Transactions and Proceedingsof thePalaeontological Society of Japan
New Series

No. 91

Palaeontological Society of Japan
September 20, 1973

Editor: Hiroshi U]lIE
Associate editors: Ikuwo OBATA, Yasuji SAITO, Kazuhiko UEMURA

Officers for 1973 - 1974
Honorary President:
President:

Teiichi KOBAYASHI

Tatsuro MATSUMOTO

Councillors (*Executive):

Kazuo ASAMA,* Kiyoshi ASANO, Kiyotaka CHINZEI,* Taka-shi HAMADA,* Tetsuro HA NAI,* Kotora HATAI, Itaru HAYAMI, Kametoshi
KANMERA,* Tamio KOTAKA, Tatsuro MATsuMoTo,* Tokio SHIKAMA, Tsugio
SHUTO, Yokichi T AKAYANAGI,* Toshimasa TANAI, Hiroshi UJIIE*
Executive Committee:
General Affairs:
Membership:

Kiyotaka CHINZEI, Yasuhide IWASAKI

Kazuo ASAMA, Ienori FUJIYAMA

Finance:

Takashi HAMADA, N aoaki AOKI

Planning:

Tetsuro HANAI, Saburo KANNO

Publications
Transactions:

Hiroshi UJIIE, Ikuwo OBATA, Yasuji SAITO, Kazuhiko UEMURA

Special Papers;"Fossils":

Kametoshi KANMERA, Itaru HAYAMI, Tomowo OZAWA

Yokichi TAKAYANAGI, ToshiakiATAKAYAMA

Fossil on the cover is Bellerophon jonesianus DE KONINCK
from the Late Permian Akasaka Series in Gifu Prefecture.

All communications relating to this journal should be addressed to the
PALAEONTOLOGICAL SOCIETY OF JAPAN
c/o Business Center for Academic Societies, Japan_
Yayoi 2-4-16, Bunkyo-ku, Tokyo 113, Japan
Sole agent:

University of Tokyo Press, Hongo, Tokyo

Tral).s. Proc. Paleont. Soc. Japan, N.S., No. 91, pp. 113-125, pIs. 17-19, September 20, 1973

620.

PLANKTONIC FORAMINIFERA OF THE NISHIKUROSA W A
FORMATION, NORTHEAST HONSHU, JAPAN*TSUNEMASA SAITO
Lamont-Doherty Geological Observatory of Columbia University,
Palisades, New York 10964

andSEljURO MAIY A
Japan Petroleum Exploration Company, Otemachi, Tokyo 100

i§ ,w.lR~ !1El¥;Q1i1::fffL!k: l'fdIl t~ :9HJiJ:=I~~b i¥i W, ~ ~tf~m: O)i1lii'l'tle R tll T Qi!i!! lR~ XI'
I?, Globorotalia peripheroronda BLOW and BANNER, G. birnageae BLOW, G. denseconnexa SUBBOTINA, Globigerina praebulloides pseudociperoensis BLOW ~-C~<fil&-:5
It I? tL Q1-'F ;Q1ti1: :ff:rLEl,,-i t:tif,f: '.!:' ~ I:H U': o ilH1',1r'i i':jIH;l: -tc III ~ ~l1'b~p I? 40 m in: 0) i!i!! lRfoj
J:rlil-c;b Qo .::. O)it1:1nf:'.!:'t.~t~T Q ~illO)'::' tL '5::"t' lellcfoiN ~ ~1,t.: ~tI"T':a'9Jj;(1l:(r 'b Ie L.. "'Ci!i
Hi1dR~o)Jl<ftt:(r~[~:TQ
BLOW (1969) 0) Zone N. 8-N. 9 le~Htl±,,*Qo Zone N. 8
N. 9 O)r.(tUJIHC!ll:~t.J: Praeorbulina ~o)~iI~ff1'£L..t.J:"\t::/l)IC, i!im.1RmtW~:(r="'?0)1Ir-0)
c'0l?iI>lel:~JET Q .::. c f;l:4-O) c .::. ;:'if,Ji;'ffi-C;b QiI~, G. peripheroronda iI'nf:~O) 1fi~t.J:t1IJ.
~~~-C<b Q*~iI\I?'i- Q c, i§mdRUf~v;l: N. 9 le:*Ht-r Q O)iI~~~ c:%'.!t I?tLQ o Globorotalia quinifalcata :to J: '(f Globigerinoides japonicus 0) 2 l¥;Q1i1::ff:rL!kfiU~*lTffTi c L.. "'C
Ilcijij(~tL"'C"\Qo
it ii.~ 'If'; 1£ • ~(: ~ ~ 'II\'! ~B

*1

c

r

c

c

copper and zinc. On the other hand,
Paleogene sediments are locally distributed in the Japanese Islands, along thesouthwestern coast and on the northernmost island of Hokkaido.
A sequence of Neogene strata exposed
along the coast of the Oga Peninsula,
Akita Prefecture, has been the focus ofparticular attention since this sequenceis widely recognized as a standard forthe correlation of Japanese Neogene
formations. There the following eight" stages" have been established in orderof decreasing age (HUZIOKA, 1956; MINATO et at., 1965): Nishioga, Daijima, Nishikurosawa, Onnagawa, Funakawa, Kita-

Introduction

Over most of the Japanese Islands thefirst major transgression occurred inearly Miocene time. This transgression
cluminated in middle Miocene time submerging most of the Islands and depositing as much as 5,000 meters of sedimentin some basins. The Neogene formations
have been studied intensively not only
because they are widely distributed but
also because of their being reservoirs ofimportant minerals·· such as petroleum,* Received March 10, 1973; read January
17, 1973 at Sendai.
113

114

Tsunemasa SAITO and Seijuro MAIY A

ura, Wakimoto and Shibikawa Stages.
The Nishioga and Daijima Stages comprise largely terrestrial and deltaic
facies deposited prior to the marinetransgression. The other six stages
include typical marine facies, representing sediments and faunas accumulated
in the Neogene sea. Thus, the Nishikurosawa Stage represents an important
period in the geologic development of
the japanese Islands marking the firststage of the extensive Neogene marinetransgression.
The name Nishikurosawa was first
introduced by OHASHI (MS) in 1918 (fide
CHITANI, 1925) as the Nishikurosawa
beds. Its type locality was chosen on
the northern coast of the Oga Peninsula,at Nishikurosawa, Oga City, Akita Prefecture, where it unconfor~ably overlies
volcanic rocks of the Nishioga Stage
and consists largely of bluish-grey calcareous sandstone. The type Nishikurosawa Formation contains abundant marine faunas such as the foraminifera
Amphistegina radiata (FICHTEL andMOLL), Miogypsina kotoi HANZA WA andOpereulina eomplanata japoniea HANZAWA; the molluscs Chlamys kaneharai(YOKOY AMA) and Anadara makiyamai(YOKOYAMA); and the echinoids Eehinolampus yoshiwarai LORIAL and Astriclypelts manni ambigenus NISHIYAMA, allindicative of a shallow marine environment. The Nishikurosawa Formation
crops out in the western part of the
Oga Peninsula, across a distance of about
15 km, along hill-sides, brook and stream
banks, road cuts and sea coast, in a trend
striking northwest-southeastward. It isonly 20 m thick at the type locality but
thickens considerably southward attaining a thickness of about 250 m on thesouthern coast of the Peninsula. Thechange in thickness is also accompanied
by facies changes and, on the southerncoast, the formation is largely composedof a grey, thinly-bedded siltstone, underlain by a thin basal conglomerate bed(HUZIOKA, 1959). These two sections of
the Nishikurosawa Formation have been
regarded as the type section of the Nishikurosawa Stage, the northern section
representing shallow-water facies andthe southern section characterized byshallow to moderately deep water facies(see MINA TO et al., 1965).
The faunas of the Nishikurosawa Formation have received considerable attention. Molluscan fossils have been described by HATAI (1938), NOMURA andHATAI (1938) and KOTAKA (1957). Larger
benthonic foraminifera have been studied by YABE (1927,1933), HANZAWA (1935,1964), U]IlE (1966) and MATSUMARU (1971).
Occurrences of benthonic smaller foraminifera have been listed by HUZIOKA (1959)
and IKEBE (1962).
The age of the Nishikurosawa Formation has so far been discussed largelyin the light of the two larger benthonicforaminifera Miogypsina kotoi HANZAW A
and Opereulina eomplanata japoniea HANZA WA. Y ABE (1927), in recognizing asimilarity of these two larger foraminifera with those from the Tertiary ofEurope, assigned a Burdigalian (middle
Miocene) age to the Nishikurosawa Formation. However, in proposing the existence of two separate stratigraphic
horizons characterized by distinct larger
benthonic foraminiferal assemblages injapan, HANZAWA (1950) reassigned a
Helvetian age to those strata containing
Miogypsina kotoi and Opereulina eomplanata japoniea assemblage and a Burdigalian age to those strata having Lepidoeyclina assemblage. However, no single
stratigraphic sequence bearing the two
faunas superposed one upon the otherhas been found in japan.

620.

115

Planktonic Foraminifera of Nishikurosawa

Field and laboratory procedures
Although the type section of the Nishikurosawa Formation has been intensively searched for planktonic foraminifera, no planktonic species have so far
been reported. The shallow marine
facies of the type Nishikurosawa Formation (indicated by the occurrence ofbenthonic foraminifera Operculina complanata japonica, Miogypsina lwtoi, Florius kidoharensis (FUKUDA), Ammonia
tochigiensis (UeHIo), Elphidium sp., andCibicides refulgens MONTFORT) is likely
to be the deciding factor for the absenceof planktonic foraminifera. A well preserved planktonic foraminiferal assemblage described here was recovered froman exposure of the Nishikurosawa Formation on the beach of Daijima at theconfluence of a small stream with thesea near the eastern edge of Daijima
Village, Oga City, Akita Prefecture, Japan (Text-fig. 1). This sample was taken
approximately 40 m below a glauconitic
sandstone bed of the basal Onnagawa
Formation and lies within the upper
part of the Nishikurosawa Formation,
which has a total thickness of about 250
m in this area.

SEA
OF

FUNAKAWA
HARBORN!

IOOO;;;;;.._~""'~=;....

Text-fig. 1.

_____
OOO M

Location of sample used in this study.

Most of the species recovered fromthis locality possess a fragile, thin,coarsely perforate wall, whereas therock sample consisting of greenish-grey
sandy siltstone was highly indurated.

Therefore, a special rock maceration
technique was needed to extract foraminifera. Crushed rocks of nut-size wereplaced in a beaker and then oven-driedfor two hours at a temperature of about

116

Tsunemasa SAITO and Seijuro MAlYA

100·C. Then boiling water saturated
with sodium sulphate (Na2S0,1) was poured over the rocks until all rock-pieces
were soaked with the liquid. After allowing about 30 minutes for the solution
to completely saturate the rocks, theexcess solution was drained off and thebeaker was placed in a cool, dry place
for about one week. By then the rockspecimens were completely disintegrated
due to the growth of sodium sulphatecrystals inside the pore space. The disintegrated rocks were then boiled inwater with the addition of 1-2% volume
of sodium hexametaphosphate. The sample was finally wet-sieved with a standard 200 mesh sieve.
Planktonic foraminifera

Since BERGGREN (1972) proposed arefined Cenozoic radiometric time-scale
to which planktonic microfossil zonal
schemes can be related, the planktonic
foraminiferal assemblage of the Nishikurosawa Formation offers an excellent
opportunity to document its precise position within the world-wide chronostratigraphic framework and to date thetime of Neogene transgression over theJapanese Islands. Three species makeup the majority of the fauna: Globorotalia peripheroronda BLOW and BANNER,
G. denseconnexa SUBBOTINA and Globigerina praebulloides praebulloides BLOW.
The other species identified are: Globigerina woodi JENKINS, G. praebulloides
pseudociperoensis BLOW, G. a ngu stiu 1Ilbilicata BOLLI, Globorotalia birnageae
BLOW, G. quini/alcata SAITO and MAIY A
n. sp., Globigerinita glutinata (EGGER),
Globoquadrina obesa AKERS and Globigerinoides japonicus SAITO and MAIY A
n. sp. Text-fig. 2 shows the rangesof these species as presently understoodin terms of the zonation of BLOW (1969).

Because the Nishikurosawa Formation
was deposited in a rather shallow-water
environment in a high northerly latitude(40·N), the fauna like those of European
type sections, is characterized by a small
number of species, precluding a full
representation of those species living
contemporaneously in deeper-tropicalwaters. Thus, species diversity is low,
and the lack of certain species cannot
positively be taken as evidence for a
specific zonal assignment. Therefore, acorrelation can best be achieved by thosespecies that are present. On the presence of G. birnageae, G. peripheroronda
and Globoquadrina obesa, the Nishikurosawa can be assigned to the interval
encompassing zones N.B and N.9 of
BLOW (1969). G. denseconnexa has notbeen recorded previously from the Far
East Neogene sequences but has beenreported by PARKER (1964) from the Experimental Mohole section near Guadalupe Island, Mexico. SUBBOTINA et al.
(1960) reported it as ranging from the
Oligocene to the Helvetian-Tortonian.
Although this is the first report ofplanktonic foraminifera from the Nishikurosawa Formation, the planktonic foraminifera from other formations assignable to the Nishikurosawa Stage havebeen reported. These are the Higashiinnai Formation of the Noto Peninsula(ASANO, 1962; SAITO, 1963), Uyashinai
Formation of Akita Prefecture (SAITO,
1963) and the Nanatani Formation of
Niigata Prefecture (SHINBO and MAIYA,
1971), and represent marine facies deeper
than that of the type Nishikurosawa
Formation. In the upper part of theseformations, the extinction point of Globorotalia peripheroronda was observed tooccur near the first appearance of C.
praemenardii CUSHMAN and STAINFORTH,
both species thus ranging concurrently
for a short stratigraphic interval. BLOW

620.

Planktonic Fomminifera of Nishikurosawa

117_____ 7___ _N:IO
Globorotalia
peripheroocuta

N.9

Text-fig. 2. Comparison of zonations and boundaries, ranges of planktonic foraminifera,
and stratigraphic position of various formations in the northeast Honshu, Japan.

(1969) showed a similar overlapping rangeof the two species occurring at the N.9j
N.10 boundary. As a result, the upper
limit of the Nishikurosawa Stage aspreviously understood by Japanese geologists extends to within Zone N.10, ahorizon somewhat higher than that indicated by the fauna from the Nishikurosawa Formation of the Oga Peninsula.
SHINBO and MAIY A (op. cit.) indicatedthat in the Japanese Neogene G. peripheroronda abounds only in strata equivalent to Zone N.9 of BLOW. Therefore,
the common occurrence of this species
in the present Nishikurosawa fauna may
also indicate its correlation with Zone
N.9, although its exclusion from Zone
N.8 cannot be ruled out on this evidence
alone.
In conclusion, our correlation of theupper Nishikurosawa Formation with
Zone N.9 would date the beginning of
the Neogene innundation of the greaterpart of the Japanese Islands roughly
about 17 million years B. P. based upon
the time-scale of BERGGREN (op. cit.).

Systematic paleontology

At least 11 species of planktonic foraminifera, of which two are new, arepresent in the Nishikurosawa Formation.
All are described and illustrated herewith the aid of a scanning electron microscope. The synonymy is not intended
to be complete; special emphasis is given
to cross-reference those reports dealing
with the western Pacific region. Mostof the illustrated specimens are deposited in the micropaleontology collectionof the National Science Museum, Tokyo,
Japan. Duplicate paratypes of two new
species are deposited in the micropaleontology collection, U. S. National Museum of Natural History, Washington, D.C.
Family Globigerinidae CARPENTER;
PARKER and JONES, 1862
Genus Glohigerina I)'ORBIGNY, 1826

Globigerina praebulloides praebulloides
BLOW, 1962

118

Tsunemasa SAITO and Seijuro MAIY A
PI. 17, fig. 1a-c

Globigerina praebulloides BLOW, 1959, pp. 180,
181, pI. 8, fig. 47a-c ; JENKINS, 1960, p. 352,
pI. 2, fig. 1a-c; SAITO, 1963, p. 187; HUANG,
1969, pI. 2, figs. 48, 49; BANDY and INGLE,
1970, figs. 7, 18, 19.
Globigerina praebulloides praebulloides BLOW.
BLOW, 1962, pp. 92, 93, pI. 9, figs. 1, 2.

Remarks :-This species is distinguished from G. bulloides by its elongate
equatorial profile, the final chamber
which increases rapidly in size, and arather low-arched aperture with a lip.
It has a smoother chamber wall thanG. woodi. Maximum diameter of figured
specimen: 0.46 mm.
Globigerina praebulloides
pselldociperoensis BLOW, 1969
PI. 17, fig. 4a-c
Globigerina

praebulloides pseudociperoensis
BLOW, 1969, pp.381-382, pI. 17, figs. 8, 9.

Remarks:-This subspecies is distinguished from the Oligocene G. ciperoensis ciperoensis BOLLI by the more
rapidly opening and higher spire. Alsoin this subspecies, chambers increasein size more gradually than those of G.
ciperoensis. It also differs from Globigerina concinna REUSS in its much smaller umbilicus and a low-arched aperture.
Maximum diameter of figured specimen:
0.22mm.
Globigerina woodi JENKINS, 1960
PI. 17, figs. 2a, b, 3
Globigerina woodi JENKINS, 1960, p. 352, pI. 2,
fig. 2a-c; TAKAYANAGI and SAITO, 1962,
p. 91, pI. 25, fig. 6a-c; SAITO, 1963, p. 188;
JENKINS, 1965b, p. 117, pI. 17; JENKINS
and ORR, 1972, p. 1090, pI. 111, figs. 10-12.
Globigerina woodi woodi JENKINS. JENKINS,
1971, pp. 159, 160, pI. 18, figs. 548-550.

Remarks:-This species is characterized by having a coarsely perforate wall,a high-arched aperture with rim, andU-shaped sutures. Maximum diameterof figured specimens: 0.32 mm.
Globigerina angustiumbilicata BOLLI, 1957
PI. 17, figs. 5, 6a, b
Globigerina

ciperoensis
angustiumbilicata
1957, p. 109, pI. 22, figs. 12, 13.
Globigerina angustiumbilicata BOLLI. BLOW,
1959, p. 172, pI. 7, figs. 2a-c ; T AKAY ANAGI
and SAITO, 1962, pp. 82, 83, pI. 28, figs.
3-9; SAITO, 1963, p. 183.
BOLLI,

Remarks:-This species has been regarded as the ancestor of G. pachyderma
by SAITO (op. cit.) and of G. qllinqlleloba
by ASANO et al. (1968). It is characterized by a very small interiomarginal
aperture, which is often concealed underneath a distinct lip.

Family Globorotaliidae CUSHMAN, 1927
Genus Globorotalia CUSHMAN, 1927
Globorotalia birnageae BLOW, 1959
PI. 18, figs. la, b, 2
Globorotalia birnageae BLOW, 1959, pp. 210,
211, pI. 17, fig. 108a-c; SAITO, 1963, p. 174,
pI. 56, fig. 3a-c; BLOW, 1969, p. 346, pI. 34,
figs. 7, 8.

Remarks:-This short-ranging species
has been reported sporadically only fromthe Caribbean region and Japan. This
species has five to six chambers in thelast whorl, most of the Nishikurosawa
specimens being five-chambered. It differs from G. siakensis in being consistently much smaller in size and in having
an almost closed umbilicus. It is also
distinguished from G. peripheroronda inhaving more circular outline and rather

620.

Planktonic Foraminifera of Nishiku'Y'osawa

tangentially elongated chambers as viewed from the spiral side. Maximum diameter of figured specimens: 0.20-0.24mm.
Globorotalia peripheroronda BLOW

and BANNER, 1966
PI. 17, figs. 7a, b, 8
Globorotalia barisanensis (sic) LERoy. STAIN·FORTH, 1948, p. 120, pI. 26, figs. 24-26.
Globorotalia fohsi barisanensis LERoy. BOLLI,
1957, p. 119, pI. 28, fig. 8a-c; CHANG, 1959
(part), pp. 68, 69, pI. 5, figs. 6, 7 (not figs.
8, 9) ; SAITO, 1963, p. 176, pI. 53, figs. 3,
4; HUANG, 1963 (part), p. 165, pI. 5, fig.
2a-c (not fig. la-c) ; JENKINS, 1972, pI. 29,
figs. 9-1l.
Globorotalia fohsi barisanensis (LERoy).
BLOW, 1959, p. 212, pI. 17, figs. 110,ll1a-c.
Globorotalia (Turborotalia) peripheroronda
BLOW and BANNER, 1966, p. 294, pI. 1,
fig. 1a-c, pI. 2, figs. 1-3.
Globorotalia fohsi peripheroronda BLOW and
BANNER. OLSSON, 1972, pp. 170-172, figs.
4-6.
Not Globorotalia barisanensis LERoy, 1939.

Remarks :-This is probably one of themost widely recorded Miocene planktonic
foraminifera (JENKINS, 1965a, p. 266). It
is characterized by a generally lobate
equatorial periphery, fairly deeply incised sutures on the spiral side, and aparticularly distinct sinuous suture between the last and penultimate chamberson the spiral side. Maximum diameterof figured specimens: 0.27-0.31 mm.
Globorotalia denseconnexa
SUBBOTINA, 1960
PI. 18, figs. 3, 4a, b
Globorotalia denseconnexa SUBBOTINA, 1960,
pp. 67-69, pI. 13, figs. 4-6; PARKER, 1964,
p. 631, pI. 102, figs. 10-12.

119Remarks:-As PARKER (op. cit.), theNishikurosawa forms were unable to becompared with topotypes or plesiotypes
of SUBBOTINA's species. Our specimens
are closely comparable with those described from the Experimental Mohole
cores by PARKER in that they are coarsely perforate for their size and have fiveto six chambers which are bound by
short, gently-curving sutures on the
spiral side. Maximum diameter of
figured specimens: 0.24-0.26 mm.
Globorotalia quinifalcata SAITO

and MAIY A. n. sp.
PI. 18, figs. 5a-c, 6a-c
Globorotalia scitula (BRADY) subsp. praesci·
tuta BLOW. JENKINS, 1960, p. 366, pI. 5,
fig. 62a-c.
Globorotalia scitula praescitula BLOW. SAITO,
1963, p. 181, pI. 53, fig. 6a-c.

Description:-Test low trochospiral,
umbilico-convex, spiral side slightly convex, umbilical side vaulted; spire opening fairly rapidly, with four to fivechambers in the last whorl; equatorial
periphery weakly lobulate, Uniformly
perforate, without carina or pseudocarina; axial periphery rounded; suturesof the spiral side depressed and strongly
curved; sutures of the umbilical side
depressed, slightly sinuous to radial;chambers almost crescent-shaped as seenfrom the spiral side; aperture interiomarginal, umbilical-extraumbilical, a low
arch with a distinct lip; wall calcareous,perforate. Maximum diameter of holotype 0.24 mm; para type (fig. 6a-c) 0.25mm.
Remarks:-This species differs fromG. peripheroronda in having chambers
more tangentially elongate, a morestrongly vaulted umbilical side, andgently curving sutures on the spiral

120

Tsunemasa SAITO and Sei}uro MAIY A

side. This form has frequ.ently been
misidentified as G. praescitula BLOW by
previous authors. Our examination of
BLOW'S holotype indicates that G. praescitula is a rather unique form having
four strongly lobulate chambers in thelast whorl (pI. 18, fig. 7a-c). It differsfrom G. quinifalcata, n. sp. in having
more strongly lobulate chambers on the
spiral side, a distinctly lobate equatorial
periphery and more strongly curved
sutures on the spiral side, and a much
deeper umbilicus. The specimen described as G. scitula praescitula by PARKER(1964) from the Experimental Mohole
core is, in our opinion, not G. praescitula
BLOW but synonymous with G. quinifalcata because of its distinctly umbilicoconvex test and the last whorl consisting of five, rather than four, less lobulate chambers. This new species iswidely distributed over the Japanese Islands and occurs commonly in association with G. peripheroronda BLOW and
BANNER. G. quinifalcata closely resembles Globorotalia canariensis (O'ORBIGNY)
var. minima AKERS, the holotype of
which is here re-illustrated (pI. 18, fig.
8a-c)_ However, G. minima can be distinguished by having a distinctly compressed periphery, and a pseudocarina

in the earlier chambers of the last whorl.
Since the specimens of this species arepoorly preserved in the Nishikurosawa
Formation, the types of G. quinifalcata
are chosen from the Hojuji Formationof the Noto Peninsula, Japan. The foraminiferal assemblage of the Hojuji
Formation is closely comparable withthe present Nishikurosawa fauna in species composition.
The specific name is from the Latin
quini, five and falcata, sickle-shaped, referring to the five tangentially elongate
chambers of the last whorl as seen fromthe spiral side.
Type locality:-Sample N-H-13, middle
part of the Hojuji Formation, from asmall road-side cliff in the village of Go,
on the north side of the road, about 3
km west of the Ukai railroad station,
Ukai City, Kanazawa Prefecture, Japan;
in a dark grey diatomaceous mudstone.
Genus Globigerinita BRONNIMANN, 1951
Globigerinita glutinata (EGGER), 1893
PI. 19, fig. 1a-c

Globigerilla glutinata EGGER, 1893, p. 371, pI.
13, figs. 19-21; TAKAYANAGI and SAITO,
1962, pp. 86-88, pI. 27, figs. 13-17; SAITO,

Explanation of Plate 17
Fig. la-c. Globigerina praebulloides praebulloides BLOW.
la, Spiral view.of hypotype (NSMT 660). 1b, Side view. 1c, Umbilical view. x102.
Figs. 2a-c, 3. Globigerina woodi JENKINS.
2a, Spiral view of hypotype (NSMT 662). 2b, Side view. 2c, 3, Umbilical view of hypotype (NSMT 663). x 128.
Fig 4a-c. Globigerina praebulloides pseudociperoensis BLOW.
4a, Spiral view of hypotype (NSMT 661). 4b, Side view. 4c, Umbilical view. x 145.
Figs. 5, 6a-b. Globigerina angustiumbilicata BOLLI.
5, Spiral view of hypotype (NSMT 664). 6a, Side view of hypotype (NSMT 665). 6b,
Umbilical view. x 145.
Figs. '{a-b, 8. Globorotalia peripheroronda BANNER and BLOW.
7a, Spiral view of hypo type (NSMT 668). 7b, Side view. 8, Umbilical view of hypotype(NSMT 669). x 145.

SAITOand MAIYA:

Planktonic Foraminifem of Nishikurosawa

Plate 17

620.

Planktonic Foraminifera of Nishikurosawa

1963, p. 185, pI. 56, fig. 4.
Globigerinita glutinata (EGGER). PARKER,
1962, pp. 246-249, pJ 9, figs. 1-16; HUANG,
1967, p. 187, pI. 16, fig. 6a, b.

Remarks:-This species usually has
three and a half inflated chambers in
the last whorl, a small umbilicus, a lowarched elongate umbilical aperture witha thin lip, and an irregular-shaped umbilical bulla with numerous infralaminal
apertures. It also has a thin but very
finely perforated wall. The umbilicalbulla of the figured specimen broke off
during the sample preparation process,and only a fraction of it can now beseen as a faint raised ring on the apertural face. The maximum diameter of
figured specimen: 0.28 mm.

Genus Cloboquadrina FINLAY, 1947
Cloboquadrina obesa AKERS, 1955
PI. 19, figs. 2a-c, 3a-c
Globoquadrina obesa AKERS, 1955, p. 661, pI.
65, fig. 5a-c.
Not Globoquadrina larmeui obesa AKEHs.
BLOW, 1969, p. 342, pI. 28, figs. 7, 9.

Remarks:- The holotype of Cloboquadrina obesa AKERS (USNM P 4758) in thecollections of the U. S. National Museumof Natural History, Washington, D. C.
has been examined. The type figure of
AKERS (op. cit.) is a fairly good representation of the specimen, portraying
three inflated chambers in the last whorl.
In the umbilical view, this species closely
resembles Clobigerina tripartita KOCH of
BANNER and BLOW (1962, pI. 10, figs. DF), but differs in having a broader apertural face which slopes more gently
towards the umbilicus. The specimen
identified by BLOW (1969, op. cit.) as C.
larmeui obesa AKERS is considered to bedifferent from C. obesa AKERS because

121

of its final whorl consisting of four,
rather than three, distinct chambers.
The Nishikurosawa specimens are closely comparable with the holotype in that
all have three inflated chambers in the
final whorl and a distinct apertural faceof the last chamber on the umbilical side.
Maximum diameter of figured specimens: 0.31-0.42 mm.

Genus Globigerinoides CUSHMAN, 1927
Globigerinoides japonicus SAITO

and MAIYA, n. sp.
PI. 19, figs. 4a-b, 5a-b, 6a-b

DescrijJtion:- Test free, medium in sizefor the genus, moderately high trochospire, equatorial profile ovoid, equatorial
periphery slightly lobulate; axial profile
suboval, axial periphery broadly roundcd; chambers rounded, inflated, fairly
rapidly and almost uniformly increasing
in size, four chambers making up eachwhorl, in all three whorls visible; intercameral sutures depressed, increasingly
so during the ontogeny, becoming almost
incised between the last few chambers;
only two apertures present on the test
exterior; primary aperture interiomarginal, a low intraumbilical arch, oftenwith a narrow rim; single spiral supplementary sutural aperture, small hole or
crescent-shaped opening with no rim,situated at the junction of the last intercameral suture and spiral sutures; wallcalcareous, thick, markedly cancellate
and punctate. Maximum diameter ofholotype 0.32 mm; paratype (fig. 4a-b)0.28 mm; para type (fig. 6a-b) 0.32 mm.
Remarks:- This species is closely related to forms referred by workers to
Globigerinoides trilobus (REUSS), G. quadrilobatus (D'ORBIGNY) and C. sacculifer(BRADY), together with various combi-

122

Tsunemasa SAITO and Seijuro MAIY A

nations of these names and so-called
subspecies. It is distinguished as a separate species because of its single spiral
supplementary aperture and a rather
high trochospiral test for the genus.
There is considerable morphological resemblance between this species and Giobigerina woodi JENKINS, although theformer has a distinct supplementary
aperture and, therefore, belongs to thegenus Giobigerinoides. This species has
so far been found only in the Nishikurosawa Formation and very little is
known about its stratigraphic range andgeographic distribution.

Acknowledgements
The samples used for this study werecollected in September, 1971, during theU. S.-Japan cooperative field work ofmarine Neogene sediments exposed along
the Sea of Japan coast. Participationof both Japanese and U. S. scientists inthe work was made possible with financial support from the Japan Society of
the Promotion of Science and the U. S.
National Science Foundation (National
Science Foundation Grant No. GA 20211).

The authors are especially grateful to
Dr. Yutaka IKEBE, a member of theBoard of Directors of the Japan Petroleum Exploration Company for making
available the company facilities for thefield work to the project. We wish to
thank Dr. Yasumochi MA TOBA, Instituteof Mining Geology, Akita University forleading the field trip to the Oga Peninsula. and indicating the presence ofplanktonic foraminifera at the Daijima
locality.
The joint laboratory work of theauthors was made possible by the Japan Petroleum Exploration Company forhaving made possible S. MAIYA'S visit
to the Lamont-Doherty Geological Observatory where research on the sample
and preparation of the manuscript wereconducted.
Miss Dee BREGER took the scanningelectron micrographs of the specimens
illustrated, and Miss Linda Lee MURPHY
typed and proofed the manuscript. This
assistance is greatly appreciated. Appreciation is also expressed to Dr. L. H.
BURCKLE and Mr. P. R. THOMPSON for
critically reviewing the manuscript andmaking many helpful suggestions.

Explanation of Plate 18
Figs. 1a-b, 2. Globorotalia birnageae BLOW.
la, Spiral view of hypotype (NSMT 666). 1b, Side view. 2, Umbilical view of hypotype(NSMT 667). x 145.
Figs. 3, 4a-b. Globorotalia denseconnexa SUBBOTlNA.
3, Spiral view of hypotype (NSMT 670). 4a, Side view of hypotype (NSMT 671). 4b,
Umbilical view. x 145.
Figs. 5a-c, 6a-c. Globorotalia quinifalcata SAITO and MAry A, new species.
5a, Spiral view of holotype (NSMT 672). 5b, Side view. 5c, Umbilical view. 6a, Spiralview of para type (NSMT 673). 6b, Side view. 6c, Umbilical view. x145.
Fig. 7a-c. Globorotalia scitula (BRADY) subsp. praescitula BLOW, 1959 [= Globorotalia praescitula
BLOW], holotype (USNM 625713) reillustrated.
7a, Spiral view. 7b, Side view. 7c, Umbilical view. x149.
Fig. 83.-c. Globorotalia canariensis (D'ORBIGNY) var. minima AKERS, 1955 [= Globorotalia minima
AKERS], holotype (USNM P4754) reillustrated.
8a, Spiral view. 8b, Side view. 8c, Umbilical view. x 145.

SA ITO and MAIY A:

Planlctonic Fot'aminifera of Nishilcu?'osawa

Plate 18

620.

Planktonic Foraminifera of Nishikurosawa

The laboratory work was supported
by National Science Foundation Grants
GA 35463X and GA 29460. This is
Lamont-Doherty Geological Observatoryof Columbia University Contribution No.
2003.
References
AKERS, W.H. (1955):. Some planktonic foraminifera of the American Gulf Coastand suggested correlations with the Caribbean Tertiary. Jour. Paleont., vol. 29,
no. 4, pp. 647-664, pI. 65, text-figs. 1-3.
ASANO, K. (1962): Faunal change of planktonic foraminifera through the Neogeneof Japan. Koninkl. Nederl. Akad. Wetensch., Proc., ser. B, vol. 65, no. 1, pp. 114129, 1 text-fig., tables 1-2.
- - , INGLE, J.C., Jr. and TAKAYANAGI, Y.
(1968):
Clobigerina quinqueloba NATLAND, origin and distribution in lateCenozoic of the North Pacific. Ciorn.
Ceo!., ser. 2, vol. 35 (1967), no. 3 (Comm.
Mediterranean Neogene Stratigr., 4thSess., Proc., pt. 3), pp. 217-246, text-figs.
1-15, table 1.
BANDY, O.L. and INGLE, J.C., Jr. (1970):
Neogene planktonic events and radiometric scale, California. Ceol. Soc. Amer.,
SPec. Paper 124, pp. 131-172, pI. 1, textfigs. 1-7.
BERGGREN, W.A. (1972): A Cenozoic timescale-some implications for regional
geology and paleobiogeography. Lethaia,
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BLOW, W.H. (1959): Age, correlation andbiostratigraphy of the upper Tocuyo (San
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planktonic foraminiferal biostratigraphy.
In: BRONNIMANN, P., and RENZ, H.H.,
Eds., Internat. Conf. Pianktonic Microfossils, 1 st, Ceneva (1967), Proc., vol. 1,
pp. 199-422, pis. 1-54, text-figs. 1-43.
and BANNER, F.T. (1962): The mid-123

Tertiary (Upper Eocene to Aquitanian)Globigerinaceae. In: EAMES, F.E., BANNER, F.T., BLOW, W.H., and CLARKE,
W.J., Fundamentals of mid-Tertiary stratigraphical correlation. London: Cambridge
Univ. Press, pt. 2, pp. 61-151, pis. 8-17,
text-figs. 6-20.
and (1966): The morphology, taxonomy and biostratigraphy of Cloborotalia
barisanensis LERoY, Cloborotalia fohsi
CUSHMAN and ELLISOR and related taxa.
Micropaleontology, vol. 12, no. 3, pp. 286302, pis. 1-2, text-figs. 1-4.
BOLLI, H.M. (1957): Planktonic foraminiferafrom the Oligocene-Miocene Cipero and
Lengua Formations of Trinidad, B.W.I.
U.S. Nat. Mus., Bull., no. 215, pp. 97-123,
pis. 22-29, text-figs. 17-21.
CHANG, L.S. (1959) : A biostratigraphic studyof the Miocene in western Taiwan basedon smaller foraminifera (Part 1: Planktonics). Ceol. Soc. China, Proc., no. 2,
pp. 47-72, pis. 1-5, text-figs. 1-5.
CIIITANI, Y. (1925): Geology and physiography of the Oga Peninsula. Jour. Ceogr.,
vol. 37, no. 436, pp. 323-330 (in Japanese).
EGGEI~, J,G. (1893): Foraminiferen aus Meeresgrundproben, gelothet von 1874 bis
1876 von S. M. Sch. Gazelle. K. Bayer.
Akad. Wiss., Malh.-Physik. Cl., Abh., Bd.
18 (1895), Abth. 2, pp. 193-458, pis. 1-21.
HANZAWA, S. (1935): Some fossil apercuiina
and Miogypsina from Japan and theirstratigraphic significance. Tohoku Imp.
Univ. Sci. Rept., 2nd ser. (Ceoi.), vol. 18,
no. 1, pp. 1-29, pis. 1-3.
- - (1950) : Paleogeography of North Japan.
Short Papers, Inst. Ceoi. Paieont., Tohoku
Univ., no. 2, pp. 74-98, 2 te~,t-figs.
- - (1964): The phylomorphogeneses of the
Tertiary foraminiferal families, Lepidocyc1inidae and Miogypsinidae. Tohoku
Univ. Sci. Rept., 2nd ser. (Ceol.), vol. 35,
no. 3, pp. 295-313, 5 text-figs.
HATAI, K. (1938): A review of the paleontology of Akita Prefecture (Ugo Province), Northeast Honshu, Japan. Jap.
Jour. Ceoi. Ceogr., vol. 15, nos. 1·-2, pp.
35-45.
HUANG, T.Y. (1963) : Planktonic foraminifera

124

Tsunemasa SAITO and Sei}uro MAIY A

from the Peikang PK-3 well in the Peikang shelf area, Yunlin, Taiwan. Petrol.
Ceol. Taiwan, no. 2, H.H. LING JubileeVol., pp. 153-181, pis. 1-6, text-figs. 1-4.
(1967) : Late Tertiary planktonic foraminifera from southern Taiwan. Tohoku
Univ. Sci. Rept., 2nd ser. (Ceol.), vol. 38,
no. 2, pp. 165-192, pis. 15-16, text-figs. 16, tables 1-8.
--. (1969): Some planktonic foraminiferafrom a bore at Shihshan, near Taitung,Taiwan. Ceo!. Soc. China, Proc., no. 12,
pp. 103-119, pis. 1-4, text-figs. 1-2, tables
1-2.
HUZIOKA, K. (1956): Study of Green Tuff(Ryokushoku Gyokaigan). Kagaku (Science), vol. 26, no. 9, pp. 440-446, text-figs.
1-4 (in Japanese).
- - (1959): Explanatory text of the geological map of Japan; Toga and Funakawa(Akita-I, 2). Kawasaki: Ceo!. Surv. Japan,
pp. 6-61 (in Japanese with English abstract).
IKEI3E, Y. (1962): Tectonic developments ofoil-bearing Tertiary and migrations of oilin Akita oil fields, Japan. Akita Univ.,
Res. Inst. Undergr. Resour. Rept., no. 26,
pp. 1-59 (in Japanese).
JENKINS, D.G. (1960): Planktonic foraminifera from the Lakes Enterance oil shaft,
Victoria, Australia. Micropaleontology,
vol. 6, no. 4, pp. 345-371, pis. 1-5, textfigs. 1-10.
- - (1965a): Planktonic foraminifera andTertiary intercontinental correlations.
Ibid., vol. 11, no. 3, pp.265-277, pis. 1-2.

- - (1965b): The origin of the species Clobigerinoides trilobus (REUSS) in New Zealand. Cushman Found. Foram. Res., Contr.,
vol. 16, pt. 3, pp. 116-120, pI. 17, text-figs.
1-3.
- - (1971): New Zealand Cenozoic planktonic foraminifera. New Zealand Ceol.
Surv., Pa/eont. Bull., no. 42, pp. 1-278, pis.
1-23, text-figs. 1-2, tables 1-58.
- - and ORR, W.N. (1972): Planktonic foraminiferal biostratigraphy of the eastern Equator.ial Pacific-DSDP Leg. 9. In:
HAYs, J.D. et al., Initial Reports of the
Deep Sea Drilling Project, Volume IX.
Washington, D.C.: U.S. Govt. Printing
Office, pp. 1059-1193, pis. 1-4, text-figs.

1-9.
KOTAKA, T. (1957): Preliminary note on the
distribution of the Miocene' molluscan
fauna in the Green tuff region of northern Honshu, Japan. Saito Ho-on Kai Mus.,
Res. Bull., no. 26, pp. 41-42.
MATSUMARU, K. (1971) : Studies on the genus
Nephrolepidina in Japan. Sci. Rept. Tohoku
Univ., 2nd ser. (Ceol.), vol. 42, pp. 97185, pis. 9-26, text-figs. 1-42.
MINATO, M., GORAl, M. and HUNAIJASI-II,
M., Eds. (1965): The geologic development of the Japanese Islands. Tokyo:
Tsukiji Shokan, pp. 1-442, 30 pis., 137
text-figs., 44 tables.
NOMURA, S. and HATAI, K. (1938): On somefossils from Akita Prefecture, Northeast
Honshu, Japan. Jap. Jour. Ceol. Ceogr.,
vol. 16, nos. 1-2, pp. 39-64.
OLSSON, RK. (1972): Growth changes in the

Explanation of Plate 19
Fig. la-c. Clobigerinita glutinata (EGGER).
la, Spiral view of hypotype with umbilical bulla removed (NSMT 674). Ib, Side view.
lc, Umbilical view. x 145.
Figs. 2a-c, 3a-c. Cloboquadrina obesa AKERS.
2a, Spiral view of hypotype with aberrant last chamber removed (NSMT 675). 2b, Side
view. 2c, Umbilical view. x 102. 3a, Spiral view of hypotype (NSMT 676). 3b, Side
view. 3c, Umbilical view showing a characteristic umbilical tooth. x 102.
Figs. 4a-6b. Clobigerinoides japonicus SAITO and MAIYA, new species.
4a, Spiral view of small paratype (NSMT 677). 4b, Umbilical view. 5a, Side view ofholotype (NSMT 678). 5b, Umbilical view. 6a, Spiral view of paratype (NSMT 679).
6b, Side view. x 128.

SAITO and !lIAIY A :Planktonic Fora?ninifera of Nishiku?"osawa

Plate 19

620.

Planktonic Foraminifera of Nishiku1'osawa

Cloborotalia fohsi lineage. Eclogae geol.
Helv., vol. 65, no. 1, pp. 165-184, text-figs.
1-12.
PARKER, F.L. (1962): Planktonic foraminiferal species in Pacific sediments. Micropaleontology, vol. 8, no. 2, pp. 219-254, pIs.
1-10.
(1964): Foraminifera from the Experimental Mohole drilling near Guadalupe
Island, Mexico. Jour. Paleont., vol. 38,
no. 4, pp. 617-636, pIs. 97-102, tables 1-3.
SAITO, T. (1963) : Miocene planktonic foraminifera from Honshu, Japan. Tohoku Univ.
Sci_ Rept., 2nd ser. (Ceol.), vol. 35, no.
2, pp. 123-209, pIs. 53-56, text-figs. 1-15,
tables 1-6.
SHINBO, K. and MAIYA, S. (1971): Neogene
Tertiary planktonic foraminiferal zonation in the oil-producing provinces ofJapan. In: Stratigraphic correlation between sedimentary basins of the ECAFE
region (Second volume). United Nations,
Mineral Resources Development Series,
no. 36 (1970), pt. B, pp. 135-142, text-figs.
B12, 1-2, tables B12, 1-2.
STAINFORTH, R.M. (1948): Applied micropaleontology in coastal Ecuador. Jour.
Paleont., vol. 22, no. 2, pp. 113-151, pis.
24-26.

125

SUBBOTINA, N.N., PISHVANOVA, L.S. and
IVANOV A, L.V. (1960): Stratigraphy of
the Oligocene and Miocene deposits of
the Fore-Carpathians on the basis of foraminifera. Leningrad,' V ses. Neft. Nauchno-Issled. Ceol.-Razved. Inst.(VNICRI),
Microfauna of the U.S.S.R., Trudy, N.S.,
vupusk 153, sbornik 11, pp. 5-127, pis. 114 (in Russian].
TAKAYANAGI, Y. and SAITO, T. (1962): Planktonic foraminifera from the Nobori Formation, Shikoku, Japan. Tohoku Univ.
Sci. Rep!., 2nd ser. (Ceol.) , Spec. Vol.,
no. 5, pp. 67-106, pIs. 24-28, text-figs. 1-2,
table 1.
U]llE, H. (1966): "Evolutionary line" of
Miocene miogypsinid populations: Restudy of the Japanese miogypsinids Part
2. Nat. Sci. Mus. Tokyo, Bull., vol. 9, no.
3, pp. 413-430, pis. 1-6.
Y ABE, H. (1927): Marine Tertiary of the
Kwanto Mountainland and of the Echigo
and Akita oil-fields. Jap. Jour. Ceol.
Ceogr., vol. 5, no. 3, pp. 95-105, text-figs.
1, 2.
- - (1933): Geological age of the Miogypsina and Operculina bed of Nishikurosawa.
Ibid., vol. 11, nos. 1-2, pp. 25-26.

Trans. Proc. Palaeont. Soc. Japan, N. S., No. 79, pp. 126-136, pis. 20, September 20, 1973

621.

MARINE DIATOM FLORA OF THE PLIOCENE TATSUNOKUCHI
FORMATION IN MIYAGI PREFECTURE':
IT ARU KOIZUMIInstitute of Geological Sciences, College of General Education, Osaka University'n'17£m, fH;:WiMt .1i!J [:"lfo,YirllO)i1iH;I,U¥.~H(q71)l\F:

fUlt~J;millil'G~I:J".i'iJ~H:.iB"','i'fW:J1J

Jim UI:J::JJJ!I!!.C O)/llJ O)fIUl!rlll' fC.J:& <5~;(fi-J- ~i¥£J r:1~* 0) 1t:fiIE~n~0) M~fJf c ;CO) *5* c~~~~o m.~~IE~gO)~.~~~~OO • • ~~~~Q~-~·"~P~fi~ft~~~,MM~mW~0).,,'6~O)n~g~L~~0 MMO)~~~~.~G~~, =hGO)n~

1i!J r:lJ\l\IO)rffll. II~ff~i;~V'J::~~~;Ch.:fhtt£{~~obO)L';Y.>~o =hcv"i5.lIHc., ~.f:ffi0)±~Jl':J*<f~ c4}r,lt*JfL'O)J::~ 51li:j; L'O)ii1*ftl!fC. ob c -::i <l\f~O)M-¥fJfil> G, rl'f~ i; J:: V' .l-.~iI~H:~~~l\ffC.~~~ff~l\HIH"i, r/:IJ~~o)obO)J:: ~ obi':£Hti1iJ!!llGL'wnX;~ht..:n~L';Y.>~=cil~5J'~o *5JiijO)c=::S,
r:lfl'iI=j~O)IE.llf~v"i±fc.m~~1?9 (7j(i~tJ:c) O)~mr.~ftlc.
J:: ~~~Jl.'j-E~~l,~obO)-C·;Y.>::S?o
Jj, >fi.
tf't

mJIntroduction
In a previous paper (KorZUMI, 1972)
Pliocene marine diatoms from the Tatsunokuchi Formation in Fukushima Prefecture was described and analysed. The
present paper is to report the results ofthe study extended further north to deal
with the diatoms assemblages from thesame formation developed in Miyagi
Prefecture including that exposed in the
Tatsunokuchi Gorge in Sendai, the type
locality of the Tatsunokuchi Formation.
In the lowland terrain located between
the Kitakami massif and the Ou rangeof Miyagi Prefecture, the Pliocene Sendai Group (IWAI, 1949) is extensively
distributed. The group, about 200m in
total thickness, is predominated by nonmarine deposits of sand, mud, gravel

and lignite seams accummulated during
the upward movement of the Ou Range
started in the Miocene and continued
through the Pliocene time. The Tatsunokuchi Formation, composed mainly ofg"rey siltstone and about 50 m in thickness, represents the lower part of thegroup and is known to be the only unit
exclusively of marine origin among the
Sendai Group.

Stratigraphic note
Table 1 shows the stratigraphic relationship and terminologies of the rockunits of the Sendai Group developedin Miyagi Prefecture. The time-stratigraphic correlation of the Kameoka andTatsunokuchi formations as defined at
type area with those correlatives in suchareas of the northern part of Miyagi
Prefecture as Sanbongi, Wakuya andWakayanagi have been sufficiently borne* Received March 20, 1973; read January
16, 1973, at Sendai.

126

621.
Ta~le 1.

Q.

~I~

Stratigraphic sequence and correlation of the formations of the Sendai Groupin the areas of Sendai, Sanbongi, Wakuya and Wakayanagi.
sENDAIshi bata.1962

Dainenj i
11JD.

z::l
11J~

u~

127

Diatom of the Tatsunokuchi FormationsANBONGI
Shibata. 1962

Formation( 30 )

OJojigahara Formation

Yagiyama Formation( 50 )WAKUYA
Takahashi & Matsuno.1969

WAKAYANAGI
Matsuno.1967

Takashimizu Format ion

Takashimizu Formation( 30)( 20 )

Hi rosegawa Tuff

Ojikakura Tuff

( 10 )( 35)

Tsukidate Formation
Onuki Formation( 0 - 50 )( 50-80)

Kazawa Formation
sanbongi Formation(16)( 5 - 55 )Formation)
a.C
Omori Formation (30) Tatsunokuchi Formation Tatsunokuchi Flrmation
Go Tatsunokuchi Formation
III(= Tatsunokuchi Formation)( 40)( 50 - 60 )( 0 - 85
Kameoka Format i on
Kameoka Formation
Okuda Formation (30) Kameoka Formation( 10 - 20 )(=Kameoka formation)(40 )( 0 - 65 )

o·~

-III

-'"t!

Kitayama Format ion_( 1-10 l(=Kit~amaout by previous studies made independently of diatoms in various disciplinesof stratigraphy (e. g. HANZA W A et al.,1953; HANZA w A et at., 1962; KITAMURA
and SHIBATA, 1963; MATSUNO, 1967;
ISHIDA et al., 1969; TAKAHASHI and MA·
TSUNO, 1969); at those localities given
in Fig. 1 the Tatsunokuchi Formationis conformable or partially interfingers
with under lied Kameoka Formation andis covered unconformably with the Kita·
yam a Formation and the correlative formations.
Kameoka Formation: The main part of
the formation consists of conglomerate,
sandstone, siltstone and mudstone intercalating tuff and lignite seams. Suchplant fossils as Glyptostrobus europaeus,
Sequoia sempervirens, Fagus crenata,
Quercus crispula and Cinnamomum scheuchzeri (OKUTSU, 1955) found from theformation indicate its age to be early
Pliocene (SHIBATA, 1962). There is no
paleontological evidence indicating positively the formation is marine origin;from the lithology and by the occurrenceof plant fossils, it seems reasonable tojudge that this unit is lagoonal and partly terrestrial in origin.
Tatsunokuchi Formation: The formation consists mainly of tuffaceous bluishgray or bluish green siltstone or mud-stone intercalated with sandstone andtuff layers. The silt and mudstones containing diatoms are massive and show
no stratification. The geologic structureof the formation is rather simple; it lies
almost horizontally throughout the distributed area. Within the Sendai Groupthe formation is characteristic by theyield of many kinds of fossil marine
animals. Especially well known is its
molluscan fauna, that by containing suchspecies as Anadara tatunokutiensis, Dosinia tatunokutiensis, Fortipecten takahasii
together with many other thick-shelledshallow water forms, represent "theTatsunokuchi Fauna" of Pliocene (NoMURA, 1938). Mainly by the molluscan
fauna, it belongs to the lower part of
the Miyagian by HAT AI (1962) and HAT AI
and MASUDA (1966); its age being early
Pliocene according to NODA (1966).
Kitayama Formation and its correlatives: The formation and its correlatives consist mainly of basal conglomerate and sandstone intercalating partly
siltstone and lignite beds as well as carbonaceous siltstone. The formation in
the Sendai area is known to containsuch plant fossils as Alnus, Fagus andSequoia. From its lignites pollen assemblages dominated by those of Alnus,
Sequoia-type and Sciadopitys have beenl28

Itaru KOIZUMI

N

f
.K.

Legend~T.

r.:;:':"':l
Ka
~

.

~M.s.
x 5

Loc.

(Jitr M.

o1

....

Scale
5km
0

oI::I-=~

lkm

IF" ~

Text-fig. 1. Partial geologic map showing the locations of the samples studied. Legend;
K. Kitayama Formation and the correlative formations; T. Tatsunokuchi Formation; Ka
Kameoka Formation; M. s. Miocene strata; Loc. Locality of the samples; M. magnificationof the circular parts.

621.

Diatom of the Tatsunokuchi Formation

129

WAKUVA
A•

17

SANBONGI

LlI!'gendo·

EJb..... 16~•I)!ll C Scal.

WAKAVANAGI,------A----,
G

R118
k15~
b'S'tHa.

~Ka.

F

i1;"dK~21..

~'9 GJ2~ >\.:

t">"1Ka.

~d1m.
Ililll3m

20·

Text·fig. 2. Columnar sections showing the stratigraphic position of the samples
studied. Legend: a, siltstone; b, sandstone; c, sand-pipe; d, tuffaceous sandstone; e,molluscan fossils; f, conglomerate; g, position of samples studied. Abbreviation: K.,
Kitayama Formation and the correlative formations; Ka., Kameoka Formation.

reported (HANZAWA et al., 1953). The
formation may be terrestrial, possibly
brackish water in part, in origin.
The geographic and stratigraphic
positions of the samples examined areshown in the geologic map (Text-fig. 1)
and the columnar sections (Text-fig. 2),
respecti vely.

Diatom flora in the Tatsunokuchi
Formation

The method of study once de~cribedby KOIZUMI (1968) is followed in thepresent study.
Among the 21 samples from the Tatsunokuchi Formation. the distributionof the 80 diatom taxa distinguished isshown in Table 2. The ecology of eachtaxon is based upon the information
mainly from the literatures of HUSTEDT(1927 et seq., 1930). JOUSE (1962). SIMONSEN(1962) and HENDEY (1964).
As shown by Table 2. the diatom assemblage in the present study is common in having, in considerable number,the neritic, tychopelagic and benthonicspe'cies. The feature has been pointed
out as one of the characteristics of the

Pliocene marine diatom assemblages
found from the land based sequencesof the circum-Pacific regions (e. g. LOHMAN, 1937; JOUSE, 1962; MERTZ, 1966;
SHESHUKOVA-PORENTZKAYA, 1967; KOIZUMI, 1968). The composition of diatom
assemblage in the formation reflects
largely the environmental changes
throughout the depositional time, withchronological changes playing a minor
role. The general tendency read froma glance of the distribution table (Table
2) is that marine tychopelagic and benthonic diatoms are dominant in thesouthern half of the area, while planktonic diatoms in the northern half. However. the relative stratigraphic positions
within the Tatsunokuchi Formation of
the diatom-bearing samples vary withlocal sections (Text-fig. 2). Accordingly
the relative stratigraphic levels of each
set of samples have to be taken into theconsideration for the analysis of theassemblage as a whole. Text-fig. 3 is toshow the proportions in each sample of
the association of fresh-water, brackishwater, marine benthonic, marine tychopelagic and marine planktonic diatoms,
that varies geographically and stratigraphically.

130

Itaru KOIZUMITable 2.

Distribution of the diatoms from the Tatsunokuchi Formationin Miyagi Prefecture.
Abbreviation: B. s., Brackish-water species; b., benthonic form.

III

.
.
-;;;

a.
III

~

~

.
Jl:

.<:.

III

ui

a:i

III

~

.e 27. C.

."upseudomarginafd

scutellum
28. C.
0.<:. 29. Cosc;nodiscus laeustr;s.

C

31. Dip/oneis smithii

35. M.

5

7

6

8

9

10

11

1

lJ

14

5 16

1
1

1

7 118 19 12C 2

1
1
1

3

1
1

2
2

1

1

3
1
1

1

1
1

1

4

3

2

1

1

1

1

3

2
1

1

1
1
2
4
1

2
1

3

65
6

4

2
4B 15 26 33
11 21 24 16

3

1

b
b
b
b

1
1
1
1

b
b

3
2

sulcata

3
3
4

62 3B
3 18

ott

.gu 36. Navicula distans

11

30. Cydohlla slriata.a 32. Grammatophoril angulosa." 3 3. Hyalodiscus scoticus
c 34. Melosira albicans

4

2

1
2

undulatu5 Y.

24. Biddulphia aurila
25. Coccone;s californica
26. C.
costata

3

1

21. Actinopfychus splendens
undulafus

22. A.
23. A.

2

1

2. Cocconr;s dim;nuta
3. C.
disculus
4. C.
placMtula
5. eye/oletla chaefoceros
kiirtzingiana
6. c.
7. C.
ocellatus
8. c.
stf'lIigera
9. Epithemia zt'bra
10. Fragilaria harrisson,,'tappan;ca
11. F.
1 2. Gomphon ('ma augur
13. Melosira granulata
14. M.
varianst 5. Pinnularia alpina
16. Mastogloria sp.1
1 7. Na~;cula hunga,;ca
lanceolala
lB. N.
19. Acfinocyclus ehrenberg;
20. A.
ehrpnbergi v.

.~
u

B

A

SamplesSpecies
1. Achnanthes lanceo/ata

1

2
1

4

1
1
4
1
5

2
1

b

2
1

5
1

4
1

~

.~~

.

..

22 16 32 18
8 13
2 10 21 14 10
9
1
2
1
1
1
2
1
2
3
1
1
3
1
1
1

6
1
1

5

6
6

3
2

spp. (4 forms)
79. T.
80. Thalass;ofhnX 10nfJissima
Diatom number (xl0 6 /1a.)

42
3

17
4

4

3
1

10 27 14
10 11
9

14
4

1
2
2
4
19 28
4
2

1

1

1

1

1
1

1

1

2

11

1

2
1

1

3

3

3

12
1
1

1
22 14 36 31
5
9 12
19 30
6 13
22
7
1
1
1

6
6
7 10
7 16
1

3

1

3

1
5

24
3

1
1

1

1

1

4
1

5
1

2

1

1

1

2
1

2

5
2

3
6
1

31
2
4
1

4

5
2

5
1

45

1
4

1
1

1
1
1

2

1

3

3

1
2

1

~

-

1 13

1

-

~

2
1

32
9

ott

37. Nitzschia granulatab2
38. Plagiogramma 'esse/ata
39. Pleusigma affineb111'<:'
40. Podosira matimab
41. Rhaphoneis angustatab 16 14margarialimba,a b 25 21
42. R.
usurirellab 19 14
43. R.
tatsunokuchiensis b
44. R.
2
2
Co
45.
SurirellafastuosabIII
46. Trachyneis asoerab1
4
47. Ac'inocyc/us curva'ulus
divisus1
48. A.
c
49. As'eromphalus hyalina
SO. Bacteriastrium spp. (2 forms)
2
51. Chaetoceros cinctus
ottcoronata
52. C.
(urceHatus
53. C.
~
lorenzianu.s
54. C.
subsecundus
55. C.
1
56. Coscinodiscus etcenfricus
4
marginatus
57. C.
2
oculus iridis
1
III 58. C.
radia,usE 59. C.
2stellaris v.
0 60. C.
61. C.
'emper,"2
3
62.
Denticulakamtschaticauseminae1
c 63. D.
01
64. Hemldiscus weissflogi:;c 65. Nitzschia f.>ttincta
1
1
c 66. N.
reinholdii
ottsiculaIi 67. N.
68. Rhizosolenia spp. (5 forms)
2
69. Stephanopy1tis furris
4
70. Tha,assionema nifzschtoides
18 10
nitzschioides Y.
4
71. T.
12 18
72. Thalassiosira antiqua
46dec;p;ens
73. T.
kryophila
74: T.
5
3
75. T.
linea'a11nidulus76. T.
5
1
77. T.
n6rdenski61dii
2zabelinae
78. T.

2
2

1

1
3

1

1
2

1
1

4

3
2

1

1
1

3
1
2

4
1

2
2

2
1
1

1

5

1

1

2
1
2

4

1
4
2
3

1

3
3
1

2
2

2
2

1
2
1
1

2

2
1

5

2

1
20

5
6
2
1
4
6
10 11

25
3

4

1

1
1
1
2
1
1
17 15 11
1
1
1

1

3

5

17

15 24 27 23
2
2
3
5
1
3
2

3
1
2
5
4
2
2
2
3
3
5 32 33 38 37 33 26 33
10 30
43 13 1261 12
4
16 13 14 16 14 19 47 36 54 65
1 4
5
4
4
1
1 11
2
4
3
1

1
1

6

2
1

5

1
18
1
1

3

6

4
1

2
1
3
1
5
9
1
1
1
2
1.3 0.6 0.4 0.7 32.0 2.6 2.4 3.5 B.O 16.0

8

1

1

2

5

1

1
4
13

4
15

1

2

19
3
1

14

5

1
5.3 3.5

3

2

2

2
1
2
1
1
12 24 40
6
1

3

1
18

2
1
4
1
23 21 239710964 53 54 55
5
2
3
5
1
3
5 13
4

4

5

1

1

5
1
2
3
9.2 5.4 B.O

11
2
5

2
10 15
7 39 .
2
1
3
2
3
2
1
39 39 34 43 28
4 14
7
5
8
24 24 42 46
7
3
8
2
3
2
3
2
4
8
9
9
1
2
4
4
4

40

4

1

4
3
2
2
5
3
16.0 6.4 4.6

621.

Diatom of the Tatsunokuchi Formation

gu. "., ,Legend131

cussed by UJIIt and KUSUKAWA (1969).
In the present study the correlation
coefficient as one of the quantitative
coefficient is used.

m~m'I'~b.
Niddl. parif.

b.

Correlation CoefficientO'"~ Low.rpa,1

5'1.
10".

35'10

Text-fig. 3.
Figure showing geographically and stratigraphically the proportions in an association of f., freshwater species; b., brackish-water species;
m. b., marine benthonic species; m. t.,
marine tychopelagic species and m. p.,
marine planktonic species in number of
specimens.

Cluster analysis and explanation
The Q-mode (sample by sample comparison) cluster analysis is applied inorder to group the aggregate of thesamples that have similar associationsof species among different localities andhorizons. In similarity coefficient there
are two kinds of qualitative and quantitative coefficients, and the comparison
between two coefficients was once dis-

where: Xi is the relative frequency ofa certain taxon in one sample X, and Yi
that of the equivalent taxon in anothersample Y, to be compared with eachother; i and yare means by Xi and Yi,
respectively; n is the total number oftaxa found in all samples under comparison (n = 80).
The result is shown in the dendrogramof Text-fig. 4-B. Seven clusters from I
to VII could be distinguished, if any
level within the interval between 0.70
and 0.75 was chosen based upon a breakin the frequency of the fusing and flatin the cumulative distributions of thefrequency as indicated in Text-fig. 4-A.
As recognized in Text-fig. 3, the sevenclusters at the 0.70 to 0.75 level are
more ciosely related to stratigraphic
horizons than to geographic distributions of samples.
Cluster I is represented only by theupper part of the formation. Clusters
II, III, IV and VII are restricted to thelower part. Cluster VI which consistsof single sample joins the large Cluster
V at a little lower level than the chosenlevel. And these clusters are represented by the middle part of the formation.
This division of the clusters is quite
reasonable also from the viewpoint of
the ecologic analyses of diatom assemblage as summarized in Text-figs. 4-C
and -D. From the comparisons of theoccurrences of fresh-water, brackish-

132

Ita1'u KO IZ UM I
UIIlllIII frt'sh-walt'f5pC'cit's

IiBj] brackish -wat., spt'tiu~ mar inll!' bf'nl honic speci,,!:§m. t ychopt'lagic s pl~ci l's~ m . P l anklon l cspt'cis

CLUSTErS~.~bLE

I

II

III

IV

0.90

CORRE LATION COEF Fi Ci ENT
0.80
0.10
0.60
0.50
0.40

0.30

":8

':~
8

E

1
.: 1

"

4

-

DIS

~
G2 . - - . - J

C. 2

.3

1
1

".4 I
V

-

9
G20
C'O

I

017

.6

VI
VII

Fl9
B 5

B

c

D

T ext-fig . 4. F ig u r es s ho w ing the samp le clus ters and eco logic census of diatom assemblag es related w ith them . A: Distribution of frequency a nd cummu la t ive f requ enc yof fus ing in the dendro g ram (B) . B: Dend rog ram of sa mple si milar ities based upon
the Corr ela t ion Coefficien t computed f rom the rela ti ve frequenc ies of diatom species . C:
Rank s of dominance of diatom species . D : Propor t ions of an assoc iat ion in te rm s of thesa lini t y of water a nd t he mode of livin g of t he cons titu ting spec ies in number of species.
E : N umber of to ta l species.

water and marine species in th e assemblages, fresh-water species are consid ered to be a llochtonou s s pecies thatwere transported by rivers and then bynormal wave currents into the marin e
sedimentary basin. OSHITE (1959) showsthat fresh-water diatoms occur, to agreat extent in com parison with th epr esent fi g ures, abnormal marine fine g rained clastic sediments. The propor tions of brackish-water species are ver yweak; namel y, the diatom assemblag e
is mostl y composed of marine s pecies.
Each cluster is eoologicall y explai ned by
the ratio in number of species and speci-

mens . among benthonic, tychopelagicand planktonic species. The ratio isr elated to the depth of the sedimentarybasin in general, and the ratio increases
wi th the decreasing depth of th e normal
marine sed imentary basi n (jOUSE, 1962).
Summary and discussion

As the r esu lt of the Q-mode cluster
ana lysis usin g the correlat ion coefficient,th ree aggregates of samples were disting uish ed. They r epresen t the lower,
midd le and upper parts of the Tatsunokuchi Fo rm atio n, respectively, among

621.

Diatom of the rpatsunoicuchi Formationdifferent localities and horizons. The
diatom assemblage was ecologically analyzed based upon the rank of dominanceof species and the proportions in theassociation of fresh-water, marine benthonic-tychopelagic and marine plank·
tonic species in number of species andof specimens. The result of this analysis explains well these three aggregates of the samples in the viewpointof geological history of the formation.
By the nature of diatoms being autotrophic algae, marine benthonic species
can not vegetate on the sea bottom beyond the reach of sufficient light. Thisdepends on the transparency of sea
water in the basin, but in turbid coastal
water 50 m in water depth would be areasonable guess for the maximum
depth. From the predominant occurrences of benthonic species, constantoccurrences of fresh-water species, andfurther by the presence of lignite seams
and sand-pipes immediately below thesampling horizon for the lower part,and by the presence of unconformity
with basal conglomerate immediately
above the sampling horizon for the upper part, the diatom assemblages of thelower and upper part of the formation
can be concluded to have been accummulated in shallower sea water of thedepth less than 50 m.
The foraminiferal assemblages fromthe formation in the western border of
Sendai consist mainly of the eulittoraland littoral species (T AKAY ANAGI, 1950).
CHINZEI and IWASAKI (1967), in discussing the paleoecology of Neogene
shallow sea molluscan faunae of Northeast Japan, distinguished two types ofthe molluscan assemblages, the shallow
sea or near-shore type and the off-shore
type, and explained the two types in
the Tatsunokuchi Formation as of geographical control. From the present

133

study, stratigraphic control of the assemblage has been revealed.
Acknowledgements: The writer isgreatly indebted to Dr. Taro KANAYA,
Nikko for his critical reading of themanuscript. Hearty thanks are also
due to Dr. Kojiro NAKASEKO, Osaka
University for his help and encouragement, Miss Taeko ZENRI for typing themanuscript and Mrs. Mineko KOIZUMI
for scrutinizing the manuscript.
References
CHINZEI, K. and IWASAKI, Y. (1967): Paleoecology of shallow sea molluscan faunaein the Neogene deposits of Northeast
Honshu, Japan. Trans. Proc. Palaeont.
Soc. Japan, N.S., no. 67, pp. 93-113.
HANZAWA, S., HATAI, K., IWAI, J., KITAMURA, N. and SHIBATA, T. (1953): Thegeology of Sendai and its environs. Sci.
Rep. Tohoku Univ., 2nd ser. (Ceol.), vol.
25, pp. 1-50.
- , ONUKI, Y. and KITAMURA, N. (1962):
The geological map of Miyagi Prefecture,scale 1: 200,000. Miyagi Prefecture.
HATAI, K. (1962): Mizuho-T6. Sci. Rep.
Tohoku Univ., 2nd ser. (Ceol.), spec. vol.,no. 5, pp. 329-348.
and MASUDA, K. (1966): The stratigraphic position of Trilophodon sendaicus
MATSUMOTO in the Mizuho-T6 of Sendai
City, Miyagi Prefecture. Saito Ho-on
J(ai Mus., Res. Bull., no. 35, pp. 1-10.
HEN DEY, N. I. (1964): An introductory account of the smaller algae of British
coastal waters. Fishery Investigations.
ser. 4, part 5, Bacillariophycease (Diatoms), pp. 1-317. London.
HUS'rEDT, F. (1927 et seq.): Die Kieselalgen
Deutschlands,
Oesterreichs und derSchweiz mit Berucksichtigung der tiber
Landen Europas sowie der anderenzen
den Meeresgebiet: In Dr. RABENHORST'S
Kryptogamen-Flora von Deutschland,
Oesterreichs und der Schweiz. vol. 7,
Teil I, pp. 1-920; Teil II, pp. 1-736; Teil
III, pp. 1-411, not yet completed. Leipzig.

134

Itaru KOIZUMIExplanation of Plate 20
15 taxa occupied the 1st to 5th ranks of dominance in each assemblage,as shown in Text-fig. 4-C, are illustrated.
(All figures, x 1000)

Figs. la, lb. Actinoptychus undulatus (BAIL.) RALFS var., slide no. 7254, G39-0S*, 17p indiameter, from A-4.
Figs. 2a,2b. Actinoptychus undulatus (BAIL.) RALFS var., slide no. 7210, L44-3E, 29 p indiameter, from D-15.
Figs. 3a, 3b. Actinoptychus undulatus (BAIL.) RALFS, slide no. 7214, H42-1SW, 38p in diameter,from D-17.
Fig. 4. Melosira sulcata (EIII~.) KUTZ., slide no. 7207, Q47-0N, 16/1 in diameter, from E-19.
Fig. 5. Melosira sulcata (EHR.) KUTZ., slide no. 7207, K43-2E, 19 p in diameter, from E-19.
Fig. 6. Thalassiosira decipiens (GRUN.) JOERG., slide no. 7238, T39-2NW, 15 p in diameter,from B-7.
Fig. 7. Thalassiosira llneata JousE, slide no. 7224, L47-0N, 21 p in diameter, from C-l1.
Fig. 8. Thalassiosira lineata JousE, slide no. 7224, E49-4NW, 50 p in diameter, from C-l1.
Figs. 9a,9b. Coscinodiscus temperi BRUN, slide no. 7210, U43-0N, 39 p in length of apical axis,
from D-17.
Fig. 10. Actinocyclus ehrenbergi RALFS, slide no. 7214, S48-0N, 34/1 in diameter, from D-I5.
Fig. 11. Actinocyclus ehrenbergi RALFS, slide no. 7252, R42-IE, 60 p in diameter, from B-5.
Fig. 12. Thalassiosira antiqua (GRUN.) A. CL., slide no., 7252, H42-0NE, 36 p in diameter,from B-5.
Fig. 13. Thalassiosira antiqua (GRUN.) A. CL., slide no., 6031, M44-0, 54p in diameter, from
D-17.
Fig. 14. Rhaphoneis tatsunokuchiensis KOIZUMI, slide no., 7216, S45-4W, 26 f1 in length of apicalaxis, from C-l1.
Fig. 15. Rhaphoneis tatsunokuchiensis KOIZUMI, slide no., 7224, N49-0E, 23 f1 in length of apicalaxis, from C-9.
Fig. 16. Nitzschia extincta Koz. and SHESIIUK., slide no., 7210, D44-4W, 23 {I in length of apicalaxis, from D-17.
Fig. 17. Nitzschia extincta Koz. and SHESHUK., slide no., 7210, M44-0NW, 31/1 iri length of
apical axis, from D-17.
Fig. 18. Rhaphoneis margaritalimbata MERTZ., slide no., 7254, M40-0W, 17/1 in length of apicalaxis, from A-4.
Fig. 19. Rhaphoneis surirella (EI-IR.) GRUN., slide no., 7254, 03I-4N, 19 f1 in length of apicalaxis, from A-4.
Fig. 20. Rhaphoneis surirella (EHR.) GRUN., slide no., 7252, W42-0N, 26 f1 in length of apicalaxis, from B-5.
Fig. 21. Rhaphoneis angustata PANT., slide no., 7210, Q44-3SE, 56 f1 in length of apical axis,
from D-17.
Fig. 22. Rhaphoneis angustata PANT., slide no. 7254, K29-0N, 38 f1 in length of apical axis,
from A-4.
Fig. 23. Thalassionema nitzschioides GRUN. var., slide no. 7249, N43-0S, 23 p in length of
apical axis, from B-8.
Fig. 24. Thalassionema nitzschioides GRUN., slide no., 7208, P39-0NW, 49 P. in length of apicalaxis, from E-18.
Fig. 25. Thalassionema nitzschioides GRUN., slide no., 7202, K29-0N, 56 P. in length of apicalaxis, from G-21.
* The position of a specimen in a strewn slide read by the England Finder.

KOIZUMI:

14

15

Plate 20

Diatorn of the Tats~mokuchi Fo?"?nation

16

17

18

19

20

21

22

24

25

621.

Diatom of the Tatsunokuchi Formation-(1930): Die Susswasser-Flora Mitteleuropas. In Bacillariophyta (Diatomeae) :Heft 10, pp. 1-466. Jena.
ISHIDA, T., OIKE, S., ONODERA, S., TAKEUTI,
S., NAKAGAWA, H., NANAsAKA, O. and
MATSUYAMA, T. (1969): Quaternarychanges in the sea level in the Tohoku
region, Japan. In Quaternary system
of Japan. Assoc. Ceol. Collab. Japan,
Monogr. no. 15, pp. 37-83. Tokyo.
IWAI, J. (1949): Stratigraphy of the Cenozoic formations of Sendai and the environs. Chikyu Kagaku (Earth Sciences),no. 1, pp. 1-5.
JousE, A. P. (1962): Stratigraphical andpaleogeographical studies in the northwestern part of the Pacific Ocean. Izd.
Akad. Nauk S. S. S. R. pp. 1-258. Moscow.
KITAMURA, N. and SHIBATA, T. (1963): The
guide-book prepared for the field trip in
the Senboku area. For the 70th annual
meeting of Geol. Soc. Japan., pp. 1-26.
KOIZUMI, I. (1968): Tertiary diatom flora of
Oga Peninsula, Akita Prefecture, Northeast Japan. Sci. Rep. Tohoku Univ., 2ndser. (Ceol.) , vol. 40, no. 3, pp. 171-240.
- - (1972): Marine diatom flora of the
Tatsunokuchi Formation in Fukushima
Prefecture. Trans. Proc. Palaeont. Soc.
Japan, N.S., no. 86, pp. 340-359.
LOHMAN, K. E. (1937): Pliocene diatoms
from the Kettleman Hills, California.
U. S. Ceol. Survey, Prof. Papers 189-C,
pp. 81-94.
MATSUNO, K. (1967): Geology of the Wakayanagi district. In Quadrangle ser., scale
1: 50,000, Akita (6) no. 69. Ceol. Survey,
Japan. pp. 1-24.
MERTZ, D. (1966): Mikropalaeontologische
und sedimentologische Untersuchung der
Pisco Formation Sudperus. Palaeontographica, Bd. 118, Abt. B, pp. 1-51.
NODA, H. (1966): The Cenozoic Arcidae of

Kameoka
Kitakami
Kitayama
MiyagiJapan. Sci. Rep. Tohoku Univ., 2nd ser.
(Ceol.), vol. 38, no. 1, pp. 1-161.
NOMURA, S. (1938): Molluscan fossils fromthe Tatsunokuchi shell bed exposed at
Goroku cliff in the western border of
Sendai. Ibid., vol. 19, pp. 235-275.
OKUTSU, H. (1955): On the stratigraphy andpaleobotany of the Cenozoic plant bedsof the Sendai area. Ibid., vol. 26, pp.
1-114.
OSHITE, K. (1959): Sedimentological studyof diatoms in marine deposits from theadjacent seas of Japan. Hokkaido Cakugei Univ., Jour., sect. B, vol. 10, no. 2,
pp. 417-495.
SHESHUKOVA-PORENTZKAY A, V. S. (1967):
Neogene marine diatoms of Saghaline
and Kamtchatka. Izd. Leningr. Univ.
pp. 1-327. Leningrad. (in Russian)
SHIBATA, T. (1962): Geology of the Sendai
and Nanakita-Sanbongi areas, Miyagi
Prefectcre. Sci. Rep. Tohoku Univ., 2ndser. (Ceol.), vol. 5, no. 3, pp. 239-301.
SIMONSEN, R. (1962): Untersuchungen zur
Systematik und Okologie der Bodendiatomeen der westlichen Ostsee. In
Internationale Revie der Gesamten
Hydrobiologie; WOLTERECK, R. (Ed.),
Beih. 1, pp. 1-44. Berlin.
T AKAHASI-II, H. and MATSUNO, K. (1969):
Geology of the Wakuya district. In
Quadrangle ser., scale 1: 50,000, scale
1 : 50,000, Akita (6) no. 78, Ceol. Survey,
Japan. pp. 1-26.
TAKAYANAGI, Y. (1950): Pliocene smaller
foraminifera from western Sendai. Short
Papers ICPS, no. 2, pp. 23-28.
UJIlE, H. and KUSUKAWA, T. (1969): Analysis of foraminiferal assemblages from
Miyako and Yamada Bays, northeasternJapan. Natl. Sci. Mus. Tokyo, Bull., vol.
12, no. 3, pp. 735-772.

1it!.

[lIi]

Ou

;11::
;11::

.J:

Sendai
Tatsunokuchi

'~;'"

III
Jill(

135

-m / n136

Itar't~ KOIZUMIERRATAKOIZUMI, 1.,

Marine Diatoms Flora of the Pliocene Tatsunokuchi Formation in Fukushima
Prefecture. Trans. Proc. Palaeont. Soc. Japan, N. S., No. 86, pp. 340-359, 1972.

The dendrogram in Text-fig. 3 of page 345 is corrected as foIlows: The group consistsof Ok. 3, Ok. 1-2 and T. 34 is 'fused together with the group consists of Tomioka 33 andOkuma 2~2, and two samples of Ok. 2-3 and T. 36 at the 0.61 level of the Jaccard Coefficient.

Trans. Proc. Palaeont. Soc. Japan, N. S., No. 91, pp. 137-150, pis. 21, 22, September 20, 1973

622.

HOLOCENE TO UPPERMOST PLEISTOCENE PLANKTONICFORAMINIFERS IN A PISTON CORE FROM OFF SAN'IN
DISTRICT, SEA OF JAPAN*
HIROSHI UmEDepartment of Paleontology, National Science Museum, Tokyo 160

andMASAKI ICHIKURA
Kamishirane Junior High School, Yokohama 241 .

LIJ~~tyJjlE ~:A r Y . ::t 71=j:1 O)'JetiT*it-M:J:i'.-II1f!i'iJi*1Er¥l2ii1:lflL!it:*0)~:A r Y' ::t70)?i?25*0)':H%f:1"J~iN~.t-o~t.J:v',

E1 t>:ihJ J:: IJ 1!Jtd'HO}jjHifi1jEkMm:i~J1£;&~~~1jn.:i:Jth:'c ~j;illJ,

J]*iw.~lfO)itFF?~~~lc~tr~*~lc1i1fIZ9T 0 ctff~%(N· 0 0 v' '? f;f?, Ijj'Ji~grJ::
IJ i~Hf.~J&rtT1<P7k~J:: iJ 1~t-=::t 7 (V28-265) v'1, 920 cm ICllil~~~fC;&'It'"C, IiiI' <"£ t.J:<r¥m11:lflL!11~lEI:BT00 ¥~T0 "Globigerina" pachyderma 0) coiling ratio 7J>t:J,::t 7Th'HlllJ:: IJ k:"J 120 cm 0) c;: 0Ic'JeliJi1!t . YiliJi!1t~W (r.~ 11,000 "l'·riij) ~i1.21>i), .;c-h~r.lllc
L- '"Ci5*iMO)J:1"1, li5IiMiHj:7J' t:Jl'ildt,(:I"J~{~:A..t.J: t: O)iif),1~0)~,~;&~£' 0 ~ c ~~I!2<:-f" 0 0<b?-"?0)~ii!~fil1'"C£'0

Globigerina umbilicata v'1,

IUfljfj::t7}l.!lrr*1Eo)lj.lcr.l~t:Jh,

III';;"H1i:If;!JI1!.:JjO)J:)~III!!HfrK.it.J:v' VYDiiJi*1E0)7i~l~flHt

c tJ: 0 7J' <b Ul,t.J:v,o t-=t.:. L-,

V28-265 1'1,

Riss-Wiirm l:ljjJ<WHclii1! L- "CV't,(v' t:J L- \'-'0(l'\;%'h'7' iliJir'mM)

biofacies including other kinds of microfossils and the lithofacies of this coreprovide us with some evidence of significant environmental change of the Sea
from the latest Pleistocene to Recent.
The origin and development of the
Sea of Japan have interested many
authors because the Sea has the oceanic
type crust transfered from the continent
type crust during the Neogene Tertiary
period; the area was a part of the
Asiatic continent at least until a certain
time of the Paleogene. Thenceforth thearea, particularly its eastern half, haschanged to the oceanic type sea, despite of its shape indicating a marginal
sea, through the process of the oceani-

Introduction and acknowledgements
In the course of study on fourty
piston cores from the Sea of Japan, we
found an interesting core which wastaken from just north off Tottori City,
San'in district of southwestern Honshu.
Unlike the other cores that are mostly
devoid of foraminiferal shells, the core,
V28-265, contains abundant planktonic
foraminifers throughout the length andindicates a definite Holocene-Pleistocene
boundary at a level between 107 cm and135 cm below the top. Besides, the* Received March 23, 1973; read January
16, 1973 at Sendai.

137

138

Hiroshi WIlE and Masaki ICHIIWRA

zation (e. g., BELOUSSOV and RUDITCH.
1961) or through the splitting-off of theJapanese Islands toward the Pacific
Ocean (e. g., MURAUCHI, 1966) ; the latteridea is related to the ocean-floor spreading theory. Therefore, the previous
investigations have been focused upon
the judgement which one of the above
two ideas is correct, mainly on the basisof comprehensive geophysical measurments. On the other hand, there arerather few studies of the sediment
samples. especially of long cores, thatshould inform the geologic age of themeasured physical properties and thehistoric change of paleoenvironment of
the Sea. Along with the prospecting of
the earliest marine sediments under thesea bottom, the researches on the derivation of oceanic condition into the area
would offer critical answers to the originof the Sea of Japan as an ocean.
The core V28-265 treated here may
give only the information about thelatest history of the Sea but may suggest
its essential characters during the glacialand post-glacial periods; the assumptions
presented in this paper may be applicable
not only to every glacial or inter-glacial
period but also to the pre-glacial period
including the earliest age of the Sea ofJapan.
This study was worked out as a partof the project entitled "Study of sedimentary deposits of the Sea of Japanand surrounding terrains" under theJapan-U. S. Cooperative Science Program (4R006). We express our sincene
thanks to all the participants from theLamont-Doherty Geological Observatoryof Columbia University for their kindcooperation, and also to the Japaneseparticipants for their discussion on the
resul ts. Weare also indebted to Dr.
William N. ORR, University of Oregon,
Eugene, Oregon and to Dr. James C.

INGLE, Jr., Stanford University, California, for furnishing us the topotypes
and hypotypes of Globigerina umbilicata
ORR and ZAITZEFF from the Rio Dell
Formation, along Centerville Beach southof Eureka, California. The manuscript
was reviewed by Miss Reiko FUSEJIMAof the National Science Museum ofTokyo.
Outline of the present environmentof the Sea of JapanThe Sea of Japan is a typical marginal
sea separated from the Pacific Ocean
by the Japanese Islands Arc. The four
outlets to the Pacific are shallower
than 130 m, but the northern half of the
Sea where the bottom is rather flatmeasures more than 3,000 m in water
depth with the oceanic type of crustunderneath. On the other hand, thesouthern half has a continental rise eastof Korea and the Yamato and KitaYamato banks at the middle, thus being
characterised by the complicated relief
implying different origins of the bed
rocks.
Warm currents called the Tsushima
Current and the East Korea Current,
enter through the Tsushima Straits into
the Sea of Japan where they seem todiminish so quickly that their influenceon the microfaunal or microfloral assemblages on the sea bottom appears tobe very small except for the narrowareas along the coast of Japan.
In contrast with the warm currents,
the cold water mass has much greater
influence on the sea bottom throughout
the whole area of the Sea. A part ofthis mass persists as a descent of the
Liman Cold Current, a portion of whichflows into the Sea through the strait
between Sakhalin and the Asiatic mainland and, to a greater extent, it is622.

Foraminifera from the Sea of Japan

Text-fig. 1.

139

Location map of the studied piston cores.
Bathymetry is shown in meters.

generated off the Asiatic continent
particularly in winter season. The
oxygen-rich surface water chilled by
the Siberian Air Mass that is developed
well in winter becomes heavier, sinks
down to the deep, and moves toward
the south. Since every southern outlet
is shallow, this cold water mass cannot
get out of the Sea of Japan and remains
there, producing a powerful effect on
the biotic and lithologic aspects of thesea bottom.
The present cold and oxygen-richwater is recognized in the hydrologic

observations cited by NUNO et al. (1969).
et al. emphasized the effect ofoxygenation on the sea bottom sediments, in which the content of organiccarbon is very low and the color of thesediments changes from olive to brownish at a very shallow depth, differingfrom the case of other normal oceans.
As fars as the top samples of 25 piston
cores treated by us are concerned, asimilar change of color from olive tobrown or yellowish brown was recognized between ca. 2,338 m and 2,226 mof water depth; that is much shallower
NUNO

140

Hiroshi UJIlE and Masaki !CHIKuRA

Table 1. 25 piston cores showing the approximate depths of the color change in the top
portions, of the lysocline, and of the calcium carbonate compensation.
Core No.

Water
Depth
(m)

Foraminiferal Shells

V28-2813588

Absent

V28-273

3533

AbsentRC12-385

3469

AbsentRC12-386

3497

Absent

V28-271

3382

AbsentRC12-382

3027

AbsentRC12-393

3010

Absent

V28-267

2831

Absent

V28-268

2692

Absent

V28-274

2677

AbsentRC12-384

2635

AbsentRC12-389

2650

AbsentRC12-388

2459

AbsentRC12-394

2338

AbsentRC12-377

2226

AbsentOlive throughout

RC12-383

2113

AbsentOlive, partly grer

RC12-374

2111

AbsentOlive throughout

RC12-380

1596

Partly dissolved

RC12-381

1437

Bartly dissolved

Olive throughout

RC12-376

1426

Partly dissolved

Olive throughout

RC12-378

1401

Partly dissolved

Olive throughout

V28-265

1218

Present throughout

Olive, partly grey

RC12-390

1103

Present throughout

Olive throughout

RC12-379

1010

Present throughout

Olive throughout

RC12-387

838

Present throughout

Olive throughout

Color in General Aspect
Top 36 em: yellowish brown to brown;
the other: olive, partly grey
Top 34 em: yellowish brown to brown:
the other: olive, partly grey
Top 11 em: brown; the other: olive,
partly grey
Top 25 em: yellowish brown to brown;
the other: olive, partly grey
Top 35 em: yellowish brown to brown;
the other: olive, partly grey
Top 30 em: yellowish brown to brown;
the other: oliye, partly grey
Top 64 em: yellowish brown to brown;
the other: olive, partly grey
Top 30 em: yellowish brown;
the other: olive, partly grey
Top 20 em: yellowish brown to brown;
the other: olive
Top 47 em : yellowish brown to brown;
the other: olive, partly grey
Top 34 em : yellowish brown;
the other: olive
Top 22 em: yellowish brown;
the other: olive, partly grey
Top 38 em: brown;
the other: olive
Top 2 em : yellowish brown;
the other: olive partly grey

622.

Foraminifera from the Sea of Japan

than the averaged depth (4,000 to 5,000 m)of the oceans.
The oxidizing effect seems to be more
distinct in the calcium carbonate compensation. As shown in Table 1 thesurface samples of the 25 cores suggest
a very shallow depth of the compensation, at a level between 1,596 m and1,437 m, and also that of the lysocline
somewhere between 1,401 m and 1,218 m.
Generally the calcium carbonate compensation depth . is regarded as thefunction of the water depth accompanied
by higher solubility owing to increasingpressure, of the carbon dioxide pressure
in water, and of the sinking rate of
calcium carbonate shells or skeltons. In
the case of the Sea of Japan, however,it appears that the rich dissolved oxygenin water affects most effectively thecompensation, different from ordinary
instances such as summarized by BERGER(1971).
We would like to conclude that thepresent day hydrology of the Sea ofJapan is characterized by extraordinarily
oxygenated condition of water. Thismay be supported by NIINO et al. (1969)
who measured very low organic carbon
content mostly less than 1% in thesurface sediments of the deep floor of
the Sea.

Core V28-265 and materials
for this study
V28-265, a piston core, was taken at
Lat. 36°17'N., Long. 134°34'E, from thewater depth of 1,218 m so that the calcareous shells of planktonic foraminifers
remain unaffected by leaching out almost
throughout the whole length of 920 cm.
Lithology of the core on a half-cut face
was described by N. FUJI of Kanazawa
University at the Lamont-Doherty Geo-

141

logical Observatory of Columbia University as his task of the Japan-U. S. Cooperative Project and, at the same time,
described and photographed by J. RIGAUD
of the Observatory as a routine work
there. The three kinds of documentation compiled by us are summarized in
the columnar section of Text-figure 2.
The core is olive-colored throughout,with a slight variation, and is composedof silty clay to clayey silt, intercalatedwith rare seams of sand, one of which
consists of foraminiferal shells. Two
acidic ash layers 1 cm thick each occur
at 183-184 cm and 511-512 cm below the
top. Upper one-third of the core iscompletely homogeneous, whereas lower
two-thirds are predominated with very
thinly laminated clay frequently accompanying homogeneous or burrowed
layers. Among the laminated, burrowed,
and homogeneous types of layers there
seems to be no definite relationship but,in the interval ranging from about 590
cm to 740cm below the top, the burrowed
layer grades upward into the homogeneous one and lies on the laminated one.
This relation might imply the origin of
the homogeneous clay that may havebeen produced through the mixing oflaminated clay by some burrowing
worms. Concerning the preservationof foraminiferal shells, however, we
could not find any evidence supporting
this process, although BERGER and
SOUTAR (1970) recognized some of theevidences.
All cores from the Sea of Japan werevertically cut into four portions, and aquarter of every core was presented tothe participants from Japan for study.
For the foraminiferal study 2 cm thickportions of this quarter of core weretaken at stratigraphic intervals of 10 cm
between 5-7 cm and 215-217 cm, and atintervals of 20 cm between 225-227 cm

l42

Hiroshi UJIlE and Masaki !CHIKURAcwz"GLOBIGERINA"
PACHYDERMA

x

RIGHT
LEFT
r-:---=IOO%-----:"1

~
<I:

w

en SPECIMEN NO. of
w
...J

Q.

.

COILING RATIO of

G. PACHYDEMA\FAUNALCOMPOSITION

r----

·/

IOO% 4/"PLANKTONICRATIO'(%)-'- ---[]J
BURROWED

B
B

FORAMINIFERALSAND SEAM

B

SAND SEAM

..

~

:::1
...
t-.q--"",.: :8:~.

It-_-~\. . ~.

..
\

\

.,

I,

,
'>

!

·
·
I

Text.fig. 2.

Foraminiferal analysis of the core V28-265.

622.

Foraminifera from the Sea of Japanand the bottom (see Text-figure 2, forthe exact pO(:,ition of samples). After
weighed in dry condition, all samples
were washed through a 200 mesh screen.
From the dried residue on the screen,
the 200-odd specimens of planktonic
foraminifers were picked out at random
under the binocular microscope (seeUJIIE, 1962, for the method of random
sampling of individuals and for thestatistical meaning of the 200-odd total
number of specimens).
Foraminiferal assemblages

The core V28-265 contains many
foraminifers sufficient for analysis, except for the part between ca. 145 cm andca. 200 cm below the top. The absenceof foraminifers in this part may be ascribed to the fact that pyroclastics aredeveloped there, particularly in the partaround an ash layer at 183-184 cm, as
indicated by a considerable amount of
volcanic glass fragments found in theresidue of washed samples. Also, an environmental condition might be anotherexplanation of this particular part. As
will be mentioned in the next section,
this part seems to have been depositedin an anoxic condition of the bottom
water where calcite shells of foraminifers may have been dissolved by thepresumably high content of carbon
dioxide.
From 45 samples we identified 7,733
specimens belonging to 11 species ofplanktonic foraminifers as recorded inTable 2. The faunal composition of all
but one samples is quite similar andsimple, with predominance of very few
cold water tolerant taxa. An exception
is the top sample where common occurrence of "Globoquadrina" dutertrei andrare Globigerinoides ruber and Globoquadrina sp. A suggests a slightly warmer

143

condition. These general aspects present
a contrast with the faunas in the Tsushima Straits where the subtropical elements are dominant (UJIIE, 1973). Sincesuch subtropical faunas were found allover the length (500 cm) of the core
RC12-373 from on the shelf off Yamaguchi Prefecture, the Tsushima Warm
Current may diminish quickly between
the localities of RC12-373 and V28-265.
According to the preliminary check of
the 25 cores mentioned above, the cold
water mass appears to affect on planktonic foraminifers of the Sea of Japanas a whole in much greater extent than
the warm water currents do; this viewagrees with that from the hydrologic
observation as mentioned already.
It is noticeable that the "cold water
fauna" is predominated only by two
species, i. e., "Globigerina" pachyderma
and Globigerina umbilicata. The" G."pachyderma dominant fauna has beenrecognized in the Recent Arctic (GREEN,
1960; BE, 1960) and Antarctic Oceans(e. g., BE, 1969). In these seas, moreover,they are predominantly left coiling shells(more than 90%). The species is also
common in the subarctic and subantarctic regions and in some upwellingareas in middle latitudes, although theright coiling shells predominate there.
The change in the coiling direction of" Globigerina" pachydenna as a paleoclimatic indication was observed first in
the deep sea cores of the Atlantic
Ocean (ERICSON, 1969) and in 12 coresfrom off California and 2 land sections
in southern California (BANDY, 1960).
Particularly using the sea bottom coresfrom off California, BANDY revealed adistinct change from the sinistraldominant population to the dextraldominant one at about 11,000 yrs B. P.
based on the carbon-14 dating, and heregarded it as an index of the Holocene-

144

Hiroshi UJIlE and Masaki IcHIKURA
Table 2.

Globigerina pachyderma(EHRENBERG) left

Globigerina pachydenna(EHRENBERG) rightGlobigerina umbilicata
ORR & ZAITZEFF

1

2 3

6

36

8 5 11 11 18

8

Occurrence chart of planktonic

9 11 13 14 15 21 22 24 26 28 30 34 3638
2 1 18 1 3 44 55 26 218 183 120 76 1

109 24 48 17 57 26 41
6

1

2

4

3

2
3

5 22 127 177 154 82

7

9 60 127 6

Globigerina cf. bulloidesl?

O'ORBIGl\YGlobigerina quinqueloba
NATLANO

Globigerina cf. anguistiumbilicata BOLLI
Globigerina sp.
Globigerinita glutinata(EGGER)

Globigerinita uvula(EHRENBERG)

Globigerinoides ruber(O'ORBIGNY)" Globoquadrina" dutertrei(O'ORBIGNY)

Globoquadrina sp. A

4

10

1

1

2

16

2

2 1 1

26

3 14

6

15

4 15

5 10

2
2
5

9

1?

1

1

1

7 70

2 11

1

1
26

2

2

2

1
1

4?

2?

I?

1

Total

216 34 59 35 68 50 47 2 26 2 12 223 218 220 230 225 241 218 25

Benthonic total

243 161 62 167 223 219 184 2 3 0 3 10 53 82 13

Pleistocene boundary. We noticed aquite similar change of coiling ratios
between Samples 11 and 14 of V28-265(Sample 12 is devoid of the species and
13 contains only one sinistral specimen),
namely, between 107 cm and 135 cm
below the top of the core. The ratios
calculated here are warranted by thestatistically sufficient number of specimens per sample as shown in Textfigure 2 and Table 2. Exceptionally in
Samples 21, 38, and 50, the 100% left
coiling is represented by 3, 1, and 1
individuals, respectively.
Along with the coiling variation, somemorphological variations are recognized
between sinistral and dextral "Clobigel'ina" pachydama of V28-265. While

0

0

0 4

the sinistral forms are dominantly provided with less lobulate four chambers
per whorl (see example, in Plate 21,
fiig. 1), many dextral ones have fourand a half, or rarely five, chambers
which are so lobulate in general shapethat they somewhat resemble "Cloboquadl'ina" dutertrei (Plate 21, fig. 3).
The former type of variation was also
found· in the Antarctic Ocean (BANDY
and THEYER, 1971), especially in theregion south of the Antarctic Convergence (KENNETT, 1968). On the other
hand, the latter variation with a greaternumber of more lobulate chambers havebeen found in the "sinistral-dominant"populations of the subantarctic region
and the Arctic Ocean (KENNETT, 1968,

622.

145

Foraminifera from the Sea of Japan

foraminifers in the core V28-265.
._---- - - - - - - - - - - - - - - _ . _ -40 42 44 46 48 50 54 56 58 60 62 64 66 68 70 72 74 76 78 80 82 84 86 88 90 92
61 142 67 87 243 1 46 74 179 31 132 18 156 178 77 154 164 145 112 230 123 155 40 129 102 129
1

4

4

2

4

7

4. 1

3

5

1

1

1

2

2

7

6

1

141 23 113 10 15 5 155 128 38 3 41 6 18 16 165 92 47 39 119 41 72 51
1

1

2

I?

1

1
13 22 10 74

1 2

12 23

21

19

15 11

1 13

11

8

4
1

I? I?
5 41

8

2 12

1?

1?

65 50 82 20
1

6 165 29 71 11
1

I?

1 15

2

2

5 15

1

2 49 11 23

3

4? I?

I?

2? I?

9 56 38 63

2?

1?

9 42

I?

4

223 233 208 218 266 9 217 250 221 36 225 28 206 202 246 247 237 221 233 280 196 219 330 279 322 230

o

0

0 17

0 4

8 147 16 37 10 6 29 161970). With regard to the grade of theencrusting process of shells, there is nodifference between the two types ofvariation in the case of V28-265, bothtypes being rather thinly encrusted,notwithstanding BANDY'S (1972) opinion.
BANDY was inclined to conclude thatthe variants with highly thickened walls
have been developed in the glacial Pleistocene and are present-day daignosticof deep polar waters. However, weagree with BANDY's view that "Globigerina" pachyderma [his Globorotalia(Turborotalia) pachydermaJ
includesGlobigerina bulloides borealis BRADY,
Globigerina incompta CIFELLI, and Globorotalia pseudopachyde.rma CIT A, PREMOLI SILVA and ROSSI as its younger

2 33

0

0 28 28

3 97

5 15

0

synonyms.
Apart from the morphologic variations
mentioned hitherto, the predominancy
of coiling direction seems to be an expressivity of the phenotypes reflecting
different water temperatures. Therefore, the quick change from the sinistraldominant population to the dextraldominant one at about 120 cm below the
top of V28-265 is thought to show apaleoclimatic change from the glacial
Peistocene to post-glacial Holocene. At
the same time, constant occurrence ofthe sinistral population from. the boundary down to the bottom of the core may'
imply absence of any interglacial orinterstadial warm stage. When ca. 1 cm
per 1,000 years of the sedimentation rate

146

Hiroshi U!IlE and ,Masaki ICHIKURA

estimated for the Holocene part* of
V28-265 is applied to the lower part, thebottom will be of about 92,000 yrs B. P.
If this would be true, there should be
the Riss-Wlirm interglacial stage.
though we do not intend to employ sucha short chronology as was maintainedby EMILIANI (1966, 1970) who copressed
the four glaciations from the Glinz to
the Wlirm stages within the last 0.4
million years and placed the upper limitof the Riss-Wlirm interglacial stage at
ca. 60,000 yrs B. P. Many authors (seeBERGGREN, 1972), however, consideredthat the four events occurred within thelast 0.7 million years. In the same way
as EMILIANI but on the basis of new
data and different interpretation of theinsolution change and the 18 0 record of
the deep sea cores, BROECKER (1966;
BROECKER and VAN DONK, 1970) ascribed
the high stands of sea to the retreat ofglacier at about 80,000 yrs B. P. In 28
piston cores from the western Gulf of
Mexico, KENNETT and HUDDLESTUN(1972) recognized planktonic foraminiferal faunas indicating an abrupt climatic change which corresponds to thatfrom the interglacial to the glacial
around 90,000 yrs B. P. In the case of
V28-265, therefore, the age about 92,000
yrs B. P. for the bottom might be an
overestimation; this is quite reasonablebecause the estimated rate of sedimentation must be higher during the glacial
stage accompanied by lowering of sea
level, particularly in a marginal sea
such as the Sea of Japan.
Another dominant taxon of planktonic* The top of the core may represent thepresent day, because the stratigraphicalchanges of diatom floras, of pollen-assemblages and of the uranium content of the corewell correspond with those of the other coresfrom the Sea, respectively (after unpublisheddata by the participants of this project).

foraminifer in V28-265 is Clobigerina
umbilicata ORR and ZAITZEFF that wasrecently (1971) described from the Upper
Pliocene in the northernmost part ofCalifornia. Fortunately we were able
to compare our specimens with topotype
specimens from the upper Rio Dell Formation on CenterviIIe Beach near Eureka
through the courtesy of W.N. ORR andwith many specimens in a washedsediment sample from the middle Rio
Dell Formation, about 1,900 feet stratigraphically below the type locality, bykindness of J.C. INGLE, Jr. INGLE (personalcommunication dated December 4, 1972)
also found this taxon in the 'Pliocene
and Pleistocene cores which were takenfrom the northeastern Pacific by Leg 18
cruise of the Deep Sea Drilling Project.
As shown in Plates 21 and 22, these
specimens from the northeastern Pacificregion are identical with our specimensfrom V28-265. Our materials, however,are seldom accompanied by Clobigerina
bulloides, whereas in the northeastern
Pacific C. umbilicata never predominates
over the always associated C. bulloides
so that INGLE thought the former taxon
to be a phenotypic variant of the latterand to be called Clobigerina bulloides
umbilicata. Nevertheless, so far as our
specimens are concerned, we are inclined
to treat C. umbilicata as an independent
taxon, especially becuase of the numberof its chambers per whorl ranging fromthree or four in juvenile stage to fiveor six in full grown stage, as stated in
the original description, different fromC. bulloides which is provided with three
and a half to four chambers per whorl
throughout the ontogeny. Moreover, theheavily thickened shell of C. umbilicata
may be one of the most important
specific characters. ORR and ZAITZEFF(1971) considered this thickening to be of
secondary [after the death ?], but we622.

Foraminifera from the Sea of Japan

think differently since other associatedtaxa, particularly "C." pachyderma,
never have such heavily thickened shells.
A stratigraphically interesting thingis that the occurrence of C. umbilicata
is limited almost to the Pleistocene
portion which yielded a considerable
number of specimens (Table 2, Textfigure 2); in the Holocene portion of thecore, only a few and probably juvenile
small specimens are found. Re-examination may be required for the occurrence of so-called Clobigerina bulloides
previously reported in the Pliocene andPleistocene faunas of the Sea of japan
region including the land sections.
Later, this species will be an index
fossil of the probably upper Pliocene toPleistocene beds in the mid-to highlatitude areas.
In this paper, we do not intend toreport or discuss the details of thebenthonic foraminifers. Howeve, wewould like to point out an interesting
fact that the benthonic faunas become
suddenly dominant over the planktonics
after the Pleistocene as seen in thechange of "planktonic ratio" of Textfigure 2. The ratio is a ratio of thetotal number of planktonics to all specimens including benthonics which wereencountered during the picking-out of
the 200-odd planktonic specimens per
sample. The distinct change of the ratio
at about 120 cm below the top of thecore may reflect the environmental
change toward the present-day oxygenated condition from the Pleistocene, inwhich an anoxic condition is supposed
as shown in the next section.
The Holocene benthonic fauna is characterized by the common occurrence ofIsrandiella, Cassidulina, Trifarina andEpistominella levicula RESIG and by theabsence of Elphidiidae. This general
aspect of faunal composition well agrees

147

with that of " A province" classified by
TROITSKA]A (1970). She treated 74 surface samples from the greater part of
the Sea of japan and divided the faunal
provinces of benthonic foraminifer into
three; A province characteristic in thecontinental shelf off the Asiatic mainland, B in the continental slope and central basin, and C in the Yamato andKita-Yamato Banks. The Pleistocene
benthonic fauna of V28-265 is very poorin numbers of taxa and specimens incomparison with the Holocene one, but
its composition is not different essentially from the latter, except for the characteristic occurrence of some bolivine
forms.

Environment suggested by thecore V28-265
As stated in the second section of thispaper, the Recent Sea of japan is notaffected largely by the warm current as
a whole, different from some previous
opinions, most of which were dependent
on the data obtained from the region
near the coasts of the japanese Islands.
Planktonic foraminifers in the Holocene
portion of V28-265 also do not indicate awarm environment. Such a cool temperate condition seems to be supported
by other microfossils in the core, suchas radiolarians, diatoms, coccoliths, andpollens, according to the japanese participants in the same project.
Thus, no contrastive difference can be
expected between the Holocene andPI.eistocene parts of the core so far as
the paleoclimatic interpretation of thesemicrofossils is concerned, except for thecoiling direction of " Clobigerina " pachyderma. However, the detailed analysesof diatoms and pollens revealed the floral
change around 138 cm and 123 cm below

148

Hiroshi UJIlE and Masaki ICHIKURA

the top, respectively, due to increasing
temperature since the latest Pleistocene.
More remarkable and interesting environment would be inferred for thelatest Pleistocene part. One of thegreatest glaciations appeared to haveoccurred in the latest Pleistocene (e. g.,
FLINT, 1971); it resulted in a marked
lowering of the sea level so that theshallow (less than ca. 130 cm) outlets of
the Sea of Japan toward the open oceansrose almost above the sea level, and sothey might have made the obstruction
against the incoming surface water fromthe open ocean. This obstructive effectseems to be reflected in the fact thatradiolarians, most typical pelagic microorganisms, are scarce or absent in the
Pleistocene part. This situation might
have affected the ratio of pelagic diatoms
to benthonic ones; namely, the ratio islower in the Pleistocene part than in the
Holocene in general.
The Sea of Japan turned into an enclosed sea like a huge lagoon or lake
may have been provided with anoxic
condition, which would be accentuatedby decreased chilling effect of the Siberian Air Mass on the surface water
during the glacial stage. Such a phenomenon was first suggested by MIYAKE

et al. (1968) who recorded an extremely

high content of uranium in the" Pleistocene" part of a short core from thenorthern part of the Sea. In an anoxic
condition, uranium in sea water is' reduced from hexavalent to tetravalentstate, to be readily precipitated to thesea bottom. In V28-265, Y. SUGIMURA
found very high values of the uranium
content such as 9.8 and 9.6 ppm at 150160 em and 200-210 cm below the top.
The reduced environment may be represented by the scarcity of benthonicforaminifers and the common occurrenceof framboidal pyrite in the Pleistocene
portion of the core. Absence of foraminifers in the uppermost Pleistocene of
the core also reflects a large-scale reduction that should produce high pressure of carbon dioxide in the bottom
water and calcareous shells would be
dissolved. Similar effect of dissolution
seems to have acted on the probably
Pleistocene part of the other cores whichcame from the water deeper than thecompensation depth of the Sea of Japan.
Unless the dissolution took place, thepart should contain foraminiferal shells
because the highly oxygenated condition
like the existing state could not be expected in the Pleistocene portion. The

Explanation of Plate 21
Figs. 1-3. "Globigerina" pachyderma (EHREl'BERG).
1: Umbilical side of a sinistral form (NSMT-Micropal. ColI. 580), from Sample 40,395397 cm below the top of the core V28-265; 2: Umbilical side of a dextral form with lesslobulate chambers (NSMT-MC 606) ; 3: Spiral side of a dextral form with lobulatechambers (NSMT -MC 605), both from Sample 8, 75-77 cm below the top of the core;
all x 200.
Figs. 4-7. Globigerina umbilicata ORR and ZAITZEFF from the middle Rio Dell Formation,
1,570 feet south of Guthrie Creek, Humbolt County, California. 4: Spiral side of a fullgrown specimen (NSMT -MC 592), x 180; 5: Umbilical side of adult specimen (NSMTMC 593), x 180; 6: Spiral side of juvenile specimen, already with thickened wall
(NSMT-MC 596), x200; 7: Lateral and apertural side of young specimen (NSMT-MC594), x 150.

UJIIE and IcHlKURA :Fomminifera frmn the Sea of Japan

Plate 21

622.

Foraminij'era j'rom the Sea oj' Japansituation is different from the case ofan anaerobic basin off California report·
ed by BERGER and SOUTAR (1970) who
recognized that the plankton shells arepreserved better there than in the adjacent areas under the normal condition.
Anoxic influence may be the color of
the probably Pleistocene parts of thecores deeper than ca. 2,500 m of the Sea
of Japan; namely, the color of the parts
turns olive from brown or yellowish
brown of the probably Holocene parts(Table 1). However, it may be difficult
to locate the Holocene base by this color
change alone, since the change is partly
due to post-burial reaction with poresolution.
The explanation of the presumed environment for the core V28-265 given inthis paper is largely dependent upon theunpublished data obtained by the participants of the project. Somewhat moredetailed data and discussion will be published as a short synthesized paper in
the near future (UJIIE et al., 1973).
References
BANDY, O. L. (1960): The geologic significance of coiling ratios in the foraminifer
Globigerina pachyderma (EHRENBERG).
Jour. Paleont., vol. 34, no. 4, pp. 671-681.
- - (1972): Origin and development of
Globorotalia (Turborotalia) pachyderma(EHRENBERG).
Micropaleontology, vol.
18, no. 3, pp. 294-318, pis. 1-8.
- - and THEYER, F. (1971): Growth variation in Globorotalia pachyderma (EHRENBERG). Antacrtic Jour. U. S., vol. 6, no.
5, pp. 172-174.
BE, A. W. H. (1960): Some observations on
Arctic planktonic Foraminifera. Contr.
Cushman Found. Foram. Res., vol. 11, pt.
2, pp. 64-68.
- - (1969): Planktonic Foraminifera. III
Amer. Geogr. Soc.: Distribution of
selected groups of marine invertebrates

149

in waters south of 35"S Latitude, Folio
11, pp. 9-12.
BELOUSSOV, V. V. and RUDITCII, E. M. (1961) :Island arcs in the development of theearth's structure. Jour. Geol., vol. 69,
pp. 647-658.
BERGER, W. H. (1971): Sedimentation ofplanktonic Foraminifera.
Mar. Geol.,
vol. 11, pp. 325-358.
and SOUTAR, A. (1970): Preservationof plankton shells in an anaerobic basin
off California. Geol. Soc. America, Bull.,vol. 81, pp. 275-282.
BERGGREN, W. A. (1972): Late PliocenePleistocene glaciation. III BERGGREN,
W. A. [ed.J. Initial Reports of th DeepSea Drilling Project, vol. 12, pp. 953-963.
BROECKER, W. S. (1966): Absolute dating
and the astronomical theory of glaciation. Science, vol. 151, pp. 299-304.
- - and VAN DONK, J. (1970): Insolation
changes, ice volumes, and the 0 18 record
in deep-sea cores. Rev. Geophys. SPace
Phys., vol. 8, no. 1, pp. 169.
EMILIANI, C. (1966): Isotopic paleotemperature. Science, vol. 154, no. 3750, pp.
851-857.
(1970): Pleistocene paleotemperatures.
Ibid., vol. 168, pp. 822-825.
ERICSON, D. B. (1969): Coiling direction of
Globigerina pachyderm a as a climatic.
index. Science, vol. 130, pp. 219, 220.
FLINT, R. F. (1971): Glacial and Quaternary geology. xii+892 pp., J. Wiley &Sons, Inc., N. Y.
GREEN, K. E. (1960): Ecology of some Arctic
Foraminifera. Micropaleontology, vol. 6,
no. 1, pp. 57-78, pI. 1.
KENNETT, J. P. (1968): Latitudinal variationin Globigerina pachyderma (EHRENBERG)
in surface sediments of the southwest
Pacific Ocean. Ibid., vol. 14, no. 3, pp.
305-318, pI. 1.
- - (1970) :Comparison of Globigerina
pachydenna (EHRENBERG) in Arctic andAntarctic areas. Contr. Cushman Found.
Foram. Res., vol. 21, pt. 2, pp. 47-49, pis.

8, 9.
- - and HUDDLESTUN, P. (1972): Abrupt
climatic change at 90,000 yr BP: Faunal

150

Hiroshi UJIlE and Masaki ]CHIKURA

evidence from Gulf of Mexico cores.
Quaternary Res., vol. 2, pp. 384-395.
MIYAKE, Y., SUGIMURA, Y. and MATSUMOTO,
E. (1968): Inonium-thorium chronologyof the Japan Sea cores. Rec. Oceanogr.
Works japan, vol. 9, no. 2, pp. 189-195.
MURAUCHl, S. (1968): Origin of the Japanese Islands. Sei-En, no. 5, pp. 20-23(in Japanese].
NIlNO, H., EMERY, K. O. and KIM, C. M.
(1969): Organic carbon in sediments ofJapan Sea. jour. Sed. Petrol., vol. 39, no.
4, pp. 1390-1398.
ORR, W. N. and ZAITZEFF, J. B. (1971) : A newplanktonic foraminiferal species fromthe California Pliocene. jour. Foram.
Res., vol. 1, no. 1, pp. 17-19, pI. 1.
TROITSKAJA, T. S. (1970): Environmental

conditions and distribution of foraminifers in the Japan Sea. Rep. Inst. Ceol.
Ceophys., Siberian Div., Acad. Sci. USSR,
fasc. 71, pp. 136-160, 8 pis. [in Russian;translated in Japanese by Y. KUWANO].
UJIIE, H. (1962): Introduction to statisticalforaminiferal zonation. jour. Ceol. Soc.
japan, vol. 68, no. 803, pp. 431-450.
- - (1973): Sedimentation of planktonic
foraminiferal shells in the Tsushima andKorea Straits between Japan and Korea.
Micropaleontology, vol. 19, no. 4 (in press).
- - , SUGIMURA, Y., FUJI, N., OINUMA, K.,
KOIZUIIIl, 1. and SUGANO, K. (1973):
Latest Quaternary environment of the
Sea of Japan suggested by a piston core.
Science (in press).

Explanation of Plate 22
Figs. 1-6. Clobigerina umbilicata ORR and ZAITZEFF from the core V28-265, x 200 excluding
fig. 6. 1: Spiral side of juvenile specimen (NSMT -MC 586), from Sample 40, 395-397
cm below the top; 2: Lateral and apertural side of juvenile specimen (NSMT-MC 587),
from Sample 40; 3: Umbilical side of young specimen (NSMT -MC 585), from Sample
40; 4: Umbilical side of adult (NSMT -MC 582), from Sample 56, 555-557 cm below the
top; 5: Lateral and apertural side of adult (NSMT -MC 583), from Sample 40; 6:
Umbilical side of adult (NSMT -MC 584), from Sample 56, x 180.

UJIIE and I CHIKUR A:

Foraminifera from the Sea of Japan

Plate 22

Trans. Proc. Palaeont. Soc. Japan, N.S., No. (n, pp. 151-160, pis. 23, 24, September 20, 1973

623.

LATE LOWER CARBONIFEROUS EOSTAFFELLA AND

HEXAPHYLLIA FROM CENTRAL OREGON, U. S. A.*
KIMIYOSI-II SADA
Department of Geology, Faculty of General Education,
Hiroshima University, Hiroshima 730

and
WILBERT R. DANNER
Department of Geological Sciences, The Universityof British Columbia, Vancouver, Canada

Oregon 1+10) III !J~·I';II.J: f) ifi~-j- 0 Eostaffella c Hexaphyllia: Oregon 1'['1 COlt 1£111!h- ;}II
fcisLllL-]- {S Crook County CO Suplee ±i!J.J!iXt::. J}11i l""C v' 0 Coffee Creek Formation OY1i
EkE!?:'; J::. iJ, ~Fl:&' G l;t Eostaffella Ut:)j~::kl;iii' G C. ~1-;t -c tdll'i5 ,~q1,t~{9IJcotJ: v' Hexaphyllia ~~~~IJ l t~o)"c, c. C. lc ffWr-]- 0 ;ic!f& 2: ~lJ:H(I;t Eostaffella oregonensis SADA andDANNER, n. sp., E. sp. A c Hexaphyllia sp. ""(:'ji;,{So C.fL,Gcor~fill:fCJ::. -:0 ""ChW)JX;2:;!l0Suplee Eostaffella 1r,:rifU)1JI)I\H;t Late Mississippian (Chesterian) 1I1}ito) <b CO c %-:Z G
i/l: 1:11 ~ ftf. DANNER, W.R.
0
0

*"0

British Columbia, Canada, but it will
be described in a later paper when its
associated fauna has been studied indetail.)The Coffee Creek Formation has beenstudied by PACKARD (1928, 1929, 1932),
MERRIAM and BERTHIAUME (1940, 1943),
MERRIAM (1942), DANNER (1965) and by
BUDDENHAGEN (1967). It was named by
MERRIAM and BERTHIAUME (1940, 1943).
MERRIAM (1942) described rugose corals
from the Formation having a closeaffinity to species from the Eurasian
Lower Carboniferous and concluded that
the Formation belonged to the Lower
Carboniferous (Mississippian). In 1962
DANNER collected organoclastic limestone consisting of coarse brachiopod
shells and shell fragments in a finer

Introduction
The primitive fusuline Eostaft'ella occurs in organoclastic limestones of the
Coffee Creek Formation and in an unnamed oolitic limestone in the Suplee
area, Crook County, central Oregon.
Two species of Eostaft"ella are associatedwith Hexaphyllia, an index coral of
Visean (Late Mississippian) age knownin Europe and Asia but previously unreported from North America. (Wehave also collected a different speciesof Hexaphyllia from a limestone body in
the Cache Creek Group near the community of Rayleigh north of Kamloops,* Received April 3, 1973; read Oct. 28, 1972
at Matsuyama.
151

152

Kimiyoshi SADA and Wilbe1"t R. DANNER

grained matrix from MERRIAM's type
locality (S2) of the coral fauna in the
Coffee Creek 'Formai:io~.'· This li~estone
contains numerous ~alcateous forami·
nifera including two species of Eastal·leila and species of Endothyra. Oolitic
limestone cropping out 3t miles to thenortheast, north of the South Fork of
Trout Creek and just east of the northernmost of the Suplee area Devonian
limestones was collected in 1966. It
also contains Endothyra and Eostaffella.
DANNER'S material was studied by SADA
during his stay as a post-doctoral Fellow(1967-1969) at the University of British
Columbia.
This paper contains the descriptionof the species of Eostafleila as Eostalleila oreganensis SADA and DANNER, n.
sp., E. sp. A and Hexaphyllia from MERRIAM's type locality (S2) of the coralfauna in the Coffee Creek Formation
north of Grindstone Creek.
The slides used as figured specimens
for this paper have been deposited with
the Division of Paleontology, U. S. National Museum, Washington, D. C. limestone specimens containing the faunas
will be kept in the stratigraphic-paleontologic reference collections of the Universityof British Columbia Departmentof Geological Sciences.
Field work in the Suplee area by DANNER and laboratory work by SADA were
financially supported by the National
Research Council of Canada and theCommittee oil Research of the Universityof British Columbia as part of along term study of western Cordilleran
Late Paleozoic faunas~ DANNER wishes
to acknowledge assistance in the fieldfrom Professor Glenn ROUSE of the
UnIversity of British Columbia, student
Kurt Nielsen and Boy Scouts Lyall
Bailey and Vladimir Krajina. Permission to c'ollect in the area was gra-ciously granted by the Hudspeth Ranch
Company. We also want to express ourappreciation to Dr. Dorothy HILL of the
University of Queensland for her information on Hexaphyllia. Further workon this project was carried out while
DANNER was visiting Professor at Hiroshima University under the auspices of
the Japan Society for the Promotion of
Science.
Geology

The Coffee Creek Formation in theSuplee area consists of scattered outcrops of complexly' folded and faulted
marine limestone and sandstone forming
ridges and knobs in the semi-arid sagebrush landscape. It is part of a sequence of Devonian, Mississippian, Pennsylvanian, Permian and Triassic rocks
forming an inlier overlain by later Mesozoic and Cenozoic rocks. MERRIAM and
BERTHIAUME (1940, 1943) described the
Coffee Creek Formation as a sequence
274 to 304 meters thick composed of:" well-bedded fairly pure limestone, carbonaceous limestone, argillaceous tosandy limesto~e and calcareous sandstone." They gave the following detailed description of 23 meters of limestone at the type locality:"Within the upper 40 feet very dark grayto black argillaceous and carbonaceous
limestones are in places rather thin-bedded.
These deposits are locally packed with thebrachiopod Striatifera. Forty-five feet fromthe top of the limestone section is a bedof very sandy limestone with Striatifera
immediately below which lies the main
Gigantella horizon. The usually large productid Gigantella is very profuse here in afine-grained and rather pure limestone ofdeep neutral gray; the large brachiopod isapparently restricted at this point to a bed
varying in thickness from one to two feet.
Within and below the Gigantella bed soli-

623.

tary and compound rugose corals areabun·
dant; these are embedded in the gray lime·stone or immediately below in argillaceous
limestones weathering to a light grayish
brown. In the lower 30 feet of this section
these argillaceous layers are interbeddedwith the purer gray limestones, while toward the base sandy limestones and calcareous sandstone predominate."

DANNER (1965) noted that part of thelimestone is oolitic, contains encrustingalgae, Endothyra, echinoid spines andthat some of the fossils are silicified.
BUDDENHAGEN's geologic map (1967) of
the central Oregon inlier shows the areal
distribution of the Coffee Creek Formation in detail.
The second locality (DS2) in the unnamed limestone lies about 3t miles
northeast of the Coffee Creek type locality and consists of a small exposureof oolitic and organoclastic limestone

MILES

o

2

3

4

SCALE
SHAW TABLE

N

1
TWELVEMILEOYAKIMA-,, WASHINGTON.

°SALEM:*P-~~-TL"~N~-------------",-:JOHN

DAY /0o 0~,I

SUPLEE
AREA: 0

OREGON

153

Eostaffella dnd Hexaphyllia from Oregoni«II- ... --------- --""II------- ___ ... __ L

CALIFORNIA;, NEVADATWEL VE

MILE

CR.

5

6
0'0
ulu

154

Kimiyoshi SADA and Wilbert R. DANNER

about 31 meters downslope from an outcrop of Devonian reef limestone. The
oolitic limestone contains Eostaffella andEndothyra and the orga~oclastic limestone contains unidentified fragments ofbryozoa and brachiopods. The age iseither Late Mississippian or Early Pennsylvanian. The oolitic limestone is overlain by chert grit.

Discussion of the EostaO'ella faunain the Coffee Creek Formation

MERRIAM (1942) described four speciesof rugose corals from the Coffee Creek
Formation. The described species are
Dibunophyllum oregonensis MERRIAM,
Lithostrotion (Lithostrotion) pac1wrdi
MERRIAM, Lithostrotion (Siplwnodendron)ol'egonensis MERRIAM and Campophyllum
readi MERRIAM. Brachiopods were also
listed, namely, Gigantella sp., Striati/era
sp. and Spiri/er d. striatus (MARTIN).
Based on these species MERRIAM (1942;
MERRIAMand BERTHIAUME, 1943)
thought the age of the fauna to beroughly Visean in terms of British succession. MERRIAM also listed Tetrataxissp., small loxonemoid gastropods, andlithistid sponge spicules in the limestone.
Our species of Eostaffella are found in
the limestone associated with the corals
at Loc. DS1 (MERRIAM'S type locality"S2 ").
Eostaffella oregonensis SADA and DANNER, n. sp. shows a certain similarity
in general outline and some internal
character of the shell to Eostaffella
thompsoni (ANISGARD and CAMPAU) from
Upper Mississippian in Michigan, E.
mosquensis ROZOVSKA Y A from Upper
Visean in Russia, E. hohsienica CHANG
from the uppermost of Lower Carboniferous in China and E. kannzerai (IGo)ranging from Late Chesterian to Mor-rowan in Japan. Eostaffella oregonensis
seems to be nearly equivalent to these
species in its evolutional stage of theshell. Eostaffella sp. A, now being held
off from final identification' because oflack of well preserved material, resembles E. cooperi (D. ZELLER) from Uppermost Chesterian in Illinois.
Eostaffella oregonensis and E. sp. A
are found in association with Hexaphyllia sp. in the Coffee Creek Formation.
This is worth noting as Hexaphyllia, oneof the more important coral fossils forthe determination of geologic age is, as
far as we can determine, known only
in Lower Carboniferous sequences in
Europe and Asia. All of the known
species of Hexaphyllia have been described from Lower Carboniferous of
Scotland (DUNCAN, 1867), Lower Carboniferous of Central Russia (STUCKENBERG, 1904) and Lower Carboniferous ofJapan (Y ABE and SUGIYAMA, 1939; KANMERA, 1952; MINA TO, 1955).
Concerning the range of Hexaphyllia,
Dr. D. HILL states (personal communication) : " I think I can safely say that
there is no proven evidence that itexisted beyond the Visean into the
Namurian. My view would be, until it
can be shown otherwise, that it is avery good indication of Visean age."
From all of these considerations, itwould seem that the Eostaffella fauna(Loc. DS1) in the Coffee Creek Formation of Oregon is of Late Mississippian (Visean) (Chesterian) age.
Localities
DS! : MERRIAM'S locality" S2" in the Coffee
Creek Formation north of Grindstone
Creek. On limestone ridge! mile east ofMills' Sheep Camp 1~ miles S. 47 degrees
E. of Wade Butte in the NW t of section
3D, T. 18 S., R. 25 E. and north of the
road.

623.

Eostaffella and Hexaphyllia from Oregon

DS2: Small limestone outcrop about 31 meters downslope and east of northernmost
outcrop of Devonian reef limestone. On
hillside north side of South Fork of Trout
Creek. SE t section 9, T. 18 S., R. 25 E.
(See DANNER, 1968, Fig. 16, p. 840.)

Systematic Paleontology
Family Ozawainellidae THOMPSON
and FOSTER, 1937
Genus Eostaffella RAUSERCHERNOUSSOVA, 1948
Type species: - Eostaffella parastruvei
RAUSER, 1948.
Synonym: - Paramillerella THOMPSON,
1951.

Eoslaffella oregonensis SADA

and DANNER, n. sp.
PI. 23, figs. 1-10, 14-16

Description :-The shell of Eostaffellaoregonensis SADA and DANNER, n. sp. islarge for the genus and discoidal inshape, having a broadly rounded periphery. The lateral slopes are convex.
The mature specimens of five volutionsare 213 to 275 microns in length and 492
to 709 microns in width, giving the form
ratios of 0.36 to 0.43. The immature
specimens of three and one half to four
volutions are 174 to 215 microns longand 367 to 437 microns wide, showing
the form ratios of 0.47 to 0.49. The holotype of five and one half volutions (pI.
23, fig. 1, Rg. No. CF-C-46c) measures
268 microns in length and 700 microns
in width. Its form ratio is 0.38. The
inner and outer volutions are generally
involute but the last volution is rarely
and partly evolute.
The outside diameter of the proloculus

155

ranges from 29 to 54 microns. The
diameters of the whorls of the 1st to
the 5th volution of nine specimens are
66-108,113-199,190-298,318-461 and 492709 microns, respectively. The radius
vectors of the 1st to the 5th volution
are 27-54,53-95,89-143,159-280 and 254389 microns, respectively, for nine specimens. The spirotheca is composed ofa distinct tectum and inner and outerdense layers. The thickness of the
spiro theca of the 1st to the 5th vol uti onof nine specimens is 4-9, 4-14, 7-20, 1930 and 14-31 microns, respectively. The
thickness of the proloculus wall varies
from 2 to 9 microns. The septa are
fairly thick and slightly bend anteriorly.
The septal counts of the 1st to the firsthalf of the 5th volution of the specimen(CF-C-15a) illustrated as fig. 16 on PI.
23 are 6, 10, 11, 16 and 7, respectively.
The chomata are distinct.
Remarl2s :-Eoslaffella oregonensis resembles E. lhomj)soni (ANISGARD and
CAMPAU) (1963, pI. 9, figs. 7-8, 11-12, 15,
pI. 10, figs. 3-5, 7) described from Upper
Mississippian in Arenac County, Michigan. However, E. thompsoni has alarger shell at maturity and larger proloculus. Eoslaffella oregonensis is somewhat similar to E. 11losquensis (RozovsKA YA 1963, pp. 93-94, pI. 16, figs. 16-17,
figs. 1-5) in shell shape. These twoforms, however, can be easily distinguished by the smaller shell of themature specimens of E. oregonensis, its
shorter length of the shell and smaller
form ratio. In general outline and development of the shell, Eostaffella oregonensis resembles E. hohsienica CHANG(1962, pp. 440-441, pI. 1, figs. 4-6, 12, 13,
18-21) from the Hochow Limestone, theuppermost of Lower Carboniferous, near
the town of Xiangquan, Hohsien, Anhui
Province in China. However, E. oregonensis differs from E. hohsienica, for it

r-

0"\

0')

Table 1. Table of Measurements of Eostaffella oregonensis SADA and DANNER, n. sp.
Specimen

Rg. No.

Pl.

fig.

1
2
3
4
5
6
7
8
9

CF-C-46c
CF-C-34a
CF-C-20a
CF-C-11a
CF-C-18a
CF-C-29b
CF-C-5a
CF-C-17b
CF-C-46a

23
23
23
23
23
23
23
23
23

1
4
2
3
8
5
7
10
9

L.

W.

O. 700O. 709
0.624
0.577
0.587
0.501
0.492
0.367
0.437

0.268
0.275
0.228
0.218
0.256
0.209
0.213
0.174
0.215

Diameter of whorl

Prol.

R.

0.070
0.076
O. 085
0.085
0.066
0.076
0.066
O. 108
0.085

0.029
0.029
0.044
0.042
0.046
0.038
0.035
0.047
0.054

0.38
0.38
0.36
0.37
0.43
0.41
0.43
0.47
0.49

2

3

0.120
O. 156
O. 167
0.167
0.133
0.153
0.113
0.199
0.166

0.204
0.285
0.275
0.285
0.228
0.251
O. 190
0.298
0.285

4

31

4~·

0.370

o 401
0.427
0.461
0.368
0.394
0.318

5

5!

0.581
O. 7090.624

O. 700

0.577
0.587
0.501
0.492

0.367

~

~
.,..

~
0
<:t.>

;;:s-

.,..

~
t:::J

~

0.437

~

<2

R..

Specimen
1
2
3
4
5
6
7
8
9

~

s:

Thickness of spirotheca

Radius vector

{I:>

1

2

3

4

5

6

0

1

2

3

4

5

6

0.027
0.044
0.048
0.038
0.038
0.038
0.033
0.054
0.040

0.053·
0.085
0.089
0.074
0.077
0.061
0.066
0.095
0.080

0.089
0.147
O. 146
0.129
0.131
0.102
O. 1040.126
0.143

O. 159
0.280
0.237

0.254
0.389
0.337
0.334
0.330
0.285
0.292

0.370

0.009
0.002
0.008
0.004
0.004
0.005
0.007
0.009
0.008

0.006
0.004
0.008
0.009
0.003
0.004
0.006
0.007
0.009

0.007
0.012
0.013
0.013
0.010
0.004
0.009
0.011
0.014

0.014
0.009
0.014
0.013
0.016
0.007
0.013
0.010
0.020

0.024
0.020
0.030
0.024
0.021
-0.021
0.019
0.011
0.019

0.031
0.023
0.028
0.022
0.014
0.009
0.016

0.023

0.21p
0.209
0.184
O. 183
O. 1900.239(Measurements in millimetres)"'l<:"'to~b::t:..

!<:

~
~

623.

Eosta.tfella and Hexaphyllia from Oregon

has shorter length of the shell, smaller
form ratio at maturity, more arcuate
periphery and more primitive chomata.
In some respects EostaffeLLa oregonensis
is somewhat similar to E. kanmerai (IGo,
1957, pp. 175-177, pI. 1, figs. 20-26, pI. 2,
fig. 14; SADA, 1964, pp. 230-231, pI. 21,
figs. 8, 16, 17; SADA, 1967, pp. 144-145,
pI. 12, figs. 1-10; SADA, 1969, pp. 120121, pI. 12, figs. 1-13, pI. 13, figs. 1-2)
from Japan. However, E. kanmerai has
a smaller shell at maturity, shorter axisof coiling and thinner spirotheca.
Occurrence: - EostaffeLLa oregonensis
SADA and DANNER, n. sp. is abundantin thin sections and associated with E.
sp. A, Endothyra sp., other foraminifera,
HexaphyLLia sp. and DibunophyLLum oregonensis MERRIAM. Fossil locality DSl.
Geological age: -Late Mississippian(Chesterian).

EostaffeLLa sp. A
PI. 23, figs. 11-13

Description:-The shell of Eostaffella
sp. A is small and discoidal, and possesses a short axis of coiling and rounded periphery. The inner two or three
volutions are endothyroid coiling but
the quter ones are involute. The specimen (Rg. No. CF -C-50b) illustrated as
fig. 11 on PI. 23 is 142 microns in lengthand 308 microns in width. Its form
ratio is 0.46. The pro loculus is verysmall and its outside diameter is 28 microns. The diameters of the whorls of
the 1st to the 4th volution of a specimen are 61, 95, 174 and 247 microns,
respectively. The radius vectors of the
1st to the 5th volution are 26, 49, 76, 123
and 190 microns, respectively. The spirotheca consists of a tectum and inner andouter dense layers and its thickness ofthe 1st to the 4th volution is 5 to 17

157

microns. The chomata are very small.
Remarlls :-Eostaffella sp. A differsfrom Eostaffella oregonensis SADA andDANNER, n. sp. in several respects. The
former species has a smaller shell, fewer
number of volutions, slower expansionof the shell for the corresponding volution, smaller proloculus, thinner spirotheca and endothyroid coiling in its inner volutions. In general shell shapeand some internal character Eostaffella
sp. A resembles Eostaffella cooperi (D.
ZELLER) (1953, pp. 194-195, pI. 27, figs.
1-11) from the Kinkaid limestone ofUppermost Chesterian in Illinois. However, we put off the final identification
until we can obtain better preserved
material.
Occurrence:-Eostaffella sp. A is rare
and associated with E. oregonensis SADA
and DANNER, n. sp., Endothyra sp., otherforaminifera, Hexaphyllia sp. and DibunophyLLum oregonensis MERRIAM. Fossil
locality DSl.
Geological age: - Late Mississippian(Chesterian).

Order Heterocorallia SCHINDEWOLF, 1941
Family Heterophylliidae DYBOWSKI, 1873
Genus Hexaphyllia STUCKENBERG, 1904

Type species:-Hexaphyllia prismatica
STUCKENBERG, 1904.
Hexaphyllia sp.
PI. 24, figs. 1-2

Description:-The coraUum is hexagonal in transverse section and has six
prominent longitudinal ridges in position corresponding to the outer bordersof the septa. The corallum is small intransverse section. The specimens illus-

158

Kimiyoshi SADA and Wilbert R. DANNER

trated as fig. 1 (Rg. No. CF -C-2) and fig.
2 (Rg. No. CF -C-101) on PI. 24 are 0.50
mm. and 0.75 mm. in diameter, respec·tively. The calice is not preserved. The
wall consists of the thin primary walland thick stereozone lining the innersurface of the former. The corallum isdivided by six septa in subequal intervals in transverse section. Two opposite
septa meet at the center of the corallumand each of four septa forms Y shapein both sides of the two opposite septa.
Remarks: -We collected only fourtransverse sections of Hexaphyllia fromthe Coffee Creek Formation. Two ofthem are illustrated herein. They havestriking similarities in the form of thecorallite and the arrangement of the
septa. The present species is somewhat
similar to Hexaphyllia 7Ilirabilis (DUNCAN)(1867, p. 646, pI. 31, figs. 5a-5h) from theLower Carboniferous in Scotland. However, H. mirabilis can be distinguishedfrom the present species by having six
distinct longitudinal ridges with spinelike processes. Hexaphyllia sp. differsfrom H. prismatica STUCK ENBERG (1904,
pp. 72-73, Taf. 3, figs. 5a-5d) from theLower Carboniferous in Central Russia
in its septal arrangement. In the general outline of the corallum and theseptal arrangement, Hexaphyllia sp.
somewhat resembles H. elegans Y ABEand SUGIYAMA (1939, pp. 500-501, pI. 26.
figs. 1-3) from the Lower Carboniferousof Kitakami Mountainland. However,the former species differs from the latter in having more prominent ridges andsmaller diameter of the corallum. The
present species seems to be a new species belonging to genus Hexaphyllia. The
final determination of the present species, however, must be postponed until
more material is obtained.
Occurrence.-Hexaphyllia sp. is rare inthin section and the species associatedwith it are Eostaffella oregonensis SADA
and DANNER, n. sp., E. sp. A, Endothyrasp., other foraminifera and Dibunophyllum oregonensis MERRIAM. Fossil locality DSl.
Geological age: -Late Mississippian(Chesterian).
References
ANISGARD, H.W. and CAlvIPAU, D.E. (1963):
Paramillerella thompsoni, n. sp. from Michigan and a redefinition of Paramillerella.
Contr. Cushman Found. Foram. Res., vol.
14, no. 3, pp. 99-108.
BUDDENHAGEN, H.J. (1967): Structure andorogenic history of the southwestern partof the John Day Uplift, Oregon. The OreBin., vol. 29, no. 7, pp. 129-13S.
CHANG, L. (1962): Fusulinids from the Hochow Limestone, Hohsien, Anhui. Acta~~~~---~~--~~-

Explanation of Plate 23
All x 100
Figs. 1-10, 14-16. Eostaffella oregonensis SADA and DANNER, n. sp.
1. Axial section of holotype: Rg. No. CF-C-46c.
2-10. Axial sections of para types : Rg. No. CF -C-20a, CF -C-lla, CF -C-34a, CF -C-29b,
CF -C-33a, CF -C-5a, CF -C-1Sa, CF -C-46a and CF -C-17b, respectively.
14-16. Sagittal sections: Rg. No. CF-C-23a, CF-C-3a and CF-C-15a, respectively.
Figs. 11-13. Eostaffella sp. A
11-12. Axial sections: Rg. No. CF -C-50b and CF -C-50a, respectively.
13. Sagittal section: Rg_ No. CF-B-7a.

SADA

and DA NNER :Eostaffella and H exaphyllia f1"Om 01"e gon

Plate 23

623.

Eostaffella and Hexaphyllia from Oregon

Paleont. Sinica, vol. 10, no. 4, pp. 434-442.
DANN·ER, W.R. (1965) : Limestone of the West·
ern Cordilleran Eugeosyncline of South·
western British Columbia, Western Wash·
in.gton and Northern Oregon. Dr. D.N.
W:adia Commem. Vol., Mining & Metallur·
gical Inst. of India, pp. 113-125.
(1968): Devonian of Washington, Ore·gon, and Western British Columbia. In·
ternat. Dev. Symp. 1967, Calgary, pp. 827842.
(1970): Carboniferous System of theWestern Cordillera of Southwestern Brit·
ish Columbia and Northwestern Washing·ton. Compte Rendu 6e Congres Internal.
Strat. Geol. Carbonif., Sheffield 1967, vol.
2, pp. 599-608.
DUNCAN, P.M. (1867): On the Genera Heter·
ophyllia, Battersbya, Palaecyclus, and As·
terosmilia: The anatomy of their species,
and their position in the classification of
the selerodermic Zoantharica. Phil. Trans.
R. Soc. London, vol. 157, pp. 643-651.
IGo, H. (1957): Fusulinids of Fukuji, south·
ern part of the Hida Massif, central Ja·
pan. Sci. Rep. Tokyo Kyoiku Daigaku, Ser.
C, vol. 5, no. 47, pp. 153-246.
KANMERA, K. (1952): The Lower Carboni·ferous Kakisako Formation of southern
Kyushu, with a description of some corals
and fusulinids. Mem. Fac. Sci. Kyushu
Univ., Ser. D, vol. 3, no. 4, pp. 157-177.
MERRIAM, C.W. (1942): Carboniferous andPermian corals from central Oregon. Jour.
Paleont., vol. 16, no. 3, pp. 372-381.
- - and BERTHIAUME, S.A. (1940): Late Pal·
eozoic history of central Oregon. Geol.
Soc. Am. Bull., vol. 51, no. 12, p. 1935.
- - and - - (1943): Late Paleozoic forma·tions of central Oregon. Ibid., vol. 54, pp.
145-172.
MINATO, M. (1955): Japanese Carboniferous
and Permian. corals. Jour. Fac. Sci. Hok·

159

kaido Univ., Ser. 4, vol. 9, no. 2, pp. 1-202.
PACKARD, E.L. (1928): A new section of Pal·
eozoic and Mesozoic rocks in central Oregon. Am. Jour. Sci., 5th Ser., vol. 15, pp.
221-224.
- - (1929): Discovery of the Baird Missis·
sippian fauna of central Oregon (Abstract). Geol. Soc. Am. Bull., vol. 40, p.
257.
- - (1932): A contribution to the Paleozoic
geology of central Oregon. Carnegie Inst.
Pub. 418, pp. 105-113.
ROSOVSKA Y A, S.E. (1963): The fossil types
of fusulinids and their ancestors. A/wd.
Nauk. USSR, Trady Paleont. Inst., Tome97, pp. 1-128.
SADA, K. (1964): Carboniferous and Lower
Permian fusulines of the Atetsu Limestone in West Japan. Jour. Sci. Hiroshima
Univ., Ser. C, vol. 4, no. 3, pp. 225-269.
- - (1967): Fusulinids of the Millerella Zoneof the Taishaku Limestone (Studies ofthe stratigraphy and microfossil faunasof the Carboniferous and Permian Taishaku Limestone in West Japan, No.1).
Trans. Proc. Paleon!. Soc. Japan, N.S., no.
67, pp. 139-147.
- - (1969): Microfossils of the lowest partof the Taishaku Limestone (Ditto, No.4).
Ibid., no. 75, pp. 119-129.
STUCKENBERG, A. (1904): Anthozoen und
Bryozoen des unteren Kohlenkalkes vonCentral-Russland. Mem. Com. Geol., nov.
Ser. 14, pp. 72-109.
YAI3E, H. and SUGIYAMA, T. (1939): Discoveryof Hexaphyllia in the Lower Carboniferous of Japan. Jour. Geol. Soc. Japan,
vol. 46, no. 552, pp. 85-88.
ZELLER, D.E.N. (1953): Endothyroid Foraminifera and ancestral fusulinids from thetype Chesteran (Upper Mississippian).
Jour. Paleont., vol. 27, no. 2, pp. 183-199.

160

Kimiyoshi SADA and Wilbert R. DANNER

Explanation of Plate 24
Figs. 1-2. Hexaphyllia sp.
1-2. Transverse sections: Rg. No. CF -C-2 (x 82) and CF -C-101 (x 67), respectively
Section (Fig. 2) includes a small bubble at the center of corallum.
Fig. 3. Photomicrograph of oolitic limestone.
Locality DS2 in Suplee area, central Oregon.
Eostaffella, Endothyra and other foraminifera. x 20.
Fig. 4. Photomicrograph of organoclastic limestone.
Locality DS1 in Suplee area, central Oregon.
Eostaffella, Endothyra, other foraminifera and shell fragments. x 20.

SA DA and D ANNER :3

4

Eostaffe lla and Hexaphyllia From Oregon

Plate 24

161

PROCEEDINGS OF THE PALAEONTOLOGICAL SOCIETY
OF JAPAN

1':1 *i!i1=.~;,*;~ 111 @1f7JJ~I;J: 1973 ~ 6 fJ 23 rI(±) Icw.rri'\\'\*~f:~f~j~MfIIK..tJv'-CIJf.Ift1\~;f1-t-: (~1mii' 48 ~I) "1 t-:'!{! 24 fl (II) IC l;J:ijt.I"JJ II (Liv ,0);:n:='*cffi tJ: C? V'(C ftTij)Pl!!0);lli+~7.I~fiN"Lt-: (~rl'l fl' i'f!: rn %:fj'O "0

Late Scythian Ammonoids from the Kitakami Massif. ......................... .
.......... BAN DO, Y. and SHIMOYAl\IA, S.
An Upper Triassic Nautiloid from Okinawa·jima .................... ISIIlBASH!, T.
TH7U'I'1 [iLl); 1-;:g:ifr;:7:/-'C T -1 "IC '?v'-C ......

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Palynological Study on 200 meters Core
Sample of Lake Biwa in Central Japan.................................. FUJI, N.

J:l!!T" ~ }jfj±r:jl0)1tl/l'i;1t:t:iIC,?v'-C ......... .
· . . . . . . . . . . . . . . . . . . . . . . . lilt 113 %:f.iL • lLi!llf # fIj~
M.m~~MK_WT~~~~M~D (~M®
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Comptoniphyl-............. : ...... tl~~*~11

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· ............. JIHP.r,0..ifl • IJ,jl!!fijj(~ • i4!in i~
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· ....................... flHIUIM~ • II'il!!".&j.~?t -1 1]1_ Tff~ =-I,/:* '" I 1::/ I· 1t71lc '? ~ '-C(ttll?\:) ... · ........................ ~~I!II0..~-O)~ AUf. :I!ltTff11 :t:iiJR*Jirr 0) -If:/ ",' ft:t:iMif;c(ttm"C) ..... ·· ..................... ~~;0..~IIH, -Nlt.7j.~:t:iEk1t0)3.lt~tff .............................. Jliijrt ffi:zll);**0mUpper Cretaceous pelecypods from theHimenoura Group, Kyushu, Japan. Part
2, Orders Solemyoida, Mytiloida, Pterioida and Trigonioida. Part 3, Orders
Veneroida and Myoida ...... TASHIRO, M.
Inoceramus hobetsensis !C.7j.~:n ~ mT-tta"J~~fC'?v'-C ........................ !IlflIl~Z~1=*ci1iJJJ!l{t:t:i Astriclypeus ~Echinodiscus
O)*~JW"H*······················· ·~T r'fil
Molluscan Fossils from the Miocene Eoil
Formation, Gampo District, Southeastside of the Korean Peninsula, Korea ..
KIM, Bong Kyun, YOON, Sun & NODA, H.

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................................. ·mllJl!aJj~

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~1t:t:i ~ O)f:YJf*· ................. Jliij:Hffi:zll);

Biostratigraphical study of the Toyama
Formation in the Kitakami Massif,
Northeast Japan ..................... .
.......... MURATA, M. & SI-lIMOYAMA, S.
Ty,m~~t.l:LLJ!t!!ICmUH c~ 2 l'llO) Permundaria(Brachiopoda) IC'?v'-C .......... ilIIJU,iflReport of Lower Trias from Pir Panjal,near Qazigund, Kashmir, India, with
Description of a few Ammonoids ..... .
............ KAPOOR, H.M. & BAN DO, Y.

~:/~~ryA rJ!i1=.!f7I.1~i!iVi{JQJ:t:iiJR· =1]1:*2. Bryozoa 0) zoarium O)~i'&.~:fi)J03'O) fi'tnJtf& ~ O)llIiH*· .il1ii!llf {~. ffi:~)lI~n
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162

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Transactions and Proceedings of the PalaeontologicalSociety of Japan

New Series No. 91

September 20, 1973

CONTENTS
TRANSACTIONS
620. SAITO, Tsunemasa and MAIY A, Seijuro : Planktonic Foraminifera of the
Nishikurosawa Formation, Northeast Honshu, Japan .................. 113
621.

KOIZUMI, ltaru: Marine diatom flora of the Pliocene Tatsunokuchi Formation in Miyagi Prefecture. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. 126

622.

UJlIE, Hiroshi and ICHIKURA, Masaki:

Holocene to uppermost Pleistocene

planktonic foraminifers in a piston core from off San'in district, Sea
of Japan ... .... ..... ... .. .. . . ......... . . ....... . ... . . .... . .. . ... .. . . .. 137
623. SADA, Kimiyoshi and DANNER, Wilbert R.: Late Lower Carboniferous
Eostaffella and Hexaphyllia from central Oregon, U. S. A. ...... .... .. 151
PROCEEDINGS ............... . .. .. ............. . . . .... .. ... . . . ..... . . . . . ...... 161