Transactions and Proceedingsof thePalaeontolqgicalSociety of Japan,,
New Series

No. 85

Palaeontological Society of Japan
April 20, 1972

Editor: Takashi HAMADA
Associate editor: Yasuhide IWASAKI

Officers for 1971 - 1972
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Trans. Proc. Palaeont. Soc. Japan, N. S., No. 85, pp. 245-259, pis. 29, 30, April 20, 1972

591.

ONTOGENY OF THREE CEDARIA ZONE TRILOBITESFROM UPPER CAMBRIAN, MONTANA*CHUNG-HUNG HU
Department of Biology, Nanyang University, Singapore**-c :/ !l 7-1-I-IJ:;·~~ 'h :/ 7" ~ 7*0) Cedaria 1\~=,:)[::::::•x~!R :=:f,llO)iibH:>J.:§E~: ~t::i~ -c :/ !l T-1+1"'T 1 '/ :/ 'h 7 :/7' 1 0)_]·.)}1177 :/ 7' ~ 7* Cedaria ;:;::f;::_~-9- 0 !::" '" !f ~ .L..~ 0)/~Efd!:.Tiffi!G
fcv'i3:-;!ix0)::::::~~1l-?1!9iilf:.J'J. C1roil'l!lt~Uf0 i.i;fr'i:lc·-n-'0, .:::.:lci?O) '5 'G:=:Z.f!EO) 3 fir(, -Tt.;::h'G Syspacheilus dunoirensis, Nixonella montanensis, Baltagnostus beltensis (C"?v'L,.:CO)f0jf*J£1=-'2w:.J.....::t.=if.i'ilf,;, '%-O)flf'i Coosella convexa -? Crepicephalus deadwoodensis:to J::: l1 Tricrepicephalus blountensis t.;:: c'O))E1=-v:=. 1]!WJ_-9 0 ,.~•.7J;;:!,.0 fJ, ~=H\f'i ~;·1 fl~ tc,
Kingstonia ara :to J::: tF Komaspidella laevis \C, 'i t:~:::':O)l'J't:'i IC, Kormagnostus simplex fC, .:Ch.:f'hj~:l,"Cv'Q.:::. ci.J;~jajj L..t.=,

L..t.=i.J;-:> "C,~rl"¥:i'i'~fcili:HdYJi,f,'2<b--:JtO)cf1HR-c~0,t.;:::F;;,.:c-O)a~ft~'2t&~t..k,.:::.hi?0)0-*JH'i**1t(l'~tJ:v' l..l'i5J

Syspacheilus dunoirensis vC"?v'"Cv'i,m ili €

colored, medium crystalline limestone,
containing an abundance of trilobite
fragments, inarticulate brachiopods, anda few intraformational pebbles. The geologic positions of the materials belong
to the Pilgrim formation, Cedaria zone,
Upper Cam brian.
The ontogenetic metamorphosis of
Syspacheilus dunoirensis is very similar
to those of Coosella convexa TASCH (Hu,
1968b), Crepicephalus deadwoodensis Hu(1968a), and Tricrepicephalus blountensis
RESSER (unpublished material); that of
J\''ixonella montanensis LOCHMAN is close
to Kingstonia ara (WALCOTT) (Hu, 1968b),
Komaspidella laevis RASETTI (Hu, 1970);
and that of Baltagnostus beltensis LOCHMAN to Kormagnostus simplex RESSER(Hu, 1968a). All members within thesame group possibly have close phylogenetic relationship, and belong to asame genetic hierarchy.
The author is deeply indebted to Dr.
K.E. CASTER, University of Cincinnati, for

Introduction
The purpose of the present study is
to illustrate the ontor.;enetic developmentof Syspacheilus dunoirensis (MILLER),
Nixonella montanensis LOCHMA!\', Baltagnostus beltensis LOCHMAN, and thesexual dimorphism of Syspacheilus dunoirensis (MILLER). The ontogenetic development of the first two species iswell known, but is incompletely known
for the last one. Both the ontogenetic
separation and the sexual determinationof the trilobites are based on the schemes in the author's earlier works (Hu,
1964, 1968a, 1970, etc.).
The materials were collected fromwest-side, South-Boulder Creek, Madison
County, Montana, and are light gray* Received Nov. 10,1970; read Jan. 23, 1972.
** Present adress : Earth Science Department, Cheng Kung University, Tainan, Taiwan, Republic of China.

245

Chung-Hung Hu

246

his supervision, thanks also go to Dr.
Anne JoHNSON, Nanyang University, forreading over the present manuscript.
The figured specimens are all stored in
the Geology Museum, University ofCincinnati, Ohio (U. C. M.). The financial
expenses of the present study were
supported by Miss Nancy NUN Science
Research Foundation, Nanyang University.
Systematic de3cription

Family Crepicephaliidae KOBA Y ASH!, 1935
Genus Syspacheilus RESSER, 1938
Syspacheilus dunoirensis (MILLER)
Pl. 29, figs. 1-34, and Text-fig. 3a-k.
Blountia dunoirensis MILLER, 1936, p. 27, pl.
8, figs. 25, 26.
Syspacheilus dunoirensis (MILLER) : LocmiAN& DUNCAN, 1944, p. 131-132, pl. 11, figs.
44, 45; pALMER, 1954, p. 734, pl. 78, fig.
9; DELAND & SHAW, 1957, p. 561, pl. 64,
Syspacheilus dunoirensis var. (MILLER) :LocHMAN & Hu, 1961, p. 135, pl. 26,.figs. 26, 37-39.
Syspacheilus accidens LocHMAN, 1950, p. 342,
pl. 50, figs. 25, 26.
Syspacheilus praecedens var. elongatus LocHMAN & Hu, 1961, p. 136, pl. 27, figs. 1928, 30.
Coosella vagrans LociiMAN & Hu, 1961, pl.
26, figs. 49-54.

Diagnosis:
Cranidium trapezoidal;
anterior border broad, con vex; glabella
conical; preglabellar field medium wide;
occipital ring crescentic, bearing a tiny
median tubercle. Fixigena less than
one-half the width of glabella; posteriorborder same width as the occipital ring.
Librigena subtrapezoidal having a rather
small genal spine ; ocular platform thesame width as lateral border. Pygidium
broadly kidney shaped, convex with two

axial rings ; marginal border broad andflat. Outer skeletal surface granulated,
and inner surface punctured ; a pair ofelongated pits on the anterior furrow,and irregular concentric ridges along
pygidial margin.
Remarks: LOCHMAN & HU (1961) reported that there are four distinct species within the present genus: they are
Syspacheilus typicalis RESSER, 1938, S.
praecedens LOCHMAN & Hu, 1961, S.
camurus LOCHMAN, 1940, and S. dunoirensis (MILLER, 1936). The first two
species have broader flat preglabellar
fields and in the last two, they are
narrow and steeply slope downward.
Furthermore, S. dunoirensis and S. praecedens have slender glabella, whereas
those of the other two are broader. The
materials which I have studied could besegregated into two different morphologic groups. The first group conforms
with " S. dunoirensis" and the second to"S. praecedens ". These bimodal traits
are here interpreted as the presence ofsexual dimorphism within the same
species population and are found in thesame ecological habitats. The first groupis presumably the female and the second
the male. If this postulation is acceptable then the S. typicalis and S. camurusare possibly another example of thedifferent sexual representatives of thesame species.
The early ontogenetic development of
the both sexes are indistinguishable: all
immature forms have the same morphologic characteristics, but in their latestages the cranidium is gradually differentiated into two forms; one groupwith slender glabella, flat preglabellar
field, and broader pygidial margin, andthe other has broader glabellar, tilted
preglabellar field, and narrow pygidial
margin.
Coosella vagrans LOCHMAN & Hu, 1961

591.

Ontogeny of three Cedaria zone trilobites

a

247

b

g

h

c

d

f

e

k

Text-fig. 1.

Syspache£/us dunoirensis (MILLER).

a, Anaprotaspis, x 50; b, Metaprotaspis, x 50; c, Paraprotaspis, x 32; d, Early meraspid
cranidium, x 20; e, f, Two late meraspid cranidia, x 9, x 8; g, Librigena, x 5; h, k, A
male pygidium and a cranidium, x '1, x 4; i, j, A female cranidium and a pygidium, x 6,
x20. (all drawings were made from photographs.)·has no distinct characters by which it·can be separated from S. dunoirensis
except the "C. vagrans" has the cranidium slightly flattened. This feature
is possibly due to compaction of the-deposits or to individual variation, but
has no specific significance.

Syspacheilus dunoirensis (MILLER),"male"

Pl. 29, figs. 14, 21, 23, 25-29, 31
and Text-fig. lh, k.

Description: The cranidium is trapezoidal in outline, highly convex; glabella
conical, short and broad, and with rounded anterior margin; the preglabellar
field is of medium width, slopes downward from the anterior glabellar, andinclined about 45 degrees; the anterior
furrow is deep and broad, possessing apair of elongate pits laterally; the248

Chung-Hung Huanterior border is narrow crescentic,
convex, arching forwardly; the occipitalring is convex both vertically and posteriorly, bearing a small median node;
the broad and deeply impressed occipital
furrow curves forward on the axial line
(sag.), and deepens both posteriorly andlaterally with a pair of elongate pits.
The fixigena is narrow, about one-halfthe width of the glabella, medium width,
convex ; the medium sized palpebral lobe
is sickle-shape, situated on the mid-lineof the glabella (tr.), and well delimited
by palpebral furrow; the palpebral lobe
is indistinct, which extends to theantero-lateral margin of the glabella
from the anterior palpebral lobe, andarches forward; the facial suture is
opisthoparian, its anterior branch is·slightly divergent and convex, and theposterior one divergent-straight, andconvex.
The subtrapezoidal librigena is convex and has the ocular platform narrowed; the large ocular ring is connected to both anterior and posterior
free margins ; the lateral furrow isshallow, and narrower than the lateralborder; the lateral border is horizontal,
convex, possesses a rather small genal
spine; posterior librigenal border absent;
the genal angle or the posterior freemargin curves into the genal spine toform a broad rounded angle and a shortbroad base indentation.
Pygidium is lenticular or kidneyshaped, convex, occupied by a broadand short axial lobe; the axis is divided
into one or two convex rings and abroad terminal portion by shallow ring
furrows; the posterior axis is slightly
elevated and moderately convex, andseparated from the terminal portion by
an indistinct furrow; the pleural lobe
is narrow, convex, slopes downward
from the shallow dorsal furrow, marked

with one or two shallow pleural furrows;:
the broad margin is delimited by theshallow inner marginal furrow, and withshallow posterior embedding.
The exoskeleton of the animal is covered by medium-sized granules, parallel.
ridges marked along the outer marginof the anterior border, faint and radial
ridges on the preglabellar field, and a.
longitudinal ridge is marked along thecentral cranidial axis.
Figured specimens: Male form: Cranidia, U. C. M. 40279m, v, x, c' ; Librigenae,..
U. C. M. 40279 n, s; Pygidia, U. C. M40279t, y, z, a'.
Syspacheilus dunoirensis (MILLER),"female"Pl. 29, figs. 16-19, 22, 24, 30, 33, 34,
and Text-fig. 1 i, j.

Comparison: The female form differs.
from the male in having the deeper andnarrower anterior furrow ; steeper pre-glabellar field ; narrower pygidial axis ;·.
broader pygidial margin, and deeply
marked pqsterior marginal embayment._
The sexual ratio is 217.
Figured specimens:
Female form :.
Cranidia, U. M. C. 40279o, p, w, d'; Librigena, U. M. C. 40279e' ; Pygidia, U. M. C..
40279r, u, b'.
Syspacheilus dunoirensis (MILLER),

ontogeny
Anaprotaspid stage (Pl. 29, fig. 1, and'Text-fig. 1a).-The shield is rounded,.
moderately convex, about 0.30 mm inlength (sag.) ; the axial lobe is convex,.
slightly above the pleural region, without any distinct dorsal furrow; the.
posterior margin is flat and slightly
curved inward.
Only a single specimen is assigned to-591.

Ontogeny of three Cedaria zone trilobites·the present stage. The shield surface
is characterized without any special
feature. Its anterior margin may bemarked by a pair of frontal pits andthe posterior marked by an elevatedoccipital node; these suggest the orientation of the shield.
Metaprotaspid stage (Pl. 29, fig. 2, and
Text-fig. lb).-The shield is roundedoval in outline, convex, about 0.30-0.35
mm in length (sag.) ; the axial lobe is
expanded forward from the posterior
end to the anterior margin; the dorsal.and the ring furrows are only recognizable on the larger specimens, otherwise
indistinct; the pleural lobe is rather
broad, about twice as wide as the axis,(tr.) ; the anterior pits are elongate, andwell imf.lressed; the posterior shield issurrounded by a flat and slightly down
sloping margin, without indication of
the segmentation, except for a rounded
occipital ring and border furrow.
The present stage differs from theanaprotaspis in having the well developed axial furrow and both of the axial
and pleural lobes.
Paraprotaspid stage (Pl. 29, figs. 3-5,
and Text-fig. lc).-The shield is oval,
consists of the cephalon and the protopygidium and is about 0.40-0.55 mm inlength (sag.) ; the distinctly differentiated axial lobe is cylindrical, expandedslightly forward, without a well developed axial ring, except for the occipitalone; the dorsal furrow is irregularlymarked, which suggests the presence of
the axial ring and ring furrows ; a pairof short eye-brow ridges extend laterally from the sides of the frontal lobe,
they are well delimited by paired anterior pits, and palpebral ridges; thepleural lobe is broad, about one and onehalf the width of the axis, convex; theposterior shield or the protopygidium is-convex, surrounded by broad flat margin,249

and divided into two or three segments;
the protopygidial axis and the pleurallobes are well differentiated into axial
rings and pleural bands by furrows.
The surface of the shield is faintly
granulated, and four pairs of coarser
grains are marked on the fixigena andthe fixigenal borders.
The present stage is characterized by
the cylindrical glabella, narrower pleurallobes, and the presence of the protopygidium.
Early meraspid stage (Pl. 29, figs. 6-9
and Text-fig. ld).- The cranidium istrapezoidal in outline, convex, about
0.65-0.70 mm in length (sag.), with welldeveloped facial sutures; the glabella iscylindrical, or slightly expanded both anteriorly and posteriorly from the central
line (tr.); the four rounded and recognizable axial rings are indistinctly divided,
and the first ring is impressed by a pairof elongate pits laterally; the occipitalring is narrow, convex, curving posteriorly bearing a minute median node,and distinctly separated by a narrowoccipital furrow; the anterior border isvery narrow, horizontal, convex, arching
forward, well delimited by a deep furrow. The fixigena is broader than theglabella (tr.), triangular, moderately convex; the palpebral ridge is situated in
front of the mid-line of the glabella (tr.),narrow, elevated, well separated fromthe fixigena by palpebral furrow, andconnected to both of the anterior pleuralridge and the glabellar margins ; theposterior border is well impressed bybroad border furrow, convex, elevated,about one and one-half width of theoccipital ring. The facial suture is the
proparian type, with its anterior branchshort and convex, and the posterior one
divergent laterally and convex. The
skeletal surface is faintly granulated,
four pairs of coarse granules on the250

Chung-Hung Hu

fixigenae and the fixigenal border.
The distinct characters of the present
stage are that the glabella becomescylindrical or oblongus, without distinct
glabellar furrow, occipital ring broadly
convex, well separated from the glabellaby occipital furrow, facial suture proparia!, vvell defined.
Late meraspid stage (Pl. 29, figs. 10-13,
and Text-fig. 1 e, f).- The trapezoidal
cranidium is convex, about 0.80 to 1.65
mm long (sag.) ; the glabella is subquadrate or oblongus, marked without
distinct glabellar furrow; the occipitalring is crescentic, convex both vertically and posteriorly, bearing a minutemedian tubercle; the preglabellar field
is narrower than the anterior border,
convex, tilted slightly anteriorly; thefrontal furrow is deep and broad, having
a pair of elongate pits laterally; thefixigena is the same width as the glabella or slightly narrower, convex, witha pair of medium-sized palpebral lobes
situated on the mid-line of the glabella(tr.) ; the palpebral furrow is narrow anddistinct. The posterior fixigena is subtriangular, convex, with posterior fixigena well demarked by a broad furrow.
convex, about the same width as theoccipital ring (sag.) ; the facial suture is
opisthoparian. its anterior branch slightly divergent-convex, and the posterior
one is divergent-straight.
The skeletal surface is covered by
faint granules, four pairs of coarse
granules are regularly marked on theglabella and three pairs on the fixigena.
The present stage differs from theprevious one in that the preglabellar
field appears, the glabella becomes oblongus, the palpebral lobe is situated on
the mid-length of the glabella, the fixigena narrower, and opisthoparian facial
suture present.
Remarks: The morphogenesis of thepresent species is very closely similar
to those of Crepicep!wlus deadwoodensis
Hu (Hu, 1968a), Coosella convexa TASCH(Hu, 1968b), Tricrepicephalus blountensis
RESSER (unpublished material). All of
the features have parallel development
during their growth stages, especiallyin the shape of their glabella, and thefour pairs of coarse granules are indistinguishable within the four species in
the immature forms. It is doubtless.
these four species are the member ofthe same family, and with close phylogenetic relationship.
Figuredspecimens:
Anaprotaspis,.
U. C. M. 40279; Metaprotaspis, U. C. M.
40279a; Paraprotaspides, U.C.M. 40279bd; Early meraspides, U. C. M. 40279e-h ;.
Late meraspides, U. C. M. 40279 i-l.
Family Pagodiidae KOBA Y ASH!, 1935
Genus Nixonella LOCHMAN, 1944
Synonym: Genus Nixon ella LocwviAN, 1944
(type species, Nixonella montanensis LocH-·
MAN).

Genus Torridella LocH MAN & I-Iu, 1962
(type species, Torridella migranta LocHMAN.
& Hu).

Remarks: The present genus is a.
common member within the Cedariazone, Upper Cambrian. Its appearance
is similar to Genevievella LOCI-IMAN,.
1936, both have no preglabellar field, a
simple anterior border, and conical glabella, except the Nixonella has the gonatoparian facial suture and the later
one the proparian. The holotype of the
N. montanensis LOCHMAN (1944, pl. 13,.
figs. 29, 30) is a small cranidium, about
2.0 mm in length (sag.), with the broad
anterior border and oblong glabella. It
is possibly not a well developed mature
specimen. The associated pygidium of
N. montanensis (LOCHMAN, 1944, pl. 13,.

5 91.

Ontogeny of three Cedaria zone trilobites

fig. 28) consists of two segments, transverse, semicircular in outline, about 1.0
mm in length (sag.), is a meraspid pygidium, and possibly belongs to cedaroid(Paracedaria ?).
A genus Torridella proposed by LOCHMAN & Hu (1962) has the type species T.
migranta about 3.0 mm in length (sag.)(pl. 6, fig. 8; holotype), with the similar
characteristics as "N. montanensis" except its glabella is conical and anteriorborder is narrower. It is presumably amature specimen. The pygidium of ·• T.
migranta" is roundly triangular in outline, convex, consists of more than six
axial rings. Since these features are distinctly different from any other species
within the same faunal assemblage, thisis possibly the correct association. These
facts here permit to state that thegenera "Torridel-la" and "Nixonella"
are synonymous, however the type species of "Nixonella montanensis" has asemicircular pygidium and that of"Torridella migranta" has conical glabella as described above, but the former
was due to the misassociation and thelatter one was the mature specimens in
the full grown stage. Therefore, these
two forms have no foundation for the
genetic separation.

Nixonella montanensis LOCHMAN
Pl. 30, figs. 1-21, and Text-fig. 2a-k.

Nixonella montanensis LocHMAN, 1944, p. 105,
pl. 13, figs. 23, 27, 29-31 only (not fig. 28) :LocHMAN & I-lu, 1962, p. 16, pl. 5, figs.
48, 50-52 only (not fig. 49).
Nixonella cf. montanensis Locl!MAN, 1944, p.
).06, pl. 27, fig. 29.
Torridella migranta LocHMAN & Hu, 1964, p.
17, pl. 6, figs. 7-18.

Diagnosis: Cranidium trpezoidal, convex; glabella conical, three pairs of251

glabellar furrows; no preglabellar field;
anterior border narrow crescentic; fixigena about one-half width of the glabella, triangular, and palpebral lobe
small ; gonatoparian facial suture present. Librigena narrow, crescentic without distinct marginal furrow and genal
spine.
Pygidium regular triangular,
convex ; six axial rings ; axis narrower
than the pleura] lobe, and not extends
to the full length of the pygidium.
Description: The regular trapezoidal
cranidium is convex, has a conical glabella marked by three pairs of shallow
glabellar furrows; the first pair of glabellar furrows is faint and short, thesecond is medium-sized, and the third
one is the largest and deeply marked,
and obliquely directed to the occipital
furrow from the posterior palpebral
lobe; preglabella field absent; the anterior border is horizontally convex,
narrow. arching anteriorly and welldelimited by the frontal furrow; theoccipital ring is crescentic, convex, arches posteriorly and bears a minutemedian tubercle; the narrow occipital
furrow arches slightly forward on the
mid-line. and is demarked with a pair ofelongate pits laterally; the dorsal furrowis deep and broad. The fixigena isnearly triangular, convex, about onehalf the width of the glabella; the small
palpebral lobe is located in front of the
mid-line of the glabella (tr.), and thepalpebral ridge is distinct; the convex
posterior fixigenal border is about thesame width as occipital ring (tr.), welldefined by a broad and shallow borderfurrow; the anterior branch of the facial
suture is slightly divergent-convex, andthe posterior one divergent-straightlaterally.
The librigena is narrow, elongate,
without genal spine; the lateral furrow
and the border are about the same

252

Chung-Hung HUwidth, and indistinctly demarked; thenarrow ocular platform is flat, with theposterior area broader than the anterior
margin ; the small oval ocular ring islocated forward from the mid-line oflibrigena (tr.), convex, and elevatedabove the ocular paltform.
Pygidium is triangular in outline,
without marginal spine, and convex
along the rounded margin ; the axial
lobe is slenderly conical, tapering posteriorly, divided by 6 or 7 narrow, convex
axial rings by indistinct furrows; theaapleural lobe is slightly broader than theaxis, delimited by a broad and deep
dorsal furrow, and has rather faintly
impressed pleural furrows; the marginalborder is broader posteriorly from thefacet angles, and demarked by a rather
indistinct inner marginal furrow.
The animal exoskeleton is covered by
faint granules, and inner surface withthe furrows deeply marked.
Figured specimens: Cranidia, U. C. M.
40280, 40280 a-c; Librigena, U. C. M.
40280t ; Pygidia, U. C. M. 40280p-s.

b

d

c

.
.

.

e

f

Text-tigure 2.

hg

Nixonella montanensis LocH:-IAK.

a, Anaprotaspis, x 32; b, Metaprotaspis, x 38; c, Paraprotaspis, x 33; d, Early meraspid
cranidium, x 28; e, f, Two late meraspid cranidia, x 15, x 12; h, Librigena, x 11; g, Adult
cranidium, x 7; i, A meraspid pygidium, x 20; j, k, Two adult pygidia, showing boththe inner and outer skeletal surface, x 5, x 9. (all drawings were made from photographs).

591.

Ontogeny of three Cedaria zone trilobites

Nixonella montanensis LOCHMAN,
ontogeny
Anaprotaspid stage (Pl. 30, fig. 14, and
Text-fig. 2a).-The shield is rounded,convex, and about 0.25 mm in length(sag.) ; the axial and the pleural lobes:are incompletely differentiated; the anterior axis is deeply impressed by apair of frontal pits on the sides of thesmall frontal lobe, and its posterior axis
is ended into a small rounded node; apair of short superciloid ridges extend
postero-laterally from the margin of thefrontal lobe, which are well delimited
by anterior pits and border furrows;
the pleural lobe is rather broad, convex,
and slightly above the narrow axis; noinner marginal furrow is marked. The
shield surface is faintly granulated.
Two or three specimens are assigned
to the present stage but are mostly in-complete. The figured specimen heresuggests the axial region is narrow,depressed, and with a few coarse grains.
These coarse grains are possibly thelimestone matrix.
Metaprotaspid stage (Pl. 30, fig. 15, and
Text-fig. 2b).-The shield is about 0.40
mm in length (sag.), round or oval in
outline, and has the axial and pleurallobes which are faintly demarked bydorsal furrows; the axis is rather nar·row, cylindrical, with the frontal lobe
slightly expanded forwardly; no axial
ring or ring furrow is visible; theposterior end of the axis or the occipitalring is convex, and well defined byfurrows; the pleural lobe is broad about
twice as wide as the axis, convex, slightly above the axis; the posterior margin
Df the shield is surrounded by a narrow
flat band, which is broad laterally andnarrower to the posterior axis to forma shallow embedding. The skeletal surface is covered by fine granules.

253

The present stage is characterized by
the well differentiated axial and thepleural lobes, and the well depressed
dorsal furrows.
Paraprotaspid stage (Pl. 30, figs. 11-13,
and Text-fig. 2c).- The shield is oval,
divided into a cranidium and a small
protopygidium, all about 0.50-0.65 mm inlength (sag.), convex, with the axial andpleural lobes well differentiated; theaxial lobe is cylindrical, expanded slightly forward, with the axial rings indistinctly marked; the broadly rounded
frontal lobe is well delimited by a pairof distinct anterior pits, and by shortsuperciloid ridges; behind the superciloid ridges is a pair of faint elevatedpalpebral ridges which arch forward
and are well delimited by furrows; theoccipital ring is well defined by furrows,
convex, and transverse-oval. The fixigena or the pleural lobe is about one
and one-half the width of the glabella,convex, with the posterior border curving inward; the posterior border furrowis well defined, and its extreme lateralend is turned forward before it reaches
the marginal border; the protopygidium
is subtriangular, convex, divided into
two to three thoracic segments, and all
are freely articulated. The surface ofthe exoskeleton is covered by faintgranules.
The present stage is characterized bya protopygidium, axial and pleural lobes
being well differentiated, and the distinct
posterior fixigenal border present.
Early meraspid stage (Pl. 30, figs. 7-10,
and Text-fig. 2d).- The cranidium istrapezoidal, with posterior border broader than the anterior one (tr.), convex,
about 0.55 to 0.80 mm in length (sag.);
the glabella is long, cylindrical, with theanterior margin slightly expanded forwardly, and four indistinctly divided
glabellar segments are visible; the254

Chung-Hung HUanterior segment is the largest, andthose of the followings-2nd, 3rd, and4th-are about equal in size; a narrowand elevated anterior border appears
along the anterior margin ; the anteriorpits are visible on the small specimens,
but becomes shallower or absent on thelarger ones; the palpebral lobe is wellelevated and separated from the anteriorborder by a narrow transverse area; theoccipital ring is deeply delimited by an
occipital furrow, convex, arches posteriorly. The fixigena is about the same
width as the glabella; the posterior
lateral fixigena is convex, slopes downward both rearly and laterally from the
deeply impressed dorsal furrow, withnarrow posterior border deeply separated by the furrow, and about one andone-half width of the occipital ring.
The skeletal surface is faintly granulated.
The present stage differs from theprevious one in that the anterior borderappears, anterior pits are shallower orabsent, palpebral ridge is separated fromthe anterior border and the facial sutureis turned onto the dorsal surface toshow the proparian type.
Late meraspid stage (Pl. 30, figs. 3-5,
and Text-fig. 2e, f).- The cranidium isconvex, trapezoidal in outline, about 1.0 to
1.5 mm long (sag.) ; the oblongus glabella
is rounded anteriorly, and without distinct glabellar furrows; no preglabellar
field ; the anterior border is rather broadand convex, crescentic, and delimited
by a deep and broad anterior furrow;the occipital ring is convex, mid-line
broader than the sides, delimited by a
deep occipital ring and bearing a minutemedian tubercle; the fixigena is slightly
narrower than the glabella, convex,
below the glabella ; a pair of small narrow palpebral lobes are situated in frontof the mid-line of the glabella (tr.); they

are elevated and distinctly delimited by
the palpebral furrow ; the palpebral
ridge is faint, but traceable, it is connected to both of the palpebral lobe andthe antero-lateral glabellar margin; thebroad posterior fixigena is convex, downward sloping, and has the narrow borderwell delimited by broad and deep borderfurrows; the postero-lateral fixigenal
border is elevated from the border furrow, and about the same width as theoccipital ring (tr.). The skeletal surface
is faintly granulated.
During the present period, the glabella.
is developed from the cylindrical to oblongus shape, the anterior border increases the width, the fixigena becomesnarrower, and the palpebral lobe islocated nearly on the mid-line of theglabella (tr.).
Remarks: The ontogenetic development of the present species is similar
to those of cedariods, but in comparing
the same sized skeletons, the glabella isbroader, and without any median expansion. The morphogenesis of thepresent species is also similar to thoseof Kingstonia ara (WALCOTT) (Hu, 1968a)
and Komaspidella laevis RASETTI (Hu,.
1970). Thus, these three species might
represent the members of the samefamily, and with close phylogenetic relationship.
Figured specimens: Anaprotaspis,
U. C. M. 40280m; Metaprotaspis, U. C. M.
40280n; Paraprotaspides, U.C.M. 40280j-l;
Early meraspides, U.C.M. 40280f-i; Latemeraspides, U.C.M. 40280c-e.

Family Spinagnostidae HOWELL, 1935
Genus Baltagnostus LOCHMAN, 1940
Baltagnostus beltensis LOCHMAN
Pl. 30, figs. 22-35, and Text-fig. 3a-e.

591.

Ontogeny of three Cedaria zone trilobites

Baltagnostus beltensis LacHMAN in LoCH·
MAN & Du::-;c.~:-.1, 1944, p. 138, pl. 12, figs.
3-5.
Baltagnostus wyomingensis LocHl\!Al' & Hu,
1960, p. 822, pl. 99, figs. 1-4.
Cf. Baltagnostus wyomingensis LoCHMA!\ &Hu, 1960, p. 822, pl. 99, fig. 32.

Diagnosis: Cranidium quadrate or
rounded. convex; axial lobe or glabella
narrower than the pleural lobe; preglabellar field narrower than the pleurallobe, no central furrow; first axial ringround, and the following ones indistinct ;anterior furrow broad, convex. Thoracic segment narrow; axial lobe broad;pleural lobe about one-half vvidth of theaxis. Pygidium quadrate or rounded,convex; three axial rings; terminal segment broadly expanded; posterior borderconvex; posterior furrow broad andconcave.
Description: The cranidium is nearlyquadrate or roundly quadrate in outline,
convex; glabella conical, convex, above
the pleural lobes, well defined by dorsal
furrows; the first glabellar segment or
the frontal lobe is rounded, convex, andisolated by furrows ; the 2nd to 4th
glabellar segments are indistinctly differentiated, and connected by a narrowand elongated longitudinal ridge; asmall but distinct node is located on thecentral portion of the third axial segment; the occipital ring is rather narrow, convex below the posterior glabella,and connected with a pair of triangularnodes laterally ; the preglabellar field isslightly narrower than the pleural lobe,
convex, downwardly sloping from theanterior glabella, marked without lvngitudinal median furrow; the anterior
furrow is deep and broad, concave, andhas a median notch toward the preglabellar field; the anterior border isbroad, convex, and decreases in width
postero-laterally; the pleural fixigei'.al255

border is narrow, delimited by a distinct
border furrow, about one-half width ofthe occipital ring, and associated by apair of short posteriorly directed spines
at its extreme lateral corners. The
thoracic segment is convex; axial lobe.
very broad and convex, and lenticularwith the half ring furrow indistinctly
marked; the pleural lobe is short, about
one-half width as the axis (tr.), andcurves strongly posteriorly; the pleuralfurrow is deep and marked along thecenter of the pleural lobe.
Pygidium is rounded or roundly quadrate, convex. occupied with a large andbroad axial lobe, and delimited by narrow and faint dorsal furrows; the axial
rings are indistinctly divided by ring
furrows; the first axial ring is narrow,.
the second is medium sized, ornamented
by a small median tubercle, and thethird one is the largest, roundly expanded posteriorly, and marked by twopairs of rounded pits on equal distances;on the nearly posterior axial margin atiny median node is marked, which issurrounded by well depressed furrow;.
the pleural lobe is about one-half widthof the axis, convex, slopes downward,
and decreases in width posteriorly; theposterior border is convex. increases inwidth posteriorly, and is defined by abroad deep border furrow ; a pair ofshort broad based spines extends rearly
from the postero-lateral margin. The
exoskeleton is covered by faint granules ..
Remarks:
The present species represents more than 30 cranidia andpygidia. The materials consist also of afew of Kormagnostus sp. specimens, but
all are poorly preserved. The cranidiumof Baltagnostus beltensis is quite different from that of Konnagnostus sp.
and it is impossible to misidentify. The
pygidium of both species closely resemble each other, and are almost indistin-Chung-Hung Hu

256

b

a

c

d

e

Text-fig. 3.

Baltagnostus beltensis LaCHMAN.

a, Early meraspid pygidium, x 28; b, Late meraspid pygidium, x 12; c, d, An adult cranidium and a pygidium, x 7; e, A thoracic segment, x 8. (all drawings were made fromphotographs).

Explanation of Plate 29
Figs. 1-34. Syspacheilus dunoirensis (MILLER).
1. An anaprotaspis, notice the indistinctly developed axis. x50, U. C. M. 40279.
2. A metaprotaspis, showing the well differentiated axial and pleural lobes. x 50, U. C. M.
40279a.
3-5. Three paraprotaspides, showing the presence of their protopygidia. 3, x 36, U. C. M.
40279b; 4, x 36, U. C. M. 40279c; 5, x 45, U. C. M. 40279d.
·6-9. Four early meraspid shields, showing the presence of their anterior border and protopygidia. 6, x 30, U. C. M. 40279e; 7, x 32, U. C. M. 40279f; 8, x 25, U. C. M. 40279g; 9, x 20,
U. C. M. 40279h.
10-13. A few late meraspid cranidia, showing the glabella iucreases the width from cylindrical to oblong and the surface covered with large and small granules. 10, x 19, U. C. M.
40279i; 11, X 12, u. C. M. 40279j; 12, X 18, u. c. M. 40279k; 13, X 12, u. c. M. 402791.
14, 23, 25, 26, 31. Four different sized male cranidia. 14, x 8, U. C. M. 40279m; 23, x 8,
U. C. M. 40279v; 25, X 5, U. C. M. 40279x; 26, 31, profile and dorsal views of a cranidium,x 4, U. C. M. 40279c'.
15, 20, 32. The librigenae; male, 15, x 6, U. C. M. 40279n; 20, x 5, U. C. M. 40279s; female,32, x 5, U. C. M. 40279e'.
18, 19, 22, 30. Four different sized female pygidia. 18, x 9, U. C. M. 40279q; 19, x 8, U. C. M.
40279r; 22, x 2, U. C. M. 40279u; 30, x 3, U. C. M. 40279b'.
16 1 17, 24, 33, 34. Four different sized female cranidia. 16, x 8, U. C. M. 40279o; 17, x 6,
U. C. M. 40279p; 24, x 6, U. C. M. 40279w; 33, 34, top and side views of a cranidium, x 2,
U. C. M. 40279d'.
21, 27-29. Four different sized male pygidia. 21, x 4, U. C. M. 40279t; 27, x 5, U. C. M. 40279y;
28, x 8, U. C. M. 40279z; 29, x 6, U. C. M. 40279a'.

Hu :Ontogeny of three Cedaria zone trilobites

2

13

3

10

Plate 29

4

9

5

6

8

7

14
15

18

17

25

24

28

27

26

31

32

33

29

30

34

591.

Ontogeny of three Cedaria zone trilobites

guishable. However, th.e present species
has a slightly narrower pygidial axis
and the posterior axial lobe slightly
touches the border furrow, whereas theaxis of Kormagnostus sp. is broader andrunning into the border furrow.
Both Baltagnostus wyomingensis LocHMAN & Hu and Cf. B. wyomingensis
LOCHMAN & Hu reported from Wyoming
have the conical pygidial axis and areapparently the immature forms of B.
beltensis.

Baltagnostus beltensis LOCHMAN,
ontogeny
The material which I have studied
contains the smallest cranidium about
1.1 mm in length and the largest one
reaching to 4.0 mm (sag.), showing thecontinuous . size variation within thelimits of these scales, but morphologicallythey are almost without differentiation.
Therefore, the cranidium gives no valuable criterion for dividing up the growthstages of the animal. The present assignations of the growth stages are
based merely on the pygidium.
Early meraspid stage (Pl. 30, figs. 2729, 31. and Text-fig. 3a).-The pygidial
shield is rounded, convex, about 0.9-1.3
mm in length (sag.) ; the axis is conical,
narrow posteriorly, and bearing an indistinct axial ring; a tiny median tubercle is borne on the second axial ring;the dorsal furrow is deep and distinct;
the pleural lobe is narrower than theaxis, convex, slopes downward, its posterior end is parenthetic, and holds theposterior axis; the convex posteriorborder increases the width posteriorly,
and is well delimited by the borderfurrow; a pair of short spines extends
posteriorly f::om the lateral margin.
The animal skeleton is covered by faint257

granules. Some small pygidia are associated with thoracic segment.
Late meraspid stage (Pl. 30, figs. 30, 34,
and Text-fig. 3b).-The pygidial shieldis quadrate, or rounded, convex, about
1.5 to 2.5 mm in length (sag.) ; the axis
is oblongus, consists of three indistinctly
divided axial rings, but of the 1st and2nd segments are about the same size,
and the last one is the largest ; the lastaxial segment is rounded, convex, andmarked by two pairs of granules on thecentral surface, and a small one at theposterior median line; the pleural lobe
is about-one-half the width of the axis,
decreases in width from the posterior
lateral margin to the posterior medianfurrow ; the posterior border furrow is
broad, convex, the posterior border isconvex with a rear median notch directed to the axial terminal portion, anda pair of short marginal spines is directed rearly from the lateral margin.
The present stage differs from theearly one in that the axial lobe is subquadrate, terminal segment increases inwidth, posterior median furrow is nearlyinvisible, and the pleural lobe decreases
in width.
Remarl<s: The present species has its
ontogenetic characteristics very similar
to that of Kormagnostus simplex RESSER(Hu, 1968a), except the cranidium iscompletely different in adult and immature morphology. The similarity ofthe pygidial development possibly indicates the close phylogenetic relationshipbetween the two species, since the pygidial variations are the main taxonomic
criteria for this group-the Agnostida.
PALMER (1955) divided the ontogenetic
metamorphosis of. Pseudagnostus communis (HALL & WHITFIELD) into immature and early mature stages earlier
than adult form. These two stages arecorrelated to the present ontogenetic

Chung-Hung Hu

258·divisions.
Figured specimens: Cranidia, U. C. M.
40281, 40281 a-d; Thoracic segment,
U. C. M. 4028lk ; Pygidia, U. C. M. 4028lj,
m; Early meraspid pygidia, U. C. M.
40281e-g, i; Late meraspid pygidia,
U. C. M. 4028lh, l.
References
B. F. and DuNCAN, D. (1939) :Middle·Upper Cambrian transition faunasin North America. Wagner Free Inst.
Sci., Bull., vol. 14, no. 1, p. 1-11, pl. 1.
Hu, C. H. (1968a) : Ontogeny and sexual
dimorphism of Lower Paleozoic Trilo·
bit a; unpublished Ph. D. disertation,

HowELL,

Univ. of Cincinnati, Ohio (accepted for
publication of Paleontographica Americana, vol. 7, no. 44, 1971).
- - (1968b) : Notes on the ontogeny andsexual dimorphism of Upper Cambriantrilobites of the Welleraspis faunule from
Pennsylvania. jour. Nanyang Univ., vol.
2, p. 321·-357, pis. 1-4.
- - (1970) : Ontogenies and sexual dimorphisms of two Upper Cambrian trilobites.
Proc. Geol. Soc. China, No. 13, p. 143-155,
pis. 1, 2.
LocH~IAN, Ch. (1936) : New trilobites genera
from the Bonneierre dolomite (Upper
Cambrian) of Missouri. jour. Paleont.,
vol. 10, p. 35-43, pl. 9.
- - (1940) : Fauna of the basal Bonneterre
dolomite (Upper Cambrian) of South-

Explanation of Plate 30
Figs. 1-21. Nixouella montanensis Loci-IMAN.
1-3, 16. Three different sized cranidia, showing the broad glabella. 1, x 7, U. C. M. 40280;
2, x 8, U. C. M. 40280a; 3, x 7, U. C. M. 40280b; 16, x 8, U. C. M. 40280c.
4-6. Three late meraspid cranidia, showing the oblong glabella. 4, x 14, U. C. M. 40280c;
5, x 12, U. C. M. 40280d; 6, x 15, U. C. M. 40280e.
7-10. Four early meraspid cranidia, showing the cylindrical glabella and the narrow anterior border. 7, x 20, U. C. M. 40280f; 8, x 25, U. C. M. 40280g; 9, x 28, U. C. M. 40280h;
10, X 27, u. C. M. 40280i.
11-13. Three paraprotaspides, showing the slightly expanded glabella and the presence ofthe protopygidium. 11, x 36, U. C. M. 40280j; 12, x 45, U. C. M. 40280k; 13, x 33, U. C. M.
402801.
14. An anaprotaspis, showing the indistinctly differentiated axial and pleural lobes. x 32,
U. C. M. 40280m.
15. A metaprotaspis, showing the indistinctly developed axis. x 38, U. C. M. 40280n.
17, 19. Two adult pygidia. 17, x 5, U. C. M. 40280p; 19, x 9, U. C. M. 40280r.
18, 20. Two immature pygidia. 18, x 9, U. C. M. 40280q; 20, x 20, U. C. M. 40280s.
21. A nearly complete Iibrigena. x 11, U. C. M. 40280t.
Figs. 22-35. Baltagnostus beltensis Locr-n·IAN.
22-26. Five different sized cranidia, showing the stabilized morphogenesis within the series.
22, x 14, U. C. M. 40281; 23, x 8, U. C. M. 40281a; 24, x 9, U. C. M. 40281b; 25, x 17, U. C. M.
40281c; 26, x 7, U. C. M. 40281d.
27-29, 31. Four early meraspid pygidia, notice the conical axis. 27, x 24, U. C. M. 40281e;
28, X 25, u. c. M. 40281£; 29, X 17, u. c. M. 40281g; 31, X 21, u. c. M. 40281i .
.30, 34. Two late meraspid pygidia, showing the cylindrical axis. 30, x 12, U. C. M. 4028lh;
34, X 7, u. c. M. 402811.
32, 35. Two adult pygidia, showing the slightly forwardly tapered axial lobe. 32, x 6,
U. C. M. 40281j; 35, x7, U. C. M. 40281m .
.33. A complete thoracic segment. x 8, U. C. M. 40281k.

Hu :Ontogeny of three Cedari a zone trilobites

Plate 30

17

2

6

18

7

19

3

20

11

12
22

14
30
23
29

25

24
27

26

33

591.

Ontogeny of three Cedaria zone trilobites

eastern Missouri. Ibid., vol. 1, p. 1-53,
pis. 1-5.
- - (1950) : Upper Cambrian faunas of the
Little Rocky Mountains, Montana. Ibid.,
vol. 24, p. 322-349, pis. 48-51.
- - (1959) : Treatise on Invertebrate Paleontology, (Part 0), Arthropoda 1. Geol.
Soc. Amer. & Univ. Kansas Press, p. 302.
- - and Du:-iCAN, D. (1944) : Early Upper
Cambrian faunas of central Montana.
Geol. Soc. Amer. Spec. Paper, no. 54, 181p,
pis. 4-17.
· - and Hu, C. I-I. (1960) : Upper Cambrianfaunas from the northwest Wind River
Mountains, Wyoming, Part I.
jour.
Paleont., vol. 34, p. 794-834, pis. 59-100.

259- - (1961) : Upper Cambrian faunas fromthe northwest Wind River Mountains,
Wyoming, Part II. Ibid., vol. 35, p. 125146, pis. 26-30.
- - (1962) : Upper Cambrian faunas fromthe northwest Wind River Mountains,
Wyoming, Part Ill. Ibid., vol. 36, p. 1-28,
pis. 1-7.
MILLER, B. M. (1936) : Cambrian trilobitesfrom northeastern Wyoming. Ibid., vol.
10, p. 35-43, pl. 8.
PALI\IER, A. P. (1955):
Upper Cambrian
Agnostidae of the Eureka district,
Nevada. Ibid., vol. 29, p. 86-101, pis. 19,
20.

Trans. Proc. Palaeont. Soc. Japan, N. S., No. 85, pp. 260-274, pis. 31, 32, April 20, 1972:

592.

ON THE LEPIDOLINA ZONE DISCOVERED FROM THE
SHIMA PENINSULA, SOUTHWEST JAPAN*NOBUO Y AMAGIW A
Institute of Geoscience, Osaka Kyoiku University

and
YUKIY ASU SAKA
Institute of Earth Science, School of Education, Waseda University*;t:!JI=!':,It,!i J: ~ ~~ ~ ht.: Lepidolina ;;jH;:-::> v' 'l : *~~~1 M:i!I:it:I$=F.if~C':lf;k:50?\=H\'=nH: ift[i:-9 {,.~~~rtf li!£:1§-ifiit',~: ~tH: O)Jij>;fi rp 7.1• Gfl~if*,!: t..- 'l iffUl',-9 0 Lepidolina kumaensis:2f1 C:i:b,!: T {) Lepidolina multiseptata multiseptata-L. kumaensis ftll~i':2~t.!.. L.-t.:oi::.C':llij>.'firpfCI1 Yabeina aff. globosa t;lt1'¥l-'lv'9o ~t\'~11C.hGC':lftll~ITcli&T{>.!:;ltrc, Lepidolina ft:fil!'i'.!: Yabeina itlll!i'C':li~H:ifdC::.-::>v''l tliifut::t.:o t.J:i>, C.hGC':lit
1'1~i!f"t9Jll!l\'111f;lt*li!ti§.fi>iln' (ii!if~:*~tti:tU'f) f:Hc'lv't.:i.l:, i::.C':lt.:<JO)[i}f)t;--c·, [jijffl
f.ti.I'G~~~1t.J:L <bGt.:rc.~.;~~!\1i!i'Cifi14S-9-{>oiLilif,~ 9lS x·J.)i¥ './,~

Geological summary

ments between longitudinal faults, andform, as a whole, the so-called sandwich
structure. The northern boundary faultof the middle sub-belt is called the Arashima-Gokasho tectonic line (Y AMAGIWA,
1957), which is easily traced owing toserpentinite intruding along its wholeextension. Some authors regard thistectonic line as an eastern equivalent of
the Kurosegawa zone (!CHIKA w A et a!.,1956) elucidated in Shikoku (e. g., HAMADA, 1963). Several lenticular bodies ofserpentinite crop out sporadically along
the southern marginal fault, too.
In the middle sub-belt the Jurassic
and the Cretaceous strata are distributed
along with the Chichibu complex. The
former, trapped in a narrow strip, iscorrelated with the Upper Jurassic Imaura group which occupies the northernPreviously the writers (1967) reported
explanatorily on the geology and geological structure of the Chichibu terrain
in the eastern part of the Shima peninsula. Kinki District. In this part of thepeninsula, the Chichibu terrain is divided
into the northern, middle and southern
sub-belts as is that of Shikoku. Eachsub-belt trends NE-SW to NNE-SSW,
and is separated from each other bymarked faults. Of these sub-belts, thenorthern one alone consists exclusivelyof the Palaeozoic Chichibu complex,
while the other two are intercalatedwith narrow slices of the Mesozoic sedi-* Received March 6, 1971; read January
25, 1969 at Tokyo and November 22, 1970 at
Hiroshima.
260

592.

261

Fusulinids from Shima..

marginal part of the southern~risub-belt. The latter, named the
Matsuo group, is distributed separately in three narrow zones.
Its age is verified palaeontologically to be of the lower Cretaceous, Kochian epoch.
The Chichibu complex constituting the middle sub-belt isknown as the Horikiri, the Aonomine and the Toya groups. The
Horikiri group, correlated with
the Middle Carboniferous system
is exposed as small lenses along
the southern boundary fault.
The Aonomine group constitutes
two zones covering the widest
area in the middle sub-belt. SevText-fig. 1.
eral fusulinid fossils found from
Fossil locality .... X
it indicate its age to be the Middle
1. ... Shiranezaki, 2 .... Toya, 3 .... Imaura,
to Upper Permian period*. On
4 .... Ogurajima, 5 .... Omurajima, 6 .... Motoura.
the other hand, no useful fossils
had been gained from the Toya groupsoutheasternmost part of the "Toyawhich is bounded both on the northerngroup" on the geological map. Theseand the southern sides by the Matsuo
fusulinid-bearing strata are bounded bothgroup up to the time when the writers
on the north and the south by longitudipreviously described the geology of thisnal faults and form a small block which
district. The writers, on this account,measures no more than 35m in width
presumed the age of the Toya group to(namely in the direction perpendicular
be the Permian period, judging from its
tothe general strike). On the south,.
lithofacies and geological situation.
they
are in contact with the alternation
Recently, the writers discovered theofsandstone
and shale, subordinate
Lepidolina multiseptata multiseptata-L.
constituent
oftheLower Cretaceous Makumaensis fauna from the strata which.
tsuogroup;
onthenorth, in contact
they had previously included in the Toyawiththesemi-schist
belonging to thegroup. The strata in question are exToya
group
barrenoffossils. Alongposed in the sea-cliff on the Toya coast
thenorthernboundary
fault,
serpentinite
facing to the east and constitute theintrudes, as is usually observed along* Neoschwagerina sakaguchii and N. fujithe longitudinal faults demarcating each
motoi were discovered from the lower partgroup within the middle sub-belt. Hereof the Aonomine group (YAMAGIWA, 1956;
in this paper, the writers, laying stress
YA:VIAGIWA and SAKA, 1967), and Yabeina
on the occurrence of this small block,katoi, Y. packardi shimensis and Y. omurenand regarding it as separate from thesis from the upper part (Y AMAGI w A, 1956;
fossil-free Toya group, propose to call
YAMAGIWA and ISHII, 1958; YAMAGIWA and
SAKA, 1967).
it the Toba group. The writers have262

N obuo YA M AGIWA an d Y~~kiyas~~ SA K A

T ext-fig . 2. The ou t crop of t he Toba g roup a t Toya, Tob a Cit y , M ie Pref ec ture .
The f oss ils were collected from sand s ton e lenses cont a ined in th e con t or t ed s hale .
SS . .. . Sandstone, SH .... S ha le.

confirmed the occurrence of this groupin no other places than along the Toyacoast, and conclude that it was squee zedout as a lenticular body along the fau lt
which forms the boundary between the
Toy a group and the Matsuo group.
The Toba group consists mainly ofsandstone and shale, with subordinate
tuff, chert and limestone. Each stratum
is so much disturbed that the abovementioned rocks except shale are torn
off into irregular-shaped frag ments ofvarious si zes scattered in the contorted
shale, thus showing a cataclastic conglomeratic aspects. Sandstone, frequently penetrated by calcite v eins, is composed mainly of quartz - and feldspargrains cemented by the matri x of arg illaceous material.
B.esides occasional
patches of shale, small amounts of frag ments of chert, limestone ig neous andmetamorphic rocks are also contained.

The mineral composition corresponds tothat of low rank g re ywacke according
to KR YN INE's classification. Under amicroscope, g rains, irregular in shapeand in si ze, are mostly in plane-contact,rarel y in suture-contact. Some quartzg rains show wa vy ex tinction. Ig neousrocks occurring as fragments in sandstone are acidic andesite and diabase,all havin g suffered altera tion. Metamorphic rocks contained are crystalline
schists of low metamorphic g rad e*.
Tuff is a lterej too, and is andesitic
in tex ture and composition. Chert isg reen in colour.
Each stratum of the Toba g roup forms
a homoclinal s tructure, strikin g N50 o70 °E and either dipping steeply to the* These met a morphi c and ig neous rocks
w ill be des cribed in de tail in f uture afte r aclose ex amin at ion.

592.

Puwulinids from Shimanorth or standing vertically.
Fusulinid fossils were found not fromlimestone which, occurring as small
lenses, is crystalline and white in colour,
but from small sandstone lenses contain·
ed in the contorted shale. Examinationof about eighty thin sections revealed
the following fossils:
Lepidolina lntmaensis
Lepidolina multiseptata gigantea
Lepidolina multiseptata multiseptata
Yabeina columbiana
Yabeina aff. globosa
Metadoliolina gravitesta
Pachyphloia sp. indet.

Though the outer volutions of these'fossils are partly broken, they are neverrounded to such a degree as would be-expected in case they had been transported to some distance. The writers
conclude, on this account, that they areallochthonous fossils in the strict sense:but not derived ones.
Geological age

The faunal assemblage of the above
mentioned fossils except Yabeina aff.
globosa is closely similar to that known
from the Kuma formation in Kyushu·(KANMERA, 1953, 1954), the Mizukoshi
formation in Kyushu (YANAGIDA, 1958),
the Maizuru group in Kinki (NOGAMI,
1958), the Haigyu formation in Shikoku(SUY ARI, 1962) and the I waizaki limestone
in Kitakami (CHOI, 1970a), so that the ageof the Toba group is undoubtedly referred to the Upper Permian. Only disparity recognized between the Toba
group and the others is that Yabeina:aff. globosa, which has never been reported to occur in the latter, co-exists
with other fusulinids in the Tobp. group,and that only the Toba group is inter-calated with chert and tuff.

26:3

KANMERA (1953, 1954) divided the Upper Permian system (Yabeina zone) ofJapan into the upper and lower sections:
According to him, the lower one. characterized by the Yabeina globosa fauna.
is represented by the Yabeina zone of
Akasaka limestone in the Mino belt, andthe upper one, characterized by the
Lepidolina toriyamai fauna, is represent. ed by the Kuma formation (Lepidolina
toriyamai zone) cited above. On theother hand, HANZAWA and MURATA (1963)
expressed an exactly opposite view, thatis, the Lepidolina fauna corresponds to
the Neoschwagerina zone which underlies
the Yabeina zone represented by the
Yabeina globosa fauna. YABE(1964b, 1965,1966) and TORIY AMA (1967) regarded the
Y abe ina globosa zone represented by the
Akasaka limestone as contemporaneouswith the Lepidolina toriyamai zone represented by the Kuma formation plus
the Yabeina shiraiwensis zone represented by the Akiyoshi limestone in Chugoku. TORIY AMA, taking note of thecomponents of these faunal assemblages
and of variance of the lithofacies, proposed the name " Kinshozan facies " forthe sequence containing the Yabeina
globosa fauna, and the " Kuma facies "for that containing the Lepidolina toriyamai fauna. He further advocated that
the Yabeina zone in Japan, represented
by the Kuma facies should be renamed
Yabeina shiraiwensis-Lepidolina toriyamai zone.
Recently, OZAWA (1970) expressed a
new opinion concerning the Upper Permian biofacies of Japan. According tohim, the V erbeekinoidea fauna known
from the Upper Permian system consistsof two groups, the Y abeina globosa fauna
and the Lepidolina multiseptata fauna.
Y abeina globosa, Y. pachardi, Neoschwagerina katoi, N. minoensis, etc. are typical of the Yabeina globosa fauna. The

264

Nobuo YAMAGIWA and Yukiyasu SAKA

Lepidolina multiseptata fauna is subdivided in to the Lepidolina multiseptata
shiraiwensis-Colania douvillei fauna of
the lower horizon and the Lepidolina
multiseptata multiseptata-Lepidolina kumaensis fauna of the upper horizon. The
former, represented by Lepidolina multiseptata shiraiwensis, Colania douvillei,
etc. is considered as contemporaneouswith the Yabeina globosa fauna. Lepidolina kumaensis, L. multiseptata multiseptata, etc. are representative of thelatter, which, he insisted, is the most
evolved type of Verbeekinoidea. Here,
what the writers should pay special attention to is that, according to OzAWA,
no cases are known where the Y abe ina
globosa co-exists with the Lepidolina
multiseptata fauna.
Several problems are left unsolved on
the biostratigraphy and biofacies of theUpper Permian Yabeina zone in Japan,
as the writers have reviewed above.
The Lepidolina-bearing fauna that thewriters lately found from the Toba groupis exactly alike that from the Kuma
formation in Kyushu with respect to its
faunal assemblage, and is considered tocorrespond to the Lepidolina multiseptata
multiseptata-Lepidolina kumaensis zoneof OzAwA. Occurrence of Y abeina aff.
globosa in this fauna is worthy to note,because, as OzAWA alreadly pointed out,
there has ever been known no parallelcase on record where Yabeina globosa
occurs in the Lepidolina multiseptata
fauna. The fact that Y abeina aff. globosa
co-exists with the members of the Lepidolina multiseptata fauna in the Toba
group may contribute to the interpretation of the Upper Permian stratigraphy
and biofacies in Japan. Also, it is interesting that, as alreadly stated, the Toba
group, consisting mainly of sandstone
and mudstone with minor amounts ofchert and tuff, shows some lithologicaldifference from the Kuma formation andother stratigraphic units characterized
by the Lepidolina multiseptata multiseptata-Lepidolina kumaensis fauna.
Acknowledgements
Here the writers wish to express theirhearty thanks to Prof. Emeritus H. FuJIMOTO of Tokyo University of Education. Prof. Emeritus S. MATSUSHITA ofKyoto University, Prof. Emeritus I. MATSUZAWA of Nagoya University and Prof..
S. SAKAGUCHI of Osaka Kyoiku University for their kind guidance. The writers are deeply grateful to Prof. K. NAKAZA wA of Kyoto University and Prof.
K. IcHIKAWA of Osaka City University
for their suggestions on the geologicaLstructure. The writers express theirgratitude to Assist. Prof. K. KANMERAof Kyushu University, Lect. K. ISHII of
Osaka City University, Dr. Y. NOGAMI
of Kyoto University and Dr. T. OZAWAof Kyushu University for their kindadvice in the study of the fusulinids.
Acknowledgement is also due to Lect ..
T. YAMAZAKI of Osaka Kyoiku Univer-sity for his kind suggestion in the
study of the igneous and metamorphic
rocks in thin sections. Thanks are alsodue to Mr. T. HABUCHI, Mr. T. IWAHASHI, Mr. T. MISI-IIMA, Miss Y. MORIMOTO,Miss K. Y AZUMI, Mr. S. OKAMOTO, MissY. YAMANE, Miss M. T AZIMI and Miss
M. TSUCHIY A for their assistance in collection of samples in the field survey.
Photographic work was done by Mr. M.
UcHIDA and Mr. T. IWAHASHI, to whom
the writers extend their thanks.
Systematic description
Order Foraminiferida
Suborder Fusulinina VON MOLLER, 187&-

592.

Fusulinids from Shima

Superfamily Verbeekinoidea STAFF
and WEDEKIND, 1910
Family Neoschwagerinidae DUNBAR
and CONDRA, 1928
Subfamily Lepidolininae MIKLUKHOMAKLA Y, 1958
Genus Lepidolina LEE, 1933
Lepidolina multiseptata gigantea (GUBLER)
Plate 31, fig. 1
1935. Neoschwagerina megaspherica var. gigantea GuBLER, Mem. Soc. Geol. France,
Nov. Ser., T. 11, Fasc. 4, pp. 116-118,
pl. 3, figs. 6, 8, 10?.
193S. Neoschwagerina douv£/lei GUBLER, Ibid.,
pp. 111-113, pl. 7, figs. 7, 8, pl. 8, fig.
6; pl. 6, fig. 2?; pl. 7, fig. 10?; pl. 8,
fig. 10?.
1954. Yabeina gubleri KANMEH.A, Mem. Fac.
Sc£. Kyushu Univ., Ser. D, vol. 4, no.
1, pp. 19-21, pl. 4, figs. 1-13.
1958. Y abe ina gubleri: NoGAtvii, Mem. Coli.
Sci. Univ. Kyoto, Ser. B, vol. 25, no. 2,
pp. 103-104, pl. 1, figs. 5-6.
1960. Y abeina gubleri: CHISAKA, Jour. Coli.
Art. Sci. Chiba Univ., val. 3, no. 2, pp.
250-251, pl. 6, figs. 1-4; pl. 7, figs. 1-6;
pl. 8, figs. 1-5.
1964. Yabeina multiseptata gigantea: IsHII
and NoGAMI, jour. Geosci. Osaka City
Univ., val. 8, Art. 2, pp. 20-22, pl. 6,
figs. 1-4.

Description :-Shell is large, elongate
fusiform with inflated central part; theirlateral slopes gently concave. Inner two· volutions are spherical or subspherical,.and the third to fifth are inflated fusiform. Beyond the 6th volution shellform resembles its mature shape. Sev·eral outer volutions are missing. The
specimen illustrated as fig. 1 on Plate 31
is 9.2 mm in length and 3.5 mm in width,_giving a form ratio of 2.6. Proloculus

265

is large; with outside diameter of 0.45
to 0.65 mm. Spirotheca is thin, composedof a tectum and a thin keriotheca withfine alveoli, measuring 0.005 to 0.01 mm.
The heights of the first to the 11th
volution of the above mentioned specimen are 0.10, 0.10, 0.12, 0.12, 0.12, 0.10,
0.15, 0.16, 0.19, 0.18 and 0.17 mm, respectively. Axial septula and primary transverse septula present throughout shelland slender. Primary transverse septula
come into contact with the top of parachomata. Secondary transverse septula
were first 2nd volution: and one septulum developed between adjacent primaryones, but beyond the fourth volution one
to two ones are generally present; they
are of generally bar-like shape, but inrare cases pendant shaped.
Remarks:- The distinct characters of
the present specimens are their large
proloculus, very thin spirotheca andelongate fusiform with inflated central
part. The features mentioned above
pratically agree with those of Lepidolina
multiseptata gigantea (GUBLER, 1935;
KANMERA, 1954; NOGAMI, 1958; CHISAKA,
1960; ISHII & NOGAMI, 1964) from theUpper Permian of Japan and Cambodia.
The present form closely resembles L.
kumaensis KANMERA (KONISHI, 1952;
KANMERA, 1954; YANAGIDA, 1958; NoGAM!, 1958; CHISAKA, 1960; SUY AI~ I. 1962;
HASEGA WA,1965; CHOI,1970a; Y AMAGIWA& SAKA, in this paper) and L. multiseptata multiseptata (DEPRAT, 1912, 1914;
0ZA WA, 1922; COLAN I, 1924; GUBLER,
1935; THOMPSON, 1948; SKINNER & WILD,
1954; ISHII & NOGAMI, 1964; SADA &YOKOYAMA, 1966; YAMAGIWA & SAKA,
in this paper) in its large proloculus,
very thin spirotheca and other importantcharacters. However, the former one canbe distinguished from the latter, having
elongate fusiform with inflated central
part.

266

Nobuo Y AMAGIWA and Yulciyasu SAKAlSHil and NOGAMI (1964)

described thisspecies under the generic name of Yabeina and then they divided it into threesubspecies, namely Y. multiseptata multiseptata, Y. multiseptata gigantea and Y.
multiseptata shiraiwensis. Very recently,
OzAwA (1970) discussed the difference
between Y abe ina and Lepidolina. According to him, Lepidolina is distinguished from Yabeina by having larger proloculus in the megalospheric generation,
larger, elongate shell of the microsphericgeneration and the essential differencein the thickness and shape of septa andseptula. In the above respects, this subspecies should be referred to Lepidolina.
The present specimens are megalospheric form.
Occurence :-The present specimens occur from the Toba group at Toya, Toba
City, Mie Prefecture, Southwest Japan.
The present form is associated with
Lepidolina kumaensis, L. multiseptata
multiseptata, Yabeina columbiana, Yabeina aff. globosa, Metadoliolina gravitesta
and Pachyphloia sp. indet.
Repository :-It is deposited in the collection of the Institute of Geoscience,
Osaka Kyoiku University. Reg. nos.
71001, 71002, 71003.

Lepidolina multiseptata mulliseptata(DEPRAT)

Plate 31, fig. 21912. Neoschwagerina (Sumatrina) multiseptata, DEPRAT, Mhn. Serv. Geol. Indochine, vol. 1, fasc. 3, pp. 53-55, pl. 3,
figs. 2-8.
1914. Neoschwagerina (Sumatrina) multiseptata, DEPRAT, Ibid., vol. 3, fasc. 1, pp.
34-35, pl. 5, figs. 7-11.
1922. Neoschwagerina (Yabeina) hayasakai,
OZAWA, Geol. Soc. Tokyo, jour., vol.
29, no. 348, pp. 369-370, pl. 4, fig. 2.

1924. Neoschwagerina mu!tiseptata : CoLAN!.
Mfmz. Serv. Geol. Indochine, vol. 11,
fasc. 1, pp. 154-155, pl. 15, fig. 1; pl.
24, figs. 12-13; pl. 25, figs. 1-8, 10-12,
14-15; pl. 26, figs. 1-2, 4, 6-18.
1935. Neoschwagerina mu!tiseptata: GuBLER,
Mfnn. Soc. Geol. F1·ance, Nov. Ser. T.
11, fasc. 4, pp. 119-123, pl. 3, fig. 5; pl.
6, figs. 1, 3, 8-10; pl. 7, fig. 5.
1935. Neoschwagerina megasphaerica, GullLER, Ibid., pp. 114-116, pl. 7, fig. 3;
pl. 6, fig. 4.
1948. Neoschwager£na multiseptata: THO~IP­
SON, Protozoa, Art. 1, Univ. Kansas,
pp. 66-67, pl. 20, figs. 5-6; pl. 22, figs.
1-5.
1954. Lepidolina multiseptata : SKII'\:'\ER and
WILD, jour. Pa!eont., vol. 28, no. 4, pp.
449-450, pl. 52, figs. 1-5.
1954. Yabeina yasubaensis, KANMERA, Mem.
Fac. Sci. Kyushu Univ., Ser. D, vol. 4,
no. 1, pp. 18-19, pl. 2, figs. 10-13; pl.
5, figs. 14-19.
1964. Y abe ina multiseptata multiseptata: IsHII
and NoGAMI, jour. Geosci. Osaka City
Univ., vol. 8, Art. 2, pp. 17-20, pl. 3,
figs. 1-3; pl. 4, figs. 1-3; pl. 5, figs. 1-4.
1966. Y abe ina multiseptata multiseptata : SADA
and YoKOYAMA, Trans. Proc.
Pa!eont. Soc. japan, N. S., no. 63, pp.
304-307, pl. 33, figs. 4-5, 7-8.

Description :-Shell is medium, inflated
fusiform. Inner two or three volutions
are spherical or subspherical, and beyond
5th volution shell form resembles its
mature shape. A few outer volutions
are missing. Shell at 11th volution in
our typical specimen (Plate 31, fig. 2) is
6.0 mm in length and 3.6 mm in width;form ratio about 1.7. Proloculus is large
and spherical. Its outside diameter is
0.45 to 0.65 mm. The heights of the firstto the 11th volution are 0.13, 0.13, 0.14,.
0.12, 0.14, 0.15, 0.17, 0.18, 0.19, 0.20 and.
0.17 mm, respectively. Spirotheca is very
thin, composed of a tectum and a keriotheca with very fine alveoli. Thicknessof spirotheca is 0.01 mm in outer volu-

592.

Fusulinids from Shimations. Septa, axial septula and primarytransverse septula present throughout
shell and slender. Secondary transverse
septula first appear in the second volution. One septulum occurs between adjacent primary ones in inner volutions
and one or two septula occur in outer
volutions. Parachomata come into contact with the top of primary transverse
septula near the center of chamber.
Remarks:-The present subspecies
closely resembles Lepidolina multiseptata
shiraiwensis (OZAWA, 1925; FUJIMOTO,
1936; TORIY AMA, 1942, 1958; CHEN, 1956;
MORIKAWA, 1956, 1958; NOGAMI, 1958,
1961; CHISAKA, 1960, 1962; ISHII & NoGAM!, 1961, 1962; SADA & YOKOYAMA,
1966; CHOI, 1970) in many important respects, but differs from the latter inhaving larger proloculus and thinnerspirotheca. It is similar to L. multiseptata gigantea (GUBLER, 1935; KANMERA,
1954; NOGAMI, 1958; CHISAKA, 1960; ISHII& NOGAMI, 1964; YAMAGIWA & SAKA, in
this paper). However, the former one
differs from the latter, having inflated
fusiform in shape. The present specimens are megalospheric form.
Occurrence:-These specimens foundin the Toba group at Toya, Toba City,
Mie Prefecture, Southwest Japan; theassociated fossils are Lepidolina kumaensis, L. multiseptata gigantea, Yabeina
columbiana, Y. aff. globosa, Metadoliolina
gravitesta and Pachyphloia sp. indet.
Repository:-The present form is deposited in the collection of the Instituteof Geoscience, Osaka Kyoiku University.
Reg. nos. 71004, 71005, 71006, 71007.
Lepidolina kumaensis KANMERA
Plate 31, fig. 3

1952.

Sumatrina annae, KoNISHI, Trans.
Proc. Palaeont. Soc. japan, N. S., no. 5,

cfr.

267

pp. 159-161, pl. 14, figs. 2-5, 7.
1954. Lepidolina kumaensis, KANMERA, Mem.
Fac. Sc£. Kyushu Univ., Ser. D, vol. 4,
no. 1, pp. 22-24, pl. 5, figs. 1-13.
1954. Lepidolina toriyamai, KANMERA, Ibid.,
pp. 24-26, pl. 6, figs. 1-19.
1958. Lepidolina cfr. toriyamai: YANAGIDA,
jour. Geol. Soc. japan, vol. 64, no. 752,
p. 228, text-fig. 2.
1958. Lepidolina kumaensis: NoGAMI, Mem.
Coll. Sci. Univ. Kyoto, Ser. B, vol. 25,
no. 2, pp. 104-105, pl. 2, figs. 8-9.
1958. Lepidolina toriyamai: NoGAMI, Ibid.,
pp. 105-106, pl. 1, figs. 1-2.
1958. Lepidolina toriyamai maizuruensis, NoGAM!, Ibid., p. 106, pl. 2, figs. 1-5.
1960. Yabeina Proboscis: CHISAKA, jour. Coll.
Art. Sci. Chiba Univ., vol. 3, no. 2, pp.
252-253, pl. 9, figs. 1-3.
1962. Lepidolina kumaensis: SuYARI, jour.
Gakugei Tokushima U1!1:v., vol. 12, pp.
38-39, pl. 12, figs. 2-4.
1965. Lepidolina kumaensis : HASEGAWA, Chikyu Kagaku, no. 76, pp. 27-32, pl. 1,
fig. 1-5, pl. 2.
1970. Lepidolina kumaensis: CHOI, jour. Fac.
Sc£. Hokkaido Univ., Ser. 4, vol. 14,
no. 3, pp. 321-324, pl. 5, figs. 1-9, pl. 6,
fig. 1.

Description :-Shell is moderately large,
elongate subcylindrical form. A few outer volutions are crushed away. Inner
two volutions are spherical or subspherical, and beyond the 4th volution shellform resembles its mature shape. Mature specimen (Plate 31, fig. 3) having 10
volutions is 6.2 mm in length and 2.1
mm in width: with form ratio of about
3.0. Proloculus is large, spherical inshape; its outside diameter about 0.3
mm. The heights of the first to the lOth
volution of the above mentioned one are
0.05, 0.06, 0.05, 0.07, 0.09, 0.10, 0.12, 0.10,
0.11 and 0.12 mm, respectively. Spirotheca is very thin, composed of a tectum
and a extremely very finely alveolar
keriotheca, but partly of a single layer.
Thickness of the spirotheca never ex-

268

Nobuo YAMAGIWA and Yukiyasu SAKA

ceeds 0.01 mm in the whole volutions.
Primary transverse
septula occur
throughout shell. Secondary transverse
septula appear first in the third and two(sometimes three) of them developed
between adjacent primary transverse
septula in the 6th to the outer volutions.
They are pendant or thin bar·likeshaped. Parachomata occur throughout
shell, and they come into contact withthe top of primary transverse septula
near the center of chamber.
Remarks:-The present specimen ischaracterized by its large proloculus,
elongate subcylindrical fusiform in shapeand very thin spirotheca. These features practically agree with those of
Lepidolina kumaensis KANMERA fromthe Kuma formation (KANMERA, 1954)
and other Upper Permian in Japan (NoGAMI, 1958; YANAGIDA, 1958; SUY ARI,
1962; HASEGAWA, 1965; CHOI, 1970). It
is closely similar to L. multiseptata gigantea (GUBLER, 1935; KANMERA, 1954;
NOGAMI, 1958; CHISAKA, 1960; ISHII &NOGAMI, 1964; YAMAGIWA & SAKA, in
this paper) in many important characters. The former is, however, different
from the latter in having elongate subcylindrical fusiform in shape. It is amegalospheric specimen.
Occurrence :-A specimen was obtained
from the Toba group at Toya, Toba City,
Mie Prefecture, Southwest Japan. It is
associated with Lepidolina multiseptata
gigantea, L. multiseptata multiseptata,
Yabeina columbiana, Y. aff. globosa, Metadoliolina gravitesta and Pachyphloia sp.
indet.
Repository :-It is deposited in the collection of the Institute of Geoscience,
Osaka Kyoiku University. Reg. no.
71008.

Subfamily Neoschwagerininae DUNBAR
and CONDRA, 1928
Genus Y abeina DEPRAT, 1914
Yabeina columbiana (DAWSON)
Plate 31, fig. 41879. Loftusia columbiana, DAWSON, Qaurt.
jour. Geol. Soc. London, vol. 35, pp.
69-75, pl. 6, figs. 1-7.
1942. Yabeina columbiana : THOMPSON andWHEELER, jour. Paleontology, v:ol. 16,
no. 6, pp. 708-710, pl. 106, fig. 5; pl.
107, fig. 5; pl. 108, fig. 1; pl. 109, figs.
1-4.
1950. Y abe ina columbiana :THOMPSON, WHEELER and DANNER, Contribution fromthe Cushman Foundation for Foraminifera Research, vol. 1, pis. 3-4, pl. 61,
pl. 8, figs. 1-3.
1954. Y abe ina columbiana : KANMERA, Mem.
Fac. Sci. Kyushu Univ., Ser. D, vol. 4,
no. 1, pp. 16-18, pl. 3, figs. 1-7.
1958. Yabeina columbiana : NoGAMI, Mem.
Call. Sci. Univ. Kyoto, Ser. B, vol. 24,
pp. 101-102, pl. 1, figs. 9-10.
1960. Yabeina columbiana: CHISAKA, jour.
Call. Art. Sci. Chiba Univ., vol. 3, no.
2, p. 249-251, pl. 7. fig. 3.

Description :-Shell is medium in size,
inflated fusiform. Several outer volutions are missing. A specimen (Plate
31, fig. 4) of 11 volutions is 4.7 mm inlength and 3.1 mm in width; form ratio
1.5. Proloculus is small, spherical inshape; its outside diameter is 0.14 mm.
The heights of the first to the 11th
volution of the above mentioned one are
0.05, 0.07, 0.07, 0.11, 0.14, 0.14, 0.17, 0.15,
0.16, 0.16 and 0.17 mm, respectively.
Spirotheca is thin, composed of a tectum
and a thin keriotheca with fine alveoli.
Thickness of the spirotheca is 0.01 to
0.015 mm in outer volutions. Primarytransverse septula are present throughout shell. Secondary transverse one first592.

Fusulinids Jrorn Shirna

appear in the fourth volution, and there
is one secondary transverse one in mostcases between adjacent primary transverse ones. They are rather irregular inshape. Parachomata extend to the topof the primary transverse one near the·Center of the chamber.
Remarks:- The present specimen is·closely allied to Yabeina columbiana(DAWSON) described and illustrated fromthe Upper Permian of Japan (KANMERA,
1954; NOGAMI, 1958; CHISAKA, 1960) andBritish Columbia (THOMPSON & WHEELER,
1942; THOMPSON, WHEELER & DANNER,
1950) in having small proloculus, inflated
fusiform, relatively thin spirotheca andother important respects. It resembles
Y abeina globosa (Y ABE, 1906; OzAwA,
1927; FUJIMOTO, 1936; MORIKAWA &SUZUKI, 1961; SUYARI, 1962) .. However,the former one can be distinguishedfrom the latter by its larger proloculus,
thinner spirotheca and more loosely·coiled inner voluions.
Occurrence :-A specimen was obtained
from the Toba group at Toba, Toba
·City, Mie Prefecture, Southwest Japan.
It is associated with Lepidolina lwmaensis, L. multiseptata gigantea, L. multiseptata multiseptata, Yabeina aff. globosa,Metadoliolina gravitesta and Pachyphloia
sp. indet.
Repository :-It is deposited in thecollection of the Institute of Geoscience,
Osaka Kyoiku University.
Reg. no.
71009.
Yabeina aff. globosa (YABE)
Plate 32, figs. 1-6

1906. Neoschwagerina globosa, YABE, jour.
Coli. Sci. Imp. Univ. Tokyo, vol. 21, no.
5, p. 4, fig. 4, pl. 2, fig. 1.
1927. Neoschwagerina globosa: OzAWA, jour.
Fac. Sci. Imp. Univ. Tokyo, Sec. 2, vol.
2, pp. 159-160, pl. 42, figs. 1-2, 4, 6.

269

1936. Yabeina globosa: FuJIMOTO, Sci. Rept.
Tokyo Bunrika Daigaku, Sec. C, vol. 1,
pp. 119-120, pl. 24, fig. 25, figs. 1-4.
1961. Yabeina g!obosa: MoRIKAWA and SuzuKI, Sci. Rept. Saitama Univ., Ser. B,
vol. 4, no. 1, pp. 67-68, pl. 10, fig. 2,
pl. 21, fig. 1.
1962. Yabeina g!obosa: SuYARI, jour. Gakugei, Tokushima Univ., Nat. Sci., vol. 12,
pp. 37-38, pl. 12, fig. 1.

Description :-Shell is medium andfusiform; with bluntly pointed poles,
straight axis of coiling. Lateral slopesof mature shell are nearly straight andslightly convex. Several outer volutions
are missing. Inner three volutions arespherical or subspherical, and beyond
the 3rd volution shell form resembles
its mature stage. The specimen illustrated as fig. 1 on Pia te 32 is 3.9 mm inlength and 2.7 mm in width, with form
ratio of 1.4. Proloculus is small, spherical or subspherical in shape, with outside diameter of 0.02 to 0.04 mm. The
heights of the first to the 12th volution.of the above mentioned specimen are
0.04, 0.03, 0.045, 0.07, 0.10, 0.10, 0.105, 0.14,
0.15, 0.17, 0.20 and 0.15 mm, respectively.
Spirotheca is rather thin, composed ofa tectum and a keriotheca with veryfine alveoli, measuring about 0.02 to
0.03 mm in later stage. Septal count isdifficult because of numerous axial septula. Axial septula first appear in the
6th volution. Primary transverse septula present throughout shell. Secondary transverse septula first appear in
the 6th or 7th volution ; there is one
septulum between two adjacent primarytransverse ones, but in rare cases thetwo occur in outer volutions. Parachomata occur throughout shell; they comeinto contact with the top of the primarytransverse septula near the center ofchamber.
Remarks:- The present form is closely

270

Nobuo YAMAGIWA and Yukiyasu SAKA

similar to Y abeina globosa (Y ABE, 1906;
OZAWA, 1927; FUJIMOTO, 1936; MORIKAWA & SUZUKI, 1961; SUYARI, 1962) inhaving small proloculus, inflated fusiform in shape, rather thin spirothecaand other characters. However, theformer one is represented by the specimens whose several outer volutions are
missing, so the detailed characters can
not be determined with accuracy. It resembles closely Yabeina sp. indet. described and illustrated from the Tsuijigroup (Upper Permian) in the southern
sub-belt of the Chichibu terrain in Shima
Peninsula by YAMAG IW A (1969) in many
improtant characters. The latter one
may belong to Y abeina globosa.
Occurrence:- The present specimens
occurred from the Toba group at Toya,
Toba City, Mie Prefecture, Southwest
Japan. The associated fossils are Lepidolina kumaensis, L. multiseptata gigantea,
L. multiseptata multiseptata, Yabeina
columbiana, Metadoliolina gravitesta andPachyphloia sp. indet..
Repository:-They are deposited in thecollection of Geoscience, Osaka Kyoiku
University. Reg. nos. 71010, 71011, 71012,
71013, 71014, 71015.
Family Verbeekinidae STAFF
and WEDEKIND, 1910
Subfamily Mise!lininae MIKLUKHOMAKLAY, 1958
Genus Metadoliolina ISHII
and NOGAMI, 1961
Metadoliolina gravitesta (KANMERA)
Plate 31, figs. 5-6
1954. Pseudodoliolina pseudolepida gravitesta,
KANMERA,Mem. Fac. Sci., Kyushu
Univ., Ser. D, vol. 4, no. 1, pp. 12-14,
pl. 2, figs. 1-6.

1954. Pseudodoliol£na n. sp. ?, KANMERA,
I bid., pp. 14-15, pl. 2, figs. 7-8.
1954. Verbeekina? n. sp., KANMERA, Ibid.,
pp. 15-16, pl. 2, fig. 9.
1960. Pseudodoliolina pseudolepida gravitesta:
CIIISAKA, jour. Colt. Art. Sci. Chiba
Univ., vol. 3, no. 2, p. 246, pl. 4, figs.
1-6.
1961. Metadoliolina gravitesta: IsHII and NoGAM!, Trans. Proc. Palaeont. Soc. japan,
N. S., no. 44, pp. 163-164, pl. 25, figs.
1-4.

Description :-Shell is medium, elongate
ellipsoidal and broadly rounded polar regions. Inner three volutions are spherical or subspherical, and beyond thefourth volution shell form resembles its
mature stage. A specimen of 10 volutions is 4.7 mm in length and 1.9 mm inwidth; form ratio about 2.6. Perhaps.
a few outer volutions are missing. Proloculus is small, spherical, and its outside diameter is 0.20 mm. The heightsof the first to the lOth volution are 0.05,
0.04, 0.07, 0.07, 0.08, 0.09, 0.12, 0.13, 0.14
and 0.16 mm, respectively. Spirotheca israther thick, composed of a thin tectum
and a thin keriotheca with very finealveoli. In outer volutions, the uppersurface of the tectum is coated with amore or less discontinuous layer ofdense material which is continuous withparachomata. Thickness of the spirotheca in the fourth to the lOth volution
are 0.01, 0.01, 0.007, 0.10, 0.01, 0.015 and0.02 mm, respectively. Parachomata are
well developed, and heights of them area half of the heights of the chamber~they are massive.
Remarks:- This form is represented
by an axial section and another transverse section alone. It is referable
to Metadoliolina gravitesta (KANMERA,.
1954; CHISAKA, 1960; ISHII & NOGAMI,
1961) from the Upper Permian in Japan.
The two ones are closely similar to each

592.

Fusulinids from Shimaother in having relatively thick spirotheca, elongate ellipsoidal form in shaps,
small proloculus, tightly coiling in inner
volutions and other important characters.
Occurrence:- The present specimens
have been obtained from the Toba groupat Toya, Toba City, Mie Prefecture,
Southwest Japan. It is associated with
Lepidolina kumaensis, L. multiseptata
gigantea, L. multiseptata multiseptata,
Yabeina columbiana, Y. aff. globosa andPachyphloia sp. indet ..
Repository:- The present ones aredeposited in the collection of the Institute of Geoscience, Osaka Kyoiku University. Reg. nos. 71016, 71017.

References
CHEN, S. (1956): Fusulinidae of South China,
Pt. 2. Palaeont. Sinica, New Ser. B, no.
6, pp. 17-71, pis. 1-14.
CHISAKA, T. (1960) : On some Permian fusulinids from the Takagami Conglomerate, Choshi Peninsula, Chiba Prefecture, Japan. jour. Coll. Art. & Sci.,
Chiba Univ., val. 3, no. 2, pp. 235-250,
pis. 1-9.
- - (1962) : Fusulinids from the vicinity of
Maiya town, Kitakami mountainland,and Upper Permian fusulinids of Japan.
Ibid., val. 3, no. 4, pp. 519-551, pis. 1-8.
CHOI, D. R. (1970a) : On Some Permian Fusulinids from Iwaizaki, N. E. Japan.
jour. Fac. Sci., Hokkaido Univ., Ser. 4,
val. 14, no. 3, pp. 313-325, pis. 5-8.
- - (1970b) : Permian fusulinids from Imo,Southern Kitakami Mountains, N. E.
Japan. Ibid., pp. 327-354, pis. 9-15.
CoLAN!, M. (1924): Nouvelle contribution a!'etude des Fusulinides de !'ExtremeOrient. Indochine Service Geol., Mhn.,
val. 11, fasc. 1, pp. 1-191, pis. 1-29.
DAWSON, G. M. (1879): On a new speciesof Loftusa from British Columbia. Quart.
jour. Geol. Soc. London, val. 35, pp. 69-271

75, pl. 6.
DEPRAT, J. (1912) : Etude des Fusulinidb
de Chine et d'lndochine et classification
des calcaires a fusulines. Mem. Serv.
Geol. l'Indochine., vol. 1, fasc. 3, pp. 176, pis. 1-9.
- - (1914) : Etude des Fusulinides du Japon,
du Chine et d'Indochine classification des.
calcaires a fusulines (III• Memoire).
Etude
comparative des Fusulinides
d'Akasaka (Japon) et des fusulinides de·Chine et d'Indochine. Ibid., vol. 3, fasc.
1, pp. 1-45, pis. 1-8.
FUJIMOTO, H. (1936) : Stratigraphical andpalaeontological studies of the Titibu
System of the Kwanto-mountainland. Pt.
2, Palaeontology. Sci. Repts., Tokyo Bun-·rika Daigaku, Sec. C, vol. 1, no. 2, pp.
29-125, pis. 1-26.
GuBLER, J. (1935) : Les Fusulinides de Permien de i'Indochine, leur structure etleur classification. Soc. Geol. France,.
Mem., New. Ser., tome ll, fasc. 4, no. 26,.
pp. 1-173, pis. 1-8 (17-24).
HAMADA, T. (1963) : The Gokasho-Arashima
fault zone in Mie Prefecture. jour. Geol.
Soc. japan, vol. 69, no. Sll, pp. 208-209.
HASEGAWA, Y. (1965): "Lepidolina" fromthe Otani conglomerate, Central Japan.
"Earth Science" (Chikyu Kagaku), no. 76,.
pp. 25-33, pis. 1-3.
HANZA\\·A, S. & MuRATA, M. (1963): The
Paleontologic and stratigraphic consideration on the Neoschwagerininae andVerbeekininae, with the descriptions ofsome fusulinid foraminifera from the
Kitakami massif, Japan. Sci. Repts. Tohoku Univ., 2nd Ser. (Geology), vol. 35,.
no. 1, pp. 1-31, pis. 1-20.
IcHIKAWA, K. et al. (1956): Die Kurosegawa
Zone (Untersuchungen i.iber das ChichibuTerrain in Shikoku III). jour. Geol. Soc.
japan, vol. 62, no. 725, pp. 82-103.
lsi·III, K. & NoGAMI, Y. (1961) : On the
new genus Metadoliolina. Trans. Proc.
Palaeont. Soc. japan, N. S., no. 44, pp.
161-166, pl. 25.
- - & - - (1962) : On Yabeina shiraiwensis.
OzAwA and Yabeina yasubaensis ToRIYAMA. jour. Geosci., Osaka City Univ.,

272

Nobuo YAMAGIWA and Yukiyasu SAKA

vol. 6, art. 2, pp. 59-72, pis. 1-2.
- - & - - (1964) : Contribution to the geology and palaeontology of Cambodia, Pt.
1, Permian fusulinids. Ibid., vol. 8, art.
2, pp. 9-37, pis. 1-8.
KANMERA, K. (1953) : The Kuma formation
with special reference to the Upper
Permian in Japan (Geological study of
the Palaeozoic in Southern Kyushu, pt.
3). jour. Ceo!. Soc. japan, vol. 59, no.
697, pp. 449-468.
- - (1954) : Fusulinids from the Upper
Permian Kuma Formation, Southern Kyushu, Japan-with special reference to thefusulinid zone in the Upper Permian ofJapan. Mem. Fac. Sci., Kyushu Univ.,
Ser. D, vol. 4, no. 1, pp. 1-38, pis. 1-6.
- - (1957) : Revised classification of Canceltina and Neoschwagerina, and evolutionof Sumatrininae and Neoschwagerininae.
Ibid., vol. 6, no. 1, pp. 47-64, pis. 19-20.
KoNISHI, K. (1952) : Permian microfossils
in the Dodo conglomerate of the Yasubatype. Trans. Proc. Palaeont. Soc. japan,
N. S., no. 5, pp. 155-165, pl. 14.
MoRIKAWA, R. (1956): Fusulinids from Onagata, Kamiyoshida-mura, northern partof Kanto mountainland. Sci. Rept., Saitama Univ., Ser. B, vol. 2, no. 2, pp. 250260, pis. 32-34.
- - (1960) : Fusulinids from the lwaizaki
limestone. Ibid., vol. 3, no. 3, pp. 273299, pis. 46-53.

- - et al. (1958) : Stratigraphical and biostratigraphy of the "lwaizaki limestone"in the southern Kitakami mountainland.
jub. Pub!. Prof. H. FUJIMOTO, pp. 81-90,
pl. 6.
- - & SuzuKI, Y. (1961); Fusulinids fromthe Akasaka limestone, Pt. 2, Sci. Rept.
Saitama Univ., Ser. B, vol. 4, no. 1, pp.
43-74, pis. 4-22.
NoGAMI, Y. (1958) : Fusulinids from the
Maizuru Zone, Southwest Japan. Pt. 1.
Ozawainellinae, Schubertellinae and Neoschwagerininae. Mem. Coil. Sci., Univ.
Kyoto, Ser. B, vol. 25, no. 2, pp. 97-114,
pis. 1-2.
- - (1961) : Permische Fusuliniden aus dem
Atetsu-Plateau Siidwest Japan, Teil 2,
Verbeekininae, Neoschwagerininae. Ibid.,
vol. 28, no. 2, pp. 159-244, pis. 1-7.
OzAwA, Y. (1.922): Permian note on theclassilication of the family Fusulinidae.
jour. Geol. Soc. japan, vol. 29, pp. 352365.
- - (1925) : Palaeontological and stratigraphical studies on the Permo-Carboniferous limestone of Nagato, Pt. 2, Palaeontology. jour. Coli. Sci., Imp~ Univ.
Tokyo, vol. 45, art. 6, pp. 1-90, pis. 1-14.
- - (1927) : Stratigraphical studies of theFusulina limestone of Akasaka, Provinceof Mino. jour. Fac. Sci., Imp. Univ.
Tokyo, Sec. 2, vol. 2, pt. 3, pp. 121-164,
pis. 34-46.

Explanation of Plate 31
Fig. 1. Lepidolina multiseptata gigantea (GUBLER).
Axial section .... x 15
Fig. 2. Lepidolina multiseptata multiseptata (DEPHAT).
Axial section .... x 15
Fig. 3. Lepidolina kumaensis KAI':VIERA.
Axial section .... x 15
Fig. 4. Yabeina columbiana (DAwsoN).
Axial section .... x 15
Figs. 5-6. Metadoliolina gravitesta (KAN:VIERA).
5. Transverse section .... x 20
6. Axial section .... x 20
Fig. 7. Pachyphtoia sp. indet.
Transverse section? .... x 40

Y AMAGIWA and SAKA:

Fusulinids from Shima

Plate 31

592.

Fusulinids from ShimaOZAWA, T. (1970): Notes on the phylogeny
and classification of the superfamily
Verbeekinoidea (Studies of the Permianverbeekinoidean Foraminifera-l). Mem.
Fac. Sci., Kyushu Univ., Ser. D, vol. 20,
no. 1, pp. 17-58, pis. 1-9.
SADA, K. & YoKoYAMA, T. (1966): Upper
Permian fusulinids from the Taisyaku
limestone in west Japan. Trans. Proc.
Palaeont. Soc. Japan, N. S., no. 63, pp.
303-315, pis. 23-24.
SKINNER, J. W. & WILDE, G. L. (1954) : Fusulinid wall structure. jour. Paleont.,
vol. 28, no. 4, pp. 445-451, pis. 46-52.
SuY ARI, K. (1962) : Geological and palaeontological studies in central and eastern
Shikoku, Japan, Pt. 2, Palaeontology.
Tokushima Univ., jour. Gakugei, Nat.
Sci., no. 12, pp. 1-64, pis. 1-12.
TlloMPSON, M. L. (1948): Studies of American fusulinids., Univ. Kansas, Paieont.
contrib., Protozoa Art. 1, pp. 1-184, pis.
1-38.
- - & WHEELER, H. E. (1942) : Permian
Fusulinids from British Columbia, Washington and Oregon. jour. Paleont., vol.
vol. 16, no. 6, pp. 700-711.
- - , - - & DA:-o;KER, W. R. (1950): Middle
and Upper Permian fusulinids of Washington and British Columbia. Contrib.
Cushman Found. Foram. Research, vol. 1,
Pts. 3-4, pp. 46-63.
ToRYAMA, R. (1942) : The fusulinids of the
Yasuba conglomerate in the Province ofTosa, Japan. jour. Geol. Geogr., vol. 18,
no. 4, pp. 237-247, pis. 24-25.
- - (1958) : Geology of Akiyoshi, Pt. 3, Fusulinids of Akiyoshi. Mem. Fac. Sci.,
Kyushu Univ., Ser. D, vol. 7, pp. 1-264,
pis. 1-48.

ImauraMotouraOgurajima
Omurajima

4-

irll

* ir ifll
~~~~

J:-h

:ktt~

273

- - (1967): The Fusulinacean Zone of Japan.
Mem. Fac. Sci., Kyushu Univ., Ser. D,.
vol. 18, no. 1, pp. 35-260.
YABE, H. (1906) : A contribution to theGenus Fusuiina, with notes on a Fusulina limestone from Korea. jour. Colt.
Sci., Imp. Univ. Tokyo, vol. 21, art. 5,.
pp. 1-36, pis. 1-3.
- - (1964a) : Lepidoiina Problem. Proc. fa·
pan Acad., vol. 40, no. 3, pp. 214-219.
- - (1964b) : Problems on the genus Lepidolina (Part 1). "Fossil" (Kaseki), Palaeont.
Soc. japan, no. 8, pp. 134-139.
- - (1965) : Problems on the genus Lepido·!ina (Part 2). Ibid., no. 9, pp. 36-55.
- - (1966) : Problems on the genus Lepidolina (Supplement). Ibid., no. 12, pp. 47-55.
YAMAGI\\' A, N. (1954) : Neoschwagerininae
from the Shima Peninsula, Japan. Trans.
Proc. Palaeont. Soc. japan, N. S., no. 23,
pp. 235-242, pl. 32.
- - (1957) : Stratigraphy and geologicalstructure of the eastern area of Shima
Peninsula. jour. Ceo!. Soc. japan., vol.
63, no. 740, pp. 263-272.
- - (1969) : Tsuiji Group in the easternarea of Shima Peninsula, Mie Prefecture.
Mem. Osaka Kyoiku Univ., III. Nat. &Applied Sci., vol. 18, pp. 71-80, pl. l.
- - & IsHII, K. (1957): Yabeina from Omura Island, Shima, Mie Prefecture. ]ubi.
Comm. Prof. H. FUJIMOTO, pp. 58-65,
pis. 3, 4.
- - & SAKA, Y. (1967) : The Mesozoic andPalaeozoic in the eastern part of Shima
Peninsula. Guide-boo!? for geologic excursion (Nagoya), pp. 1-24.
YANAGIDA, J, (1958): The Upper Permian
Mizukoshi Formation. jour. Ceo/. Soc.
japan, vol. 64, no. 725, pp. 222-231.

Shiranezaki
Toba
Toy a

8 iH ~~.~t
.~

)])]

lilt

:fr

274

Nobuo Y AMAGIWA and Y~~kiyasu SAKA--~-------------

Explanation of Plate 32
Figs. 1-6. Yabeina aff. globosa (YABE).
1. Axial section .... x 20
2. Axial section .... x20
3. Tangential section (somewhat oblique) .... x 24
4. Sagittal section .... x 20
5. Tangential section .... x 15
6. Tangential section (somewhat oblique) .... x 15

YAM AGIW A and SAKA :Fusulinids /?" O?n Shima

Plate 32

Trans. Proc. Palaeont. Soc. Japan, N. S., No. 85, pp. 275-279, pl. 33, April 20, 1972

59:3.

THE TRIASSIC BRYOZOA FROM KUSAKA, SAKAWA BASIN,
SHIKOKU, JAPANSUMIO SAKAGAMI
Department of Geology, Faculty of Education, Ehime University,
Matsuyama, Japan

iiBJ;lilfi;:JIIftJtl!.f3".fJ2!£:::::[Hc:::. fHl: i.P-:::>""C 'l'fi"t"!-tW.±t.JqJ,:JII;i~Jti!.EI r (;f:Eftj:) t.J>G9£
J"!L., Ceriopora sp. C. l..""C\\IH!f C*ileli\X) L.t.:~;,t;j;: OW.f\· 6t:l() fZ::.-:::>v'""Ct~F.iL.t.:*,'i!,1~ • .:C:11-t.J; Pseudobatostomella }!J~ O)$[rfil!-:" £, .Q:::. C;~~~j!IJOJJ L. t: O)""t', Pseudobatostomella kobayashii SAKAGAM! cif/l4'; l.. ""Ciitiiil(if£i:!fi" .Q.
:=::tlJcO):::.ltEIHi, 19631.1~ FLUGEL fZ::..t-:>""Ct-t.f.S~:l"Lt.:t.J~. :t0)1~. ·!J-J-?tO) Ellesmere ,r:.&c '/ J::'.:c. }- O)~!tl!.i.PG 11 fllit.J~)j~ijil(i~i5-~~'1""Cv'.Q, ::_O)~ifiJ)[""Cvt. FLUGEL (1963)
tJf~O) :::. :11-G O):::::ill~:::.lt !!Hz::. -:::>v'""C *-t.ft l.., ;li,hit""C ~tiWi:i:! JJ i\1li~llt.<=l~il' G~ilJI~Jl!~tW±
IZ::. .t-:> ""C tl~llllG~ ;l"Lt.: ::.It !E. (Batostomella /iJ~ C. L. ""C
3 f!fi) 0)? i? 1 f•fiil; Pseudob.
kobayashii !Z::.&(JJ,i".Q:::. ci.PG, Eiii1iiJ1ii::::.ltrt\O)J:tl!.'l!J:if!fttlt.=1~Hc<:vt.t4: ::::1HC.<:;lr,.Q:::.
7.J;piifff- ~ :11- .Q 0) ""(' fi}~i'li l? ~ -_t .Q :::. l? J1J!"" Q:!;!i J: lrf :k

*1E

c.

c.

<

0

portunity for study of the present materials. I am also deeply indebted toProfessor Kotora HAT AI of the Tohoku
University for kindly reading the manuscript and for his constant encouragement.

Introduction and acknowledgements
Some 25 years ago, Dr. Teiichi KOBAYASHI discovered a small bryozoan fauna
in a sandstone of the Oxytoma-Mytilus
beds of the Upper Triassic Kochigatani
series at Kusaka in the eastern part of
the Sakawa basin, Shikoku island, Japan.
They were identified by him with Ceriapara sp. and reported in 1948 and 1949,
but without description.
Recently, Dr. KOBAYASHI sent me the"' Ceriopora " bearing thin sections forstudy and the present article is a result-of the examination.
Before going into the description, I
would like to express my sincere thanks
to Dr. Teiichi KOBAYASHI, Professor
Emeritus of the University of Tokyofor his kindness in giving me the op-

Description of species
Pseudobatostomella kobayashii

SAKAGAMI, n. sp.
Plate 33, figs. 1-6.

1948. Ceriopora sp., KoBA Y ASH!, p. 176.
1949. Ceriopora sp., KoBAYASHI, p. 137.

Six thin sections of fragmentary
zoaria were examined. Zoaria probably
incrusting in some parts, but consistingof cylindrical stem, about 2.5 to 3.0 mm
in diameter. Zooecial tubes subangularly oval in tangential section, theirshorter diameter usually ranging from

Received March 6, 1971; read October 22,
1971 at Fukuoka.

275

276

Sumio SAKAGAMI

0.200 to 0.250 mm, 0.150 mm in minimum
diameter, and nearly straight or somewhat curved outward from the inner
region. Zooecial wall very thin in very
short distance of immature region, andgradually thickened to mature region.
Mesoecia rare, usually circular, theirdiameter ranging from 0.040 to 0.100mm.
Well developed acanthoecia surroundedby concentric fibrous tissue, ranging
from 0.040 to 0.080 mm in outer diameter,
less than 0.010 mm in inner (pore) diameter, irregularly arranged in wall andin some cases disposed at wall margin
where zooecial tubes angularly shaped.
Diaphragms very thin, at intervals of
0.25 to 0.45 mm.
Remarks:- The present species seems
to be near to Pseudobatostomella jahutica(LAZUTKINA) (1963) from the Lower
Triassic (lnduan) of Siberia and Pseudobatostomella morbosa MOROZOVA (1969)
from the Upper Triassic (Carno-Noric)·of the. southeastern part of Pamir in·their general appearances, but the pre·sent new species can be distinguishedfrom the latter two by the larger diameters of the zooecial tubes.
The present form also resembles"Batostomella"? (2) which SUGIYAMA(1941) described in association with twoother forms of " Batostomella " : B. (1)and B. (3) ·from the upper course of theMotourakawa, Mitsuishi-gun, Hidaka
province in Hokkaido, Japan in the dia-meter of the zooecial tube and otheressential characters except for the presentation of diaphragms. In SUGIYAMA's
description, however, it was stated thatthe diaphragm is probably absent, but
his illustrations show that there are twodiaphragms in a zooecial tube. Although
SUGIYAMA's original specimens should
be reexamined, there is a high possibility that " Batostomella" ? (2) is identical with the present species.
The specific name is dedicated to Dr.
Teiichi KOBAYASHI who collected thepresent materials.
Occurrence and geological age: -According to KOBAYASHI and lCHIKA W A(1950), the Upper Triassic Kochigatani
series distributed in the Sakawa basin
can be divided into three divisions, eachcharacterized by fossil zones as shownin Table 1.
The lower division of the series consists mainly of hard, massive sandstoneintercalated with conglomeratic sandstone and conglomerate and is characterized by the Oxytoma-lvfytilus fauna.
KoBAYASHI (1949) discriminated fromthat division a large number of pelecypods, one brachiopod, bryozoans and'ammonites. Among them the pelecypod·fauna was studied in detail by KOBAYASHI and lCHIKA w A (1950) and the geological age was considered to be Early
Carnic by them.
The present materials· w~re collected

Table l.

Upper Division

Mic!clle Division

Entomonotis Beds ·{ tenuic.ostata-zabaikarica Bedochotica-densistriata Bed

Late Noric

Myoconcha Beds

Late Carnic
or Early _Noric

Hatobia.Tosapecten B·ecls { Tosap~cten Beds
. · ......
,
HatobwBeds..

I

Middle Carnic..•·==-----~ :"_ -----··----·----------- - -Oxytoma·Mj!Ji{us · Be'ds. Early Carnic

1

593.

Triassic Bryozoa from Sakawa

by KOBA Y ASH! from a sandstone of the
Oxytoma-Mytilus beds at Kashiwai of
Kusaka-mura, the Sakawa basin of Kochi
Prefecture.
Repository and Specimen No.- The specimens are preserved in the collectionof the Department of Geology, Facultyof Education, Ehime University. Reg.
Nos. 1001 (holotype), 1002, 1003, 1004, 1005
and 1006 (paratypes).

Brief note on the Triassic Bryozoa
of the world
In the Triassic system, bryozoan remains are extremely rare in the world.
FLUGEL (1963) revised the Triassic Bryozoa known by that time and recognized
13 species in 4 genera of Cyclostomata
and 9 species in 7 genera of Trepostomata aside from some indeterminablespecies. Subsequently, however, 10 species of Bryozoa were newly added by
FRITZ (1961), LAZUTKINA (1963) and MoROZOVA (1965, 1970).
FRITZ (1961) described and illustrated
Arcticopora christiei FRITZ from Lake
Hazen, northeastern Ellesmere island in
Canada and the geological age was statedby BoLTON (1961) as " ... There is, therefore, little doubt that the bryozoan bed
is Triassic, not Permian .... The bryozoan
bed is thus not younger than Lower
Triassic (early Upper Scythian age)".
LAZUTKINA (1963) described one bryozoan species, Pseudobatostomella jakutica(LAZUTKINA) under the generic name of
Batostomella from the Lower Triassic(Induan) of Jakutii in Siberia, USSR.
MOROZOVA (1965) reported Polypora
darashamensis NIKIFOROVA without description from the Lower Triassic (lower
part of the Induan stage) of Zakavkas(Trans-Caucusia). Though one indeterminable species of Polypora (?) was de-277

scribed from the early Upper Triassic(upper Carnic) of Hungary by VINASSA
DE REGNY (1901), it is of doubtful material as mentioned by FLUGEL (1963) and
MOROZOVA (1965).
Recently, MOROZOV A (1969) describedfrom the Triassic in USSR, Paralioclema abnonne MOROZOVA (Carnic, northwestern part of Caucusus), Paralioclema
fonnosum MOROZOVA (Noric, northwestern part of Caucusus), Paralioclema dagysi MOROZOVA (Carnic, northwesternpart of Caucusus), Paralioclema amurense
MOROZOVA (Anisic, Primorsk), Pseudobatostomella sparsa MOROZOV A (Anisic,
northwestern part of Caucusus), Pseudobatostomella debilis MOROZOV A (CarnoLaclinic, Primorsk) and Pseudobatostomella morbosa MOROZOVA (Carno-Noric,
Pamir).
Table 2 shows the chronological rangesof the Triassic bryozoan species reporteel and/or described after the revision
by FLUGEL (1963).
It is noted that all of the bryozoans
shown in the table comprise the so-called" relic " from the Paleozoic era except
for Arcticopora christiei. a genus thatwas newly established for the species
by FRITZ (1961).
FLUGEL (1963) mentioned that "Although any Lower Triassic (Scythic) bryozoans have not been clescribecl, Fenestella and Stenopora type bryozoans havebeen reported from the GlyptophicerasOphiceras bed (lower Scythic) of east
Greenland by TRUMPY (1960). They are
expecting to be described by an American student." After the revision of
FLUGEL, howev·er, three Scythic bryozoans were added from Ellesmere island,
Siberia and Trans-Caucusia.
The present article is the first description of the Triassic Bryozoa in Japan.
However, bryozoan remains but withsome doubt have recently been recognized278

Sumw SAKAGAMI
Table 2.

1

1- Scy.
Paralioclenza anzurense MoRozovA
Paral. abnorme MoROZOVA
Paral. dagysi MoRozov A
Paral. formosum MoROZOVA
Pseudobatostomella jakutica LAZUTKINA
Pseudob. spars a MoRozov A
Pseudob. debilis MOROZOVA
Pseudob. kobayashii SAKAGAMI, n. sp.
Pseudob. morbosa MoRozov A
Arcticopora christiei FRITZPolypora darashanzensis N1 KI FOROV AAni.

I Lad. I Car. I .Nor. ~~haj~----~~------

I

I

I

--I

I

;

i
I

-----

in the lower member of the Triassic
Nakijin Formation distributed in Okinawajima, Ryukyu by ISHIBASHI (1969), but
no detailed study has been made. On
the other hand, about 30 years ago, SuGIYAMA (1941) described 3 indeterminablespecies of " Batostomella" (one of themwith a question mark) from four localities of the so-called Hidaka group distributed in central Hokkaido and he considered the geological age of the four
localities to be the same because one of
the three "Batostomella" (1) was mutual
at the four localities. However, FUKADA(1949) pointed out that the brachiopod
fauna from one of SUGIYAMA's bryozoan
localities (Iwabenosawa, Simukappumura), although not the same localityof " Batostomella " ? (2) but yielded"Batostomella" (1), is Triassic rather!
I

I

than Permian in age. " Batostomella" ?
(2) from the Hidaka group seems to bealmost identical with Pseudobatostomella
kobayashii, n. sp. described here. Under
such circumstances the three forms of" Batostomella" recorded by SUGIYAMA
should be reexamined, but unfortunately
the depository of the bryozoan specimens
studied by him is uncertain.

References
BoLTON, T .E. (1961) : Additional Arcticopora
from the Triassic of northwestern Ellesmere island. Proc. Geol. Assoc. Canada,
vol. 13, pp. 55-56.
FLOGEL, E. (1963) : Revision der triadischen
Bryozoen und Tabulaten. Akad. Wiss.,
Wien, Sitzungsber. Abt. 1, Bd. 172, pp.
225-252.

Explanation of Plate 33
Figs. 1-6. Pseudobatostomella kobayashii SAKAGA1vll, n. sp.
1, 2. Longitudinal sections of paratype (No. 1002) and holotype (No. 1001), respectively,
x 20. 3, 4. Enlarged parts of Fig. 2, x 60. 5, 6. Enlarged parts of tangential sectionsof para type (No. 1002) and holotype (No. 1001), respectively, x 60.
Photo by SAKAGAMI.

SAKAGAMI :Triassic Bryozoa fr om Sakawa

Plate 33

593.

Triassic Bryozoa from Sakawa·FRITZ, M.A. (1961) : A new bryozoan genus
from Lake Hazen, northeastern Ellesmere
island. Proc. Geol. Assoc. Canada, vol. 13,
pp. 53-55, pis. 1-3.
FUKADA, A. (1949) : On the Brachiopoda
from the "schalstein formation" in thecentral mountain range of I-Iokkaido.
jour. Geol. Soc. japan, vol. 55, nos. 648,
649, pp. 123-124.
IsHIBASHI, T. (1969) : Stratigraphy of theTriassic formation in Okinawa-jima, Ryukyus. Mem. Fac. Sc£., Kyushu UnZ:v., Ser.
D, Geology, vol. 19, no. 3, pp. 373-385, pl.
53.
]{oBAYASlli, T. (1948): The geotectonics of
the Japanese Islands. 2, Meguro Book Co.
· - - (1949) : Shikoku region. Regional geology of japan. Asakura Book Co.
·--and IciiiKAWA, K. (1950): On the Upper Triassic Kochigatani series in the
Sakawa basin in Japan and its pelecypodfaunas. jour. Fac. Sci., Univ. Tokyo, Sec.
2, vol. 7, pt. 3, pp. 179-206.
LAZUTKINA, O.F. (1963) : Nakhodka mshanki

Hidaka province
Iwabenosawa
Kashiwai
KusakaMitsuishi-gun

f]

l§i

IN

1 '7 "" Cl) iR

t8
rl

fr
T
:fi 1tF>

279

paleozoiskogo rocla Batostomella v triase.
Paleont. Zy., no. 4, pp. 126-128.
MoRozovA, I.P. (1965): BRYOZOA in Razvitie i smena morskikh organizmov na rybeze paleozoja i mezozoja (edit. RuziiENTSEV, V.E. and SARYCHEVA, T.G.). Akad.
Nauk SSSR, Trudy Paleont. !nsf., tom.
108, pp. 183-197, pis. 25-28.
- - (1969) : 0 sistematicheskom sostave irasprostranenii mshanok v triase. Akad.
Nauk SSSR, Paleont. Zy., 2, pp. 49-57, pis.
7, 8.
- - (1970): Mshanki pozdnei permi. Akad.
Nauk SSSR, Trudy Paleont. Jnst., tom.
122, pp. 1-347, pis. 1-64.
St.:GIYA:'.IA, T. (1941) : On the geological ageof the limestone containing Bryozoa inthe Hidaka group. jour. Geol, Soc. japan,
vol. 48, no. 571, pp. 189-194.
VINASSA DE REGNY, P. (1901) : Trias-TabuIaten, Bryozoen unci Hydrozoen aus dem
Bakony. Resultate wiss. Erforsch. Balatonses, Bd. 1, 1, pp. 1-22, pis. 1-3.

Motourakawa
Okina wa-jima
RyukyuSakawa basin
Simukappu-mura

7C

iill i•'J

i<P

*'11!

Jj,[

I''·

'"'
£<k

t!c Jll ~ J:[gdo 7& H

Trans. Proc. Palaeont. Soc. Japan, N.S., No. 85, pp. 280-292, pl. 34, April 20, 1972

594.

SOME BAJOCIAN AMMONITES FROM KIT AKAMI,NORTHEAST JAPANTADASHISATO
Geological Institute, Faculty of Science, University of Tokyo;!U:LIJti!lJ: I) il~LJ-=: _.,\,) 3 '/7 :/l}jlj:fifC-?v'"C: 13;$:C')---\,;/ 3 YT :/f'i 7~:fi{t:fiC')iffi:L1\,; ""7 i/'iC')fi!!.C')n~n-ri E f'IT'$t.J: n-mi.J~c:· ~ t.J:i.J' '? t-::, :li±i.fi:;!tJ:.wtl!lc:·t*l,R-zE
ht-:t':l;;Js: c., 4-'i c:·tlc~'i'E hff::::y~'i'E h"Cv't-= tl\'\*'2~N1A-:t'f'Jr:, r~f~!i!l!RC')~;t±ffi:Ji&.:t5
J: LF~Hg$k1tC') Jl 1 imll!ii.J~i.J't.J: IJ <;b u,n-mC')M~ c. t.J: .::s:::. c. i.J~;bi.J, '? t-=.
100;t±ffi:l?-l v'i:£:(:;j;:c:· 1m C. L- "C~ 1J t& ') :::. C. i.J>t: ~, 3 - P ,,,_..~t:RifflC') Otoites sauzei mfU•f'lt'i'E;h,.::S, 'it-=:JI Jiml'&f'i, d;-t.J:< C. <bil~~C'){t-Z;t1H'il'8!c~-t.::Sf.RIJ, Otoites sauzei~
Stephanoceras humphriesianum fWC')-fjf,5J'fCM.I:t~ ;h,.::S,:::. CI),J,%i:fi!l'fv'i, :£:1* c. L- "C;!t~::*ll~;!ti11.'ifi~C') I"Jn'/flt!JCI)J!ro:fi!l'f c. ~illv'i!l:*~~fifdc <0 .::s i.J~,mC')v~~~~. ®rn*~~C')~:fi!lf.C.t~m~tC')~<O.::s.
~ m~i.JqU~I'i':mi\c\Bajocian, as adopted in the recommendation of the Subcommission of Jurassicof IGC, at the Luxembourg Symposiumin 1962, is represented best by a fractionof the Jurassic column in the south Kitakami region in Japan. Its correlation
is based on the poorly known ammonite
faun ules (SA TO, 1962; TAKAHASHI, 1969),
besides some lamellibranch faunas (HAYAMI, 1961).
The faunules comprise some characteristic Bajocian species, but many are
more or less crushed and remained undescribed.
Better preserved specimens of the ammonites are recently collected by F. TAKIZA WA of the Geological Survey and
CHIKARAISHI of the Nihon University,from the Ojika Peninsula. These collections comprise some new forms not described yet, and offer more solid basisof the correlation. Bajocian, or more

precisely, a zone which should fall in·
the range from Otoites sauzei zone to·Stephanoceras humphriesianum zone isstrongly suggested by these materials.
In this occasion, old but undescribed
specimens of ammonoids collected fromthe corresponding formations and stored
in the University of Tokyo are describedand figured. These are in favour of
attributing the age of the formation to
Otoites sauzei zone, in addition to previously described Stephanoceras sp. cf.
S. plicatissimwn (QUENSTEDT) and Sonninia sp. cf. S. corrugata (SOWERBY).
The Bajocian is one of the best represented stage of Jurassic in the eastern and southern parts of the circumpacific, including western Australia. The
Bajocian ammonite faunas have, however, regional particularities by different
composition in each area, though interconnection among neighbouring areas iseasily recognized by the occurrence of
certain common genera. Since only asmall number of species have been hith-* Received March 12, 1971; read June 27,
1970 at Mito.

280

594.

Bajocian ammonites j1·om Kitakami

erto reported from Japanese Bajocian. it
will be useful from the standpoint ofpalaeogeography and correlation to givenotes here on the newly found faunules.
The ammonites of the Japanese Jurassic are generally quite poorly preserved.
The test is usually lost, and the casts
are twisted by the later tectonic deformation. This is particularly true for the
Kitakami Jurassic, where specimens sufficiently well preserved for full systematic description are rarely found up to
the present.
The newly discovered specimens represent Bajocian families of Sonninidae.
Otoitidae, Stephanoceratidae and probably Strigoceratidae. The combinationof these families are reported widelyfrom the Pacific. The common elements
are recognized between Japan and thesecountries. Among these, the south Alaskan fauna is the most closely related to
the Japanese one, as in the case of
Toarcian and Aalenian (SA TO, 1962a).
I am much indebted to Mr. T AKIZA w A.and Mr. CHIKARAISHI for kind permission·Of studying their materials, and to Prof.
HAT AI for granting me to refer to the.collection of the Tohoku University.
Thanks are also due to Dr. TAKAHASHI
for his critical discussion and to Prof.
WESTERMANN for his critical examination of the present materials.
Systematic descriptions

Genus Pelekodites BUCKMAN, 1923

Pelekodites (Spatulites) spatians(BUCKMAN)
Pl. 34, fig. 1a, b.
1928. Spatulites spatians BucK:VIAI', Type Ammonites, pl. 765.
1969. Pelekodites (Spatulites ?) n. sp. aff. P.
spatians (BcciOIA:'-:), WESTER/\IANN, pl.

281

32, fig. 4a, b.
1969. Sonninia sp., TAKA!IASIII, pl. 18, fig. 7,
9, non fig. 3 and ? pl. 19, fig. 7.
?1969. Hosoureites cf. ikianus (YoKoY Al'vlA),
TAKA! lASH!, pl. 19, fig. 8.

Material :-A single specimen preserved to the end of the whorl. but thetest was completely removed. Collection
HAY AMI.
Description:- The whorls become elliptical due to the compression acted obliquely to the axis of coiling. Diametermeasured along the longer axis is about
55 mm and that of the shorter axis about
30 mm. Thus the maximum diameter
would be of the order of 40 mm or more.
The umbilical diameter is about 20 mmalong the longer axis, thus occupies
about 36% of the diameter.
This is a small form with spatulate
lappets. The ventral aspect is not clearlyvisible but on the internal mould is observable well differentiated low hollow
keel as a trace of narrow flat belt surrounding probably fastigate venter. The
whorl section can not be confirmed correctly because of flattening, but is likely
to be rather elongated oval. The volution is rather evolute. Umbilical wall is
steeply inclined, with rounder border.
Costation is generally falcoid, rather
rursiradiate, terminating at the ventraledge without forward projection, irregularly fasciculate in inner whorls but
bundled by umbilical bullae on the lastwhorl. Ribs become abruptly weakened
on the last quarter of the last whorl,
where somewhat sinuous striae substit!lte the ribs.
Suture line is simple, characterized byslender lobes.
Remarlls :-This species resembles superficially inner whorls of certain Witchellids. Especially fasciculate and flexiradiate costation is a common characterof the two.

282

Tadashi SA TOBUCKMAN's genera, created mostly on
the basis of single species, are not generically separable from Pelekodites which
has the page priority among others.
WESTERMANN (1969, p. 116) further advanced and regards this group of minute sonninids as male equivalent of Witchellia laeviuscula- W. sutneri 'plexus'.
He tentatively admitted Spatulites as asubgenus of Pelekodites, in taking its
stronger costation than that of Pelekodites in consideration.
The present specimen is conspecificwith BuCKMAN's spatians, in general appearance, except more prominent umbilical bullae which bundle irregularly twoor three flexiradiate costae. However,the specimens can be attributed to the
BucKMAN's species, because slight differences of costation would be better
considered as intraspecific variation
rather than specific.
TAKAHASHI's 'GrajJhoceras' sp. A, and'Sonninia' sp. A are arbitrary. His pl.
18, fig. 7 and fig. 9 (and probably pl. 19,
fig. 8) are probably conspecific with this,though too much fragmentary to be determined specifically, except pl. 18, fig.
9, which has the same fasciculate strong
ribs as in the present specimen. His' Sonninia' sp. A (pl. 18, fig. 3) should be
excluded from this species, and compared
to Sonninia sp. cf. S. corrugata (SA TO,
1962a, pl. 9, figs. 3, 4).
Occurrence:- West of Tsunakizaka,
Tsunakizaka Formation.
Associatedwith Strigoceras sp. which will be described below.
Pelelwdites sp. cf. P. pelekus
BUCKMAN, 1923
Pl. 34, fig. 2a, b.
1962a. Sonninia(5405302).

sp.,

SATO,

pl.

9,

fig.

2

1969. Sonninia sp., TAKAHASHI, pl. 17, fig ..
6, 7 and ? fig. 8; ? pl. 18, fig. 4.

Material:- Two crushed specimensfrom black mudstone stored in University of Tokyo. 43IIR -5111, collection
YAMASHITA, 5405302, collection AKIYAMA.
Description:- Exact measurements are
impossible because of deformation. Specimen 43IIR-5111 which preserves lappets is about 35 mm in maximum diameter along the longer axis, and about 20
mm along the shorter axis of the deformed elliptical whorls. Thus the diameter measured just behind the aperture is likely to be of the order of 30
mm. The umbilical diameter is about
15 mm along the longer axis, occupying
about 43% of the diameter.
Small shell of rather evolute volution,.
with spatulate lateral lappets. Whorls
are likely to be slightly depressed, withbroadly convex and keeled venter. Plicate costation is appreciably rursiradiate, irregularly fasciculate and finallysmooth and striated on the last quarterof the last whorl.
Remarks :-Pele!wdites spatians, described above, is different by its smaller
conch. more markedly rursiradiate costation, and weaker umbilical bullae,.
though not totally absent.
This form is in close affinity with theEnglish Pelelwdites pele!cus BucKMAN,.
which was only figured but not described. The unfavorable state of preservation of the present form does not
permit decisive identification. 'Nannoceras nannomorphum' BUCKMAN, 1923,
is another species closely related, but
this is not specifically separable frompe/e/ws (WESTERMANN, 1969, p. 116).
TAKAHASHI's 'Sonninia ' sp. A, inwhich 8 specimens are grouped, comprises largely divergent forms. His pL

594.

Bajocian ammonites from Kitakami

17, figs. 6 and 7, and possibly fig. 8 as
well as pl. 18, fig. 4 might be conspecificwith the present one. From Wide Bayof Alaska Peninsula, WESTERMAN:\ reported Pelekodites cf. P. pelekus (1969,
pl. 32, figs. 1-2) which is also closely
related and cannot be distinguished fromthe present form even specifically.
Occurrence :-Specimen 43IIR -5111 fromthe west of Yobaijitoge, 5405302 fromTsunakizaka. Both from Tsunakizaka
Formation.

283

available.
Occurrence:- Procured from a boulder
at the Locality 54044, south of Tsunakizaka.

Genus Normannites MUNIERCHALMAS, 1892

lVonnannites (ltinsaites) sp. cf.
N. (I.) itinsae (MCLEARN)
PI. 34, figs. 3-9.

1969. Otoites sp., TAKAHASHI, pl. 9, figs. 2-5.

Genus Otoites MASCKE, 1907

Otoites sp.
PI. 34, fig. 10.

Material:-An external mould of thelast half volution found in a boulder.
Description:-Though fragmentary, thespecimen shows rather involute coiling,crater-like umbilicus with well definedand steeply inclined umbilical wall. Stoutand straight primary ribs are on theumbilical wall, terminated by minuterounded tubercles from which two or
three secondary ribs are branched off.
On the last part of the preserved whorl,
however, only two secondary ribs arebifurcated. Costation as a whole isgenerally rectiradiate, but on the lastwhorl it becomes slightly geniculatedwith rursiradiate primaries.
Remarlls :-The general appearance,
especially costation, is strongly suggestive of Otoites contractus group. Ribbing
appears in the present specimen somewhat finer than the group of contractus(SOWERBY), as in Otoites delicatus BucKMAN (1919, Type Ammonites, pl. 142).
But this might be resulted from thelateral deformation and it will be reasonable that the specific determination
is not given until better specimen is

A1aterial :-Some thirteen fragmentary
specimens which represent various developmental stages.
Description:- All the specimens are
deformed to some extent, obliquely or
perpendicularly to the coiling axis, sothat the original shell form is difficult
to be confirmed. For the same reason,
it is not quite certain that all the specimens belong to a single species, evenif each specimen presumbably represents
different developmental stage.
Coiling is rather evolute; a specimen(Pl. 34, fig. 5b) representing inner three
volutions shows open and shallow umbilicus. Overlapping of the whorl by
next one is confined to about outer one
third of the whorl height, and the umbilical suture lies approximately on theline connecting the points of bifurcationof ribs on the covered whorl.
Whorl section is likely to be depressedoval with broad and gently convex venter. A figured specimen (Pl. 34, fig. 8b)
presents depressed Teloceras-like whorl
section. But as the impression of theventral region of the preceding whorl,
left on the dorsum, is abnormally narrow and roof-shaped, this figure is not
original but deformed.
Short lateral lappets are present (Pl.

284

Tadashi SATO

34, fig. 4).
Primar y ribs of high relief are lon g,
widel y spaced, rectiradiate (slightly
prorsiradiate in smaller w horls), andtwo or more secondaries are bifurcatedat the lo wer one third of the whorlheight. The latter are finer and more
densely spaced, intercalated frequentl yby free ribs. Minu te but clearl y differentiated tubercles are superimposedon the branching points.
R emarlzs :-The possibility that thisspecies belon gs to the Stephanoceratidae
is exc luded because of the presence oflateral la ppets. Furthermore, lon g primary ribs and small secondary laterallobe which is observable in some specimens, are the characteristics favorab leto place them in Nonna-nnites, insteadof Oto ites. But there are some invo luteNonnannites superficially indistinguishable from Otoites, and the demarcation
between the two genera is riot always
easy, as ARKELL stated (1954, p. 568).
Among various Nonnannites species,
Canad ian Itin saites wo uld be comparable
directl y to this form by its sharp, hig h,and lon g primary ribs. Jti nsaites itinsae
kno wn from Queen Charlotte Island(MCL EARN, 1929, pl. XV, fig. 2- 3) and also
Cook Inlet of A laska (IMLAY, 1964, pl.
14, fig . 3- 8, 13) resembles this species ingeneral appearance.
T AKAHASHI segregated four independent but monotypical species wit hin his
Otoites, based mostl y on the different
ribbing styles.
However, even in asingle spec imen of the present collection,
ribbing is divergent from bifurcatin g tofasciculating. It seems that until better
specimens will be procured, all is betterreferred to one species.
The largest specimen, more than Ll em
in whor l thickness (Text-fig. 1), showsdense and fine ribbing. This specimen
is too much depressed to be determined

Text-fig . l. Ve ntro·lat e r a l v ie w of t heobli que ly deform ed who rl of Normannites(Itinsaites ) sp . Loc. I-!67 , Maeami. Collection T AKIZ AWA.

with confidence. But as the umbilica l
wa ll is partly observable, and reveals
the Nonnannites t ype umbilical aspect,
it is here tentatively retained in thepresent species.
Occurrence :- All the specimens a redisco vered from a seam of poorly sorted
silty sandstone, to get her with lamellibranch and be lemnite sh ell fragments,
in the state of foss il ba nk. Judging
from the litholo gy of the mother rock,
Stephano ceras sp., which will be described below is associated with thisspecies. H67 (T AKIZ AWA ), Maeami coast,
0 jika Peninsula.
Genus Stephanoceras WAAGEN, 1869
Stephanoceras sp.
Pl. 34, fig. 11.

594.

Bajocian arnmonites from Kitakami

1956. Stephanoceras sp. cf. S. piicatissimum(QuE:-:STEDT), SATo, p. 169, pl. 13, figs.
1-3, text-figs. 2-5.

J'vfaterial:-A single specimen procured
irom black sandy shale at Maeami. Collection CHIKARAISHI, his specimen number 730123.
Description:- The whorls are laterally deformed and the volution becomessomewhat elliptical; longer axis measures approximately about 90 mm, while
the shorter axis about 65 mm.
A part of the living chamber is preserved as an internal mould. but theinternal whorls are completely destroyed, but left impression, in somewhat obscure manner, as an outer cast. The
volution seems very evolute. The umbilicus is open and shallow and occupies:about 1/2 of the diameter. Whorl section
is rounded and as high as thick.
Ribbing is composed of stout primaryribs and dense, rectiradiate and generally trifurcate secondaries. The second.aries are branched off from the minute
but prominent tubercles at the inner one
tpird of the whorl height. Intercalatories are frequently inserted. Ribs arecontinuous on the venter without any
interruption or bending.
The suture line is not observable.
Remarks:- This planulate ammonite.is comparable to the species described.Previously from the Tsunakizaka shale.of the Karakuwa region as Step/wnoceras
sp. cf. plicatissimum (QUENSTEDT) ; thisKarakuwa form is characterized by rather well individualized long primary ribs.
This difference might be caused by more.advanced degree of deformation than in.the present specimens. In fact, the ribs
.appearing along the longer axis of thedeformation ellipse look like longer andsharper than those along the shorter.axis, as seen in the Karakuwa specimen

285(SA TO, 1956, pl. 13, fig. 1). In an accompanying specimen (Ditto, pl. 13, fig. 3)
shorter primaries are observable on thelast part of the preserved whorl.
No comparable species is yet known
among various stephanoceratids reported from New Guinea, Sula Island, orfrom West coast of North America
including South Alaska and British
Columbia, where the fauna of comparative age is widely developed.
Occurrence:- Maeami. collection CHIKARAISHI. judged from the lithology,
this fossil might be collected from thesame locality as T AKIZA w A's H67. Tsukinoura Formation after T AKIZA w A.

Genus Strigoceras QuENSTEDT, 1886

Strigoceras sp. cf. S. languidum(BUCKMAN)
Pl. 34, figs. 12, 13.
1969. Graphoceras sp., TAKAHASHI, pl. 19,
figs. 2, 3, 4 and ? 5.

lvf at erial:- Two outer casts of flatlycompressed and laterally deformed shells,collection l-IA Y AMI.
Description:-The maximum measurable diameter is 40 mm but 20 mm whenmeasured along the direction perpendicular to the former, thus the shell ismore or less deformed laterally. The
umbilical diameter is about 4 mm along
the longer axis of the deformation ellipseof the whorl.
Small shell with well differentiatedventral keel and involute coiling. Because of the flattening by tectonic deformation, the exact whorl section is notobservable, but it is most likely to be an
oxycone. The inner half of the flank isprobably concave. The umbilical margin
is sharply defined and the weak spiral

286

Tadashi SATO

ridge is formed at the middle height of
the flank.
The venter is not clearly observable
but it is likely to be fastigate.
The costation is characterized by thefalcoid ribs which are much more accentuated on the outer half of the flankthan on the inner half.
The suture line is not visible.
Remarks:- Various oxycone Strigoceratids are splitted into independent
genera by BUCKMAN. But these arecertainly not separable in generic leveland better put into the same genus
Strigoceras, as did ARKELL (1957). Strigites strigifer (BUCKMAN, 1924, Type Ammonites, pl. 469A) and ' Varistrigites'
compressus (BUCKMAN, pl. 468) are, among
others, closely related to the present
species, judged by their characteristic
ornamentation. But a form reported
from South Alaska by IMLAY under thename of Strigoceras cf. S. languidum(BUCKMAN) (IMLAY, 1964, pl. 23, fig. 4)
is the most resembling species known
in the circumpacific region.
This small oxycone is apparently comparable to Grap!wceras of Upper Toarcian-Aalenian age, especially to thegroup of G. concavum with rather rectiradiate ribbing. TAKAHASHI's ' Graphoceras' sp. B (1969, pl. 19, fig. 4) is judged
to be conspecific with the present species. Although Graphoceras is not easily
separable from this genus when it isimperfectly preserved, the latter should
be distinguished by its ribbing which is
not strongly rursiradiate in comparison
with that of the former and is rather irregularly branched, its complex sutureline, its very involute coiling. These
criteria are clearly visible in the present
specimens. Therefore, the materials now
in question are concerned with StJ-igoceras. TAKAHASHI's other two specimens(pl. 19, fig. 3 and fig. 5) are too fragmen-tary to be attributed to the present
species.
Occurrence:-West of Tsunakizaka.
Collection HAY AMI. Collected from thesame slab of black shale as Pelekodites(Spatulites) spatians.

Discussion on the occurrenceof ammonites
Tsunakizaka Formation:
1. Tsunakizaka
This locality is not a pinpoint locality,
but some ten different localities scattered around the site called Tsunakizaka
are designated under this name. All the
specimens procured there occur in theblack shale named Tsunakizaka Formation, which is overlain by argillaceous
sandstone and underlain by granulesandstone, both barren of ammonite.
A specimen of Pelekodites cf. pelekus(BUCKMAN) (figured formerly under thename of Sonninia sp. indet., SA TO, 1962,
pl. 9, fig. 2) was discovered from Loc.
5405302, together with Sonninia sp. (SATO,
1962a, pl. 9, fig. 3) and fragmentary Strigoceras-like shell (yet unfigured) and also
Stephanoceras sp. (unfigured). From another important locality, 5405232, Stephanoceras sp. cf. S. plicatissimum (QUENSTEDT) (SA TO, 1956, pl. 13, fig. 1) andalso Spatulites spatians BUCKMAN whichstill retains striated last whorl were collected (Collection AKIYAMA, Kesen-numaHigh School).
Stephanoceras cf. S. plicatissimum (Qu.}(SATO, 1956, pl. 13, fig. 3) was collected
at the locality 54044, which is correlated
to the top of the black shale formation,
but accompanies no other species. Otoites sp. described here was unfortunately collected from the river float, thus
bears no stratigraphical significance.
Pelekodites, Sonninia and Stephanoceras

594.

287

Bajocian ammonites from KitakamiINl

Text-fig. 2.

KS

Locality map around Tsunakizaka.

IN: Inai Group, KS: Kosaba Formation, TZ: Tsunakizaka Formation, TZs: Sandstone
overlying Tsunakizaka Formation, rW: Ishiwaritoge Formation.

are, therefore, completely coexistantstratigraphically. Discrimination of different fossil horizons is impossible inthis locality.
2. Yobaijitoge
This locality is situated about 1 km
north of the pass of the Higashi-hamaroad. The fossiliferous shale is exposed
along the trail crossing the mountain
range. Stephanoceras cf. S. plicatissimum(QUENSTEDT) (SA TO, 1956, pl. 13, fig. 2)
and Pelekodites cf. P. pelekus BuCKMAN(specimen 43IIR-5111) are discoveredfrom this locality but independently.
The stratigraphical relation between thetwo species is not clear.
The formation from which above
mentioned species were collected is about
350m thick and composed of monotonous
black shale. ONUKI (1969, p. 113) cited
three different fossil horizons within thisformation: this zonation was based on
unpublished data of TAKAHASHI, who
eventually discriminated two horizons(TAKAHASHI, 1969, p. 33), instead of three.

Tadashi SA TO

288

As discussed above, the Tsunakizaka
Formation can not be splitted into zones
from the faunal view point. Therefore,
TAKAHASHI's result appears to be based·On arbitrary splitting of the fauna into
two different lots. In fact, the Tsunaki.zaka Formation constitutes a single zone.

Tsuhnoura Formation:
1. Maeami.
This locality is the sea-side exposurenear Maeami, in the east coast of the
0 jika Peninsula. T AKIZA w A's locality
H67 yields both Stephanoceras cf. S. pli.catissimum (QuENSTEDT) and Normannites (Itinsaites) sp.
These fossils are discovered from a·seam of poorly sorted silty sandstone,
together with other lamellibranch andbelemnite shell fragments. Fossils are
more or less crushed and concentrated
in a thin seam as a shell bank. It isevident that the shells were transported
by current and brought into depositionalsite altogether.
It is safe to conclude that the species.composing the Maeami faunule are completely synchronous and indicate a single.age.

posed of black sandy shale. The lithology is quite homogeneous. There is noevidence of disordering of the bedding,such as slumping structure or turbidite.
Therefore the admixture of the fossilsof different ages is hardly admitted inthis sequence .
As discussed later in detaiL the ammonite species discovered from the Tsunakizaka Formation can coexist, as far
as judged from hitherto known rangesof every species. Therefore, the whole
Tsunakizaka Formation can be defined
as a zone .
A zone is a biostratigraphical term,so that the upper and lower limits should
be demarcated by lines on the exposure.
It· is not an abstract concept but objective. Since the ammonites are confinedin the black sandy shale sequence, andthe sequence cannot be subdivided into
smaller units, the formation represents
an ammonite zone as a matter of course.

Correlation
All the constituents of the faunules
now in question are of Bajocian age .
They are known widely around thePacific.

Note on the ammonite zone
In Japanese Jurassic, a solitary occurrence of a single individual of fossil.ammonites is not rare. The solitary.ammonite is important as a time-indi·Cator, but cannot define a zone. As I
previously noticed (SATO, 1962a, p. 40),.the term 'niveau' was used to denotethe stratigraphical horizon dated by thiskind of ammonite occurrence, instead ofusing 'zone' of OPPEL's sens. The veritable zones of ammonites exist in Japanese Jurassic; later I discriminated themfrom ill-defined 'niveaux' (SA TO, 1962b).
The Tsunakizaka Formation is com-

Tsunakizaka Formation:- The ammonite
faunule of this formation is composedof:Stephanoceras sp. cf. S. plicatissimum (QuENSTEDT)

Sonninia sp. cf. S. corrugata (J. de C. SowERBY)

Pelekodites (Spatulites) spatians (BucKMAN)
Pelekodites sp. cf. P. pelekus BucKMAN
Otoites sp.
Strigoceras sp. cf. S. languidum (B'ucK~·IAN)

Stephanoceras sp. was compared previously to S. p!icatissimum (QUENSTEDT),
but this is open to question. Because

594.

BaJ'ocian ammonites from Kitakami

the specimens are completely flattened
without exception, the identification iseven generically difficult. The specimens
are characterized apparently by shortand bullate primary ribs which are also
comparable to those of Pseudotoites.
Although the exact whorl section is notknown in the present specimens, thepossibility to belong to this particular
Pacific genus can not easily be rejected.
Pseudotoites cf. P. argentinus ARKELL(figured by WESTERMANN from Wide
Bay of Alaska Peninsula) resembles superficially this form. Even if this be a
Pseudotoites, the age which represents
the form is not be altered, because bothare of early-middle Bajocian age.
Stephanoceras (including Skirroceras
as subgenus) is a genus prolific in the
Pacific Middle Bajocian. It is so far
reported from Southern Alaska and New
Guinea, but the Stephanoceras s. s. isrelatively rare. Indisputable Stephanoceras s. s. is known only from West Irian(S. aff. S. humphriesianum (QUENSTEDT)),
British Columbia and Chile (for example
S. coamanoi McLEARN). Numerous S!?irroceras from South Alaska and Oregon
are partly transferred to Docidoceras(WESTERMANN, 1970, p. 294), of Lower
Bajocian age.
The sonninids reported from Kitakami
were compared to Sonninia corrugata
group, but these might belong to thesubgenus Euhoploceras. Associated Pelekodites is up ·to now confined to occur
in the Northeastern Pacific. This microconchiate ammonite is difficult to be determined unless the aperture is preserved. Some sonninids ever describedand of small shell diameter would be ofthis genus. For example, 'Sonninia subdeltafalcata' TORNQUIST (Pl. 5, fig. 7) and' S.' bodenbenderi of the same author(pl. 5, fig. 9) from Espinazito Pass ofArgentina might be Pelelwdites. Thus289

the distribution of the genus would be
far more wide-spread than supposed atpresent. Pelekodites is yet unknown
from the western and southwestern Pacific, and now its presence in Japanlinks paleobiogeographically the northwestern and northeastern parts of the
Pacific.
Other sonninids reported from Kitakami offer another link between Japanese and Southwestern Pacific paleobiogeographic provinces. Stephanoceratids
and a dubious Otoites sp. figured herein.
corroborate this connection.
Strigoceras is known from South Alaska (IMLAY, 1964) and doubtful one from
Supplee area of Oregon (LUPHER, 1941).
As a whole, the Tsunakizaka faunule
has a close affinity with those of South
Alaska and Western Canada, including
Western Interior of the United States,.
suggested by the common occurrence ofStephanoceras (though somewhat doubtful), Pelekodites, Strigoceras and probable
Sonninia. Especially Pelekodites is comparable between two regions even in
specific level.
Chronologically important is the Otoites, which attained the climax of prosperity in Otoites sauzei zone, although
it appeared already in the upper part ofSonninia sowerbyi zone. Unfortunately
the specimen of Otoites sp. was discovered in the river float, but it should bederived from the surrounding Tsunakizaka black shale, as suggested by its
lithology.
Among associated genera of the Tsunakizaka faunule, Stephanoceras is also
an indicator of the Otoites sauzei and Stephanoceras humphriesianum zones, notthat for Sonninia sowerbyi zone. The
presence of Sonninia sp., Pelekodites spp.,
Strigoceras sp. in association with Otoites
and Stephanoceras cannot reject the 0.

290

Tadashi SATO

sauzei zone age, because these range inwhole early and middle Bajocian.
The Tsunakizaka Formation is, therefore, of the Otoites sauzei zone age. I
previously correlated it with the Steph(Jnoceras humphriesianum zone (SATO,
1962b, p. 894), but the new collection of:ammonite does not permit to retain this.correlation.
T AKAHASI-II's Kl horizon (which wascorrelated with Upper Toarcian-Aalenian) cannot be sustained, because his
basis of correlation was on misidentified
Aalenian genera. In fact, his ' Grammoceras' sp. from Yobaijitoge might be
Asthenoceras, and ' Phymatoceras' sp.
might be Sonninia (Euhoploceras).
The chronological relation with the
Hosoura Formation which is of Upper
Toarcian-Aalenian age and is correlatedwith the Tsunakizaka Formation Kl by
TAKAHASHI, remains unsolved from thestratigraphical point of view, because
the distribution of the two formation iscompletely separated.
Tsukinoura Formation:
The collection from Maeami is important for correlation of the formation.
This faunule is composed of:Stephanoceras sp. cf. S. plicatissimum (QUENSTEDT)Normannites (Itinsaites) sp.

These are strong indicators for Stephanoceras humphriesianum zone. Normannites
is a wide spread genus, known fromSouth Alaska, Western Canada, probably
from Andes, Indonesia and Western Australia, and is known mainly from Stephanoceras humphriesianum zone. It
ranges, however, into the Otoites sauzei
zone, as exemplified by the occurrencein South Alaska. The Japanese species
resembles Itinsaites reported from the
Queen Charlotte Island, which is distri-buted in both sauzei and humphriesianum
zones.
Numerous Normannites (sometimes reported as Otoites) are found in Indonesia
and New Guinea. However, the true
Normmmites is rather rare. Normannites
etheridgei is an example, and was later
redefined as Stemmatoceras by WESTERMANN.

The combination of Stephanoceras andNormannites is known both in Otoites
sauzei and Stephanoceras humphriesianum
zones. Therefore, the Tsukinoura Formation is Middle Bajocian age, at least
its fossiliferous part.
Conclusion

In Karakuwa district of southern partof Kitakami plateau, the Jurassic sequence commences with the Kosaba
sandstone which is succeeded by the
Tsunakizaka Formation of 0. sauzei zone
age. The Kosaba sandstone is fossiliferous but barren of ammonites. Its age
is naturally before that age, but its
position in the zonal scheme remains
uncertain.
In Ojika Peninsula of the same plateau,
the Tsukinoura Formation is the basal
member of the Jurassic and is of the
Middle Bajocian age.
The underlying beds in both districts
are Triassic; thus the sedimentation did
not occur during the period coveringfrom Rhaetian to Aalenian, if the Kosaba
sandstone remains within the Bajocian.
From the structural viewpoint, both
districts are aligned on the same synclinorium axis, which runs approximately in N-S. The sequences in bothregions are not completely identical, but
it is very much likely that the Jurassic
sequence commenced with the beds ofsimilar age.

594.

Bajocian ammonites from Kitakami

References
ARKELL, W.J. (1953) : Bajocian ammonites
collected by Sir Henry HAYDEN near Kampadzong, Tibet. Geol. Mag., vol. 90, no.
5, pp. 331-336, 2 pis.
- - and PLAYFORD, P.E. (1954): The Bajocian ammonites of Western Australia.
Phil. Trans. Roy. Soc. London, Ser. B,
no. 651, vol. 237, pp. 547-605.
- - (1956) : Jurassic geology of the world.
806p., Oliver & Boyd, Edinburgh.
BoEHM, G. (1912) : Unteres Callovien undCoronatenschichten zwischen MacC!uer
Golf und Geelvink Bai. Nova Guinea,
vol. vi, Geol. abs. 1, pp. 1-20, pis. 1-5.
- - (1904-1912) : Die Siidkiisten der Sula
Inseln Taliabu und Mangoli. 1-4 Abs.,
Beitr. Geol. Niederland. Ind., Pal. Suppl.,
IV.
BucK:.-IA:>~, S.S. (1909-1930) : Yorkshire Type
Ammonites. Vols. 1-7, pis. 1-790.
FREBOLD, H. (1957) : The Jurassic FernieGroup in the Canadian Rocky mountains
and foothills. Geol. Surv. Canada, Mem.
287, 103pp., 44 pis.
- - (1969) : Toarcian and Bajocian rocks
and guide Ammonites from Southwestern
British Columbia. Geol. Surv. Canada,
Paper 67-10, pp. 1-47, pis. 1-6.
HAY AMI, I. (1961) : Successions of the Kitakami Jurassic. japan. jour. Geol. Geogr.,
vol. 32, no. 2, pp. 159-177.
IMLAY, R.W. (1964): Middle Bajocian Ammonites from the Cook Inlet Region, Alaska. Geol. Surv. Prof. Pap. 418-B, 61pp.,
29 pis.
JAWORSKI, E., KRANTZ, F. & GERTH, H.
(1926) : Beitrage zur Palaeontologie undStratigraphie des Lias, Dogger, und derUnterkreide in den Kordilleren im Siiden
der Provinz Mendoza (Argentinien). Geol.
Rund., 17a, pp. 373-427.
KRUIZINGA, P. (1926) : Ammonieten en eenige
andere Fossielen uit de Jurassische Afzettingen der Soela Eilanden. jaarb. Mijnw.
Nederl. Indie, Verh., 1 Ged., pp. 13-85,
pis. 1-14.
LUPHER, R.L. (1941) : Jurassic stratigraphy291

of Central Oregon. Bull. Geol. Soc. Amer.,vol. 52, no. 2, pp. 219-269.
McLEARN, F.H. (1929) : Contribution to thestratigraphy and palaeontology of Skidegate Inlet, Queen Charlotte Islands, B.C.
Nat. Mus. Canada, Bull., no. 54, pp. 1-27,
pis. 1-16.
0NUKI, Y. (1.969) : Geology of the Kitakami
massif, Northeast Japan. Tohoku Univ.
lnst. Geol. Paleont., Contribution no. 69,
pp. 1-239, pis. 1-4.
SATO, T. (1956) : Revision chronologique de
Ia Serie de Karakuwa (J urassique moyen).
japan. jour. Geol. Geogr., vol. 27, nos.
2-4, pp. 167-171, pl. 13.
- - (1962a) : Etudes biostratigraphiques desammonites du Jurassique du Japon. Mem.
Soc. geol. France, N.S., tome 41, fasc. 1,
pp. 1-122, pis. 1-10.
- - (1962b) : Le Jurassique du Japon-Zoned'Ammonites. Colloque du Juras. Lexembourg 1962, Comp. Rend. et Mem., pp. 885896.
TAKAHASHI, H. (1969) : Stratigraphy and ammonite fauna of the Jurassic System of
the Southern Kitakami massif, Northeast
Honshu, Japan. Sci. Rept. Tohoku Univ.,
2nd Ser., vol. 41, no. 1, pp. 1-93, pis. 1-19.
ToRNQt:IsT. A. (1898) : Der Dogger am Espinazito-Pass, nebst einer Zusammenstellung der jetztigen Kenntnisse von derargentinischen Juraformation. Pal. Abh.,
N.F., Bd. 4, Heft 2, pp. 135-204, pis. 14-23.
WESTERMANN, G.E.G. (1954) : Monographie
der Otoitidae (Ammonoidea). Beih. Geol.
jahrb., Heft 15, 364p., 33 pis.
- - (1969) : The ammonite fauna of the Kialagvik Formation at Wide Bay, Alaska
Peninsula. Part II. Sonninia sowerbyi Zone
(Bajocian). Bull. Amer. Paleont., vol. 57,
no. 255, 171 p., 47 pis.
& GETTY, T.A. (1970): New Middle
Jurassic Ammonitina from New Guinea.
Ibid., vol. 57, no. 256, pp. 231-301, pis.
48-62.
- - (1967) : Sucesion de Ammonites del Jurasico medio en Antofagasta, Atacama,
Mendoza y Neuquen. Rev. Assoc. Geol.
Argent., tomo xxii, no. 1, pp. 65-73.

Tadashi SA TO

292
Higashihama
Kitakami
KosabaMaeami

*
~t

1]\
j'Jtj

~~

J.:

•

m

Ojika
Tsukinoura
Tsunakizaka
Yobaijitoge

Jt[

!tl:
fl

I

rm

~Lt- :!1i~ill~~lt

Explanation of Plate 34
Fig. la, b. Pelekodites (Spatulites) spatians BucKMAN
la. Outer cast preserving lateral lappet. lb. Inner mould, partly preserved suture lines.
Tsunakizaka. Collection HAY AMI.
Fig. 2a, b. Pelekodites sp. cf. P. pelekus BucKJviA:-<
2a. Partly preserved last whorl, inner mould. Lateral lappet preserved. 2b. Outer castof the whole whorls. Lateral lappet is preserYed. Loc. 43IIR-5111, west of Y obaijitoge,
Collection YAM AS l-IlT A.
Figs. 3-9. Normannites (Itinsaites) sp.
3. Inner mould of obliquely deformed last ? whorl. 4. Inner mould of the last part ofthe living whorl, preserving the wide and short lateral lappet. 5a, b. Inner mould of
inner three volutions. a. Lateral view, b. Ventral view. 6a, b. Inner mould of the middle
stage of whorls. 7a, b. Inner mould of an obliquely deformed part of non septated whorl.
8a, b. Inner mould of slightly depressed beginning part of last whorl. x 1.5. 9. Inner
mould of the whorl showing transition from bifurcating to trifurcating ribbings. All
from H67, Maeami Coast. Co-llection TAKJZAWA.
Fig. 10. Otoites sp.
Gypsum model of the outer cast of a part of laterally deformed whorl. Loc. 54044, Tsunakizaka. Collection AKIY AliTA.
Fig. 11. Stephanoceras sp. cf. S. plicatissimum (QUENSTEDT)Inner mould of the last non septate whorl. Loc. H67, Maeami coast. Collection CHJKARAISHI.
Figs. 12, 13. Strigoceras sp. cf. S. languidum (BucKMAN)
Outer casts, from the same slab as Pelekodites (Spatulites) spatians BucKMAN. Tsunakizaka. Collection HAY AMI.

!!.:- SATO :BaJ·ocian ammonites from Kitakami!SHI BASH!

photo.

Plate 34

293

PROCEEDINGS OF THE PALAEONTOLOGICAL SOCIETY
OF JAPAN

JJ :;f>:Ci1:fm~S< 1972 1:f'.*.t.S< · 1:f'-4'<fd:, 19721f:-1
Jl 22 R (±) · 23 I] ( 1J) 0) 2 13 Fs9 =f*:kq~fz:J!fl'fB~S;t,j}C. L-'L~~{Jli~;!1,t-:: (f$::1JW.j!:f 110 ::f5)o... ~!!; P:/-!clm-t05l'~31illffi!r~S<nfli .. ,(!ir,lf, il!f"'t Y ::r':tfH::.w~T 0 1:!1llill00r~S<R& .. · .. · iJHil ~i±=:E*- .=:.:;:*!cl:m-t000rfi~S<RJJi .......\?;llJ~i.=:.
tM0 tMfr~'Eit'd::.B&1-t 05l'~ 51ill!'iill:ff~S<TI!ii · · · · · ·................................. ·ll'li:ft~=~ti1JJiill: 0) ~lof.ll~9i\J\'llt'Fiili1E1~}ijCJ-=f!f .... .=:.;t:n;'l~
New classifiable ferns from the JapaneseMesozoic .................... KIMURA, T.
~iliTimi¥ !::.ff:/1~ L- t-:: Liquidambar . ..... t~l'!l.3%'oi'[)v'V\9> 0~ttfl*tlfi~JJ!f!C"?v''L .... · ... · · ·. · ·........................ ~1'§3%'oi'[) . J"fJW:\!',.~

Evolutionary trend of the genus Fagus
around the Northern Pacific Basin .....
................................ TANAI, T.
tlt-=ftiki.¥l.JO)j['Qj}Jj(!::.--?v''L · · · ·· · · · · ·· · · .i;Uu9-!'l}
Calcareous nannoplankton flora of theyoungest Cenozoic of the Pacific Cen·
tral Region. . ............ TAKAYAMA, T.

'Ji 13 /j>:lffrm::::.it'dc .:t;!:J 0 i.¥il)]ii:fftL!1~5Hlf UY.:
itX!:h5J11fO)I*J11f~· ..... •io·I1J:Ci¥1kl!!~ · '1;\'ll'd.Jr::::.
Radiolarian fossils from the Nobori formation, Japan ........................... .
........ NAKASEKO, K. & NISHIMURA, A.
Neogene Actinommaridae (Radiolaria) inJapan ........................ SUGANO, K.
Permo-Carboniferous endothyraceans fromJapan, Part 1. Biseriamminidae. (f-1::1\ft)............................ OKIMURA, Y.
=r!! 00 Isla Madre de Dios jfftO)M~!.hfl:nfC"? v' 'L ........................... =f:\&j\;;0.e..:.,v-illi Minetrigoniinae !::."?v''L .... l)lj!33JI9ll![lJ:: fill rJX: Ill Jf5 illi 0)~71 r ::r"7J 1 [Sarmacina

dysteri (HUXLEY)] !C"?v'L ..... ·tffi!337}1:
A coprophagous gastropod from -the Carboniferous of Chugoku District, Japan.
............ NISHIDA, T. & NISHIKAWA, !.
Triassic pectinids from Malaya. . ... ,· ....
............................. TAMURA, M .
Discontinuous variation of an evolutionary
species, Cryptopecten vesiculosus, fromJapan ........................ HAY AMI, !.
Upper Triassic cephalopods from Tanoura
formation, Kumamoto Prefecture, Japan .
. . . . . . . . . . . . . . . . . . . . . . . . . . . . IsHIBASHI, T.
A peculiar desmoceratid ammonite from
Hokkaido. . ......................... ; ..
...... MATSU:VIOTO, T. & MuRAMOTO, T.
A small puzosiine ammonite from Hokkaido ........ MATSUMOTO, T. & lNOMA, T.
-'E- Y .?l :T1+1J:ftB 7J Y 7'!! 7*0) Cedaria 11f111t.=:.
*!:II 3ffiO)fffili*9E1: CftR)C) ........ ;IV3 :~:1!!

wr=u~:km'i O).=:.:ilHcitE!"B!l~tH ........ rr:.nuJ~t'i!iOphiuroid and associated molluscan faunafrom the Ichijiku formation, Boso Peninsula ............ OHARA, S. & SUZCKI, K ..
~Y;J<:/'/'.b. ~~\kf*!WJ!fl!]fl:n!U: 0 IJ:;f>:Wfr1: f-1:: O)±J'. ttlflfi/:"f: J:.ltlillWr::W::.:::*O) .&ftn C. EtHic J: 0~Ff-rK5-1 ..
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00!!/I, ;Ht!liU&:II.Bl~~. Reiner JoRDAN, Tuncer GUVENC.
1971 if.~l=j:l fCJ1!1'*:~ ;h,t-:~~ 315, Ralph W. CHANEY, )~ii#.ilJRi]l, ;A_f:E0.5o
1972 if-1 fl 21 1:3 O)~ij11~~~fci>v•'"(, )Jz0)~1['J50))f;~iJ;,1!J<D Gfl,f-:o Anders B. BoHLIN, Raymond
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8 4 7 8 0 'ff)±Transactions and Proceedings of the PalaeontologicalSociety of japan

April 20, 1972

New Series No. 85

CONTENTS
TRANSACTIONS
591. Hu, Chung-Hung: Ontogeny of three Cedaria zone trilobites from Upper
Cambrian, Montana ......................... . ............... . ........ 245
592. YAMAGIWA, Nobuo and SAKA, Yukiyasu : On the Lepidolina zone discovered from the Shima Peninsula, Southwest Japan . .... . . .. ..... . . . ... 260
593. SAKAGAMI, Sumio: The Triassic Bryozoa from Kusaka, Sakawa basin,
Shikoku, Japan .. . . . ........... . ....... . . . ... . ....................... 275
594. SATO, Tadashi: Some Bajocian ammonites from Kitakami, Northeast
Japan .. . ... . .... . . . .. . . . . . . .. . . . . .... . . . ........... . .. . .... . .. . .. . . . . 280
PROCEEDINGS

293