Transactions and Proceedingsof thePalaeontological Society of Japan
New Series

No. 82Palaeontological Society of Japan
June 30, 1971

Editor : Takashi HAMADA
Associate editor:

Yasuhide IWASAKI

Officers for 1971 - 1972
President:

Tokio SHIKAMA

Councillors (*Executives):

Kiyoshi AsANO*, Kiyotaka CHINZEI*, Takashi HAMADA*,

Tetsuro HANAI*, Kotora HATAI, Itaru HAYAMI, Koichiro IcHIKAWA, Taro
KANAYA, Kametoshi KANMERA, Tamio KOTAKA, Tatsuro MATSUMOTO*, Hiroshi
OzAKI*, Tokio SHIKAMA*, Fuyuji TAKAI*, Yokichi TAKAYANAGISecretaries : W ataru HASHIMOTO, Saburo KANNOExecutive Committee
General Affairs: Tetsuro HANAI, Naoaki AOKIMembership: Kiyotaka CHINZEI, Toshio KOIKE
Finance: Fuyuji T AKAI, Hisayoshi !GoPlanning:

Hiroshi OZAKI, Kazuo ASAMA

Publications
Transactions:
Special Papers:

Takashi HAMADA, Y asuhide IWASAKI
Tatsuro MATSUMOTO, Tomowo OzAwA" Fossils" : Kiyoshi ASANO, Toshiaki TAKAYAMA

All communications relating to this journal should be addressed to the
PALAEONTOLOGICAL SOCIETY OF JAPANcjo Geological Institute, Faculty of Science, University of Tokyo, Tokyo 113, Japan

Sole agent: University of Tokyo Press, Bongo, Tokyo

Trans . Proc . P a laeont. Soc. J a pa n, N . S., No. 82, pp. 61- 72, pi s . 8, 9, Jun e 30, 1971

578.

ONTOGEN IES OF TWO UPP E R CAMBRIAN TRILOBITESFROM NORTHERN BLACK HILLS, SOUTH DAKOTA':'CHU NG-HU NG I-IU ** and LI-LI N TA N
De partme nt o f Biol ogy, Na nya ng U ni ve rs ity , S in gapore

Wi f,l=z !J Black Hill s ;1Uti1Pf 0) 7J './7' ~ 7fc1~ lU r=: ·~~ ~~ 2 1> u O) fl/iii*9E~I=. : flJ; h elasp?:swalcolli RE SS I~ R t<> J:: V' Glaf;hyrasJ;is j;ar va ( W ALCO T T) O) )E ~I=_j@flj\i,>_: lilfy'[; l t-.:fr~~L
Jlj; h elas j; is wal co ll i O)Y,!Jolt ft f l. subcl-i l us , PanL bolinoi des co nl rac l u.s , P. m ous lo nu.s,
D underb urgia ? any la 1<> J:: V' Ol e'nus gibbo sus O) y)J!:LU: JJjfJ.). l , "*. t-.: Glaj;hy ra sf; is p ar v a
R: -?v' 'L ft W ell era sj;is lata , W . swarlz i, W. lo chman ae 1.> J: V' P emphigaspi s bu.llata
O) li:JJ EJH;:: ~Jif.JJ-9 ;o:::c. n~'FU -:d-.:. ;:: 0)::: c vt J:-. ~~=Mt O):=:::m 1t n ; clt. ·c':!c ~1t.:iL. L.t-.: H~Wir!X7

i'ifl :J;. ·1'[ -lgR :l<IT :Efi-g-{,1/:,0)l:·0:o:::c~ /1*7f; L..'Lv':0 .

(WALCOTT), CheilocejJ/wlu s sp., and inarticulate brachiopods specimens.
Preparation of the co llection by thesenior author yielded over 266 cranidia,
70 pyg idia, 97 librigenae, 6 h ypostomata,and 201 immature forms of Aphela sjYis
wa lcott i ; 76 cranidia, 41 pygidia, 32
librige nae, 6 hy postomata, and 49 immature forms of ClajJh yraspis jJarva(WALCOTT) ; 6 rather poorly preserved
f ragments of CheilocejJ/wlus sp., and alarger numbers of inartic ul ate brachiopods. Because the material was collectedfrom the same limited position and horizon , it is believed that each of the genera is represented by a single species
within ·which intraspecific variation may
be observed.
Two trilobites are described here:
A jJhelasjJi s walcotti and Claphy1·aspis
jJarva. They are interpreted as the sameeco log ical habitants, and the morphologic
variations within a single population are
possib ly sex ual as in so many recent
arthropods; there are distinctive differe nces between the male and the fema leforms. The male individuals are !J1Qre

Introduction
In th e summer of 1962 the seniorauthor, Dr. Christina LOCHMAN-B ALK,
and a few students of the De partmentof Geology, New Mexico Institute of
Minin g a nd Techno logy , had a Summer
Field Camp around the Black Hills, South
Dakota, to stud y the Cambrian stratigraphy and paleontology. A mon g thevarious co llections, a small samp le wasobtained from about half wa y to the topof the Moll section, Bear Butte, southeastern Deadwood City, northern Black
Hills.
The material weighs approximately 5 kgs. , and is of light gra y color.
It is a fine to medium crystalline limestone, filling w ith a few small intraformational pebbles and abundant of disarticulated trilobite fragments . It is very
fossiliferous and contains AjJhela sjJis
walcotti RESSER, ClajJhyrasjJis parva* Receive d Jul y '1, 1970 ; r ea d Sept. 12,1970 a t Na t !. Sci. Mus. , Tok yo.
• • P rese nt adr ess: E arth Scien ce Depar t me nt , Che ng K un g U ni ve rs it y , Tain a n, T a iwa n, R e publi c of C hina .
61

62Chnng-I-h mg Hu and Li-Lin TAN

abundant than th e female and often
possess a small body size. The ontogenetic separation and the sex ual recognition are based on the schemes in thesenior author works (Hu, 1968a, b).
The senior author wishes to express
his thanks to Dr. K. E. CASTER, University of Cincinnati, Ohio for his super vision. Thanks also go to Drs. Christina
LOCI-! MAN -B ALK , New Mex ico Instituteof Minin g and Technology, New Mexico
for her fi eld g uidance, and D. S. ]OHNSO 1 ,University of Singapore, for kindl y reading over the present manuscript.
All of the figured specimens are stored
in the Geology Museum of Cincinnati,
Ohio (U. C. M.).

Systematic Paleontology

Famil y Pterocephaliidae
KOB AY ASHI, 1935
Genus Aphelaspis RESSER, 1936

A /Jh elaspis walcotti RESSER
Pl. 8, fi g s . 1- 36; Pl. 9, fi gs _ 34- 36 ;. t ex t :fi g s. 1A - N

A pheLasjJis wa lcoll i R Ess ER , 1938, p. 59, pl.
13, 14; P ALMER, 195'1, p. 746, pl. 86, fi gs.
2, '1- 8; S HAW, 1956, p. 51 , pl. 3, fi g s. 1- 6;
P ALMER, 1962, p. 33, pl. 4, fi g s. 24, 28, 33;
R ASETT I, 1965, p. 76, pl. 18, fi g s. 10- 20.
Aphelaspis simulans R ESSER , 1938, p . 59, pl.
13, fi g s. 19- 21.
A phela spis minor R AS ETT I, 1962, p. 89, pl.
19, fi gs. 18- 25.
Aph elaspis tran sversa R ASETTI , 1962, p. 88,
pl. 16, figs . 21- 27.

R emar!z s : The present species is represented by a few hundreds of bothmature and immature specimens which
permitted a detailed study of individual
variati"on and of morphogenesis during
their ontogenetic developmental stages.

Accordin g to th e cranidia and pygidia,
the adult forms can be segregated intot wo clear different g roups which separate from each other in a single distinct
featur e. One g roup is characterized b y
a less relieved cranidium, shallow axial
and frontal furrows, weakly convex glabella, preglabellar field moderately slop ing downward and somewhat convex,
anterior border flat , librigena with ocular
platform broad and of low convexity,
and the short genal spine rather rapidl ytapered ; pygidi um ovate-transverse andwith the posterior margin bending slightly inward. The other group is characterized by a hi ghly relieved cranidium,
deeper axial and frontal furrows, strongly convex glabella, preglabellar field andanterior border more convex, fi x igena
convex and directed upward, librigena
with ocular platform narrow and of
hi gh convexit y, and the lon g genal spine
gently tapered ; pygidium semicirculartransverse a nd without posterior marginal border notch.
It is postulated that these slight but
consistent diffe rences in the adult exoskeletons are the expressions of sexual
dimorphism. The first g roup is tentati vely r egarded as the female form andthe second as th e male form. The sex ual
ratio of the present species is about 182.
The largest female cranidium is about
1.2 em in leng th (sag.), that of the maleis 1.0 em (sag.) only.
Careful examination of both female
and male groups indicates that thelength of the male glabella is statistically shorter than that of female andtapers shortl y, however these features
are by no means constant (compare pl.
8, figs. 30, 33 to 32, 36) and some mal es
may show both longer and nearl y subquadrate glabella resembling those of
the female. The distinct character between the fem a le and the male forms

578.

Ontogenies of two Upper Cambrian Trilobitesis that the male cranidium always possesses deeper dorsal furrows (compare
pl. 9, figs. 35 to 34, 36) than the female,and that of female is shallower.
The species Aphelaspis transversa,
Aphelaspis minor reported by RASETTI(1965) from Tennessee, and Aphelaspis
walcotti illustrated by SHAw (1956) from
Wyoming, possessing the deeper dorsal
furrows and shorter glabella are synonymized as the male form of the present
species. Aphelaspis buttsi (KOBA YASH!)
and Aphelaspis lata RASETTI reported
by RASETTI from Tennessee present
similar structure as those found in
Aphelaspis walcotti and presumably belong to a single species, the morphological differences being sexual.
The ontogenetic development of thepresent species is similar to that of
Aphelaspis subditus PALMER (Hu, 1969)
and Aphelaspis sp. (PALMER, 1962), except that the present species shows theanaprotaspid shield consisting of four
axial segments; this is the earliest larva
known. The metaprotaspid shield shows
faintly impressed cephalic segmental
furrows on the fixigenal area ; both ofthese features are well conformed withmany other species as reported by theauthor (Hu, 1968a, b) and STq)RMER (1942).

Aphelaspis walcotti RESSER, ontogeny
Anaprotaspid stage (Pl. 8, fig. 1, andtext-fig. lA). The shield is round, convex, about 0.25-0.28 mm in length (sag.).
The axial lobe is well defined by dorsal
furrows, narrowly cylindrical, and divided into four indistinct rings; the anterior lobe or the first axial ring is broadand expanding forward, and the following three are narrower and of uniform
width. The pleural lobe is convex andabout twice as wide as the axis (tr.).
The distinctly impressed anterior pits

are situated on the sides of the frontal
lobe. Short paired supercilioid ridges
extend postero-laterally from the sidesof the frontal lobe. The surface is covered with fine granules. A narrow
but well defined border surrounds theshield margin, and a longitudinal fissure
is faintly impressed along the central
axis.
The present stage is represented byonly one specimen which is low convex,
and in which the axial lobe and rings
are indistinctly marked compared withthose of the later stages. This phenomenon may indicate that the skeleton
is thin and has low hardness at thisstage, and so is deformed due to thecompaction of the sediments.
Metaprotaspid stage (Pl. 8, figs. 2, 3 andtext-fig. lB). The shield is round inoutline, convex, about 0.29-0.32 mm long(sag.). The axial lobe is slenderly cylindrical and divided into five axial rings
by well defined dorsal and ring furrows ;the first ring or the frontal lobe is roundand convex, and a pair of short supercilioid ridges extending laterally from thesides ; the second to fourth axial rings
are of about the same size, convex, andmarks with faint fissure along the central axis ; the last or the occipital ringis smaller than the previous one, which
is round and located on the posterior
margin of the shield. The pleural lobe
is convex, about twice as wide as theaxis (tr.). The surface of the shield iscovered by medium sized granules. A
pair of deeply marked pits is situatedon the sides of the frontal lobe, and thepleural lobe is faintly impressed by twoor three pairs of postero-laterally directed furrows.
The present stage differs from theprevious one is that the axial lobe has
five axial rings.
Paraprotaspid stage (Pl. 8, figs. 4-8 andChung-Hung Hu and Li-Lin TAN

64

A

c

B

D

H

G

F

E

J

K

L

N

Text-figure 1. A growth sequence of Aphelaspis walcotti REssER. A, Anaprotaspis,x 45; B, Metaprotaspis, x 45; C, D, Paraprotaspides, x 50; H, G, Early meraspides,
x 40, x 35; F, E, Late meraspides, x 30, x 20; I, A "male" pygidium, x 4; J, A "female"pygidium, x 4; L, M, A "male" cranidium and a librigena, x 4, x 3; K, N, A "female"cranidium and a librigena, x 4, x 5. (all drawings were made from photographs.)578.

Ontogenies of two Upper Cambrian Trilobites

text-figs. lC, D). The shield is roundedor subcircular in outline, convex, about
0.32-0.40 mm in length (sag.). The glabella is divided by rather deeply impressed ring furrows into a large frontal
lobe, three uniform glabellar segments,
and a small occipital ring. The frontal
pits are distinct and triangular. The
palpebral lobe is narrow, well delimited
by a furrow, and continuous with thepalpebral ridge towards the posterior
lateral margin of the frontal lobe. The
fixigena is about one and a half as wide
as the glabella, convex, and with thenarrow posterior border well delimited
by a border furrow. The posteriorborder curves slightly postero-laterally
and continues into a short and broad
fixigenal spine directed backward. The
protopygidium is lenti-form, convex,
sloping downward steeply behind of the
cranidial shield. One or two segments
are visible. The axial ring is ovaltransverse and convex above the pleurallobe. The pleural lobe is low and has
single interpleural groove. The surface
is covered by medium sized granules.
The main characters of the present
stage are that the protopygidium appears, the fixigena becomes narrower,
and the central axial fissure is absent.
Early ·meraspid stage (Pl. 8, figs. 9-13
and text-figs. lH, G). The cranidium isregularly trapezoidal in outline, convex
and about 0.45 to 0.60 mm in length(sag.). The glabella is nearly cylindricalbut expanding slightly forward. It is
divided into four convex segments; thefirst glabellar segment is the largest,
convex, and marked with a pair oflateral pits at the margin ; the second
to fourth are equal in size. The occipital ring is narrower than those of theglabellar segments, convex, and with aminute median nodule. There is a narrow, forwardly arched anterior border65

appears in front of the glabella. The
convex fixigena is about the same width
as the glabella (mid-line, tr.), with thenarrow and well elevated palpebral lobe
situated in front of the mid-length of
the glabella. The palpebral ridge iselevated, curving continuously from thepalpebral lobe and directed to the sidesof the first glabellar segment. The
posterior fixigenal furrow is distinctly
impressed, horizontal and curving for-·ward before ending at the extreme
lateral border.
The anterior facial
suture is short and convergent-convex,
and the posterior one is broadly divergent-convex. The surface is covered bymedium sized granules.
The distinct characters of the present
stage are that the cranidium is trapezoidal in outline, the glabella and the
fixigena are about the same width (tr.),and the anterior border has appeared.
Late meraspid stage (Pl. 8, figs. 14-18,
20 and text-figs. lE, F). The cranidium
is trapezoidal, convex, about 0.80-1.6 mm
in length (sag.). The glabella is cylindrical or slightly tapering forward, convex, divided into four segments by incomplete or complete glabellar furrows.
The occipital ring is crescentic, convex
both vertically and posteriorly, andbearing a tiny median tubercle. A narrow preglabellar field appears in between the glabella and the anteriorborder, and is flat to slightly convex.
The anterior border is convex, arches
slightly forward and is well delimited
by a frontal furrow. The fixigena isnarrower than the glabella, horizontallyconvex or slightly sloping upward. The
palpebral lobe is sickle-shaped, convex,
well demarked by a palpebral furrow,and its anterior end is continued by thenarrow and well elevated palpebra.! ridge.
The anterior facial suture is slightly
divergent-convex, whereas the posterior

66

Chung-Hung Hu and Li-Lin TAN

facial suture is divergent and straight.
The surface of the exoskeleton is faintly granulated.
The present stage is distinguishedfrom the previous one in having theglabella parallel sided or slightly tapering forward; the glabellar furrow complete ; fixigena narrower than the glabella ; the palpebral lobe sickle-shaped
and situated on the mid-line of theglabella (tr.), and the posterior fixigena
is greatly reduced in width (sag.).
Remarks: The morphologic changesof the present species during its ontogenetic development very closely resemble those of Aphelaspis sp. (PALMER,
1962), APhelaspis subditus PALMER (Hu,1969), Dunderburgia ? anyta (HALL &WHITEFIELD) (Hu, 1968a). Parabolinoides
contractus FREDERICKSON (HU, 1969), andParabolinoides nwustonus Hu (Hu, 1970)..
The similarities suggest that thesegenera form an allied group perhaps
are family level?
Figured spzcimens:
Anaprotaspis,
U. C. M. 40309; Metaprotaspides, U. C. M.
40309a-b;Paraprotaspides, U. C. M.
40309c-g;
Early meraspides, U. C. M.
40309h-l ;Late meraspides, U. C. M.
40309m-q, s; Immature pygidium, U.C.M.
40309u; Hypostoma, U. C. M. 40309t.
Female form: Cranidia, U.C.M. 40309d',h', i' ; Pygidia, U. C. M. 40309v, y, a';Librigena, U. C. M. 40309g'.
Male form: Cranidia, U. C. M. 40309r,
z, b', c', e', j', k'; Pygidia, U. C. M.
40309w, x; Librigena, U. C. M. 40309f'.
Family Lochocephalidae HuP£, 1953
Genus Glaphyraspis RESSER, 1937
Glaphyraspis parva (WALCOTT)
Pl. 9, figs. 1-33 and text-figs. 2A-O
Liostracus parva WALCOTT, 1899, p. 463, pl.

65, fig. 6.
Glaphyraspis parva (WALCOTT), RESSER,
1937, p. 12; LocHMAN & Hu, 1962, p. 438,
pl. 68, figs. 7-52; RASETTI, 1965, p. 40,
pl. 10, figs. 9-17.
Raaschella ornata LoCIIMAN, 1938, p. 82, pl.
18, figs. 6-10; PALMER, 1954, p. 767, pl.
98, figs. 7-9.
Raaschella occiden.talis LocHMAN, in LocHMAN & DUNCAN, 1944, p. 43-44, pl. 4,
figs. 1-5.
Glaphyraspis omata (LocHMAN), RAsETTI,
1961, p. 1.12; PALMER, 1962, p. 93, pl. 19,
figs. 15-19, 26, 27 and text-fig. 2C, and1965, p. 51, pl. 7, figs. 15-17, 20-22;
RASETTI, 1965, p. 41, pl. 10, fig. 8, andpl. 11, figs. 13, 14.
Glaphyraspis ode1·i RASETTI, 1965, p. 41, pl.
10, figs. 18-22.

Remarks: The material from the Moll
section consists of about 250 mature-and
immature specimens. The specimens
are interpreted as representing the disarticulated moults of a single population of Glaphyraspis parva which werenormally the habitants of the area during the early Aphelaspis zone period.
The smallest immature is about 0.22 mm
and the largest adult 1.8 mm in length(sag.), and the series forms a very continuous growth sequence between theselimits.
A detailed comparison of the specimens of this population reveals thattwo kinds of intraspecific variant canbe recognized in the cranidia, librigenae,
and pygidia. One group is characterized
by a shorter nearly subtrapezoidal glabella, broader ocular platform, and having the rounded pygidium well marked
by larger pleural nodes; the other groupby a slightly rectangular-oblongus glabella, narrow ocular platform, and having the pygidial margin without distinct
node. These morphologic variations
again possibly represent the sexual differences within the same species popula-578.

Ontogenies of two UppeT CambTian TTilobites

A

B

E

F

c

0

H

G

J

K

N

67

L

0

Text-ftgure 2. A growth series of Glaphyraspis parva (WALCOTT). A, Anaprotaspis,
x 60; B, C, Dorsal and lateral views of a metaprotaspis, x 60; D, E, Two paraprotaspides, x 60, x 55; F, An early meraspis, x 35; G, H, Two late meraspides, x 25, x 20;
I, M, A male and a female Iibrigenae, x 20; J, N, A male and a female pygidia, x 14,
x 20; K, Hypostoma, x 14; L, 0, A female and a male cranidia, x 12, xI l. (all drawings were prepared by tracing the outline from photographs.)

68

Chung-Hung Hu and Li-Lin TAN

tion, as seen in Aphelaspis walcotti. The
first group is tentatively designated as
the male form and the second as thefemale. The sex ratio is 123.
It seems that the ornamentations offine to coarse granules, and the occipital
median tubercle, present on the dorsal
surface of the exoskeleton may have no
actual specific significance since within
the same population these features may
or may not preserved and are veryvariable. They thus appear to be individual variations.
The species Glaphyraspis oderi reported by RASETTI (1965) from Tennessee, G.
ornata by PALMER (1965, pl. 7, figs. 16, 17
only) from Nevada and G. occidentalis
by LOCHMAN & DUNCAN (1944) fromMontana all possessing elongate glabella
are possibly the female form of G.
parva, whereas those of G. parva by
WALCOTT (1899) from Yellowstone Park,
G. ornata by RASETTI (1965) from Tennessee, by LaCHMAN (1938) from Texas,
and PALMER (1965, pl. 7, figs. 15, 20-22)
from Nevada all having the shorter
trapezoidal glabella are presumably themale form. Those cranidia illustrated
by SHAW (1956), RASETTI (1965, pi. 10,
figs. 9-16 & 1961, p1.22, figs. 14-17),and· LOCHMAN & Hu (1960, pl. 97, figs. 1-8)
with nearly parallel sided glabella do .
not belong to this species.

Glaphyraspis parva (WALCOTT),

ontogeny
Anaprotaspid stage (Pl. 9, fig. 1 andtext-fig. 2A).-The shield is about 0.200.22 mm in length (sag.), moderately
convex, and with no clear dorsal furrows. The axial lobe is slightly elevatedand with a round node at both the anterior and posterior ends.
In the present stage the specimen!>surface shows no any distinct characters,
except for a pair of elevated nodes at
the anterior and posterior margins,which suggest the orientation of theshield. The specimen is presumably as
early larva of this species before themetaprotaspid stage, and the distinctive
characters arise later in ontogeny. It
is the earliest and the smallest specimen
which has been recovered from the material, the specimen been also slightly
deformed and possibly indicates that theskeleton was thin and not well hardenedin this stage.
Metaprotaspid stage (Pl. 9, figs. 2, 3
and text-figs. 2B, C).-The shield is subcircular, convex, with well differentiatedaxial and pleural lobes, and about 0.23
to 0.28 mm in length (sag.). The axial
lobe extends the full length of the shield,
expands slightly anterioly, and is indistinctly divided into five convex segments. The pleural lobes are convex,
swelling laterally along the margin, andof about the same width as the axial
lobe. The anterior pits are indistinctly
impressed, a pair of superciliary eyebrow ridges extends posterolaterally
from the sides of the first axial segment-the frontal lobe.
The present stage differs from theprevious one in having the axis and thepleural lobes well differentiated, andthe axis divided into five convex segments. The stage can presumably becorrelated to the stage assigned by
PALMER (1962, p. 93) to the anaprotaspid
stage.
Paraprotaspid stage (Pl. 9, figs. 4-8
and text-figs. 2D, E).-The shield isconvex, about 0.30-0.35 mm long, subcircular and divided into cephalic andprotopygidial shields by a distinct suture. The cephalic shield is trapezoidal
in outline, convex, and ·well differentiated into axial and pleural lobes by57 8.

Ontogenies of two Upper ·Cambrian Trilobites

distinct dorsal furrows. The axial lobe
is expanded forward from the small
occipital ring, divided into four unequal
segments ; the anterior segment being
the largest. The fixigena is about thesame width as the axis and convex
along the lateral margin. A pair ofindistinct anterior pits is impressedon the sides of the first glabellar segment. The narrow supercilioid ridges
run postero-laterally from the sides ofthe frontal lobe along the anterior fixigenal border. The posterior fixigenal
border is deeply separated by a borderfurrow; it is narrow and curves posteriorly at the extreme lateral end. The
protopygidium slopes steeply downward
from the posterior cephalic margin. It
is presumably lenti-form and consists of
one or two segments.
The· present stage is equivalent to
PALMER's (1962) metaprotaspid and earlymeraspid stages, and it is mainly characterized by the presence of the protopygidium and broadened posterior fixigenal border, but no anterior border has
yet appeared.
Early mer.aspid stage (Pl. 9, figs. 9-12,
20 and text-fig. 2F).- The cranidium istrapezoidal in outline, convex, about
0.40 mm in length (sag.). The glabella
is regularly oblong with parallel sides,
convex, and divided into four transverse
segments. The glabellar furrows are
all shallow across the central axis anddeepen laterally. A pair of faint pits
impressed on the sides of the first glabellar segment. The occipital ring is
deeply separated by an occipital furrow,is convex posteriorly, and bears a minutemedian node. The anterior border isnarrow, distinctly marked by a frontal
furrow, and arched forward. The fixigena is about the same width as theglabella on the mid-line (tr.), convex.
The narrow palpebral lobe located late-69

rally, and the palpebral ridge is elevated,running continuously from the anterior
end of the palpebral lobe direct to thesides of the first glabellar segment. The
posterior fixigenal furrow is broad anddeep, with the elevated marginal borderslightly wider than the occipital ring.
The anterior facial suture is very shortand convex, and the posterior one isbroadly divergent-convex.
The pygidium is semicircular in outline, convex, transverse, and consists of
4 or 5 disankylosed segments. The axis
is conical, tapers slightly posteriorly andis marked with distinctly convex axial
rings. The pleural lobe is flat or slightly convex along the inner marginalborder and is wider than the axis. The
pleural bands end with a pair of shortbroad spines. The skeletal surface iscovered by dense granules, and a pairof large nodes is on the lateral ends ofeach pygidial segment.
The present stage is characterized by
the oblong glabella, narrow anteriorborder, and the disankylosed pygidial
segments.
Late meraspid stage (Pl. 9, figs. 13, 17,
21, 27, 28 and text-figs. 2G, H).-The
cranidium is rectangular in outline, convex, about 0.50 to 0.70 mm in length(sag.). The glabella is cylindrical but
tapering forward, and with a rounded
anterior margin. The glabellar furrows
are complete but the anterior one isshallower than the next. The occipitalring is crescentic convex, and well delimited by the occipital furrow, andmarked with a minute median granule.
A narrow preglabellar field appears infront of the glabella ; it is flat or slightly depressed. The anterior border isnarrower than the preglabellar field,
gently convex, arching slightly forward,
and with the median notch directed to
the glabella. The fixigena is narrower

70

Chung-Hung Hu and Li-Lin TAN

than the width of the glabella between the palpebral lobes (tr.), convex,
and the narrow small palpebral lobe islocated in front of the mid-line of theglabella (tr.) ; its end is continuous withthe well-elevated palpebral ridge forward to the anterior glabella. The posterior fixigena is rather broadly convex,
and has the posterior border about thesame length as the occipital ring (tr.).
The librigena has generally the same
form as that of the adult but slightly
narrower and the free margin curves
gently. The pygidium is subtriangularin outline, and has no marginal spine.
All of the exoskeleton is covered byfine or medium-sized granules, andparallel ridges are marked along theanterior cephalic border.
The present stage is differentiatedfrom the preceding one in having theglabella conical ; a preglabellar field;
fixigena narrower ; and subtriangularpygidium. It is differentiated from theholaspis by the slender glabella; by thefrontal furrow absence of the mediannotch; and the transverse-triangularpygidium.
Remarl<s: PALMER (1962) reported a
growth series of Glaphyraspis "ornata"from Nevada. The skeletons are beautifully preserved and silicified, showing

Explanation of Plate 8
Aphelaspis walcotti RESSER
Fig. 1. Anaprotaspid shield, showing four axial segments, x 45, U. C. M. 40309.
Figs. 2, 3. Two metaprotaspides, showing five axial segments and a longitudinal fissure
along the central axis, x 45, U. C. M. 40309a; x 45, U. C. M. 40309b.
Figs. 4-8. Five paraprotaspid shields, showing the appearence of the protopygidia, 4,x50, U.C.M. 40309c; 5, x50, U.C.M. 40309d; 6, x50, U.C.M. 40309e; 7, x50,
u. c. M. 40309f; 8, X 45, u. c. M. 40309g.
Figs. 9-13. Five early meraspid cranidia, showing the presence of the anterior border, 9,x35, U.C.M. 40309h; 10, x30, U.C.M. 40309i; 11, x40, U.C.M. 40309j; 12, x25,
u. c. M. 40309k; 13, X 30, u. c. M. 403091.
Figs. 14-18, 20. Six late meraspid cranidia, showing the .presence of the preglabellar
field, 14, x30, U.C.M. 40309m; 15, x25, U.C.M. 40309n; 16, x20, 40309o; 17, x17,
U. C. M. 40309p; 18, x 14, U. C. M. 40309g; 20, x 10, U. C. M. 40309s.
Figs. 19, 29, 30, 33. Top views of a few male cranidia, 19, x 4.5, U. C. M. 40309r; 29,
x 3.3, U. C. M. 40309b'; 30, x 3.5, U. C. M. 40309c'; 33, x 4, U. C. M. 40309e'.
Fig. 21. A complete hypostoma, x 8, U. C. M. 40309t.
Fig. 22. An immature pygidium, showing the disankylosed thoracic segments, x 20,
U. C. M. 40309u.
Figs. 23, 26, 28. Three female pygidia, showing the rounded posterior marginal border,
x 23, x 6, U. C. M. 40309v; 26, x 3, U. C. M. 40309y; 28, x 4, U. C. M. 40309a'.
Figs. 24, 25. Two male pygidia, x 7, U. C. M. 40309w; x 4, U. C. M. 40309x.
Fig: 27. Front view of a male cranidium, showing the deep dorsal furrow, x 4, U. C. M.
40309z.
Figs. 31, 32. Front and top views of a nearly complete female cranidium, showing theshallow dorsal furrow, x 3, U. C. M. 40309d'.
Fig. 34. A male librigena, showing the narrow ocular platform, x 3, U. C. M. 40309f'.
Fig. 35. A female librigena, x 5, U. C. M. 40309g'.
Fig. 36. A nearly complete female cranidium, showing the subquadrate glabella, x 3,
U. C. M. 40309h'.

Hu & TAN :Two Upper Cambrian Trilobites

2

Plate 8

3

5
6

10

11

12

9

13

33

7

14

21

19

20

8

34

35

15

16

18

17

36

57 8.

Ontogenies of two Upper Cambrian Trilobites

both ventral and dorsal well. The smallest shield "anaprotaspis" bears a pairof posterior fixigenal spines, and demonstrates the common structure held by
most of the trilobite larvae. It is unfortunate that PALMER gives only a
few figures ; more photographs would
possibly show the complete growth sequence and the adult variations.
The ontogenetic development of thepresent species is most closely similar
to that of the Welleraspis lata HOWELL(Hu, 1964), Welleraspis swartzi (TASCH),
Welleraspis lochmanae Hu, (Hu, 1969),
and Pemphigaspis bulla/a HULL (Hu,
1968b), indicating that these species are
phylogenetically closely related. HereRASETTI's (1959) taxonomic assignment(Family Lonchocephalidae) and PALMER's(1962, p. 95) interpretation are strongly
supported.
Figured specimens:
Anaprotaspis,
U. C. M. 40310; Metaprotaspides, U. C. M.
40310a-b;Paraprotaspis,
U. C. M.
40310c-g; Early meraspides, U. C. M.
40310h-k;Late meraspis, U. C. M.
403101; Immature librigena, U. C. M.
40310t; Hypostoma, U. C. M. 40310w.
Female form:
Cranidia, U. C. M.
40310m, n, q, b', f'; Pygidia, U. C. M.
40310c', d'; Librigena, U. C. M. 40310r.
Male form: Cranidia, U. C. M. 40310o,u, x, e'; Pygidia, U. C. M. 40310s, y, z,a'; Librigena, U. C. M. 40310v.
References
Hu, C. H. (1964): The ontogeny and dimorphism of Welleraspis lata HowELL (Trilobita). jour. Paleont. vol. 38 p. 95-97.
-.- (1968a) : Ontogeny and sexual dimorphism of Lower Paleozoic Trilobita;
Unpublished Ph. D. dissertation, Univ.
of Cincinnati, Ohio (accepted for Paleontogr. Amer.).
(1968b) : Notes on the ontogeny and71

sexual dimorphism of Upper Cambriantrilobites of the Welleraspis faunule from
Pennsylvania. jour. Nanyang Univ., vol.
2, p. 321-357.
(1.969) : Ontogeny and sexual dimorphism of three Upper· Cambrian trilobites. jbid., vol. 3, p. 438-462.
- - (1970) : Ontogenies and sexual dimorphisms of two Upper Cambrian trilobites.
Proc. Ceo!. Soc. China, no. 13, p. 143155.
LacHMAN, Ch. (1938):
Upper Cambrianfauna of the Cap Mountain formation of
Texas. jour. Paleont, vol. 12, p. 461-477.
- - & DuNCAN, D. (1944): Early Upper
Cambrian faunas of central Montana.
Geol. Soc. Amer., Spec. Paper., no. 54,
p. 43.
- - & Hu, C. H. (1960): Upper Cambrianfaunas from the Northwest Wind River
Mountains, Wyoming. Part I. jour.
Paleont., vol. 34, p. 793-834.
& - - (1962) : An Aphelaspis zone
faunule from Logan, Montana. Ibid.,
vol. 36, p. 431-441.
PALMER, A. R. (1954): The faunas of the
Riley formation in central Texas. Ibid.,
vol. 28, p. 709-780.
(1962) : Comparative ontogeny of some
Opisthoparian, Gonatoparian, and Proparian Upper Cambrian trilobites. Ibid.,
vol. 36, p. 87-96.
- - (1965) : Trilobites of the Late Cambrian pterocephallid biome in the GreatBasin, United States. Geol. Surv. Prof.
Paper, 493, 105p.
RASETTI, F., et al. (1959) : Treatise on Invertebrate Paleontology, part 0, Arthropoda 1. Geol. Soc. Amer. & Univ. Kansas. P. 279.
- - (1961.) : Dresbachian and Franconian
trilobites of the Conocochegue and Frederick limestone of the central Appalachians. jour. Paleont., vol. 35, p. 104124.
- - (1965): Upper Cambrian trilobite faunasof northeastern Tennessee. Smithson.
Mis. Coli., vol. 143, no. 3, 1.27 p.
SHAW, A. B. (1956): A Cambrian Aphelaspis
fauna from Steel Butte, near Boulder,72

Ch~~ng-H~mg

HU and Li-Lin TA N

Wyoming. j our. Pal eont ., vol. 30, p. 4852 .
ST¢'RMER, L. (1942) : Studies on t rilobi temorpholo gy Part II . The la r va l de velop-

ment , t he segmentation and the sutures,and their bearing on trilobite classification. No rsl< Geol. Tid sl<r., bd. 21, p. 49164, pls. 1, 2.

Exp lanation of Plate 9Giaphyrasj;is parva (WALCOTT)
F ig. 1. A s lightly de fo rmed anaprotaspid s hi eld, sho wing no di s tin ct a x ial segments,
X 60, u. c. M. L
10310.
F igs. 2, 3. Two meta protasp id s hi e ld s, s howing the we ll differe ntiated dors a l furrows
and axia l rin gs, x 60, U. C. M. 40310a; x 60, U. C. M. <10310b.
F igs. 4-8. Five paraprotaspid s hi eld s, s howing t he appearence of protopygidi um , 4, x 60,
U.C.M. 40310c; 5, x 50, U.C.M. 40310d ; 6, x 55, U.C.M. 40310e; 7, x'10, U.C. M .
40310g.
F igs. 9- 12. Four ea rl y me rasp id cra nidi a, no t ice the prese nce of the anterio r border, 9,x 35, U .C.M. 40310h; 10, x 35, U.C.M. 40310i ; 11, x 35, U.C.M . 40310i; 12, x 30,
U. C. M. 40310k.
F ig. 13. A la te me ra s pid cranidium , s howing the appea re nce of t he preg labe ll ar fie ld ,X 25, u. C. M. '103101.
F igs. 14, 15, 18, 29, 33. A few female cranidi a, s ho win g t he rect a ngu la r-oblon gus g la bell a,
14, x 20, U.C.M. 40310 m; 15, x 22, U.C.M. 40310n; 18, x 24, U . C.M. 40310q; 29,
X 15, u. c. M. 40<
U0b'; 33, X 12, u. c. M. <10310£'.
F igs . 16, 22, 25, 32. Fo ur m a le cranidia, sho win g th e trapezoida l g la bell a, 16, x 22, U. C. M .
40310o; 22, x 15, U. C. M. 40310u ; 25, x 20, U. C. M. 40310x; 32, x 11, U. C. M. 40310e'.
Figs. 17, 21. Two immature li brigenae, x 20, U. C. M. 40310p ; x 26, U. C. M. 40310t.
Fig. 19. A fema le li brigena, x 20, U. C. M. 40310 n.
F igs. 20, 26- 28. Four mal e pygidia, 20, x 30, U. C. M. '10310s; 26, x 14, U. C. M . '10310y; 27,
x 11, U. C. M. 40310z ; 28, x 30, U. C. M. '10310a' .
F ig. 23. A mal e libri ge na, x 20, U . C. M . 40310v.
F ig . 24. A h yposto ma, x 14, U. C. M . 40310w .
F igs. 30, 31. T wo fe male pyg idi a, s ho wing the smaller pleural granules, x 17, U. C. M .
40310c'; X 20, U. C. M. 40310d'.
Aph.elaspis wa/cotti R ESSER
F igs. 34, 36. T wo ma le cranidia, s ho w in g th e deepe r dor sal furrows a nd longer g labellae,
x 6, U.C. M. 40309j'; x 4, U.C.M. 40309k'.
F ig. 35. A fema le cra nidium , s ho w in g t he sha ll ow dorsal f urro ws, x 3.6, U. C. M. 40309i' .

Hu & TAN:

Two Upper Cambrian Trilobite sPlat e 9

1

3

2

4

10

15

6

9

8

7

11

17

;. ti

.1.. ---·

18

.

23
13

14

24

25

28
.; ,· ,k~ ·.·· .
r/""
r .-

.

•

.~
T'.:~.

, ·.

--.d."l·
~.

• •

.•

.I

32

31

29

30

33

34

35

36

Trans. Proc. Palaeont. Soc. Japan, N.S., No. 82, pp. 73-92, pis. 10-12, June 30, 1971

579.

SOME NEOGENE CHEILOSTOMATA (BRYOZOA)FROM OKINAWA-JIMA*TOMOKO HAY AMI
Institute of Geology and Paleontology, Faculty of Science,
Tohoku University, Sendai, Japan#k."l~GfJn' I?O)WJi'~=:~l"fl=l J:i'i C::. tt:l:t): t'Pk."lfi.~'.)O)::. tt!ltfi:TilJ::;l(t.:i\f!~-,~q-v-cv't.J:It 'n~.
-0-@ilitH~f\}.t:O)-c::.::. 1;:: nut;--l ~;,0 20 llli 33l!fi~l"l~t:iic•l& t... i'im.t~t.J: nJ~ GiH::. t.. t:,;:m
Introduction and Acknowledgments

*

{,f\.

=r-

hoku University, for his kindness andguidance throughout the course of thepresent work. Thanks are due to Dr.
Hiroshi NonA of the same Institute forhis kind offer of the specimens and valuable information on the stratigraphic
position of the fossils. Appreciation isdue to Messrs. Kimiji KUMAGAI and Shohei 0TOMO of the same Institute for
their photographic work.

The fossil bryozoans described in thepresent article form the first record of
the phylum from Okinawa-jima. The
specimens were collected by Dr. Hiroshi
NonA of the Institute of Geology andPaleontology, Tohoku University, during
his field work and fossil collecting inseveral parts of Okinawa-jima in thewinter of 1969. The bryozoans are allfrom the single newly discovered locality in the lower part of a cliff newly cut
for the purpose of building a fertillizer
mixing tank, and situated near to the
Yagena Harbor, Yonagusuku-son in thesouth-central part of the Island.
The purpose of this article is to describe the bryozoan fauna and thus contribute to the geological distribution of
the phylum in the Cenozoic rocks ofJapan and to aid in the establishmentof a bryozoan chronological scale forJapan.
Here the writer expresses her thanks
to Professor Kotara HATAI of the Institute of Geology and Paleontology, To-

Notes on the Stratigraphy of theFossil Bryozoan Sandstone Beds
The fossil bryozoans described in thepresent article were collected with otherfossil invertebrates by Hiroshi NonA
from a newly cut cliff not far from theYagena Harbor, Yonagusuku-son in thesouth-central part of Okinawa-jima (Textfig. 1). This cliff measures about 20
meters in width and more than 10 metersin height, and in it is exposed the following sequence. In the lower part ofthe cliff is developed the Yonabaru Clayof a little more than 8 meters in thickness and its base is not exposed. Superposed on the Y onabaru is a laminatedsandstone of about 50-60 em in thickness,* Received July 15, 1970; read June 27, 1970
at the Ibaraki University, Mito.

73

74

Tomoko HAYAMI

Text-fig. l.

Map showing the position of the fossil localities.

succeeded upward with about 3m thickfossiliferous sandstone (bryozoans andmolluscs), and a 5 m thick white tuff
intercalated with siltstone at the top.
The sandstone situated above the Yonabaru Clay is correlated by NonA withthe lowest part of the Shinzato Tuff of
MACNEIL (1960). The mentioned sequ-ence was not exposed at the time of
MACNEIL's survey.
The stratigraphic position of the Shinzato Tuff according to the classification
by MACNEIL (1960) is as shown in Table 1.
The stratigraphic sequence observedin the newly cut cliff is remarkably
similar to that of the type locality (MAC-579.

Neogene Bryozoa from Okinawa-J'ima

Table l. Stratigraphic classification of
the younger Neogene rocks in Okinawajima, according to MAcNEIL (1960).
Machinato limestonec
Yontanlimestone ( Residuum="Kunigami"
in partIr::.2 Absent?

0

1 Shinzato
1

I

tuff

memberE- - - - --- ---.L~~"'-------~__,>I
1 i>
Clay andr::

CIJ.E.~....

!UQ;

CIJ

:§' Absent

: ~f

<..)

E

1

0

~

~

silty sand-@E --------:~ Massive sand

NEIL, 1960).
The fossil bryozoans are from thefossiliferous sandstone mentioned above,and in association there were foundabundant, well preserved specimens ofgastropods, bivalves and solitary corals.
The gastropods and bivalves are now
being studied by NooA.
The geological age of the Shinzato
Tuff was stated to be Miocene or Pliocene by MACNEIL, but NODA is in theopinion that the basal part of the formation which is represented by the fossiliferous sandstone mentioned above
may be Early Pliocene in age (oral communication).

The Fossil Bryozoa
The fossil bryozoans washed out of
the fossiliferous sandstone are represented by 33 species distributed among
20 genera (Table 2). These bryozoans
are rather well preserved as shown in
the annexed plates and represent the75

first record of the phylum from the Island. From the occurrence of the bryozoans some interesting features can berecognized concerning their geographic
distribution (Text-fig. 2). Among the 33
species distinguished in the fauna, only
13 are in common with the fauna of theso-called " Ryukyu Limestone" (KAT AOKA, 1960). The Ryukyu Limestone issuperposed with unconformity upon the
Shinzato Tuff in Okinawa-jima and thus
one would expect a larger number of
species mutual between the two formations. Probably bottom control and local
ecological factors played an importantrole in establishing the dissimilar bryozoan fauna of the Ryukyu Limestone
and Shinzato Tuff. Only two species(Steganoporella magnilabris (BusK) andParasmittina trispinosa (JOHNSTON)) seemto be cosmopolitan in distribution, being
recorded from the Philippine Region, Kii
Peninsula, Sagami Bay and its vicinity,
Tsugaru Strait and Mutsu Bay, Off Florida
and Tortugas Islands, Galapagos Islands,
Panama Canal Zone, the Cenozoic ofVenezuela, Pleistocene of Kikai-jima and
the Quaternary of Louisiana. The remaining species are all of Indo-Pacificdistribution, Recent and fossil. Since
none of the 33 species are known fromthe waters around the Kuril Islands andHokkaido, it is evident that the fauna
is a typical Indo-Pacific one. The two
species (Caberea hataii OKADA and Parasmiltina trispinosa (JOHNSTON)) that havebeen recorded from Mutsu Bay in northern Northeast Honshu seem to be, at a
glance, species having relation with coolwater temperature. However, it is known
that the bay is influenced by the warm
water Tsushima Current; the same two
species are also known from off Florida
and Tortugas Island. Thirteen of the 33
species are known from the Philippine
Islands and neighboring seas. Three spe-

Tomoko HAYAMI

76
Table 2.

Distribution of the Bryozoa; numbers refer to Text-fig. 2.

,- species--.=-----_Distribution
Genus
and
-__

11213141516171819110111112113114115116·l·i········.··+I·r·. ..
...

I
I...... +Antropora tincta (HAsTINGs) · · · · · · · • • • • · • · • · · · • · · · · · · ·Cranosina coronata (HINCKS) •.•......•••.......•.... + .

Copidozoum planum (HINCKS) • · · · · · · · • • • • · • • · · · · · · · · · · · + · · · ··· +Steganoporella magnilabris (BusK) • · · · · • · · · · · · · • · · · · + + + + · · ·"j"· + · ·'· · · · + +Thalan:oporella novae-hollandiae (HASWELL) · · · · · • · · + ·+J ·i· ··J · ·· ·· ·· ·· ·· ·.

Cellana punctata (BusK) • · · · · · · · · · · • · • • · · · · · · • • • · · · · · · + +I+
Caberea halaii OKADA · · • • · · · · · · · · · · · · · · • · · · · · • · · · · · · · + · · · · +Schizomavella ovoidea CANU & BASSLF-Il · · · · · · • · · · · · + · · · · · ·S. sp.
Cleidochasma biavicularia (CANU & BASSLF-R)········ ·· ·· ·· ·· +1·· ·· ·· ·· ·· ++ ·· ·· ·· ·· ·· ·· ·· ·· ·· · · ·· +C. bassleri (CAL VET) · • · · · · · · · · · · · · · · · · · · · · · • · · · · · · • · • · · · · · +C. granifera (CANU & BASSLER) · · · · · · • • · · • · · · · · · · · · +C. aff. fallax (CANU & BASSLER) • · · · · · • • · · · · · · · · · · · · · · · · · · · · · · · · · · • · • · · · • · · · +Hippoporella spinigera (PHILIPPS)···················· +Cigclisula occlusa (BusK) · · · · • · • · · · · · · · • · · · · · · · · • · · · · +Mucronella sp.
Parasmittina aviculoumbonata KATAOKA · · • · • · · · • · • · · · · · · · · · · ·1· · · · · · · · · · · · · · +P. spathulata (SMnT) · · · · · · · · .. ·. · · .. · · · · · · · · · · · · · ·· · · · + ··+ · ·1+
P. peristoaviculata KATAOKA · · · · · · · · · ·• · · · · ...•. · • . .
· · · ·, +P. trispinosa (JoHNSTON) ••...•........................ + .. + + .... + + + .... 1+
Smittina sp.

I

1

Smittoidea acaroensis (LEVINSEN) · · · · · • · · · · · · · · · · · · · ·Rhynchozoon aff. grandicella CANU & BAssLER

R. sp.
R. (.)? sp.
Adeonellopsis arculifera (CANU & BASSLER)
A. subteres (ROEMER)· · · · ·

+
I

1

I
· · · · ·. ·.

· ·· ········ ·· ·•·· ···· ···

I It
I ,1

+

· ·· ·· ·· ·· ·· ·· + ·· ++ + + +1· ' · · · · · · · · · · .,. · +~~":i':;;:;:~",:,:'~:~: ~A;~<~C~~,~~~~ ••••••••••• :cies (Steganoporella magnilabris (BusK),
Cellaria puncta/a (BusK) and Costazia
radiata (ORTMANN)) extend their range
northward to the Izu Peninsula, Shizuoka
Prefecture and six are known from theKii Peninsula, Wakayama Prefecture.

· · · . . · · · · ·1

A. yarraensis (WATERS) · · · · • · • · • · • · • • • • • • • · · · · · · · · · + · · · · + ·Holoporella palmata (MICHELIN)
H. sp.
Costazia rad~ata (ORTMANN)

··

j__

J----~~

Thus as mentioned above, the bryozoan fauna is typically Indo-Pacific in
geographical distribution. However, explanation for the difference in the bryozoan biota between the Shinzato Tuffand superjacent "Ryukyu Limestone"

579.

Neogene Bryozoa from Okinawa-jima

~

-rr~

,
6

NORTH AMERICA

t.r!:?/

ASIA

77

/-~

.V"- ATLANnc

~

OCEAN

13
(]

IJ,?

PACIFIC OCEAN

di~
-~~ ~

~
\)

Text-fig. 2.

;;~

Index map of localities showing geographical distributions.

1. Philippine Region. 2. Kii Peninsula. 3. Izu Peninsula. 4. Sagami Bay and its vicinity.
5. Tsugaru Strait and Mutsu Bay. 6. Kuril Islands and neighbouring district. 7. Gulf of
Mexico. 8. Off Florida and Tortugas Islands. 9. Panama Canal Zone. 10. Galapagos Islands.
11. Quaternary of Louisiana. 12. Cenozoic of Venezuela. 13. Pleistocene of Kikai-jima. 14.
Miocene of Hokkaido. 15. Tertiary of Southwest Victoria. 16. Tertiary of New Zealand.

must be reserved until the bryozoans
from more localities of the two formations have been studied.
The environment of the bryozoan
fauna, so far as the present locality isconcerned, is judged to have been awarm water inner neritic zone area probably not influenced directly by the open
sea although free connection therewith
is evident from the assemblage of thebryozoans, gastropods and bivalves.
Descriptions and Remarkson th~ Bryozoa

Order Cheilostoinata BusK, 1852
Suborder Anasca LEVINSEN, 1909

Family Hincksinidae CANU
& BASSLER, 1927
Genus Antropora NoRMAN, 1903

Antropora tincta (HASTINGS, 1930)
Pl. 10, fig. 1.

1930. Crassimarginatella tincta HASTINGS, p.
708, pl. 5, figs. 16-19; pl. 17, fig. 120.
1950. Antropora tincta (HAsTINGS); OsBURN,
p. 54, pl. 4, fig. 7; pl. 29, figs. 7, 8.
1965. Antropora tincta (HASTINGS); MAWA·
TAR!, p. 600.

Description: Zoarium encrusts shellfragment. Zooecium oval, distal partnarrower than proximal. Gymnocyst
vestigial or wanting. Mural rim smooth

Tornoko HAYAMI

78

and not bearing spines, cryptocyst narrow. Vestigial avicularia triangular andsmall at proximal end of each zooecium.
One septule located on distal wall. No
dietellae. Ovicell not found.
Measurements (in mm):

Zoaria: Lz=0.60-0.64, Wz=0.44-0.48;
Opecia : lop=0.40-0.42, wop=0.32-0.36.
Distribution: Recent : Galapagos Islands, Panama Canal Zone (HASTINGS,
1930), Point Conception, California to
Peru a-nd Galapagos Islands [4-143 m](OSBURN, 1950).
Depository: IGPS coil. cat. no. 91480.

Distribution: Recent: Philippine, Ceylon (HINCKS, 1881 and 1882), Celebes, New
Guinea [18-32 m] (HARMER, 1926), Philippine Region [53-104m] (CANU & BASSLER,
1929). Pleistocene: Kikai-jima (KATAOKA,
1960a).
Depository: IGPS coli. cat. no. 91481.

Family Calloporidae NORMAN, 1903
Genus Copidozoum HARMER, 1926
Copidozoum Planum (HINCKS, 1880)
Pl. 10, fig. 2.

Genus Cranosina CANU & BASSLER, 1933
Cranosina coronata (HINCKS, 1881)
Pl. 10, fig. 4.
1881. Membranipora coronata HINCKS, p. 147,
pl. 10~ fig. l.
1882. Membranipora coronata HINCKS; HINCKs, p. 118.
1920. Ellisina coronata (HINCKs); CANU &BASSLER, p. 126.
1926. Setose!!ina coronata (l-IINCKS); HARM:
EI~, p. 265, pl. 16, figs. 2-4.
1929. El!isina coronata (HINCKs); CANU &BASSLER, p. 104, pl. 7, figs. 9, 10.
1953. Cranosina coronata (HINCKs); BAssLER, p. 160, fig. 122, 6.
1960a. Cranosina coronata (l-IINCKs); KATAOKA, p. 227, pl. 25, fig. 7.

Description: Zoarium encrusting. Zooecia large, without gymnocyst, aperture
occupying the entire front; spines wanting. Cryptocyst narrow but deep, strongly tuberculate, particularly at the sides
of opecia. Avicularium at distal end ofeach zooecium placed transversely. Porechambers and ovicells not found.
Measurements (in mm):

Zooecia: Lz=0.80-1.04, Wz=0.56-0.60;
Opecia : lop=0.48-0.56, wop=0.20-0.24.

1880. Membranipora plana l-IINCKS, p. 81, pl.
11, fig. 2.
1923. Membranipora vibraculoides OKADA, p.
223, fig. 25.
1930. Copidozoum planum (l-IINCKS); HASTINGS, p. 713.
1950. Copidozoum planum (HINCI<S); OsBURN,
p. 73.
1965. Copidozoum planum (l-IINCKS); MA\L"TAI~J, p. 601, fig. 54b.

Descri}Jtion: Zoarium encrusting. Zooecia moderate size, distinct, oval. Gymnocyst slightly developed, and cryptocyst
narrow, descending to center, crenated.
Mural rim smooth, without spines. Interzooecial avicularia placed scattering.
Ovicell globose, perforated With small
pores. Dietellae and septules not found.
Measurements (in mm):

Zooecia : Lz=0.60-0.72, W z=0.32-0.44;
Opecia: lop=0.48-0.60, wop=0.24-0.32;
Interzooecial avicularia :lav=0.48, wav=0.20;
Diameter of ovice\1=0.32.
Distribution: Recent: Panama Region[18-55 m] and Galapagos Islands [9-11 m](HASTINGS, 1930), Straits of Korea [218m] (OKADA, 1923).
Depository: IGPS coli. cat. no. 91482.

579.

Neogene Bryozoa from Okinawa-}inw,

Family Steganoporellidae HINCKS, 1884
Genus SteganoP01'ella SMITT, 1873
Steganoporella magnilabris (BUSK, 1854)
Pl. 10, figs. 3, 11.

1884. Steganoporel!amagni!abris (BusK);
BusK, p. 75, pl. 23, fig. 2.
1890. Steganoporellamagnilabris (BusK);
ORTMANN, p. 30, pl. 2, fig. 7.
1923. Steganopore!.!.amagnilabris (Busi<);
OKADA, p. 224.
1923. Steganoporellamagnilabris (Busi<);CANU & BASSLER, p. 63, pl. 14, figs.
12, 13.
1926. Steganoporellamagnilabris (BusK);
HARMER, p. 277, pl. 167, figs. 1-3, 7, 9,
12, text-fig. 10.
1928. Steganoporellamagni!abris (BusK);CANU & BASSLER, p. 64, pl. 7, figs. 812 ; pl. 32, fig. 6.
1929. Steganoporellamagnilabris (BusK) ;CANU & BASSLER, p. 144, pl. 1.5, figs.

1, 2.
1935. Steganoporellamagnilabris (Busi<) ;OKADA & MAWATARI, p. 130.
1941. Steganoporellamagnilabris (Busi<) ;Sru1N, p. 62.
magnilabris (BusK);
1952. Steganoporella
MAWATARI, p. 263.
magnilabris (BusK) ;1953. Steginoporella
BASSLER, p. 172, figs. 132, la, lb.
1960a. Steginoporella magnilabris (BusK) ;KATAOKA, p. 236, pl. 28, fig. 9.
1965. Steginoporella magnilabris (Busi<);
MAWATARI, p. 604, figs. 63a-d.
1967. Steginoporella magnilabris (Busi<) ;WEISBORD, p. 35, pl. 2, figs. 1-3; pl.
6, fig. 1.
1967. Steganoporella magnilabris (Busi<);
RUCKER, p. 824, fig. 13, i.

Description: Zoarium encrusts pelecypod-shell, uni- or bilamellar. Zooecia
distinct, large, separated by a shallow
furrow. Mural rim thin, salient. Frontal
cryptocyst finely porous. Opecia irregular or semilunar, a little elongate.

79

Mcasureme.nts (in mm):
A-Zooecia: Lz=0.80-1.20, Wz=0.60-0.72;
B-Zooecia : Lz= 1.00-1.40, W z=0.80-0.88.
Distribution: Recent: Sagami Bay [0366 m] (ORTMANN, 1890), Straits of Korea[93-110 m] (OKADA, 1923), Philippine,
Celebes Region [0-350 m] (HARMER, 1926),
Gulf of Mexico Region [44-333 m] (CANU& BASSLER, 1928), Philippine Region [37421 m] (CANU & BASSLER, 1929). lzu (Japan) (OKADA & MAWATARI, 1935), Japan[0-600 m] (SILEN, 1941), Venezuela (WEIS·
BORD, 1967). Lower Pliocene : Venezuela(WEISBORD, 1967). Pliocene and Miocene:
Florida (CANU & BASSLER, 1923).
Depository: IGPS coll. cat. no. 91483.

Family Thalamoporellidae
LEVINSEN, 1902
Genus Thalamoporella HINCKS, 1887
Thalamoporella novae-hollandiae(HASWELL, 1880)
Pl. 10, fig. 8.

1926. Thalamoporella novae-hollandiae (HAsWELL); HARMER, p. 295, pl. 19, figs.
. 14-16, 18, 19, text-fig. 11.
1960a. Thalamoporella novae-hollandiae (HAsWELL); KATAOKA, p. 238, pl. 27, fig. 12.

Description: Zoarium free, cylindrical,
stem quadrangular. Zooecia large, elongate, separated by a thin thread. Frontal porous cryptocyst. Aperture almost
round, with proximal round wide sinus.
Two large opeciules asymmetrical, pierced, porous cryptocyst. Avicularium interzooecial larger than zooecia, roundeddistally.
Measurements (in mm):
Zooecia: Lz=0.92-l.OO, Wz=0.40-0.44;
lnterzooecial avicularia:
lav=L08, wav=0.42.

Tomoko HAYAMI

80

Distribution: Recent: Jedan, Aru Island [13m] (HARMER, 1926), Pleistocene:
Kikai-jiina (KATAOKA, 1960a).
Depository: IGPS coil. cat. no. 91484.

Family Cellariidae HINCKS, 1880
Genus Cellaria ELLIS & SOLANDER, 1786

Cellaria punclata (BusK, 1852)
Pl. 12, fig. 7.
1890. Cellaria triangularis ORTMANN, p. 32,
pl. 2, fig. 13.
1921. Cellqria triangularis BusK; OKADA, p.
30, text-fig. 7.
1926. Cellaria punctata (BusK); HARMER, p.
337, pl. 21, figs. 14-16, text-fig. 13, a.
1929. Cellaria japonica CANU & BASSLER, p.
171, pl. 20, fig. 8.
1935a. Cellaria triangularis ORTMANN; SAKAKURA, p. 15.
1935b. Cellaria triangularis ORTMANN; SAKAKURA, p. 108.
1935. Cellaria triangularis ORTMANN; OKADA& MAWATARI, p. 1.32.
1941. Cellaria punctata (BusK) ; SILEN, p. 70,
figs. 85, 86.
1952. Cellaria punctata (BusK); MAWATARI,
p. 275, pl. 12, fig. 6, text-fig. 10.
1957. Cel!aria. punctata (BUsK); KATAOKA,
p. 145.
1960a. Cellaria punctata (BusK:); KATAOKA,
p. 240, pl. 27, fig. 13.
1.965. Cellaria punctata (BusK); MAWATARI,· p. 605, text-figs. 68a-d. ·Description: Zoarium free, articulated ; segments cylindrical, formed of 8
rows of zooecia. Zooecia distinct, separated by a slight furrow, hexagonal,
arranged in transverse rows. Mural rim
thick, smooth ; cryptocyst deep, lozengeshaped, smooth. Aperture semilunar,transverse, bordered by a thick salient
peristome; pro_ximal border ~rraightsometimes . mounted, with two lateral

denticles. A 'vicularia interzooecial, as
large as, or sometimes larger than zooecia.

Measurements (in mm):
Zooecia: Lz=0.40-0.42, W z=0.30-0.32;
Avicularia: lav=0.40-0.44, wav=0.36;
Diameter of zoarium=LOO.
Distribution: Recent: Japan [64-275m] (ORTMANN, 1890), japan [18-128 m](OKADA, 1921), Philippine Region [0-113m] (HARMER, 1926), Japan Sea (CANU &BASSLER, 1929), japan and Straits of Korea (OKADA & MAWATARI, 1935), Bonin
Islands [100-120 m] (SILEN, 1941). Pleistocene: Boso (Japan) (SAKAKURA, 1935a),
Kikai-jima (KATAOKA, 1960a). Pliocene:
Aomori (Japan) (KATAOKA, 1957).
Depository: IGPS coil. cat. no. 91485.

Family Scrupocellariidae LEVINSEN, 1909
Genus Caberea LAMOUROUX, 1816

Caberea hataii OKADA, 1929
Pl. 12, fig. 12.
1929. Caberea hataii OKADA, p. 13, pl. 1, fig.
2; pl. 4, fig. 2, text-fig. 2.
1935b. Caberea hataii OKADA; SAKAKURA, p.
109.
1937. Caberea hataii OKADA; OKADA & MAW A TAR I, p. 437.
1941. Caberea hataii OKADA; SILEN, p. 82,
figs. 96, 97; pl. 5, fig. 19; pl. 6, fig. 22.
1965. Cab ere a hataii OKADA; MAWATARI, p.
610, figs. 88d-f.

Description: Zoarium free, tuft irregu-.
Jar flabellate. Zooecia arranged in transverse rows of four serial, somewhat
elongate, nearly uniformly wide throughout length. Scutum may not entirely
fill opecia. Two spines present at distal
part of mural r.im. Avicularia locatedat proximal part of zooecium, single orpaired.

579.

Neogene Bryozoa from Okinawa-j-ima

Measurements. (in mm):
Zooecia: Lz=0.48, Wz=0.28.
Distribution: Recent: Goto Islands (Japan) [200-300 m] and Sagami Bay (Japan) [50-600 m] (SILEN, 1941), Tsugaru
Strait (Japan) (OKADA, 1929).
Depository: IGPS coli. cat. no. 91486.

Family Schizoporellidae ]ULLIEN, 1903
i'

Genus Schizomavella CANU &BASSLER, 1917
Schizomavella ovoidea CANU &BASSLER, 1929
Pl. 10, fig. 12.

1929. Schizomavella ovoidea CANU & BAssLER, p. 305, pi. 33, figs. 6-8.
1960a. Schizomavella ovoidea CANU & BAssLER; KATAOKA, pi. 33, fig. 13.

Description: Zoarium multilamellar,
encrusts she.U fragment. Zooecia dis. tinct, separated by a thin thread. Frontal
granular, bordered by a row of thread
like areolar pores. Aperture pyriform,
with two small cardelles. No lyrula.
Avicularia small, located before aperture, median rounded. Peristome thin.
Measurements (in mm):
Zooecia: Lz=0.44-0.52, Wz=0.40-0.48.
Distribution: Recent : Philippine Region [35-48 m] (CANU & BASSLER, 1929).
Pleistocene: Kikai-jima(KATAOKA, 1960a).
Depository: IGPS coli. cat. no. 91487.

Schizomavella sp.
Pl. 11, fig. 5.

Description: Zoarium encrusting, zooecia of moderate size. Frontal porous
cryptocyst. Aperture almost round andproximally wide a round sinus. Two

81

lateral cardelles. Suboral avicularium
small, triangular, transverse. Ovicell not
found.
Measurements (in mm):
Zooecia : Lz=0.76, W z=0.44-0.48.
·I
Remarlls: The present specimens resemble Schizomavella cincta (HINCKS),
but differ from it in having no prominent umbo.
Depository: IGPS coli. cat. no. 91488.

Family Cleidochasmatidae CHEETHAM& SANDBERG, 1964
Genus Cleidochasma HARMER, 1,957
Cleidochasma biavicularia (CANI!' &BASSLER, 1929)
Pl. 10, fig. 9.
1929. Gemellipora biavicularia CANU & BAssLER, p. 312, pi. 34, fig. 7.
1960a. Gemelliporella biavicularia (CANU &BASSLER); KATAOKA, p. 252,· pi. 29,
fig. 3.

Description: Zoarium free, bilamellar.
Zooecia distinct, undulated, convex·, separated by a deep furrow. Frontal reticulate, pores sporadic, or marginal areolae present. Aperture keyhole-shaped.
Frontal avicularia, transverse and suboral avicularia present. Ovicell not
found.
Measurements (in mm):
Zooecia: Lz=0.48-0.68, Wz=0.40-0.48.
Remarks: According to the originaldescription by CANU & BASSLER (1929),
this species . is an encrusting type, but
KATAOKA (1960a) stated" the zoarial features have two types, one is the sameas the original description ; encrusting
form, and the other is. the bifurcating
narrow cylindrical tube .type." ·The
present writer found only the narrow

82

Tomoko HAYAMI

cylindrical type in the present collection.
The zooecia are arranged back to back.
Distribution: Recent: Philippine Region [39-104 m] (CANU & BASSLER, 1929).
Pleistocene: Kikai-jima(KATAOKA, 1960a).
Depository: IGPS coli. cat. no. 91489.

Depository:

IGPS coli. cat. no. 91490.

Cleidochasma granifera (CANU &BASSLER, 1929)
Pl. 10, fig. 7.

Cleidochasma bassler£ (CALVET, 1931)
Pl. 10, fig. 13.
1890. Schizoporella cleidostoma ORTMANN, p.
49, pl. 3, fig. 37.
1890. ? Schizoporella cleidostoma var. inermis
ORTMANN, p. 50.
1890. ? Schizoporella cleidostoma var. japonica
ORTMANN, p. 50.
1929. ? Hippoporina planulata CANU & BAssLER, p. 321, pl. 37, fig. 6, text-figs. 132],
133C.
1929. Hippoporina fallax (pars) CANU &BASSLER, p. 320, text-figs. 1.32 I, 1.33 B.
1957. Cleidochasma bassleri (CAL VET) ; HARMER, p. 1042, pl. 71, figs. 5, 16.
1965. C!eidochasma bass!eri (CAL VET); MAWATARI, p. 616, figs. 114a, .b ..

Description: Zoarium encrusts on shellfragment, bilamellar. Zooecia subhexagonal, obscure. Frontal smooth, flat,
marginal with several pores. Aperture
keyhole-shape with two cardelles, avicularia small, triangular, aperture unilateral or bilateral, sometimes wanting,typically directed outwards and distally.
Ovicells small, smooth, immersed distal
zooecium. No spines.
Measurements (in mm):
Zooecia: Lz=0.60-0.62, Wz=0.48-0.50;
Aperture: lap=0.28, wap=0.14.
Distribution: Recent: Sagami Bay (Japan) [183m] (ORTMANN, 1890), Philippine
Region [35-422 m] (CANU & Bf\SSLER,
1929), Sulu Archipelago [16-23 m], Sumbawa [69 m], and Badjo Bay [0-40 m](HARMER, 1957).

1929. Hippoporina granifera CANU & BAssLER, p. 319, pl. 35, fig. 10.

Description: Zoarium encrusts on shellfragment. Zooecia distinct, separated bya little elongated furrow, deformed by
avicularium. Frontal very convex, ornamented with large granulations. Aperture keyhole-shaped, avicularia lateraland under aperture, forming small umbo.
Ovicell hyperstomial, globose, numerous
granular, not closed by operculum.
Measurements (in mm):
Zooecia: Lz=0.36-0.48, Wz=0.24-0.40;
Ovicell: lov=0.24, wov=0.24.
Distribution: Recent : Philippine Region [421 m, 11.6.C] (CANU & BASSLER,
1929).
•
Depository: IGPS coli. cat. no. 91491.

Cleidochasma aff. fallax (CANU &BASSLER, 1929)
Pl. 11, fig. 9.
Aff.:1929. Hippoporina fallax CANU & BASSLER,
p. 320, pl. 37, figs. 4, 5.
1929. Gemelliporella obesa CANU & BASSLER,
p. 313, pl. 35, figs. 3, 4.
1957. Cleidochasma faltax (CANU & BAssLER); HARMER, p. 1043, pl. 71, figs. 6-8.
1960a. Gemelliporella cf. fallax (CANU &BASSLER); KATAOKA, p. Z52, pl. 37,
fig. 5.

Description: Zoarium encrusts on shellfragment. Zooecia distinct, frontal garnished, reticulate, marginal pores rare.

579.

Neogene Bryozoa from Okinawa-J·ima

Aperture keyhole-shaped : peristome notsalient. Avicularia frontal with pivot,
its direction inconstant and sometimes
form umbo. Ovicell hyperstomial, reticulate, no pores.
Afeasurements (in mm):
Zooecia: Lz=0.44-0.52, Wz=0.36-0.48;
Aperture: lap=0.20-0.22, wap=0.12;
Ovicell: lov=0.25, wov=0.20.
Distribution: Recent: Philippine Region [35-439 m] (CANU & BASSLER, 1929),
New Guinea and Timor [0-118m] (HARMER, 1957). Pleistocene: Kikai-jii:na (KATAOKA, 1960a).
Remarks: The present specimen resembles this species by the charactersof the frontal, aperture, and other features, but differs from it in the character of the avicularia. It may be a
new species.
Depository: IGPS coli. cat. no. 91492.
Family Hippoporinidae BASSLER, 1935
Genus Hippoporella CANU, 1917

Hippoporella spinigera (PHILIPPS, 1899)
Pl. 10, fig. 10.
1929. Hippoporina squamosa CANU & BAssLER, p. 322, pl. 37, figs. 8, 9.
1957. Hippoporella spinigera (PHILIPPS); HARMER, p. 1100, pl. 73, fig. 13.

Description: Zoarium encrusts on shellfragments. Zooecia small, smooth, outline slightly indistinct. Aperture subcircular, transverse; suboral lip distallywith a straight, denticulate edge overhanging orifice; rising gradually on one
side, descending on other, where a minute sinus exists. Suboral avicularia
acute, present on both sides of aperture,
frontal avicularia larger than suboral
one, their orientation inconstant. Spines
6 to 8.

83

Measurements (in mm):
Zooecia: Lz=0.28-0.32, Wz=0.28-0.36.
Distribution: Recent: Philippine Islands (CANU & BASSLER, 1929), Sumbawa[69 m] (HARMER, 1957).
DejJOsitory: IGPS coli.· cat. no. 91493.
Suborder Ascophora LEVINSEN, 19'09
Family Stomachetosellidae CANU &BASSLER, 1917
Genus Cigclisula CANU & BASSLER, 1927

Cigclisula occlusa (BUSK, 1884)
Pl. 10, fig. 5.
1884. Escharoides occlu.sa BusK, p. 150, pl.
21, figs. 8-8b.
1927. Cigclisula (Escharoides) occlusa (BusK);CANU & BASSLER, p. 7.
1929. Cigclisula occlusa (BusK); CANU &BASSLER, p. 291. pl. 31, figs. 3-10.
1953. Cigclisula occlusa (BusK) ; BASSLER, p.
200, fig. 150, 2.
1957. Cigclisula occlusa (BusK); HAR:VIER, p.
1057, pl. 69, figs. 16-18.

Description: Zoarium free, ramose.
Zooecia large, separated by a thread,back to back. Frontal very porous
pleurocyst, marginal pores large. Aperture large, with small lateral cardelles.
Suboral avicularium located laterally
under aperture, form small umbo. Ovicell hyperstomial with marginal grilled
pores. Frontal avicularia small, 1-6, interzooecial avicularium large, spatulate.
Measurements (in mm):·
Zooecia: Lz=0.96-1.20, Wz=0.52-0.92;
Avicularia: lav=0.80, wav=0.60.
Distribution: Recent: Indian Ocean[384m] (BUSK, 1884), Philippine Region[37-104 m] (CANU & BASSLER, 1929), Timor [0-40 m] (HARMER, 1957).
DejJository: IGPS colt.· cat. no. 91494.

Tornoko HAYAMI

84

Family Smittinidae LEVINSEN, 1909
Genus Mucronella HINCKS, 1880

Mucronella sp.
Pl. 11, fig. l.

Description: Zoarium encrusts, bilamellar. Zooecia of moderate size, distinct, separated by a ·salient thread.
Frontal small granular, with a row ofmarginal areolae. Aperture rather round,with a broad lyrula at proximal portion.
No avicularia, or cardelles. Ovicell not
found.
Remarks: The present specimen resembles M. major (HINCKS), but differsfrom it by lacking of the oral spineand smaller measurements.
Depository: IGPS coli. cat. no. 91495.
Genus Parasmittina OsBURN, 1952

Parasmittina aviculoumbonata
KATAOKA, 1960
Pl. 11, fig. 6.
1960a. Parasmittina aviculoumbonata KATAOKA, p. 256, pi. 36, fig. 8.

Description: Zoarium encrusts, bilamellar. Zooecia distinct, separated by asalient thread, rectangular, arranged inlinear series. Frontal granular, bordered by a row of areolar pores. Aperture
subcircular, with broad lyrula and no
cardelles. Small avicularia on both sides
of aperture, frontal avicularia one or
two, sometimes wanting, small, spatulate.
Ovicell hyperstomial, large globose withperforated area bordered by raised thinridge on the frontal.
Measurements (in mm):
Zooecia : Lz=0.80, W z=0.40-0.48;
Ovicell: lov=0.36, wov=0.52.
Distribution: Pleistocene: Kikai-jima(KATAOKA, 1960a),

Depository: IGPS coli. cat. no. 91496.
Parasmittina spathulata (SMITT, 1873)
Pl. 11, fig. 2.
1928. Smittina tr£spinosa spathulata SrviiTT;CANU & BAssum, p. 114, pl. 15, figs.
9-13, text-fig. 21.
1929. Smittina trispinosa var. spathulata
SMITT; CANU & BASSLER, p. 349.
1952. Parasmittina spathulata (SMITT); OsBURN, p. 415, pl. 49, figs. 12-14.
1960a. Parasmittina spathulata (St..! ITT); KA·
TAOKA, p. 258, pi. 35, fig. 4.
196 11. Parasmittina spathulata (SMITT); CHEETHAM & SANDBERG, p. 1.037, text-figs.
44-47.

Description: Zoarium encrusts on shellfragments. Zooecia large, distinct, separated by a salient thread. Frontal granulated, polished, bordered by a row ofareolar pores, sometimes additional porespresent, especially at proximal part.
Aperture rounded, with large lyrula.
Peristome thin not raised, not bearing
spines. Frontal avicularia of three types;
one very large and spatulate, other small,oval and very long.
Measurements (in mm):
Zooecia: Lz=0.60-0.92, Wz=0.32-0.60.
Distribution: Recent : Gulf of Mexico
Region (CANU & BASSLER, 1928), Florida[24-81 m] (CANU & BASSLER, 1929), Galapagos Islands [46-183 m] (OSBURN, 1952).
Quaternary: Louisiana (CHEETHAM &SANDBERG, 1964). Pleistocene: Kikai-jima(KATAOKA, 1960a).
Depository: IGPS coil. cat. no. 91497.

Parasmittina peristoaviculata
KATAOKA, 1960
Pl. 11, fig. 7.
1960a. Parasmittina peristoaviculata
OKA, p. 256, pi. 34, llg. 4.

KATA-

579.

Neogene Bryozoa Jrmn Okinawa-jima

DescrijJtion: Zoarium encrusting, bilamellar. Zooecia very large, exceeding
1.00 mm in length, distinct, separated
by a thread. Frontal granulated, bordered by large areolar pores, slightly costate. Aperture somewhat elliptical, withbroad lyrula in proximal part. Peristomie entire, thick, salient especially at
distal part. A vicularium occurs along
peristomie in peristomice. Ovicell not
found.
Measurements (in mm):
Zooecia: Lz= 1.00-1.52, W z=0.48-0.60.
Distribution: Pleistocene: Kikai-jima(KATAOKA, 1960a).
Depository: IGPS col!. cat. no. 91498.

85

Measurements (in mm):
Zooecia: Lz=0.56-0.68, Wz=0.40-0.44.
Distribution: Recent: Cosmopolitan
down to a depth of 160m (CANU & BASSLER, 1923), Philippine Region [42 m] andChina Sea [198m] (CANU & BASSLER,
1929), Galapagos Islands [62-73 m] (CANU& BASSLER, 1930), from Oregon to the
Galapagos Islands (OSBURN, 1952). Pleistocene: South Carolina (CANU & BASSLER, 1923), Kikai-jima (KATAOKA, 1960a).
Pliocene: Florida (CANU & BASSLER,
1923). Miocene: North Carolina (CANU& BASSLER, 1923).
Depository: IGPS col!. cat. no. 91499.
Genus Smittina NORMAN, 1903

Parasmittina trispinosa (JOHNSTON, 1838)

Smittina sp.

Pl. 11, fig. 3.
Pl. 11, fig. 8.
1890. Smittina trispinosa JoHNSTON; Owr·
MANN, p. 45, pl. 3, fig. 26.
1923. Smittina trispinosa JoHNSTON; CANU &BASSLER, p. 143, pl. 22, figs. 7-14.
1929. Smittina trispinosa JoHNSTON; CANU &BASSLER, p. 340, pl. 41, figs. 1-3.
1930. Smittina trispinosa JoHNSTON; CANU
& BASSLER, p. 27, pl. 4, figs. 1-5.
1953. Parasmittina trispinosa (JoHNSTON);OsBURN, p. 412, pl. 49, figs. 7, 8.
1960a. Parasmittina trispinosa (JoHNSTON);KATAOKA, p. 258, pl. 35, fig. 3.
1960b. Parasmittina trispinosa (JoHNSTON);KATAOKA, p. 397.
1965. Parasmittina trispinosa (JoHNSTON) ;MAWATARI, p. 619, fig. 125c.

Description: Zoarium short cylindrical, multilamellar (?). Zooecia distinct,
separated by a salient thread, forms anddirection and regular. Frontal granular,bordered by a row of small, rounded
areolar pores. Peristome thin, sometimes
rises on side. Aperture rough, circular,
with narrow lyrula. Two frontal avicularia small, short spatulate or oval. Ovicells not found.

Description: Zoarium encrusting, multilamellar. Zooecia distinct, pores large.
Aperture rather round with large lyrula
bearing avicularium. Every zooeciumwith avicularium cradled in depressed
incomplete part of peristome. Oral spinesand ovicell not found.
Measurements (in mm):
Zooecia: Lz=0.52-0.72, Wz=0.40-0.44.
Remar!?s: The present specimen resembles S. canui ROGICK, 1956, but differs from it in the smaller measurements,
shape of lyrula, and because the ovicells
were not found, specific determinationis reserved.
Depository: IGPS col!. cat. no. 91500.
Genus Smittoidea OsBURN, 1952

Smittoidea acaroensis (LEV!NSEN, 1909)
Pl. 10, fig. 6.
1952. Smittina acaroensis LEVINSEN; BROWN,
p. 329, fig. 253.

Tornoko HAYAM I

86

Description: Zoarium encrusting, unilamellar. Zooecia vary in size, distinct,
a thin thread on surface. Frontal granulate, bordered by a row of areolar
pores. Aperture round when non-ovicelled and somewhat rectangular whenovicelled, with lyrula. Median avicularium small and oval, placed always insame location, within peristome border,
proximal and just external to lyrula.
Ovicell hyperstomial, not globose, front
face punctured by a number of small
irregular pores. Two small cardelles
present.
Measurements (in mm):
Zooecia: Lz=0.56-1.04, Wz=0.28-0.40;
Ovicell: lov=0.32.
Distribution: Recent: New Zealand,
Curtis Island, Bass Strait, Great Barrier
Reef (BROWN, 1952). Upper Pliocene :Castlecliff (BROWN, 1952).
Depository: IGPS col!. cat. no. 91501.

not found.
Measurements (in mm):
Zooecia: Lz=0.52-0.96, Wz=0.56-0.64;
Frontal avicularia: !a v=0.32, wav=0.08.
Distribution: Recent: OSBURN (1952)
stated "The known range is from about
34 o to 28° N Lat. and the bathymetricrange from 33 m to 121 m." Pleistocene :Southern California (CANU & BASSLER,
1923).
Ajfinities: The present specimen agrees with the original description of
CANU & BASSLER, except for the presence of frontal avicularium. And thisalso resembles OSBURN's description. But
because the ovicell was not found specific determination is withheld until more
specimens are found.
Depository: IGPS col!. cat. no. 91502.

Rhynchozoon sp.
Pl. 12, fig. 2.

Family Reteporidae SMITT, 1867
Genus Rhynchozoon HINCKS, 1895
Rhynchozoon aff. grandicella CANU
& BASSLER, 1923
Pl. 12, fig. 3.
Aff.:

1923. Rhynchozoim grandicella CANU & BASSLER, p. 156, pl. 47, figs. 7, 8.
1956. Rhynchozoon grandicella CANU & BAssLER; OsBURN, p. 459, pl. 54, figs. 7,8, 11.

Description: Zoarium encrusts on shellfragment. Zooecia distinct, separated bya furrow, elongated. Frontal smooth,with few areolar pores in marginal part.
Aperture rounded, proximal somewhat
sinuate. Avicularia usually placed lateral of aperture, forming large umbonate
process. Frontal avicularia elongate,
sometimes oblique. Spines and ovicell

Description: Zoarium encrusting, bilamellar. Zooecia distinct, quincunx, separated by a thin thread. Frontal reticulate, with marginal spotted areolar
pores. Aperture rounded, with asymmetrical narrow sinus. Suboral avicularium chamber forming small umbonate
process, and located somewhat peristomie. No frontal avicularia.
Measurements (in mm):
Zooecia: Lz=0.64-0.88, Wz=0.40-0.44.
Remarlls: This specimen belongs to
the genus Rhynchozoon and may represent a new species.
Depository: IGPS col!. cat. no. 91503.
Rhynchozoon (?) sp.
Pl. 11, fig. 10.

Description: Zoarium erect, free, forming semicyclic column, multilamellar.

579.

Neogene Bryozoa from Okinawa-Jima

Zooecia distinct, rather inflated frontal,
bordered by a row of round areolar
pores. Frontal smooth or sometimes
reticulate, umbo places at middle or lateral of aperture; aperture semicircular,
with more or less straight proximal
border. A vicularia of moderate size andlocated that tip of umbo. No spines.
Measurements (in mm):
Zooecia: Lz=0.52-0.60, W z=0.32-0.44 .
. Remarks: The present specimen resembles Holoporella, but differs from it
in wanting the interzooecial avicularium.
Whether this specimen belongs to thisgenus or some other one must be determined after more and better preserved
specimens are found.
Depository: IGPS coil. cat. no. 91504.

Family Adeonidae ]ULLIEN, 1903
Genus Adeonellopsis MACGILLIVRAY, 1886

Adeonellopsis arculifera (CANU &BASSLER, 1929)
Pl. 11, fig. 12.
1929. Adeona arcu/ijera CANU & BASSLER,
p. 377, pl. 52, figs. 1, 2.
1957. Adeonel!opsis arculifera (CANU & BAssLER); HARMER, p. 800, pl. 53, figs.
13, 14, text-figs. 82C, 84A.

Description: Zoarium free, bilamellar.
Zooecia distinct, separated by a furrowwith a marginal row of sporadic pores.
Aperture semicircular, transverse; peristome somewhat salient proximally.
Ascopore small. Between aperture andascopore, a triangular avicularium withacute tip proximally or sometimes transverse. Interzooecial avicularia almost
as large as suboral one, and directeddistally or transverse.
Measurements (in mm):
Zooecia: Lz=0.60, Wz=0.36-0.40;

87

Peristome: lper=0.08-0.10,
wper = 0.12-0.20.
Distribution: Recent: Philippine Islands [39-53 m] (CANU & BASSLER, 1929),
Paternoster Island (North of Sumbawa)[0-36 m] (HAI~MER, 1957).
Depository,· IGPS coil. cat. no. 91505.

Adeonellopsis subteres (ROEMER, 1863)
Pl. 11, fig. 4.
1968. Adeonel!opsis subteres (ROE!VIER); DAvm & PouYET, p. 89, pl. 13, figs. 7, 8.

Description: Zoarium free, bilamellar ;frond fiat, rarely convex. Zooecia distinct, separated by a shallow furrow andsurrounded by a row of slit-like pores.
Aperture semicircular and transverse.
Peristome salient in proximal part. Ascopore small, 4-8 stellate pores present.
Between aperture and ascopore, one triangular avicularia present, tip directed obliquely distally and outward frommedian line of zooecium.
Measurements (in mm):
Zooecia: Lz=0.52-0.60, Wz=0.32;
Peristome: lper=0.10-0.12,
wper=0.14-0.16.
Distribution: Chattien: Kassel (Germany) (DAVID & POUYET, 1968).
Depository: IGPS coil. cat. no. 91506.
Adeonellopsis yarraensis (WATERS, 1881)
Pl. ll, fig. 11.
1881.. Microporel!a yarraensis WATERS, p.
331, pl. 15, figs. 27, 28.
1881. ? Microporella clavata WATERS, p. 332,
pl. 18, fig. 84.
1884. Adeonella tuberculata BusK, p. 180.
1890. Adeonella tuben:ulata BusK; ORTMANN,
p. 53, pl. 4, figs. 9a, b.
1929. Adeonellopsis pentapora CANU & BAssLER, p. 382, pl. 53, figs. 1-5.

Tomoko HAYAMI

88

1957. Adeonellopsis yarraensis (WATERS);BROWN, p. 79.
1957. Adeonellopsis yarraensis (WATERS);HARI\!ER, p. 799, pl. 53, figs. 18, 19.
1960a. Adeonellopsis pentapora CANU & BAssLER; KATAOKA, p. 264, pi. 32, fig. 10.

Description : Zoarium free, bilamellar ;frond flat or somewhat inflated. Zooecia rather distinct, separated by a shallow furrow and surrounded by a row ofpores. Aperture somewhat embedded,
semicircular, transverse. Cribriform area
small, perforated by stellate pores. Between aperture and cribriform area, two
avicularia, sometimes only one. Salient
avicularium on front, at base of eachzooecium but sometimes wanting.
Measurements (in mm):
Zooecia: Lz=0.48-0.52, Wz=0.32.
Distribution: Recent: Maizuru [64-73
m] and Sagami Bay [183m] in Japan(ORTMANN, 1890), Philippine Region [37970 m] (CANU & BASSLER, 1929). Pleistocene : Kikai- jima (KATAOKA, 1960a).
Miocene (?): Victoria (Australia) (WATERS, 1881).
Depository: IGPS col!. cat. no. 91507.

Family Celleporidae BusK, 1852
Genus Holoporella WATERS, 1909

Holoporella palmata (MICHELIN, 1847)
Pl. 12, fig. l.
1930. Holoporella palmata (MICHELIN) ; CANU
& LECOINTRE, p. 111, pl. 23, figs. 1-11.

Description: Zoarium free, ramose,
zooecium of moderate size, distinct, narrow, with shallow groove, frontal smooth
but sometimes reticulate with a row ofmarginal areolae pores. Aperture rather
round with very narrow lyrule and cardelles. Two different avicularia present; one at tip of umbo lateral of aperture, and another interzooecial and aslarge as or larger than suboral avicularia. Both with pivot. No spines, ovicell not found.
Afeasurements (in mm):
Zooecia: Lz=0.56-0.72, Wz=0.48;
Aperture: lap=0.20.
Distribution: Miocene: Touraine(France) (CANU & LECOINTRE, 1930).
Depository: IGPS col!. cat. no. 91508.

------

Explanation of Plate 10
Fig. 1.
Antropora tincta (HASTINGS), x 20.
Fig. 2.
Copidozoum planum (HINcKs), x 20.
Figs. 3, 11. Steganoporella magnilabris (BusK), x 30.
Basal view of zoarium.
3.
11. Frontal view of another zoarium.
Fig. 4.
Cranosina coronata (HINCKs), x 30.
Fig. 5.
Cigclisula occlusa (BusK), x 20.
Fig. 6.
Smittoidea acaroensis (LEVINSEN), x 30.
Fig. 7.
Cleidochasma granifera (CANU & BASSLER), x 20.
Fig. 8.
Thalamoporella novae-hollandiae (HASWELL), x 20.
Fig. 9.
Cleidochasnza biavicularia (CANU & BASSLER), x 20.
Fig. 10. Hippoporella spinigera (PHILIPPS), x 30.
Fig. 12. Schizomavella ovoidea CANU & BASSLER, x 20.
Fig. 13. Cleidoc!zasnza bassleri (CAL VET), x 20.

HAYAMI:

Neogene Bryozoa from Okinawa-jima

Plate 10

579.

Neogene Bryozoa from Okinawa-jima

Holoporella (?) sp.
Pl. 12, fig. 6.

Description: Zoarium encrusting, unilamellar. Zooecia somewhat indistinct,
convex, with many irregularly directedavicularia; elongated triangular, or shorttriangular, sometimes ovate in shape.
Knob-like salient at proximal and lateralof aperture. Proximal one with elongated triangular avicularium. Areolar
pores sometimes at marginal portion.
Measurements (in mm):
Zooecia: Lz=0.60, Wz=0.52.
Remarks: The present specimen resembles Holoporella and Hippoporella (especially Hippoporella gorgonensis HASTINGS), but differs from them by lacking
spines.
Depository: IGPS coil. cat. no. 91509.

89

Zooecia: Lz=0.52, Wz=0.44-0.48;
Aperture: lap=0.18, wap=0.14;
Peristome: lper=0.28-0.48,
wper=0.22-0.44 ;Avicularia: lav=0.16, wav=0.10.
Distribution: Recent: Sagami Bay (Japan) [61-73 m] (ORTMANN, 1890), Japan
Sea and Philippine Region [ 42-53 m](CANU & BASSLER, 1929). Pleistocene :Kikai-jima (KATAOKA, 1960a).
Depository: IGPS coil. cat. no. 91510.

Family Conescharellinidae
LEVINSEN, 1909
Genus Conescharellina D'ORBIGNY, 1852
Conescharellina concava CANU &BASSLER, 1929
Pl. 12, figs. 8, 9.

Genus Costazia NEVIANI, 1895
Costazia radiata (ORTMANN, 1890)
Pl. 12, figs. 4, 5.
1890. Cellepora radiata ORTMANN, p. 56, pl.
1, fig. 14.
.
1929. Costazia radiata (ORTMANN) ; CANU &BASSLER, p. 432, pl. 63, figs. 8, 9.
1935. Cellepora radiata ORTMANN; OKADA &MAWATARI, p. 141.
1960a. Costazia radiata (ORTMANN); KATA·
OKA, p. 267, pl. 33, fig. 3.

Description: Zoarium encrusting, unilamellar. Zooecia distinct, short cylin·
drical, salient, nearly smooth. Basalborder of zooecia with areolar pores.
Peristome salient, tubular with a pairof avicularia on each side of peristome,
but sometimes wanting. Avicularia withpivot. Aperture semicircular with wide
triangular sinus in proximal part. Ovicell not found.
Measurements (in mm):

1929. Conescharellina concava CANU & BAssLER, p. 488, pl. 66, figs. 8, 9.

Description: Zoarium free, large coneshaped, transverse. Zooecia arranged inradial rows, with apertures very close
together. Apertures elliptical with awide semielliptical sinus. Radial rows
separated by shallow furrows containing
a row of small poriform avicularia close
together. Base concave, perforated bylarge scattered pores.
Measurements (in mm):
Zoaria : height of zoaria=3.80,
diameter of zoaria=2.50-4.00.
Distribution: Recent : China Sea [161m] (CANU & BASSLER, 1929).
Depository: IGPS coli. cat. no. 91511.

Conescharellina cf. breviconica

CANU & BASSLER, 1929
Pl. 12, figs. 10, 11.

Tomoko HAYAMI

90

Cf.:
1929. Conescharellina breviconica CANU &BASSLER, p. 491, pl. 69; figs. 10-17.

Description: Zoarium free, short conical, less than 2.0 mm high. Zooecia large,
numerous arranged in quincunx. Aperture long elliptical, with wide sinus. Interzooecial avicularium large, elliptical.
Base flat, exhibits zooecial ribs arranged
around a more or less large cancellated
center.
Afeasurements (in mm):
Zoaria: height of zoaria=l.83,
diameter of zoaria=l.80.
Remarks: The present specimens resemble C. breviconica, but differ fromit in the measurements which are higher
than wide, and sometimes as wide as
high.
Distribution: Recent : Philippine Region [145-214 m] (CANU & BASSLER, 1929).
Depository: IGPS coli. cat. no. 91512.

References
BASSLER, R.S. (1953) : Treatise on Invertebrate Paleontology, (G), Bryozoa. Geol.
Soc. America and Univ. Kansas, pp. l--253,
figs. 1-175.

BROWN, D.A. (1952): The Tertiary Cheilostomatous Polyzoa of New Zealand. Brit.
Mus. (Nat. Hist.), Zool., pp. 1-405, textfigs. 1-296.
- - (1.957) : Fossil Cheilostomatous Polyzoa
from Southwest Victoria. Geol. Surv.
Victoria, Mem., No. 20, pp. 1-90, text-figs.
1-83.
BusK, G. (1884) : Polyzoa I, The Cheilostomata. in Report on the scientific resultsof the voyage of H.M.S. Challenger, Zoology, vol. 10, pt. 30, pp. 1-216. pis. 1-36.
CANU, F. & BASSLER, R.S. (1920): North
American Early Tertiary Bryozoa. U.S.
Nat!. Mus., Bull., 106, pp. 1-877, pl. 1-47.
- - & - - (1927) : Classification of the
CheilostomatousBryozoa. U.S. Natl. Mus.,
Proc., val. 69, no. 14, pp. 1-43, 1 pl.
- - & --- (1928) : Fossil and Recent Bryozoa of the Gulf of the Mexico Region.
Ibid., val. 72, pp. 1-165, pis. 1-34.
-- & (1929) : Contributions to the biology of the Philippine Archipelago andadjacent regions; Bryozoa. U.S. JYatl.
Mus. Bull. 100, vol. 9, pp. 1-685, pis. 1-94.
--- & (1930) : The Bryozoan Faun.a of
the Galapagos Islands.· U.S. Natl. Mus.
Proc., val. 75, art. 13, pp. 1-78, pis. 1-14.
& LECOINTRE, G. (1930): Les Bryozoaires Cheilostomes Faluns de Touraine etd•Anjou. Soc. Ceo!. France, Mem., N.S.
tome 6, fasc. 1, mem. 4, pp. · 83-130, pjs.

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

Explanation of Plate 11
Fig. l. Mucrone!!a sp., x 20.
Fig. 2. Parasmittina spathulata (SM ITT), x 30.
Fig. 3. Parasmittina trispinosa (JoHNSTON), x 20.
Fig. 4. Adeone!lopsis subteres (RoEMER), x 30.
Fig. 5. Schizomavella sp., x 30.
Fig. 6. Parasmittina aviculoumbonata KATAOKA, x 20.
Fig. 7. Parasmittina peristoaviculata KATAOKA, x 30.
Fig. 8. Smittina sp., x 30.
Fig. 9. Cleidochasma aft. fall ax (CANU & BASSLER), x 20.
Fig. 10. Rhynchozoon (?) sp., x20.
Fig. 11. Adeonellopsis yarraensis (WATERS), x 30.
Fig. 12. Adeonellopsis arculifera (CANU & BASSLER), x 20.

HAYAMI:

Neogene Bryozoa from Okinawa-jima

Plate 11

.'579.

Neogene B1·yozoa front Okinawa-J·ima

1.6-25.
CHEETHAM, A.H. & SANDBERG, P.A. (1.964):
Quaternary Bryozoa from Louisiana Mudlumps. jour. Paleont., vol. 38, no. 6, pp.
1013-1046, text-figs. 1-59.
DAVID, L. & PouYET, S. (1968): Les Bryozoaires Cheilostomes du Chattien de Ia
region de Kassel (Hesse, Allemagne).
Geobios, Fac. Sci. Lyon, no. 1, pp. 81.-102,
figs. 1, 2, pis. 13, 14.
HARMER, S.F. (1926): The Po!yzoa of the
Siboga Expedition, Pt. II, pp. 24-501, pis.
13-34.
(1957): Op. cit. Pt. IV, pp. 642-1147,
pis. 42-74.
HASTINGS, A.B. (1929): Cheilostomatous
Polyzoa from the Vicinity of the Panama
Canal collected by Dr. C. CROSSLAND on
the Cruise of the S.Y. 'St. George'. Zoot.
Soc. London, Proc., no. 47, pp. 697-740,
pis. 1-7.
HINCKS, T. (1880) : Contributions towards a
General History of the Marine Polyzoa,
II Foreign Membraniporina (1st ser.),Ann. Mag. Nat. Hist., ser. 5, no. 6, pp.
81-92.
- - (1.881): Op. cit. IV Foreign Membraniporina (2nd ser.), Ibid., ser. 5, no. 7, pp.
147-156, pis. 8-1.0.
- - (1882) : Op. cit. X Foreign Cheilostomata. Ibid., ser. 5, no. 9, pp. 116-127.
KATAOKA, }. (1.957): Bryozoa from the Daishaka Formation (Pliocene), Minami-Tsugaru-Gun, Aomori Prefecture. Trans. Pro c.
Palaeont. Soc. japan, N.S., no. 28, pp. 143153, 1 pl.
- - (1960a): Bryozoa Fauna from the "Ryukyu Limestone" of Kikai-jima, Kagoshima
Prefecture, Japan. Tohoku Univ., Sci.
Rep., 2nd ser., vol. 32, no. 2, pp. 214-272,
pis. 1-13.
- - (1960b): Bryozoa from Mogami-Tai, Japan Sea. Ibid., Spec. vol., no. 4, pp. 394399, 1 pl.
MAcNEIL, F.S. (1960): Tertiary and Quaternary Gastropoda of Oki'nawa. U.S. Geol.
Surv. Prof. Paper 339, pp. 1-148, pis. 1-19.
MAWATARI, S. (1952): Bryozoa of Kii Peninsula. Mar. Biol. Lab., Publ., II (2), pp.
261-288, 1 pl.

91- - (1965): Bryozoa; in New Ilustrated Encyclopedia of the Fauna of Japan. pp.
585-628. (in Japanese) Hokuryu-Kan
OKADA, Y. (1921.): Notes of Some Japanese
Chei!ostomatous Bryozoa. Ann. Zoot. japan., vol. 10, art. 3, pp. 19-32, text-figs.
1-7.
- - (1923): On a Collection of Bryozoa fromthe Straits of Corea. Ibid., vol. 10, art.
22, pp. 21.5-234, 1 pl.
- - (1929) : Report of the Biological Surveyof Mutsu Bay, 12, Cheilostomatous Bryozoa of Mutsu Bay. Tohoku Imp. Univ.,
Sci. Rep .. 4th ser. Biology, vol. 4, no. 1,
fasc. l, pp. 11-35, pis. 1-5.
- - (1933): On a Collection of Bryozoa fromthe Northern Kurile Expedition. Biogeogr.
Soc. japan, Bull., vol. 4, no. 3, pp. 213216.
- - & MAWATARI, S. (1935): Bryozoa Fauna
collected by the "Misago" during the Zoological Survey around Izu Peninsula (I).
Tolzyo Bunrika Daigaku, Sci. Rep., Sec. B,
vol. 2, no. 35, pp. 127-148, pis. 10, 11.
ORTMANN, A. (1890) : Die Japanische Bryozoenfauna. Arch. f. Naturgesch., Bd. 1,
H. 1, pp. 1-74, pis. 1-4.
OsBURN, R.C. (1952) : Bryozoa of the Pacific
Coast of America, Pt. 2, CheilostomatousAscophora, vol. 14, no. 2, pp. 271-611, pis.
30-64.
RucKER, }.B. (1967): Paleoecological analysis of Cheilostome Bryozoa from Venezuela-British Guiana shelf sediments. Bull.
Marine Sci., vol. 17, pp. 787-839, figs. 116.
SAKAKURA, K. (1935a): Pliocene and Pleistocene Bryozoa from the Boso Peninsula·(I). Imp. Univ. Tokyo, jour. Fac. Sci.,
sec. II, vol. 4, pp. 1-48, pis. 1-7.
- - (1935b): Bryozoa from Toyama Bay, Sea
of Japan. Ann. Zoot. japan., vol. 15, no.
1, pp. 106-119, 1 pl., text-figs. 1, 2.
SILEN, L. (1941): Cheilostomatous Anasca(Bryozoa) collected by Prof. Sixten BocKs
Expedition to Japan and the Bonin Island,
1914. Arkiv fijr Zoologi, vol. 33a, no. 12,
pp. 1-130, pis. 1-9.
WATERS, A.W. (1881): Fossil Cheilostomatous Bryozoa from South West Victoria,

92

Tomoko HAYAM/

Australia. Geol. Soc. London, Quart. jour.,vol. 37, no. 1.47, pp. 309-347.
WEISBORD, N.E. (1967) : Some Late Cenozoic

ChinenKunigami
Naha
RyukyuTengan-gawa
Yonabaru
Yontan (Yomitan)

~11

•B'

00

jiJi

Jill
lTrt

:tit

L~

51

x ~rt Jll

LJ- ~HAM<

ll'iC

Bryozoa from Cabo Blanco, Venezuela.
Amer. Paleont. Bull., vol. 53, no. 237, pp
1-247, pis. 1-12.

Katsuren-son
Machinato (Minato)
Nakoshi (Nakaoshi)
Shimajiri
YagenaYonagusuku-son

1131 iili H
41l
iJ.!i
{rp M:\ {XJib/Ji.
ffi fX\! 45.EJ.nJilJ>~H~

Explanation of Plate 12
Fig. 1.. Holoporella palmata (MICHELIN), x 20.
Fig. 2. Rhynchozoon sp., x20.
Fig. 3. Rhynchozoon aff. grandicella CANU & BASSLER, x 20.
Figs. 4, 5. Costazia radiata (ORTMANN), x30.
4. A pair of avicularia of peristome.
5. Another zoarium; cylindrical zooecia, avicularia obscured.
Fig. 6. Holoporella (?) sp., x30.
Fig. 7. Cellaria punctata (BusK), x30.
Figs. 8, 9. Conescharellina conca11a CANU & BASSLER,
8. Basal view of large conical zoarium, x 20.
9. Lateral view of the same zoarium, x 30. ··Figs. 10, 11. Conescharellina cf. breviconica CANU & BASSLER.
10. Lateral view of conical zoarium, x 30.
11. Basal view of the same zoarium, x 30.
F'ig. 12. Caberea hataii OKADA, x 30.

H A YAM!:

Neogene B1·yozoa from Okinawa-J.i?na

Plate 12Trans. Proc. Palaeont. Soc. Japan, N.S., No. 82, pp. 93-116, pis. 13, 14, June 30, 1971

580.

FUSULINID BIOSTRATIGRAPHY AND MOLLUSCAN FAUNAFROM THE UPPERMOST PART OF THE SAKAMOTOZA W A
FORMATION, AND THE PRE-KANOKURA UNCONFORMITY,
IN THE SOUTHERN PART OF THE KITAKAMIMASSIF, NORTHEAST JAPANMASAFUMI MURAT A
Institute of Geology and Paleontology, Tohoku Universityi¥it't[);Jt.J:Lll!t!!~:$:iRl\'l:l!Ll:firlt7){i::::fil\'llf cm!:1*WJ:ro1t::fiW~. ~izrH:: ")tP-hfHJt=1~!lit" IC-=>v''"C: 1¥il'iii;Jt.l:iJJ±t!!lc§Eiii"0 --.:.;t-.b.*~:ljs:iRJWI7):®:J:1fll7G!GiRli'.Y'!ci-!Si1Jtt7):fitl'l • {i::::fiWilf~~~Hq)M*,~S~::fi~~SMJ:$c~~ftmq:JOO~K~0~c~m~Lk,~k~IIl*f:i!l!Kt7)7G!fJiRliYt'Htlll\"i d: IJ ffli:ll', u~~tki*mJJqf!.l{l::.::finH 1J 11m 1 r.ffq)Dfi.lf:lffi, 311Jl3 f.\l!t7)n£Z.lEn!, 1 f.lfl!.i.l ~l%"ts 4ilr. s 'fffiq:J~.lf:~n~~clfi~ u~. u" Gf:l:, i"""'L .Hi~q:Jiltifl\"i.:to .J: V::;l(NJ ;;f:~t7)!1iJJt71JlFfc.:tl<!ill~t~fiili:*.HiJ!'"t',
-?

'"C,

jj!ijffq:Jfl,filc:~f[..-v' R;J.rE9f,flf:f~f:l:::(-ft£LtJ:v', Lk,Q~"JI:Ilttfff.n:::f!l1l-" fi±t!!:l)llt~I"JtJ: t 17) c HH61ii" ~.

ntiffi717)i!/Elftli~H'-~-17)5J;{f]~;!J-ri\i: L '"C t

tt III 1E )[uppermost part of the Sakamotozawa
Formation in the type and the Setamai
areas, it was found that the fusulinid
fauna of the uppermost part of the Sa·
kamotozawa Formation is characterizedby Pseudofusulina ambigua (DEPRAT),
Misellina sp. and Monodiexodina matsubaishi (FUJIMOTO), and that the Motoiwazawa Sandstone Member of ONUKI (1956)
in the Setamai District is contemporaneous with the uppermost part of the
thick limestone (Shiratorizawa Limestone
Member) cropping out in the lower courseof the Kanokurazawa Valley. The Mo·
toiwazawa Sandstone Member yielded
many brachiopods and molluscs, comprising among the latter, three species ofgastropods distributed among three genera, five species of bivalves belonging
to four genera and one species of cephalopod. Among these nine species, twoof bivalves and one cephalopod were

Introduction and Acknowledgement
The Permian System in the southernpart of the Kitakami Massif has been
accepted as one of the standard typesections in Japan. Among the problems
still remaining on the geology, that on
the "pre-Kanokura unconformity" isimportant for the Permian stratigraphy
and tectonics in the Kitakami Massif.
There are two views on the post-Sakamotozawa pre-Kanokura break, one emphasizes a significant tectonic movement(MINATO, 1966) and the other denies suchtectonism ; (ONUKI, 1956, 1969; SAITO,
1965, 1968). From a bio-stratigraphicalstudy of the Sakamotozawa Formation
based on the fusulinids, and a paleontological study of the molluscs from theReceived July 16, 1970; read June 27, 1970
at the Ibaraki University, Mito.

93

94

Masaf~~mi MURATA

described by HAYASAKA (1925, 1962), HAYAMI (1960) and NAKAZAWA and NEWELL(1968) from the Kanokura Formation.
The gastropods described in this workas new to science are from the Tenjinnoki Formation in the Maiya District.
In general, the molluscan fauna of theuppermost part of the Sakamotozawa
Formation extends upward to the superjacent Kanokura Formation.
The writer here offers his cordial
thanks to Professor Kotora HATAI of
the Institute of Geology and Paleontology, Tohoku University, for his help
and advice during the course of thisstudy. Acknowledgments are due toProfessor Y oshio ONUKI of the Department of Geology, Miyagi College of Education, Professor Keiji N AKAZA w A of the
Department of Geology and Mineralogy,
Faculty of Science, Kyoto University, andDr. Yasuji SAITO of the Department of
Geology, National Science Museum fortheir suggestions and discussions.

Note on the Stratigraphy of the
Sakamotozawa Formation
In general, the pre-Permian formationsin the southern part of the Kitakami
Massif comprise six major anticlinal
structures, each plunging southwards,
with the axes trending in N -S to NNESSW directions. They are na:ned the
Tsuchikura Anticline, Takainari Dome,
Odaira Dome, Orikabe Anticline, Senmaya Dome and Tobigamori Dome, inthe order from east to west. The
Permian System in the south Kitakami
Massif rests on the Early and Middle
Carbrniferous formations with distinct
unconformity, and is distributed aroundthe anticlinal structures and in the synclinal parts between them. Early to
Middle Permian rocks in the southernpart of the Kitakami Massif differ considerably with area, due to the different movement of the basement complex(MURATA, 1964b, 1969; SAITO, 1968). The
Sakamotozawa and its synonymous formations are developed in two belt areas
each with N-S trend, and separated bya formation contemporaneous in age butof different litho-facies. The eastern
belt area is named to the Hikoroichi District and extends along the western limbof the Takainari Dome from the northeast of Yokamachi, Sumita-cho, Kesengun, Iwate Prefecture, to the south of
Hikoroichi, Ofunato City, Iwate Prefecture, via the type area of the Sakamotozawa Formation. The formation in thewestern belt covers the wide area between the western limbs of the Odaira
Dome and the Orikabe Anticline, andextends from the east of Ohazama, Hienuki-gun, Iwate Prefecture, to the vicinity of Kesennuma City, Miyagi Prefecture and includes the Tatsusobe, Otomo,
Setamai, and Yahagi areas (Text-fig. 1).
The Early Permian Sakamotozawa Formation was named by ONUKI (1937, 1938)
the Sakamotozawa "Stage" (formationin the present sense) of his Yukizawa"Series" (group in the present sence)for the sequence of basal conglomerate,
sandstone, slate and thick limestone, exposed in the Sakamotozawa Valley west
of Sakamotozawa, Hikoroichi-machi, Ofunato City, Iwate Prefecture, in his study
on the Palaeozoic stratigraphy of thesouthern part of the Kitakami Massif.
MINATO et al. (1954) studied the stratigraphy of the Permian System in the
Setamai District and proposed a timestratigraphic subdivision, and distinguished three litho-stratigraphic units
in the Sakamotozawa Series, e. g. Group
VII, Group IX and Group X in ascending order. The Group VIII begins withremarkable basal conglomerate and con-

580.

Sakamotozawa Molluscan Fauna

95

sists mainly of sandstone and slate layers. The Group IX is a thick limestone
formation. And the Group X is mainlyof sandstone facies. Subsequently, ONUKI(1956) summarized the geology of theKitakami Massif and established a standard succession of the Paleozoic andMesozoic rocks distributed in the southern part of the massif. ONUKI accepted
the three litho-stratigraphic units of the
Sakamotozawa Formation in the Setamai
District of MINATO et al. (1950) and proposed for them the names of Yubanosawa Slate, Shiratorizawa Limestone andMotoiwazawa Sandstone members 'in
upward sequence.

skm

Granodiorite

Ultramatic rocks
Other Permian formations
Koworogi Formation
Konokuro and Toyama fms.

[;:(~\J Pre- Permian formations

Text-fig. 1. Distribution of the Sakamotozawa Formation. Large Capitals-area mentioned in text.

Hikoroichi District
The Sakamotozawa Formation in the
Hikoroichi District, includes the typearea, lies upon the Middle Carboniferous
Nagaiwa Formation (ranging from thelate Millerella Zone to the Profusulinella
Zone) with a distinct unconformity. The
formation begins with notable basal conglomerate, sandstone and slate facies,
and is succeeded upwards with conformity by a thick limestone intercalatedwith sandstone and slate lenses. ONUKI(1956) classified the Sakamotozawa Formation in the type section into two parts,
the Yubanosawa Slate Member and thethick limestone facies as the Shiratorizawa Limestone Member, and supposed
the Motoiwazawa Sandstone Member in
the Setamai District to be missing in thetype area. Recently, MIKAMI (1965, 1969)and KANMERA and MIKAMI (1965a, b)
studied the succession, sedimentologicalfeatures and fusulinid fauna of the type
Sakamotozawa Formation shown in Textfig.2. They subdivided this formation into
two subformations by a disconformity.
The Lower Subformation was classified
into the basal part (Sa) and the mainpart of three members (Sb 1 _ 3 ), and theMasafumi MuRAT A·

96

(3)

KANOKURAZAWA

(4)

(7)

(5)
MOTOIWAZAWA(8)NEofTATSUSOBE

Nof KESENN~A.

Qscndstont:[8 conglol".era:<.'[]srot·~Q

Text-fig. 2.

scnay slate

0'""
X
IOC:Jirfy Of
Monxf,O'x m:JisutJoiSf·i'·

IOC·Jhlyof

rrotrus;::::n fauna

Columnar sections of the Sakamotozawa Formation.

Upper Subformation into the main (Member Sc) and uppermost (Member Sd) parts.
The Sa of the Lower Subformation corresponds to the Yubanosawa Slate Member of ONUKI (1956) and the Sbl-3 andthe Upper Subformation to his Shiratorizawa Limestone Member.
The disconformity between the Lower
and Upper subformations is an unevensurface and the basal limestone-conglomerate or conglomerate at the basal partof the Upper Subformation, is distributed
northward from Sakamotozawa to thenortheast of Yokamachi. However, noevidence of this disconformity has beenfound in the other districts in the southern part of the Kitakami Massif. The
disconformity may be a local phenomenon of an uplifted belt. The Member
Sc of the Upper Subformation is about
60 meter~ in thickness, and consists main-

ly of bedded limestone of three cycles:of sedimentation, except at the basai
part. Member Sd, nearly 30-50 metersin thickness, is composed of an alternation of sandstone and slate of various
thickness, intercalated with limestonelenses. The lateral changes in lithofacies
and thickness are striking in this partof the formation in north to south direction. The sandstone facies is welldeveloped in the northern part of this.
district, in contrast to the slate and limestone facies which thicken towards thesouth.
The upper part of the Upper Subformation in the type section of the Sakamotozawa Formation is missing by erosions. However, elsewhere the Member
Sd of the Upper Subformation is overlain with conformity by an alternationof coarse to medium grained sandstone·

580.

Sakamotozawa .Molluscan Fauna:and black slate about 50 meters ip. ,thickness, and is succeeded upwards by athick bed of the so-called Usuginu Con,glomerate. They had been referred to
the Kanokura Formation by ONUKI (1956),
YAMADA (1959), MIKAMI (1965, 1969), KANMERA and MIKAMI (1968a, b) and SAITO(1968). The alternation facies yielded nofossil to date, but the writer considers
that, the alternation should better berefered to the Motoiwazawa Sandstone
Member of ONUKI (1956) than to the
Kanokura Formation, because the fusulinid fauna from the upper part of theMember Sd indicates an age slightly·Older than the top of the Sakamotozawa
Formation in the Setamai Area.
In the west of Yokamachi, a thick limestone is exposed along the eastern limb
·Of the Odaira Dome with N-S trend at
Okunigiri, Mt. Horo-oroshi and Mt. Azumane. It was considered to be Permianin age and was referred to the Sakamotoza\va Formation by ONUKI (1956) and.SAITO (1966, 1968). Thus, the Sakamotozawa Formation was thought to be continuous from the Hikoroichi District to
the Setamai area. However, this limestone yielded Middle Carboniferous corals:as Siphonodendron pseudomartini (Y ABEand HAYASAKA), Dibunophyllum sp., Syringopora sp., Kueichoupora setamaiensis
MINATO, etc. The Permian System inthe belt area between the Hikoroichi
District and the eastern limb of the·Odaira Dome begins with poorly devel·oped basal conglomerate or conglomeratic coarse sandstone, and is succeeded
upwards by coarse to medium grainedsandstone, thick black slate intercalatedwith sandstone and thin limestone lay·ers, and has at the upper part thickblack slate with lenticular limestone andthe so-called Usuginu Conglomerate. The
lithofacies of the lower. part of thisPermian System changes eastward !at-97

erally to grade into the type Sakamotoza~a Formation.
And the upper partof. tne System succ~eds conformably thejust mentioned, " Kanokura Formation"in the I-Iikoroichi District. Lithologically, the Permian sequence in the belt area
between the Hikoroichi District and theq~,aira Dome differs distinctly from the
Sakamotozawa and the Kanokura formations by the poor development of basal
conglomerate, limestone in the lower partand sandstone in the upper part, and by
the lack of the basal conglomerate of
Kanokura Formation. This formation
should be referred to the Kowaragi Formation of ONUKI (1956, 1969) in the Karaku wa Peninsula.
Ohazama-Kesennuma District
The Permian System in this wide belt
area is distributed along the western
limb of the Orikabe Anticline and in the
synclinorium between the Orikabe Anticline and the Odaira Dome. The Permian
formations in the Tatsusobe area, thenorthern end of the Orikabe Anticline,
was named by HIROKAWA and YOSHIDA(1956) as the Tatsusobe Formation in thelower and the Kumonoue-yama Formation in the upper. In this paper the
Tatsusobe Formation is considered to bea synonym of the Sakamotozawa Formation, because of their mutual lithofacies and stratigraphic position. The
Kumonoue-yama Formation is a synonymof the Kanokura Formation for the same
reasons.
In general, the lithofacies and stratigraphic successions of the three lithostratigraphic units of the Sakamotozawa
Formation, defined by MINATO et al.
(1954) and named by ONUKI (1956), extend
over the district. The lateral change inlithofacies is rather distinct in east to
west direction due to the different movement of the basement of and around the

98

Masafumi MuRAT A

Odaira Dome and the Orikabe Anticline.
The Sakamotozawa Formation of thewestern slope of the Orikabe Anticline
covers the Middle Carboniferous limestones as in the Hikoroichi District, andalso the Lower Carboniferous formations
with distinct clino-unconformity. The
basal conglomerate of the Sakamotozawa
Formation is well developed near both
anticlinal structures. The sandstone andslate facies of the Yubanosawa Slate
Member which intercalate dacitic tuff in
the Ohazama-Kesennuma District are
thicker and richer in coarse materials
than at the type area, amounting to about
50 to 200 meters in thickness. The sandstone facies just mentioned becomes thinner in north to south direction along the
Orikabe Anticline.
The Shiratorizawa Limestone Member
consists of a thin alternation of blackslate and muddy limestone, and thickbedded gray limestone in ascendingorder. The alternation facies of thelower part is developed only along thewestern slope of the Odaira Dome. Consequently, the thick bedded gray limestone covers the Yubanosawa Slate Member directly in the Orikabe Anticline
area. According to the biostratigraphical evidence, as mentioned in the next
paragraph, the lowermost part of the
thick bedded gray limestone in the \Vestern part of this belt area corresponds tothe top of the lower part (less than 30
meters in thickness) of ·the limestone
member in the eastern part. The total
thicknesl!>"Of the member attains nearly
250 i:neters in the western limbs of the
Odaira Dome and the Orikabe Anticline,
but decreases westtward to 110 meters in
the eastern limJ:y'\Qf/the Orikabe Anticline. No evidences for the unconformity,
found by MIKAMi (1965) between the Upper and Lower subformations of the type
Sakamotozawa Formation, have beenfound in the Ohazama-Kesennuma District.
The type section of the Motoiwazawa
Sandstone Member is along the lower
course of the Motoiwazawa Valley southwest of Kawaguchi in the Setamai area,.
where the axial part of the synclinorium
between the Odaira Dome and the Orikabe Anticline is developed. In the typesection, this member lies on the thickbedded gray limestone of the Shiratorizawa Limestone Member with conformity, and consists of calcareous slate ofabout 30 meters in thickness and small
limestone lenses in the lower part, andmedium grained massive sandstone ofnearly 150 meters in thickness in the·upper part. The sandstone facies changes
laterally eastward to calcareous slate.
The thickness of the Motoiwazawa Sandstone Member changes from 0 to 300·
meters, reversally to the development of
the Shiratorizawa Limestone Member..
The Motoiwazawa Sandstone Member is.
not developed in the eastern margin of
this district, but it thickens towards the·Orikabe Anticline.
The Sakamotozawa Formation in the·Ohazama-Kesennuma District is overlain
by the Kanokura Formation. In general,.
the Kanokura Formation begins withbasal conglomerate, and is succeeded upwards by thick sandstone facies of the
Kattisawa Sandstone Member, and calcareous rocks of the Iwahata Limestone
Member of ONUKI (1956). The type locality of the Kanokura Formation is along·the middle course of the Kanokurazawa.
Valley, west of Kachizawa in the eastern
marginal part of the Setamai area. In
this area, the thick gray limestone of the
Shiratorizawa Limestone Member is infault contact with the basal granule to·pebble conglomerate (about 7 meters inthickness) of the Kanokura Formation_
A hornblende porphyrite dyke intrudes.

Sakamotozawa .Molluscan Fauua

580.

along the fault. The Motoiwazawa Sandstone Member is overlain by the basal
conglomerate of the Kanokura Formationin the larger part of the Ohazama-Kesennuma District. The basal conglomerateof the Kanokura Formation is not distributed throughout the district. In the
Tatsusobe area, the basal conglomerate
is of pebble to cobble size distributed
throughout, the size and thickness of thegravels decreases in south or southeast
direction, and becomes a conglomeratewith sporadic distribution of its granules
in the Yahagi and the Kesennuma area.
The lithofacies of the Sakamotozawa
Formation in the Ohazama-Kesennuma
District changes laterally into the pyroclastic Ubaishi Formation and into thelower part of the slaty Ochiai Formation
at the west.

Fusulinid Biostratigraphy of the
Sakamotozawa Formation
The Shiratorizawa Limestone Memberof the Sakamotozawa Formation has
yielded a rich fauna of fusulinids frommany horizons of the limestone. MINATOet al. (1954) subdivided the Sakamotozawa Series in the Setamai area into the

Subformation
Upper Subformation

MemberSd

I

Kawaguti and the Kabayama stages on
the basis of the fusulinids. Subsequently MINATO, KATO and HASEGAWA (1964)
referred the Kawaguti stage to the
Pseudoschwagerina zone and the Kabayama stage to the Pseudo fusulina zone.
According to those authors the Pseudoschwagerina zone in the Kitakami Massif
is characterized by Pseudoschwagerina(Robustoschwagerina) schellwieni HANZAWA, and the Pseudofusulina zone by
the Pseudofusulina vulgaris and Pseudof.
kraffti faunas.
KANMERA and MIKAMI (1965a, b) published the results of their biostratigraphical and paleontological studies on the
Sakamotozawa Formation in the typearea. They recognized five fusulinidzones in the Sakamotozawa Formation,
two of which were referred to the Lower
Subformation, and these to the Upper,
as follows:In general, the Early Permian formations in the southern part of the Kitakami Massif yield the same kind of fusulinid fauna as the Sakamotozawa Formation in its type area. However, thevertical ranges, abundancy and distribution of the fusulinids differ with areaeven within the Sakamotozawa Formation.

·-------------:~~~~~~~~~~

zone

subzone-~~~~~---------------, Pseudofusulina ambigua

I Pseudo/. fusiformis
Sc

99

I. Pseudo/. vulgaris (s.l.)

N agatoella minatoi
Pseudo/. krafjti
Pseudo/. aff. japonica!

Lower Subformation !

Sb 2

Monodiexodina langsonensisNipponitella explicata
I Zellia nunosei

:

1

Sb 1

Rugosofusulina alpina

100

Masafumi MuRAT A

The faunal assemblage and stratigraphical distribution of the fusulinid
fossils of the Sakamotozawa Form;1tion
in the type area as described by KANMERA and MIKAMI (1965a, b), are shownin Text-fig. 2. In the Hikoroichi district,
Quasifusulina tenuissima (SCHELLWIEN),
Rugosofusulina alpina (SCHELLWIEN),
Monodiexodina langsonensis (S AURIN)
and Nipponitella explicata HANZA w A areabundant in many horizons of the mainpart of the Lower Subformation. Zellia
nunosei HANZA w A is also abundant, but
is limitted to Member Sb 1 of the Lower
Subformation in the Hikoroichi District.
Member Sc of the Upper Subformationis characterized by abundant Pseudofusulina aff. japonica (GUMBEL), Pseudo f.
vulgaris vulgaris (SCHELLWIEN and DYRENFURTH), Pseudo/. vulgaris globosa(SCHELLWIEN and DYRENFURTH), Pseudo/.
krajfti krajfti (SCHELLWIEN and DYRENFURTH) and Schwagerina aff. compacta(WHITE). Among the listed species,
Pseudo/. vulgaris vulgaris decreases inabundancy upward from the base of·Member Sc, and Pseudo/. krajfti krajfti
is limitted nearly to the upper part ofMember Sc. The stratigraphical rangeof Pseudoschwagerina (Robustoschwagerina) shellwieni HANZA WA, an important
Early Permian species in the Kitakami
Massif, extends from Member Sb 2 up to
the upper part of Member Sc. The horizon of maximum abundancy of Pseudoschwagerina (Robustoschwagerina) schellwieni in this district is apparently in thelower part of the Member Sc. The
larger part of Member Sd is characterized by Pseudofusulina fusiformis(SCHELLWIEN and DYRENFURTH) and Nagatoella minatoi KANMERA and MIKAMI.
The uppermost part of Member Sd yielded Pseudofusulina ambigua (DEPRAT).
The lower part of the Shiratorizawa
Limestone Member in the eastern halfof the Ohazama-Kesennuma District,consists of a thin alternation of blackslate and muddy limestone. In the eastern part of the Setamai area, Quasifusulina tenuissima (SCHELLWIEN), Rugosofusulina alpina (SCHELLWIEN), R. cf.
rossica (SCHELLWIEN), and Paraschwagerina (Acervoschwagerina) sp. in association with a few Monodiexodina langsonensis (SAURIN) and Nipponitella sp.
have been found. Zellia nunosei HANZA WA is found rarely in the lower partof the Shiratorizawa Limestone Member.
Near the top of the lower part of the
Shiratorizawa Limestone Member 8 meters below the base of its upper part,
abundant Pseudoschwagerina (Robustoschwagerina) schellwieni HANZA WA were
found in association with some Zellia
nunosei HANZAWA, Rugosofusulina cf.
rossica (SCHELL WIEN) and Paraschwagerina (Acervoschwagerina) sp. This horizon is the lowest of the abundant occurrence of Pseudoschwagerina (Robustoschwagerina) schellwieni HANZAWA inthis district, and it probably correspondswith the Horizon I2 of MINATO et al.
(1954).
Three fusulinid zones and subzones of
the Upper Subformation in the Sakamotozawa Formation, defined by KANMERA and MIKAMI (1965a, b) are recognized in the Ohazama-Kesennuma District in the upper part of the Shiratorizawa Limestone Member. The fusulinid
fauna in the lower and middle parts ofthe mentioned limestone, except thelowermost part in the Orikabe Anticline
area, belongs to the Pseudofusulina vulgaris (s.l.) and Pseudo/. fusifonnis zones.
The lowermost part of the gray limestone in the Orikabe Anticline area, lessthan 20 meters thick, where the upper
part of the limestone member contacts
with the Yubanosawa Slate Member directly, yielded abundant, Pseudoschwa-

580.

Sakamotozawa Molluscan Fauna

gerina (Robustoschwagerina) schellwieni
HANZA w A, in association with Zellia
nunosei HANZAW A, Quasifusulina cf. tenuissima (SCHELLWIEN), Rugosofusulina
cf. rossica (SCHELLWIEN) and Paraschwagerina (Acervoschwagerina) sp. Thesefusulinids are succeeded upwards by thefauna of the Pseudofusulina vulgaris (s.l.)zone. The just cited faunal assemblage
is of the same composition as the faunafrom the uppermost part of the lower
part of the Shiratorizawa Limestone
Member in the Odaira Dome area. The
Pseudofusulina vulgaris (s.l.) zone in the
Ohazama-Kesennuma District contains
rarely Paraschwagerina (Acervoschwagerina) sp. in the lower horizon, and thefaunal difference between the subzones
of Pseudofusulina aff. japonica and Pseudofusulina kraffti is not clear. The
stratigraphical range of Pseudofusulina
kraffti kraffti (SCHELLWIEN and DYREN·
FURTH) extends from the middle levelof the Pseudofusulina vulgaris (s.l.) zone
up to the Pseudofusulina fusiformis zone
in this district, although there is adecrease in abundancy upwards. The
Pseudofusulina fusiformis zone can berecognized by the common occurrenceof Nagatoella minatoi KANMERA andMIKAMI, Eoverbeekina cf. cheni THOMPSON and FOSTER and Sp!werulina eras jispira (LEE). The range of Pseudofusu·
lina fusiformis (SCHELLWIEN and DYRENFURTH) overlaps that of Pseudofusulina
ambigua (DEPRAT) at the highest levelof the Pseudof fusiformis zone. Toriyamaia laxiseptata KANMERA is rare in
the Pseudofusulina vulgaris (s. 1.) and thePseudofusulina fusiformis zones. The
Pseudofusulina ambigua zone in this district is characterized by abundant Pseudo fusulina ambigua (DEPRAT) and Pseudofusulina sp. as in the type area of the
Sakamotozawa Formation. The zone isrecognized in the upper part of the gray101

limestone along the eastern margin of
the Setamai area, and in the uppermost
part on the western slope of the Orikabe
Anticline. In the lower course of the
Kanokura Valley, the highest level ofthe Pseudofusulina fusiformis zone isabout 100 meters above the base of theupper part of the Shiratorizawa Limestone Member. The thickness of thePseudofusulina ambigua zone is nearly
20 meters. The Misellina sp. zone about
20 meters in thickness, occurs above thePseudofusulina ambigua zone and ischaracterized by Misellina sp., Pseudofusulina ambigua (DEPRAT) and Pseudof
spp. The uppermost part of the Shiratorizawa Limestone Member, about 30
meters in thickness in the Kanokurazawa
Valley in the eastern margin of the Setamai area yielded ill-preserved Pseudofusulina sp. The limestone member isin contact with the Kanokura Formation
by a fault. At some horizons in theupper part of the Shiratorizawa Limestone Member abundant well-preserved" Mizzia" spp. and J\!Iichelinia (Michelinapora) multitabulata Y ABE and HAY ASAKA have been found.
The stratigraphically and paleontologically highest parts of the Shiratorizawa
Limestone Member differ with area.
Measured from the bottom, the highest
part of the member is higher than the
Misellina sp. zone in the eastern marginof the Setamai area. The limestone
member is distributed in the Tatsusobe,
the Otomo and the Kesennuma areas in
the Hikoroichi District and the western
limb of the Orikabe Anticline where it
restricted t0 the top of the Pseudofusulina ambigua zone. In the Motoiwazawa
Sandstone Member the limestone member is named the Pseudo fusulina fusiformis zone. In the eastern slope of the
Orikabe Anticline, the limestone member
is distributed in the eastern part of the102

Masafumi MURATA

Tatsusobe area, the Yokoiwazawa Valley
and in the Yahagi area, where it does
not extend up to the top of the Pseudofusulina vulgaris (s. 1.) zone. IvliNATO,
KATO and HASEGAWA (1964) and MINATO
and KATO (1965) reported on the occurrence of Misellina claudiae (DEPRAT),
Pseudofusulina kraffti (SCHELLWIEN)," Parafusulina" sp., lv!ichelinia (Michelinapora) multitaburata Y ABE and HAYASAKA, Yatsengia kabayamensis MINATO
and W entzelophyllum sp. from the topof the Shiratorizawa Limestone Member,and designated the fossil horizon as
Horizon J,. However, there still remains
doubt as to whether the horizons of
their different localities are the same.
The fusulinid fauna of the Motoiwazawa Sandstone Member was not known
before the discovery by the writer ofMisellina sp., Pseudofusulina ambigua(DEPI~AT), Pseudo/. sp. and Monodiexodina matsubaishi (FUJIMOTO) from four
localities in this district, one of which
includes the type locality of the sandstone member. In the type section, thelower part of the member, which consists of calcareous slate with small limestone lenses, yielded poorly preserved
Monodiexodina matsubaishi (FUJIMOTO)
admixed with a rich molluscan fauna inthe slate facies and abundant Misellina
sp. Pseudofusulina ambigua (DEPRAT)
and Pseudo/. sp. from the limestonelenses. This fossiliferous horizon corresponds to the J\!fisellina sp. zone in the
Kanokurazawa Valley. At about 80 meters below the base of the Kanokura
Formation in the Motoiwaza wa Valley,
Monodiexodina matsubaishi (FUJIMOTO)
was found. The same species is abundant in the lower part of the Kanokura
Formation where it forms a fossil layer
several centimeters thick. Monodiexodina matsubaishi (FUJIMOTO) was alsocollected from the middle and upperparts of this sandstone member in the
Yokoiwazawa Valley, east of Orikabe,
and at Yahagi in the Kesennuma Area.

Molluscan Fauna from the Upper Partof Sakamotozawa Formation
The Motoiwazawa Sandstone Memberof the upper part of the Sakamotozawa
Formation is short of macro-fossil records in general, however, some brachiopods and a coral were reported ; MOTEGI(1956, MS.) collected Buxtonioides sp.
from the upper part of the Sakamotozawa Formation in the Kesennuma area.
Phricodothyris sp., Avonia echidniformis
GRABAU em. CHAO, ]uresania juresanensis (TSCHERNYSCHEW), Mesolobus mesolobus (NORWOOD and PRATTEN) and Productus yohi CHAO were described by
NAKAMURA (1959), from his lower partof the Sakamotozawa Series, which however, was revised by MINATO and KATO
(1965) to the Upper Sakamotozawa Series.
This fossiliferous part was designatedby MINATO and KATO (1965) as Horizon] 2•
TAKEDA (1963, MS) collected a poorly
preserved Michelinia (Michelinopora) sp.
from a sandstone of the upper part of
the Sakamotozawa Formation in the
Tatsusobe area.
Recently, a rich molluscan fauna wasfound from the lower part of the Motoiwazawa Sandstone Member at its typesection and in the Yokoiwazawa Valley.
The fauna included Avonia echidnijonnis
and Mesolobus mesolobus and fragmentsof other brachiopods. From the fauna
the writer distinguished one species ofnautiloid, three species of gastropods
distributed among three genera and fivespecies of bivalves belonging to four
genera include one new genus, as follows:-

580.

Salcamotozawa Molluscan Fauna

Nautiloidea
Tainoceras kitakamiense HAY ASAKA
Gastropoda
Bellerop!wn (Bellerophon) flitakamiensis MURATA, n. sp.
Knightitej (Retispira ?) hanzawai
MURATA, n. sp.
" lvfurchisonia" n. sp.
Bivalvia
Towapteria nipponica N AKAZA wA
and NEWELL
W aagenoperna (Permoperna)
hayamii NAKAZAWA and NEWELL
Aviculopecten sp.
Aviculopecten ? sp.
Pseudoactinodontop!wra yabei
MURATA, n. gen. and n. sp.
Among the listed species Tainoceras llitakamiense, Towapteria nipponica, andW aagenoperna (Permoperna)
hayamii
were described by HAYASAKA (1925, 1962),
HAY AMI (1960), NAKAZAWA and NEWELL(1968) from the lower part of the Kanokura Formation in the Kesennuma areaand from the Tenjinnoki Formation in
the Maiya District which is an equivalentof the lower part of .the Kanokura. Although Actinodontop!wra katsurensis !CHIKA w A differs from Pseudoactinodontophora yabei generically, the former isseemingly the most closely related species to the latter. A. katsurensis was
also recorded by NAKAZAWA and NEWELL(1968) from the Kanokura Formation in
the Kesennuma area. The proposed new
gastropod species also occurred from theTenjinnoki Formation in the Maiya District.
As a result of this work, it may beconcluded that the molluscan fauna from
the Motoiwazawa Sandstone Member of
the Sakamotozawa Formation like Monodiexodina matsubaishi (FUJIMOTO) extends
upwards to the Kanokura Formation.
The continuous vertical distribution of
the fossils is interesting from the view103of the pre-Kanokura unconformity andsuggests that there was no significant
time gap between the two formations.
Also it may be added that the said breakis one of the unsettled problems on the
Permian stratigraphy in the JapaneseIslands.

On the Pre-Kanokura Unconformity
The stratigraphical and geo-tectonicalsignificance of the basal conglomerate of
the Kanokura Formation has been a subject of disputation by many authors. The
pre-Kanokura unconformity was statedto be significant by MINATO et al. (1954),
and to indicate the Abean Movement(MINATO, 1960, 1966, 1968). MINATO (loc.
cit.), from reading of the geological mapof the Setamai area concluded that theunconformity between the Sakamotozawa and the Kanokura formations
showed a structural difference and thatthe upper part of the Sakamotozawa
Formation was eroded away before deposition of the Kanokura Formation. The
pre-Kanokura disturbance was stated by
MINATO (1966) to indicate a slight positive diastrophic movement, less positive
than the pre-Sakamotozawa movement,
and was correlated w·ith the " Saalisch"phase of the Variscan Orogeny. However, ONUKI (1956, 1969) doubted the importance of the pre-Kanokura unconformity. SAITO (1968) admitted the presence of an unconformity, and without
giving any evidence denied a tectonic
movement between the two formations.
Meanwhile, some authors (KANO and
SEKI, 1954 ; KANO, 1955 ; YAMASHITA,
1957) gave weight to the pre-Kanokura
Unconformity pertaining to the granitic
plutonism. In the Kitakami and Abukuma massifs, the so-called "Usuginu Conglomerate" which commonly contains

104

Masafumi MURATA

pebbles of granitic rocks is intercalated
in different horizons of the Permian
System. The conglomerate occurs in theupper part of the Kanokura Formationin the areas of distribution of the Sakamotozawa Formation. The basal conglomerate of the Kanokura and Sakamotozawa formations contain only few
pebbles of granitic rocks. The Hikami
Granite a possible origin of the pebbles
of granite, which is exposed in the southof Hikoroichi, was K-A dated to be> 222 X 106 y. B. P., according to KAWANO
and UEDA (1964).
MINATO (1966).and his co-workers (1964,1965) figured a generalized stratigraphicalsection of the Carboniferous and Permian
formations in the southern part of theKitakami Massif, when they proposed
the pre-Kanokura disturbance. The contact of the basal conglomerate of the
Kanokura Formation with the Shiratorizawa Limestone Member in the Kanokurazawa and the Kachizawa valleys
was explained by them as the result offolding and erosion before the depositionof the Kanokura Formation. Their figure
showed that, the Shiratorizawa Limestone
Member was originally covered uniformly with the Motoiwazawa Sandstone
Member, and after the folding due tothe pre-Kanokura disturbance the upper
part of the Sakamotozawa Formation
over the Horizon ]0 was eroded away at
the crest of an anticline before the deposition of the Kanokura Formation.
However, recent stratigraphical and biostratigraphical evidences show that, theShiratorizawa Limestone Member along
the eastern margin of the Setamai area(including the Kanokurazawa, Kachizawa
and Kamiyashiki valleys) is developed
to its highest horizon, and is in contact
with the basal csnglomerate of the Kanokura Formation with a fault and theMotoiwazawa Sandstone Member wasprobably not deposited there. The stratigraphically highest part of the limestone
member differs in the other areas. The
highest part just mentioned belongs to
the Pseudofusulina ambigua zone in the
Hikoroichi District and in the western
limb of the Orikabe Anticline, to the
Pseudofusulina fusiformis zone in thetype area of the Motoiwazawa Sandstone
Member and to the Pseudofusulina vulgaris (s. 1.) zone in the Y okoiwazawa
Valley, east of Orikabe. In the areas
just mentioned the Motoiwazawa Sandstone Member is developed between the
Shiratorizawa Limestone Member and the
Kanokura Formation. The Misellina sp.
zone stretches over both the upper partof the limestone member in the eastern
margin of the Setamai area and theMotoiwazawa Sandstone Member in its
type area. The faunal assemblages Cif
the topment level of the limestone member and of the Motoiwazawa Sandstone
Member are not known however, the biostratigraphical evidences may support
the change in lithofacies from the upper
part of the Shiratorizawa Limestone
Member laterally to the Motoiwazawa
Sandstone Member.
The basal conglomerate of the Kanokura Formation is an extraneous conglomerate with the "Usuginu Conglomerate". It is succeeded upwards by athick sandstone formation, and is developed in nearly all areas of distributionsof the Kanokura Formation. But, thecanglomerate is missing in some areasin the southern and south-eastern partsof the Ohazama-Kesennuma District, because of the lateral change in grain size
and thickness of the conglomerate decreasing south- and east-wards, simultaneously with the increase in thicknessof the overlying sandstone facies. The
Tenjinnoki Formation in the NagasakaMaiya District in the southwestern part

580.

Sakamotozawa Molluscan Faunaof the Kitakami Massif, which is anequivalent of the Kanokura Formation,
has basal conglomerate like that of the
Kanokura Formation. But, there aremany broad areas in the southern partof the Kitakami Massif where neither
the basal conglomerate nor the thicksandstone formation is developed, except
in the Ohazama-Kesennuma and theNagasaka-Maiya districts. Further, thestratigraphical ranges of Monodiexodina
matsubaishi (FUJIMOTO) and the molluscan fauna of the Motoiwazawa Sandstone
Member both extend up to the Kanokura
Formation and cross the pre-Kanokura
unconformity. From these reasons, thewriter considers that the pre-Kanokura
unconformity may be a local one due tothe different movements of the sedimentary basin.
The pre-Kanokura unconformity isthought to have no relation with thegranitic plutonism, even though pebbles
of granitic rocks are found in theso-called " U suginu Conglomerate". Because the deposition of the "U suginu
conglomerate commenced during deposition of the Pseudofusulina ambigua
zone in the southwestern part of theKitakami Massif, as pointed out by
MURATA and MAIYA (1964), SAITO (1966,1968), ONUKI (1959) and MURATA (1969).
Some pebbles of the granitic rocks arealso found in the tuffaceous sandstoneof the Yubanosawa Slate Member of the
Sakamotozawa Formation, at Kashiwari,in the Setamai area. Further, the absolute age of a granite pebble from theso-called "Usuginu Conglomerate" atKogaizawa, Sumita-cho, Kesen-gun, Iwate
Prefecture, which belongs to the Ochiai
Formation, is determined recently to be420-425x 10 6 y. B. P. by the K-A method(UEDA, MS). Therefore the pebbles of
granitic in the so-called Usuginu Conglomerate are of a different origin.

105

Systematic Description of
Molluscan Fauna

Class Gastropoda CUVIER, 1797
Order Archaeogastropoda THIELE, 1825.
Suborder Bellerophontina ULRICH
and SCOFIELD, 1897
Superfamily Bellerophontacea
M'COY,. 1851
Family Bellerophontidae M'COY, 1851
Subfamily Bellerophontinae M'COY, 1851
Genus Bellerophon MONTFORT, 1808
Subgenus Bellerop!wn (Bellerop!wn)
MONTFORT, 1808

Bellerophon (BelleropJwn) kitakamiensis
MURAT A, n. sp.
Pl. 13, figs. 1-3.

Description :-Somewhat elongate, rather large bellerophontid gastropods withselenizone on a raised median crest,
apertural opening elongate cardiform ;earliest growth stage unknown; early
growth stages coiled uniformly to threefourths of body-whorl, but loosely inmature stage, whorl profile varying fromslightly compressed to elongate subcardiform ; upper surface well arched inearly stages with a high, distinct mediancrest, but decreasing in curvature inmature stage; lateral surfaces slightly
flattened, though not set off from uppersurface by angulation; selenizone convex
on median crest; slit depth unknown,
but probably less than 10 per cent ofbody-whorl circumference; lateral lips
curving back from anterior lips, theirjunction with body-whorl simple in early
growth stages, becoming slightly reflex-

Masafumi MuRAT A

106
Table 1.
Specimen
91389. 91390A
91390B
91390C
91390091390E

Holotype
Para typeMeasurements (in mm.) of Bellerophon (Bellerophon)kitakamiensis MURATA, n. sp.
LengthWidthThickness

33. 7
34. 0+
19. 0+
22. 2+
24. 0+
16. 2+

20.5
23. 0+
15. 0+
18. 0+
19. 6+
15. 5+

19. 5+

ed with maturity and a little thickened ;interior of lateral lips curved, but not
excavated; spiral ornament lacking; mature stage characterized by increasing
rugosities of growth lines.
The measurements of Bellerophon (Bellerophon) kitakamiensis MURATA, n. sp.
are given in Table 1.
Remarks:- This species is based on six
specimens, including a nearly perfectmold specimen. Although this new species is similar to many described Upper
Palaeozoic species, the ontogenic changesof shell form serve to distinguish it fromany of them. Bellerophon (s. str.) timorensis WANNER, 1922, B. (s. str.) timorensis
gibber WANNER, 1922, and B. (s. str.)
triangularis W AAGEN, 1881, seem to beclosely related to this new species, butthey have a more elongate shell and amore distinct median crest.
Repository:
Holotype-IGPS* coil. cat. no. 91389.
Paratypes-IGPS coli. cat. nos. 91390A-E.
Occurrence :-Common in the lower
part of the Motoiwazawa Sandstone
Member of the Sakamotozawa Formationin the Motoiwazawa Valley, southwestof Kawaguchi, Sumita-cho, Kesen-gun,
Iwate Prefecture. Several specimens of
this species were also collected from thelower part of the Kanokura Formation* Abbreviation for the Institute of Geology
and Paleontology, Tohoku University, Sendai,
Japan.

13. 0+
13. 5+

in Kesennuma City, Miyagi Prefecture,and from the Tenjinnoki Formation in
the Teranosawa, Valley, Towa-cho, Tomegun, Miyagi Prefecture.

Subfamily Knightitinae KNIGHT, 1956
Genus Knightites MOORE, 1941
Subgenus Retispira KNIGHT, 1945
Knightites (Retispira ?) hanzawai

MURATA, n. sp.
Pl. 13, figs. 4-6.

Description :-Rather elongate bellerophontid gastropods with collabral undulation and a distinct selenizone on low
median crest; shell medium in size, coiled uniformly in early growth stages,
loosening to nearly straight i11 mature
stage without aperture flare; upper surface arched moderately in early stages,
flattened in mature stage, with a low
distinct median crest ; lateral slopes wellrounded in early stages, becoming flatwith maturity, so whorl profile in mature stage more angular ; selenizone
concave on low median crest, borderedby lirae; slit deep, approximately 25 percent of body-whorl circumference; aperture not flaring; narrowly phaneromphalous, details of umbilicus unknown;
ornamented by numerous spiral lirae in
two sets, two to four finer lirae inter-

580.

107

Sakamotozawa Molluscan Fauna

Table 2. Measurements (in mm.) of Knightites (Retispira ?)hanzawai MuRATA, n. sp.
Specimen

LengthWidthThickness

91391
91392A
91392B
91392C
91392D
91392E

23.0
23.8+
18. 5+
22.4+
17. 2+
16. 7

13.2
14. 0+
13.2+
14.4+

10. 5+

Holotype
Para type,calated between two coarser lirae, ornamented also by faint growth lines ; shell
modified by transverse undulations on
upper surface and upper part of lateralsurfaces, strengthened at shoulder.
The measurements of Knightites (Retispira ?) hanzawai MURATA, n. sp. aregiven in Table 2.
Remarks:-This new species is basedon five molds of more or less deformed
specimens. The selenizone on the low
but distinct median crest of this species
resemble Bellerophon (Pharkidonotus) of
GIRTY (1912) rather than I\.nightites (Retispira) of KNIGHT (1845). But its narrowly
phaneromphalous umbilici, deeper slit
and surface ornamentations have closeaffinity to Knightites (Retispira). Therefore, this species is referred to Knightites(Retispira) MooRE (Op. cit.) with question.
This new species is not identifiable withany known species of Bellerophon (Pharkinodotus) nor Knightites.
Repository:
Holotype-IGPS coli. cat. no. 91391.
Paratypes-IGPS coli. cat. nos. 91392A-E.
Occurrence :-Rather common in thelower part of the Motoiwazawa Sandstone Member of the Sakamotozawa Formation in the Motoiwazawa Valley.
Order ? Archaeogastropoda THIELE, 1925
Suborder Murchisoniina Cox& KNIGHT, 1960

10.0+
15. 6+

11. 4+

Superfamily Murchisoniacea KOKEN, 1896
Family Murchisoniidae KOKEN, 1896
Genus Murchisonia D' ARCHIAC& DE VERNEUIL, 1841
" Murchisonia" n. sp.
Pl. 13, figs. 7-10.

Description :-Shell high-spired turbinate with ten or more whorls, spireslightly convex conical whorl with anangular spiral ridge bearing selenizone
on mid-whorl periphery; protoconch unknown; selenizone flat to concave; suture indistinct ; surface with narrow
spiral threads and collabral nodes, about
five spiral threads distributed on lower
two-thirds of upper whorl surface, twoor three more distinct spiral threads onlower whorl between sutures, collabral
nodes developed regularly on upper
whorl face only.
The measurements of " Murchisonia"
n. sp. are given in Table 3.
Remarks :-Four fragmental externalmolds of high-spired gastropods are in
the present collection. All of them areelongated or compressed by deformation,
but the surface sculpture is well preserved. (Pl. 13, fig. 7).
The present material, although notabundant, serves to show that they represent an undescribed species. Amongthe known species of Murchisoniidae, theMasafumi MURATA

108
Table 3.

Measurements (in mm.) of "Murchisonia" n. sp.

Specimen

Number ofwhorl

Height

Width

Whorl
heightApical angle(degrees)

91393A
91393B
91393C
91393D

10
11
7+
7+

38.2
30. 5 ?
20. 0+
14.2+

6. 8+
8.5
4.8+
11.1 ?

6.2+
5. 8+
5. 0+
4.3

12
17
13
41 ?

general shape and surface ornamentations of this species suggest affinity with
"Murchisonia" yabei HAY ASAKA (1943, p.
32, pl. 2, figs. 2, 3 ; pl. 4, figs. 1, 2 ; pl. 5 ;text-fig. 2) from the Middle Permian
Akasaka Limestone in Japan. But thecollabral nodes of " Murchisonia" yabei
are developed on the upper and the lower whorl faces and sepa.rated with doublecrested selenizone. The characters of
the surface ornamentationand selenizoneof these species suggest two different
genera, one resembles Helicospira of
GIRTY (1915) and the other is similar to
Micrentoma of DONALD (1898) rather thanMurchisonia of D' ARCHIAC and DE VERNEUIL (1841). Two of the present specimens, show a large, ovoidal apertural
opening with a siphonal canal. Fromsuch characters the present species
should be referred to some order otherthan the present one.
Repository :-IGPS coli. cat. nos. 91393
A-E.
Occurrence:- Rather common in thelower part of the Motoiwazawa Sandstone Member of the Sakamotozawa: Formation in the Motoiwazawa Valley, southwest of Kawaguchi, Sumita-cho, Kesengun, Iwate Prefecture.

Class Cephalopoda CUVIER, 1797
Subclass Nautiloidea AGASSIZ, 1847
Order Nautilida AGASSIZ, 1847

Superfamily Tainoceratacea
HYATT, 1883
• Family Tainoceratidae HYATT, 1883
Genus Tainoceras HYATT, 1882
Tainoceras kitakamiense HAY ASAKA, 1962
Pl. 14, fig. 13.
1962. Tainoceras kitakamiense . HAY ASAKA,
Bull. Natl. Sci. Mus., v. 6, n. 2, p. 140,
Text-fig. 2, pl. 12, figs. 1, 2.

Remarlzs :-A single incomplete steinkern of a heavily compressed specimen
is at hand. It appears to be a part ofthe living chamber and eight chambersof the phragmocone. Although smaller
in size (about two-thirds), this form may
be identical with Tainoceras lzitakamiense
HAYASAKA, 1962, from the Kanokura
Formation at Imo, Yahagi-cho, RikuzenTakada City, Iwate Prefecture, by thecharacteristic features of its row oflarge, prominent nodes on the ventrolateral border. The slightly concaved
broad median depression is borderedwith by pair of rows of less prominent
nodes. The sutures are moderately closely set (ca. 6 mm on venter).
Repository :-IGPS coli. cat. no. 91394.
Occurrence :-Rare in the lower partof the Motoiwazawa Sandstone Memberof the Sakamotozawa Formation in theMotoiwazawa Valley, southwest of Kawaguchi, Sumita-cho, Kesen-gun, Iwate
Prefecture.

580.

Sakamotoza.wa Molluscan Fauna

Class Bivalvia LINNE, 1758
Subclass Pteriomorphia BEURLEN, 1944
Order Pterioida NEWELL, 1965
Suborder Pteriina NEWELL, 1965
Superfamily Pteriacea GRAY: 1845
Family Bakevelliidae KING, 1850
Genus Towapteria NAKAZAWA
and NEWELL, 1968

Towapteria nipjJonica N AKAZA w A
and NEWELL, 1968
Pl. 14, figs. 5-8.
1959. Pteria sp., NAKAZAWA, Mem. Col!. Sci.,
Univ. Kyoto, Ser. B, v. 27, no. 2, p. 196,
Text-fig. 1.
1968. Towapteria nipponica NAKAZAWA and
NEWELL, Mem. Fac. Sci., Kyoto Univ.,
Ser. Geol. & Min., v. 35, n. 1, p. 59,
pl. 3, figs. 5-8.

Remarks:- There are four left and
one right ·valves at hand. They are all
externaL and internal molds, and moreor less deformed obliquely by compression. Taking the deformation into account, the present form is quite identicalwith Towapteria nipponica NAKAZAWA
and NEWELL, 1968, from the Tenjinnoki
Formation at Tenjinnoki, Maiya, Towacho,. Tome-gun, Miyagi Prefecture. NAKAZA WA and NEWELL (1968) also recordTable 4.

109

ed this species from the same formation
at Teranosawa, Maiya, Towa·cho, theKanokura Formation at Kamiyasse, Kesennuma City, Miyagi Prefecture, and
the Gujo Formation at Gujo, Oe-cho,
Kyoto Prefecture.
The measurements of the present specimens of Towapteria nipponica NAKAZA w A and NEWELL are given in Table 4.
Repository :-!GPS col!. cat. nos. 91395
A-E.
Occurrence :-Common in the lower
part of the Motoiwazawa Sandstone
Member of the Sa.kamotoza.wa Formation in the Motoiwazawa Valley, southwest of Kawaguchi, Sumita"cho, Kesengun, I wate Prefecture.
Family Isognomonidae WoODRING, 1925
Genus W aagenoperna TOKUY AMA, 1959
Subgenus Permoperna NAKAZAWA
and NEWELL, 1968

W aagenoperna (Permoperna) hayamii
NAKAZAWA and NEWELL, 1968
Pl. 14, figs. 9, 11.
1925. Liecea sinensis NEWELL, FRECH, HAYASAKA (non FRECH, 1911), Sci. Rep., Tohoku Imp. Univ., 2nd Ser. v. 8, n. 2,
p. 14, pl. 8, figs. 11, 12, 13 ?
1960. "]sognomon" n. sp., HAY AMI, jour. Fac.
Sci., Univ. Tokyo, Sec. 2, v. 12, pt. 2,
p. 327, Text-fig. 6.

Measurements (in n1m.) of Towapteria nipponica NAKAZAW A and NEWELL.

Specimen

LengthHeightHinge length----------··-------

91395A LV
91395B
91395C
91395D
91395E RV

15.2

11.5
10. 2+
9.8
11.4
LV: Left valve.

9.8?
7.5
6. 5+

13.9
10.2
10.0

7. 1

7. 0+

7.2

9.6

RV: Right valve.

Masafnmi MURATA

110

1968. Waagenoperna (Permoperna) hdyamii
NAKAZAWA and NEWELL, Mem. Fac.
Sci., Kyoto Univ., Ser. Geol. & Min.,v. 35, n. 1, p. 62, pl. 3, figs. 9-11.

Remarl<s :-Two specimens, one larger
and the other smaller are in the collection. The smaller one is represented bya rather severely deformed internal moldof a right valve but most features except the anterior ear and surface ornamentations are preserved. The ligamentarea is provided with four ligament pits.
Near the last ligament pit a weak posterior lateral tooth extends posteroventrally. The other one is represented by
an external mold of a nearly perfect left
valve except the posteroventral margin.
The anterior ear is small, subtriangularand clearly demarcated from the body ofthe shell by a furrow. Apical angle
about 55 degrees. The smaller specimen
is quite identical with Waagenoperna(Permoperna) hayamii NAKAZAWA and
NEWELL from the Tenjinnoki Formationin the Maiya District. The other specimen is larger than the type specimensof Waagenoperna (Permoperna) hayamii
NAKAZAWA and NEWELL, and as large
as the specimens of HAY ASAKA (1925)
from the Kanokura Formation in the
Yahagi area, and of HAY AMI (1960) fromthe same formation in the Kesennuma
area.
The measurements of the present specimens of Waagenoperna (Permoperna)
hayamii NAKAZAWA and NEWELL are
in Table 5.
Repository:-IGPS coli. cat. nos. 91397,
Table 5.

91398.
Occurrence :-Rather rare from thelower and middle parts of the Motoiwa·
zawa Sandstone Member of the Sakamotozawa Formation in the Motoiwazawa and the Yokoiwazawa valleys, Sumita-cho, Kesen-gun, Iwate Prefecture.

Superfamily Pectinacea
RAFINESQUE, 1815
Family Aviculopectinidae MEEK
and HAYDEN, 1864
Subfamily Aviculopectininae MEEK
and HAYDEN, 1864
Genus Aviculopecten M'CoY, 1851,
em. NEWELL, 1938
Aviculopecten sp.
Pl. 14, figs. 12a, b.

Remarl<s :-A single fragmental compressed external mold of right valve isat hand. The radial costae of different
strength may be classified into threeorders. First order costae 8 or 9 innumber. Between two of them a costaof the second order is intercalated irregularly and attains a size of first one
in the early growth stage. Third ordercostae are more delicate and placed irregularly. The ornamentation is somewhat similar to that of Aviculopecten
hataii MURATA, (1964b), and A. cf. hataii
by NAKAZAWA and NEWELL (1968).
Repository :-IGPS coli. cat. no. 91396.

Measurements (in mm.) of Waagenaperna (Permoperna)lzayamii NAKAZAWA and NEWELL.

Specimen

LengthHeightHinge length

91397 RV
91398 LV

14. 5+
35.4

25.4 ?
42.2

11. 2
22.8

580.

Salcamotozawa Molluscan Fauna

Occurrence :-Rare; the lower part of
the Motoiwazawa Sandstone Member of
the Sakamotozawa Formation in the Motoiwazawa Valley, southwest of Ka waguchi, Sumita-cho, Kesen-gun, Iwate Prefecture.
AviculojJecten ? sp.
Pl. 14, fig. 10.

Remarks :-A small external mold of
a left valve of Aviculopecten-like shell,
the ligamenta! area is not preserved.
The surface of the shell is ornamented
with several weak radial costae.
Repository :-IGPS coli. cat. no. 86884.
Occurrence :-Rare, the middle part of
the Motoiwazawa Sandstone Member of
the Sakamotozawa Formation in the Yokoiwazawa Valley, near Orikabe, Sumitacho, Kesen-gun, Iwate Prefecture.

Subclass Palaeoheterodonta
NEWELL, 1965
Order U nionoida STOLICZKA, 1871
Superfamily U nionacea FLEMING, 1828

? Family Actinodontophoridae
NEWELL, 1969
Genus Pseudoactinodontophora
MURATA, new genus
Type species: Pseudoactinodontop!wra
yabei, new species, Sakamotozawa Formation, northeast Japan; Early Permian.
Diagnosis :-Shell medium in size, equivalve, elongate elliptical ; umbo prosogyre, located at least at one-fourth ofshell length from anterior margin, only
slightly salient above hinge margin ;dorsal margin nearly straight, ventral
margin broadly convex, anterior margin

111

short and well rounded, posterior margin probably subrounded and truncate
obliquely; escutcheon distinct, deeply incised, bounded by a sharp ridge extending to near posterior end of hinge ;lunule unknown ; ligament opisthodetic,
nymphs well defined ; anterior muscle
scar subcircular, deeply impressed close
to anterodorsal margin with buttress,
posterior scar large, obscure; surface
with growth lines. Hinge-plate with aseries of radiating cardinal and subcardinal teeth located below beak, and an
obscure lateral tooth and socket in eachvalve; four strong cardinal teeth, ornamented with rather coarse striations oneach side three of which run anteroventrally, posterior most cardinal toothvertical or directed slightly posteroventrally; seven to nine subcardinal teeth,
directed posteroventrally, and becoming
short and thin posteriorly.
Remarlls :-The external and internal
characters of the proposed genus are
similar to the Permian Actinodontophora
ICHIKAWA (1951, p. 327, type: A. /latsurensis ICHIKAWA), but the details of thedentition are different. Actinodontophorallatsurensis ICHIKAWA, which is the only
known species of the genus, posseses" two (in one case, three ?) cardinals andfive to seven subcardinals" and thus differs from Pseudoactinodontophora. Actinodontophora is known from the Middle
or Upper Permian formation at Katsura
in Shikoku, and from the Middle Permian
Kanokura Formation in the Kesennuma
area. Pseudoactinodontop!wra is from theLower Permian Sakamotozawa Formation in the Setamai area. Although thepresent new genus differs from Actinodontophora, the latter seems to be themost closely related genus to the present one. Possibly, Actinodontophora may
be a descendant of Pseudoactinodontop!wra. The Upper Triassic Palaeop!zarus

Masafumi MuRAT A

112
Tab_le 6.

Measurements (in mm.) of Pseudoactinodontophorayabei MuRATA. n. gen. n. sp.

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

Specimen
86885
86886A
86886B
86886C
86886D
86886E

Holotype RV
LVPara type LV
LV
RV
RV
RV
-

LengthHeight

76.5

19.0

45.8+
44.0+
ca 27.0
43.5+
ca 56

22.2
19.4
12.5
14.2
1.3.0

------- - - - - - - - - -KITTL (1907, p. 34, type: P. schell DIENER)
is another genus similar to the newly
proposed one but it can be distinguishedfrom the new genus in the dentition andornamentati_on of the shell surface.
Pseudoactinodontophora yabei MURAT A,

n. gen. and n. sp.
Pl. 14, figs. 1-4.

Description :-Shell m~dium in size,
equivalve, inequilateral, strongly elongated posteriorly ; umbo subdued located at one-fourth to one-ninth of shelllength from anterior margin. Dorsal
margin nearly straight or gently conve~, ventral margin broadly convex,
anterior margin short and well rounded, posterior margin probably subrounded and tn.J.ncate obliquely; escutcheon
long and d.eep, bounded by sharp ridge
extending to near posterior end of
hinge; ligament opisthodetic, nymphs
well defin!'lcl ; dentition of four cardinalteeth, anterior three strong, thick, andbecoming short posteriorly, but posterior most cardinal tooth longer thanothers and bisected in right valve, sevento nine subcardinal teeth thin and somewhat geniculate.
The measurements of Pseudoactinodontophora yabei MURATA, n. sp. aregiven in Table 6.

Remarks:- This new species is basedon about ten specimens, all of which
are internal and external molds of .incomplete valves. Their preservations
are not so good, but the characters of
their dentition are well observed in somespecimens. As mentioned above, thepresent form seems to be closely related
to ActinodontopJwra katsurensis ICHIKAwA, but the dentition is different. This
species is named in honor of the lateDr. Hisakatsu YABE, who died on June
23, 1969.
Repository:Holotype-IGPS coli. cat. no. 86885.
Paratype-IGPS coli. cat. nos. 86886A-I.
Occurrence :-Abundant in the lower
part of the Motoiwazawa Sandstone
Member of the Sakamotozawa Formation in the Motoiwazawa Valley, southwest Kawaguchi, Sumita-cho, Kesen-gun,
Iwate Prefecture.

References
Cox, L.R. and KNIGHT, ].B. (1960): Subordersof Archaeogastropoda. Malac. Soc. London, Proc., vol. 33, part 6, pp. 262-264.
DoNALD, Jane (1898): Observations on thegenus Aclisina DE KoNINCK, with descriptions of British species and of son:ie other
Carboniferous Gastropoda. Geol. Soc: London, Quart. jour., vol. 54, pp. 45-71, pis.
3-5.

580.

Sakamotozawa Molluscan Fauna

GIRTY, G.H. (1915): Fauna of the Wewoka
formation of Oklahoma. U.S. Ceo/. Surv.,
Bull., no. 544, pp. 5-271, 35 pis.
HAY AMI, I. (1960) : Occurrence of an isognomonid in the Japanese Permian. Univ.
Tokyo, jour. Fac. Sci., Sec. 2, val. 12, pt.
2, Appendix, pp. 327-328, 1 text-fig.
HAY AS AKA, I. (1925) : On some Paleozoic
molluscs of Japan, 1. Lamellibranchiata
and Scaphopoda. Tohoku Imp. Univ., Sci.
Rep. 2nd Ser. (Ceo/.), vol. 8, no. 2, pp.
1-29, pis. 8-9.
- - (1943) : On some Permian gastropods
from Kinsy6zan, Akasaka-mati, Gifu Prefecture, Pt. l. Taihoku Imp. Univ., Mem.
Fa c. Sci. Ser. 3, vol. 1, no. 2, pp. 23-48,
2 text-figs., pis. 1-5.
- - (1962) : Two species of Tainoceras fromthe Permian of the Kitakami Mountains.
Nat/. Sci. Mus. (Tokyo), Bull., val. 6, no.
2, pp. 137-143, 2 text-ftgs., pis. 11-12.
HIROKAW A, 0. and YosHIDA, T. (1956): Explanatory text of the geological map of] a pan, Scale 1: 50,000, Ohazama. Ceo/.
Surv. japan. (in ] apanese with English
abstract)lCHIKAW A, K. (1951): AcUnodontophora, nov.
and other Permian Mollusca from Katsurain the Sakawa basin, Shikoku, southwest
Japan. Univ. Tokyo, jour. Fac. Sci., Sec.
2, val. 7, Pt. 6, pp. 317-335, pl. 1.
KANMERA, K. and MtKAMI, T. (1965a): Succession and sedimentary features of thelower Permian Sakamotozawa formation.
Kyushu Univ., Mem. Fac. Sci.,. Ser. D,
Ceo/., vol. 16, no. 3, pp. 265-274, 2 textfigs.
- - and - - (1965b): Fusuline zonation of
the lower Permian Sakam?tozawa series.
Ibid., pp. 275-320, 1 table, pis. 44-53.
KANO, H. (1955) : Preliminary notes on tectonic relations between the granitic rocks
and their country rocks in the Kitakamicentral zone (II). Ceo/. Soc. japan, jour.
vol. 61, no. 714, pp. 124-139, 20 text-figs.
(in Japanese)- - and SEI<I, Y. (1954): Geology of themedian zone in the Kitakami mountainlands, Iwate Prefecture. Guide-book of
the geological excursion, 61st Ann. Meet.,

113

Ceo/. Soc. japan, pp. 1-27, 8 text-figs., 3
tables. (in Japanese)
KAWANO, Y. and UEDA, Y. (1964): K-A
dating on the igneous rocks in Japan (I).
japan. Assoc. Min. Petr. Econ. Ceo/., jour.
vol. 51, no. 4, pp. 127-148, 4 text-figs., 7
tables. (in Japanese)
KNIGIIT, ].B. (1945): Some new genera of
the Bellerophontacea. jour. Paleont., val.
19, no. 4, pp. 333-340, pis. 49:- - (1956): New families of Gastropoda.
Washington Acad. Sci., jour. vol. 46, no.
2, pp. 41-42.
MIKAMI, T. (1965): The type Sakamotozawa
formation. Ceo/. Soc. japan, jour. val. 71,
no. 841, pp. 475-493. (in Japanese)- - (1969) : A sedimentological study of thelower Permian Sakamotozawa formation.
Kyushu Univ., Mem. Fac. Sci., Ser. D,
Ceo/., vol. 19, no. 3, pp. 331-372, 15 textfigs., pis. 46-52.
MINATO, M. (1960) : Three major orogenic
movementc; in Japanese Islands, with special remarks on granitic conglomerate ofmollasse type. Chikyu-Kagaku (Earth Science), no. 46, pp. 30-37. (in Japanese)- - (1966) : Paleozoic stratigraphy in the
Kitakami Mountains and the Abean orogenic movements in Japan. Kyoto Univ.,
Prof. S. MATSUSIIITA Mem. Vol., pp. 143159, 1 text-fig., 1 table. (in Japanese)- - (1968) : Basement complex and Paleozoic orogeny in Japan. "Pacific Geology"
1, pp. 85-96, 5 text-figs. Tsukiji Shokan
Pub!. Co. Ltd., Tokyo.
- - , HASHIMOTO, s., SUYA1v!A, K., TAKEDA,
Y., SuzuKI, Y., KAKIMI, T., YAMADA,
K., KIMURA, S., IsHIKAWA, T. und SuETO\!!, H. (1954): Biostratigraphie derpermischen Formation des Setamai-Gelandes im Slid-Kitakami Gebirge. (Stratigraphische und tektonische Untersuchungen des japanischen Paleozoikums, Teil
9.) Ceo/. Soc. japan, jour. val. 60, no.
708, pp. 378-387, 2 text-figs. (in Japanese)- - , KATO, M. and HASEGAWA, Y. (1964):
A note on the boundary between Pseudofusulina and Parafusulina zones in Japan.
japan Acad., Proc. val. 40, no. 10, pp.
827-831, 1 text-fig., 1 table.

114

Masaf~~mi--and KATO, M. (1965): Waagenophyllidae.
Hokkaido Univ., jour. Fac. Sci., Ser. 4,
Geol. Min., vol. 12, nos. 3-4, pp. 1-241,
56 text-figs., pis. 1-20.
MooRE, R.C. (1941): Upper Pennsylvaniangastropods from Kansas. State Geol. Surv.
Kansas, Bull. 38, pt. 4, pp. 121-164, pis.
1-3.
MoTEGI, M. (1956) : Geology of Kamiyasse
and Imo districts, southern Kitakami massif, Japan. Graduation Thesis, Tohoku
Univ., Inst. Geol. Paleont. (MS. in Japanese)
MuRATA, M. (1964a): Some middle Permian
Aviculopectinidae from theKitakami massif, Northeast Japan. Palaeont. Soc. japan,
Trans. Proc. N.S., no. 54, pp. 215-233, 5
text-figs., 6 tables, pis. 34-35.
- - (1964b): Geological age of the Kanokura
formation in the southern part of theKitakami massif, northeast Japan. Saito
Ho-on Kai Mus., Res. Bull., no. 33, pp.

MURATA
17-29, 1 text-fig., 1 table.
- - (1969) : Molluscan fauna of the Toyama
formation (Late Permian). Ibid., no. 38,
pp. 1-22, 2 text-figs., 7 tables, pis. 1-4.
- - and MArY A, S. (1964) : Geological ageof the Ubaishi formation. Geol. Soc. fapan, jour. vol. 70, no. 826, p. 382. (inJapanese)
NAKAZAWA, K. (1959): Permian and Eo-Triassic Myophoriidae from the Maizuru
zone, southwest Japan. Univ. Kyoto, Mem.
Coli. Sci., Ser. B, vol. 26, no. 2, pp. 193213, 7 text-figs., 1 table, pis. 3-4.
- - and NEWioLL, N.D. (1968): Permian bivalves of Japan. Kyoto Univ., Mem. Fac.
Sci., Ser. Geol. & Min., vol. 35, no. 1, pp.
1-108, 3 charts, 2 text-figs., 1 table, pis.
1-ll.
NEWELL, N.D. (1938): Late Paleozoic pelecypods; Pectinacea. State Geol. Surv.
Kansas, vol. 10, PP• 10-123, 42 text-figs.,
3 tables, pis. 1-20.

Explanation of Plate 13
Figs. 1-3. Bellerophon (Bellerophon) kitakamiensis MuRATA, n. sp.
1a, b. Right side and a pert ural views of a gum-type of the holotype; IGPS coli. cat. no.
91389, X l.
1c, 3. Enlarged view of the gum-type of the holotype and a paratype to show details of
the umbilicus and surface ornamentation; IGPS coli. cat. no. 31389, 91390A, x 2.
2a-c. Adapertural, left side and posterior views of the gum-type of a para type; IGPS
coli. cat. no. 91390B, x 2.
Horizon and Locality: Lower part of the Motoiwazawa Sandstone Member of the Sakamotozawa Formation (Early Permian) in the Motoiwazawa Valley, Sumita-cho, Kesen-gun,
Iwate Prefecture.
Figs. 4-6. Knightites (Reptispira ?) hanzawai MuRATA, n. sp.
4a-d. Adapertural, oblique adapertural, right side and posterior views of the gum-typeof the holotype; IGPS coli. cat. no. 91391, x 2.
4e. Enlarged view of gum-type of the holotype to show the details of surface ornamentation, x 3.
5a, b. Left side and adapertural views of internal mold of para type; IGPS coli. cat. no.
91392A, x2.
6. Ada pert ural view of the gum-type of a para type; IGPS coli. cat. no. 91392B, x 2.
Horizon and Locality: Same as figs. 1-3.
Figs. 7-10. "Murchisonia" n. sp.
7, 8. Apertural view of gum-types; IGPS coli. cat. nos. 91393A, B, x 2.
9, 10. Lateral view of gum-types; IGPS coli. cat. nos. 91393C, D, x 2.
Horizon and Locality: Same as figs. 1-3.

MURATA:

Sakamotozawa 111olluscan Fauna

K . KUMAGAI &S. 0HTOMO photo.

Plate 13

580.

Salcamotozawa Molluscan Fa~(na- - (1965) : Classification of the Bivalvia.
Amer. Mus. Novitates, no. 2206, pp. 125, 3 text-figs., 1 table.
- - (1969) : Mollusca 6, Bivalvia: in MooRE,
R.C., Treatise on Invertebrate Paleontology, Part N. Geol. Soc. Amer., & Univ.
Kansas Press, pp. N468-N470.
ONUKI, Y. (1937): On the Paleozoic formation near Sakamotozawa, Kitakami mountainland. Geol. Soc. japan, jour. vol. 44,
no. 522, pp. 168-186, 8 text-figs., 3 tables.
(in Japanese)- - (1938) : On the Chichibu system of the
Kesen-gun district, Iwate prefecture.
Ibid., vol. 45, no. 532, pp. 48-78, 5 textfigs., 10 tables. (in Japanese)- - (1965) : Geology of the Kitakami massif: One of the explanatory texts of thegeological map (scale 1: 100,000) of Iwate
Prefecture. Iwate Prefectural Office, pp.
1-187, 36 text-figs., 39 tables. (in Japanese)- - (1969) : Geology of the Kitakami massif, northeast Japan. Tvhoku Univ., Inst.
Geol. Paleont., Contr., no. 69, pp. 1-239, 55
text-figs., 32 tables, pis. 1-4. (in Japanese)
SAITO, Y. (1966) : Geology of the Setamai

115

district, southern Kitakami massif, northeast Japan. Ibid., no. 62, pp. 55-67, 3
text-figs., 1 table. (in Japanese)- - (1968) : Geology of the younger Paleozoic system of the southern Kitakami
massif, Iwate prefecture, Japan. Tohoku
Univ., Sci. Rep. 2nd Ser. (Ceo!.), vol. 40,
no. 2, pp. 79-137, 24 text-figs., 4 tables,pls. 18-19.
TAKEDA, T. (1963): Geology of the Tatsusobe district, Iwate prefecture. Graduation Thesis, Toholw Univ., Inst. Geol. Paleon!. (MS. in Japanese)W AAGEN, W. (1881): Productus Limestone
fossils. Paleont. Indica, Ser. 13, Salt
Range Fossils 1, pp. 75-183, pls. 7-16.
WANNER, C. (1922) : Die Gastropoden undLamellibranchiaten der Dyas von Timor.
Paliiont. von Timor, vol. 11, pp. 1-158,
pls. 1-21.
YAM ADA, Y. (1959): On the unconformityof the post-Nagaiwa pre-Sakamotozawa
epoch in the Hikoroiti district. Ceo!. Soc.
japan, jour. vol. 65, no. 771, pp. 713-724,
8 text-figs. (in Japanese)
YAMASHITA, N. (1957) : Mesozoic era. Assoc.
Ceo!. Collab., Tokyo. (in J'!-panese).

------

Azumane
Gujo
Hikami
Hikoroichi
Horooroshi
Kachizawa· Kanokurazawa
Karakuwa Peninsula
Kawaguchi
Kesennuma
Kogaizawa
Kowaragi
Maiya
Motoiwazawa
Nagaiwa

:liT

~l'f.

0

Ji:

;i)\

J:

di
H}: J'-CT
II t([{?i Jl!J, iP.

u+ tr iP.
J,if~~'l':,l;,!j

Jll

1=1

/~

'J]
l1i1 lll

Xl

cr- f!;;J iP.
;J\ IJ\(;)j(*~

7C {' :· il~

H.:

'".

{

Nagasaka
OdairaOhazamaOkunigiri
OrikabeOtomo
Sakamotozawa
Setamai
Sumita-cho
Takainari
Tatsusobe
YahagiYokamachi
Yokoi wazawa
Yukizawa

-F:

tR

*-

-'f)J}*

Jf! :rrr l;IJ

+rr

~

;;:_

;J\

iP.
:lJX
Ill: ILl :)j~
it ILl IDJ*!Ui fiT\ {iij

J:t fft l~ll
:X.

I'F

Fl JHJ
hYi '/:· iF-.!
}\.

'I~

-'

iJ~

116

Masafuqni Jl!J~URATA

Explanation of Plate 14
Figs. 1-4. Ps eudoactinodontophora yabei M uRATA, n. gen. n . sp.
1a, b, 4. Gum-t y pe of left and right va lves of the same indi v idual, holot ype; IGPS coil.
cat. no. 86885, x 1.
2. Gum-t ype of left valve, posterior part of hinge-plate shif ted slightly, para t ype; IGPS
coli. cat. no. 86886A, x i.
3a, b. Extern a l mold and gum-type of left va lve, para type; IGPS coil. cat. no. 86886B,
3a. x 1, 3b. x2.
Horizon and Loca li ty: Lower part of t he Motoiwazawa Sandstone Member· of tl1e Sakamoto zawa Fo rmati on (Early Permian) in t he Motoiwazawa Va ll ey, Sumi ta-cho, Kese n- gu n,
l wate Prefectur e.
Figs . 5-8. Towapteria nipponica NAKAZAWA a nd NEWELL.
5a- c. Externa l a nd in terna l molds a nd g um- type of left valve; IGPS coil. cat. no. 91395A,
x 2.
6a, b, Sa, b. Exte rnal mold an d gum-types of left va lves; IGPS coli. cat. nos. 91395B , D,
x 2.
7. Gum-type of left va l ve ; IGPS coil. cat. no. 91395C, x 2.
Horizon an d Locality: Same as fi gs . 1- 4.
Figs. 9, 11. Waagenoj;erna ( Permoperna) hayamii N AKAZA w A a nd NEWELL. ·9. Intern a l mold of right va lve; IGPS coli. cat. no . 91397, x 2.
Horizon and Loca li ty: Same as figs. 1-4.
ll.a , b. Externa l mold and gum-t ype of left va lve; IGPS coil. cat. no. 91398, x 1.
Horizon and Loca li ty: Middle pa rt of the Moto i wazawa Sandstone Member of the Sakamo tozawa Format ion (Ea rly Permian) in the Yoko i wazawa Va ll ey, so utheast of Orikabe ,Sumita-cho, Kesen-gun; Iwate Prefecture.
F ig. 10. Aviculoj;e cten ? sp .
Extern al' mold of left va l ve; IGPS coll. cat. no. 86884, x l.
Hori zo n a nd Loca li ty: Sa me as fi g. 1.1..
F ig. 12. AviculojJect en sp .
a, b. Exte rn a l mold and gum-t ype of ri g ht va lve; IGPS coli. cat. no. 91396, x 2.
Horizon and Locali ty : Sam e as figs. 1- 4.
Fig. 13. Taino ceras ilitalwmiense I-I AYASA KA.
Ve ntra l view of ste in ke rn ; coli. cat . no. 91394, x l.
Hori zon an d Loca li ty: Same as figs . 1- 4.

MURATA:K. K uMAGA I

Sakan~otozawa

Molluscan Fauna& S. OHTOMO photo.

Plate 14

Trans. Proc. Palaeont. Soc. Japan, N.S., No. 82, pp. 117-128, June 30, 1971

581.

CORRELATION OF LATE CENOZOIC MARINE SECTIONSIN JAPAN AND THE EQUATORIAL PACIFICLLOYD H. BURCKLE
Lamont-Doherty Geological Observatory of Columbia University
Palisades, New York, USAs :;ls:71J~ tJ:. ~~:>cn::Will::t-f-~~O){~!tJJ*If1:.ttmm<:.~WO)M 1:1: = l'j:IJ::l'fii':Hifi:!!:tP G :mi:!!:vc:bf;:_ :t>i.!fi!iff'.:!:Jiii\1!0) ~tJ:(I'9J-:n'!l::i::' :Wifi::t-f-i:f;J,.JitO) i4iJIJttttJ~~'l4:1C -::lv'"C~1JiiH>b,~l'j:IO)f!fJ.O)j~fl::.:.fi~Ftc "ttl!!.m%1\lil'tUt~xtJ:.;.:t:-~1-::i::'I"J-~cO)~Pffi 3 - P "',~O)tl\'i~~Ftc Ht*.!i:~~tc.o :Wit::t-'1'-i-'!'~O)v' <-::liPO) tifi~HHi B:;ls:71J~O) f&Ftvc t l±lJfi. L.., jilijJ:ti!,~O)*'-fl:t::i::'"iiJil~ICl.."Cv':t>o cO)UltiCJ: 1), z:.·~i-c·~X.I?~"C~tc.~Jm~~O)J:i!l~O)~f\::::i::(XO)J:'5 IUiT.IEi' :t> O)iJ~~ ~-c· <b :t> c O)~f,t.iiC)~ L-tc.o 1) lliiJII/\'1 J::f.~ Utitlf&lil:J'f~i!f~Mtvc:Mlt~ ~. 2) l'jl*lf-ffl.'t*lfff.i'cO)l:J't~'Hi to.:C G <fflrlJ lll~tfl'f~lc 111:18: L.., 3) "tcJ II~ l:tf~lil:J'f~l'jl*lfi:!!:::!:*ts"Tii~ttil~ <b :t>cO)MltvcJ: :t> c95~~~0)f&Jj';O)-tf~ (17JJX.Ii"tcJIIffll:J'f~U&JII~Ttf~) li/F!li;-ICJ::t>]!JU~Uil,<b:t>v'vi:ltffl~~O);B~tJ:.ii!(:J>::!:ffil.."Cv':t> J: -5 vcJl,X.:t>o .:tm.mrnli, 1) Rhizosolenia praebergonii O)jft{i::.IC J: :t>:ll'l:tflO) l±lJJl.li:Will:!Jil('"t'lil:J'f~f!'t~i:!!:TJ'f~ (Gauss .IEmtili.l\Jll'jltf~) IC, ~Jm~~'"t'liM&JIIf&l=j:!J'f~IC~?r!,IJ)/?~:t>o cO)fillvi:Will:!Jii('"C·Jftfi::.L..t:O)'"t', .:C~O)
S:;fs:7JJJft;dctolt :t>:®:tflO) /±',Jfi.li{rU¥~ C. [jj')~il'<b :t> v'vi:j~ICfJ:. :t> lif-e· <b :t>o 2) Thalassiosira nativa ~O)fillli, :Will:I!!.!U~ ~Jm~J&'.i-c·rn.J t-7i1'!1::!:'ffi-9 o 3) :Will:!Jil(-c·:f&JtJJI=jl*lfi:!!:tflJt)JIC*E.IY!Zi- :t> Coscinodiscus yabei il~"tcJ 11m-c· I"Jtiftvc *E.I!\X L.. "Cv' :t> c C. li, "tcJ II~ O)J::J'tH 1&ltll
l'jliflfiftvC.JmT :t, c C ::i::ffiTo
Lloyd H. BURCKLE
0sections of Japan (KANAYA, 1959; KorZUMI, 1966, 1968). These include suchforms as: Actinocyclus ellipticus GRUN.
var. javanicus REINHOLD, Coscinodiscus
endoi KANA YA, C. vetustissimus P ANTOCSEK, C. yabei KANA YA, penticula hustedtii
SIMONSEN and KANA YA, Rouxia californica PERAGALLO, R hizosolenia praebergonii MUCHINA and Thal(!ssiosira nativa
SHESHUK. The purpose of this paper isto report on the geologic ranges of these
species in the Equatorial Pacific and their
possible correlation to sections in Japan.
During the course of my discussion somequestions must be raised regarding theage of certain formations on Japan.
Since 1962, ships of the Lamont-Doherty
Geological Observatory have recovered

Introductory note
For the past year I have been studying
Late Cenozoic diatoms in deep-sea sediment cores recovered from the eastern
Equatorial Pacific. This work has been
carried out in conjunction with similar
studies on the Radiolaria, Foraminifera
and paleomagnetic stratigraphy in thesame cores (see for example; HAYS etal., 1969; SAITO et al., in prep.). In thecourse of this study it soon became apparent that some of the more stratigraphically useful diatom species arealso present in the Miocene and Pliocene
Received August 3, 1970; read September
13, 1970 at Tokyo.

117

Lloyd H. BU RCKLE

118

Table 1.
PositionCore No.
RC12-63
RC12-65
RC12-66

LatitudeLongitude

05•58'N
04•39'N
02•36. 6'N

142•39'W
144•58'W
148•12.8'W

more than 200 deep-sea sediment coresfrom the eastern Equatorial Pacific.
These cores range in age from Eocene toPleistocene and in length from less thana few centimeters to over 28 meters.
The Eocene cores are generally Radiolarian oozes with few diatoms, while
Oligocene and Early Miocene sediments
tend to be richly calcareous, containing
mostly coccoliths although some diatoms
and Radiolaria are also present. The
Middle Miocene to Pleistocene cores, on
the other hand, contain mostly diatoms
and Radiolaria with few calcareous
nannofossils and even fewer Foraminifera.
Since 1966, all cores taken by LamontDoherty ships have been oriented for
paleomagnetic measurements. This technique is especially useful to the marine
micropaleontologists because it permits
him to compare ranges of microfossil
species against actual time-lines (OPDYKE
et al., 1966; HAYS and OPDYKE, 1967;
HAYS et al., 1969). Of the cores recovered from the Equatorial Pacific since
1966, three are of special interest to thisstudy (Table 1). They all penetrate into
the Miocene and, on the basis of magnetic stratigraphy, have essentially complete Pliocene and Pleistocene sections.
One core (RC12-65) penetrates the Late
Miocene and bottoms in the uppermost
part of the Middle Miocene (Text-fig. 1).
The diatom stratigraphy and the paleomagnetic stratigraphy of these threecores will provide the basis for the dis-(M)

·Length(em)

4949±10
4868
4755

1558
2426
2800

Water Depth

cussion to follow.
Acknowledgements
I wish to thank Drs. T. SAITO and
N.D. OPDYKE for critically reviewing themanuscript and making numerous helpful suggestions. I am especially gratefulto Dr. OPDYKE for generously supplying
the author with records of the paleomagnetic stratigraphy for the cores usedin this study and to Dr. SAITO for advice
and help in searching through Japanese
literature. Thank are also extended to
Linda MURPHY for typing and proofreading the manuscript and to D. jOHNSON for drafting. The cores used in thisstudy were curated under the directionof Mr. Roy CAPO.
This work was supported throughgrants from the National Science Foundation (GA 1193 and GA 10635).

Previous work
Modern work on Equatorial Pacificfossil diatoms began in 1954 when KOLBE
published a study of diatoms in coresfrom this area taken by the Swedish
Deep-Sea Expedition. Besides making ataxonomic study, he listed those forms
which were restricted to the pre-Pleistocene and made an attempt to define the
Pliocene/Pleistocene boundary in one of
the cores (SW76). KANA YA (1969) subsequently presented evidence that the581.

Correlation of Late Cenozoic Sections

boundary defined by KOLBE was really.:an erosiona.l unconformity.
MUCHINA (1963) discussed geologic
ranges of selected diatom species froma single core from the Equatorial Pacific.:and included in her discussion two stratigraphically important species: Rhizoso.lenia praebergonii and Thalassiosira con.vexa (MUCHINA, 1965). In subsequent. papers (MUCHINA, 1966, 1969) these spe·cies were used as early Pleistocene guidefossils with the first appearance of Th.
convexa being used to define the Pliocene/
Pleistocene boundary and the range ofR. praebergonii being used to define theupper part of the lower Pleistocene.

119

MUCHINA (1969) further reported on theoccurrence of Coscinodiscus yabei KANAYA in Equatorial Pacific sediments anddefined 'it as a largely Miocene species.
More recently HAYS et al. (1969) pub·lished a combined· biostratigraphic (Fo·raminifera, Radiolaria, diatoms and discoasters) and paleomagnetic study of
selected Pliocene-Pleistocene cores fromthe Equatorial Pacific while BURCKLE(1969) related a Late Miocene to Pleistocene diatom zonation for this region to
zonations based upon other microfossil
groups as well as to the record of paleomagnetic reversals. These last two
papers will be discussed more fullY

Ja.G:'iETIC
EPOCH

FORMA- OGA

TION DIATOM
ZONES

i1

BRUNHESJARAMILLO

MATUYAMAOLDUVAI7

GAUSS
GILBERT
B

EPOCH 5
EPOCH 6I

EPOCH7

EPOCH 8
EPOCH 9I-~---....______ __

---~

..._

EPOCH 10
EPOCH 11

Text-fig. 1. Proposed correlation between the Equatorial Pacific and the Oga Peninsula·section, Japan. Letter designations indicate the following species: A. Rhizosolenia praebergonii MucH. ; B. Thalassiosira nativa SHESHUK. ; C. Denticula hustedtii SIMONSEN and·. KANAYA; D. Coscinodiscus yabei KANAYA; E. Coscinodiscus endoi KANAYA; F. Rouxia.californica PERAGALLO; G. Coscinodiscus vetustissimus PANTOCSEK. Japanese diatom zones.are after KOIZUMI, 1968.

120

Lloyd H. BURCKLE

later on.
Modern work on Japanese fossil diatoms began in 1950 with publication by
ICHIKAWA on a comparison of marine
Miocene diatoms between the Noto Peninsula and the environs of Kanazawa
City. KANA YA (1959) defined several
diatom zones in the middle Miocene Onnagawa Formation of the Oga Peninsulaand demonstrated that these zones wererecognizable over a considerable area.
This observation was amply borne out
by subsequent work on the Miocene of
Hokkaido (SAW AMURA and YAMAGUCHI,
1961, 1963) and of Honshu (SAWAMURA,
1963). Eventually it came to be recognized that there were significant timeparallel, sequential changes in diatom
species combinations that could be recognized in widely different localities(SAWAMURA, 1963). In 1966 KOIZUMI discussed the late Tertiary diatoms of the
Ajigasawa district and in 1968 establisheda diatom zonation for the middle Miocene
to Pliocene of the Oga Peninsula.

Stratigraphy
Paleomagnetic Stratigraphy- HARRISON
and FUNNELL (1964) and FULLER et a!.
(1966) were the first to record polarity
reversals in deep-sea sediment cores
while OPDYKE et a!. (1966) were the firstto show that the direction of remanent
magnetism, can be correlated from core
to core. These same authors also related
paleomagnetic correlations to correlations based upon microfossils. Where
the paleomagnetic stratigraphy is known,
the ranges of microfossil species can bematched with it. Thus, for the last four
million years, an absolute or near absolute
time value can be placed upon the firstand last appearance of species.
Subsequent work on deep-sea cores has
served to strengthen the interdependenceof paleomagnetic stratigraphy and "biostratigraphy (see for example; HAYS andOPDYKE, 1967 ; BERGGREN et a!., -1967 ;HAYS et al., 1969). Additional work has·also pushed our knowledge of geomagnetic reversals back into the Tertiary.
Recently, FosTER and OPDYKE (1970}
reported on the paleomagnetic stratigraphy on a long core (RC12-65) recovered from the eastern, Equatorial Pacific.
The core extends into the uppermost
part of the Middle Miocene, is essentiallycontinuous and contains eleven magnetic·
Epochs (Text-fig. 1). As mentioned previously, this core along with several
others from the Equatorial Pacific forms.
the basis of my discussion (Table 1).
Cores used in this study were internally oriented by cutting a groove down
its length as it is extruded on board
ship. Into this groove a string is laid"
which serves to retain the orientationof the core during shipment. In the·laboratory, the core is split along thisstring making possible the detection ofreversals as 180° shifts in magnetic declination. Specimens were removed fromthe split cores at intervals of from 10'
to 20 em and measured on a 5 cps spinner magnetometer (FOSTER, 1966) afterpartial demagnetization by alternating
fields.
Middle/Upper Miocene Boundary-The
Tortonian stage was originally proposedby MAYER EYMAR in 1857. More recently,
GIANOTTI (1953) proposed a type sectionin the valley of the Rio MazzapiediRio De Castellania, east of Tortona. In
a discussion of this stage, CIT A and BLOW
(1970) present evidence that the base of
the Tortonian is referable to a horizonin the upper part of Zone N15 (BLOW,.
1969). This is the Globorotalia (T.) continuosa Zone of BLOW (1969) and the·Globorotalia menardii Zone of BoLLI.
(1957).

581.

Correlation of L.ate Cenozoic Sections

Because there are few foraminifera in
our Equatorial Pa~ific cores it was notpossible to use these criteria for defining
the base of the Tortonian. However,
WILCOXON and BRAMLETTE (1967), studying Middle Tertiary samples from theCipero section of Trinidad have related
nannoplankton zones to. the foraminiferal
zones of BOLLI. The most important of
the nannoplankton within the G. menardii
Zone is Discoaster hamatus MA,RTINI and
BRAMLETTE which appears to be exclusive to this zone. In one of our Equatorial Pacific cores (RC12-65) D. hamatusis present in two samples near the bottom of the core within Geomagnetic
Epoch 11. Ruling out any significant
hiatuses in the lower part of the core I
suggest that the very bottom of core
RC12-65 penetrates into the up.permost
part of the Middle Miocene and the
Middle/Upper Miocene boundary falls
somewhere within Geomagnetic Epoch 11.
Miocene/ Pliocene Boundary-Using
planktonic Foraminifera it has, so far,proved difficult to relate the Miocene/
Pliocene boundary in Italy with sections
elsewhere in the world. The main reason
for this is that the type Lower Pliocene{Tabianian of MAYER EYMAR, 1868) contains a planktonic foraminiferal faunaindigenous to the intra-Mediterranean
region. To circumvent this problem
some authors (for example, BLOW, 1969 ;PARKER, 1967) have studied the morerichly fossiliferous " trubi beds" (typesection of the Zanclian of SEGUENZA,
1868) of Sicily, a unit which is believed
to be correlative with the Tabianian ofnorthern Italy. Recently, however, BLOW
(1969) and CIT A and BLOW (1970) havepointed out that the base of the Zanclian
is younger than the base of the Tabianian and, therefore, not strictly correlative. BLOW (1969) indicates that the
Miocene/Pliocene boundary, if based on

121

the beginning of the Zanclian, falls within
his Zone N18, whereas, if it is based upon
the beginning of the Tabianian the epochal boundary will fall near the Zone
N17 /N18 boundary.
Because of the presence of the easily
recognizable and widespread Sphaeroidinella dehiscens datum some 12 to 15 meters
above the base of the " trubi beds" CIT A
and BLOW (1970) argue that the Zanclian
be utilized as the base of the Pliocene
in preference to the Tabianian. This
criterion was applied to a long core
(RC12-66) from the Equatorial Pacific by
SAITO et al. (in prep.) and found to fall
below the " c " event of the Gilbert Reversed Magnetic Epoch (Text-fig. 1). If
this criterion is to be used, therefore,
the Miocene/Pliocene boundary would
occur near the boundary of the Gilbert
Reversed. Epoch and Magnetic Epoch 5.
If the beginning of the Tabianian isused as the base of the Pliocene thanthe Miocene/Pliocene boundary, based
upon faunal criteria developed by SAITO
et al. (in prep.) should fall between theend of Magnetic Epoch 6 and the beginning of the Gilbert Reversed Magnetic
Epoch. Sin~e the Tabianian has priority
as the type section for the Lower Pliocene I choose to follow the suggestionof SAITO et al. (in prep.) in the placement of this boundary with respect tothe magnetic stratigraphy.
The placement of the Miocene/Pliocene
boundary in japan has been a matter ofsome concern owing to the paucity inthis part of the section of fossils which
can be used to correlate with the standard sections of Europe. In the Oga Peninsula section the boundary is normallyplaced at the contact between the Kitaura Formation and the Wakimoto Formation lsee for example, SAITO, 1963).
TAKAYANAGI and 0BA (1966) reported
that the highest occurrence of Sphaeroi-

122

Lloyd H. BURCKLE

dinellopsis seminulina (SCHWAG.) within
the Kitaura Formation and placed the
Miocene/Pliocene boundary at the topof this unit. KOIZUMI (1968) followed
the " general practice " but points outthat the exact positioning of the boundary is open to question.
Pliocene/ Pleistocene Boundary-During
the latter half of the 19th century andearly part of the 20th century, the stratigraphy of the continental and marine
Pleistocene was roughed out in Europe.
An important contribution was made by
DE STEFANI .(1876) who introduced thefollowing chronological succession in
Italy : Pliocene, Lower Post Pliocene andUpper Post Pliocene. The base of theLower Post Pliocene was marked by theimmigration of cold water species into
the Mediterranean. GIGNOUX ·(1910, 1913)
introduced the term Calabrian, and designated the type section for the Calabrian at Santa Maria de Catanzaro insouthern Italy. He differed with DE
STEFANI's chronology in placing the Calabrian in the uppermost part of the Pliocene. This designation was never universally accepted and RuGGIERI and SELLI(1950) redesignated it as the lowest Pleistocene stage. The. 18th International
Geological Congress (London, 1948) madea recommendation that the lower Pleistocene should include as its basal member in the type-area the Calabrian formation and invited the Italian GeologicalSociety to select a type area for the
Pliocene/Pleistocene boundary.
In 1961, EMILIANI et at. proposed thatthe type Plio-Pleistocene boundary berecognized at Le Castella (Calabria).
Their reasons for proposing this section
were that it was close to the classic
Calabrian section at Catanzaro, wasthicker, and less tectonically disturbed
than the section in Catanzaro.
A proposal was made and accepted at

the 7th INQUA Congress in Denver, Colorado,· USA (1965) that the type sectionof the Plio-Pleistocene be established at
Le Castella (Calabria), Italy. However,.
as RICHMOND (1967) has pointed out, this
proposal has no legal force since it must.
be passed on by the International Geological Congress. Most workers, however, accept the Le Castella section as.
the type section for the Plio-Pleistocene
boundary.
The Pliocene/Pleistocene boundary in
deep-sea sediments was first defined by
ARRHENIUS (1952) on the basis of carbonate content. KOLBE (1954) utilized paleontologic criteria in placing the boundary in core 76 of the Swedish Deep-Sea
Expedition-a boundary which KANAYA(1969) has since shown to be an unconformity. RIEDEL (1957) suggested that.
the last appearance of Pterocanium prismatium RIEDEL and Eucyrtidium elongatum peregrinum RIEDEL in tropical Pacificcores be used to make the base of the
Pleistocene. ERICSON et at. (1963) reported on a significant floral and faunalchange in eleven deep-sea cores which
they suggested be used to define the'beginning of the Pleistocene. This boundary was approximately correlative withthe last appearance of Pteror:anium Prismatium (RIEDEL et at., 1963) in the Equatorial Pacific.
Although T AKAY ANAGI and SAIT0(1962)
first suggested that their new species.
Globorotalia tosaensis may be ancestral
to G. truncatulinoides (D'ORBIGNY) it was.
BANNER and BLOW (1965) who applied
this criterion to the Pliocene/Pleistocene
section at Le Castella. Near the base of
the Calabrian they noted the first evolutionary appearance of G. truncatulinoides
from G. tosaensis. The utility of thiszonation was demonstrated by PARKER(1967) in deep-sea cores from the tropical Indo-Pacific. BERGGREN et al. (1967),581. Correlation of Late Cenozoic Sections
in a combined paleomagnetic and paleontologic study of a deep-sea core fromthe North Atlantic, discovered that thisevolutionary transition occurred in the
Olduvai Event of the Matuyama Reversed
Magnetic Epoch at about 1.71-1.86 m. y.
(FOSTER and OPDYKE, 1970). This finding was later corroborated by GLASS
et al. (1967). Subsequent papers havedeveloped criteria from other microfossil
groups for defining this boundary. HAYS
(in HAYS et al., 1969), for example, foundthat Pterocanium prismatium disappeared
just after the Olduvai Event in the Equatorial Pacific, while BURCKLE (in HAYSet al., 1969), working on the same core,found that Rhizosolenia praebergonii also
disappeared just after the Olduvai. Subsequently, BuRCKLE (1969) pointed outthat the first appearance of Pseudoeunotia
doliolus (WALL.) GRUN. occurs in the
Olduvai Event and may be used to define
the base of the Pleistocene.
In the Japanese section the transition
from G. tosaensis to G. truncatulinoides
has been recorded by TAKAYAMA (inIKEBE, 1969) in the Umegase Formationof the Boso Peninsula, central Japan justbelow the U6 tephra. Concommitantwith this, NAKAGAwA et al. (1969) haveshown that the U6 horizon corresponds
to a magnetic polarity event which iscorrelated with the Olduvai.
Discussion of floras

Having defined the Late Cenozoic epoch
boundaries with respect to the various
biostratigraphic and paleomagnetic criteria we now have the basis by which
we can relate the Late Cenozoic diatom
zones in the Equatorial Pacific to thoseon the Japanese Island. Of the several
Miocene-Pliocene diatom species which
occur in both the Equatorial Pacific andJapan, two are considered most signifi-

123

cant: Rhizosolenia praebergonii and Coscinodiscus yabei (Plate I). As can beseen in Text-fig. 1, R. praebergonii first
appears in the middle of the Gauss
Normal Magnetic Epoch, a time-interval
which we identify with the lower partof the Upper Pliocene (HAYS et al., 1969).
Since this species bears a fairly close
resemblance to R. bergonii PERAG., I
suggest that this species is its mostimmediate ancestor. In fact, within a 10
em interval below the first appearance ofR. praebergonii a few forms are present
which are morphologically intermediate
between R. bergonii and R. praebergonii,
indicating that its first appearance inthe Equatorial Pacific is evolutionary
rather than ecological.
Except for its occurrence in the Oga
Peninsula section of Japan (KOIZUMI, 1968)
R. praebergonii appears to have been
restricted to the low latitudes. It has
not been found in the North or South
Pacific (DONAHUE,· Personal Communication) nor has it been reported in any of
the higher latitude land sections in thecircum-Pacific area. Its presence inJapan, however, may be attributed to
the northward flowing warm water Tsushima Current (ASANO, 1957).
I
KOIZUMI (1968) reports the first appearance of R. praebergonii in the middle ofthe Miocene Funakawa Formation of the
Oga Peninsula (Base of Diatom Zone 4).
The fact that this species appears tohave originated in lower latitudes suggests that a Miocene designation for the
Funakawa is, in part at least, incorrect.
If a direct correlation is drawn between
the first appearance of R. praebergonii
in the Equatorial Pacific and that in the
Oga Peninsula section, the middle partof the Funakawa Formation should beearly Late Pliocene in age, or younger.
This means that the overlying Kitaura
Formation, a unit which is normally

T24.

Lloyd H. BURCKLE·placed within the Miocene, should also
be moved up .into the Pliocene. Should
the range of R. praebergonii in the Oga
Peninsula section approximate that of
the Equatorial Pacific, the Pliocene/Pleistocene boundary should fall within the.upper part of the Kitaura Formation or
the Shibikawa Formation.
That this correlation is reasonable
seems to be borne out by examinationof ranges of other species which arecommon to both Japan and the Equatorial Pacific. Thalassiosira nativa, forexample, first appears in Epoch 5 (latest
Miocene) in Equatorial Pacific cores and,
although its occurrence is sporadic,
ranges concurrently with R. praebergonii.
In the Japanese section, Th. nativa appears in the lower part of the Funakawa
Formation (Oga Diatom Zone 3) andranges concurrently with R. praebergonii
to the upper part of Diatom Zone 5(KOIZUMI, 1968). The species Coscinodis.cus vetustissimus also has similar ranges
in the Equatorial Pacific and Japan.
A noticeable departure from this pattern is Denticula hustedtii. In the Equatorial Pacific, this form disappears in thelower part of the upper Miocene. Thisobservation is borne out by MUCHINA{1969) who places the range of D. hustedtii in her upper Miocene and lower
Pliocene. In the Japanese section, on theother hand, KOIZUMI (1968) records thisspecies well into the upper Pliocene.
Such an observation appears to be consistant with my results for higher latitudes where I see this form ranging up
through much of the Pliocene.
Still another important form found inboth the Equatorial Pacific and Japan is
Rouxia californica. Although describedby PERAGALLO, it was HANNA (1930) who
first emphasized the stratigraphic valueof this species. He pointed out that it
occurs abundantly in a narrow zone

some 500 feet below the top of theMonterey shale and its stratigraphic
equivalents. KANAYA (1959) reported itfrom the Matazawa Formation of Japanbut not from any of its stratigraphic.equivalents. KOIZUMI (1968), on the other
hand, does not report its occurrence
from the Oga Peninsula section. In
Equatorial Pacific cores this form occurs
rarely in the middle part of the upper
Miocene (i. e. approximately in the uppermost part of Geomagnetic Epoch 8
and the lower half of Geomagnetic Epoch
7). Since this species is rare in the
Equatorial Pacific we cannot draw anexact correlation between high and low
latitudes. However, the range of thisspecies in higher latitudes must encompass the middle part of the upper Miocene.
A final species of importance to both
the Japanese and Equatorial Pacific section is Coscinodiscus yabei. KANA YA(1959) described and named this species
and pointed out its importance as a
middle Miocene marker fossil. The valueof this form in correlation has been demonstrated by a number of Japanesediatomists (see for example ; SAw AMURA,
1963 ; ONO, 1968; KOIZUMI, 1968). In the
Equatorial Pacific, BURCKLE (1969) notesthat this species ranges up into the lower
part of the. upper Miocene, while MuCHINA (1969) records a sharp drop inabundance for the species across her
Miocene/Pliocene boundary and thennotes its sporadic occurrence throughout
the Pliocene. In Text-fig. 1, I present evidence that this species disappears well
below the Miocene/Pliocene boundary.
It would appear then that KANAYA's(1959) conclusion that the last appearanceof this species defines the top of the
Middle Miocene is essentially correct
although my data places its last appearance somewhat later in the early Late

581. Correlation of Late Cenozoic Sections:Miocene.
If we accept the last appearance of C.
yabei and the first appearance of R. praebergonii as valid datum points which can·be correlated with the Equatorial Pacific·section then it follows that the Miocene/
Pliocene boundary in the Oga Peninsula
section must fall in the upper part of
the Onnagawa Formation or the lower
half of the Funakawa Formation. Sucha correlation also imp,lies that this partof the section between the upper partof the Onnagawa Formation and thelower part of the Funakawa Formation{KOIZUMI's Diatom Zones 2 and 3) has
been greatly shortened. Forms such as
R. californica which occur between theupper limit of C. yabei and the lower
limit of R. praebergonii in the Equatorial
Pacific have not been reported from asimilar stratigraphic position in the Oga
Peninsula section (KOIZUMI, 1968).

Summary and conclusions
In this report I have tried to pointout the utility of diatoms in correlaitng
between Late Cenozoic sediments in the
Equatorial Pacific and the Japanese Islands. In this case, their value is further
enhanced because the diatom zones inthe Equatorial Pacific have been related
to zonations based upon other microfossil groups as well as the paleomagnetic stratigraphy. Such an interdisciplinary approach permits us to develop
fossil diatom criteria with which· to define epoch boundaries.
When such criteria are applied to the
Oga Peninsula section it becomes appar·
ent that some adjustment i.n the age
designations of these units are in order.
These adjustments may be summarized
as follows:
1. The upper part of the Funakawa
Formation and the oveilying Kitaura

125. Formation, units which _have beenplaced in the Miocene, should be as·signed to the upper part of the Pliocene.
2. The Miocene/Pliocene boundary, if
it is present in the Oga Peninsula sections, probably falls within the lower
part of the Funakawa Formation.
3. The upper part of the Onnagawa
Formation probably extends into theLate Miocene.
4. Since some parts of the Oga Peninsula section appear to be greatly shortened or truncated (eg. lower part of
the Funakawa and upper part of the
Onnagawa Formations) it is possiblethat unconformities or at least intervals of reduced sedimentation rates
are present.
The basis upon which the above conclusions are drawn may be summarized
as follows:
1. The first evolutionary appearanceof R. praebergonii in the Equatorial
Pacific occurs in the middle part of
the Gauss Normal Magnetic Epoch(early Late Pliocene). In the Oga Peninsula section it first appears in the
middle of the Funakawa Formation(Base of Diatom Zone 4). Available
evidence indicates that this form waslargely restricted to tropical and subtropical water and its first appearancein higher latitude sediments must
either be correlative with or post-date
its first appearance in lower latitude
sediments.
2. The first appearance of Th. nativa
in the Equatorial Pacific occurs inGeomagnetic Epoch 5 near the Miocene/Pliocene transition and ranges
concurrently, though sporadically, with
R. praebergonii. In the Oga Peninsula
section, Th. nativa first .appears in thelower part of the Funakawa Formation

Lloyd H. BURCKLE

126(Diatom Zone 3) where I suggest the
Miocene/Pliocene boundary might beplaced.
3. In the Equatorial Pacific, Coscinodiscus yabei extends into the lower
part of the Upper Miocene while in
the Oga Peninsula section it last occurs in the upper part of the Onnagawa Formation (Diatom Zone 1). KANAYA (1959) and, later, KOIZUMI (1968)
used the last appearance of this species · to define the middle Miocene.
Although it would be premature to
say that the last appearance of thisspecies in Japan and in the Equatorial
Pacific is time-correlative, I would
sugggest that part of the Upper Miocene may be also included in the Onnagawa Formation.
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128

Lloyd H. BURCKLE

boundary. Science, 159, p. 410.
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Ibid., 12, no. 11, pp. 885-890, 2 figs.

-.· - and -.- (1963): Subdivision of Miocene by fossil diatom in the Tsubetsu
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Planktonic foraminifera from the Nobori
Formation, Shikoku, Japan. Tohoku Univ.
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and significance of planktonic foraminifera from the Oga Peninsula. Ceo!. Soc.
japan, jour., 72, pp. 35-47. 4 text-figs ..
WILCOXON, }.A. and BRAMLETTE, M.N. (1967) :Middle Tertiary calCareous nannoplankton of the Cipero section, Trinidad, W.I.
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pis.
LAMONT-DOHERTY GEOLOGICAL OBSERVATORY CONTRIBUTION 1673.

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Transactions and Proceedings of the PalaeontologicalSociety of Japan

New Series No. 82

June 30, 1971

CONTENTS
TRANSACTIONS
578. Hu, Chung-Hung and TAN, Li-Lin: Ontogenies of two Upper Cambriantrilobites from northern Black Hiiis, South Dakota . . . . . . . . . . . . . . . . . . . . 61
579. HAY AMI, Tomoko: Some Neogene Cheilostomata (Bryozoa) from: Okinawajima......... . ............... . . . ...... . ..... . ....... .. .................. 73580. MURATA, Masafumi: Fusulinid biostratigraphy and moiluscan fauna fromthe uppermost part of the Sakamotozawa formation, and the pre-Kanokura unconformity, in the southern part of the Kitakami massif, Northeast Japan.. . ..... ... .... . .. . ............... . ................. . . . ....... 93581. BURCKLE, Lloyd H.: Correlation of Late Cenozoic marine sections in Japanand the Equatorial Pacific . .................. . . ... ........ . ...... . ...... 117