ISSN 0031-0204

a ~'1;-f.~~~.~·!~tTransactions and Proceedingsof the\,"Palaeontological Society of Japan
New SeriesNo. 114

Palaeontological Society of Japan
July 15, 1979

Co-Editors
Associate edito1'

Itaru HAYAMI and Tsunemasa SAITO
Tomowo Ozawa

Officers for 1979-1980

Honorary President:
President:

Teiichi KOB AY ASH!

Tetsuro HANAI

Councillors:

Kazuo ASAMA, Kiyotaka CHINZEI, Takashi HAMADA, Tetsuro HANAI,Haru HAYAMI, Hisayoshi IGO, Kametoshi KANMERA, Tamio KOTAKA, Tatsuro MATSUMOTO, Ikuwo OBATA, Tsunemasa SAITO, Tsugio SHUTO, Yokichi
TAKAYANAGI, Toshimasa TANAI, Ryuzo TORIYAMA
Members of Standing Committee:

Kazuo ASAMA (Finance), Kiyotaka CHINZEI(General Affairs), Takashi HAMADA (Planning), Itaru HAY AMI (Transactions),
Hisayoshi IGO (Foreign Affairs), Ikuwo OBATA (Membership), Tsunemasa
SAITO (Transactions), Tsugio SHUTO (Special Papers), Yokichi TAKA YANAGI("Fossils")
Secretaries:

Hiromichi HIRANO and Yasumitsu KANIE (Me mbership), Kunihiro ISHI-ZAKI ("Fossils"), Tomowo OZAWA (Transactions), Toshiyuki YAMAGUCHI(General Affairs), Juichi YANAGIDA and Ienori FUJIYAMA (Special Papers)
Auditor:

Sumio SAKAGAMI

The fossil on the cover is Nipponiteila explicata HANZA WA, an aberran t
uncoiled fusulinacean from the Lower Permian Sakamotozawa Formation,southern Kitakami, Northeast Japan.

All communications relating to this Journal should be addressed to the
PALAEONTOLOGICAL SOCIETY OF JAPAN,
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University of Tokyo Press, Hongo 7-3-1, Tokyo, Japan.

Trans. Pruc. Palaeont. Soc. japan, N. S., No. 114, pp. 49-63, pis. 8, 9, july 15, 1979

701.

ONTOGENIC STUDIES OF A FEW UPPER CAMBRIAN
TRILOBITES FROM THE DEADWOOD FORMATION,
SOUTH DAKOTACHUNG-HUNG HU
Department of Physics, Taiwan Normal University, Taiwan

Abstract. The purpose of the present study is to illustrate the ontogenetic
development of Elvinia roemeri (SHUMARD), Cliffia typica, n. sp., Irvingella major
ULRICH and RESSER, and Cameraspis convexa (WHITFIELD). All of the studiedmaterials were collected from the Deadwood Formation, Elvinia Zone, Upper Cam·brian, located in the Black Hills, South Dakota. The result of this study indicatesthat the phylogenetic development of Elvinia roemeri and Irvingella major is closely
related, that the morphogenesis of Cliffia typica is similar to those of Ponumia
obscura and Housia canadensis, and that Ccmeraspis convexa is possibly an immediate derivative of the genus Dunderbergia.

and Aphelotoxon sp. (unpublished materials) are comparable and bespeak possible
common descent from a common ancestral stock. Since the late meraspis of
Cameraspis coiwexa (WHITFIELD) is morphologically very similar to that of thegenus Dunderbergia, it is presumably
an immediate derivative of that trilobite.
The present materials were collectedfrom the Deadwood Formation, Elvinia
Zone, Upper Cambrian, located aroundthe Black Hills, South Dakota while attending a summer camp in 1962. Thissummer camp was directed by Dr.
Christian LOCI-IMAN-BALK, known Cambrian specialist of the New Mexico Institute of Mining and Technology. The
author considers that it was a rare opportunity to participate in this field work,and now to have the present collections
for study.
The author wishes to express his
thanks to Dr. Christina LOCHMAN-BALK,
for her guidance and the permission to

Introduction
The ontogenic stages of Elvinia roemeri(SCHMARD), Cliffia typica, n. sp., Irvingellamajor ULRICH and RESSER, and Cameraspis
convexa (WHITFIELD) are here described.
The ontogenic sequences of the first two
species are completely recovered; thesecond pair are incompletely known.
The development is divided into fivemorphologic stages: anaprotaspid, metaprotaspid, paraprotaspid, early meraspid,
and late meraspid, as proposed by theauthor in his earlier trilobite ontogenic
studies (Hu, 1970, 1971, etc.). The morphogenesis of Elvinia roemeri and Irvingella major are closely similar. They
apparently developed from the same ancestor. The early ontogenies of Cliffia
tyPica, n. sp., Ponumia obscura (LOCHMAN),
Housia canadensis WALCOTT (Hu, 1970)* Received Aug. 29, 1978; read june 9, 1979,
at Tatsunokuchi.
49

Chung-Hung Hu

50

study a part of her collections; andthose especially relating to the present
studies. Thanks also go to Dr. K. E.
CASTER, University of Cincinnati, forreading the present manuscript. The
figured specimens are all deposited in
the Geology Museum, University ofCincinnati, Ohio (UCGM).
Systematic Paleontology

Family Elviniidae KOBAYASHI, 1935
Genus Elvinia WALCOTT, 1924
Elvinia roemeri (SHUMARD)a transverse oval pygidium unlike thatof Elvinia. But since the specimen wasrecovered from the same shale bed bearing
Elvinia roemeri as seen on pI. 8, figs. 22, 25,
28, and show only minimal differences,
the author would at least temporarily
assign them to the same species. The
similarities in this instance between
Elvinia and Parabolinoides are possibly
due to compaction and deformation of the
shale matrix.
Occurrences.-Galina, Brownsville junction, Little Elk creek, Boxelder, Nemo,and Dark canyon, along the east side of
the Black Hills, between Deadwood and
Rapid city, South Dakota.

PI. 8, figs. 1-28 and Text.fig. 1
Dikelocephalus roemeri SHUMARD, 1861, p. 220,22l.
Elvinia roemeri (SHUMARD) : WALCOTT, 1924,
p. 56; PALMER, 1965, pI. 3, figs. 9, 11, 14,
16, p. 44. (synonymy up to date.)

Remarks.-The present species is acommon member in the Elvinia Zone,
Upper Cambrian. The materials herestudied were collected from several localities in the general region of theBlack Hills, South Dakota. They are allidentical. The ontogenic sequences arecomparable with those reported by
LOCHMAN and Hu (1960), from materials
collected in the Wind River Mountains,
Wyoming. However, the Wyoming se·quences are incomplete.
A complete trilobite specimen (pI. 8,
fig. 21) was collected from Brownsvill
junction, about 2 miles south of Deadwood city. It is a greenish gray, thinly
bedded shale. The specimen is about
8mm long and has 10 thoracic segments,
a slightly deformed cephalic shield, anda complete pygidium. Dr. J. L. WILSON
of Rice University has suggested that it
is possibly a parabolinoid trilobite, since
the cephalon has a broad glabella, andElvinia roemeri (SHUMARD), ontogeny
Metaprotaspid stage (PI. 8, figs. 1-8 andtext-fig. lA, B).-The shield is about
0.25-0.35 mm in sagittal length, moderately convex, well defined into axial andpleural lobes by dorsal furrows; the axial
lobe is expanded forward, and subdivided
into five axial segments by faint furrows; the first axial segment is the frontal lobe, which is large, rounded nodose,convex, well delimited by a pair of small
but distinct pits at the sides, and a pairof superciloid ridges is expanded laterally
from the anterolateral margin; the second to third axial segments are twopairs of well defined lobes; the fourthaxial segment is rather faint, and thefifth is the smallest and round; thepleural lobe is less broad than the axis,
convex; a pair of palpebral ridges extends from the lateral margin of thefrontal lobe behind the frontal pits, andruns posterolaterally to end at the midtransverse line of the shield; a narrow
border is faintly defined by a marginal
furrow, and shows a short fringe along
the posterior shield margin. The skeleta I
surface is faintly granulated.

701.

A

Ontogenies of Cambrian Trilobites

c

B

G

51

D

F

E

H

K
Text-fig_ 1. Elvinia roemeri (SHUMARD)
A, B, two metaprotaspides, showing the formation of the forth axial ring andthe presence of the rudimentary protopygidium, x 44; C, E, paraprotaspides, showing the morphogenesis of the protopygidium, x 48, x 29; D, an early meraspid
cranidium, showing the presence of the anterior border, x 20; F, G, two latemeraspid cranidia; note the increase of the preglabellar field, x 8, x 6; H, anearly holaspid cranidium, x 3_5; J, an holaspid cranidium associates with left side
librigena, x 2; I, K, a small and a large pygidium, x 3. (All drawings were madefrom photographs.)

The main morphogenesis of the instars
during the present stage is: the earliest
ins tar has the axis composed of a large
frontal lobe, two pairs of medium sizedcentral bodies, an incompletely developed
fourth axial ring, and a terminal portion-the occipital ring; during the lateperiod the two pairs of central lobes

are fused, and the fourth axial ring iswell elevated, and therefore the axial
lobe contains five well-developed axial
segments; the posterior shield margin isgently and bent inwardly and shows no
pygidial segment.
Paraprotaspid stage (PI. 8, figs. 9-11 andtext-fig. Ie, E).-The shield is round to52

Chung-Hung Huoval in outline, moderately convex, andis about 0.35-0.45 mm in length (sag.);
the axial lobe is distinctly demarked bydorsal furrows, expands forwardly fromthe occipital ring or is slender and fusiform with a rounded anterior first axial
segment; the second to fourth segments
are transverse oval and convex; theterminal segment is the occipital ringwhich is the smallest segment; thepaired anterior pits are distinctly demarked at the sides of the frontal lobe,
and continue with a pair of lateral furrows that separate the anterior brim into
a pair of superciloid ridges from thepleural lobe; the pleural lobe is about
the same width as the axis or slightly
wider and convex along the anterior
margin; the narrow palpebral ridge islocated in front of the midline of theshield (tr.), and curves anterolaterally;
the posterior lateral lobe of 1 he fixigena
is 'surrounded by a narrow marginalborder and a pair of short-based postfixigenal spines; there is a small transverse protopygidium at the posteriorshield margin, and shows one or two
well-marked segments. The instar surface is covered by medium-sized granules.
During the present stage, the shield isdifferentiated into a cranidium and a
protopygidium and the narrow anteriorborder appears; the pygidial segments
increase in number; the facial suture isturned on to the dorsal surface; theposterior fixigena broadens in width witha pair of short posteriorly directed fixigenal spines. The skeletal granules
become coarser than in the earlier form.
This stage correlates with "series ofmeraspids" by LOCHMAN and Hu (1960)(pI. 96, figs. 43, 44 only).
Early meraspid stage (PI. 8, figs. 12-16
and text-fig. ID). -The cranidium is trapezoidal in outline, convex, and about
0.70-0.90 mm in length (sag.) ; the glabella

is slenderly cylindrical, tapering forward,
and has four well-defined glabellar segments; the first glabellar segment islarge and quadrate, and the second to
fourth ones are transverse oval; theoccipital ring is roundly subtriangular,
convex, arches posteriorly, and bears aminute median-node; the dorsal furrowis distinctly demarked; the convex anterior border arches forward, and is welldelimited by a frontal furrow; the broad
triangular fixigena is convex, and has
the narrow elevated palpebral lobe located at the second glabellar segment(tr.); the short anterior facial suture isconvergently convex, and the posterior
one is laterally divergent, and is. straightto barely convex; the posterior fixigenal
border is deeply defined by a borderfurrow and is about the same width as
the occipital ring. It is (tr.) convex, anddirected slightly posteriorly at its extreme end. The skeletal surface iscovered by medium-sized granules, andsparsely by coarse ones.
The morphogenesis of the instars during the present stage is: the anteriorborder increases in width; the glabella
becomes slenderly cylindrical; the facial
sutures are diagonally cutting the cranidial margin to form a regular trapezoid;
the palpebral lobe moves posteriorly
from the nearly anterior border to thesecond glabellar segment (tr.), and iswell defined by the palpebral furrow.
This stage agrees with LOCHMAN and
Hu's (1960) "series meraspids" (pI. 96,
figs. 39, 42 only).
Late meraspid stage (PI. 8, figs. 17, 18
and text-fig. IF. G).-The cranidium istrapezoidal in outline, convex, about 1.0
to 1.5 mm in sagittal length; the glabella
is truncatoconical, tapers slightly anteriorly, and is divided into four glabellar
segments; the anterior two glabellar
segments are defined by shallow and701.

Ontogenies of Cambrian Trilobites

faint glabellar furrows; the third to
fourth glabellar segments are deeply
delimited by furrows which are concave
posteriorly, distinct, and transversely Ushaped; the occipital ring is convex,
medium-sized, distinctly defined by theoccipital furrow and bears a minutemedian tubercle; the dorsal furrow deepens posteriorly and shallows acrossthe anterior glabellar margin.
The narrow preglabellar field is present in front of the glabella. It slopes
downward from the anterior glabellar
margin and is well delimited by thefrontal furrow; the narrow sickle-shaped
anterior border is convex, and arches
forward; the fixigena is slightly narrower
than the glabella (tr.), convex, has themedium-sized palpebral lobe located on
the second glabellar furrow (tr.). It isnarrowly elevated and distinctly definedby the palpebral furrow; the elevatedposterior fixigenal border is about thesame width as the occipital ring. The
anterior facial suture is slightly convergent-convex, and the posterior one isdivergent-posteroiaterlaly and convex.
During the present stage, the glabellar
furrows are complete; the glabella increases its width; the preglabellar field
widens; the fixigena becomes narrower;
the granules reduce in size. This stage
correlates well with LaCHMAN and Hu's
(1960) "early holaspid cranidium" (pI. 96,
figs. 40, 41 only).
Figured specimens. - Metaprotaspides,
UCGM. 43372a-g.
Paraprotaspides, UCGM. 43372h-j.
Early meraspid cranidia, UCGM. 43372ko.
Late meraspid cranidia, UCGM. 43372p,
q.
Holaspid cranidia, UCGM. 43372r-w.
Librigenae, UCGM. 43372x, y.
Pygidia, UCGM. 43372z, a /.

53

Family Komaspiidae KOBA Y ASH!, 1935
Genus Irvingella ULRICH and RESSER, 1924

Irvingella major ULRICH and RESSER
PI. 8, figs. 29-36 and text-fig. 2

Irvingellamcjor ULRICH and RESSER, In
WALCOTT, 1924, p. 58, pI. 10, fig. 3;
PAUIER, 1965, p.48, pI. 6, fig. 5, GRANT,
1964, p. 16, pI. 10, figs. 8, 9, 11. (synonymy
up to date.)

Remarhs.- The synonymy of the present
species is given in detail by FREDERICKSON (1949), GAINES (1951), and PALMER(1965), and their opinions are accepted
here. The present species is represented
by a few skeletons, ranging from small
to large size, from a single small pieceof yellowish gray limestone. They arerecognized as belonging to the same species, but represent an incomplete growthseries.
Occurrences.-Moll section, near Bear
Butte, about 6 miles southeast of Deadwood, South Dakota.
Irvingella major ULRICH and RESSER,
ontogeny
lvletaprotaspid stage (PI. 8, fig. 28, andtext-fig. 2A).-The shield is rounded tosubrounded in outline, convex, and about
0.4 mm in sagittal length; the axis andthe pleuron are distinctly defined bydorsal furrows; the axis is extended in
the full length of the shield, cylindrical,
slightly expanded anteriorly from theoccipital ring, and divided into fiveglabellar segments by indistinct furrows;
the anterior first glabellar segment isround, and continues with a pair of superciloid ridges from the anterolateral
margin; it is well defined by a pair ofdistinct lateral pits; the second to fourth
glabeUar segments are transverse, faintlyChung-Hung Hu

54

o
A

c

B

E

G

Text-fig_ 2. /rvingella major ULRICH and RESSER
A, a paraprotaspis, x 34; 8, metaprotaspis, x 33; C, an early meraspid cranidium, x 15; D, an immature pygidium, showing a few dis-ankylosed segments, x 20;
E, a late meraspid cranidium, showing a broad truncato-conical glabella, x 28 ;F, a mature cranidium associated with the left librigena, x 2; G, a pygidium, x 1.5.
(All drawings were made from photographs; figs. F, E, were redrawn from PALMER,
1965, pI. 6, figs. 10,11.)defined by a central longitudinal furrow,so as to separate these segments into
three pairs of round convex lobes; thedorsal, or occipital, ring is small, convex,
triangular; the pleural lobe is convex,
wider than the axis, and slopes downward
along the margin; a pair of faint palpebral ridges extend behind the anteriorpits, and anterolaterally to end at thefirst glabellar furrows (tr.); the posterior
margin of the shield has a pair of shortbroad spines which project from the narrow flat border; the skeletal surface iscovered by minute granules.
Paraprotaspid stage (PI. 8, fig. 30, andtext-fig. 2B).-The skeleton is elongate
to oval, separated into cranidial andprotopygidial shields by an archingfoward suture, and is about 0.60 mm intotal length (sag.); the cranidial shieldis roundly trapezoidal and well defined bya dorsal furrow; the glabella is cylindrical, faintly divided into four glabellar
segments; the occipital ring is transverse
oval, convex; no median tubercle is recognizable; the pleural lobe of the fixigena is slightly wider than the axis,
convex along the free margin; themedium-sized palpebral lobe is elevated,narrow, and situated in front of the
mid-length of the glabella; the posterior
fixigenal border is elevated, directed posterolaterally from the side of the occipitalring and ends in short, broad-based projection.
The protopygidium is semicircular andconsists of 2-3 dis-ankylosed segments;
the axis is convex, about the same width
as the pleuron, conical, and tapers posteriorly; the pleural furrow is deeper
than the interpleural groove, and curves
posterolaterally from the dorsal furrow;701. Ontogenies of Cambrian Trilobites
the margin is irregular, narrow and fiat.
Early meraspid stage (PI. 8, fig. 31, andtext-fig. 2C).-The cranidium is trapezoidal in outline, convex, about 1.0 mm
in sagittal length, with a deeply depressed
dorsal furrow; the glabella is cylindrical,
rounded anteriorly, convex, has two pairsof rather faint glabellar furrows and a
deeply demarked third glabellar segmental furrow; the occipital ring is lenticular,
convex both vertically and posteriorly;
it bears a minute median tubercle; thenarrow anterior border is elevated convex, faintly delimited by a frontal furrow, and has no median niche. The
fixigena is convex, slightly narrower
than the glabella between the palpebral
lobe and the dorsal furrows; the palpebral
ridge is narrow and long, sickle-shaped,
distinctly demarked by the palpebral
furrow and situated on the mid-lengthof the glabella (sag.); the anterior facial
suture is short, convergent, and the posterior one is divergent-posterolaterally;
the rear fixigenal border is distinctly
impressed by a furrow which is narrow,elevated, and about the same width asthat of the occipital ring (tr.). The surface of the cranidium is faintly granulated.
Late meraspid stage (PI. 8, fig. 35 andtext-fig. 2E).-The cranidium is nearly
subtrapezoidal in outline, convex and has
the dorsal furrow distinctly demarked;
it is about 2.0 mm in sagittal length; theglabella is truncato-conical, convex above
the fixigena and with the anterior twopairs of glabellar furrows indistinct; thethird glabellar furrow and the occipital
furrow are deeply demarked and transversely U-shaped; the medium-wide occipital ring is concave, lenticular (horizontal) and convex (vertical); the occipital tubercle is minute; the anteriorbrim is divided by a distinct frontal furrow into a narrow convex preglabellar

55

field, and a narrow anterior border; there
is no median notch on the anterior furrow. The fixigena is about two-thirds
the width of the glabella, convex, withthe maximal width on the transverse
mid-line of the cranidium; the palpebral
ridge is rather short, well elevated, andcontinues with a very long but narrowpalpebral lobe. Both the anterior andposterior facial sutures are very shortdue to the presence of the long ocularlobe.
The immature pygidium (PI. 8, figs. 3234 and text-fig. 2D).-No adult pygidial
skeleton was recovered except for a few
early instars. The smallest pygidium isabout 0.5 mm in sagittal length, semicircular in outline and consists of 5-6
dis-ankylosed freely articulated segments,and has the axis tapering posteriorly;
the pleural lobe is wider than the axis,
convex, and has the pleural band curving
posteriorly, and ending into a pair ofshort broad spines; the interpleural furrow is deep and broad. These pygidia
are judged as the meraspid form whencompared with the adult form (MOORE,
1959, p. 295).
Remarks.- The ontogenic developmentof the present species is closely similar
to that of Elvinia roemeri (SHUMARD);
both have similar protaspides and meraspides, which probably indicates thatthey belong to the same super-genericlevel and have close phylogenetic relationship. Certainly this evidence would
support common assignment to the
El viniidae.
Figured specimens. - Metaprotaspis,
UCGM.43375
Paraprotaspis, UCGM. 43375a.
Early meraspis, UCGM. 43375b.
Late meraspis, 43375f.
Immature, pygidia, UCGM. 43375c-e.
Cranidia, UCGM. 43375g.

Chung-Hung Hu

56

Family Pterocephaliidae KOBAYASHI, 1936
Genus Cameraspis ULRICH and RESSER, 1926
Cameraspis convexa (WHITFIELD)
PI. 9, figs. 30-36 and text·fig. 3
Cameraspis convexa (WHITFIELD): GRANT,
1965, p. 140, pI. 10, fig. 6. (synonymy up
to date.)Remarks.-The present species is represented by a few small and large size
cranidia and pygidia. The small cranidium is about 1.7 mm and the biggest is
8.3 mm in length (sag.). All show acontinuous morphologic sequence. The
smallest cranidium is assigned to thelate meraspis. It is characterized by asubquadrate shield, conical glabella, andwell impressed dorsal furrow. The dorsal
furrows become shallower during its lateAcgrowth stage (figs. 35-37). The surfaceof the skeleton is covered by coarse
granules in the small instars but these
become either much finer or absent
during later growth periods. These
instars are morphologically very similar
to the genus Dunderbergia, a geochronologically slightly earlier trilobite. It
seems likely that the genus Cameraspis isa direct descent of Dunderbergia.
A few early meraspid pygidia werealso recovered. They are all characterized by 5-6 segments, semicircular inoutline and convex; a few of the anterior
segments are non-ankylosed, and theposterior ones are fused as a terminal
plate (pI. 9, figs. 31-33); the axis isconical, tapering posteriorly, and welldivided by ring-furrows; the posterior
marginal border is narrow and flat andthe anterior ones are spinous; the spines

B

D

Text-fig. 3 Cameraspis convexa (WHITFIELD)
A, an immature cranidium x 3; B, an adult cranidium associated with the left
librigena, showing both of the internal and external skeletal surfaces, x 6; C, anearly immature pygidium articulated with two thoracic segments, x 20; D, anholaspid pygidium, x 3. (All drawings were made from photographs, except fig. C,
which was redrawn from LOCHMAM and Hu, 1960 and GRANT, 1965.)

701.

Ontogenies of Cambrian Trilobites

are the lateral projections of the freely
articulated anterior segments or thethoracic segments.
LOCHMAN and Hu (1960) reported a few
early instars supposedly pertaining tothis form from the Wind River Mountains,
Wyoming (pI. 96, figs. 10, 12, 17), whichshow a broader and shorter glabella, anda wider preglabellar field. This is possibly an erroneous interpretation.
Occurrence.-Rapid creek section, Dark
canyon, about 2 miles southwest of
Rapid City, South Dakota.
Figured specimens.-Cranidia, UCGM.
43376d-g.
Pygidia, UCGM. 43376a-c, 43376.
Family Solenopleuridae ANGELIN, 1854
Genus Cliffia WILSON, 1951

Cliffia typica, n. sp.
PI. 9, figs. 1-29 and text·fig. 4

Diagnosis.-Cranidium trapezoidal in
outline, moderately convex; glabella
short, broad, conical, and marked withthree pairs of glabellar furrows; occipitalring bearing a medium-sized occipitalspine; preglabellar field less than onehalf the length of glabella, convex, distinctly defined by frontal furrow; theanterior border narrow, crescentic, convex, arching forward; palpebral lobe
about one-third the width of glabella:palpebral lobe small, situated on the midline of glabella (tr.). Librigena crescentic,
elongate, convex; genal spine mediumsized. Pygidium rhomboid, containing
more than three segments.
Description.- The cranidium is trapezoidal in outline, moderately convex,
and has the distinctly defined V-shaped
dorsal furrow; the glabella is mediumwide, conical, convex, and marked bythree pairs of very distinct glabellar

57

furrows; the first pair of glabellar furrows is short and faint, and is locatedat about the same level as the palpebral
ridges, or slightly posteriorly; the second
and the third ones are deeper, shorter,and gently directed centroposteriorly;
the crescentic, or transverse lenticular,
occipital ring is convex, and bears a
broadly based, small, posteriorly directed
occipital spine; no mediam occipital node
is known; the preglabellar area is moderately convex, about one-third thelength of the glabella, and well definedby a frontal furrow; the anterior borderis narrowly crescentic, convex, and arches
forward; the concave frontal furrow has
no median embayment; the fixigena is
about one-half the width of the glabella,convex, has the medium-sized palpebral
lobe situated between the second andthird glabellar furrows (tr.) ; the palpebral
lobe is well defined by a furrow, elevated,and continues with the faintly elevatedpalpebral ridge directed obliquely to theanterolateral glabella; the posterior fixigena is medium-wide, convex, slopes
downward from the dorsal furrow, andthe convex border is about the same
width as the occipital ring or narrower.
The librigena is elongate, moderately
convex; the medium-wide ocular platform
is gently convex, and more than twice
as wide as the lateral border (sometimes
considerably broader); the medium-sizedocular ring is forwardly situated in the
inner free margin-the facial suture line;
the round, convex, lateral border ismedium-wide, well defined by a broad
lateral furrow; the lateral and posterior
librigenal furrows are not connected at
the genal angle; the genal region is flatand extends into a medium-sized genal
spine.
The pygidium is rhomboidal in outline
and convex along the axis; the axial
lobe is conical, tapering posteriorly, andChung-Hung Hu

58

deep pleural furrows are seen, and theinterpleural grooves are faint.
The skeletal surface is covered bymedium-to-coarse granules, and irregularradial ridges are developed both on the
preglabellar field and the platform.
Remarks.- The present species is re-does not extend the full length of thepygidium; it is divided by furrows into
three convex rings, and a small terminal
portion; the dorsal furrow is medium
deep; the pleural lobe slopes downward
from the dorsal furrow and is about thesame width as the axis; two to three

A

c

B

E

o

F

G

H

J

K

L

Text-fig. 4. Cliffia typica, n. sp.
A, anaprotaspis, x 52; B, metaprotaspis, x 52; C, D, two paraprotaspides,
showing the presence of the rudimentary pygidium, x24, x37; G, a paraprotaspid
cranidium, x32; F, an early meraspid cranidium, x28; E, H, two late meraspid
cranidia; notice the widening of the preglabellar field, x 25, x 26; I, a mature
cranidium associated with left librigena, x 8; j, K, L, a growth series of pygidia,
showing the disappearance of thoracic segments and the presence of the pygidial
plate, x 20. (All drawings were made from photographs.)

701.

Ontogenies of Cambrian Trilobites

presented by numerous early instars andmature skeletons which show a continuous growth sequence; the largest
cranidium is about 2.0 mm in length andthe small protaspis is 0.24 mm in length(sag.). This species differs from the typespecies Cliffia lataegenae (WILSON) by theshallower dorsal furrow, narrower preglabellar field and fixigena; the palpebral
lobe is of lower elevation, and thepygidium is broader.
Occurrence. - Boxelder section, near
Nemo, about 8 miles northwest of Rapid
City, South Dakota.

Cliffia typica, n. sp., ontogeny
Anaprotaspid stage (PI. 9, fig. 1 andtext-fig. 4A).-The shield is fiat or gently
convex, nearly dome-shaped, round to
subround, about 0.24 mm in sagittal
length; it is without distinct dorsal furrows, except for a rather faint depression along the axial region, which suggests the position of the axial lobe; theaxis is slender fusiform, tapering bothanterior and posterior from the midlength of the axis; no distinct frontal
pits or superciloid ridges are known;
the skeletal surface is smooth or faintly
granulated.
Metaprotaspid stage (PI. 9, figs. 2, 3 andtext-fig. 4B).-The shield is oval, moderately convex, about 0.25-0.35 mm inlength (sag.); the slender fusiform axis
is faintly delimited by a dorsal furrow;it tapers slightly both anteriorly andposteriorly from the mid-line of the axis(tr.) ; no distinct axial segments of frontal
pits are recognizable; the posterior
margin of the shield bears a small transverse median lens-shaped area, whichsuggests the possible position of theoccipital ring. The skeletal surface iscovered by minute granules.
Paraprotaspid stage (PI. 9, figs. 4-12

59

and text-fig. 4C, D, G).-The shield may
or may not bear a protopygidium; It IS
subround to trapezoidal in outline, convex; the complete paraprotaspid shield
is about 0.35 mm in length from theanterior cephalic to the posterior protopygidal margins; the largest cranidium
may sometimes measure as much as 0.50
mm in length (sag.); the axis or theglabella is slenderly conical, tapering
anteriorly without a distinct segmental
furrow, except that certain specimen
shows three to four pairs of faint depressions near the dorsal furrows; thefrontal pits are rather faint; the pleuraor the fixigena is about the same width
as the axis; no palpebral ridges are recognizable only on larger cranidia; theprotopygidium is transverse lenticular
to subtriangular, convex, composed of
one to three well differentiated pygidial
segments, and slopes downward rapidly
from the posterior cranidial border. The
surface is faintly granulated.
During the present stage of morphogenesis, the protopygidial segments
increase in number, the palpebral lobe
and the ocular ridges appear, the dorsal
furrow becomes deeper, and the fixigena
increases in width.
Early meraspid stage (PI. 9, figs. 13-16
and text-fig. 4E).-The cranidium is trapezoidal in outline, convex, and about
0.25-0.65 mm in sagittal length ; the dorsal
furrow is deep and V-shaped in crosssection; the glabella is conical, convex,
tapering anteriorly and has a rounded
anterior margin; a pair of delicate glabellar furrows are visible, of which theanterior first two pairs are short andnearly horizontal, and the third is longand directed posterolaterally from thedorsal furrow; the narrow crescentic
occipital ring is convex both dorsallyand posteriorly, marked off deeply fromthe glabellar base by a distinct occipital

60

Chung-Hung Hu

furrow, and bears a minute mediantubercle; a narrow convex preglabellar
field appears in front of the glabella; it
has a median depression in the earlier
instars but smoothes out laterally; thecranidial surface is covered by bothcoarse and faint granules.
During the present stage, the glabellametamorphoses from slender conical tobroad conical, the preglabellar field fromnarrow to broad; the fixigena becomesnarrower. It is differentiated from earlier
stage by the presence of the preglabellar
field, conical glabella, and the coarse
granules.
Late meraspid stage (PI. 9, figs. 17-20
and text-fig. 4E, H).-The cranidium isof regular trapezoidal outline, convex,
with distinctly impressed dorsal furrow,
it is about 0.70-0.85 mm in length (sag.) ;the glabella is slender conical, tapering
rapidly from the anterior first glabellar
furrows; the first glabellar segment isroundly quadrate; the second to fourthones are transversely elongate, convex,
well separated by glabellar furrows; theoccipital ring is convex both verticallyand posteriorly; there is possibly aminute median tubercle; a narrow, elevated anterior border appears in front of
the glabella, and arches forward; thefixigena is about the same width as theglabella between the palpebral lobe andthe dorsal furrow; the narrow, less ele-

Explanation of Plate 8
Figures 1-28. Elvinia roemeri (SHUMARD)
1-8. a growth series of metaprotaspides, showing the differentiation of the glabella and thepleural lobes, and the completion of the glabellar segments. 1, x 44, UCGM. 43372; 2,
x 44, UCGM. 43372a; 3, x 44, UCGM. 43372b; 4, x 44, UCGM. 43372c; 5, x 40, UCGM.
43372d; 6, x50, UCGM. 43372e; 7, x50, UCGM. 43372f; 8, x50, UCGM. 43372g.
9-11. paraprotaspides, showing the presence of the protopygidium. 9, x48, UCGM. 43372h;
10, x48, UCGM. 43372h; 10, x48, UCGM. 43372i; l1, x48, UCGM. 43372j.
12-16. a few early meraspid cranidia, showing the presence of the anterior border. 12,
x29, UCGM. 43372k; 13, x20, UCGM. 433721; 14, x24, UCGM.43372m; 15, x20, UCGM.
43372n; 16, x 20, UCGM. 433720.
17,18. two late meraspid cranidia, showing the development of the preglabellar field andthe completion of the glabellar furrows. x 9, UCGM. 43372p; x 8, UCGM. 43372q.
19-24. several small and large sized cranidia, showing the broadens of the glabella and thedifference between shale and limestone specimens. 19, x 6, UCGM. 43372r; 20, x 3.5,
UCGM. 43372s; 21, a slightly deformed complete shale specimen, showing the animal
body has 10 thoracic segments, x 5, UCGM. 43372t; 22, x 2, UCGM. 43372u; 23, x 3.5,
UCGM. 43372v; 24, x 2, UCGM. 43372w.
25,27. a large and a small sized librigenae. 25, x 1.6, UCGM. 43372x; 27, x 11, UCGM.
43372y.
26,28. a shale and a limestone pygidia. x 3, UCGM. 43372z; x 3, UCGM. 43372a'.
Figures 29-36. Irvingella major ULRICH and RESSER
29. a complete early metaprotaspis, x 34, UCGM. 43375.
30. an incomplete paraprotaspis, x 33, UCGM. 43375a.
31. an early meraspid cranidium, showing the cylindrical glabella, x 15, UCGM. 43375b.
32-34. three well preserved meraspid pygidia. 32, x 20, UCGM. 43375c; 33, x 20, UCGM.
43375d; 34, x 20, UCGM. 43375e.
35,36. a late meraspid and an holaspid cranidia, showing the truncato·conical glabella.
x 28, UCGM. 43375f; x 2, UCGM. 43375g.

C. H. Hu,'

Trilobite ontogenies

2

7

Plate 8

3

4

8

16

15

5

9

10

14

13

6

11

12

18

19

17

29

26

30

21

20
32
31
22
33

23
34

24

35

36

701.

Ontogenies of Cambrian T1-ilobitesvated, palpebral lobe is faintly impressedby a palpebral furrow, which is situatedat the same elevation as the first glabellar furrow (tr.); the palpebral ridge
is faintly divided and is directed obliquelyfrom the palpebral lobe to the side of
the anterolateral glabellar margin; theanterior facial suture line is convergently
convex, and the posterior one is divergentposteriorly and straight. The cranidial
surface is faintly granulated.
During the present stage the anteriorborder changes from linear to the narrowsickle-shape, the glabella from slenderto broad based conical; the fixigena decreases in width.
Growth of the pygidium.- The earliest
known pygidium (pI. 9. fig. 24 and textfig. 4]) is semicircular in outline, convex,
and consists of about 6-7 freely articulated segments, it is about 0.50 mm inlength (sag.); the segments are all deeply
impressed by pleural furrows and extend
laterally into a pair of short broad-based
terminal spines; the conical axis tapers
posteriorly and is distinctly separated
by a ring furrow. This pygidium belongs
possibly to the early meraspid stage.
The next large pygidium measures between 0.8 and 1.0 mm (pI. 9, fig. 23 andtext-fig. 4K) ; it is triangular or transverse
rhomboidal in outline, convex, and consists of one or two free segments anda lenticular terminal pygidium; thepygidium bears 3-4 ankylosed segments;
the axis is convex, elevated above thepleural lobe, and well demarked by furrows; the pleural lobe is about the same
width as the axis and convex along themargin; neither marginal spine nor special border separation are known. This
pygidium is assigned as the late meraspid
stage.
Remarlls.- The early instars of thisspecies are closely similar to those of
Housiacanadensis

WALCOTT,

Pon1l11lia

61

obscura (LacHMAN) (Hu, 1970) and Aphelotoxon sp. (unpulished material). These

genera are possibly common descendantsof this ancestral stock.
Figured specimens.-Anaprotaspid shield,
UCGM. 43373a; Metaprotaspides, UCGM.
43373b, c ; Para prot asp ides, UCGM. 43373dI; Early meraspides, UCGM. 43373m-p;
Late meraspides, UCGM. 43373q-s, 43374c ;Cranidia, UCGM. holotype, 43373, paratypes, 43373v-x; Librigenae, UCGM.
43373t, u; Pygidia, UCGM. para types,
43374, 43374a, 43374b.
References
BELL, W. C., FENIAK, O. W. and KURTZ, V. E.
(1952): Trilobites of the Franconian
Formation, southeast Minnesota. Jour.
Paleont., vol. 25, no. 2, p. 175-188, pis.
29-38, 1 text-fig.
DELAND, C. R. and SHAW, A. B. (1959): Upper
Cambrian trilobites from western Wyoming. Jour. Paleont., vol. 30, no. 3, p. 542562, pI. 63-67.
FREDERICKSON, E. A. (1948): Upper Cambriantrilobites from Oklahoma. Jour. Paleont.,
vol. 22, no. 6, p. 798-803, pI. 123.
- - (1949): Trilobites fauna of the Upper
Cambrian Honey Creek Formation. Jour.
Paleont., vol. 23, no. 4, p. 341-363, pI. 70-

72.
GAINES, R. B. (1951): Statistical study of
Jrvingelia, Upper Cambrian tri lobi teo
Texas Jour. Sci., vol. 3, no. 4, p.60fi.-615.
GRAj\;T, R. E. (1965): Faunas and Stratigraphyof the Snowy Range Formation (Upper
Cambrian) in south western Montana andnorthwestern Wyoming. Ceol. Soc. America Mem. 96, 167p., 15 pis.
Hu, C. H. (1970): The ontogenies of Ponumia
obscura (LOCHMAN), n. g., and the Housia
canadensis (WALCOTT) (Trilobita) fromthe Upper Cambrian of the Big Horn
Mountains,
Wyoming.
Trans.
Proc.
Paleont. Soc. Japc.n, N. S. no. 77, p. 253-264, pis. 27, 28.
- - (1971): Ontogeny and sexual dimrophismof Lower Paleozoic Trilobita. Palceon.

Chung-Hung Hu
tographica Americana, vol. 7, no. 44, p.
31-135, 26pls.
LOCH~IAN, C. (1964): Upper Cambrian faunas
from the subsurface Deadwood Formation,
Williston Basin, Montana. jour. Paleont.,
vol. 38, no. 1, p. 33-60, pis. 9-15.
LOCH MAN, C. and Hu, C. H. (1960): Upper
Cambrian faunas from the northwest Wind
River Mountains, Wyoming (Part J). jour.
Paleont., vol. 34, no. 5, p. 793-834, pI.
95-100.
MOORE, R. C. (1959): Treatise on Invertebrate
Paleontology (Arthropoda 1, Part 0). Geol.
Soc. America and Univ. Kansas press,
560p.

PALMER, A. P. (1965): Trilobites of the Late
Cambrian pterocephaliid Biomer in the
Great Basin, United States. U. S. Ceol.
Surv. Prof. Paper 493, 101p.
RESSER, C. E. (1942): New Upper Cambriantrilobites. Smith. Misc. Call., vol. 103,
no. 5, 131p, 21pls.
Cambrian-Ordovician
STITT, J. H. (1971):
trilobites western Arbuckle Mountains.
Oklo Ceol. Survey, Bull. 110, 80p.
WILSON, J. L. (1949): The trilobites faunasof the Elvinia zone in the basal Wilberns
Limestone of Texas. jour. Paleont., vol.
25, no. 1, p. 25-44, pis. 9-11.

Explanation of Plate 9
Figures 1-29. Cliffia typica, n. sp.
1. anaprotaspis, showing the round shield without distinct differentiation of axial andpleural lobes. x 52, UCGM. 43373a.
2,3. a broken and a complete metaprotaspides, showing the presence of the axial and pleurallobes. x 52, UCGM. 43373b. x 50, UCGM. 43373c.
4-12. several paraprotaspid shield; notice the presence of the protopygidium and the metamorphosis of the glabella, the early shield has the glabella cylindrical and the laterones are conical. 4, x46, UCGM. 43373d; 5, x45, UCGM. 43373e; 6, x41, UCGM. 43373f;
7, x40, UCGM.43373g; 8, x40, UCGM. 43373h; 9, x37, UCGM. 43373i; 10, x37, UCGM.
43373j; 11, x30, UCGM. 43373k; 12, x32, UCGM. 433731.
13-16. four early meraspid cranidia, showing the presence of the anterior border and thebroadens of the posterior fixigenal border. 13, x 30, UCGM. 43373m; 14, x 26, UCGM.
43373n; 15, x 28, UCGM. 433730; 16, x 28, UCGM. 43373p.
17 -20. four late meraspid cranidia, showing the broadens of the preglabellar field. 17, x 25,
UCGM. 43373q; 18, x25, UCGM. 43373r; 19, x23, UCGM. 43373s; 20, x26, UCGM. 43374c.
21,22. two librigenae; notice the long genal spine and the flat genal area. 21, x 20, UCGM.
paratype, 43373t; 22, x 30, UCGM. paratype, 43373u.
23-25. two meraspid and an adult pygidia, showing the morphogenesis during their different
stages. 23, x 20, UCGM. 43374; 24, x 20, UCGM. 43374a; 25, x 20, UCGM. paratype,43374b.
26-29. four incomplete cranidia; notice the short glabella and the small palpebral lobe.
26, x 10, UCGM. paratype, 43373r; 27, x 9, UCGM. paratype, 43373w; 28, x 8, holotype,
UCGM. 43373; 29, x 12, paratype, UCGM. 43373x.
Figures 30-37. Cameraspis convexa (WHITFIELD)
30-33. a growth series of meraspid pygidia, showing the ankylosis of the pygidial segments
and the freely articulated thoracic segments. 30, x 20, UCGM. 43376; 31, x 20, UCGM.
43376a; 32, x 20, UCGM. 43376b; 33, x 20, UCGM. 43376c.
34-37. four cranidia, showing the morphogenesis from the late meraspid to adult stages.
34, x10, UCGM. 43376d; 35, x6, UCGM. 43376e; 36, x4, UCGM. 43376f; 37, x3, UCGM.
43376g.

C. H. Hu: Trilobite ontogenies

2

12

11

Plate 9

3

4

10

9

5

6

8

7

35

36

37

701. Ontogenies of Cambrian Trilobites~TO)m~· -:1 ~Deadwood Jflii:f&WJ;h '/ 7' ~ 7*c~~!R 0) M {* re 1=.: Elvinia roemeri
Cliffia typica, n. sp., Irvingella major ULRICH and RESSER t.e 0 lYle
Cameraspis convexa (WHITFIELD) O)m{$:re1=.le'0~'-Ciiciill L.t-:o fitr 2 ~tellkl L. -C~:tB: "'71';~t.ere1=.~WlO)WftJfiJ;-c'~, -to)*5:lr-: E. roemeri c I. major cl:t.~b.lb-CJ: <mfj;J,L.td'&
J1l!Jta:t-: c' ~ C c iJ, 0, ;J:!<JllH!l:9Gta: {, '0:T Ii" - 7°iek~--t ~ C c iJ;~ 0iJ'lct.e -:> t-:o C. convexa
O)f&Wl-" '7 ;7..\::°;7..I:t. Dunderbergia ~O)-tnc*ll'£J: < fj;J,-C:f; I), convexa iJ>cO)~iJ'00)@:~O)5ttz-c';6 ~ c ~;t -C J: ~ '0 C. typica O)fJJWlre1=.J&j:!liH:t. Ponumia obscura (LOCI'I~IA"),
Housia canadensis WALCOTT, Aphelotoxon sp. tt. c' c Jt~-c' ~, ~ 'i'n {, ;ltjjO)t!l:9G1*ta:(SHUMARD),{,'0{,O)c.7,..0n~063Trans . Proc. Palaeont. Soc. Japan, N. S., No . 114, p. 64, Jul y 15, 1979.

SHORT NOTES
16. SOME NEWLY DISCOVERED LATE PERMIAN CORALSFROM THE MAIZURU GROUP *SHIGEYUKI SUZUKI
Departm e nt of Earth Science, Facult y of Sc ience,Oka yama Univers it y, Oka ya ma 700

andNOBUO Y AMAGIWA
Department of Earth Science, Facult y of Education,
Osaka K yoiku Univers it y , Osaka 543

The Late Permian corals from theMai zuru Group were reported previousl yby Y AiVlAG IW A (1960). Recent ly, the seniorauthor has collected some more corals
from this group at the following four
localities in Maizuru Cit y, K yoto Prefectur e :Loc. 1 1.5 km SSE of Kawara , Maizuru
City
Loc. 2 0.5 km S of Kinoshita, Maizuru
City
Loc. 3 2.0 km SSW of Kinoshita, Maizuru City
Loc. 4 0.2 km N of Shiratori-toge, Maizuru City
WaagenoPhyllum (Waagenophyllum) virgalense (W AAGE N and WENTZEL) occurs inlimestone lenses at Locs. 1 and 2, andW . ( W. ) sp. indet. in a conglomeraticrock at Loc. 3. Loc. 4 yielded W. ( w. )aff. pulchrum, Lo phophyllidium? sp. indet.
and V erbeekiella? sp. indet. in a conglomeratic rock.
Of these, WaagenojJhy llum ( ltV aagenophyllum) vi rgalense is associated with
Palaeofusulina aff. sinensis - Colaniellaparva fauna, and other fossils occurs
in common with Lepidolina Immaensis
fauna. Accordi ng to ISH II, OKJiVlURA and
NAKAZAWA (1975), the form e r fauna is
yo unger than the latter fauna and indicates a Latest Permian age. These
corals w ill be described in detail onanother occasion .
This short paper presents the flrst re-

Text-fig . 1. Waagenophyllu m ( Waag enophyllum ) virg aiense (W AAG EN and W ENT ZEL) A: Trans ve rs e section. B: Longitudinal
section. Localit y : 0.5 Km S of Kinoshita,
Maizuru Cit y .

port of a Late Permian coral faunule
found together with the Palaeofusu linaaff. sinensis-Colaniella pm-va fauna inJapan .
Thanks are due to Professor C. MITS U '0
of Okayama University for his kind
guidance and to Associate Professor Y.
OKJiVl URA of Hiroshima Universit y for his
advice encountered on the foraminiferal
fossils.

References
ISI-III, K., OI{IMURA, Y. and NAI<AZAWA, K.
(1975) : On th e genus Colaniella and its
biostratig raphic sig nificanc e . j our. Ceosci.,
Osaka City Univ. , vol. 19, art . 6, p. 107138, pIs. 1- 4.
Y AMAG IWA, N. (1960) : Th e Late Pal eozoic
corals from th e Maizuru zon e , So u thwest
Japan . M em. Osa ka Univ. Lib . A rt . and
Edu c., B, Na t. Sc i., no. 9, p. 72- 81, pI. 1.

* Rece ived March 28, 1979.

64

Trans. Proc. Palaeont. Soc. japan, N. S., No. 114, pp. 65-76, pis. 10, 11, july 15, 1979

702.

A NEW GAUDRYCERATID AMMONITE
FROM EASTERN HOKKAIDO(STUDIES OF THE CRETACEOUS AMMONITES FROMHOKKAIDO AND SAG HALlEN-XXXVII)TATSURO MATSUMOTO
Seinan.gakuin University, Fukuoka 814

and
SABURO YOSHIDA
Department of Earth Sciences, Yamagata University, Yamagata 990

Abstract. Since YOSHIDA'S (1958) preliminary report, fairly numerous ammonite
specimens have been collected from two localites in the Hamanaka area (eastern
Hokkaido). They represent a new species of Gaudryceras, which is allied to G.
varicostatum VAN HOEPEN in the septate shell but is distinguished by the persistency
of Vertebrites type lirae up to the adult body-whorl. It was once provisionallycalled Vertebrites aff. kayei (FORBES), but it has the typical pattern of Gaudryceras
suture and is distinct from V. kayei in its shell-form and surface ornamentation.
This new species occurs in a sandstone bed belonging to the main part of the Akkeshi Formation C=N4J of the Nemuro Group. The ammonite·bearing bed is probably assigned to the upper part of the chronological equivalent Ci. e. K6bJ of theMaastrichtian in the japanese scale.

S. YOSHIDA (in 1956), W. HASHIMOTO, S.
YOSHIDA, S. KANNO etc. (in 1957), H. KIDO
and T. MATSUMOTO (in 1958), and S.
YOSHIDA and others (in 1963 and 1964).
Before going further, we thank Dr.
Wataru HASHIMOTO, who provided us thecollection of Tokyo Kyoiku Daigaku[TKDJ [=Tokyo University of Education, now turned to be the University ofTsukubaJ for our study, Mr. Hideo KIDO
of the Japan Petroleum Exploitation Co.
Ltd., Mr. Kojiro IWATA, Chairman of theBoard of Education (Haman aka-mach i)and M. Tamiji ITO of Ponporoto, whohelped us in the field work, Dr. Kazushige
TANABE and Miss Kazuko HARA, who
assisted us in preparing the plates andtypescript, Dr. Ikuwo OBATA, Mr. C. W.
WRIGHT, Dr. J. M. KENNEDY and Dr. M. V.

Introduction

The Nemuro Group distributed in theeastern part of Hokkaido is chronostrigraphically interesting in that it ranges
from the Campanian to Palaeocene andthat the Cretaceous-Tertiary boundary
should be located somewhere in the upper
part of the sequence. Several species ofammonites have been reported from thegroup, without a full description andillustration.
This paper is to give a palaeontologicaldescription of one of the ammonite
species, which occurred at two localities
in the Hamanaka area. The specimens
were collected on several occasions by
Received December 31, 1978; read October
14, 1978 at Yamagata.

65

Tatsuro MATSUMOTO and Saburo YOSHIDA66

HOWARTH, who kindly gave to one of us(T. M.) valuable information on somerelevant species from Shikoku, New
Zealand, South Africa, Europe and India,
and Dr. Masayuki TASHIRO, who kindly
identified some bivalve species from theammonite bearing bed.
A part of the expenditures for thisstudy was defrayed through the grant(No. 334043) in aid of the Ministry of Education, Science and Culture [MonbushoJ.
Note on Stratigraphy

The Nemuro Group is made up primarily of marine deposits of partly terrigenous and partly volcanogenic origin,about 3000 m thick, and stratigraphicallysubdivisible into six units, simply marked
as units NO, Nl, N2, N3, N4 and N5 in
ascending order by MATSUMOTO (1970).
As it is ~xposed for a considerable extent in eastern Hokkaido; lJulny local
formational names have been proposedby various authors, especially those of
Table 1.

NAGAO

I
I

the explanatory texts of the geologicalmaps (on scale 1: 50,000).
The Hamanaka area, where the described ammonite species came, is in thegeological map of "Kiritappu" [=KiritapJ(NAGAO et al., 1966) and the formational
names in that sheet·· are indicated inTable 1.
Recently, KIMINAMI (1975-76) has accomplished an interesting sedimentological investigation of the Nemuro Groupand also (1978) summarized its lithostratigraphy. His scheme in general agrees
with MATSUMOTO'S, although there arestill some unsettled problems from abiostratigraphic viewpoint.
Anyhow,these two schemes are also shown in
Table 1, along with that of NAGAO et al.
The ammonite specimens to be de. scribed in this pap~r were found fromsandstones which are assignable to thelower member of the Akkeshi Formationof KIMINAMI i.e. t~~ :lower part of N4
of MATSUMOTO or the lower part ofMember At 2 of NAGAO et al. (see Textj

Stratigraphic division of the Nemuro GroupF.=Formation M.=Member

et aI., 1966

I MATSUMOTO, 1970 I

Kiritappu F.

I

I

N5

Kiritappu F.
Tokotan F.

At 3

I

I
0.
::l
0

....

v
0

....

I

Upper M.
Akkeshi F.

I

I

N4
Akkeshi F.

At 2Lower M.

I
i
I

I

::l

E
(1)

At 1

I
~

Hamanaka F.
N3
Oborogawa F.

Poroto F.

Z

Karikan F.
N2Monshizu F.

N1

Otamura F.

NONokkamappu F.

Monshizu F.
iI

Middle M.

Otamura F.
(not exposed)

I

I
1

702.

A New Gaudryceratid Ammonite

fig. 1). The Akkeshi Formation [N4]consists mainly of mudstone and sandstone alternating in various grades ofthickness. In the eastern part of theoutcropping area of the group, i. e., from
Nemuro through Hamanaka to Akkeshi,
slump structures are characteristicallydeveloped in the formation. One of thetwo fossil localities at Ponporoto, indicated as A in Fig. 1, is in a less disturbed
bed of sandstone, but the other, indicatedas B, about 250 m west of loco A, is in asandstone (of similar lithology) within
the contorted sediments. The containedsandstone is contemporary with the hostmudstone of the same formation and notderived from the underlying formations,as KIMINAMI (1975-76; 1978) discussed at
length. The slump structures can beinterpreted to have been caused by frequent intrusions of dolerite sills into the
NO to N4 formations, which took placewhen the sediments were unconsolidated
and still contained much water, as suggested by pillow structures in the dolerite(see Y AGI, 1968). The slump structures
are absent or infreq uen t in the westernarea where the dolerite is poorly developed.
Among the guide species from the Nemuro Group, Inoceramus (Sphenoceramus)
schmidti MICHAEL from NO indicates K6a(Campanian) stage, Inoceramus (Endocostea) shikotanensis NAGAO and MATSUMOTO from N1 the lower K6b (probably
the lowest part of the Maastrichtian),
Inoceramus (s.l.) kusiroensis NAGAO and
MATSUMOTO and Pachydiscus sp. from N2
mid-K6b (somewhere in Maastrichtian),and Zelandites varuna japonica MATSUMOTO and "Pachydiscus subcompressus
obsoletus MATSUMOTO" from the upper
part of the Senposhi Formation (either
upper N3 or lower N4) the upper K6b.

,

- .,.,

Ot\~,,,,\-----------_.-

,

~H

Ka

.'.,
\
Ka

Po
\

------..''----·Atl'\ ----;:t"i-----------------------'-,,--_ .... ---At1
D1

2km

Text.fig. l.

67

Geological map of the coastal area of Hamanaka, eastern Hokkaido(terrace deposits omitted)
Symbols of the formations (F.) in ascending order--Ot: Otamura F., Mo: Monshizu F.,
Ka: Karikan F., Po: Poroto F., At I-At 3: Akkeshi F. (subdivided into three parts), 01:
Dolerite sill. Place names.--E : Esashito, H: Hamanaka (s. str.), P: Ponporoto. Ammonites
localities A-D indicated by small solid circles. Inset at the lower right corner map of Hok·kaido indicating the location of Hamanaka with H and the outcropping Nemuro Group withsolid black.

68

Tatsuro MATSUMOTO and Saburo YOSHIDA

On the other hand, N5 is certainly of
Palaeocene age on the evidence of planktonic foraminifers from it [locally called
the Chipomanai or the Kiritappu Formation] (ASANO, 1962; YOSHIDA, 1967).
Therefore, the ammonites from the Akkeshi Formation [N4] must represent theupper part of the Maastrichtian equivalent(i. e. K6b) in the Cretaceous of Japan.
In addition to the gaudryceratid ammonite to be described below, YOSHIDA
once collected an example of another ammonite species referable to "Pachydiscus
subcompressus obsoletus" from the same
member At 2 at a locality (C in Fig. 1)
near Esashito about 8.5 km east of Ponporoto. The benthonic foraminifers fromAt 2 show an Upper Cretaceous faunalaffinity and some species of them arecommon with those from At 3 (YOSHIDA
in NAGAO et aI., 1966, table 2). No planktonic foraminifer has been detected fromthe Akkeshi Formation of the Hamanaka
area. ASANO (1962) once reported theoccurrence of Danian planktonic foraminifers, Globigerina compressa PLUMMER,
G. daubjergensis BRONNIMANN, G. pseudobulloides PLUMMER and G. ct. triloculinoides PLUMMER, from N4 [locally called
the Choboshi Formation] at Ochiishi(southwest of Nemuro), but some ammonites have been found by us from thesame member.
ASANO'S foraminifer
specimens have not been illustrated andare now unfortunately missing, and noplanktonic foraminifers have subsequently
been detected from the same member.
This is a questionable point, although
Ochiishi is located outside of the Hamanaka area.
Palaeontological Description

Subclass Ammonoidea
Order Lytoceratida

Family Gaudryceratidae SPATH, 1927
Genus Gaudryceras DE GROSSOUVRE, 1894
Type-species :-AmnlOnites mitis HAUER,
1866 (designated by BOULE, LEMOINE and
THE VENIN, 1906, p. 11).
Remarks: - At present we follow
WRIGHT and MATSUMOTO, 1954, in regarding Neogaudryceras SHIMIZU, 1934 (withtype-species G. tenuiliratum YABE) as asynonym of Gaudryceras. The extremely
fine lirae on the ventral part which arebranched from and also inserted between
the less fine lirae on the umbilical shoulder
and inner lateral part of the whorl at
the immature stage is one of the characteristic features of the subgroup of G.
tenuiliratum, but was not mentioned by
SHIMIZU. This character, which can becalled the Vertebrites-like ornament, is
not recorded with respect to G. mite andallied species. In G. teuuiliratum, it occurs
in a limited period of the immature
stage and is hardly observable unless theouter whorl is taken off. Therefore, itwould be practically unwise to separate
Neogaudryceras from Gaudryceras on thisaccount. This Vertebrites-like ornament
does appear in several species of Gaudryceras and very remarkably so (almost
throughout growth) in the new species
to be described below. In other words,
this species could represent a subgenus
of Gaudryceras, should the genus Gaudryceras be divided into subgenera on sufficient grounds. In this paper, however,
we would not dare to propose the subgenus.
Gaudryceras hamanakense sp. nov.
PI. 10, Figs. 1-3, PI. 11, Figs. 1-2;
Text·fig. 2.

Material :-Holotype, GK. H5873, consisting of the complementary two pieces.

702.

A New Gaudryceratid Ammonite

i. e. (a) internal mould plus most of theshell and (b) external mould with some
attached pieces of the shell, in calcareous
sandstone obtained by H. Kmo and T.
MATSUMOTO (1959-8-13) at point KUl056
of loco A of Ponporoto, Hamanaka, eastern
Hokkaido. Paratypes, YO. C7615-C7622(colI. S. YOSHIDA), 4 specimens of TKD.
30480-30483 (colI. W. HASHIMOTO, S. YoSHIDA, S. KANNO, etc.) and GK. H5874(ColI. Kmo and MATSUMOTO from point
KUl057), GK. H5875 and H5876 (colI. W.
HASHIMOTO, etc.) from the same bed of
the same cliff (loc. A) as the holotype.
Also a number of specimens from loco
B of Ponporoto, are comparable withthose from the type-locality.
SPecific characters :-Shell of moderate
size at the adult stage, about 100 mm in
the maximum diameter. It consists ofpolygyral whorls: 9 septate ones plus theliving chamber of about 300·.
In the immature shell, up to diameterof 45 mm or so, the shell is evolute, only
the ventral part of the inner whorl being
overlapped by the outer one, and has awide umbilicus, which occupies about oreven a little more than 50 percent of theentire shell diameter. The whorl is muchbroader than high at the early stage(e. g. B/H=2.0), increasing more rapidly
in height with growth, and at or near
the last part of the septate shell, atdiameter of 55 mm or so, it is slightly
broader than high (with B/H approximately 1.1). The whorl-section changes
from a depressed crescent to a subcircular outline. It is broadest at a point
somewhat below the middle of the whorlheight.
The last whorl increases moderately
rapidly in height, becoming higher thanbroad, with a more narrowly arched
venter, gently convex flanks and abruptly
rounded umbilical shoulders. It overlaps
about one third to nearly a half of the69

next inner whorl.
Constrictions are frequent mainly inthe second whorl following the nepionicconstriction. They are marked fairly
regularly on the internal mould of themain part of the septate shell, numbering
4 per whorl. Each of them is accompanied
behind by the rib, which is raised when
the shell material is preserved. It runs
obliquely forward around the umbilicus,
especially remarkably so at about theumbilical shoulder, is slightly prorsiradiateon the main part of the flank, showing
a gentle sinuosity, and crosses the venterwith some convexity.
On the living chamber, the constrictions or the major ribs are of nearly thesame frequency in its earlier part as in
the preceding septate part, but becomes
more frequent in its later part, numbering 4 within the last quarter whorl.
The surface of the shell is ornamented
with numerous lirae which run in parallelwith the constrictions. On the main partof the septate shell the lirae are sharpheaded and distinct on the umbilicalwall, being separated by somewhat wider
interspaces. At or near the umbilicalshoulder somewhat finer intercalary lirae
appear between the longer and more
distinct ones. These lirae become finerand less raised as they go outwards andbifurcate on the flank, where they areintercalated by still more lirae. Thus,on the ventral part the surface of theshell has numerous, dense, extremely finelirae. The number of the lirae are, forinstance, in the last portion of the septate
whorl within the distance (at mid-flank)
as long as the whorl-height, about 12 on
the umbilical wall, becoming as large as
120 on the venter. That is, the extremely
fine lirae on the ventral part are about
ten times as numerous as the lirae aroundthe umbilicus. The lirae are well observable on the surface of the outer shell

Tatsuro MATSUMOTO and Saburo YOSHIDA

70

layer but scarcely or hardly discernible
on the inner shell layer. They are notimpressed on the internal mould.
The outer surface of the shell of theliving chamber has the same kind oflirae as above and the major ribs arecovered with these fine lirae. Those on
the umbilical wall are fairly coarse andmay be very faintly impressed on theinternal mould, but those on the ventral
surface are kept extremely fine, dense
and numerous.
Suture is of the same pattern as thatof Gaudryceras tenuiliratum YABE (compare Fig. 2 of this paper with fig. Ie in
MATSUMOTO, 1942).
Remarks:- The living chamber of theholotype is somewhat secondarily compressed and partly detached.
Otherspecimens of similar sizes (TKD. 30480,
TKD. 30482, GK. H5875 and GK. H5876)
Table 2.

Measurements (in mm.) of G. hamanakense sp. nov.

Specimen
DiameterGK. H5873 (septate part) 55.0(1)YU. C7615
59.0(1)
YU. C7616 ( -60°)
57.0(1).YU. C7617
53.5(1)( -90°)
46.0(1)"have also a more or less deformed living
chamber. The septate whorls of these
specimens are not deformed.
YU. C7615 (PI. 10, Fig. 2) is nearly ascompletely preserved as the septate partof the holotype, in showing the characteristic lirae and other features. Other
specimens of similar or smaller sizes
ha ve less well preserved outer shelllayers or are represented by internalmoulds.
Even in the septate stages, there issome variation in the growth-rate of thewhorl. For example, YU. C7616 andC7617 show a slightly slower growth and,accordingly, a wider umbilicus than YU.
C7615 and GK. H5873 of the corresponding size.
Whether the variation isnormal or bimodal is not determined fromthe available number of specimens (seeTable 2).

Umbilicus
26.5(.48)
27.8(.47)
28.4(.50)
25.7 (. 48)
23.0(.50)

Height17.8 (.32)
18.7 (. 31)
17.0(.29)
17.4(.32)
14.5(.31)

Breadth19.8(.36)
20.5(.34)
20.0 (.35)
19.7 (.37)
16.4 (.35)

B./H.
1.11
1.10
1.17
1.13
1.13

Text-fig. 2. Gaudryceras hamanakense sp. nov.
Suture at diameter=38.5 mm of an immature specimen, TKD. 30481. (T. M. delin.)

702.

A New Ga'L~dryceratid Ammonite

Comparison and discussion:- The immature shell of the present species resembles the holotype of Caudryceras
varicostatum VAN HOEPEN (1921, p. 7, pI.
2, figs. 10-12, text-figs. 3, 4), from Pondoland (South Africa) in its shell-form,
constrictions, surface ornamentation andsutures.
According to KENNEDY (letter of 19788-9 in response to T. M.'s inquiry),
HOEPEN's holotype is immature and theadult stage of the same species is represented by the holotype of Caudryceras
cinctum SPATH (1922, p. 118, pI. 9, fig. 3),
which has stronger, coarser and more
flexuous lirae on the outer whorl thanthose of the immature C. varicostatum.
Thus, in the adult shell the specific distinction between C. varicostatum and C.
hamanakense is clearly shown.
Caudryceras tenuiliratum YABE, 1903,
from the Coniacian and Santonian (andalso Lower Campanian) of japan andother areas of northern Pacific region,
resembles the present species with respect
to the character of the lirae on the immature whorl, bllt its outer whorls havenot so much multiplied, extremely finelirae on the ventral part as in the present
species. Normally C. tenuiliratum has anarrower umbilicus than the present
species. A form called var. ornata by
Y ABE (1903, p. 24, pI. 3, fig. 2) is as widely
umbilicate as the present species in theimmature shell, but it has the same typeof outer whorl as the normal form of
C. tenuiliratum.
In other words, C.
varicostatum VAN HOEPEN emend KENNEDY may be closely related to nearly
contemporary C. tenuiliratum throughthis variety. The species called C.
tenuiliratum by JONES (1963, p. 26, pI. 10,
figs. 1-3), from the Zone of Pachydiscus
kamishakensis of southern Alaska, isdistinct from true C. tenuiliratum and C.
hamanakense in its coarser I:ibbing on the71

adult shell. Incidentally, the specimen
from the Urakawa area illustrated by
YOKOYAMA (1890, pI. 18, fig. 12) under
Lytoceras sacya was designated as thelectotype of C. tenuiliratum (see MATSUMOTO, 1963, p. 29; also JONES, 1963, p. 28).
It is preserved in Munich.
The present species was once provisionally called Vertebrites aff. kayei(FORBES) (MATSUMOTO, 1970). Depite theVertebrites-like surface ornamentation,
the assignment of the present species toVertebrites was incorrect. As is wellshown by V. murdochi MARSHALL, 1926,
the type-species of Vertebrites, the internal suture of this genus is dissimilar
to that of Caudryceras in having an independent pair of lobes (U1) between I
and obliquely descending lobules of asuspensive lobe (U3=S). In addition tothe original illustration of MARSHALL(1926, pI. 20, fig. 9a), another figure isshown here (Text-fig. 3) in comparison
with the suture of the present species(Text-fig. 2).
Ammonites kayei FORBES, 1846 wasestablished on a number of syntypes (seeKOSSMAT, 1895, p. 124). The specimen
illustrated by FORBES (1846, p. 101, pI. 8,
fig. 3) [8M. C. 51050J is a small, probably
immature specimen. Dr. M. V. HOWARTH(letter of 1978-10-18) wrote, in responseto the inquiry from one of us (T. M.),tha t this specimen shows the Vertebrites
VI

[2

~~
Text·fig. 3.

Vertebrites murdochi

MARSHALL

Internal suture at whorl-height=3.6 mm,breadth=7.0mm ofthe specimen C.W.W.N.Z.
27. (T. M. delin.)

72

Tatsuro MATSUMOTO and Saburo YOSHIDA

type internal suture. It was erroneously
indicated as holotype by MATSUMOTO(1959, p. 146), but is designated here as
the lectotype of Vertebrites kayei (FORBES).
Another, larger syntype [BM. C 51049J
illustrated by KOSSMAT (1895, pI. 17, fig.
2a, b) is, according to PHILLIPS (1977) andHow ARTH, a more grown example of thesame species. The specimens of C.
hamanakense as large as this KOSSMAT'S
figured one are distinguished in having
more rounded whorls, with less angularumbilical shoulders and the maximum
breadth somewhat above (but not at)
the umbilical shoulder. On the umbilicalwall and shoulder the lirae are muchfiner in KOSSMAT'S specimen than in C.
hamanakense of the corresponding size.
Unless the internal suture is examined
it seems us to be difficult to identify
Vertebrites kayei on small, probably immature specimens. Despite the unclear
definition, many ammonites have beenreported under this specific name fromvarious regions. They need restudy,
although some of them (e. g. examples
from the Lower Maastrichtian of Madagascar, such as COLLIGNON, 1956, pI. 6,
fig. 5) may be correct.
Lytoceras (Caudryceras)coalingense
ANDERSON (1958, p. 184, pI. 68, fig. 1) andL. (C.) birkhauseri ANDERSON (1958, p.
185, pI. 68, fig. 4), from the Maastrichtian
equivalent of California, were once included by MATSUMOTO (1959, p. 146) in
C. (V.) kayei currently understood at that
date.
They somewhat resembles C.
hamanakense, but if we examine the liraeon the outer shell layer which is partly
preserved on the holotypes of these
ANDERSON'S species, we notice a distinction. The lirae of our species are coarser
at and near the umbilical shoulder but
distinctly finer on the outer part of thewhorl, with more intercalation andbifurcation than those of the California

species. In other words, the California
form is closer to V. kayei, although its
internal suture has not been examined.
The possibility that it may represent ageographical subspecies of V. kayei still
remains.
A fragmentary ammonite from the Shimantogawa Group (Furumugi Formation)
at Mugi (Shikoku), which OBATA (in SuYARI et aI., 1967) called C. (V ertebrites)
sp. ct. C. (V.) kayei (FORBES), likewise,shows the kayei type lirae, which areless coarser near the umbilical shoulder
and less finer on the outer part thanthose of C. hamanakense. Incidentally
this specimen seems to have a Vertebrites
type internal suture, although mucheroded.
Caudryceras crassicostatum (JIMBO) (1894,
p. 36, pI. 6, fig. 7) (Y ABE, 1903, p. 29, pI. 4, fig. 4), from the Campanian of Soya
(northern Hokkaido), has the living chamber which is similar to that of the present species, but its major ribs become
thicker than in the latter. Its inner
whorls are as polygyral and as evoluteas in the present species, but less broader
and have less rounded umbilical shoulder
than in the latter. Again the lirae ofC. crassicostatum are less coarser near
the umbilical shoulder and less finer on
the ventral part than those of the present
species.
Occurrence:- Two localities, indicatedas A and B on the map of Text-fig. 1,
which are cliffs at Ponporoto, Hamanakamachi [previously Hamanaka-mura], Akkeshi-gun, eastern Hokkaido. A is thetype-locality situated at 49°8'47" N, 145°
9'59" E, where the described ammonites
occurred commonly in a sandstone bed,
either in the contained calcareous nodules
or in the calcareous part of the sandstone,
exposed in the upper part of the outcropping beds (Text-fig. 4). This locality was
numbered 7688 by W. HASHIMOTO. KIDO

702.

A New Gal,~drycemtid Ammonite

73

Concluding Remarks

Te x t-fig. 4. Sandstone outc rop on acliff of loco A at Ponporoto. A man ishandling the ammonite bearing bed at point
KU 1056. A fau lt cuts the bed near thewestern (left) end of this picture and aslump structure is partl y sho w n on its westside . (S. Y. photo)

and MATSUMOTO distinguished samples
KU. 1055 - KU. 1060 within this bed, of
which the holotype was from KU. 1056,
near the western end of the outcropping
sandstone bed (i. e. the point where aman is handling in Text-fig. 4). A t loco
B, situated about 250 m west of loco A,
the specimens are not so we ll preserved
as at A.
The ammonite bearing bed belongs to
the lower part of At 2 defined by AGAO
et al. (1966). At 2 is the main part of the
Akkeshi Formation of these authors.
According to KnvII NAMI (1978), who defines At 2 only as the Akkeshi Formation , the fossiliferous bed is assigned to
the lower member of his Akkesh i Formation (see Table 1 and also Note on Stmtigraphy). From the same bed occurred
Opis hokkaidoensis UEDA, L imopsis shinwnadaensis (ICHIKAWA and MAEDA), Acila(T runcacila) n. sp., Izumicardia parva
ICHIKA w A and MAEDA, T enea japonica
ICHIKA w A and MA ED A, Periplomya elliptica
NAGAO and OTATUME and some brachiopods (UEDA, 1963; additional identification by M. TASHIRO, letter of 1978-1213).

The ammonite specimens from Pon poroto of the Hamanaka area, eastern
Hokkaido, represent a new species ofCaud ryceras in the upper part of K6b(approximate time-equivalent of Maastrichtian ) in Japan. This species, named
C. hamanakense MATSUMOTO and YOSHIDA, sp. nov. , is allied to C. varicos tatwn
VAN HOEPEN, from the Santonian ofSouth Africa and Madagascar, in the
septate shell but has persistent lIertebriteslike lirae in addition to the freq uent,narro w major ribs on the adult living
chamber. It has, however, the t ypical
pattern of Caudrycems suture.
Species of Cau drycems generall y havea long stratigraphical range, ex tending
over two or more stages, and also a wide
geographical distribution. Therefore, thetrue vertical and hori zontal ran ge of thisspecies should be worked out in the
future. It is noted that this species has
not yet been found from K6b of central
Hokkaido, where different species ofgaudryceratids are found, though not yet
described. A ccording to T ASHIRO (lette rof 1978- 12- 13), the bi val ve species fromthe bed with C. hamanalzense are also of
the fauna of upper K6b (TASHIRO, 1977).

References Cited
A NDERSON, F. M. (1958) : Upper ~C retac e ousof t he P ac ific coast. Ceol. Soc. Amer.
Mem. 71, 378 p., 75 pis.
ASAN O, K . (1962) : Japanese Paleoge ne fromthe v iew-point of foraminifera w ith descriptions of seve ral new species. ContI'.
I ns /. Ceol. Paleont. Toh oku. Univ ., no. 57 ,p. 1- 32, pI. 1 (i n Japanese w ith English
abstract) .
BOULE, M., LEMO INE, P . and TI-I EVENIN, A .
(1906) : Paleontologie de Madaga scar, 111Ce phalopodes cretaces des environs deDiego-Suarez . Ann . Pa teon t., vol. 1, p.

74

Tats'nro MATSUMOTO and Saburo YOSHIDA

173-192, pis. 14-20.
COLl,IG:-;O)l, M. (1956): Ammonites neocretacees du Menabe (Madagascar). IV.-Les
Phylloceratidae, V.-Les Gaudryceratidae,
VI.-Les Tetragonitidae. Ann. Geol. Servo
Mines, no. 23, p. 1-100, pIs. 1-11.
FORBES, E. (1846): Report on the fossil Invertebrata from southern India, collectedby Mr. KAYE and Mr. CUNLIFFE. Trans.
Geol. Soc. London, ser. 2, vol. 7, p. 97174, pIs. 7-19 (for 1845).
GROSSOC\'RE, A. DE (1894): Recherches surla Craie superieure. II. Paleontologie.
Les ammonites de la Craie superieure.
Mem. Carte Geol. France, 246 p., 39 pis.
(for 1893).
HAUER, F. VOi': (1866): Neue Cephalopoden
aus den Gosaugebilden der Alpen. Sitzgsber. Akad. Wiss. Wien, vol. 53, p. 300-308,
pIs. 1-2.
HOEPE:-;, E. C. N. VAN (1921): Cretaceous
cephalopoda from Pondoland. Ann. Tl'ansvaal Museum, vol. 8, no. 1, p. 1-48, pis.
1-11.
jl~IBO, K. (1894):
Beitrage zur Kenntniss
der Fauna der Kreideformation von Hokkaido. Geol. Palaeont. Abh., N. F., vol. 2,
no. 3, p. 149-194, pIs. 17-25.
JONES, D. L. (1963): Upper Cretaceous (Campanian and Maastrichtian) ammonites
from southern Alaska. U. S. Geol. Surv.
Prof. Paper 432, p. 1-53, pIs 1-41.
KEvIINA~II, K. (1975-76):
Sedimentology of
the Nemuro Group. Parts 1-4. Jour. Geol.
Soc. Japan, vol. 81 (1975), p. 215-232, (pt.
1) (in English); p. 697-708 (pt. 2); p.

755-768 (pt. 3); Ibid., vol. 82 (1976), p.
773-782 (pt. 4) (pts. 2-4 in japanese withEnglish abstract).
- - (1978): Stratigraphic re-examination of
the Nemuro Group. Chikyu-kagaku, vol.
32, p. 120-132 (in japanese with English
abstract) .
KOSSMAT, F. (1895): Untersuchungen liber
die siidinciische Kreideformation. I. Beitr.
Pclaont. Geol. Osterr-Ungarns Orients,
vol. 9, p. 97--203, pIs. 15-25.
MARSHALL, P. (1926): The Upper Cretaceousammonites of New Zealand. Trc.ns. N. Z.
Inst., vol. 56, p. 1:i9-210, pis. 19-47.
MATSUMOTO, T. (1942): A note on the japanese Cretaceous ammonites belonging to
the Gaudryceratidae. Proc. Imp. Acad.
Japan, vol. 18, p. 666-670.
- - (1959): Upper Cretaceous ammonites ofCalifornia, Part I I. Mem. Fac. Sci., Kyushu Univ., ser. 0, GeoL, spec. vol. 1, p.
1-172, pIs. 1-41.
- - (1963): In MATSUMOTO, T., HAYAMI, I.
and ASANO, K. (1963): A survey of fossils from japan illustrated in classicalmonographs, Part VII. Palaeont. Soc.
Japan 25th Anniv. Vol., 27-32, pis. 44-51.
- - (1970): Geological age of the Mesozoic
systems. Kc.gaku, vol. 40, p. 248-255 (injapanese) .
NAGAO, S., ISIIIY AMA, S. and YOSHIDA, S.
(1966): Kiritappu. Expl. Text. Geol. Map.
Japan, scale 1: 50,000, 38 p. (in japanesewith English abstract).
PHILLIPS, D. (1977): Catalogue of the typeand figured specimens of Mesozoic Am-

Explanation of Plate 10
Figs. 1-3. Gaudryceras hamanakense sp. nov ........................................... Page 68
1. Holotype, GK. H5873a, from KUl056 of loc. A (Text-fig. 1) , Ponporoto, Hamanaka-machi,
eastern Hokkaido (ColI. H. KIDO and T. MATSUMOTO). Lateral view of the entire
shell (a), x about 0.7; the same without the outer quarter whorl to show more completely the next inner whorl (b), xl.
2. Paratype, YU. C7615, from the type-locality (ColI. S_ YOSHIDA), two lateral (a, b) andventral (c) views, xl.
3. Paratype, TKO. 30481, from the type-locality (ColI. W. HASHIMOTO etc.). Lateral (a)and frontal (b) views of an inner whorl, whose suture is illustrated in Text-fig. 2.
Kyushu University photos (K. T ANAEE), without whitening.

MATSUMOTO and YOSHIDA:

Gaudryceras hamanakense

Plate 10

702.

A New Gaudryceratid Ammonite

monoidea in the British Museum (Natural
History). 220 p., Brit. Mus. (Nat. Hist.),London.
SIIlMIZU, S. (1934): Ammonoidea. In SHIMI·ZU, S. and OBATA, T.: Cephalopoda.
Iwanami's Series Ceol. & Palaeont., 137
p., Tokyo (in japanese).
SPATH, L. F. (1922): On the Senonian ammonit~s fauna of Pondoland. Trans. Roy.
Soc. South Africa, vol. 10, p. 113-147, pis.
5-9.
- - (1927): Revision of the jurassic cephalopod fauna of Kachh. Mem. Ceol. Surv.
India, Palaeont. Indica, (n. s.], vol. 9, no.
2, pt. 1, p. 1-71, pis. 1-7.
SUYARI, K., BANDO, H. and OBATA, I. (1967) :Discovery of a Cretaceous ammonite fromthe Shimanto terrain, eastern Shikoku.
Jour. Ceol. Soc. Japan, vol. 73, p. 535-536(in japanese).
TASHIRO, M. (1977): Bivalve faunas of theCretaceous Himenoura Group in Kyushu.
Palaeont. Soc. Japan Spec. Pap. no. 19, p.
1-102, pis. 1-12.

75

WRIGHT, C. W. and MATSUMOTO, T. (1954):
Some doubtful Cretaceous ammonite genera
from japan and Saghalien. Mem. Fac.
Sci., Kyushu Univ., ser. D, Geol., vol. 4,
no. 2, p. 107-134, pis. 7-8.
Y ABE, H. (1903): Cretaceous Cephalopoda
from Hokkaido. part I. Jour. Coll. Sci.,
Imp. Univ. Tokyo, vol. 18, art. 2, p. 1-55,
pis. 1-7.
Y AGI, K. (1968): Petrology of the Alkalic
deposits of the Nemuro peninsula, japan.
Ceol. Soc. Amer. Mem. 115, p. 103-147.
YOKOYAMA, M. (1890): Versteinerung aus
der japanische Kreide. Palaeontographica,
vol. 36, p. 159-202, pis. 18-25.
YOSHIDA, S. (1958): Ammonites occurringcommonly from the Cretaceous of eastern
Hokkaido. Jour. Ceol. Soc. Japan, vol. 64,
p. 206 (in japanese).
- - (1967): Planktonic foraminifera from the
Paleocene Kiritappu Formation and its
biostratigraphic significance. Contributions to Celebrate Prof. Ichiro Hayasaka's
76th Birthday, Kanazawa, p. 85-90.

Akkeshi (J~*),
Chipomanai (9:il:1J~),
Choboshi (~W),
Esashito Cm~A),
Furumugi ("i!l$~),Hamanaka (~*),
Karikan (:h ~ :h :/),
Kiritappu (i¥~;fp),
Monshizu (r~~),Mugi ($~),
Nemuro (tlUiD,
Ochiishi 0&::5),
Oborogawa(M§iJIlf.JlI),
Otamura (:;krnH) ,Ponporoto (9fiJllf.p) ,Poroto (iJIlf.p),
Senposhi({ljlill\~[I:),Soya (*1':t) ,Tokotan (*if-) ,Urakawa (lilifPJ)~tlliJ;iitlRfflli£:O)::{- f~-t7AHO)i'fru'7:/-'1':7"11-:~.lR UUllhffi:.lRffllJ O)tlt~~,JlfiJ'
Gft, 1'rTfiO) 7 :/-'1':7"1 I- O)i£:tI:liJ~*--lfGn -C\"0iJ~, ~u'ilca\li:iJ~t.e\"o ;:: ;::v::'ft~O),*,0) 1 fm~ilcU\li:-t 0 0 ~nftW*'Il1\~,*,UIJ9fiJllf.PO)wmv::.llitl:l-t 0W*~ At 2 (~1 ~:&lf~

11Z1~W?t)iJ'Gi£:Lt.=iJ,t.e I) O)~O)~;;jq::.£-? < >60)-c-, *nX:~lt1JO)mHt Caudryceras varicostatum v AN HOEPEN v::.lrld);}.-t 0 iJ~, nX:iF-lt!lvU.e...., -C >6 l'&~lID 0) !¥f1N&ft'J t.e Vertebrites ~0)~M!iJ~ff~-t0;::'!: -c-~liiii::.12L'i]Ij~n00 LiJ' Uii~M!fl Vertebrites ~-c-f1t.e <, JlI!~
It-Jt.e Caudryceras ~-C-~00 ?HL1::iJ'G, iJ,....,-c:;$:fi~fJiv::. V. aff. kayei .!:I!f-,z,-C-\"t.=;::.!: iJ~~ 0 iJ~, ~nlllE L t.e\' '0 Ammonites kayei FORBES ft Vertebrites I::'~ L, "i t.=lf;i:%~~M!O)tt~ >6, ~ L <~nff:;$:fil1 UU.e 0 0 :;$::filHHI :;$:(c:wft 0'" 7-1- !J t. -T y->Wd:ffll
tl3~Mlv::.i£: L -C\" 0 iJ~, ~O)Jlj;O)1:.ffJWPrJlllA,l~~~ Lt.eftnfit.e Gt.e h<f'l*~&~ • 01I1~&11

76

Tatsuro MATSUMOTO and Saburo YOSHIDA

Explanation of Plate 11
Figs. 1-2. Gaudryceras hamanakense sp. nov ........................................... Page 68
1. Paratype, TKD. 30480, from the type·locality (CoIl. W. HASHIlvIOTO etc.). Lateral (a)and back (b) views of an adult example, xL
2. Paratype, YO. C7615, from the type·locality (CoIl. S. YOSHIDA). Lateral (a) and bad:(b) views, enlarged (x about 1.5) to show the characteristic lirae.
Photos by K. TANABE (1) and S. YOSHIDA (2), without whitening.

MATSUMOTO and YOSHIDA:

Gaudryceras hamanakense

Plate 11

Trans. Proc. Palaeont. Soc. japan, N. S., No. 114, pp. 77-86, pIs. 12, 13, july 15, 1979

703. TRIASSIC BRYOZOANS FROM THE HIDAKA GROUPIN HOKKAIDO, JAPAN*
SUMIO SAKAGAMI. Department of Earth Sciences, Faculty of Science
Chiba University, Chiba, 260

andAKIRA SAKAI
Geology Department, Geological Survey of japan
Kawasaki, 213

Abstract. Five bryozoan species from the Hidaka Group: Leioclema sugiyamai
SAKAGAMI, n. sp., Leioclema sp. indet., Pseudobatostomella kobayashii SAKAGAMI,
Dyscritella hidakaensis SAKAGAMI, n. sp. and Dyscritella sp. indet. are described.
Leioclema sugiyamai, n. sp. and Pseudobatostomella kobayashii which was described
originally from the Upper Triassic Kochigatani Series of the Sakawa basin are
identical with Batostomella (1) and Batostomella? (2), respectively, both of whichwere recorded from the Hidaka Group by SUGIYAMA (1941). Thus the present
bryozoan fauna is concluded to be Late Triassic (most probably early Carnian) inage. It is also supported by the conodont fauna associated with the bryozoans.

from the Oxytoma-Mytilus beds of theUpper Triassic Kochigatani Series distributed in the Sakawa basin, Shikoku
and he mentioned that P. kobayashii isvery close to Batostomella? (2) which
SUGIYAMA (1941) described from the Hidaka Group. At that time, SAKAGAMI
suggested that the three forms of
Ba tostomella recorded by SUGIYAMA may
indicate to be Triassic and they should be
reexamined.
On the other hand, the junior author(AS) engaged in the field survey of theareas of the upper courses of Motourakawa (river) and Kerimai (river) andcollected some bryozoans and conodont
remains from the limestone lenses embedded in the "Schalstein" member. In

Introduction
In 1941, SUGIYAMA reported three formsof Batostomella from some localities ofthe Hidaka Group in Hidaka and Ishikari
Provinces in Hokkaido, and he consideredthat these forms indicate a Permian age.
Subsequently FUKADA (1949), however, on
the evidence of brachiopods from one of
the SUGIYAMA'S bryozoan localities, concluded that the Hidaka Group belongs to
the Triassic rather than the Permian.
One of the authors, SAKAGAMI (1972)
described Pseudobatostomella kobayashii
SAKAGAMI which KOBA YASH! collected* Received Feb. 21, 1979; read jan. 22,
1979, at Fukuoka.

77

78

Sumio SAKAGAMI and Akira SAKAI

the summer of 1976, the senior author(SS) went there under the guidance ofthe junior author and could collect manybryozoan samples.
The present article is the result ofstudy on the bryozoans collected at one
locality in the Motourakawa and two in
the Kerimai rivers.
Outline of geology and fossil localities(by A. SAKAI)The formation containing the bryozoan
bearing limestone lenses distributed inthis area has been hitherto known as the"Schalstein Formation" by TAKEUCHI and
SANBONSUGI (1938), the Kerimaigawa
Formation and/or Shunbetsugawa Formation by HASEGAWA and SAKO (1958), andthe lwashimizu Formation by MATSUSHITA and SUZUKI (1962). SAKAI (1976),
however, proposed that the Naizawa
Formation is most suitable for the given
name, because this formation develops
typically in the Naizawa valley which isone of the tributaries of Motourakawa(river).
The Naizawa Formation belongs to the
Hidaka western diabase belt by SUZUKI(1977) and it can be distinguished fromthe Sorachi Group which is typically
distributed in the Kamuikotan tectonic
belt, because the fossil evidences are
distinctly different from each other. The
Naizawa and surrounded formations arebordered by the Cretaceous Yezo Group
with thrust faults on the west, and by
the Kamui Group with intrusions of theWesternmost Hidaka serpentinite belt on
the east.
The Naizawa Formation consists mainly of basic lava, pillow lava and hyaloclastite, accompanied with chert, limestone, sandstone and mudstone, and inwhich many small network veins ofcalcite, albite, prehnite, etc. are developed.

The modes of occurrence of the bryozoan bearinlS limestones are as follows:
1. Motourakawa (Poronaizawa, tributary of Naizawa river)A small limestone lens cropped out atthe left side of this valley, about 4 m
thick. This limestone is overlain by athin mudstone bed (ca. 5 cm in thickness)and successively by green pillow lava,
and is underlain by green hyaloclastite.
The limestone consists of massive micrite,
pale brownish gray to pale gray in color,
includes small greenish angular hyaloclastitic fragments. The bryozoans occur
in the massive part of the limestone
without hyaloclastitic fragments. In thislimestone, conodont remains identified
withNeogondolella
polygnathifonnis(BUDUROV and STEF ANOV) were found.
2. Kerimai (1) (Nukibetsuzawa, tributary of Kerimai river)A small limestone lens, probably several meters thick, cropped out only at theleft side of the valley, embedded in hyaloclastite bed, pale reddish brown topale brownish gray in color, including
dark reddish brown to green hyaloclastitic fragments in part. The bryozoans occur in the massive part of thelimestone just like at Motourakawa.
3. Kerimai (2) (Oimatezawa, tributaryof Kerimai river)A small limestone lens, consisting of 3
to 4 m thick, cropped out at the rightside of the valley, pale brownish grayto pale gray in color, contains green hyaloclastitic fragments in part. This limestone lens is embedded in hyaloclastite
bed.
Further SAKAI (1976) found someconodont remains, smaller foraminifers,
fish teeth, shark scales, etc. in the limestone lens located at about 4.5 km NNWof the bryozoan locality in Motourakawa(see Text-fig. 1). The conodont fauna
includes Neogondolella polygnathiformis

703. Triassic Bryozoans from the Hidaka G1'O~~P

79§

Ye z o G .

DNa i zawa F .

[IJJ
[XJ

•
A

K amuiG.

Se r p ent i ni te
Br yozoa
Conodontr~

Ca pe Eri ma

o

2

3 KM

Te x t·fig . 1. Geological map showing the localities of br yozoans and conodonts.
1. Motouraka wa , 2. Kerim a i (1) , 3. Kerimai (2) .

(Tex t-fig. 2), N. excelsa, N. navicula,
Enantiognathus ziegleri, etc. and ma y
indicate the late Ladinian to early Carnian of Triassic age.
The tectonic and stratigraphic discussions and the conodont stud y in detailwill be made by S AKAI in the near future.
IGO et al. (1974) recorded the Triassic
conodonts from three loca lities in the

Hidaka Mountains. At one of their lo ca lities situated at northern part ofNishicha (upper course of Horobetsu
river), Ej)igondo lella abneptis and Enantiogna thus ziegleri were found in the
gra yish white chert. This chert member
ma y be included in the Naizawa Formation of the present author but the conodont fauna indicates s lightl y younger

80

Sumio SAKAGAMI and Akira SAKAI
Table 1. The br yozoans from the Hidaka
Group by SUGIYAMA (1941).

~
Forms

a

b

c

d

- - - - - - --Baloslomella (1)B alo slomella? (2)B ato slom ella (3)

0

0
0
0

0

0

a:

the upper course of Kerimai ri ver, Mitsuishi-gun.
b: the upper course of Moto urakawa river,
Mitsuishi-gun.
c: Iwabenosawa (v alle y) of Shimukappu mura, Yufutsu-gun .
d: Fujinosawa (v alley ) of Minamifuranomura, Minami-sorachi -gun.

Text-fig_ 2_ N eogondolella polygnalhiform is(BUD UNOV and STEr-ANOV) from the conodont
local ity in Motourakawa.

horizon than that in the limestone described here.

Bryozoans and their geologic age(by S. SAKAG AMI)
The bryozoans reported by SUGIYAMA(1941) and their localities in the Hidaka
Group are shown in Table l.
Although the author could not reexamine the original specimens of SUGIYAMA (1941) because the depository is
uncertain, from SUGIYAMA'S descriptions
and illustrations, it is clear that there
are two common species between SUGIY AM A'S
and the presen t specimens.
Namely, Batostomella (1) is identical with
Leioclema sugiyamai, n. sp. and Batostomella? (2) is identical with the previousl y described species: Pseudobatostomella lzo bayashii, but Batostomella (3)could not be found in the present collections.
The br yozoans studied here and theirlocalities are shown in Table 2. They
are composed of one known species, 2
new and 2 indeterminable species. Among

Table 2. Loca lities of the bryozoans
in the H idaka Group.

"'Ht;"~
SpeciesI
20'"E 'L:'E"

';:

Q)

Q)

:,c :,c~- - -- - - - - - - - - - " '1- - - - Leioclema sllgiy amai SAKAGAM I,
n. sp . ( = Batostom ella (1) of 0
SUGIYAMA (1941»
Leioclema sp. indet.
P seudob al ostomella Iw bay ashii
SAKAGAMI (1972)o(= B al os/o mella? (2) of
SUG IYA MA (1941»
Dysc r ilella hidakaensis
SAI< AGA MI, n. sp.
Dy scri tella? sp. indet.
o

0

o
0

o
0

them, the known species: Pseudobatostomella lzobay ashii SAKAGAMI was origin ally described from the lower Carnian(Upper Triassic) of the Sakawa basin as
alread y mentioned. L eioclema sugiyamai,n. sp. is ' nearest to L eioclema abnonne
MOROZOVA which was described from theCarnian of the north western part of
Caucasus and Dyscl-itella hidakaensis, n.
sp. differs from th e previously described
species of the genus. In these circum-

703.

Triassic Bryozoans from the Hidaka Groupstances, the present bryozoan fauna isconsidered to be most probably early
Carnian of Late Triassic in age.
As already mentioned by SAKAGAMI(1972), the bryozoan remains are extremely rare in the Triassic System of
the world, and he recognized only 32
species of the Triassic bryozoans by thattime. After that, YANG and HSIA (1975)
described and illustrated five species of
the genus Paralioclema from the Everest
regions. They are Paralioclema multus
YANG et HSIA, P. paucus Y. et H., P.
pilula Y. et H., P. lioclemafonnis Y. et H.
and P. tulungense Y. et H., which occurredfrom the upper part of the Ti1lung Formation (Triassic) except for the last one
from the middle part of the Ti1lung.
The genus Paralioclema was establishedby MOROZOVA (1960), but it may be ajunior synonym of the genus Leioclema
ULRICH.
Further BIZZARINI and BRAGA (1976,1978) reported and described some Triassic cyclostomatous bryozoans from theS. Cassiano Formation (Upper Triassic)of the Dolomites (Eastern Alps), northern
Italy. They consist of seven species inall: "Ceriopora" gnemidium (KLIPSTEIN),"C". montisspeciei BIZZARINI et BLAGA (n.
sp.), "C". sp. 1, "C". sp, 2, Seelandia annosciai B. et B. (n. gen. and n. sp.), S.
lagaaiji B. et B. (n. gen. and n. sp.) andCassianopora giulinii B. et B. (n. gen. andn. sp.), but the newly established two
genera were described as "Incertae sedis"
in Cyclostomata.
Depositories: The specimens treatedin the present article are registered andpreserved in the Collections of Department of Earth Sciences, Faculty of
Science, Chiba University (DESC).
The holotype and para types of Pseudobatostomella kobayashii SAKAGAMI which
SAKAGAMI (1972) described and illustrated
from the Sakawa basin are also registered81

and preserved in the Collections of DESC
from the Ehime University Collections(EEG) as follows:
EEG-1001 (holotype) - DESC-79001
EEG-1002 (para type) - DESC-79002
EEG-1003 (paratype) - DESC-79003
EEG-1004 (para type) - DESC-79004
EEG-1005 (paratype) - DESC-79005
EEG-1006 (paratype) - DESC-79006
Systematic description of
Ectoprocta (Bryozoa)(by S. SAKAGAMI)
Genus Leioclema ULRICH, 1882
Leioclema sugiyamai SAKAGAMI, n. sp.
PI. 12, Figs. 1-5.
1941. Batostomella (1) SUGIYAMA, pp. 190,191,
figs. 1-3.

Zoarium ramose, probably attached toforeign substance such as brachiopod
shell, its diameter ranging from 2 mm to
5mm.
In longitudinal section, zooecial tubes
trend parallel to longitudinal directionof zoarium in immature region, curved
gradually outward and making a rightangle with surface. Zooecial wall thickened gradually from immature to mature
regions and the boundary between these
two regions indistinct. Diaphragms occur
abundantly in zooecia and mesoecia,
spaced at intervals of usually about
0.100 mm in average, ranging from 0.040
to 0.150 mm, very thin, complete andnearly straight or slightly concave.
In tangential section, zooecial tubes
rather small, circular to subcircular, theshorter diameter ranging from 0.095 to
0.125 mm, longer diameter ranging from0.125 to 0.156 mm, irregularly arranged
but usually 7 zooecia in 2 mm length of
longitudinal direction. Mesoecia circular

82

Sumio SAKAGAMI and Akira SAKAI

PI. 12, Fig. 8.

In longitudinal section, zooecial tubes
trend parallel to longitudinal direction of
zoarium in immature region, curved
gradually outward and making nearly aright angle with surface. Zooecial wallthin in immature region and becoming
gradually thick to mature region. Usually
only one diaphragm disposed at nearlyproximal part of mature zone of zooecial
tube, thin, complete and nearly straight.
Diaphragms in mesoecia seem to be more
numerous, spaced at intervals of lessthan 0.010 mm.
In tangential section, zooecial tubes
circular or subcircular, the shorter diameter 0.100 to 0.125 mm, longer 0.125 to0.150 mm. Mesoecia numerous, trigonalor quadrate with rounded corners, usually
0.025 to 0.050 mm in diameter. Acanthoecia present but not so prominent,
surrounded by dark colored concentric
fibrous tissue, the outside diameter usuallyless than 0.050 mm and inner about 0.006
mm, usually disposed at each point ofintersection of zooecial tubes.
Remarks:- The present form can beeasily distinguished from Leioclema sugiyamai, n. sp. by the smaller zoarium,
fewer number of diaphragms in zooecial
tube, less developed acanthoecia and otheressential characters. The present form
is not unlike to Paralioclema fonnosum
MOROZOVA (1969) which was describedfrom the Norian of the northwestern partof Caucasus but is not identical. Becauseof only two oblique sections at hand,the detailed comparison with the previously described species of the genus
and the specific decision are deferred
until more specimens accumulate.
Occurrence :-Rare in Kerimai (1).
Specimen No.: - DESC-79012a and
DESC-79010.

Zoariumprobably ramose, about 1.5 to
2 mm in diameter.

Genus Pseudobatostomella
MOROZOV A; 1960

to subcircular, ranging from 0.045 to
0.095 mm in diameter. Acanthoecia also
well developed, usually 4 to 5, occasionally 6 surrounding each zooecial tube,
surrounded by concentric fibrous dark
dense tissue, segregated from zooecial
wall material, the outside diameter ranging from 0.040 to 0.070 mm and inside
diameter ranging from 0.010 to 0.015 mm.
Remarks:-The present species coincides with Batostomella (1) which SUGIYAMA (1941) described and illustrated
from four localities in the Hidaka Groupof Hokkaido. SUGIYAMA stated that
"Diaphragms irregular in density, butrare, .... ". However, the careful observation of the present specimens madeclear that many diaphragms are regularly
arranged, but in some cases, some diaphragms had fallen off because they arevery thin and fragile.
The present species seems to be nearest
to Paralioclema abnorme which MOROZOVA(1969) described from the Carnian of thenort·hwestern part of Caucasus, but thepresent species differs from that in thesmaller zooecial diameter and the modeof curvature of zooecial tubes fromimmature to mature regions.
The specific name, sugiyamai is dedi-.
cated to .the late Dr. Toshio SUGIYAMA
who introduced originally the occurrenceof bryozoans including the present speCies
from the HidakaGroup.
Occurrence: - Very abundan t in the
Kerimai (2) and rare in Motourakawa.
SPecimen No. :-DESC-79018 (holotype),
DESC-79019, DESC-79020 (Kerimai (2));
DESC-79009a (Motourakawa).
Leioclema sp. indet.

703.

Triassic Bryozoans from the Hidaka Group

Pseudobatostomella kobayashii SAKAGAMI
PI. 12, Figs. 6,7; PI. 13, Figs. 1, 2.
Batostomella? (2) SUGIYAMA, p. 191,
figs. 4, 5.
1972. Pseudobatostomella kobayashii SA"AGA~'",
pp. 275-277, pI. 33, figs. 1-6.
1941.

Zoarium ramose, usually about 4 to 5
mm in diameter.
In longitudinal section, zooecial tubes
trend parallel to longitudinal directionof zoarium in immature region, curve
gradually outward at posterior end of
mature tube, then straighten in mature
region and making large angle with surface. Zooecial wall very thin in immature region and gradually thickened
to mature region. Usually 2 to 3 verythin diaphragms usually disposed at intervals of 0.6 to 1.0 mm, but in somecases, disposed more densely.
In tangential section, zooecial tubes
subangularly oval, their shorter diameter
usually ranging from 0.150 to 0.185 mm
and longer diameter ranging from 0.185
to 0.250 mm. Mesoecia rare, usually circular, their diameter ranging from 0.050
to 0.100 mm. Acanthoecia well developed,
usually 5 to 6 surrounding each zooecial
tube, surrounded by concentric fibrous
tissue, outside diameter usually 0.040 to
0.080 mm, and inner diameter very small,less than 0.005 mm.
Remarks:- The present form agrees
with Pseudobatostomella kobayashii, which
SAKAGAMI (1972) described from the
Oxytoma-Mytilus beds (lower Carnian) of
the Sakawa basin, Shikoku of Japan, in
all of the essential characters. The
preservation is better than the typespecimens from the Sakawa. At thattime, SAKAGAMI (1972) pointed out that
Pseudobatostomella Iwbayashii resembles
Batostomella? (2) which SUGIYAMA (194l)
described in association with two other83

forms of Batostomella from the uppercourse of Motourakawa.
One of thelocality of the present form may be thesame with the SUGIYAMA'S B.? (2) locality, and the present form undoubtedly
coincides with Batostomella? (2).
Although, in SUGIYAMA'S description,
it was stated that the diaphragm is probably absent, his photographic illustrations show that there are two diaphragms
in a zooecial tube. Unfortunately I could
not reexamine SUGIYAMA'S bryozoan
specimens, but I am of the opinion that
Batostomella? (2) should be included in
the Pseudobatostomella Iwbayashii.
Occurrence:- Very abundant in Motourakawa and rare in Kerimai (1).
SPecimen No.: - DESC-79007, DESC79008,
DESC-79009b(Motourakawa);
DESC-79014 (Kerimai (1».
Genus Dyscritella GIIny, 1911
Dyscritella hidakaensis SAKAGAMI, n.sp.
PI. 13, Figs. 3-5.

Zoarium ramose, its diameter about
5.5mm.
In longitudinal section, zooecial tubes
trend parallel to longitudinal directionof zoarium, nearly straight but slightly
curved outward and making a large angle
with surface. Zooecial wall relatively
thick in immature region and thickened
gradually to mature region. Diaphragmlacking in almost of zooecial tubes but
in one case, one complete diaphragm canbe observed at the proximal part ofmature region of zObecial tube.
In tangential section, zooecial tube irregularly formed, amoeba like shaped in
extreme cases, the diameter measured
about 0.180 to 0.250 mm. Mesoecia probablyabsent. Acanthoecia well developed, surrounded by concentric fibrous tissue, less than 0.015 mm in inner diameter,

84

Sumio SAKAGAMI and Akira SAKAI

irregularly arranged in wall, usually 5
to 6 disposed at wall margin where
zooecial tube angularly shaped.
Remarks :-Only one species of thegenus Dyscritella has been hitherto known
from the Triassic in the world. It is
Dyscritella agischevi which NEKHOROSHEV(1949) described from the Norian of theKolyma river basin, Siberia, USSR. The
present form can be distinguished fromD. agischevi in many respects, especiallyby the peculiar form of zooecial tube in
the tangential section, which is the mostconspicuous character of the present new
species.
Occurrence :-Rare in Kerimai (1).
SPecimen No. :-DESC-79013 (holotype)
and DESC-79012b.

0.150 mm in shorter diameter. Mesoecia
small and very rare, less than 0.050 mm
in diameter. Acanthoecia well developed,
irregularly arranged in wall, surroundedby concentric fibrous tissue, the outside
diameter ranging from 0.030 to 0.045 mm,
inner diameter very small and not measurable.
Remarks:-The present form apparently
differs from the previously described
species: D. agischevi and D. hidakaensis,
n. sp. However, the specific denomination must be reserved, because only a
few oblique sections at hand are too poor
for specific identification.
Occurrence :-Rare in Motourakawa andKerimai (1).
SPecimen No.:- DESC-79010, DESC79011, DESC-79015 and DESC-79017.

Dyscritella sp. indet.

References

PI. 13, Fig. 6.

Zoarium ramose, about 2 mm III diameter.
Zooecial tubes trend parallel to longitudinal direction of zoarium in immature
region, curved gradually outward andmaking a large angle with surface.
Zooecial wall gradually thickened fromimmature to mature regions. Diaphragmlacking. Zooecial tubes oval, 0.100 to·

BIZZARINI, F. and BRAGA, G. (1976): I Briozoi
del Trias superiore (Formazione di S.
Cassia no) dell'alpe di Specie (prov. diBolzano) (Nota preliminare). Atti. e Mem.
Acc. Patavina Sc. Lett. Arti, vol. 88, pt.
II, cl. Sc. mat. e nat., p. 55-68.
- - and - - (1978): Upper Triassic newgenera and species of fair and questionable Bryozoa and Chaetetida from the S.
Cassiano Formation of the Dolomites(Eastern Alps).
Bull. Soc. Pa/eont.

Explanation of Plate 12
Figs. 1-5. Leioclema sugiyamai SAKAGAMI, n. sp.
1. Obliquely but nearly longitudinal section, holotype (No. DESC-79018), x 20, Loc.:
Kerimai (2), 2. Tangential section, paratype (No. DESC-79009a), x 20, Loc.: Motourakawa,
3, 4. Enlarged longitudinal and tangential parts of Fig. 1, respectively, x 60, 5. Enlarged
part of another section, paratype (No. DESC-79020), showing the well developed acanthoecia, x 60, Loc.: Kerimai (2).
Figs. 6, 7. Pseudobatostomella kobayashii SAKAGAMI
6. Transverse section (No. DESC-79008), x 20, Lac.: Motourakawa, 7. Longitudinal section(No. DESC-79014), x 20, Loc.: Kerimai (1).
Fig. 8. Leioclema sp. indet.
Oblique section (No. DESC-79016), x 20, Lac.: Kerimai (1).

S AKACAMI

and SAKAI:

Hidaka bryozoans

Plate 12

703.

Triassic Bryozoans from the Hidaka Group

Italiana, vol. 17, (1), p. 28-48, pis. 1-7.
FUKADA, A. (1948): On the Brachiopoda fromthe "Schalstein Formation" in the Central
mountain range of Hokkaido. (abstract),
Jour. Ceo!. Soc. Japan, vol. 55, (648-649),
p. 123, 124.
HASEGAWA, K. and SAKO, S. (1958): Thegeological sheet map "Kamuidake", scale
1 : 50,000, and its explanatory text. Hokkaidl) Development Agency, 53 pp.
IGo, Hy., KOIKE, T., IGO, Hh. and KINOSIlITA,
T. (1974): On the occurrence of Triassic
conodonts from the Sorachi Group in the
Hidaka Mountains, Hokkaido. Jour. Ceol.
Soc. Japan, vol. 80, (3), p. 135, 136.
MATSUSHITA, K. and SUZUKI, M. (1962): Thegeological sheet map "Noya", scale
1 : 50,000, and its explanatory text. Hokkaido Development Agency, 38 pp.
MOROZ OVA, I. P. (1960): Devonskie mshanki
Minskikh i Kuznetzkoi Kotlovin. Trudy
Paleont. Inst., Akad. Nauk SSSR., vol.
86, p. 1-172, pis. 1-34.
- - (1969): a sistematicheskom sostave irasprostranenii mshanok v triase. Akad.
Nauk SSSR., Pa!eont. Zhy. (2), p. 49-57,
pis. 7, 8.
NEKHOROSHEV, V. P. (1949) : Pervaja nakhodka

85

triasovykh mshanok v. SSSR. Dokl. Akad.
Nauk SSSR. (N. 5.), vol. 66, (3), p. 459461.
SAKAGA!vIl, S. (1972): The Triassic Bryozoa
from Kusaka, Sakawa basin, Shikoku,
Japan. Trans. Proc. Palaeont. Soc. Japan,
N.S., (85), p. 275-279, pI. 33.
SAKAI, A. (1976): The Hidaka Supergroupin the Motourakawa river area, Hokkaido.
Preprint for 83th Ann. lvleeting, Ceo!.
Soc. Japan, p. 39.
SUGIY A!vIA, T. (1941): On the geological ageof the limestone containing Bryozoa inthe Hidaka Group. Jour. Ceo!. Soc. Japan,
vol. 48, (571), p. 189-194.
SUZUKI, M. (1977): Characteristics of diabaseand spilitic rocks in the axial region of
Hokkaido and genesis of spilite. Rep. Ceo!.
Surv. Hokkaido, (49), p. 1-39.
TAKEUCHI, K. and SA:'iBO~SUGI, M. (1938) : Thegeological sheet map "U rakawa", scale
1: 100,000, and its explanatory text. Hokkaido Indus!. Res. Inst., 23 pp.
Y A~G, K. C. and HSIA, F. S. (1975): Bryozoan
fossils of the Everest regions. Sci. Rep.
Everest Regions, 1966-1968, Palaeontology(1), p. 39-57, pis. 1-8.

Fujinosawa &\"±O)iR,
Hidaka BiWi,
Horobetsu ~5JIJ,
Ishikari 151~,
Iwabenosawa -{ '7 -'"'O)iR,
Iwashimizu !fiiJ!f7Jc,
Kamui tlPmlG,
Kamuikotan fIlIJi5i1il\'l,Kerimai ~~,Kochigatani fiiIP3?":fr,
Maikawa ~lll,
Minamifurano-mura m1:l~!J!ftt,Minamisorachi-gun m~~ll1l,
Mitsuishi-gun ::'::15i$,
Motourakawa :7Clrlilll,
Naizawa -r -{ iR,
Nishicha f!!i~,Nukibetsuzawa 1t~~IJiR,
Oimatezawa-< TiR,
Poronaizawa ;t; p -r -{ iR,
Sakawa {teJlI,
Shimukappu-mura r:!:iJaH,
Shunbetsugawa
1"j5JIJJII,
Sorachi ~*n,Yezo AAE/&,
Yufutsu-gun YJ1Lll1l,
Tulung (Chinese) ±Jli

* -{;ltWJ:g:B i%I\l'iMi£O)::.::i1:$c,: ft£l;!,ft,15: B tfJ~Mi£O).: ft£l;!,ft,155frJL Leioclema sugiyamai
SAKAGAMI, n. sp., Leioclema sp. indet., Pseudobatostomella kobayashii SAKAGA1'dl,
Dyscritella hidakaensis SAKAGA~II, n. sp., Dyscritella sp. indet. ~licjlllt Lt..::o Leioclema
sugiyamai, n. sp. c {telll itJl.gO) J::ffil::.::i1:*Mr"J?" :fr$IEb' I?,*~cjfjl(; ~ h t..:: Pseudobatostomella
kobayashii f:t.~W (1941) b~ B ~IiilMb' 1?$IH1r Lt..:: Batostomella sp. (l)Batostomella?
sp. (2) i:.-th-FhJRJ~~;h.oo ':O)J: 5t.c@.)ab'l?, .: ·1o.I:.*11r-t.o.:ft£l;!,!ffb!ffoMO):it!!.'f{If.¥c~d::.::.e.M~I?<~-~7~~MM) ~~.ocM.~;h.oo ,:O),:cd~i£-t.o~/r~~D~MKJ:~~t~M~h.oo~J::~~ ••*•86

S~~mio SAKAGAMI and Akira SAKAI

Explanation of Plate 13
Figs. 1, 2. Pseudobatostomella kobayashii SAKAGAMI
1. Longitudinal section (No. DESC-79007), x 20, 2. Tangential section (No. 79009b), x 60,
Loc.: Motourakawa.
Figs. 3-5. Dyscritella hidalwensis SAKAGAMI, n. sp.
3. Tangential section, paratype (No. DESC-79013), 4. Typical longitudinalsec'tion, holotype(No. DESC-79012b), x 20, Loc.: Kerimai (1), 5. Enlarged part of Fig. 3, showing thezooecial shapes, x 60.
Fig. 6. Dyscritella sp. indet.
Oblique section (No. DESC-79015), x 20, Loc.: Kerimai (1),

SAKAGAMI and SAKAI:

Hidaka bryozoans

Plate 13

Trans. Proc. Palaeont. Soc. japan, N. S., No. 114, pp. 87-96, pIs. 14, 15, july 15, 1979

704. EARL Y CRETACEOUS PLANTS FROM THE TOKURAZA W A
FORMATION, GUMMA PREFECTURE, IN THE INNERZONE OF NORTHEAST JAPAN*
T ATSUAKI KIMURATokyo Gakugei Uni versi ty, Koganei, Tokyo 184

SHIGERU SAITO
Yokohama-Minami Senior High School, Yokohama 233

and
TAKAO TOjO
Kamo junior High School, Ichikawa 290

Abstract: A small early Cretaceous flora is reported from the Tokurazawa
Formation. The locality is located in Northeast japan, about 120 km east of the
Itoigawa-Shizuoka Geotectonic Line. The flora includes several species characteristicof the Inner Zone 'Tetori'-type flora and no species characteristic of the Outer
Zone 'Ryoseki'-type flora except Onychiopsis elongata. The evidence from thepresent flora agrees with that from the fauna of the Tokurazawa Formation.
We describe here the following fossil plants from the upper part of the Tokurazawa Formation: Asplenium dicksonianum, Adiantopteris sewardii, Cladophlebis sp.
A, C. sp. B, Sphenopteris sp., Onychiopsis elongata, Cff. Czekanowsfcia nipponica,
Leptostrobus sp. and Podozamites dr. lanceolatus.

mura, Tone-gun, Gumma Prefecture, along
the upper course of the Katashina River(Text-fig. 1). It has been studied or reviewed by KAWADA (1955), MURA YAMA
and KA W ADA (1956), HA YASHI et ai. (1965),
Toy A et ai. (1965), SUDO (1976) and CHIHARA et ai. (1977).
According to Toy A et ai. (1965), theTokurazawa Formation is lithologicallydivisible into three members as shownin Table 1. In this paper, we adopt thename of Tokurazawa Formation as defined by HAY AMA et ai. (1969), instead ofIntroductory remarks
This paper deals with the descriptionof a fossil flora newly found from theTokurazawa Formation with reference toits significance for the Cretaceous paleogeography.
The Tokurazawa Formation (HA YAMA
et aI., 1969), surrounded by basic igneousrocks, is narrowly distributed - in thenortheastern part of Tokura, Katashina* Received Nov. 20, 1978; read September
23, 1975 at Kanazawa.

87Tatsuaki KIMURA, Shigeru SAITO and Takao TOjO

88•

Exposures of theTetor; Supergroup

Table 1. Brief stratigraphy of the
Tokurazawa Formation(after Toy A et aI., 1965)
Upper member; consisting of alternation ofcross-laminated sandstone and shale(300 m thick); yielding abundant Corbicula tetoriensis KOBAY ASH! and St;ZUKI
Middle member; consisting of arkose andleucocratic sandstone with subordinate
conglomeratic layers (200 m thick)Lower member; consisting of alternation ofsandstone and shale, and massive blackshale (30 m thick) ; yielding belemnites(Fossil plants here described are found fromthe Upper member)Outer Zone of Southwest Japan

Text-fig. 1. Location of the Tokurazawa
Formation (pointed by arrow), the distributionof the Tetori Supergroup in the Inner Zone ofSouthwest Japan (with reference to MAEDA'S
figure), and the major geological provinces
and geotectonic lines of Japan.

Text-fig. 2.

the Tokura Formation proposed by MuRAYAMA and KAWADA (1956), because thename 'Tokura' was previously used for
the Tertiary volcanic rocks near Tokura(KUNO et aI., 1954).
The Tokurazawa Formation is intrudedby the Tokura Basic Rocks and is cov-

Distribution of the Tokurazawa Formation and associated geological units.

704.

Early Cretaceous plants from the Tohwazawa Formation

ered by the volcanic rocks, and its lowest
and uppermost parts are concealed.
During the period from 1975 to 1977,
SAITO and TOlO worked vigorously collecting fossil plants from the Tokurazawa
Formation and obtained some 250 specimens from the upper member exposed
along the Tokurazawa and the Urushizawa valleys. Text-fig. 2 gives thegeneral geology of this area by SAITO
and TOlO with the fossil plant localities,
and Text-fig. 1 shows the fossil locality
in relation to the major geological provinces of japan.
Tokurazawa Flora and its geologicalsignificanceA large number of fossil plants occur
in the upper member of the Tokuzawa
Formation. In this horizon the flora isuniform in composition. The rocks weremetamorphosed by the intrusion of igneous rocks, and the cuticles were destroyed. The plant fossils are preserved
as impressions, showing macroscopic
features only.
The following genera and species havebeen recognized in our collection andthis assemblage is here called Tokurazawa Flora:
Ferns; Asplenium dicksonianum HEER,
Adiantopteris sewardii (Y ABE) V ASSILEVSKAlA, Cladophlebis sp. A, C. sp.
B, Sphenopteris sp. and Onychiopsis
elongata (GEYLER) YOKOYAMA.
Czekanowskiales; Cfr. Czekanowskia
nipponica KIMURA and OHANA and
Leptostrobus sp.
Conifer; Podozamites efr. lanceolatus(LINDLEY and HUTTON) BRAUN.
Although the flora is small, it includes
species or genera characteristic of the
Inner Zone floras of 'Tetori' -type inSouthwest japan, while it lacks species
characteristic of the Outer Zone florasof the same age. Such elements of the89'Tetori' -type floras as Dicksoniaceae andGinkgo leaves have not been observed.
The following species are regarded as
the elements of Inner Zone floras.
1) Asplenium dichsonianum and its allied
forms have been known in the early
Neocomian Oguchi Flora (KIMURA and
SEKIDO, MS), the late Neocomian Akaiwa Flora (KIMURA and SEKIDO, 1976,1978) and the Aptian Tamodani Flora(KIMURA and HORIUCHI, 1979), allfrom the Inner Zone of Southwest
japan, as well as in the early Cretaceous floras in East Siberia. But theyha ve not been found in the coeval
floras from the Outer Zone of japan.
2) Adiantopteris sewardii is also abundant in the Oguchi (OISHI, 1940) andthe Akaiwa (KIMURA and SEKIDO,
1978) Floras. It occurs also in the early
Cretaceous Nagdong Flora (Y ABE,
1905; OISHI, 1940) and the jurassoCretaceous flora from Mongolia(jAHNICHEN and KAHLERT, 1972). But
it has not been found in the coeval
floras from the Outer Zone of japan.
3) Czekanowskians are common to thefloras from the Tetori Supergroupand the coeval floras from East Siberia and NE-China, but they have notbeen found among the coeval floras
from the Outer Zone of japan.
4) Podozamites leaves are also common
to the floras from the Tetori Supergroup and the coeval floras from East
Siberia and NE-China, but they havenot been found in the coeval floras
from the Outer Zone of japan, except
for some doubtful records.
In a flora of Outer Zone type in thisage, the following species might be expected; Matoniaceous ferns, Zamites
buchianus, Ptilophyilum ex gr. pecten, Nilssonia ex gr. schaumburgensis, Nageiopsis
spp. and Cupressinocladus sp. These
species are not found in the present col-

90

Tatsuaki KIMURA, Shigeru SAITO and Takao TOjo

lection from the Tokurazawa Formation.
JUdging from the species composition,
the Tokurazawa Flora may correspondin age to either of the Oguchi, the Akaiwa and the Tamodani Floras in the
Itoshiro Group of the Tetori Supergroup.
This agrees with the view mentioned by
HA YASHI et al. (1965) that the Tokurazawa Formation corresponds in age tothe Itoshiro Group, based on the abundantoccurrence of Corbicula tetoriensis, abrackish or fresh-water bivalve in thesestrata.
During the late jurassic-early Cretaceous, the floral composition differs considerably between the Inner and Outer Zonesof Southwest japan (KIMURA, 1975a, b,
1976; KIMURA and HIRATA, 1975; KIMURA and ASAMA, 1975). The Outer Zone
floras in those days are of North European
Wealden-type, and this zone is includedin the VAKHRAMEEV'S Indo-European
Palaeofloristic Area. While the coeval
floras from the Inner Zone of Southwest
japan, called the 'Tetori' -type floras, aresimilar in composition to those of the
VAKHRAMEEV'S Siberian Palaeofloristic
Area, possibly representing its marginal
facies.
Acknowledgements
We first express our sincere gratitudes
to Professor Emeritus Thomas M. HARRIS,
F. R. S. of the University of Reading forhis very helpful suggestions in palaeobotany and his critical reading of thepresent manuscript.
We also thank Miss Tamiko OHANA, agraduate student of the Tokyo Gakugei
University for her kind help in drawing
the figures in this paper. We are muchindebted to the Oze Ringyo Co. Ltd. forpermitting us to collect the fossil plants
herein described in the company-owned
land. This study was supported in partby the Scientific Research Fund from the
Ministry of Education, japan (no. 354290'78).
Systematic description
Filicales
Genus Asplenium LINNE
Asplenium dicksonianum HEER
PI. 14, fig. 1: PI. 15, fig. 1.
Text-fig. 3 (1)Asplenium dicksonianum HEER: 1874, p. 31,
pI. 1, figs. 1-5 (Lower Cretaceous ofGreenland) ; KIMURA and HORIUCHI 1979,
p. 10, pI. 1, fig. 6; text-figs. 5a, b (Chinaboradani Formation, Fukui Prefecture).
Asplenium dr. dicksonianum HEER; KIMURA
and SEKIDO: 1976, p. 353, text-fig. 11(Osugidani, Akaiwa Formation); 1978, p.
260 (Oi tto) .
For further references, see KRYSHTOFOVICH
and BAIKOVSKAJA, 1960, p. 1l.

Description: Several specimens wereobtained. PI. 14, fig. 1 shows a delicate
penultimate pinna fragment. Ultimate
pinnae are set rather remotely, 1 cm distant, and at an angle of 45 degrees tothe axis with a distinct median furrow.
Pinnules are anadromic in order, and are
as a whole elongate-rhomboidal in form,
1.8 cm long and 5 mm wide at the widest
portion. Their apical halves are usually
deeply dissected into 1-3 pairs of narrow
lobes. Each lobe is directed forward andits apex is acutely pointed or sometimes
shallowly serrated. Nerves are delicate
and Sphenopteris-type, secondaries fork
twice or thrice. Each lobe receives a setof secondary nerves. PI. 15, fig. 1 andText-fig. 3(1) show the venation. (Fructification has not been known).
Remarks: Although our specimens are
all incomplete, they are referable ingeneral form to Asplenium dicksonianum

704.

Early Cretaceous plants from the Tokurazawa Formation

widely known from the younger Mesozoic
plant-beds in the Northern Hemisphere.
Our specimens closely resemble someof the figures of this species but otherfigures differ and the leaf is evidently
rather variable. However it seems constant and characteristic that the orderof branching of the pinnules is anadromic.
ENDO'S specimens regarded by him(1925) as Asplenium dicksonianum (?) fromthe Upper Cretaceous of Hokkaido, japan,
though very small pinna fragments, aresimilar in form to ours. Asplenium cfr.
dicksonianum described by KIMURA and
SEKIDO (1976) from the Osugidani vallyof the Akaiwa Formation, is now referable to A. dicksonianum.
Occurrence: Common.
SPecimens: TK -063, 069, 075, 092, 103.
Genus Adiantopteris V ASSILEVSKAJA,
1968: 49
Adiantopteris sewardii (Y ABE)

VASSILEVSKAJA
PI. 14, figs. 2-4; PI. 15, fig. 2; Text-fig. 3(2-4)
For further references, see KIMURA and SEKIDO, 1978, p. 265-266.

Remarks: Many pinna fragments wereobtained. They are all referable to
Adiantopteris sewardii originally described by YABE as Adiantites sewardi(1905) from the Lower Cretaceous ofjapan and Korea. This species is common to the Oguchi and Akaiwa Floras.
Occurrence: Very abundant.
SPecimens: TK -015, 020, 043, 053, 059,
088, 203 and many others.

Form-genus Cladophlebis BRONGNIART,
1849: 105
Cladophlebis sp. A
Text-fig. 3 (5)91Several pinna fragments were obtained,
one of which is shown in Text-fig. 3 (5).
Pinnules are of Pecopteris-type, triangularor finger-shaped, small-sized, with entire
margin, ending with the obtusely pointed
apex, and attached to the axis at a wide
angle. Nerves are invisible.
The present specimens resemble thesterile pinnae of Gleichenites nipponensis
OISHI known from the Lower Cretaceousof the Inner Zone of japan and of Lotzu-kou, NE-China.
Occurrence: Rather rare.
Specimens: TK-097, 101.
Cladophlebis sp. B
PI. 14, fig. 5; Text-fig. 3(6)A single pinna fragment shown in PI.
14, fig. 5 was obtaind. Pinnules are set
closely, small-sized, triangular in form,
with entire margin, ending with theobtusely pointed apex, 0.5 cm long and2.5 mm wide at the base, and attached bytheir whole base to the pinna axis at awide angle. Midnerve is persisting to
the tip and sending off 5 pairs of secondaries which fork once in the manner asshown in Text-fig. 3 (6).
The present pinnules resemble thoseof Cladophlebis ex gr. denticulata or apicalpinnules of C. ex gr. williamsonii both ofwhich are common to the Oguchi and the
Akaiwa Floras.
The name Cladophlebis ex gr. denticulata
is comprehensively used by workers injapan. Specimens reported as Cladophlebis
ex gr. denticulata from the Lower Cretaceous plant beds in the Outer Zone ofSouthwest japan are regarded as rather different in general form from thosefrom the coeval plant beds in the Inner
Zone of japan, as mentioned by KIMURA
and KANsHA (1978, p. 111).
Occurrence: Rare.

92

Tatsuaki KIMURA, Shi geTu SAITO and Takao TOjO

1

6 ~I

2

10 «!J':'
0,-,_ _~_~? em

11

Text-fig _ 3. 1. Asplenium dicksonianum HEER; a penultimate pinna fragment,
drawn from the specimen shown in PI. 14, fig. 1 (TK - 103) , 2- 4. A dian lopleris
sewardii (Y ABE) VASS ILE VSKA JA ; a ll pinna fragments, 2; TK - 01S, 3; drawn f rom
PI. 14, fig, 2 (TK- OS9) , 4; TK - OS3 , S. Cladophlebis sp. A; TK - 101. 6. Cl adophlebis
sp. B; drawn from PI. 14, fig, S (TK- 197) , 7, Sj)henopte7'is sp,; drawn from PI. IS,
fig , 3 (TK- 168) . 8. Onychiopsis elongala (GEYLER) YOKOYAMA ; showing fertile
pinnules (sori?) on the left side of pinna axis and ster il e one on the right, drawn
from PI. IS, fig. 6 (TK- 167) . 9, efr. Czekanowslzia nipponica KI MURA and Ol-IANA ;drawn partl y from PI. IS, fig. 8, showing two branching leav es w ith a single ve inon each lamina (TK- 1S2) . 10. L eploslro bus sp, ; a n incompletely preserved va lve,
drawn from PI. 14, fig, 8 (TK- 17S), 11. Podo zamites cfr. lanceolatus (LI NDL EY andH UTTON) BRAUN; drawn from PI. 14, fig. 7 (TK- 229),

Specimen: TK-197.
Form-genus Sphenopteris (BRONGNIART)STERNBERG, 1825: 15

Sphenopteris sp.
PI. 14, fig, 6; PI. IS , fig, 3; Text,fig, 3(7)Several pinna fragments as shown in
PI. 14, fig. 6 and PI. 15, fig. 3 were obtain-ed, Pinnae are delicate. Pinnules are set
closel y, elongate-oblong in form , anddirected forwards but often bending outwa rd . Laminae are shallowly divided
into four lobes directed forward, Midnerve is sinuous, of Sphenopteris-t ype,and sending off four pairs of simple
secondaries.
Each lobe receives one
secondary nerve in the manner as shownin Text-fig. 3 (7).

704.

Early Cretaceous plants from the Tokurazawa Formation

The present pinnules differ in form
from those of Onychiopsis elongata known
abundantly from the Upper Jurassic to
the Lower Cretaceous plant beds in Japan,
and also differ in venation from those of
Asplenium dicksonianum described here.
Occurrence: Rare.
Specimens: TK-ll0, 168.
Genus Onychiopsis YOKOYAMA, 1889: 26
Onychiopsis elongata (GEYLER)YOKOYAMA
PI. 15, figs. 4-7; Text-fig. 3(8)Thyrsopteris eiongata GEYLER; 1877, p. 224,
pI. 30, fig. 5; pI. 31, figs. 4-5 (Kuwashima,
Oguchi Formation).
For further references, see KIMURA, 1975a,
p. 77.

Many specimens referable to this wellknown species were obtained. PI. 15, figs.
4-5 show sterile leaf-fragments and figs.
6-7 fertile pinna fragments, a part ofwhich is shown in Text-fig. 3 (8). Unfortunately the details of the fructification
are not recognizable because of the poor
state of preservation.
Occurrence: Very abundant.
Specimens: TK-018, 021, 049, 055, 078,
083, 107, 112, 114, 129, 137, 167 and manyothers.
Czekanowskiales
Genus Czekanowskia HEER, em. HARRIS
and MILLER, 1974: 92
Cfr. Czekanowskia nipponica KIMURA
and OHANA
PI. 15, fig. 8; Text·fig. 3 (9)Comparable specimens:Czekanowskia nipponica KIMURA and OHANA;

93

1978, p.595, figs. 1-12 (Upper Cretaceous
Omichidani Formation, Ishikawa Prefecture).

Description: Many leaf-fragments wereobtained as shown in PI. 15, fig. 8. Leaves
are branching four times dichotomously
but asymmetrically with a small angle,
but the whole shape is unknown. Laminae
are rather slender, 0.7-1.1 mm wide but
1.4 mm just below the branching andwith a single vein throughout as shownin Text-fig. 3 (9).
Remarks: The present leaves agree
fully with Czekanowskia nipponica inmacroscopic characters and, in our opinion, are somewhat different from several other species, but these differences areslight.
The fact that the vein is clearly visible
is a point of agreement, since in many
species the vein is very difficult to be
seen. Since the cuticle is not preservedin the present specimens, however, we
prefer to call them Cfr. Czekanowskia nipponica, reserving full taxonomic determination to specimens confirmed by the
cuticle.
As mentioned recently by KIMURA and
OHANA (1978), Czekanowskia is one of thecharacteristic members not only in theolder Mesozoic floras in the Northern
Hemisphere, but also in the late Jurassic
to the early Cretaceous floras of the
VAKHRAMEEV'S Siberian Palaeofloristic
Area and the coeval floras in the Inner
Zone of Japan.
After examining the present good material of Czekanowskia as well as the
specimens described by KIMURA and
OHANA (1978), we revise the former
determination of Czekanowskia sp. (KIMURA, 1958, p. 37, text-fig. 10). We now
consider the specimen generically indeterminable.
Occurrence: Probably common.
Specimen: TK -152.

94

Tatsuaki KIMURA, Shigeru SAITO and Takao TOjO
Genus Leptostrobus HEER, 1876 em.
HARRIS, 1951: 485
Leptostrobus sp.
PI. 14 fig. 8; Text-fig. 3(10)Several detached valves as shown in
PI. 14, fig. 8 (pointed by arrows) wereobtained. They are all crushed, but someof them faintly reveal their surface ornamentation as shown in Text-fig. 3 (10).
Their outer margins are missing, andsome are represented only by their sedimentary fillings.
From the preserved ridges on the uppersurface of each valve, we are certainthat the present material belongs to
Leptostrobus. The valves differ fromthose described by KIMURA and SEKIDO(1976, p. 370, pI. 38, fig. 7) from the Akaiwa Formation in being somewhat smaller
and in having fewer ridges. If, as we
believe, these valves belong to Cfr.
Czekanowskia nipponica, they are surely
an element of the Inner Zone flora.
Occurrence: Rare.
Specimens: TK -151, 175.
Conifers
Genus Podozamites BRAUN, 1843
Podozamites cfr. lanceolatus (LINDLEY

and HUTTON) BRAUN

PI. 14, fig. 7; Text-fig. 3 (11)An incomplete lanceolate leaf shownin PI. 14, fig. 7 was obtained. Its apicaland basal parts are missing. Nerves are
numerous, forking dichotomously near
the base, then parallel to each other asshown in Text-fig. 3 (11); the density is
22 per cm at the middle.
The present specimen resembles a detached leaf of Podozamites lanceolatus.
But we reserve its full taxonomic identification with this comprehensive species
because of its poor state of preservation
Occurrence: Rare.
SPecimen: TK-229.
Repository: All the specimens here
described are deposited in the Departmentof Astronomy and Earth Sciences, Tokyo
Gakugei University.
References
CHII-IAI~A, K., SI-II!v1AZU, M. and KUl~OKA\vA, K.

(1977): Geological structure and its development of the western part of thejoetsu Tectonic Belt, Central japan. Part
1. Geology. Sci. Ref). Niigata Univ., ser.
E, no. 4, p. 1-48.
E>':DO, S. (1925): Nilssonia-Bed of Hokkaido
and its flora. Sci. Rep. Tohoku Imp. Univ.,
sec. ser. (Ceol.) , vol. 7, no. 3, p. 57-72,
pIs. 11-17.
GEYLER, H. T. (1877): Ueber Fossile Pflanzen
aus der Juraformation japans. Palaeontographica, Bd. 24, p. 221-232, pIs. 31-34.

Explanation of Plate 14(All enlarged twice, unless otherwise mentioned)

Fig. 1. Asplenium dicksonianum HEER; TK-103.
Figs. 2-4. Adiantopteris sewardii (YABE) VASSILEVSKAJA; Fig. 2; TK-059, Fig. 3; TK-171.
Fig. 4; TK-203.
Fig. 5. Cladophlebis sp. B; TK-197.
Fig. 6. Sphenopteris sp.; TK-157, x3.
Fig. 7. P()dozamites cfr. lanceolatus (LemLEY and HUTTON) BRAUN; TK-229.
Fig. 8. Leptostrobus sp.; TK-175.

KIMURA et al.:

Early Cretaceous plants

Plate 14

704.

Early Cretaceous plants from the Tokurazawa Formation

HAYAMA, Y., KIZAKI, Y., AOKI, K., KOBAYA·
SHI, S., TOYA, K. and YAMASHITA, N.
(1969): The joetsu Metamorphic Belt andits bearing on the geologic structure of
the japanese Islands. Mem. Ceol. Soc.
Japan, no. 4, p. 61-82.
HAYASHI, S., KANZAWA, K., KIZAKI, Y.,OTAKE, S., TAKEI, K., TOYA, K. and YA·
MASHITA, N. (1965): On the 'Tetori
Series' found in the upstream of the River
Katashinagawa, Gumma Prefecture. Journ.
Ceol. Soc. Japan, vol. 71, no. 833, p. 76-77(in japanese).
HEER, O. (1874):
Die Kreide-Flora derarctischen Zone. J{. Svensk. Vet.-Akad.
Handl., Bd. 12, no. 6, p. 1-138, pIs. 1-38.
jAHNICHEN, H. and KAHLERT, H. (1972): Vbereine mesozoische Flora aus der mongolischen Volksrepublik. Ceology, jahr.
21. H. 8, p. 964-1001, incl. pIs. 1-6.
KAWADA, K. (1955): Geological Map of japan.
1: 50000, 'Nantaizan', and its explanatory
text. Ceol. Surv. Japan (in japanese withEnglish abstract).
KIMURA, T. (1958): On the Tetori Flora(Part 1). Mesozoic plants from the Kuzuryu Subgroup, Tetori Group, japan.
Bull. Sen. High Sch., Tolzyo Univ. Educ.,
no. 2-2, p. 1-47, pIs. 1-4.
- - (1975a): Middle·late early Cretaceous
plants newly found from the upper courseof the Kuzuryu River area, Fukui Pre·
fecture, japan. :Trans. Proc. Palaeont.
Soc. Japan, N. S., no. 98, p. 55-93, pis. 5-8.
- - (1975b): Notes on the early Cretaceous
Floras of japan. Bull. Tokyo Cakugei
Univ., ser. 4, vol. 27, p. 218-257.
- - and ASAMA, K. (1975): On the Paleozoic
and Mesozoic Land Floras of japan, withspecial reference to the stratigraphicaldistribution of early Cretaceous plants in
Kochi Prefecture, in the Outer Zone ofSouthwest japan. Mem. Natn. Sci. Mus.,no. 8, p. 91-114 (in japanese).
- - and HIRATA, M. (1975): Early Cretaceous
plants from Kochi Prefecture, Southwest
japan. Ibid., p. 67-90, pis. 10-13.
- - and HORIUCHI, j. (1979): Some lateearly Cretaceous plants from Fukui Prefecture, in the Inner Zone of japan.

95

Trans. Proc. Palaeont. Soc. Japan, N. S.
no. 113, p. 1-14, pI. 1.
- - and KANSHA, Y. (1978) : Early Cretaceous
plants from the Yuasa District and theAridagawa Valley, Wakayama Prefecture,in the Outer Zone of japan. Part 1. Bull.
Natn. Sci. Mus., ser. C, (Ceol. Paleont.) ,vol. 4, no. 3, p. 99-116, pis. 1-4.
- - and OHANA, T. (1978): CzekanolVskia
nipponica sp. nov. from the Upper Creta·
ceous Omichidani Formation, Ishikawa
Prefecture in the Inner Zone of Central
japan. Proc. Japan Acad. vol. 54, ser. B,
no. 10, p. 595-600.
- - and SEKIDO, S. (1976): Mesozoic plantsfrom the Akaiwa Formation (Upper Neo·comian), the Itoshiro Group, Central
Honshu, japan. Trans. Proc. Palaeont.
Soc. Japan, N. S., no. 103, p. 343-378, pIs.
36-39.
- - and - - (1978) : Addition to the Mesozoic
plants from the Akaiwa Formation (Upper
Neocomian), the Itoshiro Group, Central
Honshu, Inner Zone of japan. Ibid., no.
109, p. 259-279, pis. 36-38.
and (1978, MS): The Oguchi Flora(earliest Cretaceous) in the Inner Zoneof japan.
KRYSHTOFOYICH, A.N. and BAIKOYSKAJA, T.N.
(1960): Mesozoic flora from Sakhalin.
J{omarov Bot. Inst., Acad. Sci. USSR,
Moscow·Leningrad, p. 1-122, pis. 1-21 (inRussian) .
KUNO, H., YAMASAKI, M., SEKI, Y., MATSUI,
T. and SHIMIZU, j. (1954): Geology ofOzegahara and surrounding area. Sci. Res.
Ozegahara Moor, Tokyo, p. 68-77, with
1 map.
MURAYAMA, K. and KAWADA, K. (1956) : Geological Map of japan. 1: 50000, 'Hiuchidake', and its explanatory text. Ceol.
Surv. Japan (in japanese with English
abstract) .
olSI-II , S. (1940)': The Mesozoic floras ofjapan. Journ. Fcc.- Sci., Hokkaido Imp.
Univ., vol. 5, nos. 2-4, p. 123-480, pIs. 148.
SUDO, S. (1976): Geology of the Katashina
Area, .Gumma Prefecture, .Central japan.
Mem. Ceol. Soc; -japan, no .. I3,p.,,229-240

96

Tatsuaki KIMURA, Shigeru SAITO and Takao TOjO

(in Japanese with English abstract).
TOYA, K., HAYAMA, Y., HAYASHI, S., KANAZAWA, K., KIZAKI, Y., OTAKE, S., TAKAHASHI, K., TAKAHASHI, T., TAKEI, K. andY AMASHIT A, N. (1965): The Mesozoic
Formation in the upstream of the River

Katashinagawa. journ. Ceol. Soc. japan,
vol. 71, no. 838, p. 375 (in Japanese).
Y ABE, H. (1905):
Mesozoic plants from
Korea. journ. Coli. Sci., Imp. Univ. Tokyo,
vol. 20, art. 8, p. 1-59, pis. 1-4.

Akaiwa ~:B'
Chinaboradani ~Qmi1l'J:fr,
Itoigawa-Shizuoka :fM:liUII-jfjlp.i';l,Itoshiro
Iwamuro :B~,
Kami-Uchinami 1:hlW,
Katashina JtJfJ'1>
Kuruma *,~,
Kuwashima (=Kuwajima) ~Iih,
Kuzuryu fLJjj'{Jt,Lo-tzu-kou lifiirim,
Nagdong(=Naktong) i'il*,Oguchi ~IJ,
Omichidani ::k)g:fr,
Osugidani ::kt~:fr,Tamodani
EEa:fr (1J,fJ)::fr),
Tetori (=Tedori) =FI&,
Tokura p~,
Tokurazawa P~lR,
Tone-gun tUm-TIll,
Urushizawa 7*lR

E11&8,f¥,~!JjI,fIJm-TIIIJt~ttp~, Jt~}II1:iJlE~luHl?tf,i;f.::.it!±l-r- .0P~lRJfib' 0, -0 ~(J) J: ? t.c=F
I&~(J)1lil~{I:Eb~~0nt.::(J) -C:'itcllli; • ¥Ii~-r- .0;

Asplenium dicksonianum, Adiantopteris
sewardii, Cladophlebis sp. A, C. sp. B, Sphenopteris sp., Onychiopsis elongata, Cfr.
Czekanowskia nipponica, Leptostrobus sp., :to J: rJ Podozamites dr. lanceolatus.
1:.1-1:1:1:. \, 'Tn {" =FI&~Jfif¥(J)E11& 8 ~f¥(J)mr~f¥v.::.~ilR-r- .0 {, (J) -C:', ;:: n 0 (J){I:;P b' 0 ~Ij
l*JT-r-.0~! I), p~lRRiH:l:.Tffll8!lE*(J)EiI&8Jif1f¥v.::.%jJt~n.0o U.::b:-?L, ;::(J)*~I:I:., ~~ (J):B~~Jiflb' 0*,~~(J)mr4o/;{r.;Pb;ge5e. ~ nt.::;:: c c sltz.A., -e, tlmr4o/;~i'l~v'::' {" ggl¥.f 13 *fi'l*b:, J,' <c {, *~t 13 *(J) Jt~}lliJlE~ffllv'::'~*~n.0;:: CI:l:.lit~c ~;t 0n.0op~lRJifI(J)mr~{I:EI:I:., -'t:-(J) 1:ffllJfi(J) i6 .0 ~$I'::'W~ L L i£-r- .0b:, kf[JjX;li!iiff.i!l-C:'i6 .0"it.::tJ1:(J) p~lRJfi(J)mr~{I:E (J) ? i?, Onychiopsis elongata UYl-(J) {, (J) 1:1:., Yl-*(J) f~JtIl:; "'7 *c:to J: V:lliIM8!lE*cmr~f¥I.::.I:I:.;!: t-=~ 0n L\',t.c\' '0*tt~iJJ3 • 1fiii*~[li~
0a·Explanation of Plate 15(All enlarged twice, unless otherwise mentioned)
Fig. 1. Asplenium dicksonianum HEER; TK-075.
Fig. 2. Adiantopteris sewardii (Y ABE) VASSILEVSKAJA; TK-053B.
Fig. 3. Sphenopteris sp .. ; TK-168.
Figs. 4-7. Onychiopsis elongata (GEYLER) YOKOYAMA; Figs. 4-5; sterile leaves, Fig. 4; TK112, Fig. 5; TK-221. Figs. 6-7; fertile parts of leaves, Fig. 6; TK-167, Fig. 7; TK-112.
Fig. 8. Cfr. Czekanowskia nipponica KIMURA and OHANA; branching parts are pointed by arrows, TK-152, natural size.

KIMURA et al.: Early Cretaceous plants

Plate 15

97

PROCEEDINGS OF THE P ALAEONTOLOG ICALSOCIETY OF JAPAN

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Miocene benthonic Foraminifera from the
Sendai area and its environs (Part 1) "...... HASEGAWA, S. and TAKAYANAGI, Y.
~ti19*3jZt$O):all:Wl:~ft15 (DSDP Leg 56) ..... .

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Discovery of Visean brachiopods from theupper part of the Karaumedate Formation,southern Kitakami mountains ........... .
.............. TAZAWA, J. and OSAWA, M.
Ontogenic studies of a few Upper Cambriantrilobites from the Deadwood Formation,
South Dakota (~Wi:) •••...•....... Hu, C. H.
Life habit of a giant patelliform gastropod
from the Upper Cretaceous of Saghalien
and Japan ...... HAYAMI, I. and KANIE, Y.
~tl'faim:WlJlJjmmmO)IIJ'IrrJ!;!l C9='mXifC) ~ Dosinia

Cretaceous area ......................... .
. ......... MATSUMOTO, T. and KANIE, Y.
Notes on Pachydiscus from Hokkaido ..... .
MATSUMOTO, T., KANIE, Y. and YOSHIDA, S.
Some ammonites from the Yatsushiro Formation of Kyushu and their implications ..
............ MATSUMOTO, T. and OHTA, Y.
Restorative aspect on the jaw apparatus of
tetragonitid ammonites ................. .
· .KANIE, Y., FUKUDA, Y. and TANABE, K .
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Calcareous nannoplankton from the Cretaceous along Kanajirizawa and Akanosawa,Obira area, Hokkaido ........ OKAMURA, M.
l,'b~7.J15JR'l1t1"~/ 7,,}~!1 r ~ Coccolithus
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102

CONSTITUTION
of the
PALAEONTOLOGICAL SOCIETY OF JAPAN(Jan. 20, 1978 amended)
ArticleArticle1. The Society shall be known as the Palaeontological Society of Japan.
2. The object of the Society is to promote the study and popularization of palaeontology and related sciences.
Article 3. The Society, to execute Article 2, shall undertake the following business:
1. Issue the Society journal and other publications.
2. Hold or sponsor scientific lectures and meetings.
3. Popularize the science by field trips, scientific lectures and other projects.
4. Aid and encourage research work; award outstanding contributions to theSociety; carry out the objectives stated in Article 2.
Article 4. To attain the object of the Society, the Society may, by decision of the General
Meeting, establish within it research committees.
Article 5. The Society shall be composed of members who are active or interested in palaeontology or related sciences.
Article 6. The members shall be known as Regular Members, Fellows, Patron and Honorary
Members.
Article 7. Persons desiring membership in the Society are requested to fill out the necessary
application forms and receive the approval of the Council.
Article 8. Fellows are persons who have held Regular Membership in the Society for morethan ten years, have contributed to the science of palaeontology, have been
nominated by five Fellows and approved by the Council.
Article 9. Patrons are organizations supporting Article 2 and recommended by the Council.
Article 10. Honorary Members are persons of distinguished achievement in palaeontology.
They shall be recommended by the Council and approved by the General Meeting.
Article 11. The members of the Society shall be obliged to pay the annual dues stated in
Article 12. Members shall enjoy the privilege of receiving the Society journal andparticipating in the activities stated under Article 3.
Article 12. The rates for annual dues shall be decided by the General Meeting. Rates forannual dues are: Regular Members, Yen 4,500; Fellows, Yen 6,000; and Foreign
Members, Yen 6,000 or its equivalent in U. S. dollars; Patrons are organizations
donating more than a share (Yen 10,000) annually; Honorary Members are freefrom obligations.
Article 13. The budget of the Society shall be from membership dues, donations and bestowals.
Article 14. The Society, by decision of the Council, may expel from membership persons who
have failed to pay the annual dues or those who have disgraced the Society.
Article 15. The officers of the Society shall be composed of one President, fifteen Councillors
and several Executive members. The term of office is two years and they may be
eligible for re-election without limitation. The President may appoint several
persons who shall be Secretaries and Assistant Secretaries. An Executive Council
shall be nominated and approved by the Council. If necessary, several Executive
members, who must be Fellows, may be added with the Council's approval. Councillors shall be elected from Fellows by vote of returned mail unsigned ballot.
Article 16. The President shall be a Fellow nominated and approved by the Council. The
President shall represent the Society and supervise the business affairs. The

103
President may appoint a Vice-President when he is unable to perform his duties_
Article 17_ The Society may have the Honorary President. The Honorary President shall berecommended by the Council and approved by the General Meeting. The Honorary
President may participate in the Council.
Article 18. The Society shall hold regularly one General Meeting a year. The President shallbe Chairman and preside over the administrative affairs. The program for the
General Meeting shall be decided by the Council. The President may call ;;Special Meeting when he deems it necessary. The General Meeting requires theattendance of more than one-tenth of the members. The President shall call aSpecial ~Meeting at the written request of more than one-third of the members.
The request shall be granted only if the written statement fully explains thereasons for assembly and items for discussion.
Article 19. Members unable to attend the General Meeting may give as attending member awritten statement signed by himself trusting the bearer with the decision of businessmatters. Only one attending member may represent one absentee.
Article 20. The decision of the General Meeting shall be by majority vote. When the numberof votes is equal, the President shall cast the deciding vote.
Article 21. The President and Councillors shall compose the Council. The dicision of theGeneral Meeting concerning administration shall be considered and implemented by
the Council.
Article 22. The Executive Council shall carry out the decisions of the Council.
Article 23. An auditor shall be elected by the Council from Fellows excluding Councillors andSecretaries. The term of office is two years and he may be eligible for re-election.
Article 24. The fiscal year of the Society shall begin on the first of January each year andend on the thirty-first of December of the same year.
Article 25. The amendments to the Constitution of the Society shall be decided at the General
Meeting and must be approved by more than two-thirds of those members who are
in attendance.
Addendum 1)

Voting in the Council shall be by unsigned ballot.

104
POLICY PROVISIONS OF THE TRANSACTIONS AND PROCEEDINGS OF
THE PALAEONTOGICAL SOCIETY OF JAPAN(January 16, 1973)
Publishment and Editing
IA Issue-1 The "Transactions and Proceedings of the Palaeontological Society of Japan"(TPPSJ) will be published quarterly.
IB Contents-1 TPPSJ will include original papers and notes that comply with Article 2 of theConstitution of the Society as well as the proceedings of the Society meetings andnews concerning any aspect of palaeontology.
-2 Contributions will be published in the order of the acceptance by the Editorial
Board.
IC Circulation-1 All members of the Society and some organizations specified by the Council will
generally receive TPPSJ free of charge. Non-members and institutions are invited
to become subscribers.
ID Editorial Board-1 The Editorial Board will be responsible for editing TPPSJ according to the policy
provisions of the Society.
-2 The Editorial Board will be composed of the Editor in Chief, who must be a member of the Council, and several members designated by the Executive Committee.
All editorial meetings will be called by the Editor in Chief.
-3 The Editor in Chief will have the authority to submit a copy of the manuscript
under consideration to an appropriate person for reviewing_-4 The final decision on the acceptance or rejection of submitted manuscript will bemade by the Editorial Board at an editorial meeting. The Editor in Chief willreport the results of the meeting to the Executive Committee.
-5 Rejected manuscript will be returned to the author with an explanation of thereason for its rejection.
-6 An author who disagrees with the decision of the Editorial Board may take hiscomplaint to the Council. Both the Editorial Board and the author must abide by
the final judgemen t of the Council.
IE Proof Reading-1 Proofs will be read, as a rule, by the Editorial Board. A set of page proofs without
the original manuscript \,;-ill be sent to the author.
n Contribution
IIA Eligibility-1 All members of the Society may submit contributions to TPPSJ. Contributions
from non-members will be accepted for publication if they are approved by the
Executive Committee.
-2 Manuscript should be written, as far as possible, in English, French or German, andshould have been read at an annual meeting or ordinary meeting of the Society.
IIB Limitation of Manuscript-1 Manuscript should be typewritten, and should be limited to 24 printed pages including tables and text-figures. Two plates may also be added to it. Plates may not be
attached to the articles of up to 4 printed pages only without the approval of the
Editorial Board. Notes may not exceed one printed page, and no plate may be
used for it.
I105-2 Ten figures or 600 cm 2 of the total printed area will be permitted for a single
article. Two figures or 200 cm" of the total for article of less than 4 printed pages.
The original illustrations should be neat and legible to permit reduction to either
the width of one printed page (13.4 cm) or one column (6.4 cm). Figures should
be kept separate from the text of the manuscript.
-3 Excess printing charges for articles exceeding the stated limit must be borne by
the author.
lIC Style of Manuscript-1 Generic and specific names and special words should be indicated in the manuscript.
-2 Suggested positions of tables and text-figures should be indicated in the margin of
the text.
-3 Captions and explanations of text-figures, tables and plates should be submitted on
separate sheets of paper numbered independently from the text.
-4 References cited should be listed in a bibliography at the end of the text in alphabetical order under the author's name, and in chronological order, as follows:
Author's name, year, title of article, name of journal (underlined), vol., no.,pages, plates, etc.
-5 It is recommended that an alphabetical list of romanized geographical names be
included with Kanji (Chinese ideograph), if any. The annotated list will be placedat the end of the text.
-6 Name(s) and professional or private present address of the author(s) should appear
below the title of the manuscript.
-7 All manuscripts with the exception of notes should be accompanied by an abstract
in Japanese of SOO·words or less on separate sheet(s) of ·paper. The abstract should
include the title in Japanese and the author'S name. Abstracts of papers by nonJapanese speaking authors will be prepared by the Editorial Board if an English
abstract be submitted with the manuscript.
IID Obligation of Author-1 Authors are expected to fo11o\\' the directions of the Editorial Board regarding
editorial matters.
-2 Manuscripts will be returned to an author if he wishes to make large-scale revisions. The re\'ised manuscript must be submitted as a new contribution.
-3 Manuscript should be accompanied by a complete copy including text-figures, tables
and plates. Manuscript should be sent toEditor in Chief
Palaeontological Society of Japan
c/o Business Center for Academic Societies
4-16, Yayoi 2 chome, Bunkyo·ku, 113 Tokyo, JAPAN-4 The author should fill out the register card for contributions and send it to theSociety ofilce under separate cover.
IIE Reprints-1 120 reprints without co\'ers will be furnished free of charge. Excess charges forprinted covers, additional reprint copies, etc. will be borne by the author who must
pay the amount directly to the publisher.
Provisoi) Effecting, amending or rescinding of policy prOVISIOns will be considered by theCouncil, and must be approved by the general meeting of the Society.
ii) The approved policy provisions will nullify and replace existing "Regulations for
Publication in Transactions and Proceedings of the Palaeontological Society of Japan ".

106

PALAEONTOLOGICAL SOCIETY OF JAPAN, SPECIAL PAPERS, NUMBER 24 ~ 19S0 ~m):::.
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107
Palaeontological Society of Japan Special Papers No. 22

Bibliography of Palaeontology in Japan, 1961-1975
Edited by Kametoshi KANMERA and Hiroshi UJIIE
Issued March 30, 1978, x+263 pp.

Price (postage and handling inc!.) ¥6,900 or equivalent US dollars
This is the third issue of the Bibliography of Palaeontology in Japan, containing about
3100 literatures of palaeontology and related disciplines published during fifteen years from1961 to 1975. This includes articles written by Japanese authors using materials not only fromJapan but also from foreign countries, articles by foreign authors using materials from Japanand its adjacent seas, and also articles by foreign authors that appeared in Japanese journals.
The contents of this volume consist of two parts; one is the author catalogue arrangedalphabetically by senior author name with full title, medium of publication and prefixed withitem number; the other consists of indices of three groups-junior author, geologic age andtaxa.
This volume is indispensable not only for all palaeontologists but also for researchers of
the related sciences in our own and other count ries.

The following back numbers of the Special Papers are on sale at the Society. Orders mustbe accompanied by remittance made payable to Dr. Tsugio SHUTO, Editor of the Special Papers,
Palaeontological Society of Japan, c/o Department of Geology, Faculty of Science, Kyushu
University, 33, Fukuoka (Hakata) 812, Japan.
Number 12 (Issued Sept. 20, 1966): Postcranial Skeletons of Japanese
Desmostylia. By Tokio SHIKAMA ....................... ¥5, 000 or equivalent US dollars.
Number 13 (Issued March 16, 1968): The Echinoid Fauna from Japanand Adjacent Regions. Part II. By Shozo NISIYAMA ................... ¥7, 400 or ditto.
Number 15 (Issued Feb. 25, 1971): Early Devonian Brachiopods fromthe Lesser Khingan District of Northeast China.
By Takashi HAMADA ..................................................... ¥ 4,400 or ditto.
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By Saburo KANNO. . ..................................................... ¥5, 600 or ditto.
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Comparison with Asian, Pacific and Other Faunas.
By Teiichi KOBAYASHI and Takashi HAlI·IADA ........................... ¥5, 100 or ditto.
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Himenoura Group in Kyushu. By Masayuki TASHIRO. . ................. ¥ 4,700 or ditto.
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Comparison with Asian, Pacific and other Faunas.
By Teiichi KOBAYASHI and Takashi HAMADA ........................... ¥6, 900 or ditto.
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Symposium, 1976. By Tatsuro MATSUMOTO (org.) ...................... ¥5, 800 or ditto.

108

Sessions of the International Geological Congress have been held every
four years since 1878. The 26th session will celebrate the Centenary of thisorganization convened under the auspices of the International Union of Geological
Sciences.
Organization Committee
Timetable

Chairman: Jean AUBOUIN
Secretary General : Paul SANGNIER- 26 june to 5 july - Pre-congress scientific excursions- 7 to 17 july - The Congress will meet at the Palais des Congres at
Porte Naillot- 18 to 27 july - Post-Congress scientific excursions.

Scientific Progr~I) Opening Scientific Meeting: Leading specialists will survey five main

themes concerning the current state of scientific progress.

2) Sections : The proposed program covers almost the entire field of the
Earth Sciences and is divided into 20 sections. The Organization Cormnittee has
also planned to have the work of the various international scientific organizations

affiliated with the International Union of Geological Sciences integrated into
the program of the Congress. Authors are free to choose their own subjects forcommunications and these should be sent to the Secretary General before
I october 1979 for the publication of abstracts.
3) Colloquia : The program for the colloquia was chose.n so as toillustrate the main themes of curr~nt scientific and economic interest.. There
will be seven in all and they will he chaired by leading scientific figures.
Communications to the Colloquia are made by invitation only.

Excursions
The Organization Committee in association with the National Committees
for Geology of 18 european countries has organized an attractive program ofgeological excursions. The chosen themes make it possible to offer Congress
participants a survey of all aspects of the geology of Western Europe. 85
different excursions each lasting for 9 days are planned from 26 JUNE to 6 JUlY1980 or from 19 JUlY to 26 JULY 1980. Since only a limited number of persons
can participate in the excursions the pl<lces will be reserved by the Organizing
Committee in october 1979 in the order in which the reservation forms werereceived.

Exhibition
An exhibition to be called "GEOEXPO 80" will be held in the same
premises as the Congress from 7 to II july 1980. It will be open to allinternational institutions and will make it possible for exchanges of ideas <lnd
contacts to take place with scientists from allover the world.
Social Program

Since the Congress is taking place in Paris the organizers will be able
to plan a very attractive program for the participants and a special program fQr
persons accompanying them.

State of Advancement of Congress Preparation
80,000 copies of the first circular were sent out in october 1977. By
december 1978 the Organization Committee had received 5,800 answers from 114
different countries and 4,000 persons· had asked to take part in the excursions.
The second circular is now available and contains the final registration form.
Those interested in participating in the Congress and wishing to receive

the second circular should request it from the :Secretariat General du 26eme Congres Geologique International
Maison de 1a Geologie
77-79, rue Claude Bernard
75005 PARIS - FRANCE

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Transactions and Proceedings of the PalaeontologicalSociety of Japanjuly 15, 1979

New Series No. 114

CONTENTS
TRANSACTIONS
701. Hu, Chung-Hung: Ontogenic Studies of a few Upper Cambrian Trilobitesfrom the Deadwood Formation, South Dakota .. ..... . ........ .. ... ... 49
702.

MATSUMOTO, Tatsuro and YOSHIDA, Saburo: A New Gaudryceratid Ammonite
from Eastern Hokkaido (Studies of the Cretaceous Ammonites from
Hokkaido and Saghalien-XXXVII) . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. .. 65703. SAKAGAMI, Sumio and SAKAI, Akira: Triassic Bryozoans from the Hidaka
Group in Hokkaido, japan .... . ..... . ... . ... . .. . . ..... ... .. ....... . ... 77704. KIMURA, Tatsuaki, SAITO, Shigeru and TOlO, Takao: Early Cretaceous Plantsfrom the Tokurazawa Formation, Gumma Prefecture, in the Inner Zoneof Northeast japan ...... . . .... ...... .. . ............... . ............ . 87
SHORT NOTES
16. SUZUKI, Shigeyuki and YAMAGIWA, Nobuo: Some Newly Discovered Late
Permian Corals from the Maizuru Group. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 64
PROCEEDINGS ....... . ....... . ... . .. . .... . .. . .. . . .. .. . .... ........ . .. . ..... .. . 97