Transactions and Proceedings

of the

Palaeontolqgical,, Society of Japan

New Series No. 85

Palaeontological Society of Japan April 20, 1972 Editor: Takashi HAMADA Associate editor: Yasuhide IWASAKI

Officers for 1971 - 1972

President: Tokio SHIKAMA Councillors (* Executives): Kiyoshi AsANO*, Kiyotaka CHINZEI*, Takashi HAMADA*, Tetsuro HAN AI*, Kotora HAT AI, Itaru HAY AMI, Koichiro ICHIKAwA, Taro KANAYA, Kametoshi KANMERA, Tamio KOTAKA, Tatsuro MATSUMOTO*, Hiroshi OZAKI*, Tokio SHIKAMA*, Fuyuji TAKA!*, Yokichi TAKAYANAGI Secretaries: Wataru HASHIMOTO, Saburo KANNO Executive Committee General Affairs: Tetsuro HANAI, Naoaki AOKI Membership : Kiyotaka CHINZEI, Toshio KOIKE Finance: Fuyuji T AKAI, Hisayoshi !GO Planning: Hiroshi OZAKI, Kazuo ASAMA Publications Transactions: Takashi HAMADA, Yasuhide IWASAKI Special Papers: Tatsuro MATSUMOTO, Tomowo OzAwA " Fossils" : Kiyoshi ASANO, Toshiaki TAKAYAMA

All communications relating to this journal should be addressed to the PALAEONTOLOGICAL SOCIETY OF JAPAN c/ o Business Center for Academic Societies, Japan. Yayoi 2-4-16, Bunkyo-ku, Tokyo 113, Japan Sole agent : University of Tokyo Press, Hongo, Tokyo Trans. Proc. Palaeont. Soc. Japan, N. S., No. 85, pp. 245-259, pis. 29, 30, April 20, 1972

591. ONTOGENY OF THREE CEDARIA ZONE TRILOBITES FROM UPPER CAMBRIAN, MONTANA*

CHUNG-HUNG HU

Department of Biology, Nanyang University, Singapore**

-c :/ !l 7-1-I-IJ:;·~~ 'h :/ 7" ~ 7*0) Cedaria 1\~=,:)[::::::•x~!R :=:f,llO)iibH:>J.:§E~: ~t::i~ -c :/ !l T-1+1 "'T 1 '/ :/ 'h 7 :/7' 1 0)_]·.)}1177 :/ 7' ~ 7* Cedaria ;:;::f;::_~-9- 0 !::" '" !f ~ .L..~ 0)/~Efd!:.Tiffi!G fcv'i3:-;!ix0)::::::~~1l-?1!9iilf:.J'J. C1roil'l!lt~Uf0 i.i;fr'i:lc·-n-'0, .:::.:lci?O) '5 'G:=:Z.f!EO) 3 fir(, -Tt.;::h 'G Syspacheilus dunoirensis, Nixonella montanensis, Baltagnostus beltensis (C"?v'L, .:CO)f0jf*J£1=-'2w:.J.....::t.=if.i'ilf,;, '%-O)flf'i Coosella convexa -? Crepicephalus deadwoodensis :to J::: l1 Tricrepicephalus blountensis t.;:: c'O))E1=-v:=. 1]!WJ_-9 0 ,.~•.7J;;:!,.0 fJ, ~=H\f'i ~;·1 fl~ tc, Kingstonia ara :to J::: tF Komaspidella laevis \C, 'i t:~:::':O)l'J't:'i IC, Kormagnostus sim­ plex fC, .:Ch.:f'hj~:l,"Cv'Q.:::. ci.J;~jajj L..t.=, L..t.=i.J;-:> "C, .:::.hi?0)0-*JH'i**1t(l'~tJ:v' l..l'i5J ~rl"¥:i'i'~fcili:HdYJi,f,'2

colored, medium crystalline limestone, Introduction containing an abundance of trilobite fragments, inarticulate brachiopods, and The purpose of the present study is a few intraformational pebbles. The ge­ to illustrate the ontor.;enetic development ologic positions of the materials belong of Syspacheilus dunoirensis (MILLER), to the Pilgrim formation, Cedaria zone, Nixonella montanensis LOCHMA!\', Balta­ Upper Cam brian. gnostus beltensis LOCHMAN, and the The ontogenetic metamorphosis of sexual dimorphism of Syspacheilus duno­ Syspacheilus dunoirensis is very similar irensis (MILLER). The ontogenetic de­ to those of Coosella convexa TASCH (Hu, velopment of the first two species is 1968b), Crepicephalus deadwoodensis Hu well known, but is incompletely known (1968a), and Tricrepicephalus blountensis for the last one. Both the ontogenetic RESSER (unpublished material); that of separation and the sexual determination J\''ixonella montanensis LOCHMAN is close of the trilobites are based on the sche­ to Kingstonia ara (WALCOTT) (Hu, 1968b), mes in the author's earlier works (Hu, Komaspidella laevis RASETTI (Hu, 1970); 1964, 1968a, 1970, etc.). and that of Baltagnostus beltensis LOCH­ The materials were collected from MAN to Kormagnostus simplex RESSER west-side, South-Boulder Creek, Madison (Hu, 1968a). All members within the County, Montana, and are light gray same group possibly have close phylo­ * Received Nov. 10,1970; read Jan. 23, 1972. genetic relationship, and belong to a ** Present adress : Earth Science Depart­ same genetic hierarchy. ment, Cheng Kung University, Tainan, Tai­ The author is deeply indebted to Dr. wan, Republic of China. K.E. CASTER, University of Cincinnati, for 245 246 Chung-Hung Hu his supervision, thanks also go to Dr. axial rings ; marginal border broad and Anne JoHNSON, Nanyang University, for flat. Outer skeletal surface granulated, reading over the present manuscript. and inner surface punctured ; a pair of The figured specimens are all stored in elongated pits on the anterior furrow, the Geology Museum, University of and irregular concentric ridges along Cincinnati, Ohio (U. C. M.). The financial pygidial margin. expenses of the present study were Remarks: LOCHMAN & HU (1961) re­ supported by Miss Nancy NUN Science ported that there are four distinct spe­ Research Foundation, Nanyang Univer­ cies within the present genus: they are sity. Syspacheilus typicalis RESSER, 1938, S. praecedens LOCHMAN & Hu, 1961, S. Systematic de3cription camurus LOCHMAN, 1940, and S. duno­ irensis (MILLER, 1936). The first two Family Crepicephaliidae KOBA Y ASH!, 1935 species have broader flat preglabellar fields and in the last two, they are Genus Syspacheilus RESSER, 1938 narrow and steeply slope downward. Syspacheilus dunoirensis (MILLER) Furthermore, S. dunoirensis and S. pra­ ecedens have slender glabella, whereas Pl. 29, figs. 1-34, and Text-fig. 3a-k. those of the other two are broader. The materials which I have studied could be Blountia dunoirensis MILLER, 1936, p. 27, pl. segregated into two different morpho­ 8, figs. 25, 26. logic groups. The first group conforms Syspacheilus dunoirensis (MILLER) : LocmiAN & DUNCAN, 1944, p. 131-132, pl. 11, figs. with " S. dunoirensis" and the second to 44, 45; pALMER, 1954, p. 734, pl. 78, fig. "S. praecedens ". These bimodal traits 9; DELAND & SHAW, 1957, p. 561, pl. 64, are here interpreted as the presence of Syspacheilus dunoirensis var. (MILLER) : sexual dimorphism within the same LocHMAN & Hu, 1961, p. 135, pl. 26, species population and are found in the . figs. 26, 37-39. same ecological habitats. The first group Syspacheilus accidens LocHMAN, 1950, p. 342, is presumably the female and the second pl. 50, figs. 25, 26. the male. If this postulation is accept­ Syspacheilus praecedens var. elongatus LocH­ able then the S. typicalis and S. camurus MAN & Hu, 1961, p. 136, pl. 27, figs. 19- 28, 30. are possibly another example of the Coosella vagrans LociiMAN & Hu, 1961, pl. different sexual representatives of the 26, figs. 49-54. same species. The early ontogenetic development of Diagnosis: Cranidium trapezoidal; the both sexes are indistinguishable: all anterior border broad, con vex; glabella immature forms have the same mor­ conical; preglabellar field medium wide; phologic characteristics, but in their late occipital ring crescentic, bearing a tiny stages the cranidium is gradually dif­ median tubercle. Fixigena less than ferentiated into two forms; one group one-half the width of glabella; posterior with slender glabella, flat preglabellar border same width as the occipital ring. field, and broader pygidial margin, and Librigena subtrapezoidal having a rather the other has broader glabellar, tilted small genal spine ; ocular platform the preglabellar field, and narrow pygidial same width as lateral border. Pygidium margin. broadly kidney shaped, convex with two Coosella vagrans LOCHMAN & Hu, 1961 591. Ontogeny of three Cedaria zone trilobites 247

a b c d

h g f e

k

Text-fig. 1. Syspache£/us dunoirensis (MILLER). a, Anaprotaspis, x 50; b, Metaprotaspis, x 50; c, Paraprotaspis, x 32; d, Early meraspid cranidium, x 20; e, f, Two late meraspid cranidia, x 9, x 8; g, Librigena, x 5; h, k, A male pygidium and a cranidium, x '1, x 4; i, j, A female cranidium and a pygidium, x 6, x20. (all drawings were made from photographs.)

·has no distinct characters by which it Pl. 29, figs. 14, 21, 23, 25-29, 31 ·can be separated from S. dunoirensis and Text-fig. lh, k. except the "C. vagrans" has the crani­ Description: The cranidium is trape­ dium slightly flattened. This feature zoidal in outline, highly convex; glabella is possibly due to compaction of the conical, short and broad, and with round­ -deposits or to individual variation, but ed anterior margin; the preglabellar has no specific significance. field is of medium width, slopes down­ ward from the anterior glabellar, and inclined about 45 degrees; the anterior Syspacheilus dunoirensis (MILLER), furrow is deep and broad, possessing a "male" pair of elongate pits laterally; the 248 Chung-Hung Hu anterior border is narrow crescentic, with one or two shallow pleural furrows;: convex, arching forwardly; the occipital the broad margin is delimited by the­ ring is convex both vertically and post­ shallow inner marginal furrow, and with eriorly, bearing a small median node; shallow posterior embedding. the broad and deeply impressed occipital The exoskeleton of the animal is cov­ furrow curves forward on the axial line ered by medium-sized granules, parallel. (sag.), and deepens both posteriorly and ridges marked along the outer margin laterally with a pair of elongate pits. of the anterior border, faint and radial The fixigena is narrow, about one-half ridges on the preglabellar field, and a. the width of the glabella, medium width, longitudinal ridge is marked along the convex ; the medium sized palpebral lobe central cranidial axis. is sickle-shape, situated on the mid-line Figured specimens: Male form: Crani­ of the glabella (tr.), and well delimited dia, U. C. M. 40279m, v, x, c' ; Librigenae,.. by palpebral furrow; the palpebral lobe U. C. M. 40279 n, s; Pygidia, U. C. M- is indistinct, which extends to the 40279t, y, z, a'. antero-lateral margin of the glabella from the anterior palpebral lobe, and Syspacheilus dunoirensis (MILLER), arches forward; the facial suture is opisthoparian, its anterior branch is "female" ·slightly divergent and convex, and the Pl. 29, figs. 16-19, 22, 24, 30, 33, 34, posterior one divergent-straight, and and Text-fig. 1 i, j. convex. The subtrapezoidal librigena is con­ Comparison: The female form differs. vex and has the ocular platform nar­ from the male in having the deeper and rowed; the large ocular ring is con­ narrower anterior furrow ; steeper pre-­ nected to both anterior and posterior glabellar field ; narrower pygidial axis ;·. free margins ; the lateral furrow is broader pygidial margin, and deeply shallow, and narrower than the lateral marked pqsterior marginal embayment._ border; the lateral border is horizontal, The sexual ratio is 217. convex, possesses a rather small genal Figured specimens: Female form :.. spine; posterior librigenal border absent; Cranidia, U. M. C. 40279o, p, w, d'; Libri­ the genal angle or the posterior free gena, U. M. C. 40279e' ; Pygidia, U. M. C.. margin curves into the genal spine to 40279r, u, b'. form a broad rounded angle and a short broad base indentation. Syspacheilus dunoirensis (MILLER), Pygidium is lenticular or kidney­ ontogeny shaped, convex, occupied by a broad and short axial lobe; the axis is divided Anaprotaspid stage (Pl. 29, fig. 1, and' into one or two convex rings and a Text-fig. 1a).-The shield is rounded,. broad terminal portion by shallow ring moderately convex, about 0.30 mm in furrows; the posterior axis is slightly length (sag.) ; the axial lobe is convex,. elevated and moderately convex, and slightly above the pleural region, with­ separated from the terminal portion by out any distinct dorsal furrow; the. an indistinct furrow; the pleural lobe posterior margin is flat and slightly is narrow, convex, slopes downward curved inward. from the shallow dorsal furrow, marked Only a single specimen is assigned to- 591. Ontogeny of three Cedaria zone trilobites 249

·the present stage. The shield surface and divided into two or three segments; is characterized without any special the protopygidial axis and the pleural feature. Its anterior margin may be lobes are well differentiated into axial marked by a pair of frontal pits and rings and pleural bands by furrows. the posterior marked by an elevated The surface of the shield is faintly occipital node; these suggest the orien­ granulated, and four pairs of coarser tation of the shield. grains are marked on the fixigena and Metaprotaspid stage (Pl. 29, fig. 2, and the fixigenal borders. Text-fig. lb).-The shield is rounded­ The present stage is characterized by oval in outline, convex, about 0.30-0.35 the cylindrical glabella, narrower pleural mm in length (sag.) ; the axial lobe is lobes, and the presence of the proto­ expanded forward from the posterior pygidium. end to the anterior margin; the dorsal Early meraspid stage (Pl. 29, figs. 6-9 .and the ring furrows are only recogniz­ and Text-fig. ld).-The cranidium is able on the larger specimens, otherwise trapezoidal in outline, convex, about indistinct; the pleural lobe is rather 0.65-0.70 mm in length (sag.), with well broad, about twice as wide as the axis developed facial sutures; the glabella is ,(tr.) ; the anterior pits are elongate, and cylindrical, or slightly expanded both an­ well imf.lressed; the posterior shield is teriorly and posteriorly from the central surrounded by a flat and slightly down line (tr.); the four rounded and recogni­ sloping margin, without indication of zable axial rings are indistinctly divided, the segmentation, except for a rounded and the first ring is impressed by a pair occipital ring and border furrow. of elongate pits laterally; the occipital The present stage differs from the ring is narrow, convex, curving post­ anaprotaspis in having the well develop­ eriorly bearing a minute median node, ed axial furrow and both of the axial and distinctly separated by a narrow and pleural lobes. occipital furrow; the anterior border is Paraprotaspid stage (Pl. 29, figs. 3-5, very narrow, horizontal, convex, arching and Text-fig. lc).-The shield is oval, forward, well delimited by a deep fur­ consists of the cephalon and the proto­ row. The fixigena is broader than the pygidium and is about 0.40-0.55 mm in glabella (tr.), triangular, moderately con­ length (sag.) ; the distinctly differen­ vex; the palpebral ridge is situated in tiated axial lobe is cylindrical, expanded front of the mid-line of the glabella (tr.), slightly forward, without a well devel­ narrow, elevated, well separated from oped axial ring, except for the occipital the fixigena by palpebral furrow, and one; the dorsal furrow is irregularly connected to both of the anterior pleural marked, which suggests the presence of ridge and the glabellar margins ; the the axial ring and ring furrows ; a pair posterior border is well impressed by of short eye-brow ridges extend lateral­ broad border furrow, convex, elevated, ly from the sides of the frontal lobe, about one and one-half width of the they are well delimited by paired an­ occipital ring. The facial suture is the terior pits, and palpebral ridges; the proparian type, with its anterior branch pleural lobe is broad, about one and one­ short and convex, and the posterior one half the width of the axis, convex; the divergent laterally and convex. The posterior shield or the protopygidium is skeletal surface is faintly granulated, -convex, surrounded by broad flat margin, four pairs of coarse granules on the 250 Chung-Hung Hu fixigenae and the fixigenal border. present species is very closely similar The distinct characters of the present to those of Crepicep!wlus deadwoodensis stage are that the glabella becomes Hu (Hu, 1968a), Coosella convexa TASCH cylindrical or oblongus, without distinct (Hu, 1968b), Tricrepicephalus blountensis glabellar furrow, occipital ring broadly RESSER (unpublished material). All of convex, well separated from the glabella the features have parallel development by occipital furrow, facial suture prop­ during their growth stages, especially aria!, vvell defined. in the shape of their glabella, and the Late meraspid stage (Pl. 29, figs. 10-13, four pairs of coarse granules are indis­ and Text-fig. 1 e, f).-The trapezoidal tinguishable within the four species in cranidium is convex, about 0.80 to 1.65 the immature forms. It is doubtless. mm long (sag.) ; the glabella is sub­ these four species are the member of quadrate or oblongus, marked without the same family, and with close phy­ distinct glabellar furrow; the occipital logenetic relationship. ring is crescentic, convex both vertical­ Figured specimens: Anaprotaspis,. ly and posteriorly, bearing a minute U. C. M. 40279; Metaprotaspis, U. C. M. median tubercle; the preglabellar field 40279a; Paraprotaspides, U.C.M. 40279b­ is narrower than the anterior border, d; Early meraspides, U. C. M. 40279e-h ;. convex, tilted slightly anteriorly; the Late meraspides, U. C. M. 40279 i-l. frontal furrow is deep and broad, having a pair of elongate pits laterally; the Family Pagodiidae KOBA Y ASH!, 1935 fixigena is the same width as the gla­ bella or slightly narrower, convex, with Genus Nixonella LOCHMAN, 1944 a pair of medium-sized palpebral lobes situated on the mid-line of the glabella Synonym: Genus Nixon ella LocwviAN, 1944 (tr.) ; the palpebral furrow is narrow and (type species, Nixonella montanensis LocH-· MAN). distinct. The posterior fixigena is sub­ Genus Torridella LocH MAN & I-Iu, 1962 triangular, convex, with posterior fixi­ (type species, Torridella migranta LocHMAN. gena well demarked by a broad furrow. & Hu). convex, about the same width as the occipital ring (sag.) ; the facial suture is Remarks: The present genus is a. opisthoparian. its anterior branch slight­ common member within the Cedaria ly divergent-convex, and the posterior zone, Upper Cambrian. Its appearance one is divergent-straight. is similar to Genevievella LOCI-IMAN,. The skeletal surface is covered by 1936, both have no preglabellar field, a faint granules, four pairs of coarse simple anterior border, and conical gla­ granules are regularly marked on the bella, except the Nixonella has the gon­ glabella and three pairs on the fixigena. atoparian facial suture and the later The present stage differs from the one the proparian. The holotype of the previous one in that the preglabellar N. montanensis LOCHMAN (1944, pl. 13,. field appears, the glabella becomes ob­ figs. 29, 30) is a small cranidium, about longus, the palpebral lobe is situated on 2.0 mm in length (sag.), with the broad the mid-length of the glabella, the fixi­ anterior border and oblong glabella. It gena narrower, and opisthoparian facial is possibly not a well developed mature suture present. specimen. The associated pygidium of Remarks: The morphogenesis of the N. montanensis (LOCHMAN, 1944, pl. 13,. 5 91. Ontogeny of three Cedaria zone trilobites 251 fig. 28) consists of two segments, trans­ glabellar furrows; no preglabellar field; verse, semicircular in outline, about 1.0 anterior border narrow crescentic; fixi­ mm in length (sag.), is a meraspid pygi­ gena about one-half width of the gla­ dium, and possibly belongs to cedaroid bella, triangular, and palpebral lobe (Paracedaria ?). small ; gonatoparian facial suture pre­ A genus Torridella proposed by LOCH­ sent. Librigena narrow, crescentic with­ MAN & Hu (1962) has the type species T. out distinct marginal furrow and genal migranta about 3.0 mm in length (sag.) spine. Pygidium regular triangular, (pl. 6, fig. 8; holotype), with the similar convex ; six axial rings ; axis narrower characteristics as "N. montanensis" ex­ than the pleura] lobe, and not extends cept its glabella is conical and anterior to the full length of the pygidium. border is narrower. It is presumably a Description: The regular trapezoidal mature specimen. The pygidium of ·• T. cranidium is convex, has a conical gla­ migranta" is roundly triangular in out­ bella marked by three pairs of shallow line, convex, consists of more than six glabellar furrows; the first pair of gla­ axial rings. Since these features are dis­ bellar furrows is faint and short, the tinctly different from any other species second is medium-sized, and the third within the same faunal assemblage, this one is the largest and deeply marked, is possibly the correct association. These and obliquely directed to the occipital facts here permit to state that the furrow from the posterior palpebral genera "Torridel-la" and "Nixonella" lobe; preglabella field absent; the an­ are synonymous, however the type spe­ terior border is horizontally convex, cies of "Nixonella montanensis" has a narrow. arching anteriorly and well semicircular pygidium and that of delimited by the frontal furrow; the "Torridella migranta" has conical gla­ occipital ring is crescentic, convex, ar­ bella as described above, but the former ches posteriorly and bears a minute was due to the misassociation and the median tubercle; the narrow occipital latter one was the mature specimens in furrow arches slightly forward on the the full grown stage. Therefore, these mid-line. and is demarked with a pair of two forms have no foundation for the elongate pits laterally; the dorsal furrow genetic separation. is deep and broad. The fixigena is nearly triangular, convex, about one­ half the width of the glabella; the small Nixonella montanensis LOCHMAN palpebral lobe is located in front of the Pl. 30, figs. 1-21, and Text-fig. 2a-k. mid-line of the glabella (tr.), and the palpebral ridge is distinct; the convex Nixonella montanensis LocHMAN, 1944, p. 105, posterior fixigenal border is about the pl. 13, figs. 23, 27, 29-31 only (not fig. 28) : same width as occipital ring (tr.), well LocHMAN & I-lu, 1962, p. 16, pl. 5, figs. defined by a broad and shallow border 48, 50-52 only (not fig. 49). furrow; the anterior branch of the facial Nixonella cf. montanensis Locl!MAN, 1944, p. suture is slightly divergent-convex, and ).06, pl. 27, fig. 29. the posterior one divergent-straight Torridella migranta LocHMAN & Hu, 1964, p. 17, pl. 6, figs. 7-18. laterally. The librigena is narrow, elongate, Diagnosis: Cranidium trpezoidal, con­ without genal spine; the lateral furrow vex; glabella conical, three pairs of and the border are about the same 252 Chung-Hung HU width, and indistinctly demarked; the pleural lobe is slightly broader than the narrow ocular platform is flat, with the axis, delimited by a broad and deep posterior area broader than the anterior dorsal furrow, and has rather faintly margin ; the small oval ocular ring is impressed pleural furrows; the marginal located forward from the mid-line of border is broader posteriorly from the librigena (tr.), convex, and elevated facet angles, and demarked by a rather above the ocular paltform. indistinct inner marginal furrow. Pygidium is triangular in outline, The animal exoskeleton is covered by without marginal spine, and convex faint granules, and inner surface with along the rounded margin ; the axial the furrows deeply marked. lobe is slenderly conical, tapering poste­ Figured specimens: Cranidia, U. C. M. riorly, divided by 6 or 7 narrow, convex 40280, 40280 a-c; Librigena, U. C. M. axial rings by indistinct furrows; the 40280t ; Pygidia, U. C. M. 40280p-s.

a b c d

. . a . f e h g

Text-tigure 2. Nixonella montanensis LocH:-IAK. a, Anaprotaspis, x 32; b, Metaprotaspis, x 38; c, Paraprotaspis, x 33; d, Early meraspid cranidium, x 28; e, f, Two late meraspid cranidia, x 15, x 12; h, Librigena, x 11; g, Adult cranidium, x 7; i, A meraspid pygidium, x 20; j, k, Two adult pygidia, showing both the inner and outer skeletal surface, x 5, x 9. (all drawings were made from photographs). 591. Ontogeny of three Cedaria zone trilobites 253

Nixonella montanensis LOCHMAN, The present stage is characterized by the well differentiated axial and the ontogeny pleural lobes, and the well depressed Anaprotaspid stage (Pl. 30, fig. 14, and dorsal furrows. Text-fig. 2a).-The shield is rounded, Paraprotaspid stage (Pl. 30, figs. 11-13, convex, and about 0.25 mm in length and Text-fig. 2c).-The shield is oval, (sag.) ; the axial and the pleural lobes divided into a cranidium and a small :are incompletely differentiated; the an­ protopygidium, all about 0.50-0.65 mm in terior axis is deeply impressed by a length (sag.), convex, with the axial and pair of frontal pits on the sides of the pleural lobes well differentiated; the small frontal lobe, and its posterior axis axial lobe is cylindrical, expanded slight­ is ended into a small rounded node; a ly forward, with the axial rings indis­ pair of short superciloid ridges extend tinctly marked; the broadly rounded postero-laterally from the margin of the frontal lobe is well delimited by a pair frontal lobe, which are well delimited of distinct anterior pits, and by short by anterior pits and border furrows; superciloid ridges; behind the super­ the pleural lobe is rather broad, convex, ciloid ridges is a pair of faint elevated and slightly above the narrow axis; no palpebral ridges which arch forward inner marginal furrow is marked. The and are well delimited by furrows; the shield surface is faintly granulated. occipital ring is well defined by furrows, Two or three specimens are assigned convex, and transverse-oval. The fixi­ to the present stage but are mostly in­ gena or the pleural lobe is about one -complete. The figured specimen here and one-half the width of the glabella, suggests the axial region is narrow, convex, with the posterior border curv­ depressed, and with a few coarse grains. ing inward; the posterior border furrow These coarse grains are possibly the is well defined, and its extreme lateral limestone matrix. end is turned forward before it reaches Metaprotaspid stage (Pl. 30, fig. 15, and the marginal border; the protopygidium Text-fig. 2b).-The shield is about 0.40 is subtriangular, convex, divided into mm in length (sag.), round or oval in two to three thoracic segments, and all outline, and has the axial and pleural are freely articulated. The surface of lobes which are faintly demarked by the exoskeleton is covered by faint dorsal furrows; the axis is rather nar· granules. row, cylindrical, with the frontal lobe The present stage is characterized by slightly expanded forwardly; no axial a protopygidium, axial and pleural lobes ring or ring furrow is visible; the being well differentiated, and the distinct posterior end of the axis or the occipital posterior fixigenal border present. ring is convex, and well defined by Early meraspid stage (Pl. 30, figs. 7-10, furrows; the pleural lobe is broad about and Text-fig. 2d).-The cranidium is twice as wide as the axis, convex, slight­ trapezoidal, with posterior border broad­ ly above the axis; the posterior margin er than the anterior one (tr.), convex, Df the shield is surrounded by a narrow about 0.55 to 0.80 mm in length (sag.); flat band, which is broad laterally and the glabella is long, cylindrical, with the narrower to the posterior axis to form anterior margin slightly expanded for­ a shallow embedding. The skeletal sur­ wardly, and four indistinctly divided face is covered by fine granules. glabellar segments are visible; the 254 Chung-Hung HU anterior segment is the largest, and are elevated and distinctly delimited by those of the followings-2nd, 3rd, and the palpebral furrow ; the palpebral 4th-are about equal in size; a narrow ridge is faint, but traceable, it is con­ and elevated anterior border appears nected to both of the palpebral lobe and along the anterior margin ; the anterior the antero-lateral glabellar margin; the pits are visible on the small specimens, broad posterior fixigena is convex, down­ but becomes shallower or absent on the ward sloping, and has the narrow border larger ones; the palpebral lobe is well well delimited by broad and deep border elevated and separated from the anterior furrows; the postero-lateral fixigenal border by a narrow transverse area; the border is elevated from the border fur­ occipital ring is deeply delimited by an row, and about the same width as the occipital furrow, convex, arches poste­ occipital ring (tr.). The skeletal surface riorly. The fixigena is about the same is faintly granulated. width as the glabella; the posterior During the present period, the glabella. lateral fixigena is convex, slopes down­ is developed from the cylindrical to ob­ ward both rearly and laterally from the longus shape, the anterior border in­ deeply impressed dorsal furrow, with creases the width, the fixigena becomes narrow posterior border deeply sepa­ narrower, and the palpebral lobe is rated by the furrow, and about one and located nearly on the mid-line of the one-half width of the occipital ring. glabella (tr.). The skeletal surface is faintly granu­ Remarks: The ontogenetic develop­ lated. ment of the present species is similar The present stage differs from the to those of cedariods, but in comparing previous one in that the anterior border the same sized skeletons, the glabella is appears, anterior pits are shallower or broader, and without any median ex­ absent, palpebral ridge is separated from pansion. The morphogenesis of the the anterior border and the facial suture present species is also similar to those is turned onto the dorsal surface to of Kingstonia ara (WALCOTT) (Hu, 1968a) show the proparian type. and Komaspidella laevis RASETTI (Hu,. Late meraspid stage (Pl. 30, figs. 3-5, 1970). Thus, these three species might and Text-fig. 2e, f).-The cranidium is represent the members of the same convex, trapezoidal in outline, about 1.0 to family, and with close phylogenetic re­ 1.5 mm long (sag.) ; the oblongus glabella lationship. is rounded anteriorly, and without dis­ Figured specimens: Anaprotaspis, tinct glabellar furrows; no preglabellar U. C. M. 40280m; Metaprotaspis, U. C. M. field ; the anterior border is rather broad 40280n; Paraprotaspides, U.C.M. 40280j-l; and convex, crescentic, and delimited Early meraspides, U.C.M. 40280f-i; Late by a deep and broad anterior furrow; meraspides, U.C.M. 40280c-e. the occipital ring is convex, mid-line broader than the sides, delimited by a deep occipital ring and bearing a minute Family Spinagnostidae HOWELL, 1935 median tubercle; the fixigena is slightly narrower than the glabella, convex, Genus Baltagnostus LOCHMAN, 1940 below the glabella ; a pair of small nar­ Baltagnostus beltensis LOCHMAN row palpebral lobes are situated in front of the mid-line of the glabella (tr.); they Pl. 30, figs. 22-35, and Text-fig. 3a-e. 591. Ontogeny of three Cedaria zone trilobites 255

Baltagnostus beltensis LacHMAN in LoCH· border is narrow, delimited by a distinct MAN & Du::-;c.~:-.1, 1944, p. 138, pl. 12, figs. border furrow, about one-half width of 3-5. the occipital ring, and associated by a Baltagnostus wyomingensis LocHl\!Al' & Hu, pair of short posteriorly directed spines 1960, p. 822, pl. 99, figs. 1-4. at its extreme lateral corners. The Cf. Baltagnostus wyomingensis LoCHMA!\ & Hu, 1960, p. 822, pl. 99, fig. 32. thoracic segment is convex; axial lobe. very broad and convex, and lenticular Diagnosis: Cranidium quadrate or with the half ring furrow indistinctly rounded. convex; axial lobe or glabella marked; the pleural lobe is short, about narrower than the pleural lobe; pre­ one-half width as the axis (tr.), and glabellar field narrower than the pleural curves strongly posteriorly; the pleural lobe, no central furrow; first axial ring furrow is deep and marked along the round, and the following ones indistinct ; center of the pleural lobe. anterior furrow broad, convex. Tho­ Pygidium is rounded or roundly quad­ racic segment narrow; axial lobe broad; rate, convex. occupied with a large and pleural lobe about one-half vvidth of the broad axial lobe, and delimited by nar­ axis. Pygidium quadrate or rounded, row and faint dorsal furrows; the axial convex; three axial rings; terminal seg­ rings are indistinctly divided by ring ment broadly expanded; posterior border furrows; the first axial ring is narrow,. convex; posterior furrow broad and the second is medium sized, ornamented concave. by a small median tubercle, and the Description: The cranidium is nearly third one is the largest, roundly ex­ quadrate or roundly quadrate in outline, panded posteriorly, and marked by two convex; glabella conical, convex, above pairs of rounded pits on equal distances; the pleural lobes, well defined by dorsal on the nearly posterior axial margin a furrows; the first glabellar segment or tiny median node is marked, which is the frontal lobe is rounded, convex, and surrounded by well depressed furrow;. isolated by furrows ; the 2nd to 4th the pleural lobe is about one-half width glabellar segments are indistinctly dif­ of the axis, convex, slopes downward, ferentiated, and connected by a narrow and decreases in width posteriorly; the and elongated longitudinal ridge; a posterior border is convex. increases in small but distinct node is located on the width posteriorly, and is defined by a central portion of the third axial seg­ broad deep border furrow ; a pair of ment; the occipital ring is rather nar­ short broad based spines extends rearly row, convex below the posterior glabella, from the postero-lateral margin. The and connected with a pair of triangular exoskeleton is covered by faint granules .. nodes laterally ; the preglabellar field is Remarks: The present species re- slightly narrower than the pleural lobe, presents more than 30 cranidia and convex, downwardly sloping from the pygidia. The materials consist also of a anterior glabella, marked without lvngi­ few of Kormagnostus sp. specimens, but tudinal median furrow; the anterior all are poorly preserved. The cranidium furrow is deep and broad, concave, and of Baltagnostus beltensis is quite dif­ has a median notch toward the pre­ ferent from that of Konnagnostus sp. glabellar field; the anterior border is and it is impossible to misidentify. The broad, convex, and decreases in width pygidium of both species closely resem­ postero-laterally; the pleural fixigei'.al ble each other, and are almost indistin- 256 Chung-Hung Hu

a b c d

e

Text-fig. 3. Baltagnostus beltensis LaCHMAN. a, Early meraspid pygidium, x 28; b, Late meraspid pygidium, x 12; c, d, An adult crani­ dium and a pygidium, x 7; e, A thoracic segment, x 8. (all drawings were made from photographs).

Explanation of Plate 29

Figs. 1-34. Syspacheilus dunoirensis (MILLER). 1. An anaprotaspis, notice the indistinctly developed axis. x50, U. C. M. 40279. 2. A metaprotaspis, showing the well differentiated axial and pleural lobes. x 50, U. C. M. 40279a. 3-5. Three paraprotaspides, showing the presence of their protopygidia. 3, x 36, U. C. M. 40279b; 4, x 36, U. C. M. 40279c; 5, x 45, U. C. M. 40279d. ·6-9. Four early meraspid shields, showing the presence of their anterior border and proto­ pygidia. 6, x 30, U. C. M. 40279e; 7, x 32, U. C. M. 40279f; 8, x 25, U. C. M. 40279g; 9, x 20, U. C. M. 40279h. 10-13. A few late meraspid cranidia, showing the glabella iucreases the width from cylin­ drical to oblong and the surface covered with large and small granules. 10, x 19, U. C. M. 40279i; 11, X 12, u. C. M. 40279j; 12, X 18, u. c. M. 40279k; 13, X 12, u. c. M. 402791. 14, 23, 25, 26, 31. Four different sized male cranidia. 14, x 8, U. C. M. 40279m; 23, x 8, U. C. M. 40279v; 25, X 5, U. C. M. 40279x; 26, 31, profile and dorsal views of a cranidium, x 4, U. C. M. 40279c'. 15, 20, 32. The librigenae; male, 15, x 6, U. C. M. 40279n; 20, x 5, U. C. M. 40279s; female, 32, x 5, U. C. M. 40279e'. 18, 19, 22, 30. Four different sized female pygidia. 18, x 9, U. C. M. 40279q; 19, x 8, U. C. M. 40279r; 22, x 2, U. C. M. 40279u; 30, x 3, U. C. M. 40279b'.

161 17, 24, 33, 34. Four different sized female cranidia. 16, x 8, U. C. M. 40279o; 17, x 6, U. C. M. 40279p; 24, x 6, U. C. M. 40279w; 33, 34, top and side views of a cranidium, x 2, U. C. M. 40279d'. 21, 27-29. Four different sized male pygidia. 21, x 4, U. C. M. 40279t; 27, x 5, U. C. M. 40279y; 28, x 8, U. C. M. 40279z; 29, x 6, U. C. M. 40279a'. Hu : Ontogeny of three Cedaria zone trilobites Plate 29

2 3 4 5 6

13 10 9 8 7

14 15

17 18

25 24

29 26 27 28 30

31 32 33 34 591. Ontogeny of three Cedaria zone trilobites 257 guishable. However, th.e present species granules. Some small pygidia are as­ has a slightly narrower pygidial axis sociated with thoracic segment. and the posterior axial lobe slightly Late meraspid stage (Pl. 30, figs. 30, 34, touches the border furrow, whereas the and Text-fig. 3b).-The pygidial shield axis of Kormagnostus sp. is broader and is quadrate, or rounded, convex, about running into the border furrow. 1.5 to 2.5 mm in length (sag.) ; the axis Both Baltagnostus wyomingensis LocH­ is oblongus, consists of three indistinctly MAN & Hu and Cf. B. wyomingensis divided axial rings, but of the 1st and LOCHMAN & Hu reported from Wyoming 2nd segments are about the same size, have the conical pygidial axis and are and the last one is the largest ; the last apparently the immature forms of B. axial segment is rounded, convex, and beltensis. marked by two pairs of granules on the central surface, and a small one at the posterior median line; the pleural lobe Baltagnostus beltensis LOCHMAN, is about-one-half the width of the axis, ontogeny decreases in width from the posterior lateral margin to the posterior median The material which I have studied furrow ; the posterior border furrow is contains the smallest cranidium about broad, convex, the posterior border is 1.1 mm in length and the largest one convex with a rear median notch di­ reaching to 4.0 mm (sag.), showing the rected to the axial terminal portion, and continuous . size variation within the a pair of short marginal spines is di­ limits of these scales, but morphologically rected rearly from the lateral margin. they are almost without differentiation. The present stage differs from the Therefore, the cranidium gives no valu­ early one in that the axial lobe is sub­ able criterion for dividing up the growth quadrate, terminal segment increases in stages of the animal. The present as­ width, posterior median furrow is nearly signations of the growth stages are invisible, and the pleural lobe decreases based merely on the pygidium. in width. Early meraspid stage (Pl. 30, figs. 27- Remarl

·divisions. Univ. of Cincinnati, Ohio (accepted for Figured specimens: Cranidia, U. C. M. publication of Paleontographica Ameri­ 40281, 40281 a-d; Thoracic segment, cana, vol. 7, no. 44, 1971). U. C. M. 4028lk ; Pygidia, U. C. M. 4028lj, -- (1968b) : Notes on the ontogeny and sexual dimorphism of Upper Cambrian m; Early meraspid pygidia, U. C. M. trilobites of the Welleraspis faunule from 40281e-g, i; Late meraspid pygidia, Pennsylvania. jour. Nanyang Univ., vol. U. C. M. 4028lh, l. 2, p. 321·-357, pis. 1-4. -- (1970) : Ontogenies and sexual dimor­ References phisms of two Upper Cambrian trilobites. Proc. Geol. Soc. China, No. 13, p. 143-155, HowELL, B. F. and DuNCAN, D. (1939) : pis. 1, 2. Middle·Upper Cambrian transition faunas LocH~IAN, Ch. (1936) : New trilobites genera in North America. Wagner Free Inst. from the Bonneierre dolomite (Upper Sci., Bull., vol. 14, no. 1, p. 1-11, pl. 1. Cambrian) of Missouri. jour. Paleont., Hu, C. H. (1968a) : Ontogeny and sexual vol. 10, p. 35-43, pl. 9. dimorphism of Lower Paleozoic Trilo· -- (1940) : Fauna of the basal Bonneterre bit a; unpublished Ph. D. disertation, dolomite (Upper Cambrian) of South-

Explanation of Plate 30

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

17 18 2

6 7 19 3

20

11 12 22

14

30 23

29

25

24

27

26 33 591. Ontogeny of three Cedaria zone trilobites 259

eastern Missouri. Ibid., vol. 1, p. 1-53, -- (1961) : Upper Cambrian faunas from pis. 1-5. the northwest Wind River Mountains, -- (1950) : Upper Cambrian faunas of the Wyoming, Part II. Ibid., vol. 35, p. 125- Little Rocky Mountains, Montana. Ibid., 146, pis. 26-30. vol. 24, p. 322-349, pis. 48-51. -- (1962) : Upper Cambrian faunas from -- (1959) : Treatise on Invertebrate Pale­ the northwest Wind River Mountains, ontology, (Part 0), Arthropoda 1. Geol. Wyoming, Part Ill. Ibid., vol. 36, p. 1-28, Soc. Amer. & Univ. Kansas Press, p. 302. pis. 1-7. -- and Du:-iCAN, D. (1944) : Early Upper MILLER, B. M. (1936) : Cambrian trilobites Cambrian faunas of central Montana. from northeastern Wyoming. Ibid., vol. Geol. Soc. Amer. Spec. Paper, no. 54, 181p, 10, p. 35-43, pl. 8. pis. 4-17. PALI\IER, A. P. (1955): Upper Cambrian ·- and Hu, C. I-I. (1960) : Upper Cambrian Agnostidae of the Eureka district, faunas from the northwest Wind River Nevada. Ibid., vol. 29, p. 86-101, pis. 19, Mountains, Wyoming, Part I. jour. 20. Paleont., vol. 34, p. 794-834, pis. 59-100. Trans. Proc. Palaeont. Soc. Japan, N. S., No. 85, pp. 260-274, pis. 31, 32, April 20, 1972:

592. ON THE LEPIDOLINA ZONE DISCOVERED FROM THE SHIMA PENINSULA, SOUTHWEST JAPAN*

NOBUO Y AMAGIW A

Institute of Geoscience, Osaka Kyoiku University

and

YUKIY ASU SAKA

Institute of Earth Science, School of Education, Waseda University

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

Geological summary ments between longitudinal faults, and form, as a whole, the so-called sandwich Previously the writers (1967) reported structure. The northern boundary fault explanatorily on the geology and geo­ of the middle sub-belt is called the Ara­ logical structure of the Chichibu terrain shima-Gokasho tectonic line (Y AMAGIWA, in the eastern part of the Shima penin­ 1957), which is easily traced owing to sula. Kinki District. In this part of the serpentinite intruding along its whole peninsula, the Chichibu terrain is divided extension. Some authors regard this into the northern, middle and southern tectonic line as an eastern equivalent of sub-belts as is that of Shikoku. Each the Kurosegawa zone (!CHIKA w A et a!., sub-belt trends NE-SW to NNE-SSW, 1956) elucidated in Shikoku (e. g., HAMA­ and is separated from each other by DA, 1963). Several lenticular bodies of marked faults. Of these sub-belts, the serpentinite crop out sporadically along northern one alone consists exclusively the southern marginal fault, too. of the Palaeozoic Chichibu complex, In the middle sub-belt the Jurassic while the other two are intercalated and the Cretaceous strata are distributed with narrow slices of the Mesozoic sedi- along with the Chichibu complex. The * Received March 6, 1971; read January former, trapped in a narrow strip, is 25, 1969 at Tokyo and November 22, 1970 at correlated with the Upper Jurassic Ima­ Hiroshima. ura group which occupies the northern 260 592. Fusulinids from Shima 261

marginal part of the southern ~ .. ri sub-belt. The latter, named the Matsuo group, is distributed se­ parately in three narrow zones. Its age is verified palaeontologi­ cally to be of the lower Creta­ ceous, Kochian epoch. The Chichibu complex consti­ tuting the middle sub-belt is known as the Horikiri, the Aono­ mine and the Toya groups. The Horikiri group, correlated with the Middle Carboniferous system is exposed as small lenses along the southern boundary fault. The Aonomine group constitutes two zones covering the widest area in the middle sub-belt. Sev­ Text-fig. 1. eral fusulinid fossils found from it indicate its age to be the Middle Fossil locality .... X 1. ... Shiranezaki, 2 .... Toya, 3 .... Imaura, to Upper Permian period*. On 4 .... Ogurajima, 5 .... Omurajima, 6 .... Motoura. the other hand, no useful fossils had been gained from the Toya group which is bounded both on the northern southeasternmost part of the "Toya and the southern sides by the Matsuo group" on the geological map. These group up to the time when the writers fusulinid-bearing strata are bounded both previously described the geology of this on the north and the south by longitudi­ district. The writers, on this account, nal faults and form a small block which presumed the age of the Toya group to measures no more than 35m in width be the Permian period, judging from its (namely in the direction perpendicular lithofacies and geological situation. to the general strike). On the south,. Recently, the writers discovered the they are in contact with the alternation Lepidolina multiseptata multiseptata-L. of sandstone and shale, subordinate kumaensis fauna from the strata which constituent of the Lower Cretaceous Ma- they had previously included in the Toya . tsuo group; on the north, in contact group. The strata in question are ex­ with the semi-schist belonging to the posed in the sea-cliff on the Toya coast Toya group barren of fossils. Along facing to the east and constitute the the northern boundary fault, serpentinite intrudes, as is usually observed along * Neoschwagerina sakaguchii and N. fuji­ the longitudinal faults demarcating each motoi were discovered from the lower part group within the middle sub-belt. Here of the Aonomine group (YAMAGIWA, 1956; YA:VIAGIWA and SAKA, 1967), and Yabeina in this paper, the writers, laying stress katoi, Y. packardi shimensis and Y. omuren­ on the occurrence of this small block, sis from the upper part (Y AMAGI w A, 1956; and regarding it as separate from the YAMAGIWA and ISHII, 1958; YAMAGIWA and fossil-free Toya group, propose to call SAKA, 1967). it the Toba group. The writers have 262 N obuo YAM AGIWA an d Y~~k i yas~~ SA K A

T ext-fi g . 2. The outcrop of t he Toba g roup at Toya, Toba City , M ie Prefecture. The fossils were collected from sandstone lenses conta ined in the contorted shale. SS . .. . Sandstone, SH .... Shale. confirmed the occurrence of this group The mineral composition corresponds to in no other places than along the Toya that of low rank g reywacke according coast, and conclude that it was squeezed to KR YN INE's classification. Under a out as a lenticular body along the fault microscope, grains, irregular in shape which forms the boundary between the and in size, are mostly in plane-contact, Toya group and the Matsuo group. rarely in suture-contact. Some quartz­ The Toba group consists mainly of grains show wavy ex tinction. Igneous sandstone and shale, with subordinate rocks occurring as fragments in sand­ tuff, chert and limestone. Each stratum stone are acidic andesite and diabase, is so much disturbed that the above­ all having suffered alteration. Meta­ mentioned rocks except shale are torn morphic rocks contained are crystalline off into irregular-shaped fragments of schists of low metamorphic grade*. various sizes scattered in the contorted Tuff is alterej too, and is andesitic shale, thus showing a cataclastic con­ in tex ture and composition. Chert is glomeratic aspects. Sandstone, frequent­ green in colour. ly penetrated by calcite veins, is com­ Each stratum of the Toba g roup forms posed mainly of quartz- and feldspar­ a homoclinal structure, striking N50 o- grains cemented by the matrix of argil­ 70 °E and either dipping steeply to the laceous material. B.esides occasional patches of shale, small amounts of frag­ * These meta morphic and ig neous rocks ments of chert, limestone igneous and will be described in detail in future after a metamorphic rocks are also contained. close examination. 592. Puwulinids from Shima 26:3 north or standing vertically. KANMERA (1953, 1954) divided the Up­ Fusulinid fossils were found not from per Permian system (Yabeina zone) of limestone which, occurring as small Japan into the upper and lower sections: lenses, is crystalline and white in colour, According to him, the lower one. char­ but from small sandstone lenses contain· acterized by the Yabeina globosa fauna. ed in the contorted shale. Examination is represented by the Yabeina zone of of about eighty thin sections revealed Akasaka limestone in the Mino belt, and the following fossils: the upper one, characterized by the Lepidolina toriyamai fauna, is represent- Lepidolina lntmaensis . ed by the Kuma formation (Lepidolina Lepidolina multiseptata gigantea toriyamai zone) cited above. On the Lepidolina multiseptata multiseptata other hand, HANZAWA and MURATA (1963) Yabeina columbiana expressed an exactly opposite view, that Yabeina aff. globosa is, the Lepidolina fauna corresponds to Metadoliolina gravitesta the Neoschwagerina zone which underlies Pachyphloia sp. indet. the Yabeina zone represented by the Though the outer volutions of these Yabeina globosa fauna. YABE(1964b, 1965, 'fossils are partly broken, they are never 1966) and TORIY AMA (1967) regarded the rounded to such a degree as would be Y abe ina globosa zone represented by the -expected in case they had been trans­ Akasaka limestone as contemporaneous ported to some distance. The writers with the Lepidolina toriyamai zone re­ conclude, on this account, that they are presented by the Kuma formation plus allochthonous fossils in the strict sense the Yabeina shiraiwensis zone represent­ :but not derived ones. ed by the Akiyoshi limestone in Chu­ goku. TORIY AMA, taking note of the Geological age components of these faunal assemblages and of variance of the lithofacies, pro­ The faunal assemblage of the above posed the name " Kinshozan facies " for mentioned fossils except Yabeina aff. the sequence containing the Yabeina globosa is closely similar to that known globosa fauna, and the " Kuma facies " from the Kuma formation in Kyushu for that containing the Lepidolina tori­ ·(KANMERA, 1953, 1954), the Mizukoshi yamai fauna. He further advocated that formation in Kyushu (YANAGIDA, 1958), the Yabeina zone in Japan, represented the Maizuru group in Kinki (NOGAMI, by the Kuma facies should be renamed 1958), the Haigyu formation in Shikoku Yabeina shiraiwensis-Lepidolina toriya­ (SUY ARI, 1962) and the I waizaki limestone mai zone. in Kitakami (CHOI, 1970a), so that the age Recently, OZAWA (1970) expressed a of the Toba group is undoubtedly refer­ new opinion concerning the Upper Per­ red to the Upper Permian. Only dis­ mian biofacies of Japan. According to parity recognized between the Toba him, the V erbeekinoidea fauna known group and the others is that Yabeina from the Upper Permian system consists :aff. globosa, which has never been re­ of two groups, the Y abeina globosa fauna ported to occur in the latter, co-exists and the Lepidolina multiseptata fauna. with other fusulinids in the Tobp. group, Y abeina globosa, Y. pachardi, Neoschwa­ and that only the Toba group is inter­ gerina katoi, N. minoensis, etc. are typi­ -calated with chert and tuff. cal of the Yabeina globosa fauna. The 264 Nobuo YAMAGIWA and Yukiyasu SAKA

Lepidolina multiseptata fauna is subdi­ difference from the Kuma formation and vided in to the Lepidolina multiseptata other stratigraphic units characterized shiraiwensis-Colania douvillei fauna of by the Lepidolina multiseptata multisep­ the lower horizon and the Lepidolina tata-Lepidolina kumaensis fauna. multiseptata multiseptata-Lepidolina ku­ maensis fauna of the upper horizon. The Acknowledgements former, represented by Lepidolina multi­ septata shiraiwensis, Colania douvillei, Here the writers wish to express their­ etc. is considered as contemporaneous hearty thanks to Prof. Emeritus H. Fu­ with the Yabeina globosa fauna. Lepido­ JIMOTO of Tokyo University of Educa­ lina kumaensis, L. multiseptata multi­ tion. Prof. Emeritus S. MATSUSHITA of septata, etc. are representative of the Kyoto University, Prof. Emeritus I. MA­ latter, which, he insisted, is the most TSUZAWA of Nagoya University and Prof.. evolved type of V erbeekinoidea. Here, S. SAKAGUCHI of Osaka Kyoiku Univer­ what the writers should pay special at­ sity for their kind guidance. The writ­ tention to is that, according to OzAWA, ers are deeply grateful to Prof. K. NA­ no cases are known where the Y abe ina KAZA wA of Kyoto University and Prof. globosa co-exists with the Lepidolina K. IcHIKAWA of Osaka City University multiseptata fauna. for their suggestions on the geologicaL Several problems are left unsolved on structure. The writers express their­ the biostratigraphy and biofacies of the gratitude to Assist. Prof. K. KANMERA Upper Permian Yabeina zone in Japan, of Kyushu University, Lect. K. ISHII of as the writers have reviewed above. Osaka City University, Dr. Y. NOGAMI The Lepidolina-bearing fauna that the of Kyoto University and Dr. T. OZAWA writers lately found from the Toba group of Kyushu University for their kind is exactly alike that from the Kuma advice in the study of the fusulinids. formation in Kyushu with respect to its Acknowledgement is also due to Lect .. faunal assemblage, and is considered to T. YAMAZAKI of Osaka Kyoiku Univer­ correspond to the Lepidolina multiseptata -sity for his kind suggestion in the multiseptata-Lepidolina kumaensis zone study of the igneous and metamorphic of OzAwA. Occurrence of Y abeina aff. rocks in thin sections. Thanks are also­ globosa in this fauna is worthy to note, due to Mr. T. HABUCHI, Mr. T. IWAHA­ because, as OzAWA alreadly pointed out, SHI, Mr. T. MISI-IIMA, Miss Y. MORIMOTO, there has ever been known no parallel Miss K. Y AZUMI, Mr. S. OKAMOTO, Miss­ case on record where Yabeina globosa Y. YAMANE, Miss M. T AZIMI and Miss occurs in the Lepidolina multiseptata M. TSUCHIY A for their assistance in col­ fauna. The fact that Y abeina aff. globosa lection of samples in the field survey. co-exists with the members of the Lepi­ Photographic work was done by Mr. M. dolina multiseptata fauna in the Toba UcHIDA and Mr. T. IWAHASHI, to whom group may contribute to the interpreta­ the writers extend their thanks. tion of the Upper Permian stratigraphy and biofacies in Japan. Also, it is inter­ esting that, as alreadly stated, the Toba Systematic description group, consisting mainly of sandstone Order Foraminiferida and mudstone with minor amounts of chert and tuff, shows some lithological Suborder Fusulinina VON MOLLER, 187&- 592. Fusulinids from Shima 265

Superfamily Verbeekinoidea STAFF is large; with outside diameter of 0.45 and WEDEKIND, 1910 to 0.65 mm. Spirotheca is thin, composed of a tectum and a thin keriotheca with Family Neoschwagerinidae DUNBAR fine alveoli, measuring 0.005 to 0.01 mm. and CONDRA, 1928 The heights of the first to the 11th volution of the above mentioned speci­ Subfamily Lepidolininae MIKLUKHO­ men are 0.10, 0.10, 0.12, 0.12, 0.12, 0.10, MAKLA Y, 1958 0.15, 0.16, 0.19, 0.18 and 0.17 mm, respec­ tively. Axial septula and primary trans­ Genus Lepidolina LEE, 1933 verse septula present throughout shell Lepidolina multiseptata gigantea (GUBLER) and slender. Primary transverse septula come into contact with the top of para­ Plate 31, fig. 1 chomata. Secondary transverse septula were first 2nd volution: and one septu­ 1935. Neoschwagerina megaspherica var. gi­ lum developed between adjacent primary gantea GuBLER, Mem. Soc. Geol. France, Nov. Ser., T. 11, Fasc. 4, pp. 116-118, ones, but beyond the fourth volution one pl. 3, figs. 6, 8, 10?. to two ones are generally present; they 193S. Neoschwagerina douv£/lei GUBLER, Ibid., are of generally bar-like shape, but in pp. 111-113, pl. 7, figs. 7, 8, pl. 8, fig. rare cases pendant shaped. 6; pl. 6, fig. 2?; pl. 7, fig. 10?; pl. 8, Remarks:-The distinct characters of fig. 10?. the present specimens are their large 1954. Yabeina gubleri KANMEH.A, Mem. Fac. proloculus, very thin spirotheca and Sc£. Kyushu Univ., Ser. D, vol. 4, no. elongate fusiform with inflated central 1, pp. 19-21, pl. 4, figs. 1-13. part. The features mentioned above 1958. Y abe ina gubleri: NoGAtvii, Mem. Coli. pratically agree with those of Lepidolina Sci. Univ. Kyoto, Ser. B, vol. 25, no. 2, multiseptata gigantea (GUBLER, 1935; pp. 103-104, pl. 1, figs. 5-6. KANMERA, 1954; NOGAMI, 1958; CHISAKA, 1960. Y abeina gubleri: CHISAKA, Jour. Coli. Art. Sci. Chiba Univ., val. 3, no. 2, pp. 1960; ISHII & NOGAMI, 1964) from the 250-251, pl. 6, figs. 1-4; pl. 7, figs. 1-6; Upper Permian of Japan and Cambodia. pl. 8, figs. 1-5. The present form closely resembles L. 1964. Yabeina multiseptata gigantea: IsHII kumaensis KANMERA (KONISHI, 1952; and NoGAMI, jour. Geosci. Osaka City KANMERA, 1954; YANAGIDA, 1958; No­ Univ., val. 8, Art. 2, pp. 20-22, pl. 6, GAM!, 1958; CHISAKA, 1960; SUY AI~ I. 1962; figs. 1-4. HASEGA WA,1965; CHOI,1970a; Y AMAGIWA & SAKA, in this paper) and L. multisep­ Description :-Shell is large, elongate tata multiseptata (DEPRAT, 1912, 1914; fusiform with inflated central part; their 0ZA WA, 1922; COLAN I, 1924; GUBLER, lateral slopes gently concave. Inner two 1935; THOMPSON, 1948; SKINNER & WILD, · volutions are spherical or subspherical, 1954; ISHII & NOGAMI, 1964; SADA & .and the third to fifth are inflated fusi­ YOKOYAMA, 1966; YAMAGIWA & SAKA, form. Beyond the 6th volution shell in this paper) in its large proloculus, form resembles its mature shape. Sev­ very thin spirotheca and other important ·eral outer volutions are missing. The characters. However, the former one can specimen illustrated as fig. 1 on Plate 31 be distinguished from the latter, having is 9.2 mm in length and 3.5 mm in width, elongate fusiform with inflated central _giving a form ratio of 2.6. Proloculus part. 266 Nobuo Y AMAGIWA and Yulciyasu SAKA

lSHil and NOGAMI (1964) described this 1924. Neoschwagerina mu!tiseptata : CoLAN!. species under the generic name of Ya­ Mfmz. Serv. Geol. Indochine, vol. 11, beina and then they divided it into three fasc. 1, pp. 154-155, pl. 15, fig. 1; pl. subspecies, namely Y. multiseptata multi­ 24, figs. 12-13; pl. 25, figs. 1-8, 10-12, 14-15; pl. 26, figs. 1-2, 4, 6-18. septata, Y. multiseptata gigantea and Y. 1935. Neoschwagerina mu!tiseptata: GuBLER, multiseptata shiraiwensis. Very recently, Mfnn. Soc. Geol. F1·ance, Nov. Ser. T. OzAwA (1970) discussed the difference 11, fasc. 4, pp. 119-123, pl. 3, fig. 5; pl. between Y abe ina and Lepidolina. Ac­ 6, figs. 1, 3, 8-10; pl. 7, fig. 5. cording to him, Lepidolina is distinguish­ 1935. Neoschwagerina megasphaerica, Gull­ ed from Yabeina by having larger pro­ LER, Ibid., pp. 114-116, pl. 7, fig. 3; loculus in the megalospheric generation, pl. 6, fig. 4. larger, elongate shell of the microspheric 1948. Neoschwager£na multiseptata: THO~IP­ generation and the essential difference SON, Protozoa, Art. 1, Univ. Kansas, in the thickness and shape of septa and pp. 66-67, pl. 20, figs. 5-6; pl. 22, figs. septula. In the above respects, this sub­ 1-5. 1954. Lepidolina multiseptata : SKII'\:'\ER and species should be referred to Lepidolina. WILD, jour. Pa!eont., vol. 28, no. 4, pp. The present specimens are megalosph­ 449-450, pl. 52, figs. 1-5. eric form. 1954. Yabeina yasubaensis, KANMERA, Mem. Occurence :-The present specimens oc­ Fac. Sci. Kyushu Univ., Ser. D, vol. 4, cur from the Toba group at Toya, Toba no. 1, pp. 18-19, pl. 2, figs. 10-13; pl. City, Mie Prefecture, Southwest Japan. 5, figs. 14-19. The present form is associated with 1964. Y abe ina multiseptata multiseptata: IsHII Lepidolina kumaensis, L. multiseptata and NoGAMI, jour. Geosci. Osaka City multiseptata, Yabeina columbiana, Yabe­ Univ., vol. 8, Art. 2, pp. 17-20, pl. 3, ina aff. globosa, Metadoliolina gravitesta figs. 1-3; pl. 4, figs. 1-3; pl. 5, figs. 1-4. 1966. Y abe ina multiseptata multiseptata : SA­ and Pachyphloia sp. indet. DA and YoKOYAMA, Trans. Proc. Repository :-It is deposited in the col­ Pa!eont. Soc. japan, N. S., no. 63, pp. lection of the Institute of Geoscience, 304-307, pl. 33, figs. 4-5, 7-8. Osaka Kyoiku University. Reg. nos. 71001, 71002, 71003. Description :-Shell is medium, inflated fusiform. Inner two or three volutions are spherical or subspherical, and beyond Lepidolina multiseptata mulliseptata 5th volution shell form resembles its mature shape. A few outer volutions (DEPRAT) are missing. Shell at 11th volution in Plate 31, fig. 2 our typical specimen (Plate 31, fig. 2) is 6.0 mm in length and 3.6 mm in width; 1912. Neoschwagerina (Sumatrina) multisep­ form ratio about 1.7. Proloculus is large tata, DEPRAT, Mhn. Serv. Geol. Indo­ and spherical. Its outside diameter is chine, vol. 1, fasc. 3, pp. 53-55, pl. 3, 0.45 to 0.65 mm. The heights of the first figs. 2-8. 1914. Neoschwagerina (Sumatrina) multisep­ to the 11th volution are 0.13, 0.13, 0.14,. tata, DEPRAT, Ibid., vol. 3, fasc. 1, pp. 0.12, 0.14, 0.15, 0.17, 0.18, 0.19, 0.20 and. 34-35, pl. 5, figs. 7-11. 0.17 mm, respectively. Spirotheca is very 1922. Neoschwagerina (Yabeina) hayasakai, thin, composed of a tectum and a kerio­ OZAWA, Geol. Soc. Tokyo, jour., vol. theca with very fine alveoli. Thickness 29, no. 348, pp. 369-370, pl. 4, fig. 2. of spirotheca is 0.01 mm in outer volu- 592. Fusulinids from Shima 267 tions. Septa, axial septula and primary pp. 159-161, pl. 14, figs. 2-5, 7. transverse septula present throughout 1954. Lepidolina kumaensis, KANMERA, Mem. shell and slender. Secondary transverse Fac. Sc£. Kyushu Univ., Ser. D, vol. 4, septula first appear in the second volu­ no. 1, pp. 22-24, pl. 5, figs. 1-13. 1954. Lepidolina toriyamai, KANMERA, Ibid., tion. One septulum occurs between ad­ pp. 24-26, pl. 6, figs. 1-19. jacent primary ones in inner volutions 1958. Lepidolina cfr. toriyamai: YANAGIDA, and one or two septula occur in outer jour. Geol. Soc. japan, vol. 64, no. 752, volutions. Parachomata come into con­ p. 228, text-fig. 2. tact with the top of primary transverse 1958. Lepidolina kumaensis: NoGAMI, Mem. septula near the center of chamber. Coll. Sci. Univ. Kyoto, Ser. B, vol. 25, Remarks:-The present subspecies no. 2, pp. 104-105, pl. 2, figs. 8-9. closely resembles Lepidolina multiseptata 1958. Lepidolina toriyamai: NoGAMI, Ibid., shiraiwensis (OZAWA, 1925; FUJIMOTO, pp. 105-106, pl. 1, figs. 1-2. 1936; TORIY AMA, 1942, 1958; CHEN, 1956; 1958. Lepidolina toriyamai maizuruensis, No­ GAM!, Ibid., p. 106, pl. 2, figs. 1-5. MORIKAWA, 1956, 1958; NOGAMI, 1958, 1960. Yabeina Proboscis: CHISAKA, jour. Coll. & 1961; CHISAKA, 1960, 1962; ISHII No­ Art. Sci. Chiba Univ., vol. 3, no. 2, pp. GAM!, 1961, 1962; SADA & YOKOYAMA, 252-253, pl. 9, figs. 1-3. 1966; CHOI, 1970) in many important re­ 1962. Lepidolina kumaensis: SuYARI, jour. spects, but differs from the latter in Gakugei Tokushima U1!1:v., vol. 12, pp. having larger proloculus and thinner 38-39, pl. 12, figs. 2-4. spirotheca. It is similar to L. multisep­ 1965. Lepidolina kumaensis : HASEGAWA, Chi­ tata gigantea (GUBLER, 1935; KANMERA, kyu Kagaku, no. 76, pp. 27-32, pl. 1, 1954; NOGAMI, 1958; CHISAKA, 1960; ISHII fig. 1-5, pl. 2. & NOGAMI, 1964; YAMAGIWA & SAKA, in 1970. Lepidolina kumaensis: CHOI, jour. Fac. this paper). However, the former one Sc£. Hokkaido Univ., Ser. 4, vol. 14, no. 3, pp. 321-324, pl. 5, figs. 1-9, pl. 6, differs from the latter, having inflated fig. 1. fusiform in shape. The present speci­ mens are megalospheric form. Description :-Shell is moderately large, Occurrence:-These specimens found elongate subcylindrical form. A few out­ in the Toba group at Toya, Toba City, er volutions are crushed away. Inner Mie Prefecture, Southwest Japan; the two volutions are spherical or subsph­ associated fossils are Lepidolina kuma­ erical, and beyond the 4th volution shell ensis, L. multiseptata gigantea, Yabeina form resembles its mature shape. Ma­ columbiana, Y. aff. globosa, Metadoliolina ture specimen (Plate 31, fig. 3) having 10 gravitesta and Pachyphloia sp. indet. volutions is 6.2 mm in length and 2.1 Repository:-The present form is de­ mm in width: with form ratio of about posited in the collection of the Institute 3.0. Proloculus is large, spherical in of Geoscience, Osaka Kyoiku University. shape; its outside diameter about 0.3 Reg. nos. 71004, 71005, 71006, 71007. mm. The heights of the first to the lOth volution of the above mentioned one are 0.05, 0.06, 0.05, 0.07, 0.09, 0.10, 0.12, 0.10, Lepidolina kumaensis KANMERA 0.11 and 0.12 mm, respectively. Spiro­ theca is very thin, composed of a tectum Plate 31, fig. 3 and a extremely very finely alveolar 1952. cfr. Sumatrina annae, KoNISHI, Trans. keriotheca, but partly of a single layer. Proc. Palaeont. Soc. japan, N. S., no. 5, Thickness of the spirotheca never ex- 268 Nobuo YAMAGIWA and Yukiyasu SAKA ceeds 0.01 mm in the whole volutions. Subfamily Neoschwagerininae DUNBAR Primary transverse septula occur and CONDRA, 1928 throughout shell. Secondary transverse septula appear first in the third and two Genus Y abeina DEPRA T, 1914 (sometimes three) of them developed between adjacent primary transverse Yabeina columbiana (DAWSON) septula in the 6th to the outer volutions. Plate 31, fig. 4 They are pendant or thin bar·like shaped. Parachomata occur throughout 1879. Loftusia columbiana, DAWSON, Qaurt. shell, and they come into contact with jour. Geol. Soc. London, vol. 35, pp. the top of primary transverse septula 69-75, pl. 6, figs. 1-7. 1942. Yabeina columbiana : THOMPSON and near the center of chamber. WHEELER, jour. Paleontology, v:ol. 16, Remarks:-The present specimen is no. 6, pp. 708-710, pl. 106, fig. 5; pl. characterized by its large proloculus, 107, fig. 5; pl. 108, fig. 1; pl. 109, figs. elongate subcylindrical fusiform in shape 1-4. and very thin spirotheca. These fea­ 1950. Y abe ina columbiana :THOMPSON, WHEE­ tures practically agree with those of LER and DANNER, Contribution from Lepidolina kumaensis KANMERA from the Cushman Foundation for Foramini­ the Kuma formation (KANMERA, 1954) fera Research, vol. 1, pis. 3-4, pl. 61, and other Upper Permian in Japan (No­ pl. 8, figs. 1-3. GAMI, 1958; YANAGIDA, 1958; SUY ARI, 1954. Y abe ina columbiana : KANMERA, Mem. Fac. Sci. Kyushu Univ., Ser. D, vol. 4, 1962; HASEGAWA, 1965; CHOI, 1970). It no. 1, pp. 16-18, pl. 3, figs. 1-7. is closely similar to L. multiseptata gi­ 1958. Yabeina columbiana : NoGAMI, Mem. gantea (GUBLER, 1935; KANMERA, 1954; Call. Sci. Univ. Kyoto, Ser. B, vol. 24, NOGAMI, 1958; CHISAKA, 1960; ISHII & pp. 101-102, pl. 1, figs. 9-10. NOGAMI, 1964; YAMAGIWA & SAKA, in 1960. Yabeina columbiana: CHISAKA, jour. this paper) in many important charac­ Call. Art. Sci. Chiba Univ., vol. 3, no. ters. The former is, however, different 2, p. 249-251, pl. 7. fig. 3. from the latter in having elongate sub­ cylindrical fusiform in shape. It is a Description :-Shell is medium in size, megalospheric specimen. inflated fusiform. Several outer volu­ Occurrence :-A specimen was obtained tions are missing. A specimen (Plate from the Toba group at Toya, Toba City, 31, fig. 4) of 11 volutions is 4.7 mm in Mie Prefecture, Southwest Japan. It is length and 3.1 mm in width; form ratio associated with Lepidolina multiseptata 1.5. Proloculus is small, spherical in gigantea, L. multiseptata multiseptata, shape; its outside diameter is 0.14 mm. Yabeina columbiana, Y. aff. globosa, Meta­ The heights of the first to the 11th doliolina gravitesta and Pachyphloia sp. volution of the above mentioned one are indet. 0.05, 0.07, 0.07, 0.11, 0.14, 0.14, 0.17, 0.15, Repository :-It is deposited in the col­ 0.16, 0.16 and 0.17 mm, respectively. lection of the Institute of Geoscience, Spirotheca is thin, composed of a tectum Osaka Kyoiku University. Reg. no. and a thin keriotheca with fine alveoli. 71008. Thickness of the spirotheca is 0.01 to 0.015 mm in outer volutions. Primary transverse septula are present through­ out shell. Secondary transverse one first 592. Fusulinids Jrorn Shirna 269

appear in the fourth volution, and there 1936. Yabeina globosa: FuJIMOTO, Sci. Rept. is one secondary transverse one in most Tokyo Bunrika Daigaku, Sec. C, vol. 1, cases between adjacent primary trans­ pp. 119-120, pl. 24, fig. 25, figs. 1-4. verse ones. They are rather irregular in 1961. Yabeina g!obosa: MoRIKAWA and Suzu­ shape. Parachomata extend to the top KI, Sci. Rept. Saitama Univ., Ser. B, vol. 4, no. 1, pp. 67-68, pl. 10, fig. 2, of the primary transverse one near the pl. 21, fig. 1. ·Center of the chamber. 1962. Yabeina g!obosa: SuYARI, jour. Gaku­ Remarks:-The present specimen is gei, Tokushima Univ., Nat. Sci., vol. 12, ·closely allied to Yabeina columbiana pp. 37-38, pl. 12, fig. 1. (DAWSON) described and illustrated from the Upper Permian of Japan (KANMERA, Description :-Shell is medium and 1954; NOGAMI, 1958; CHISAKA, 1960) and fusiform; with bluntly pointed poles, British Columbia (THOMPSON & WHEELER, straight axis of coiling. Lateral slopes 1942; THOMPSON, WHEELER & DANNER, of mature shell are nearly straight and 1950) in having small proloculus, inflated slightly convex. Several outer volutions fusiform, relatively thin spirotheca and are missing. Inner three volutions are other important respects. It resembles spherical or subspherical, and beyond Y abeina globosa (Y ABE, 1906; OzAwA, the 3rd volution shell form resembles 1927; FUJIMOTO, 1936; MORIKAWA & its mature stage. The specimen illust­ SUZUKI, 1961; SUYARI, 1962) .. However, rated as fig. 1 on Pia te 32 is 3.9 mm in the former one can be distinguished length and 2.7 mm in width, with form from the latter by its larger proloculus, ratio of 1.4. Proloculus is small, spheri­ thinner spirotheca and more loosely cal or subspherical in shape, with out­ ·coiled inner voluions. side diameter of 0.02 to 0.04 mm. The Occurrence :-A specimen was obtained heights of the first to the 12th volution from the Toba group at Toba, Toba .of the above mentioned specimen are ·City, Mie Prefecture, Southwest Japan. 0.04, 0.03, 0.045, 0.07, 0.10, 0.10, 0.105, 0.14, It is associated with Lepidolina lwma­ 0.15, 0.17, 0.20 and 0.15 mm, respectively. ensis, L. multiseptata gigantea, L. multi­ Spirotheca is rather thin, composed of septata multiseptata, Yabeina aff. globosa, a tectum and a keriotheca with very Metadoliolina gravitesta and Pachyphloia fine alveoli, measuring about 0.02 to sp. indet. 0.03 mm in later stage. Septal count is Repository :-It is deposited in the difficult because of numerous axial sep­ collection of the Institute of Geoscience, tula. Axial septula first appear in the Osaka Kyoiku University. Reg. no. 6th volution. Primary transverse sep­ 71009. tula present throughout shell. Second­ ary transverse septula first appear in Yabeina aff. globosa (YABE) the 6th or 7th volution ; there is one septulum between two adjacent primary Plate 32, figs. 1-6 transverse ones, but in rare cases the two occur in outer volutions. Paracho­ 1906. Neoschwagerina globosa, YABE, jour. Coli. Sci. Imp. Univ. Tokyo, vol. 21, no. mata occur throughout shell; they come 5, p. 4, fig. 4, pl. 2, fig. 1. into contact with the top of the primary 1927. Neoschwagerina globosa: OzAWA, jour. transverse septula near the center of Fac. Sci. Imp. Univ. Tokyo, Sec. 2, vol. chamber. 2, pp. 159-160, pl. 42, figs. 1-2, 4, 6. Remarks:-The present form is closely 270 Nobuo YAMAGIWA and Yukiyasu SAKA similar to Y abeina globosa (Y ABE, 1906; 1954. Pseudodoliol£na n. sp. ?, KANMERA, OZAWA, 1927; FUJIMOTO, 1936; MORI­ I bid., pp. 14-15, pl. 2, figs. 7-8. KAWA & SUZUKI, 1961; SUYARI, 1962) in 1954. Verbeekina? n. sp., KANMERA, Ibid., having small proloculus, inflated fusi­ pp. 15-16, pl. 2, fig. 9. 1960. Pseudodoliolina pseudolepida gravitesta: form in shape, rather thin spirotheca CIIISAKA, jour. Colt. Art. Sci. Chiba and other characters. However, the Univ., vol. 3, no. 2, p. 246, pl. 4, figs. former one is represented by the speci­ 1-6. mens whose several outer volutions are 1961. Metadoliolina gravitesta: IsHII and No­ missing, so the detailed characters can GAM!, Trans. Proc. Palaeont. Soc. japan, not be determined with accuracy. It re­ N. S., no. 44, pp. 163-164, pl. 25, figs. sembles closely Yabeina sp. indet. de­ 1-4. scribed and illustrated from the Tsuiji group (Upper Permian) in the southern Description :-Shell is medium, elongate sub-belt of the Chichibu terrain in Shima ellipsoidal and broadly rounded polar re­ Peninsula by YAMAG IW A (1969) in many gions. Inner three volutions are spheri­ improtant characters. The latter one cal or subspherical, and beyond the may belong to Y abeina globosa. fourth volution shell form resembles its Occurrence:-The present specimens mature stage. A specimen of 10 vo­ occurred from the Toba group at Toya, lutions is 4.7 mm in length and 1.9 mm in Toba City, Mie Prefecture, Southwest width; form ratio about 2.6. Perhaps. Japan. The associated fossils are Lepido­ a few outer volutions are missing. Pro­ lina kumaensis, L. multiseptata gigantea, loculus is small, spherical, and its out­ L. multiseptata multiseptata, Yabeina side diameter is 0.20 mm. The heights columbiana, Metadoliolina gravitesta and of the first to the lOth volution are 0.05, Pachyphloia sp. indet.. 0.04, 0.07, 0.07, 0.08, 0.09, 0.12, 0.13, 0.14 Repository:-They are deposited in the and 0.16 mm, respectively. Spirotheca is collection of Geoscience, Osaka Kyoiku rather thick, composed of a thin tectum University. Reg. nos. 71010, 71011, 71012, and a thin keriotheca with very fine 71013, 71014, 71015. alveoli. In outer volutions, the upper surface of the tectum is coated with a more or less discontinuous layer of Family Verbeekinidae STAFF dense material which is continuous with and WEDEKIND, 1910 parachomata. Thickness of the spiro­ Subfamily Mise!lininae MIKLUKHO­ theca in the fourth to the lOth volution are 0.01, 0.01, 0.007, 0.10, 0.01, 0.015 and MAKLAY, 1958 0.02 mm, respectively. Parachomata are Genus Metadoliolina ISHII well developed, and heights of them are and NOGAMI, 1961 a half of the heights of the chamber~ they are massive. Metadoliolina gravitesta (KANMERA) Remarks:-This form is represented by an axial section and another trans­ Plate 31, figs. 5-6 verse section alone. It is referable 1954. Pseudodoliolina pseudolepida gravitesta, to Metadoliolina gravitesta (KANMERA,. KANMERA, Mem. Fac. Sci., Kyushu 1954; CHISAKA, 1960; ISHII & NOGAMI, Univ., Ser. D, vol. 4, no. 1, pp. 12-14, 1961) from the Upper Permian in Japan. pl. 2, figs. 1-6. The two ones are closely similar to each 592. Fusulinids from Shima 271 other in having relatively thick spiro­ 75, pl. 6. theca, elongate ellipsoidal form in shaps, DEPRAT, J. (1912) : Etude des Fusulinidb small proloculus, tightly coiling in inner de Chine et d'lndochine et classification volutions and other important charac­ des calcaires a fusulines. Mem. Serv. ters. Geol. l'Indochine., vol. 1, fasc. 3, pp. 1- 76, pis. 1-9. Occurrence:-The present specimens -- (1914) : Etude des Fusulinides du Japon, have been obtained from the Toba group du Chine et d'Indochine classification des. at Toya, Toba City, Mie Prefecture, calcaires a fusulines (III• Memoire). Southwest Japan. It is associated with Etude comparative des Fusulinides Lepidolina kumaensis, L. multiseptata d'Akasaka (Japon) et des fusulinides de· gigantea, L. multiseptata multiseptata, Chine et d'Indochine. Ibid., vol. 3, fasc. Yabeina columbiana, Y. aff. globosa and 1, pp. 1-45, pis. 1-8. Pachyphloia sp. indet .. FUJIMOTO, H. (1936) : Stratigraphical and Repository:- The present ones are palaeontological studies of the Titibu deposited in the collection of the Insti­ System of the Kwanto-mountainland. Pt. 2, Palaeontology. Sci. Repts., Tokyo Bun-· tute of Geoscience, Osaka Kyoiku Uni­ rika Daigaku, Sec. C, vol. 1, no. 2, pp. versity. Reg. nos. 71016, 71017. 29-125, pis. 1-26. GuBLER, J. (1935) : Les Fusulinides de Per­ mien de i'Indochine, leur structure et References leur classification. Soc. Geol. France,. Mem., New. Ser., tome ll, fasc. 4, no. 26,. CHEN, S. (1956): Fusulinidae of South China, pp. 1-173, pis. 1-8 (17-24). Pt. 2. Palaeont. Sinica, New Ser. B, no. HAMADA, T. (1963) : The Gokasho-Arashima 6, pp. 17-71, pis. 1-14. fault zone in Mie Prefecture. jour. Geol. CHISAKA, T. (1960) : On some Permian fu­ Soc. japan, vol. 69, no. Sll, pp. 208-209. sulinids from the Takagami Conglom­ HASEGAWA, Y. (1965): "Lepidolina" from erate, Choshi Peninsula, Chiba Prefec­ the Otani conglomerate, Central Japan. ture, Japan. jour. Coll. Art. & Sci., "Earth Science" (Chikyu Kagaku), no. 76,. Chiba Univ., val. 3, no. 2, pp. 235-250, pp. 25-33, pis. 1-3. pis. 1-9. HANZA\\·A, S. & MuRATA, M. (1963): The -- (1962) : Fusulinids from the vicinity of Paleontologic and stratigraphic consider­ Maiya town, Kitakami mountainland, ation on the Neoschwagerininae and and Upper Permian fusulinids of Japan. Verbeekininae, with the descriptions of Ibid., val. 3, no. 4, pp. 519-551, pis. 1-8. some fusulinid foraminifera from the CHOI, D. R. (1970a) : On Some Permian Fu­ Kitakami massif, Japan. Sci. Repts. To­ sulinids from Iwaizaki, N. E. Japan. hoku Univ., 2nd Ser. (Geology), vol. 35,. jour. Fac. Sci., Hokkaido Univ., Ser. 4, no. 1, pp. 1-31, pis. 1-20. val. 14, no. 3, pp. 313-325, pis. 5-8. IcHIKAWA, K. et al. (1956): Die Kurosegawa -- (1970b) : Permian fusulinids from Imo, Zone (Untersuchungen i.iber das Chichibu­ Southern Kitakami Mountains, N. E. Terrain in Shikoku III). jour. Geol. Soc. Japan. Ibid., pp. 327-354, pis. 9-15. japan, vol. 62, no. 725, pp. 82-103. CoLAN!, M. (1924): Nouvelle contribution a lsi·III, K. & NoGAMI, Y. (1961) : On the !'etude des Fusulinides de !'Extreme­ new genus Metadoliolina. Trans. Proc. Orient. Indochine Service Geol., Mhn., Palaeont. Soc. japan, N. S., no. 44, pp. val. 11, fasc. 1, pp. 1-191, pis. 1-29. 161-166, pl. 25. DAWSON, G. M. (1879): On a new species -- & -- (1962) : On Yabeina shiraiwensis. of Loftusa from British Columbia. Quart. OzAwA and Yabeina yasubaensis ToRI­ jour. Geol. Soc. London, val. 35, pp. 69- YAMA. jour. Geosci., Osaka City Univ., 272 Nobuo YAMAGIWA and Yukiyasu SAKA

vol. 6, art. 2, pp. 59-72, pis. 1-2. -- et al. (1958) : Stratigraphical and bio­ -- & -- (1964) : Contribution to the geol­ stratigraphy of the "lwaizaki limestone" ogy and palaeontology of Cambodia, Pt. in the southern Kitakami mountainland. 1, Permian fusulinids. Ibid., vol. 8, art. jub. Pub!. Prof. H. FUJIMOTO, pp. 81-90, 2, pp. 9-37, pis. 1-8. pl. 6. KANMERA, K. (1953) : The Kuma formation -- & SuzuKI, Y. (1961); Fusulinids from with special reference to the Upper the Akasaka limestone, Pt. 2, Sci. Rept. Permian in Japan (Geological study of Saitama Univ., Ser. B, vol. 4, no. 1, pp. the Palaeozoic in Southern Kyushu, pt. 43-74, pis. 4-22. 3). jour. Ceo!. Soc. japan, vol. 59, no. NoGAMI, Y. (1958) : Fusulinids from the 697, pp. 449-468. Maizuru Zone, Southwest Japan. Pt. 1. -- (1954) : Fusulinids from the Upper Ozawainellinae, Schubertellinae and Neo­ Permian Kuma Formation, Southern Kyu­ schwagerininae. Mem. Coil. Sci., Univ. shu, Japan-with special reference to the Kyoto, Ser. B, vol. 25, no. 2, pp. 97-114, fusulinid zone in the Upper Permian of pis. 1-2. Japan. Mem. Fac. Sci., Kyushu Univ., -- (1961) : Permische Fusuliniden aus dem Ser. D, vol. 4, no. 1, pp. 1-38, pis. 1-6. Atetsu-Plateau Siidwest Japan, Teil 2, -- (1957) : Revised classification of Cancel­ Verbeekininae, Neoschwagerininae. Ibid., tina and Neoschwagerina, and evolution vol. 28, no. 2, pp. 159-244, pis. 1-7. of Sumatrininae and Neoschwagerininae. OzAwA, Y. (1.922): Permian note on the Ibid., vol. 6, no. 1, pp. 47-64, pis. 19-20. classilication of the family Fusulinidae. KoNISHI, K. (1952) : Permian microfossils jour. Geol. Soc. japan, vol. 29, pp. 352- in the Dodo conglomerate of the Yasuba­ 365. type. Trans. Proc. Palaeont. Soc. japan, -- (1925) : Palaeontological and stratigra­ N. S., no. 5, pp. 155-165, pl. 14. phical studies on the Permo-Carboni­ MoRIKAWA, R. (1956): Fusulinids from Ona­ ferous limestone of Nagato, Pt. 2, Pal­ gata, Kamiyoshida-mura, northern part aeontology. jour. Coli. Sci., Imp~ Univ. of Kanto mountainland. Sci. Rept., Sai­ Tokyo, vol. 45, art. 6, pp. 1-90, pis. 1-14. tama Univ., Ser. B, vol. 2, no. 2, pp. 250- -- (1927) : Stratigraphical studies of the 260, pis. 32-34. Fusulina limestone of Akasaka, Province -- (1960) : Fusulinids from the lwaizaki of Mino. jour. Fac. Sci., Imp. Univ. limestone. Ibid., vol. 3, no. 3, pp. 273- Tokyo, Sec. 2, vol. 2, pt. 3, pp. 121-164, 299, pis. 46-53. pis. 34-46.

Explanation of Plate 31

Fig. 1. Lepidolina multiseptata gigantea (GUBLER). Axial section .... x 15 Fig. 2. Lepidolina multiseptata multiseptata (DEPHAT). Axial section .... x 15 Fig. 3. Lepidolina kumaensis KAI':VIERA. Axial section .... x 15 Fig. 4. Yabeina columbiana (DAwsoN). Axial section .... x 15 Figs. 5-6. Metadoliolina gravitesta (KAN:VIERA). 5. Transverse section .... x 20 6. Axial section .... x 20 Fig. 7. Pachyphtoia sp. indet. Transverse section? .... x 40 Y AMAGIWA and SAKA: Fusulinids from Shima Plate 31 592. Fusulinids from Shima 273

OZAWA, T. (1970): Notes on the phylogeny -- (1967): The Fusulinacean Zone of Japan. and classification of the superfamily Mem. Fac. Sci., Kyushu Univ., Ser. D,. Verbeekinoidea (Studies of the Permian vol. 18, no. 1, pp. 35-260. verbeekinoidean Foraminifera-l). Mem. YABE, H. (1906) : A contribution to the Fac. Sci., Kyushu Univ., Ser. D, vol. 20, Genus Fusuiina, with notes on a Fusu­ no. 1, pp. 17-58, pis. 1-9. lina limestone from Korea. jour. Colt. SADA, K. & YoKoYAMA, T. (1966): Upper Sci., Imp. Univ. Tokyo, vol. 21, art. 5,. Permian fusulinids from the Taisyaku pp. 1-36, pis. 1-3. limestone in west Japan. Trans. Proc. -- (1964a) : Lepidoiina Problem. Proc. fa· Palaeont. Soc. Japan, N. S., no. 63, pp. pan Acad., vol. 40, no. 3, pp. 214-219. 303-315, pis. 23-24. -- (1964b) : Problems on the genus Lepido­ SKINNER, J. W. & WILDE, G. L. (1954) : Fu­ lina (Part 1). "Fossil" (Kaseki), Palaeont. sulinid wall structure. jour. Paleont., Soc. japan, no. 8, pp. 134-139. vol. 28, no. 4, pp. 445-451, pis. 46-52. -- (1965) : Problems on the genus Lepido· SuY ARI, K. (1962) : Geological and palaeont­ !ina (Part 2). Ibid., no. 9, pp. 36-55. ological studies in central and eastern -- (1966) : Problems on the genus Lepido­ Shikoku, Japan, Pt. 2, Palaeontology. lina (Supplement). Ibid., no. 12, pp. 47-55. Tokushima Univ., jour. Gakugei, Nat. YAMAGI\\' A, N. (1954) : Neoschwagerininae Sci., no. 12, pp. 1-64, pis. 1-12. from the Shima Peninsula, Japan. Trans. TlloMPSON, M. L. (1948): Studies of Amer­ Proc. Palaeont. Soc. japan, N. S., no. 23, ican fusulinids., Univ. Kansas, Paieont. pp. 235-242, pl. 32. contrib., Protozoa Art. 1, pp. 1-184, pis. -- (1957) : Stratigraphy and geological 1-38. structure of the eastern area of Shima -- & WHEELER, H. E. (1942) : Permian Peninsula. jour. Ceo!. Soc. japan., vol. Fusulinids from British Columbia, Wash­ 63, no. 740, pp. 263-272. ington and Oregon. jour. Paleont., vol. -- (1969) : Tsuiji Group in the eastern vol. 16, no. 6, pp. 700-711. area of Shima Peninsula, Mie Prefecture. --, -- & DA:-o;KER, W. R. (1950): Middle Mem. Osaka Kyoiku Univ., III. Nat. & and Upper Permian fusulinids of Wash­ Applied Sci., vol. 18, pp. 71-80, pl. l. ington and British Columbia. Contrib. -- & IsHII, K. (1957): Yabeina from Omu­ Cushman Found. Foram. Research, vol. 1, ra Island, Shima, Mie Prefecture. ]ubi. Pts. 3-4, pp. 46-63. Comm. Prof. H. FUJIMOTO, pp. 58-65, ToRYAMA, R. (1942) : The fusulinids of the pis. 3, 4. Yasuba conglomerate in the Province of -- & SAKA, Y. (1967) : The Mesozoic and Tosa, Japan. jour. Geol. Geogr., vol. 18, Palaeozoic in the eastern part of Shima no. 4, pp. 237-247, pis. 24-25. Peninsula. Guide-boo!? for geologic ex­ -- (1958) : Geology of Akiyoshi, Pt. 3, Fu­ cursion (Nagoya), pp. 1-24. sulinids of Akiyoshi. Mem. Fac. Sci., YANAGIDA, J, (1958): The Upper Permian Kyushu Univ., Ser. D, vol. 7, pp. 1-264, Mizukoshi Formation. jour. Ceo/. Soc. pis. 1-48. japan, vol. 64, no. 725, pp. 222-231.

Imaura 4- irll Shiranezaki 8 iH ~~.~t Motoura * ifll Toba .~ )])] Ogurajima ~~~~ ir J:-h Toy a lilt :fr Omurajima :ktt~ 274 Nobuo Y AMAGIWA and Y~~kiyasu SAKA

--~------Explanation of Plate 32

Figs. 1-6. Yabeina aff. globosa (YABE). 1. Axial section .... x 20 2. Axial section .... x20 3. Tangential section (somewhat oblique) .... x 24 4. Sagittal section .... x 20 5. Tangential section .... x 15 6. Tangential section (somewhat oblique) .... x 15 YAM AGIW A and SAKA : Fusulinids /?"O?n Shima Plate 32 Trans. Proc. Palaeont. Soc. Japan, N. S., No. 85, pp. 275-279, pl. 33, April 20, 1972

59:3. THE TRIASSIC BRYOZOA FROM KUSAKA, SAKAWA BASIN, SHIKOKU, JAPAN

SUMIO SAKAGAMI

Department of Geology, Faculty of Education, Ehime University, Matsuyama, Japan

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

c. 7.J;piifff- ~ :11- .Q 0) ""(' fi}~i'li l? ~ -_t .Q :::. c. l? J1J!"" Q 0 :!;!i J: lrf :k

portunity for study of the present ma­ Introduction and acknowledgements terials. I am also deeply indebted to Some 25 years ago, Dr. Teiichi KOBA­ Professor Kotora HAT AI of the Tohoku YASHI discovered a small bryozoan fauna University for kindly reading the manu­ in a sandstone of the Oxytoma-Mytilus script and for his constant encourage­ beds of the Upper Triassic Kochigatani ment. series at Kusaka in the eastern part of the Sakawa basin, Shikoku island, Japan. Description of species They were identified by him with Ceria­ para sp. and reported in 1948 and 1949, Pseudobatostomella kobayashii but without description. SAKAGAMI, n. sp. Recently, Dr. KOBAYASHI sent me the Plate 33, figs. 1-6. "' Ceriopora " bearing thin sections for study and the present article is a result 1948. Ceriopora sp., KoBA Y ASH!, p. 176. -of the examination. 1949. Ceriopora sp., KoBAYASHI, p. 137. Before going into the description, I would like to express my sincere thanks Six thin sections of fragmentary to Dr. Teiichi KOBAYASHI, Professor zoaria were examined. Zoaria probably Emeritus of the University of Tokyo incrusting in some parts, but consisting for his kindness in giving me the op- of cylindrical stem, about 2.5 to 3.0 mm in diameter. Zooecial tubes subangu­ Received March 6, 1971; read October 22, larly oval in tangential section, their 1971 at Fukuoka. shorter diameter usually ranging from 275 276 Sumio SAKAGAMI

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

Table l.

Entomonotis Beds ·{ tenuic.ostata-zabaikarica Bed Late Noric Upper Division ochotica-densistriata Bed Late Carnic Myoconcha Beds or Early _Noric

Mic!clle Division Hatobia.Tosapecten B·ecls { Tosap~cten Beds .. I Middle Carnic ..• . · ...... , HatobwBeds 1 ·==-----~ :"_ -----··----·------Oxytoma·Mj!Ji{us · Be'ds . Early Carnic 593. Triassic Bryozoa from Sakawa 277 by KOBA Y ASH! from a sandstone of the scribed from the early Upper Triassic Oxytoma-Mytilus beds at Kashiwai of (upper Carnic) of Hungary by VINASSA Kusaka-mura, the Sakawa basin of Kochi DE REGNY (1901), it is of doubtful mate­ Prefecture. rial as mentioned by FLUGEL (1963) and Repository and Specimen No.-The spe­ MOROZOVA (1965). cimens are preserved in the collection Recently, MOROZOV A (1969) described of the Department of Geology, Faculty from the Triassic in USSR, Paralio­ of Education, Ehime University. Reg. clema abnonne MOROZOVA (Carnic, north­ Nos. 1001 (holotype), 1002, 1003, 1004, 1005 western part of Caucusus), Paralioclema and 1006 (paratypes). fonnosum MOROZOVA (Noric, northwest­ ern part of Caucusus), Paralioclema da­ gysi MOROZOVA (Carnic, northwestern Brief note on the Triassic Bryozoa part of Caucusus), Paralioclema amurense of the world MOROZOVA (Anisic, Primorsk), Pseudo­ batostomella sparsa MOROZOV A (Anisic, In the Triassic system, bryozoan re­ northwestern part of Caucusus), Pseudo­ mains are extremely rare in the world. batostomella debilis MOROZOV A (Carno­ FLUGEL (1963) revised the Triassic Bry­ Laclinic, Primorsk) and Pseudobatosto­ ozoa known by that time and recognized mella morbosa MOROZOVA (Carno-Noric, 13 species in 4 genera of Cyclostomata Pamir). and 9 species in 7 genera of Treposto­ Table 2 shows the chronological ranges mata aside from some indeterminable of the Triassic bryozoan species report­ species. Subsequently, however, 10 spe­ eel and/or described after the revision cies of Bryozoa were newly added by by FLUGEL (1963). FRITZ (1961), LAZUTKINA (1963) and Mo­ It is noted that all of the bryozoans ROZOVA (1965, 1970). shown in the table comprise the so-called FRITZ (1961) described and illustrated " relic " from the Paleozoic era except Arcticopora christiei FRITZ from Lake for Arcticopora christiei. a genus that Hazen, northeastern Ellesmere island in was newly established for the species Canada and the geological age was stated by FRITZ (1961). by BoLTON (1961) as " ... There is, there­ FLUGEL (1963) mentioned that "Al­ fore, little doubt that the bryozoan bed though any Lower Triassic (Scythic) bry­ is Triassic, not Permian .... The bryozoan ozoans have not been clescribecl, Fene­ bed is thus not younger than Lower stella and Stenopora type bryozoans have Triassic (early Upper Scythian age)". been reported from the Glyptophiceras­ LAZUTKINA (1963) described one bryo­ Ophiceras bed (lower Scythic) of east zoan species, Pseudobatostomella jakutica Greenland by TRUMPY (1960). They are (LAZUTKINA) under the generic name of expecting to be described by an Amer­ Batostomella from the Lower Triassic ican student." After the revision of (Induan) of Jakutii in Siberia, USSR. FLUGEL, howev·er, three Scythic bryo­ MOROZOVA (1965) reported Polypora zoans were added from Ellesmere island, darashamensis NIKIFOROVA without de­ Siberia and Trans-Caucusia. scription from the Lower Triassic (lower The present article is the first descrip­ part of the Induan stage) of Zakavkas tion of the Triassic Bryozoa in Japan. (Trans-Caucusia). Though one indeter­ However, bryozoan remains but with minable species of Polypora (?) was de- some doubt have recently been recognized 278 Sumw SAKAGAMI

Table 2. 1 Ani. I Lad. I Car. I . Nor. ~~haj 1- Scy. ~--- -~~------I Paralioclenza anzurense MoRozovA Paral. abnorme MoROZOVA I Paral. dagysi MoRozov A I Paral. formosum MoROZOVA Pseudobatostomella jakutica LAZUTKINA --- Pseudob. spars a MoRozov A I I Pseudob. debilis MOROZOVA ; Pseudob. kobayashii SAKAGAMI, n. sp. Pseudob. morbosa MoRozov A i I Arcticopora christiei FRITZ ! --- I Polypora darashanzensis N1 KI FOROV A --- I in the lower member of the Triassic than Permian in age. " Batostomella" ? Nakijin Formation distributed in Okina­ (2) from the Hidaka group seems to be wajima, Ryukyu by ISHIBASHI (1969), but almost identical with Pseudobatostomella no detailed study has been made. On kobayashii, n. sp. described here. Under the other hand, about 30 years ago, Su­ such circumstances the three forms of GIYAMA (1941) described 3 indeterminable " Batostomella" recorded by SUGIYAMA species of " Batostomella" (one of them should be reexamined, but unfortunately with a question mark) from four locali­ the depository of the bryozoan specimens ties of the so-called Hidaka group dis­ studied by him is uncertain. tributed in central Hokkaido and he con­ sidered the geological age of the four localities to be the same because one of References the three "Batostomella" (1) was mutual at the four localities. However, FUKADA BoLTON, T .E. (1961) : Additional Arcticopora from the Triassic of northwestern Elles­ (1949) pointed out that the brachiopod mere island. Proc. Geol. Assoc. Canada, fauna from one of SUGIYAMA's bryozoan vol. 13, pp. 55-56. localities (Iwabenosawa, Simukappu­ FLOGEL, E. (1963) : Revision der triadischen mura), although not the same locality Bryozoen und Tabulaten. Akad. Wiss., of " Batostomella " ? (2) but yielded Wien, Sitzungsber. Abt. 1, Bd. 172, pp. "Batostomella" (1), is Triassic rather 225-252.

Explanation of Plate 33

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

Photo by SAKAGAMI. SAKAGAMI : Triassic Bryozoa from Sakawa Plate 33 593. Triassic Bryozoa from Sakawa 279

·FRITZ, M.A. (1961) : A new bryozoan genus paleozoiskogo rocla Batostomella v triase. from Lake Hazen, northeastern Ellesmere Paleont. Zy., no. 4, pp. 126-128. island. Proc. Geol. Assoc. Canada, vol. 13, MoRozovA, I.P. (1965): BRYOZOA in Razvi­ pp. 53-55, pis. 1-3. tie i smena morskikh organizmov na ry­ FUKADA, A. (1949) : On the Brachiopoda beze paleozoja i mezozoja (edit. RuziiENT­ from the "schalstein formation" in the SEV, V.E. and SARYCHEVA, T.G.). Akad. central mountain range of I-Iokkaido. Nauk SSSR, Trudy Paleont. !nsf., tom. jour. Geol. Soc. japan, vol. 55, nos. 648, 108, pp. 183-197, pis. 25-28. 649, pp. 123-124. -- (1969) : 0 sistematicheskom sostave i IsHIBASHI, T. (1969) : Stratigraphy of the rasprostranenii mshanok v triase. Akad. Triassic formation in Okinawa-jima, Ryu­ Nauk SSSR, Paleont. Zy., 2, pp. 49-57, pis. kyus. Mem. Fac. Sc£., Kyushu UnZ:v., Ser. 7, 8. D, Geology, vol. 19, no. 3, pp. 373-385, pl. -- (1970): Mshanki pozdnei permi. Akad. 53. Nauk SSSR, Trudy Paleont. Jnst., tom. ]{oBAYASlli, T. (1948): The geotectonics of 122, pp. 1-347, pis. 1-64. the Japanese Islands. 2, Meguro Book Co. St.:GIYA:'.IA, T. (1941) : On the geological age ·-- (1949) : Shikoku region. Regional geo­ of the limestone containing Bryozoa in logy of japan. Asakura Book Co. the Hidaka group. jour. Geol, Soc. japan, ·--and IciiiKAWA, K. (1950): On the Up­ vol. 48, no. 571, pp. 189-194. per Triassic Kochigatani series in the VINASSA DE REGNY, P. (1901) : Trias-Tabu­ Sakawa basin in Japan and its pelecypod­ Iaten, Bryozoen unci Hydrozoen aus dem faunas. jour. Fac. Sci., Univ. Tokyo, Sec. Bakony. Resultate wiss. Erforsch. Bala­ 2, vol. 7, pt. 3, pp. 179-206. tonses, Bd. 1, 1, pp. 1-22, pis. 1-3. LAZUTKINA, O.F. (1963) : Nakhodka mshanki

Hidaka province f] l§i IN Motourakawa 7C iill i•'J I''· Iwabenosawa 1 '7 "" Cl) iR Okina wa-jima i

Simukappu-mura do 7& H Trans. Proc. Palaeont. Soc. Japan, N.S., No. 85, pp. 280-292, pl. 34, April 20, 1972

594. SOME BAJOCIAN AMMONITES FROM KIT AKAMI, NORTHEAST JAPAN

TADASHISATO

Geological Institute, Faculty of Science, University of Tokyo

;!U:LIJti!lJ: I) il~LJ-=: _.,\,) 3 '/7 :/l}jlj:fifC-?v'"C: 13;$:C')---\,;/ 3 YT :/f'i 7~:fi{t:fiC')iffi:L1\ i.JqU~I'i':mi\c\ ,; ""7 i/'iC')fi!!.C')n~n-ri E f'IT'$t.J: n-mi.J~c:· ~ t.J:i.J' '? t-::, :li±i.fi:;!tJ:.wtl!lc:·t*l,R-zE ht-:t':l;;Js: c., 4-'i c:·tlc~'i'E hff::::y~'i'E h"Cv't-= tl\'\*'2~N1A-:t'f'Jr:, r~f~!i!l!RC')~;t±ffi:Ji&.:t5 J: LF~Hg$k1tC') Jl 1 imll!ii.J~i.J't.J: IJ <;b u,n-mC')M~ c. t.J: .::s:::. c. i.J~;bi.J, '? t-=. 100;t±ffi:l?-l v'i:£:(:;j;:c:· 1m C. L- "C~ 1J t& ') :::. C. i.J>t: ~, 3- P ,,,_..~t:RifflC') Otoites sauzei m fU•f'lt'i'E;h,.::S, 'it-=:JI Jiml'&f'i, d;-t.J:< C.

Bajocian, as adopted in the recommen­ precisely, a zone which should fall in· dation of the Subcommission of Jurassic the range from Otoites sauzei zone to· of IGC, at the Luxembourg Symposium Stephanoceras humphriesianum zone is in 1962, is represented best by a fraction strongly suggested by these materials. of the Jurassic column in the south Kita­ In this occasion, old but undescribed kami region in Japan. Its correlation specimens of ammonoids collected from is based on the poorly known ammonite the corresponding formations and stored faun ules (SA TO, 1962; TAKAHASHI, 1969), in the University of Tokyo are described besides some lamellibranch faunas (HA­ and figured. These are in favour of YAMI, 1961). attributing the age of the formation to The faunules comprise some charac­ Otoites sauzei zone, in addition to pre­ teristic Bajocian species, but many are viously described Stephanoceras sp. cf. more or less crushed and remained un­ S. plicatissimwn (QUENSTEDT) and Son­ described. ninia sp. cf. S. corrugata (SOWERBY). Better preserved specimens of the am­ The Bajocian is one of the best re­ monites are recently collected by F. TA­ presented stage of Jurassic in the east­ KIZA WA of the Geological Survey and ern and southern parts of the circum­ CHIKARAISHI of the Nihon University, pacific, including western Australia. The from the Ojika Peninsula. These collec­ Bajocian ammonite faunas have, how­ tions comprise some new forms not de­ ever, regional particularities by different scribed yet, and offer more solid basis composition in each area, though inter­ of the correlation. Bajocian, or more connection among neighbouring areas is easily recognized by the occurrence of * Received March 12, 1971; read June 27, certain common genera. Since only a 1970 at Mito. small number of species have been hith- 280 594. Bajocian ammonites j1·om Kitakami 281

erto reported from Japanese Bajocian. it 32, fig. 4a, b. will be useful from the standpoint of 1969. Sonninia sp., TAKA!IASIII, pl. 18, fig. 7, palaeogeography and correlation to give 9, non fig. 3 and ? pl. 19, fig. 7. ?1969. Hosoureites cf. ikianus (YoKoY Al'vlA), notes here on the newly found faunules. TAKA! lASH!, pl. 19, fig. 8. The ammonites of the Japanese Juras­ sic are generally quite poorly preserved. Material :-A single specimen pre­ The test is usually lost, and the casts served to the end of the whorl. but the are twisted by the later tectonic defor­ test was completely removed. Collection mation. This is particularly true for the HAY AMI. Kitakami Jurassic, where specimens suf­ Description:-The whorls become ellip­ ficiently well preserved for full system­ tical due to the compression acted obli­ atic description are rarely found up to quely to the axis of coiling. Diameter the present. measured along the longer axis is about The newly discovered specimens re­ 55 mm and that of the shorter axis about present Bajocian families of Sonninidae. 30 mm. Thus the maximum diameter Otoitidae, Stephanoceratidae and prob­ would be of the order of 40 mm or more. ably Strigoceratidae. The combination The umbilical diameter is about 20 mm of these families are reported widely along the longer axis, thus occupies from the Pacific. The common elements about 36% of the diameter. are recognized between Japan and these This is a small form with spatulate countries. Among these, the south Alas­ lappets. The ventral aspect is not clearly kan fauna is the most closely related to visible but on the internal mould is ob­ the Japanese one, as in the case of servable well differentiated low hollow Toarcian and Aalenian (SA TO, 1962a). keel as a trace of narrow flat belt sur­ I am much indebted to Mr. T AKIZA w A rounding probably fastigate venter. The .and Mr. CHIKARAISHI for kind permission whorl section can not be confirmed cor­ ·Of studying their materials, and to Prof. rectly because of flattening, but is likely HAT AI for granting me to refer to the to be rather elongated oval. The volu­ .collection of the Tohoku University. tion is rather evolute. Umbilical wall is Thanks are also due to Dr. TAKAHASHI steeply inclined, with rounder border. for his critical discussion and to Prof. Costation is generally falcoid, rather WESTERMANN for his critical examina­ rursiradiate, terminating at the ventral tion of the present materials. edge without forward projection, irregu­ larly fasciculate in inner whorls but bundled by umbilical bullae on the last Systematic descriptions whorl. Ribs become abruptly weakened Genus Pelekodites BUCKMAN, 1923 on the last quarter of the last whorl, where somewhat sinuous striae substi­ Pelekodites (Spatulites) spatians t!lte the ribs. (BUCKMAN) Suture line is simple, characterized by slender lobes. Pl. 34, fig. 1a, b. Remarlls :-This species resembles su­ perficially inner whorls of certain Wit­ 1928. Spatulites spatians BucK:VIAI', Type Am­ monites, pl. 765. chellids. Especially fasciculate and flex­ 1969. Pelekodites (Spatulites ?) n. sp. aff. P. iradiate costation is a common character spatians (BcciOIA:'-:), WESTER/\IANN, pl. of the two. 282 Tadashi SA TO

BUCKMAN's genera, created mostly on 1969. Sonninia sp., TAKAHASHI, pl. 17, fig .. the basis of single species, are not gen­ 6, 7 and ? fig. 8; ? pl. 18, fig. 4. erically separable from Pelekodites which has the page priority among others. Material:-Two crushed specimens WESTERMANN (1969, p. 116) further ad­ from black mudstone stored in Univer­ vanced and regards this group of min­ sity of Tokyo. 43IIR -5111, collection ute sonninids as male equivalent of Wit­ YAMASHITA, 5405302, collection AKI­ chellia laeviuscula-W. sutneri 'plexus'. YAMA. He tentatively admitted Spatulites as a Description:-Exact measurements are subgenus of Pelekodites, in taking its impossible because of deformation. Spe­ stronger costation than that of Peleko­ cimen 43IIR-5111 which preserves lap­ dites in consideration. pets is about 35 mm in maximum diame­ The present specimen is conspecific ter along the longer axis, and about 20 with BuCKMAN's spatians, in general ap­ mm along the shorter axis of the de­ pearance, except more prominent umbili­ formed elliptical whorls. Thus the dia­ cal bullae which bundle irregularly two meter measured just behind the aper­ or three flexiradiate costae. However, ture is likely to be of the order of 30 the specimens can be attributed to the mm. The umbilical diameter is about BucKMAN's species, because slight dif­ 15 mm along the longer axis, occupying ferences of costation would be better about 43% of the diameter. considered as intraspecific variation Small shell of rather evolute volution,. rather than specific. with spatulate lateral lappets. Whorls TAKAHASHI's 'GrajJhoceras' sp. A, and are likely to be slightly depressed, with 'Sonninia' sp. A are arbitrary. His pl. broadly convex and keeled venter. Pli­ 18, fig. 7 and fig. 9 (and probably pl. 19, cate costation is appreciably rursira­ fig. 8) are probably conspecific with this, diate, irregularly fasciculate and finally though too much fragmentary to be de­ smooth and striated on the last quarter termined specifically, except pl. 18, fig. of the last whorl. 9, which has the same fasciculate strong Remarks :-Pele!wdites spatians, de­ ribs as in the present specimen. His scribed above, is different by its smaller ' Sonninia' sp. A (pl. 18, fig. 3) should be conch. more markedly rursiradiate cos­ excluded from this species, and compared tation, and weaker umbilical bullae,. to Sonninia sp. cf. S. corrugata (SA TO, though not totally absent. 1962a, pl. 9, figs. 3, 4). This form is in close affinity with the Occurrence:-West of Tsunakizaka, English Pelelwdites pele!cus BucKMAN,. Tsunakizaka Formation. Associated which was only figured but not de­ with Strigoceras sp. which will be de­ scribed. The unfavorable state of pre­ scribed below. servation of the present form does not permit decisive identification. 'Nanno­ ceras nannomorphum' BUCKMAN, 1923, Pelelwdites sp. cf. P. pelekus is another species closely related, but BUCKMAN, 1923 this is not specifically separable from pe/e/ws (WESTERMANN, 1969, p. 116). Pl. 34, fig. 2a, b. TAKAHASHI's 'Sonninia ' sp. A, in 1962a. Sonninia sp., SATO, pl. 9, fig. 2 which 8 specimens are grouped, com­ (5405302). prises largely divergent forms. His pL 594. Bajocian ammonites from Kitakami 283

17, figs. 6 and 7, and possibly fig. 8 as available. well as pl. 18, fig. 4 might be conspecific Occurrence:-Procured from a boulder with the present one. From Wide Bay at the Locality 54044, south of Tsunaki­ of Alaska Peninsula, WESTERMAN:\ re­ zaka. ported Pelekodites cf. P. pelekus (1969, pl. 32, figs. 1-2) which is also closely related and cannot be distinguished from Genus Normannites MUNIER­ the present form even specifically. CHALMAS, 1892 Occurrence :-Specimen 43IIR -5111 from the west of Yobaijitoge, 5405302 from lVonnannites (ltinsaites) sp. cf. Tsunakizaka. Both from Tsunakizaka N. (I.) itinsae (MCLEARN) Formation. PI. 34, figs. 3-9.

1969. Otoites sp., TAKAHASHI, pl. 9, figs. 2-5. Genus Otoites MASCKE, 1907 A1aterial :-Some thirteen fragmentary Otoites sp. specimens which represent various de­ PI. 34, fig. 10. velopmental stages. Description:-All the specimens are Material:-An external mould of the deformed to some extent, obliquely or last half volution found in a boulder. perpendicularly to the coiling axis, so Description:-Though fragmentary, the that the original shell form is difficult specimen shows rather involute coiling, to be confirmed. For the same reason, crater-like umbilicus with well defined it is not quite certain that all the spe­ and steeply inclined umbilical wall. Stout cimens belong to a single species, even and straight primary ribs are on the if each specimen presumbably represents umbilical wall, terminated by minute different developmental stage. rounded tubercles from which two or Coiling is rather evolute; a specimen three secondary ribs are branched off. (Pl. 34, fig. 5b) representing inner three On the last part of the preserved whorl, volutions shows open and shallow um­ however, only two secondary ribs are bilicus. Overlapping of the whorl by bifurcated. Costation as a whole is next one is confined to about outer one generally rectiradiate, but on the last third of the whorl height, and the um­ whorl it becomes slightly geniculated bilical suture lies approximately on the with rursiradiate primaries. line connecting the points of bifurcation Remarlls :-The general appearance, of ribs on the covered whorl. especially costation, is strongly sugges­ Whorl section is likely to be depressed tive of Otoites contractus group. Ribbing oval with broad and gently convex ven­ appears in the present specimen some­ ter. A figured specimen (Pl. 34, fig. 8b) what finer than the group of contractus presents depressed Teloceras-like whorl (SOWERBY), as in Otoites delicatus BucK­ section. But as the impression of the MAN (1919, Type Ammonites, pl. 142). ventral region of the preceding whorl, But this might be resulted from the left on the dorsum, is abnormally nar­ lateral deformation and it will be rea­ row and roof-shaped, this figure is not sonable that the specific determination original but deformed. is not given until better specimen is Short lateral lappets are present (Pl. 284 Tadashi SATO

34, fig. 4). Primary ribs of high relief are long, widely spaced, rectiradiate (slightly prorsiradiate in smaller whorls), and two or more secondaries are bifurcated at the lo wer one third of the whorl height. The latter are finer and more densely spaced, intercalated frequently by free ribs. Minute but clearly dif­ ferentiated tubercles are superimposed on the branching points. Remarlzs :-The possibility that this species belongs to the Stephanoceratidae is excluded because of the presence of lateral la ppets. Furthermore, long pri­ mary ribs and small secondary lateral lobe which is observable in some speci­ mens, are the characteristics favorable to place them in Nonna-nnites, instead of Otoites. But there are some involute Nonnannites superficially indistinguish­ Text-fig. l. Ventro·latera l vie w of t he able from Otoites, and the demarcation obli quely deformed whorl of Normannites between the two genera is riot always (Itinsaites) sp. Loc. I-!67 , Maeami. Col­ easy, as ARKELL stated (1954, p. 568). lection T AKIZ AWA. Among various Nonnannites species, Canadian Itinsaites would be comparable with confidence. But as the umbilical directly to this form by its sharp, hig h, wall is partly observable, and reveals and long primary ribs. Jti nsaites itinsae the Nonnannites t ype umbilical aspect, known from Queen Charlotte Island it is here tentatively retained in the (MCL EARN, 1929, pl. XV, fig. 2-3) and also present species. Cook Inlet of Alaska (IMLAY, 1964, pl. Occurrence :- All the specimens a re 14, fig . 3-8, 13) resembles this species in discovered from a seam of poorly sorted general appearance. silty sandstone, together with lamelli­ T AKA HASHI segregated four indepen­ branch and belemnite shell fragments, dent but monotypical species within his in the state of fossil bank. Judging Otoites, based mostly on the different from the lithology of the mother rock, ribbing styles. However, even in a Stephanoceras sp., which will be de­ single specimen of the present collection, scribed below is associated with this ribbing is divergent from bifurcating to species. H67 (T AKIZ AWA ), Maeami coast, fasciculating. It seems that until better 0 jika Peninsula. specimens will be procured, all is better referred to one species. The largest specimen, more than Ll em Genus Stephanoceras WAAGEN, 1869 in whorl thickness (Text-fig. 1), shows Stephanoceras sp. dense and fine ribbing. This specimen is too much depressed to be determined Pl. 34, fig. 11. 594. Bajocian arnmonites from Kitakami 285

1956. Stephanoceras sp. cf. S. piicatissimum (SA TO, 1956, pl. 13, fig. 1). In an accom­ (QuE:-:STEDT), SATo, p. 169, pl. 13, figs. panying specimen (Ditto, pl. 13, fig. 3) 1-3, text-figs. 2-5. shorter primaries are observable on the last part of the preserved whorl. J'vfaterial:-A single specimen procured No comparable species is yet known irom black sandy shale at Maeami. Col­ among various stephanoceratids report­ lection CHIKARAISHI, his specimen num­ ed from New Guinea, Sula Island, or ber 730123. from West coast of North America Description:-The whorls are lateral­ including South Alaska and British ly deformed and the volution becomes Columbia, where the fauna of compara­ somewhat elliptical; longer axis meas­ tive age is widely developed. ures approximately about 90 mm, while Occurrence:-Maeami. collection CHI­ the shorter axis about 65 mm. KARAISHI. judged from the lithology, A part of the living chamber is pre­ this fossil might be collected from the served as an internal mould. but the same locality as T AKIZA w A's H67. Tsu­ internal whorls are completely destroy­ kinoura Formation after T AKIZA w A. ed, but left impression, in somewhat ob­ scure manner, as an outer cast. The volution seems very evolute. The um­ Genus Strigoceras QuENSTEDT, 1886 bilicus is open and shallow and occupies :about 1/2 of the diameter. Whorl section Strigoceras sp. cf. S. languidum is rounded and as high as thick. (BUCKMAN) Ribbing is composed of stout primary ribs and dense, rectiradiate and gener­ Pl. 34, figs. 12, 13. ally trifurcate secondaries. The second­ 1969. Graphoceras sp., TAKAHASHI, pl. 19, .aries are branched off from the minute figs. 2, 3, 4 and ? 5. but prominent tubercles at the inner one tpird of the whorl height. Intercalato­ lvf at erial:-Two outer casts of flatly ries are frequently inserted. Ribs are compressed and laterally deformed shells, continuous on the venter without any collection l-IA Y AMI. interruption or bending. Description:-The maximum measura­ The suture line is not observable. ble diameter is 40 mm but 20 mm when Remarks:-This planulate ammonite measured along the direction perpendi­ .is comparable to the species described cular to the former, thus the shell is .Previously from the Tsunakizaka shale more or less deformed laterally. The .of the Karakuwa region as Step/wnoceras umbilical diameter is about 4 mm along sp. cf. plicatissimum (QUENSTEDT) ; this the longer axis of the deformation ellipse Karakuwa form is characterized by rath­ of the whorl. er well individualized long primary ribs. Small shell with well differentiated This difference might be caused by more ventral keel and involute coiling. Be­ .advanced degree of deformation than in cause of the flattening by tectonic de­ .the present specimens. In fact, the ribs formation, the exact whorl section is not .appearing along the longer axis of the observable, but it is most likely to be an deformation ellipse look like longer and oxycone. The inner half of the flank is sharper than those along the shorter probably concave. The umbilical margin .axis, as seen in the Karakuwa specimen is sharply defined and the weak spiral 286 Tadashi SATO ridge is formed at the middle height of tary to be attributed to the present the flank. species. The venter is not clearly observable Occurrence:-West of Tsunakizaka. but it is likely to be fastigate. Collection HAY AMI. Collected from the The costation is characterized by the same slab of black shale as Pelekodites falcoid ribs which are much more accen­ (Spatulites) spatians. tuated on the outer half of the flank than on the inner half. The suture line is not visible. Discussion on the occurrence Remarks:-Various oxycone Strigo­ of ammonites ceratids are splitted into independent genera by BUCKMAN. But these are Tsunakizaka Formation: certainly not separable in generic level 1. Tsunakizaka and better put into the same genus This locality is not a pinpoint locality, Strigoceras, as did ARKELL (1957). Stri­ but some ten different localities scatter­ gites strigifer (BUCKMAN, 1924, Type Am­ ed around the site called Tsunakizaka monites, pl. 469A) and ' Varistrigites' are designated under this name. All the compressus (BUCKMAN, pl. 468) are, among specimens procured there occur in the others, closely related to the present black shale named Tsunakizaka Forma­ species, judged by their characteristic tion, which is overlain by argillaceous ornamentation. But a form reported sandstone and underlain by granule from South Alaska by IMLAY under the sandstone, both barren of ammonite. name of Strigoceras cf. S. languidum A specimen of Pelekodites cf. pelekus (BUCKMAN) (IMLAY, 1964, pl. 23, fig. 4) (BUCKMAN) (figured formerly under the is the most resembling species known name of Sonninia sp. indet., SA TO, 1962, in the circumpacific region. pl. 9, fig. 2) was discovered from Loc. This small oxycone is apparently com­ 5405302, together with Sonninia sp. (SATO, parable to Grap!wceras of Upper Toar­ 1962a, pl. 9, fig. 3) and fragmentary Stri­ cian-Aalenian age, especially to the goceras-like shell (yet unfigured) and also group of G. concavum with rather recti­ Stephanoceras sp. (unfigured). From an­ radiate ribbing. TAKAHASHI's ' Grapho­ other important locality, 5405232, Steph­ ceras' sp. B (1969, pl. 19, fig. 4) is judged anoceras sp. cf. S. plicatissimum (QUEN­ to be conspecific with the present spe­ STEDT) (SA TO, 1956, pl. 13, fig. 1) and cies. Although Graphoceras is not easily also Spatulites spatians BUCKMAN which separable from this genus when it is still retains striated last whorl were col­ imperfectly preserved, the latter should lected (Collection AKIYAMA, Kesen-numa be distinguished by its ribbing which is High School). not strongly rursiradiate in comparison Stephanoceras cf. S. plicatissimum (Qu.} with that of the former and is rather ir­ (SATO, 1956, pl. 13, fig. 3) was collected regularly branched, its complex suture­ at the locality 54044, which is correlated line, its very involute coiling. These to the top of the black shale formation, criteria are clearly visible in the present but accompanies no other species. Oto­ specimens. Therefore, the materials now ites sp. described here was unfortunate­ in question are concerned with StJ-igo­ ly collected from the river float, thus ceras. TAKAHASHI's other two specimens bears no stratigraphical significance. (pl. 19, fig. 3 and fig. 5) are too fragmen- Pelekodites, Sonninia and Stephanoceras 594. Bajocian ammonites from Kitakami 287

IN l KS

Text-fig. 2. Locality map around Tsunakizaka. IN: Inai Group, KS: Kosaba Formation, TZ: Tsunakizaka Formation, TZs: Sandstone overlying Tsunakizaka Formation, rW: Ishiwaritoge Formation. are, therefore, completely coexistant from this locality but independently. stratigraphically. Discrimination of dif­ The stratigraphical relation between the ferent fossil horizons is impossible in two species is not clear. this locality. 2. Yobaijitoge The formation from which above This locality is situated about 1 km mentioned species were collected is about north of the pass of the Higashi-hama 350m thick and composed of monotonous road. The fossiliferous shale is exposed black shale. ONUKI (1969, p. 113) cited along the trail crossing the mountain three different fossil horizons within this range. Stephanoceras cf. S. plicatissimum formation: this zonation was based on (QUENSTEDT) (SA TO, 1956, pl. 13, fig. 2) unpublished data of TAKAHASHI, who and Pelekodites cf. P. pelekus BuCKMAN eventually discriminated two horizons (specimen 43IIR-5111) are discovered (TAKAHASHI, 1969, p. 33), instead of three. 288 Tadashi SA TO

As discussed above, the Tsunakizaka posed of black sandy shale. The litho­ Formation can not be splitted into zones logy is quite homogeneous. There is no from the faunal view point. Therefore, evidence of disordering of the bedding, TAKAHASHI's result appears to be based such as slumping structure or turbidite. ·On arbitrary splitting of the fauna into Therefore the admixture of the fossils two different lots. In fact, the Tsunaki­ of different ages is hardly admitted in .zaka Formation constitutes a single zone. this sequence. As discussed later in detaiL the am­ Tsuhnoura Formation: monite species discovered from the Tsu­ 1. Maeami. nakizaka Formation can coexist, as far This locality is the sea-side exposure as judged from hitherto known ranges near Maeami, in the east coast of the of every species. Therefore, the whole 0 jika Peninsula. T AKIZA w A's locality Tsunakizaka Formation can be defined H67 yields both Stephanoceras cf. S. pli­ as a zone. .catissimum (QuENSTEDT) and Normanni­ A zone is a biostratigraphical term, tes (Itinsaites) sp. so that the upper and lower limits should These fossils are discovered from a be demarcated by lines on the exposure. ·seam of poorly sorted silty sandstone, It· is not an abstract concept but objec­ together with other lamellibranch and tive. Since the ammonites are confined belemnite shell fragments. Fossils are in the black sandy shale sequence, and more or less crushed and concentrated the sequence cannot be subdivided into in a thin seam as a shell bank. It is smaller units, the formation represents evident that the shells were transported an ammonite zone as a matter of course. by current and brought into depositional site altogether. It is safe to conclude that the species Correlation .composing the Maeami faunule are com­ All the constituents of the faunules pletely synchronous and indicate a single now in question are of Bajocian age. .age. They are known widely around the Pacific. Note on the ammonite zone Tsunakizaka Formation:-The ammonite In Japanese Jurassic, a solitary occur­ faunule of this formation is composed rence of a single individual of fossil of: .ammonites is not rare. The solitary .ammonite is important as a time-indi­ Stephanoceras sp. cf. S. plicatissimum (QuEN­ ·Cator, but cannot define a zone. As I STEDT) previously noticed (SATO, 1962a, p. 40), Sonninia sp. cf. S. corrugata (J. de C. Sow- .the term 'niveau' was used to denote ERBY) Pelekodites (Spatulites) spatians (BucKMAN) the stratigraphical horizon dated by this Pelekodites sp. cf. P. pelekus BucKMAN kind of ammonite occurrence, instead of Otoites sp. using 'zone' of OPPEL's sens. The veri­ Strigoceras sp. cf. S. languidum (B'ucK~·IAN) table zones of ammonites exist in Japa­ nese Jurassic; later I discriminated them Stephanoceras sp. was compared previ­ from ill-defined 'niveaux' (SA TO, 1962b). ously to S. p!icatissimum (QUENSTEDT), The Tsunakizaka Formation is com- but this is open to question. Because 594. BaJ'ocian ammonites from Kitakami 289 the specimens are completely flattened the distribution of the genus would be without exception, the identification is far more wide-spread than supposed at even generically difficult. The specimens present. Pelekodites is yet unknown are characterized apparently by short from the western and southwestern Pa­ and bullate primary ribs which are also cific, and now its presence in Japan comparable to those of Pseudotoites. links paleobiogeographically the north­ Although the exact whorl section is not western and northeastern parts of the known in the present specimens, the Pacific. possibility to belong to this particular Other sonninids reported from Kita­ Pacific genus can not easily be rejected. kami offer another link between Japa­ Pseudotoites cf. P. argentinus ARKELL nese and Southwestern Pacific paleobio­ (figured by WESTERMANN from Wide geographic provinces. Stephanoceratids Bay of Alaska Peninsula) resembles su­ and a dubious Otoites sp. figured herein. perficially this form. Even if this be a corroborate this connection. Pseudotoites, the age which represents Strigoceras is known from South Alas­ the form is not be altered, because both ka (IMLAY, 1964) and doubtful one from are of early-middle Bajocian age. Supplee area of Oregon (LUPHER, 1941). Stephanoceras (including Skirroceras as subgenus) is a genus prolific in the As a whole, the Tsunakizaka faunule Pacific Middle Bajocian. It is so far has a close affinity with those of South reported from Southern Alaska and New Alaska and Western Canada, including Guinea, but the Stephanoceras s. s. is Western Interior of the United States,. relatively rare. Indisputable Stephano­ suggested by the common occurrence of ceras s. s. is known only from West Irian Stephanoceras (though somewhat doubt­ (S. aff. S. humphriesianum (QUENSTEDT)), ful), Pelekodites, Strigoceras and probable British Columbia and Chile (for example Sonninia. Especially Pelekodites is com­ S. coamanoi McLEARN). Numerous S!?ir­ parable between two regions even in roceras from South Alaska and Oregon specific level. are partly transferred to Docidoceras Chronologically important is the Otoi­ (WESTERMANN, 1970, p. 294), of Lower tes, which attained the climax of pros­ Bajocian age. perity in Otoites sauzei zone, although The sonninids reported from Kitakami it appeared already in the upper part of were compared to Sonninia corrugata Sonninia sowerbyi zone. Unfortunately group, but these might belong to the the specimen of Otoites sp. was discov­ subgenus Euhoploceras. Associated Pele­ ered in the river float, but it should be kodites is up ·to now confined to occur derived from the surrounding Tsunaki­ in the Northeastern Pacific. This micro­ zaka black shale, as suggested by its conchiate ammonite is difficult to be de­ lithology. termined unless the aperture is pre­ Among associated genera of the Tsu­ served. Some sonninids ever described nakizaka faunule, Stephanoceras is also and of small shell diameter would be of an indicator of the Otoites sauzei and Ste­ this genus. For example, 'Sonninia sub­ phanoceras humphriesianum zones, not deltafalcata' TORNQUIST (Pl. 5, fig. 7) and that for Sonninia sowerbyi zone. The ' S.' bodenbenderi of the same author presence of Sonninia sp., Pelekodites spp., (pl. 5, fig. 9) from Espinazito Pass of Strigoceras sp. in association with Otoites Argentina might be Pelelwdites. Thus and Stephanoceras cannot reject the 0. 290 Tadashi SATO sauzei zone age, because these range in buted in both sauzei and humphriesianum whole early and middle Bajocian. zones. The Tsunakizaka Formation is, there­ Numerous Normannites (sometimes re­ fore, of the Otoites sauzei zone age. I ported as Otoites) are found in Indonesia previously correlated it with the Steph­ and New Guinea. However, the true (Jnoceras humphriesianum zone (SATO, Normmmites is rather rare. Normannites 1962b, p. 894), but the new collection of etheridgei is an example, and was later :ammonite does not permit to retain this redefined as Stemmatoceras by WESTER­ .correlation. MANN. T AKAHASI-II's Kl horizon (which was The combination of Stephanoceras and correlated with Upper Toarcian-Aale­ Normannites is known both in Otoites nian) cannot be sustained, because his sauzei and Stephanoceras humphriesianum basis of correlation was on misidentified zones. Therefore, the Tsukinoura For­ Aalenian genera. In fact, his ' Grammo­ mation is Middle Bajocian age, at least ceras' sp. from Yobaijitoge might be its fossiliferous part. Asthenoceras, and ' Phymatoceras' sp. might be Sonninia (Euhoploceras). Conclusion The chronological relation with the Hosoura Formation which is of Upper In Karakuwa district of southern part Toarcian-Aalenian age and is correlated of Kitakami plateau, the Jurassic se­ with the Tsunakizaka Formation Kl by quence commences with the Kosaba TAKAHASHI, remains unsolved from the sandstone which is succeeded by the stratigraphical point of view, because Tsunakizaka Formation of 0. sauzei zone the distribution of the two formation is age. The Kosaba sandstone is fossili­ completely separated. ferous but barren of ammonites. Its age is naturally before that age, but its Tsukinoura Formation: position in the zonal scheme remains The collection from Maeami is impor­ uncertain. tant for correlation of the formation. In Ojika Peninsula of the same plateau, This faunule is composed of: the Tsukinoura Formation is the basal member of the Jurassic and is of the Stephanoceras sp. cf. S. plicatissimum (QUEN­ Middle Bajocian age. STEDT) Normannites (Itinsaites) sp. The underlying beds in both districts are Triassic; thus the sedimentation did These are strong indicators for Stephano­ not occur during the period covering ceras humphriesianum zone. Normannites from Rhaetian to Aalenian, if the Kosaba is a wide spread genus, known from sandstone remains within the Bajocian. South Alaska, Western Canada, probably From the structural viewpoint, both from Andes, Indonesia and Western Aus­ districts are aligned on the same syn­ tralia, and is known mainly from Ste­ clinorium axis, which runs approxi­ phanoceras humphriesianum zone. It mately in N-S. The sequences in both ranges, however, into the Otoites sauzei regions are not completely identical, but zone, as exemplified by the occurrence it is very much likely that the Jurassic in South Alaska. The Japanese species sequence commenced with the beds of resembles Itinsaites reported from the similar age. Queen Charlotte Island, which is distri- 594. Bajocian ammonites from Kitakami 291

of Central Oregon. Bull. Geol. Soc. Amer., References vol. 52, no. 2, pp. 219-269. McLEARN, F.H. (1929) : Contribution to the ARKELL, W.J. (1953) : Bajocian ammonites stratigraphy and palaeontology of Skide­ collected by Sir Henry HAYDEN near Kam­ gate Inlet, Queen Charlotte Islands, B.C. padzong, Tibet. Geol. Mag., vol. 90, no. Nat. Mus. Canada, Bull., no. 54, pp. 1-27, 5, pp. 331-336, 2 pis. pis. 1-16. -- and PLAYFORD, P.E. (1954): The Bajo­ 0NUKI, Y. (1.969) : Geology of the Kitakami cian ammonites of Western Australia. massif, Northeast Japan. Tohoku Univ. Phil. Trans. Roy. Soc. London, Ser. B, lnst. Geol. Paleont., Contribution no. 69, no. 651, vol. 237, pp. 547-605. pp. 1-239, pis. 1-4. -- (1956) : Jurassic geology of the world. SATO, T. (1956) : Revision chronologique de 806p., Oliver & Boyd, Edinburgh. Ia Serie de Karakuwa (J urassique moyen). BoEHM, G. (1912) : Unteres Callovien und japan. jour. Geol. Geogr., vol. 27, nos. Coronatenschichten zwischen MacC!uer 2-4, pp. 167-171, pl. 13. Golf und Geelvink Bai. Nova Guinea, -- (1962a) : Etudes biostratigraphiques des vol. vi, Geol. abs. 1, pp. 1-20, pis. 1-5. ammonites du Jurassique du Japon. Mem. -- (1904-1912) : Die Siidkiisten der Sula Soc. geol. France, N.S., tome 41, fasc. 1, Inseln Taliabu und Mangoli. 1-4 Abs., pp. 1-122, pis. 1-10. Beitr. Geol. Niederland. Ind., Pal. Suppl., -- (1962b) : Le Jurassique du Japon-Zone IV. d'Ammonites. Colloque du Juras. Lexem­ BucK:.-IA:>~, S.S. (1909-1930) : Yorkshire Type bourg 1962, Comp. Rend. et Mem., pp. 885- Ammonites. Vols. 1-7, pis. 1-790. 896. FREBOLD, H. (1957) : The Jurassic Fernie TAKAHASHI, H. (1969) : Stratigraphy and am­ Group in the Canadian Rocky mountains monite fauna of the Jurassic System of and foothills. Geol. Surv. Canada, Mem. the Southern Kitakami massif, Northeast 287, 103pp., 44 pis. Honshu, Japan. Sci. Rept. Tohoku Univ., -- (1969) : Toarcian and Bajocian rocks 2nd Ser., vol. 41, no. 1, pp. 1-93, pis. 1-19. and guide Ammonites from Southwestern ToRNQt:IsT. A. (1898) : Der Dogger am Es­ British Columbia. Geol. Surv. Canada, pinazito-Pass, nebst einer Zusammenstel­ Paper 67-10, pp. 1-47, pis. 1-6. lung der jetztigen Kenntnisse von der HAY AMI, I. (1961) : Successions of the Kita­ argentinischen Juraformation. Pal. Abh., kami Jurassic. japan. jour. Geol. Geogr., N.F., Bd. 4, Heft 2, pp. 135-204, pis. 14-23. vol. 32, no. 2, pp. 159-177. WESTERMANN, G.E.G. (1954) : Monographie IMLAY, R.W. (1964): Middle Bajocian Am­ der Otoitidae (Ammonoidea). Beih. Geol. monites from the Cook Inlet Region, Alas­ jahrb., Heft 15, 364p., 33 pis. ka. Geol. Surv. Prof. Pap. 418-B, 61pp., -- (1969) : The ammonite fauna of the Kia­ 29 pis. lagvik Formation at Wide Bay, Alaska JAWORSKI, E., KRANTZ, F. & GERTH, H. Peninsula. Part II. Sonninia sowerbyi Zone (1926) : Beitrage zur Palaeontologie und (Bajocian). Bull. Amer. Paleont., vol. 57, Stratigraphie des Lias, Dogger, und der no. 255, 171 p., 47 pis. Unterkreide in den Kordilleren im Siiden - & GETTY, T.A. (1970): New Middle der Provinz Mendoza (Argentinien). Geol. Jurassic Ammonitina from New Guinea. Rund., 17a, pp. 373-427. Ibid., vol. 57, no. 256, pp. 231-301, pis. KRUIZINGA, P. (1926) : Ammonieten en eenige 48-62. andere Fossielen uit de Jurassische Afzet­ -- (1967) : Sucesion de Ammonites del Ju­ tingen der Soela Eilanden. jaarb. Mijnw. rasico medio en Antofagasta, Atacama, Nederl. Indie, Verh., 1 Ged., pp. 13-85, Mendoza y Neuquen. Rev. Assoc. Geol. pis. 1-14. Argent., tomo xxii, no. 1, pp. 65-73. LUPHER, R.L. (1941) : Jurassic stratigraphy 292 Tadashi SA TO

Higashihama ~~ Ojika !tl: Jt[ Kitakami *~t J.: Tsukinoura fl I rm Kosaba 1]\ Tsunakizaka ~Lt- :!1i Maeami j'Jtj m• Yobaijitoge ~ill~~lt

Explanation of Plate 34

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

!SHI BASH! photo. 293

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JJ :;f>:Ci1:fm~S< 1972 1:f'.*.t.S< · 1:f'-4' 0~ttfl*tlfi~JJ!f!C"?v''L .... · ... · · ·. · · -'E- Y .?l :T1+1J:ftB 7J Y 7'!! 7*0) Cedaria 11f111t.=:...... ~1'§3%'oi'[) . J"fJW :\!',.~ *!:II 3ffiO)fffili*9E1: CftR)C) ...... ;IV3 :~:1!! Evolutionary trend of the genus Fagus wr=u~:km'i O).=:.:ilHcitE!"B!l~tH ...... rr:.nuJ~t'i!i around the Northern Pacific Basin ..... Ophiuroid and associated molluscan fauna ...... TANAI, T. from the Ichijiku formation, Boso Penin- tlt-=ftiki.¥l.JO)j['Qj}Jj(!::.--?v''L · · · ·· · · · · ·· · · .i;Uu9-!'l} sula ...... OHARA, S. & SUZCKI, K .. Calcareous nannoplankton flora of the youngest Cenozoic of the Pacific Cen· ~Y;J<:/'/'.b. ~~\kf*!WJ!fl!]fl:n!U: 0 IJ:;f>: tral Region...... TAKAYAMA, T. Wfr1: f-1:: O)±J'. ttlflfi/:"f: J 'Ji 13 /j>:lffrm::::.it'dc .:t;!:J 0 i.¥il)]ii:fftL!1~5Hlf UY.: :.ltlillWr::W::.:::*O) .&ftn C. EtHic J: 0~Ff-rK5-1 .. itX!:h5J11fO)I*J11f~· ..... •io·I1J:Ci¥1kl!!~ · '1;\'ll'd.Jr::::...... •..•.....•...•..... ili1:1115K~..\L Radiolarian fossils from the Nobori forma- tion, Japan ...... ~um 7,..-;;-'}" • "~.r:rJ:~m_tO) ~\kf*mtJ~J]ftnO)~ ;~ ...... r:u ~t•*[)t.l~ ...... NAKASEKO, K. & NISHIMURA, A. Neogene Actinommaridae (Radiolaria) in Cii*IiP'r"lg"WHfcO).&mftnm ...... ·*d~tJIIi'~c Japan ...... SUGANO, K. ~I•OOJ:~:;I;{Ji/Ut~!f .:t-oJ: U: Jllfl · ~\l'U~~O)_&fl: Permo-Carboniferous endothyraceans from Ent r~ J: 0 -~~ ...... lliiJ:;t>:tn::k: -Jl1 Japan, Part 1. Biseriamminidae. (f-1::1\ft) :lt:*-'f}fJ~:IJixO)l/ifr:tH.=:.if.c-1 .?t-v f31-1t:P!t'F ...... •...... tiM III:>¥:- Jl!i) ...... OKIMURA, Y. =r!! 00 Isla Madre de Dios jfftO)M~!.hfl:nfC %Tr1ii'E*O)M rt~ c. .P. itn 0)/Wflr.J'i':l:JJ:ttJ. ~.i'i®il~il'li "? v' 'L ...... =f:\&j\;;0 ~::6 B- ~:t ~ffij .e..:.,v-illi Minetrigoniinae !::."?v''L .... l)lj!33JI9ll![l J:: fill rJX: Ill Jf5 illi 0)~71 r ::r"7J 1 [Sarmacina 294

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900 flj Transactions and Proceedings of the Palaeontological Society of japan

New Series No. 85 April 20, 1972

CONTENTS

TRANSACTIONS 591. Hu, Chung-Hung: Ontogeny of three Cedaria zone trilobites from Upper Cambrian, Montana ...... 245

592. YAMAGIWA, Nobuo and SAKA, Yukiyasu : On the Lepidolina zone discov- ered from the Shima Peninsula, Southwest Japan ...... 260

593. SAKAGAMI, Sumio: The Triassic Bryozoa from Kusaka, Sakawa basin, Shikoku, Japan ...... 275

594. SATO, Tadashi: Some Bajocian ammonites from Kitakami, Northeast Japan ...... 280

PROCEEDINGS 293