. As understood fromthis table, globivalvulinid foraminifera
occur more abundantly from micritic
limestones, especially such limestones as
foraminiferal or crinoidal biomicrite, thanfrom sparitic ones. Such occurrence may
be related to the paleoecology of theFusulinella imamurai-F. biconica zone
Profusulinella toriyamai-P. beppensis zone
Pseudostaffella antiqua zone
Eostaffella sp. A-Millerella sp. A zone
- - - Disconformity - - Mediocris sp. A-M. mediocris zone
Endostaffella delicata zone
Endothyra sp. A zone

The upper four zones are characterized with primitive fusulinaceans, while
the lower three with smaller foraminifers. The writer (1963, 1966) also emphasized that Globivalvulina is one of
the characteristic genera in the Millerellazone.
Table 2 shows the biostratigraphic distribution of Globivaluulina in the Taishaku, Atetsu and Akiyoshi limestones.
Among 239 specimens in 64 thin sections(a section 30 X 20 mm in area) examined,
151 one (about 67.3%) were obtained fromthe Eostaffella sp. A-Millerella sp. A zone,
where the genus is occassionally greater

Table 2. Frequency of Globivalvulina with relation to the divisions of the
Permo-Carboniferous limestones in Chugoku Region. Numerals fn and out of brackets
indicate the number of thin sections containing Globivalvulina and that of specimensof the genus respectively.
Taishakul.s.

Atetsul.s.

Akiyoshil.s.

~: ~~~ .1 .........................

Total

Y abe ina zone
Pseudoschwagerina zone

20
19

(2)
(3)

Fusulinella zone
Profusulinella zone
Pseudostaffella antiqua zone
Eostaffella sp. AMillerella sp. A zone

4
1

(3)
(1)
0

7
3

(2)
(1)

2
1
4

41 (18)43(9)67 (13)151 (40)Total

85 (27)80 (21)74 (16)239 (64)

not exam ...

0

(1)
(1)
(1)

1...

34
32

(9)
(5)

6
9
7

(4)
(4)
(2)

-

604.

I • ''~;·. •Permo-Carboniferous endothyraceans

425

Table 3. Frequency of Globivalvulina with relation to the petrographicaldivisions of limestones. Numerals show the number of thin sections containing
Globivalvulina. In each box the number of the Carboniferous sections is set below
and that of the Permian ones above.
Taishakul.s.

Atetsul.s.

Sparite41

53

Sparudite

0
0

0
5

Micrite117

40Micrudite

0
1

0
4

Biolithite

0
3

0
0

5
22

9
12

Total

genus. However, it is difficult to makeclear the pa:leoecological environment,
because what factors influence the frequency of Paleozoic smaller foraminifera
is not well known.
In this respect, the study of CRONEISand TOOMEY (1965) is worth appending,which reported the composition of theforaminiferal population on four thinsections (a section 30x30 mm. in area)from the Gunsight limestones (Virgilian).
According to it, 200 specimens of globivalvulinids on an average are counted
from the foraminiferal-brachiopoda! biomicrudite (coral horizon) accompaniedwith a few sessile foraminifera, while
only 3 specimens from the algal-foraminiferal biomicrudite in which the remainsof calcareous algae and sessile foraminifera are the dominant faunal elements.
It was supposed by them that the depositional environment of the former
was under normal marine, clear, shallow
water, and that of the latter under very
shallow, marine, quiet water.

I
_J

I
I

I
I

Akiyoshi
l.s.

2
1
2
10
1
16

I

Total

I
I
I
I
I
I
I

15
6
24
15
4
64

References
BocusH, O.I. and JuFEREV, O.V. (1962) : Foraminifers and stratigraphy of the Carboniferous deposits in Karatau and Talasskii Alatau. Alzad. Nauk, USSR, Rept.
Siberian Inst.G eo!. Geograph., p. 1-234,
pis. 9 (in Russian).
BRADY, H.B. (1876) : A monograph of Carboniferous and Permian Foraminifera (thegenus Fusulina excepted). Pal. Soc. London, Monograph, no. 30, p. 1-166, pis. 12.
CIIERNYSI-IEVA, N.E. (1941) : A new genus ofForaminifera from the Tournaisian deposits of the Urals. Akad. Nauk, USSR,
Doklady, val. 32, no. 1, p. 69-70.
- - (1948) : Some new species of. Foraminifera from the Visean of the Makarov district (South Urals). Akad. Nauk, USSR,!nsf. Geol. Nauk, Trudy, no. 62 (Geol. Ser.
no. 19), p. 246-250, pl. 1 (in Russian).
CRONEis, C. and TooMEY, D.F. (1965) : Gunsight (Virgilian) Wewokellid sponges andtheir depositional environment~ ]o.ur. Paleont., vol. 39, no. 1, p. 1-16, pis. 7.
CUSHMAN, J.A. and WATERS, J.A. (1928) : Additional Cisco Foraminifera from Texas.

426

Yuji OKIMURA

Contrib. Cushman Lab. Foram. Research,
vol. 4, no. 3, p. 1-16, pis. 8.
- - and - - (1930) : Foraminifera of the.
Cisco group of Texas. Univ. Texas Bull.,no. 3016, p. 22-81, pis. 11..
GALLOWAY, J.J. and RYNIKER, C. (1930): Foraminifera from the Atoka Formation of

Oklahoma. Oklahoma Geol. Survey, Circ.,
no. 21, p. 1-27, pis. 5.
HARL TON, B.H. (1928) : Pennsylvanian Foraminifera of Oklahoma and Texas. jour.
Paleont., vol. 1, p. 305-310, pis. 2.
KocHANSKY-DEVIDE, V. (1970) : Permski Mikrofosili Zahodnih Karavank. Geol. Razpr.

Explanation of Plate 50(All figures x 100)

Globivalvulina kamensis REITLINGER
Figs. 1 and 3.

Nearly sagittal section (1, YOTM40; 3, YOTM109) from the Mediocris

mediocris zone of the Taishaku limestone.
Fig. 2. Tangential section (YOAD17) from the upper part of the Millerella sp. A zone of
the Akiyoshi limestone.
Fig. 4. Nearly sagittal section (YOAD13-2) from the upper part of the Millerella sp. A
zone of the Akiyoshi limestone.
Fig. 5. Nearly sagittal section (YOA3-l) from the lower part of the Millerella sp. A zcneof the Akiyoshi limestone.
Fig. 6. Nearly sagittal section (YOAD26-2) from the Pseudostaffella antiqua zone of the
Akiyoshi limestone.
Fig. 7. Parallel section (YOAD24-1) from the upper part of the Millerella sp. A zone of
the Akiyoshi limestone.
Fig. 8. Nearly apertural section (YOTM109-2) from the Mediocris mediocris zone of the
Taishaku limestone.
Globivalvulina mosquensis REITLINGER
Figs. 9-11. Nearly sagittal sections (9, YOADll-1; 10, YOAD24-2; 11, YOAD24-3) fromthe upper part of the Millerella sp. A zone of the Akiyoshi limestone.
Fig. 12. Parallel section (YOAKJ2-1) from the lower part of the Millerella sp. A zone of
the Akiyoshi limestone.
Globivalvulina sp. cf. G. kantharensis REICHEL
Figs. 13 and 14. Nearly sagittal section (13, YOTUYM18-1; 14, YOTUYM18-2) from thePseudoschwagerina zone of the Taishaku limestone.
Globivalvulina regularis sp. nov.
All specimens from the Nagaiwa formation (Projusulinella zone) of the Kitakami Massif.
Figs. 15 and 16. Nearly sagittal sections (15, YONG6-ll; 16, YONG6-12).
Fig. 17. Parallel section (YONG6-13).
Fig. 18. Neaaly apertural section (YONG6-14), Para type.
Fig. 19. Sagittal section (YONG6-15), Holotype.
Globivalvulina sp. A
Fig. 20. Parallel section (YOAD28-2) from the Profusulinella beppensis zone of the Akiyoshi limestone.
Fig. 21. Nearly apertural section (YOAD3) from the lower part of the Millerella sp. A
zone of the Akiyoshi limestone.
Fig. 22. Nearly sagittal section (YOAD14) from the upper part of the Millerella sp. A
zone of the Akiyoshi limestone.

GKIMURA:

Permo-Carboniferous endothyraceans

Plate 50

4

11

604.

Permo-Carboniferous endothyraceans

Por., vol. 13, p. 175-250, pis. 26 (in Jugoslavian).
LIE Bus, A. (1932) : Die Foraminiferen In:
Die Fauna des Deutschen Unterkarbons.
Pt. 3. Preuss. Geol. Landesanst., Bah., n.s.,
no. 141, p. 133-175, pis. 2 (in German).
MooRE, R.C., edit. (1964) : Treatise on Invertebrate Paleontology. Geol. Soc. Amer.
and Univ. Kansas Press.
MOROZOVA, V.G. (1949) : Representatives of
the Families Lituolidae and Textulariidae
from the Upper Carboniferous and Artinskian Deposits of the Bashkiria; Pre-Ural.
Akad. Nauk, USSR, Inst. Geol. Nauk,
Trudy, no. 105 (Geol. Ser. no. 35), p. 244275, pis. 5 (in Russian).
0KIMURA, Y. (1963) : Characteristics of the
Smaller Foraminiferal Assemblage fromthe Carboniferous limestone of the Chugoku Province. Kaseki (Fossils), no. 6,
p. 1-6 (in ] apanese).
- - (1966) : Microbiostratigraphical Studies
on the Foraminiferal Faunas of the Lower
Carboniferous Formations of the Chugoku
Region, Southwest Japan. Geol. Rep. Hiroshima Univ., no. 15, p. 1-46, pl. 1 (inJapanese).
PLUMMER, H.]. (1948) : Morphology of Globivalvulina. Amer. Mid. Naturalist, vol.
39, p. 166-173.
POTIEVSKAYA, P.D. (1962): Representativesof certain Families of small Foraminifera.
Akad. USSR, Kiev, Inst. Geol. Sci., Trudy,

AkiyoshiAtetsuJinseki-gun
Kakisako
Kitakami

f:k

s

'ill
f411:ilNI:till i.E!
[\iif

~1:;

J:

427

Ser. Strati, and Paleont., no. 44, p. 4994, pis. 8 (in Russian).
RAUSER-CHERNOUSSOVA, D.M. and REITLIN·
GER, E.A. (1957) : Phylogeny of Paleozoic
Foraminifera and its stratigraphical significance. Izvest. Akad. Nauk, USSR, Ser.
Geol., vol. 11, p. 103-124 (in Russian).
--and FuLSENKO, A.B., edit. (1959) : Osnovy
Paleontologii. Izdat. Akad. Nauk, USSR,
Moskva (in Russian).
REICHEL, M. (1946) : Sur Queleques Foraminiferes nouveaux du Permien Mediterranean. Eclog. Geol. Helvetiae, vol. 38, p.
524-560, pis. 19.
REITLINGER, E.A. (1950) : Foraminifera of
the Middle Carboniferous Formations of
the Central part of the Russian Platform(Exclusive of the family Fusulinidae).
Akad. Nauk, USSR, Inst. Geol. Nauk,
Trudy, no. 126 (Geol. Ser. no. 47), p. 1127, pis. 22 (in Russian).
ScHUBERT, R. (1921) : Paleontologische Daten
zur Stammesgeschichte der Protozoen.
Pal. Zeitschr., Berlin, vol. 3, no. 2, 1-153.
St. ]EAN, ]. (1957) : A Middle PennsylvanianFauna from Dubois County, Indiana. Indiana Geol. Survey, Bull., no. 10, p. 166, pis. 5.
WARTHIN, A.S. (1930) : Micropaleontology of
the Wetumka, Wewoka, and Holdenville
Formations. Oklahoma Geol. Survey, Bull.,no. 53, p. 1-95, pis. 7.

Kobatake
KoyamaKuma
Nagaiwa
Taishaku

1]'

il1li

...
13

w

l'Jt Ill.ffi: !6
'iff fR428

Yuji OKIMURA

Explanation of Plate 51(All figures x 100)

Globivalvulina granulosa compressa REITLINGER
Fig. 1. Nearly apertural section (YOAD22-1) from the upper part of the Millerella sp. A. zone of the Akiyoshi limestone.
Figs. 2 and 3. Nearly sagittal sections (2, YOAKJ4; 3, YOAKJ2-2) from the lower partof the Millerella sp. A zone of the Akiyoshi limestone.
Fig. 4. Sagittal section (YOADll-2) from the upper part of the Millerella sp. A zone of
the Akiyoshi limestone.
Fig. 5. Apertural section (YOAD22-2) from the same horizon as the above.
Fig. 6. Parallel section (YOA3-2) from the lower part of the Millerella sp. A zone of the
Akiyoshi limestone.
Globivalvulina sp. cf. G. gracea REICHEL
Fig. 7. Nearly sagittal section (YOTUYM51) from the Parafusulina zone of the Taishaku
limestone.
Fig. 8. Nearly sagittal section (YOTNDA4) from the Pseudoschwagerina zone of the Taishaku limestone.
Fig. 9. Sagittal section (YOTUYM18-3) from the Pseudoschwagerina zone of the Taishaku
limestone.
Fig. 10. Parallel section (YOTG27) from the Fusulinella zone of the Taishaku limestone_
Globivalvulina sp. B
All specimens from the Yabeina zone of the Taishaku limestone.
Fig. 11. Sagittal section (YOTKSH1).
Fig. 12. Nearly sagittal section (YOTKSH2).
Fig. 13. Tangentially oblique section (YOTKSH3).

OKIMURA:

Permo-Carboniferous endothymceans

Plate 51

Trans. Proc. Palaeont. Soc. Japan, N.S., No. 87, pp. 429-435, September 30, 1972

605. A NOTE ON THE DISTRIBUTION OF BRAARUDOSPHAERABIGELOW! (GRAN AND BRAARUD) DEFLANDRE IN THE
BOTTOM SEDIMENTS OF SENDAI BAY, JAPAN*
TOSHIAKI TAKAYAMA
Institute of Geology and Paleontology, Faculty of Science,
Tohoku University, Sendai, Japan

fiJIT:fi;~Jm.l]'ifr:pO)

Braarudosphaera bige/owi (GRAN and BRAARUD) DEFLANDRE [C.

"?v'"C : flili:i'i~ J:: fJ };;(~ LJ-:: 18 jlli]O)!ii'&1i\Jtrfr:J:1 O)::p'g(f~-;1- Y I 7" 7 Y ~ r Y]\t~fC "?v' "C t~
ilt L-, )XO)*t;* ::!::j~t:o Braarudosphaera bigelowi fi7Ki~ 24m .L:.l,i~O)±!Etfl!fi;J"i" fC:~rli\r:::.~
IL', ~ h 0 0) feli L-, Cyclococcolithus leptoporus fi.:C O)!>'Hl!IJO) J:: fJ iA~v '±iEh't!f!JJ rj" rc ~ iflii' 0,jilijf.Ti0)5~;{fiO)rx:Jl:*ri,

MARTINI (1967) ;?;----:,~.- Y'7iPJr:::..t>v'-c :r;-~~ L t.:f:;'i* c -rxi' 0!l'li iJJ {~ A[l0mation in California (BRAMLETTE andSULLIVAN, 1961), the Middle Oligocene"Rupelton" of the Mainz Basin (MARTINI, 1960) and the Sarmatian of theVienna Basin (STRADNER, 1960). MAXWELL et al. (1970) studied the deep sea
cores taken from the South Atlantic
Ocean and found several layers of Braarudosphaera chalk of the kind that
occur most frequently in the Oligocene.
According to them these layers of chalkconsist almost exclusively of Braarudosphaera rosa and are distributed widelyin the South Atlantic. They consideredthat these chalk layers originated atbathyal depths on the basis of the floral
and faunal evidences associated with
Braarudosphaera rosa and they proposed
two hypotheses to explain the origin,
i.e. either unusual oceanographic conditions such as the so-called •· red-tide "bloom must have prevailed in this region
for a short interval of geologic time orcurrents carried these shallow water
deposits into deep water.

Introduction:- The living calcareous
nannoplankton species Braarudosphaera
bigelowi (GRAN and BRAARUD) DEFLANDRE has twelve regular pentagonal calcareous skeletal elements around the cellwhich make a dodecahedral form (Textfig. 1-a). Each pentagonal skeletal element consists of five segments of crystallographic units which are joined along
straight sutures that radiate from thecenter of the plate (Text-fig. 1-b). This
species was first described by GRAN and
BRAARUD in 1935 as Pontosphaera bigelowi
and since then it has been reported fromthe sediments of the Jurassic to the Recent by many investigators from many
parts of the world.
Abundant occurrences of fossil Braarudosphaera bigelowi have been reported from various stratigraphic horizons:the Danian of south-west France (MARTINI, 1961), the Lower Eocene Lodo For-* Received Feb. 25, 1972; read Jan. 25, 1969
at Tokyo.
429

Toshiaki TAKAYAMA

430

Text-fig. l.

Braarudosphaera bigelowi (GRAN and BRAARUD)
coccosphere (a) and its single plate (b).

It is generally accepted that modern
Braarudosphaera bigelowi occurs in abundance only from the near shore waterand that it is very rare or absent in the
typical pelagic sediments despite a few
exceptions (GRAN and BRAARUD, 1935;
GAARDER, 1954). MARTINI (1967) investigated the distribution pattern of Braarudosphaera bigelowi and Cyclococcolithus
leptoporus in the recent sediments of the
Persian Gulf, the Gulf of Oman and thenorthern part of the Arabian Sea andreported as follows ; Braarudosphaera
bigelowi which is fairly abundant in the
Persian Gulf drastically reduces its number at the Strait of Hormz, becomes few
in the northwestern part of the Gulf ofOman and almost absent in the greaterpart of the Gulf of Oman and northern
Arabian Sea; on the other hand thenumber of specimens of Cyclococcolithus
leptoporus which is abundant in all samples from the Gulf of Oman, decreases
abruptly at the Strait of Hormz, becomesrare in the eastern part of the Persian
Gulf and almost absent in the central
part of the same Gulf.
As the calcareous nannoplankton uses
the energy of sunlight for photosynthe-

DEFLANDRE;

sis like other plants, they are mainly
concentrated in the upper layers of theocean within the reach of sunlight.
Therefore it seems probable that suchfactors as salinity and the temperatureof the surface water are more significant in the control of their distribution,
than the depth of water. Their distribution patterns are considered to beclosely related to the present current
systems. Nevertheless, Braarudosphaera
bigelowi is assumed as a species that
inhabits coastal waters and through its
life-history the free-swimming generation appears to alternate with filamentous or other sessile forms that colonize
on rocks or other solid foundations.
It is considered that the detailed studies of the modern Braarudosphaera bigelowi may afford some solution to theorigin of the spectacular burst of fossil
Braarudosphaera at these stratigraphicalhorizons. However, these data are still
incomplete and fragmentary, and theorigin is still a mystery. With this viewin mind the present writer contributes·some data on the distribution pattern ofBraarudosp!wera bigelowi in the bottom
sediments of Sendai Bay.

605.

Distribution of Braarudosphaera bigelowt

Materials :-Sendai Bay is located on
the eastern side of Miyagi Prefecture;
approximately at 38.30' to 37.50'N. Lat.
and 141.00' to 142.20'E. Long. and issurrounded by the Ojika Peninsula at
the north and by a gentle concave coastline at the west (Text-fig. 2). The coastline between Ishinomaki and Soma Cities
is interrupted by the recently submerged
Matsushima Bay. On the land area surrounding Sendai Bay, the Miyagino
coastal plain is headed at the north by
the southern part of the Paleozoic andMesozoic systems of the Kitakami Massif.
The main drainages into Sendai Bay are
the Kitakami, Naruse, Nanakita, Natoriand the Abukuma rivers. A total of 18

Text-fig. 2.

431

samples were taken from the bottom of
Sendai Bay in November, 1966, extending from shallow water (19m) to theupper part of the continental slope (203m). The sampling localities are shownin Text-fig. 2. The samples were takenby the Phleger sampler (PHLEGER, 1951,1960) and the uppermost one centimeterin thickness, comprising approximately
10 cc of wet sediment, was cut off fromeach core and examined for the present
study. At the time of sampling, measurements were made of the depth ofwater and the surface and bottom watertemperatures. The bottom water temperature was measured on board theship from the water obtained by theChart of Sendai Bay, showing locations of the samples.

Toshiaki TAKAYAMA

432

Phleger sampler before removing thesediment. These data are as follows:
Site No.

Water depth
(m)

127
128
130
137
138
139
140
141
142
143
144
145
146
147
148
153
154
174

19
22
24
87
109
130
143
142
203
144
147
126
103
76
55
34
28
130

Temperature oc
Surface Bottom
15.8
16. 1
16.4
17.9
17.8
17.8
17.6
17.7
17.9
17.9
18.7
19.3
19.5
19. 7
19. 7
18.9
18.9
18.5

12.5
14.0
14.5
15.5
15.5
14.0
14.0
12.5
12.4
13.5
13.5
14.8
15. 1
16.0
16.0
15.5
15.5
14.5

The present materials were processedand examined according to the following
methods outlined by STRADNER and P APP(1961). Disintegration of a very small
quantity of the samples was placed in asmall glass. Water was added until adepth of 3-4 em was obtained. The glass
was placed in a ultrasonic equipment at
moderate vibration level. After settlingof the heavier particles, a few drops
were sucked from the upper layer ofthe suspension with a drinking straw
and settled out on a microscopic coverglass and dried on an electric hot-plate
carefully. Caedax (n=l.55) was thenspread over it,· dried and a large deck
glass was pressed on it. This was examined under a Nikon binocular polarizing microscope with phase contrast
equipment. A magnification of 1,500X
with oil-immersion objective lens wasnecessary.
Distribution pattern:- In each sample
two hundred specimens of coccoliths
were counted. The relative frequenciesof the species obtained are listed inTable 1. Under the light microscopenearly half of the total specimens were
too small (less than 3p) for precise iden~_tification, though they _were considered
to belong to Emiliania huxleyi, "Coccolithus doronicoides" and broken specimens of Gephyrocapsa oceanica. Therefore they are lumped together under
miscellaneous in Table 1. Among theremaining ones the fairly dominant species is Gephyrocapsa oceanica. In addition, Coccolithus pelagicus, Braarudosphaera bigelowi,
Helicopontosphaera
kamptneri, Cyclococcolithus leptoporus,
Rhabdosphaera clavigera and Syracosphaera pulchra were found, though rare
and sporadic in occurrence. Of the distribution patterns the following are recognized : 1) Braarudosphaera bigelowi

Table 1. Abundance in counted specimen; 200 in each sample.
1~1~1~1~1~1~1~1~1~1~1~1~1~1~1~1~1~1~
Species ----------- Sample--------------Braarudosphaera bigelowi
4 8 2 0 2 1 0 1 0 0 0 0 0 0 0 0 0 0
Coccolithus pelagicus
8 3 3 2 2 2 3 2 7 2 3 2 9 1 3 9 7 6
f!eclococcolithus leptoporus
0 0 0 2 0 0 2 0 3 2 6 3 5 1 7 8 5 3
eP.hyrocatsa oceanica, 85 42 62 100109 ~ 50 90 47 28 30 25 88 33 58 ~ 31 57
Helicopon osphaera kamptneri
1 1 3 0 0 0 0 1 1 0 0 0 3 0 0 1 0 1
Rhabdosphaera clavigera. 1 1 1 1 0 1 1 0 0 0 0 3 0 0 0 0 2 0
3
2 0 0 1 3 2 3 0 1 0 4 0 0 0 0 0 0~racosphaera pulchra
iscellaneous
I 98 1~ 129 95 86 165 142 103 142 167 161 163 95 165 132 139 155 133
- -

1

M~

I
I

-

De_Pth (_lllL___

IDDDDD~D~DDDDDDDD~~_ , 19_E___3_4_ 28 34 55- 76 87 103 109 126 130_E_O 142 ~1,;3__1_44 ~605.

Distribution of Braarudosphaera bigelowi

433

Table 2. Abundance in counted specimen ; 200 in each sample(Gephyrocapsa oceanica and miscellaneous excluded).

~=;=~<~, s~~~~ T127128130 15415314a1471371-4G138145139 174141l~o 1~3_144142_
1

BraarUf}osphaera ~tgelowt

I

90 99 82-

54 28 45 Cyc(ococcoltfhus leptoporus . . 4 5 10 ICoccoltthus.pelagtcus
Reltcopontosphgera kamptnert
7 2 7 1i Ooltthotus anttllarum.

Rhabdosphaera clavtgera
Syracosphaera pulchra
Total
Depth(m)'0 0 0 4 8 8 41 58 48 200 200 200 19 22 24 28- 17 - 8 15 7 3 3 4 1 2 5 6 6- 48 - 53 76 66 63 52 64 75 86 59 61 93- 52 - 41 90 77 118 86 64 89 101 107 100 95- 21 - 10 8 8 3 15 6 15 2 24 9 7 !
- 0 - 0 1 0 1 3 1 4 0 2 2 1'
- 17 - 14 2 8 3 10 20 3 0 2 15 o
- 45 - 74 8 34 9 31 41 13 9 1 7 4- 200 - 200 200 200 200 200 200 200 200 200 200 200
34 55 76 S7103 109126 130130 142 143144147 203

is found only from the sediments lessthan 87 m in water depth and it is thecharacteristic species of the inner partof the bay; 2) Cyclococcolithus leptoporus
is rare or almost absent in the nearshore sediments; 3) Syracosphaera pulchra occurs from the sediments lessthan 130 m in water depth.
To reveal the distribution patterns ofthese species more clearly, in each sample 200 coccoliths specimens except Gephyrocapsa oceanica and miscellaneous
specimens were counted at random again
and identified. The relative frequenciesof the species obtained are listed in Table
2. On this occasion station nos. 147, 153
and 154 were excluded because only asmall number of minute specimens ofcoccoliths were found from these samples. During the cruise several boring
were made in the area between station
nos. 130 and 137 and between 148 and
152, but no cores could be taken becauseof the distribution of bedrocks. HATTORI(1967) studied the bottom sediments of
Sendai Bay and divided them into thre~units on the basis of texture, composition, minor structures of the sediments
and their presumed historical ages, i.e.
Younger Suites, Older Sands A and Older
Sands B. Sample nos. 147, 153 and 154
were obtained from the area of his Older
Sands B, which were considered by him
to be in the non-depositional area. Thismay be the reason why only a small

number of specimens were found fromthese cores and also in some part of thesea floor of this area bed-rocks are exposed. Table 2 shows that the near shore
sediments shallower than 24 m are characterized by the abundant occurrence ofBraarudosphaera bigelowi compnsmg
nearly 50 percent of the assemblage. On
the contrary Cyclococcolithus leptoporus
is almost absent in this area. The distribution patterns of these two species,
which are substantially the same as
MARTINI's (1967), are shown in Text-fig.
3 and Text-fig. 4. Judging from thepresent data, the distribution of Braarudosphaera bigelowi is apparently controlled only by the depth of water. To
obtain a clear understanding of the realfactors involved, it is also necessary toassume other factors such as fresh waterand nutrients provided by the drainages
like the Kitakami River. At present nodata concerning these factors are available, and there is room for further investigation.
Acknowledgements:-The author wishes
to acknowledge his grateful thanks toProfessor Kiyoshi ASANO of the Instituteof Geology and Paleontology, Tohoku
University and Dr. Herbert STRADNER
of the Geological Survey of Austria for
their interest and encouragement. Deep
appreciation is due to Professor Kotara
HATAI and Dr. Yokichi TAKAYANAGI of
the Institute of Geology and Paleontolo-

Toshiaki T AKAY AMA

434

.0
'

~ •t. of B~aarudosphaera bigelowi
in total assemblage

Te xt -fig. 3.

Percentage distr ibut ion map of Braarudospha era bigelowi.

~ "!. of Cyc/ococco/ithus /eptoporus
in total assemblage

Text-fig. 4.

Percentage distribution map of Cyclococcolithus leptopo rus.

605.

Distribution of Braarudosphaera bigelowi

gy, Tohoku University for their criticalreading of the manuscript. The bottom
sediments were obtained by the research
vessel Tansei-maru of the Oceanographic
Institute, University of Tokyo; acknowledgements ar'e expressed to the crewof this ship for their kind assistance incollecting the samples.

References
BRAMLETTE, M.N. & SULLIVAN, F.R. (1961):
Coccolithophorids and related nannoplankton of the early Tertiary in California.
Micropaleontology, vol. 7, no. 2, pp. 129188, 14 pls.
GAARDER, K.R. (1954) : Coccolithineae, Silicoflagellatae, Pterospermataceae and otherforms from the "Michael Sars" North
Atlantic Deep Sea Expedition 1910. Rep.
Sars N. All. Deep Sea Exped. 1910, vol.
2, no. 4, pp. 1-20.
GRAN, H.H. & BRAARUD, T. (1935) : A quantitative study of the phytoplankton in the
Bay of Fundy and the Gulf of Maine.
jour. Bioi. Board Canada, vol. 1, pp. 279467.
HATTORI, M. (1967) : Recent sediments of
Sendai Bay, Miyagi Prefecture, Japan. Sci.
Rept. Tohoku Unip., 2nd Ser. (Ceo!.), vol.
39, no. 1, pp. 1-61.
MARTINI, E. (1960) : Braarudosphaeriden, Dis-

435

coasteriden und verwandte Formen aus
dem Rupelton des Mainzer Beckens. Notizbl. hess. L..-Amt Bodenforsch., vol. 88,
pp. 65-87, pls. 8-11.
- - (1961) : Ein Kalkflagellat in den Meerender Gegenwart und Vorzeit. Natur u.
Volk, vol. 91, no. 9, pp. 335-339.
- - (1967) : Nannoplankton und Umlagerungserscheinungen im Persischen Golf
und im nordlichen ArabischenM eer. Neus
jahrb. Ceo!. Paliiont. Monatsh., vol. 10, pp.
597-607.
MAXWELL, A.E., HERZEN, R.P. von, HsU,
K.]., Al'DREWS, ].E., SAITO, T., PERCIVAL, S.F., MrLow, E.D., Jr. & BoYCE,
R.E. (1970) : Deep sea drilling in theSouth Atlantic. Science, vol. 168, no. 3:?35,
pp. 1047-1059.
PHLEGER, F.B. (1951) : Ecology of Foraminifera, northwest Gulf of Mexico, Pt. I., Foraminifera distribution. Ceo!. Soc. Amer.,
Mem., 46, pp. 1-88, pls. 1, 2.
--· (1960) ·: Ecology and distribution of
Recent Foraminifera. The john Hopkins
Press, Baltimore, viii+297p, pls. 1-ll.
STRADNER, H. (1960) : Dber NannoplanktonInvasionen im Sarmat des Wiener Beckens.
Erdoe!zeitschr. vol. 76, no. 12, pp. 430-432.
- - & PAPP, A. (1961): Tertiare Discoasteriden aus Osterreich und deren stratigraphische Bedeutung mit Hinweisen auf
Mexico, Rumanien und Italien. jahrb.
Ceo!. Bundesanst. [Wien], Sonderband,
vol. 7, pp. 1-159, pls. 1-42.

- - - - - - - - - . - - ---·-----·----

AbukumaIshinomaki
Kitakami
Matsushima
Miyagi
Miyagino[liiffi\:flN
T=i ~
;It;

_L:

t~

llh

fr

tl!\

7;•;JJN.'J!fNanakita
NaruseNatoriOjika
SendaiSoma-t::ltl!l... i~hi:f=, lf:'ilkIII'!.']

u
frlJ
1'11

,L,

r::t

...If'..;

Trans. Proc. "Palaeont. Soc. Japan, N.S., No. 87, pp. 436-445, pis. 52, 53, September 30, 1972

606. FUSULINIDS OF THE PROFUSULINELLA ZONE OF THE
TAISHAKU LIMESTONE (STUDIES OF THE STRATIGRAPHY
AND THE MICROFOSSIL FAUNAS OF THE
CARBONIFEROUS AND PERMIAN TAISHAKULIMESTONE IN WEST JAPAN, NO.2)"'
KIMIYOSHI SADA
Department of Geology, Faculty of General Education,
Hiroshima University~iHREEk~~O) Profusulinella 11\'0)f;/jiil!!i\ C:fim • =:lll:~7iHR::fifk;{'50)/\"i/J; c IJ~it:.:fillilr.Jf1
f.FIC"?It''LO)lijfy"E, No. 2): ~~viiff,'~R:Pfk~O) Profusulinella ;fW (1'!.:133, 1967) IC:."?It''LO)/i}f~il'~ 2 fi]O) Profusulinella c 4 fi.J!O)~tHm~~}]lj L.. ;I::O)"""C", ;: ;: !;:~~!Ill( • i!H5·T.Q. il~lllX~nt.:f'!IHi Projusulinella fusijormis SADA, sp. nov., P. toriyamai SADA,
Millerella sp. B, Pseudostaffella taishakuensis SADA, sp. nov., Nankinella yokoyamai
SADA, sp. nov., Staffella akagoensis ToRIYAMA """C"~.Q, ;:tt,~O)f)j~!i\f<::.J:: -:>'L!f.\'~-::3ft ~tt,.Q'ffr~R:r-i/.1(~0) Profusulinella 11Hi, F>iiftFG/.1(~0) Profusulinella toriyamai Tif(f!i:III, 1961, 1964, 1965), f:XE.f:fi/.1(~0) Profusulinella beppensis ;lW (.~LIJ. 1954, 1958),
rliitl!!O) Profusulinella /ukujiensis(~~J!II. 1957) f<::.M!t~n. ~ ~~;:::, ~1::.*0) Early
Atokan 0) Profusulinella it:.=F-illi!J~ll'ff::.IH£~i'L.Q.
ft.: Ill /];; ~i-*to say, the Profusulinella beppensis zone
(TORIY AMA, 1958) of the Akiyoshi Limestone, the Profusulinella fukujiensis zone
(IGo, 1957) of the Ichinotani formation in
Gifu Prefecture and Profusulinella toriyamai zone (SADA, 1961) of the Atetsu
Limestone in Okayama Prefecture. And
these zones are mostly characterized bysuch genera as Profusulinella, Pseudostaffella, Millerella, Nankinella, Staffella,
Eoschubertella and Akiyoshiella, all rather
primitive genera except for the last one.
Recently, the Atetsuan was proposed by
TORIYAMA (1967) for the time stratigraphic unit equivalent to the zone ofProfusulinella in Japan based on theProfusulinella toriyamai zone in the
middle part of the Kodani formation of
the Atetsu Limestone (SADA, 1961).

Introduction
Having a very short stratigraphic
range, the genus Profusulinella RAUSERCHERNOUSSOVA and BELJ AEV is regarded
as being one of the best index fossils in
the lower part of the Middle Pennsylvanian. The Profusulinella zones in Japan have been reported from several
areas since the first discovery of thiszone (TORIY AMA, 1954) in the Akiyoshi
Limestone in Yamaguchi Prefecture but
the Profusulinella zones whose zone fossils had been described and illustrated
are very few. As far as our knowledge
goes, they are only three zones, that is* Received May 17, 1972; read Jan. 21, 1967
at Tokyo.

436

606.

Fusulinids of Taishaku Limestone

The Carboniferous and Permian Taishaku Limestone about 30 km to thewest of the Atetsu Limestone, having
been studied by me since 1965, comprizes
in its lower part the Profusulinella zone
designated in my preceding paper (1967).
The Profusulinella zone in this area, as
I described before, conformably overlies
the Lower Pennsylvanian Millerella zone
and also is covered by the Fusulinellazone, while the species identified fromthe zone are Profusulinella toriyamai
SADA, P. fusiformis SADA, sp. nov., Millerella sp. B, Pseudostaffella taishakuensis
SADA, sp. nov., Nankinella yokoyamai
SADA, sp. nov. and Staffella akagoensis
TORIY AMA. The present fauna consisting of them closely resembles in specificor generic composition the Profusulinella
toriyamai fauna of the Atetsu Limestone.
For example, Profusulinella toriyamai
SADA is a representative species in both
Profusulinella faunas of the Taishaku
and the Atetsu Limestone. Pseudostaffella taishakuensis SADA, sp. nov. is similar to P. kanumai IGO from the Ichinotani formation and the Atetsu Limestone
in some respects and they are almost of
the same stage in the evolutional development of the shell. Accordingly, thepaleontological similarities between these
two faunas indicate that the Profusulinella fauna of the Taishaku Limestoneis, to be sure, of the Atetsuan age. And
also the present fauna may be considered to be of the equivalent age to theProfusulinella faunas in the lower partof the Middle Pennsylvanian in North
America. In this paper are given six
species of fusulinids cited above fromthe Profusulinella zone of the Taishaku
Limestone.
Financial aid for this work was givenby the Ministry of Education and Matsunaga Science Foundation.

437

Systematic Paleontology
Family Ozawainellidae THOMPSON& FOSTER, 1937
Genus Millerella THOMPSON, 1942
Type species.-Millerella
THOMPSON, 1942.

marblensis

Millerella sp. B
Pl. 53, figs. 13-14

Descriptive remarks.- The present specimens are poorly preserved but the shell
shape and some internai characters suggest that the present forms are ascribable to genus Millerella. The shell of
the present species is small and discoidal
in shape. The periphery of the outer
volution is broadly rounded to subangular and the shell has a short axis ofcoiling, possessing the umbilicate poles.
The specimen illustrated as fig. 14 on
Pl. 53 is 188,u long and 566,u wide. Itsform ratio is 0.3.
The present species resembles somewhat Millerella ? sp. A (SADA, 1969, p.
120, pl. 12, figs. 20-21) from the Chesterian Eostaffella zone of the lower partof the Taishaku Limestone. The former
species, however, can be distinguishedfrom the latter one in having a longer
axis of coiling, a larger form ratio andan incomplete evolute form in the outer
volutions.
Table 1. Measurements ofMillerella sp. B.
SpecimenPl. fig.
LengthWidthForm ratio

A12801D2e
53-13
0.226
0. 6600.3

A12801D10g
53-14
0.188
0.566
0.3

(Measurements in mm)

Kimiyoshi SADA

438

Occurrence.-Rare in the Profusulinellazone of the Taishaku Limestone. Associated fusulinids are Profusulinella toriyamai SADA, P. fusiformis SADA, sp. nov.,
Pseudostaffella taishakuensis SADA, sp.
nov., Nankinella yokoyamai SADA, sp.
nov. and Staffella akagoensis TORIY AMA.
Type locality is Loc. No. A12801D.

Family Fusulinidae VON MOLLER, 1878
Subfamily Fusulininae VON MOLLER, 1878
Genus Profusulinella RAUSERCHERNOUSSOV A and
BELJAEV, 1936
Type species.-Profusulinella aljutovica
RAUSER-CHERNOUSSOVA, 1938.
Profusulinella toriyamai SADA
Pl. 52, figs. 1-4
1958. Profusulinella sp. A, ToRIYAMA. Mem.
Fac. Sci. Kyushu Univ., Ser. D, Geol.,
vol. 7, pp. 35-36, pl. 1, figs. 20-21.
1961. Profusulinella toriyamai SADA. jour.
Sci. Hiroshima Univ., Ser. C, vol. 4, no.
1, pp. 97-99, pl. 9, figs. 1-13.

Table 2.
Length
1. 151

Measurements of Profusulinella toriyamai SADA
Specimen A12801D2a: Pl. 52, fig. 1.
Width
0. 944

Radius vector
Vol.
1
2
3
4
5

Description.- The shell is small andellipsoidal in shape. The mature specimen of five volutions illustrated as fig.
1 on Pl. 52 is 1151,u long and 944,u wide,
having a form ratio of 1.2. The lateralslopes are straight to convex. The ratiosof the half length to the radius vectorof the 1st to the 5th volution are 1.0,
0.8, 1.5, 1.4 and 1.2, respectively.
The proloculus is minute and its outside diameter is 37,u. The expansion of
the shell is slow. The radius vectors of
the 1st to the 5th volution in a specimen
are 56, 113, 188, 302 and 510,u, respectively. The spirotheca is thin and consists of a tectum and inner and outer
tectoria in all volutions. The thicknessof the spirotheca of the 1st to the 5th
volution at the central part of the shellis 23, 23, 23, 39 and 50 ,u. respectively.
The septa are unfiuted throughout thelength of the shell. The tunnel is low
and broad. The chomata are massivein the outer volutions.
Remarks.-In the shell shape, the internal character and the measured values,
the present species agrees closely with
Profusulinella toriyamai SADA (1961, pp.
97-99, pl. 9, figs. 1-13) from the Atetsu
Limestone in Okayama Prefecture, West

0.056
0.113
0.188
0.302
0.510

Form ratio
1.2

Ratio of HI. to Rv.
Vol.
1
2
3
4
5

1.0
0.8
1.5
1.4
1.2

Pro!.
0.037

Thickness of spirothecaVol.
00. 009
1
0.023
2
0.023
3
0.023
4
0.039
5
0.050
(Measurements in mm)

606.

Fusulinids of Taishaku Limestone

Japan.
Occurrence.-Abundant in the Profusulinella zone of the Taishaku Limestone.
Associated fusulinids are Millerella sp.
B, Profusulinella fusiformis SADA, sp.
nov., Pseudostaffella taishakuensis SADA,
sp. nov., Nankinella yokoyamai SADA, sp.
nov. and Staffella akagoensis TORIY AMA.
Type locality is Loc. No. A12801D.
Profusulinella fusiformis SADA, sp. nov.
Pl. 52, figs. 5-12

Description.- The shell is small andfusiform in shape, having a straightaxis of coiling and bluntly pointed poles.
The lateral slopes are slightly concave.

439

The holotype of four volutions (Rg. No.
A12801D13b) illustrated as fig. 8 on Pl.
52 is 1227 p long and 528p wide, giving
a form ratio of 2.3. The fully grownspecimen of five volutions (Rg. No.
A12801D13a) (Pl. 52, fig. 5) is 1567 p longand 755p wide and its form ratio is 2.1.
The inner two volutions are tightly coiled and spherical to ellipsoidal, and beyond the 3rd volution the shell attains
its mature shape. The ratios of the half
length to the radius vector in the 1st to
the 5th volution of four specimens are
1.0-1.7, 1.0-3.0, 1.6-2.9, 1.9-2.2 and 2.3,
respectively.
The proloculus is small. The outside
diameter of the holotype is 75p. The
radius vectors of the 1st to the 5th

Table 3. Measurements of Profusulinella jusijormis SADA, sp. nov.
A12801D13a
52-5
1. 5670. 7552.1
0.037

A12801D14b
52-6
1. 511
0. 736
2.0
0.056

A12801D13b
52-8
1. 227
0.528
2·3
0.075

A12801D8d
52-10
1.038
0.547
1.9
0.056

Vol.
1
2
3
4
5

0.056
0.094
0.151
0.264
0.377

0.056
0.094
0.188
0.321

0.056
0.094
0.151
0.283

0.075
0.113
0.188
0. 302

Ratio of HI. to Rv.

1
2
3
4
5

1.7
2.0
2.4
2.2
2.3

1.7
2.4
2.6
2.2

1. 7
3.0
2.9
2.1

1.0
1.0
1.6
1.9

Thickness of
spirotheca

0
1
2
3
4
5

0.013
0.016
0.016
0.023
0.025
0.039

0.011
0.021
0.021
0.018
0.032

0.018
0.011
0.009
0.018
0.027

0.016
0.025
0.016
0.021
0.011

SpecimenPl. fig.
LengthWidthForm ratio
Pro!.
Radius vector(Measurements in mm)

440

Kimiyoshi SADA

volution of four specimens are 56-75,
94-113, 151-188, 264-321 and 377p, respectively. The spirotheca is thin and composed of a tectum and inner and outer
tectoria. The spirothecal thickness ofthe 1st to the 5th volution of four specimens is 11-25, 9-21, 18-23, 11-32 and
39p, respectively. The septa are almost
plane and closely spaced. The septal
counts of the 1st to the 6th volution ofa specimen illustrated as fig. 12 on Pl.
52 are 5, 11, 13, 15, 15 and 20, respectively. The chomata are well developed
and massive in the outer volutions. The
tunnel path is almost straight. The
tunnel angle of the 3rd volution of theholotype is 32°.
Remarks.-ln the shell size, the shell
shape, the number of volutions, therate of expansion, the spirothecal structure, and the mould of chomata, Profusulinella fusiformis SADA, sp. nov. is
closely allied to Profusulinella sp. B described by SADA (1961, pp. 105-107, pl.
10, figs. 4-8) from the Profusulinellazone in the middle part of the Kodani
formation of the Atetsu Limestone. The
striking similarities between these two
species indicate that they are indubitably conspecific each other. The present
species differs from Profusulinella toriyamai SADA (1961, pp. 97-99, pl. 9, figs.
1-13 and figs. 1-4 on Pl. 52 in this paper)from the Atetsu Limestone and the Taishaku Limestone in that the former species is fusiform in the shell shape andhas the larger form ratio and the slower
expansion of the shell. Profusulinella
fusiformis SADA, sp. nov. somewhat resembles P. beppensis TORIY AMA (1958,
pp. 31-33, pl. 2, figs. 1-6) from the Akiyoshi Limestone. However, P. fusiformis
can be easily distinguished from P. beppensis by its shape of the· shell, itslonger axis of coiling, its slower expansion, its larger form ratio and its larger

proloculus.
Occurrence.-Commonly found in theProfusulinella zone of the Taishaku. Limestone. Associated fusulinids are
Millerella sp. B, Profusulinella toriyamai
SADA, Pseudostaffella taishakuensis SADA,
sp. nov., Nankinella yokoyamai SADA, sp.
nov. and Staffella akagoensis TORIY AMA.
Type locality is Loc. No. A12801D.

Genus Pseudostaffella THOMPSON, 1942
Type species.-Pseudostaffella needhami

THOMPSON, 1942.
Pseudostaffella taishakuensis

SADA, sp. nov.
Pl. 52, figs. 13-21; Pl. 53, fig. 12

Description.- The shell of the present
species is small and spherical to subspherical in shape. The specimens offive volutions are 679 to 830p in lengthand 660p in width, giving the form ratioof 1.0 to 1.3. The shells of four volutions are 528 to 660p long and 528 to 622p
wide, having form ratio of 0.9 to 1.3.
The inner one to two volutions are tightly coiled and they show commonly endothyroid coiling.
The outside diameter of the proloculus
is 75p in the illustrated specimens. The
radius vectors of the 1st to the 5th volution of four specimens are 75, 94-132,
170-188, 207-321 and 358-396p, respectively. The spirotheca is thin and consists of a tectum and inner and outer
tectoria. The thickness of the spirothecaof the 1st to the 5th volution is 16-27,
16-23, 13-27, 23-29 and 25-34p, respectively. The chomata are well developed
and massive and asymmetrical in theouter volutions.
Remarks.-Pseudostaffella taishakuensis

SADA, sp. nov. is somewhat similar to606.

Fusulinids of Taishaku Limestone

441

Table 4. Measurements of Pseudostaf/ella taishakuensis SADA, sp. nov.
SpecimenPl. fig.
LengthWidth.
Form ratia
Pro!.
Radius vector

Thickness of
spirotheca

Vol.
1
2
3
4
5
0
1
2
3
4
5

Al2801D5b
52-13
0.660
0.528
1.3
0.075

A12801D10c
53-12
0.528
0.622
0.9
0.075

0.075
0.113
0.170
0.207

0.075
0.132
0. 188
0.321

0.034
0.027
0.021
0.021
0.025

0.013
0.016
0.016
0.013
0.029

A12801D7c
52-21
0.830
.0. 660
1.3
0.075

A12801D4d
52-20
0.679
0.660
1.0

0.094
0.188
0.283
0.396

0.094
0.188
0.245
0.358

0.018
0.021
0.016
0.025
0.025

0.023
0.023
0.027
0.023
0.034

(Measurements in mm)

Pseudostaffella kanumai IGO (1957, pp.
194-196, pl. 4, fig. 26, pl. 5, figs. 1-5) andP. kanumai pauciseptata IGO (1957, pp.
196-197, pl. 5, figs. 6-8) from the Ichinotani formation in the Fukuji area, Gifu
Prefecture, Central Japan. The former,
however, can be distinguished from thelatter two by its smaller shell, rather
larger form ratio and larger proloculus.
Pseudostaffella taishakuensis, sp. nov. can· be recognized from P. rotunda DoUGLASS(1971, pp. 6-9, pl. 2, figs. 4-21), which
was described from Peratovich Island
near Prince of Wales Island, Southeastern Alaska, by its smaller size of theshell, the smaller chomata and the narrower tunnel angles. Pseudostaffella taishakuensis, sp. nov. differs from P. sandersoni THOMPSON (1965, p. 227, pl. 33,
figs. 10-18) from British Columbia in
having a larger shell and thicker spirotheca.
Occurrence.-Common in the Profusulinella zone of the Taishaku Limestone.

Associated fusulinids are Millerella sp.
B, Profusulinella toriyamai SADA, P.
fusiformis SADA, sp. nov., Nankinella
yokoyamai SADA, sp. nov., Staffella akagoensis TORIY AMA. The type locality is
Loc. No. A12801D.
Family Staffellidae MIKLUKHOMAKLAY, 1949
Genus Nankinella. LEE, 1931
Type species.-Staffella discoides LEE,
1931.
Nankinella yokoyamai SADA, sp. nov.
Pl. 52, fig. 22; Pl. 53, figs. 1-2, 4-11

Description.-The shell of Nankinella
yokoyamai SADA, sp. nov. is discoidal
and planispiral throughout growth andhas umbilicate to partial umbilicate poles
and angular periphery in general. The
axial length and median width of theKimiyoshi SADA

442
Table 5.
SpecimenPl. fig.
LengthWidthForm ratio
Pro!.
Radiusvector

Vol.
1
2
3
4
5
6
7

Thicknessofspirotheca-~~-~---~

0
1
2
3
4
5
6
7

Measurements of Nankinella yokoyamai SADA, sp. nov.

A53112704
53-1
0.453
1. 4730.3
0.075

A12S01D4c
53-9
0.377
0.849
0.4
0.056

0.075
0.132
0.207
0.283
0.396
0. 566
0. 7550.075
0.132
0. 188
0.283
0.472

0.075
0. 132
0. 188
0.321
0.472

0.056
0.113
0.170
0.264
0.396

0.094
0. 188
0.283
0.415
0.566

0.056
0.113
0. 188
0.283
0.415
0.603

0.025

0.034
0.018
0.018
0.018
0.025
0.023

0. 011.
0.011
0.013
0.011
0.016
0.023

0.018
0.025
0.018
0.023
0.023
0.021

0. 011
0.032
0.023
0.023
0.021
0.025

0. 018
0.018
0.013
0.021
0.021
0.023
0.029

0.013
0.025
0.046
0.023

A12801D6c A12801D6d A12801D15b A12801D14c
53-10
53-11
53-4
53-6
0.415
0.245
0.510
0.340
1. 2080.849
0.698
1. 085
0.5
0.4
0.4
0.3
0. 056 ~
0.075
0.075
0.037

~-----·--------(Measurements in mm)

Explanation of Plate 52
Figs. 1-4. Profusulinella toriyamai SADA
1-2. Axial sections: Rg. No. A12801D2a (x22) and A12801D10a (x22), respectively.
3-4. Sagittal sections: Rg. No. A12801D6a ( x 22) and A12801D8f ( x 22), respectively.
Figs. 5-12. Profusulinella fusijormis SADA, sp. nov.
8. Axial section of the holotype: Rg. No. A12801D13b ( x 22).
9. Enlarged figure of Fig. 8 ( x 50).
5-6, 10-11. Axial sections of para types: Rg. No. A12801D13a ( x 22), A12801D14b (x 22),
A12801D8d (x22) and A12801D2b (x22), respectively.
7, 12. Sagittal sections of para types: Rg. No. A12801D8c ( x 22) and A12801D10a ( x 22),
respectively.
Figs. 13-21. Pseudostaf[ella taishakuensis SADA, sp. nov.
20. Axial section of the holotype : Rg. No. A12801D4d ( x 63).
13-17,21. Axial sections of paratypes: Rg. No. A12801D5b (x63), A12801Dla (x63),
A12801D4b (x63), A12801D1b (x63), A12801D4e (x63) and Al2801D7c (x63), respectively.
18-19. Sagittal sections of paratypes: Rg. No. A12801D9c (x63) and A12801D5a (x63).
Fig. 22. Nankinella yokoyamai SADA, sp. nov.
22. Sagittal section of a paratype: Rg. No. A12801D6b (x63).

606.

Fusulinids of Taishaku Limestone

holotype of the species (A53112704) illustrated as fig. 1 on Pl. 53, are 453 and1473p, respectively. Its form ratio is 0.3.
The specimens of five to six volutionsare 245 to SlOp long and 698 to 1208p
wide. Their form ratios range from 0.3
to 0.5.
The proloculus has the outside diameter of 37 to 75p in six specimens. The
radius vectors of the 1st to the 7th volution are 56-94, 113-188, 170-283, 264-415,
396-566, 566-603 and 755p, respectively.
The spirotheca is partly replaced by thesecondary mineralization and it seems
to be composed of three layers in the
inner volutions and four layers consisting of a tectum, diaphanotheca and innerand outer tectoria in the outer two volutions. The septa are unfluted and extend forward slightly. The septal countsof the specimen illustrated as fig. 7 on
Pl. 53 are 7, 9, 11 and 15, respectively,
for the 1st to the 4th volution. The
chomata are low. The tunnel angles of
the 3rd to 5th volutions of the holotype
are 14, 14 and 12 degrees, respectively.
Remarks.-Nankinella yokoyamai SADA,
sp. nov. resembles in some respects Nankinella plummeri THOMPSON (1947, pp.
155-157, pl. 32, figs. 11-16, pl. 33, figs.
10-11) from the Pennsylvanian rocks of
the Llano Uplift in Texas. However,
the mature form of the former species
has a longer axis of coiling, generally
larger proloculus and fairly thicker
spirotheca. Nankinella yokoyamai SADA,
sp. nov. is similar to Nankinella sp. A
by KOCHANSKY-DEVIDE (1965, p. 118, pl.
2, figs. 14-18). The former species, however, can be distinguished from the latter one by the larger shell, the larger
proloculus and the umbilicate form of
the former species. The species nameis dedicated to Dr. Tsuruo YoKOYAMA
who formerly carried on the study ofthe stratigraphy of the Taishaku Lime-

443

stone.
Occurrence.-Commonly found in theProfusulinella zone of the Taishaku
Limestone. Associated fusulinids are
Millerella sp. B, Profusulinella toriyamai
SADA, P. fusiformis SADA, sp. nov., andStaffella akagoensis TORIY AMA. The type
locality is Loc. No. A12801D.

Genus Staffella OzAWA, 1925
Type species.-Staffella sphaerica VON
MOLLER, 1878.
Staffella akagoensis ToRrY AMA
Pl. 53, fig. 3

1958. Staffella akagoensis ToRIYAMA. Mem.
Fac. Sci., Kyushu Univ., Ser. D, Geol.,
vol. 7, pp. 22-24, pl. 1, figs. 6-8.

Description.- The shell of Staffella akagoensis TORIY AMA is small, subsphericaland planispiral, having a broadly rounded periphery. The specimen of six volution (Pl. 53, fig. 3) is 566p long andlOOO,u wide, possessing a form ratio of
0.5.
The proloculus is small and its outside
diameter is 56p. The radius vectors of
the 1st to the 6th volution of a specimen
are 56, 94, 188, 283, 377 and 528p, respectively. The spirotheca is thin and seems
to consist of four layers such as a tectum,
a lighter layer seemingly like a diaphanotheca and inner and outer tectoria. The
thickness of the spirotheca of the outer
three volutions of a specimen is 18 to
25p. The chomata are low and asymmetrical.
Remarlzs.-The present species resembles closely Staffella akagoensis TORIY AMA (TORIY AMA, 1958) from the Profusulinella zone of the Akiyoshi Limestone
in all respects except for the length of
the shell and the form ratio. The pre-

Kimiyoshi SADA

444

Table 6. Measurements of Stafjellaakagoensis TORIYAMA.
Specimen A53112704Jb: Pl. 53, fig. 3.
Length0.566

Width
1. 000Radius vector
Vol.
1
0.056
2
0.094
0. 188
3
4
0.283
5
0.377
0.528
6

Form ratio
0.5

Prol.
0.056

Thickness of spirotheca
Vol.
0
1
2
3
4
0.018
0.018
5
0.025
6
(Measurements in mm)

sent form has the slightly shorter lengthof the shell and the smaller form ratio.
However, it seems that such a difference
between these two forms falls within
the specifk variation of Staffella akagoensis TORIYAMA.
Occurrence.- Abundant in the Profusulinella zone of the Taishaku Limestone.
Associated fusulinids are Millerella sp.
B, Profusulinella toriyamai SADA, P. fusijormis SADA, sp. nov., Pseudostaf!ella taishakuensis SADA, sp. nov. and Nankinella
yokoyamai SADA, sp. nov. Type locality
is Loc. No. Al2801D.

References(See also the references cited in the preceding papers by SADA (1967, 1969 and 1970))
DouGLAss, R.C. (1971) : Pennsylvanian Fusulinids from Southeastern Alaska. Geol.
Surv. Prof. Paper 706, pp. 1-20, pls. 1-7.
KocHANSKY-DEVIDE, V. (1965) : Die Fusuliniden Foraminiferen aus dem Karbon
und Perm im Velebit und in der Lika
(Kroatien) Mittleres und Oberes Perm.
jugoslavenska Akademija znanosti i Umjetnosti Odjel za Prirodne Nauke, Acta
geologica v, str. pp. 101-150, pls. 1-13.
SADA, K. (1961) : Profusulinella of Atetsu
Limestone. jour. Sci. Hiroshima Univ.,
Ser. C, val. 4, no. 1, pp. 95-116, pls. 9-10.
- - (1964) : Carboniferous and Lower Permian Fusulines of the Atetsu Limestone
in West. Japan. Ibid., val. 4, no. 3, pp.
225-269, pls. 21-28.
- - (1965) : Carboniferous and Permian
Stratigraphy of the Atetsu Limestone inWest Japan. Ibid., val. 5, no. 1, pp. 2180.
- - (1967) : Fusulinids of the Millerella
Zone of the. Taishaku Limestone (Studies of the Stratigraphy and the Microfossil Faunas of the Carboniferous andPermian Taishaku Limestone in WestJapan, No.1). Trans. Proc. Palaeont. Soc.
japan, N.S. no. 67, pp. 139-147, pls. 12-13.
(1969) : Microfossils of the Lowest Part

Explanation of Plate 53
Figs. 1-2, 4-11. Nankinella yokoyamai SADA, sp. nov.
1. Axial section of the holotype: Rg. No. A53112704 (x55).
2, 4-6, 9-11. Axial sections of paratypes: Rg. No. A12801D7a (x60), A12801D15b (x60),
A12801D13c ( x 60), A12801D14c ( x 60), A12801D4c ( x 65), A12801D6c ( x 60) and
A12801D6d (x60), respectively.
7-8. Sagittal sections of para types: Rg. No. A53112704Ja ( x 60) and A12801D8a ( x 60),
respectively.
Fig. 3. Stafjera akagoensis TORIYAMA
3. Axial section : Reg. No. A53112704Jb ( x 60).
Fig. 12. Pseudostafjella taishakuensis SADA, sp .. nov.
12. Axial section of a paratype: Rg. No. A12801D10c (x60).
Figs. 13-14. Millerella sp. B
13-14. Axial sections: Rg. No. A12801D2e ( x 91) and A12801D10g ( x 100).

SADA :

Fusulinids of Taishaku Limestone

Plate 52·~~~,_~ 3 ·~4
2

8

•

~

12

. ,

18

SADA:

Fusulinids of Taishalc~~ Limestone

Plate 53

606.

Fusulinids of Taishaku Limestone445

of the Taishaku Limestone (Ditto, No. 4).
Ibid., no. 75, pp. 119-129, pis. 12-13.
& YoKOYAMA, T. (1970): Fusulinids ofFusulinella Zone of the Taishaku Limestone (Ditto, No: 3). Mem. Fac. General
Educ. Hiroshima Univ. II I, vol. 4, pp. 4554, pl. 1.
THOMPSON, M.L. (1947) : Stratigraphy andFusulinids of Pre-Desmoinesian Pennsylvanian Rocks, Llano Uplift, Texas. jour.
Paleont., vol. 21, no. 2, pp. 147-164, pis.

31-33.
(1965) : Pennsylvanian and Early Permian Fusulinids from Fort St. JamesArea, British Columbia, Canada. Ibid.,
vol. 39, no. 2, pp. 224-234, pis. 33-35.
ToRIYAMA, R. (1954) : Geology of Akiyoshi.
Pt. 1. Study of the Akiyoshi LimestoneGroup. Mem. Fac. Sci., Kyushu Univ., Ser.
D, Geol., vol. 4, no. 1, pp. 40-97.
(1967) : The Fusulinacean Zones of Ja·
pan. Ibid., vol. 18, no. 1, pp. 35-260.

Akiyoshi Limestone 1':k2f:r:ifk:'G
Atetsu LimestonelliiJtf:r:ifk:'G
Fukujirffi
J:lli

Ichinotani
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PROCEEDINGS OF THE PALAEONTOLOGICAL SOCIETY
OF JAPAN

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Prefecture ........ HAT AI, K. & NooA, H.
Scaphopoda-!ike fossils from the Udo Formation (Miocene) of Miyazaki Prefecture, Japan ........................... .
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the Tetori Group, Central Honshu, Japan.
................ KIMURA, T. & SEKIDO, s.
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Lower Carboniferous Visean faunas discovered from Mitsusawa, southeastern partof the Kwanto massif, Japan, Part 1.
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Transactions and Proceedings of the PalaeontologicalSociety of Japan

New Ser ies No. 87

September 30, 1972

CONTENTS
TRANSACTIONS
601.

MATSUMOTO, Tatsuro, MURAMOTO, Tatsuo and !NOMA, Akitoshi:

602.

small desmoceratid ammonites from Hokkaido (Studies of the Cretaceous ammonites from Hokkaido and Saghalien-XXIV) .. . .. .... .. . .. 377
MASUDA, K6ichir6: Swiftop ecten of the Northern Pacific . ............... 395

603.

Two

HAT AI, Kotora, NODA, Hiroshi and OGASAHARA, Kenshiro: Scaphopodalike fossils from the Udo formation (Miocene) of Miyazaki Prefecture,

604.

Japan . . .. . .... .. ....... . ............ .. ... .... . .... . . . . . . .. . ... .. . . .. . 409
OKIMURA, Yuji: Permo-Carboniferous endothyraceans from Japan, Part

605.

1. Biseriamminidae .... . . ... . . . . . . . . ..... . .. . . . ..... . ..... ..... ... ... 414
TAKAYAMA, Toshiaki: A note on the distribution of Braa rudosphaera
bigelowi (GRAN & BRAARUD) DEFLANDRE in the bottom sediments of

Sendai Bay, Japan ..... ... ... . .. . .. ... .............. .... . . . . . . .. .. .. . . 429
606. SADA, Kimiyoshi : Fusulinids of the Profu sulinella zone of the Taishaku
Limestone. (Studies of the stratigraphy and microfossil faunas of the
Carboniferous and Permian Taishaku Limestone in West japan, No.2) . . 436
PROCEEDINGS . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 446