Transactions and Proceedings
of the Palaeontological Society of Japan
New Series No. 87
Palaeontological Society of Japan September 30, 1972 Editor: Takashi HAMADA Associate editor: Yasuhide IWASAKI
Officers for 1971 -1972
President: · Tokio SHIKAMA Councillors (* Executives): Kiyoshi ASANO*, Kiyotaka CHINZEI*, Takashi HAMADA*, Tetsuro HANAI*, Kotora HATAI, Itaru HAYAMI, Koichiro IcHIKAWA, Taro KANAYA, Kametoshi KANMERA, Tamio KOTAKA, Tatsuro MATSUMOTO*, Hiroshi OZAKI*, Tokio SHIKAMA *, Fuyuji TAKA!*, Yokichi TAKA YANAGI Secretaries: W ataru 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, Y asuhide 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. 87, pp. 377-394, pl. 47, September 30, 1972
601. TWO SMALL DESMOCERATID AMMONITES FROM HOKKAIDO
(STUDIES OF THE CRETACEOUS AMMONITES FROM HOKKAIDO AND SAGHALIEN-XXIV)*
TATSURO MATSUMOTO!), TATSUO MURAMOT02> and AKITOSHI INOMN>
~l::.ffljitffti:-T:A.:c-e 7 :Af31.'H~~7 :..-'.:C-;1-1 ~ 2 f!fi: -t'O) 1 fi~~}]IJ!I!!)JJ3.!1E.;'f-O)r$-e / ~ =- 7 :..-'0) Mantelliceras japonicum 1\'.'17• t?:>iit L. t: "b 0)'"(', Wfr~Wfrm! C. VC:::.. :::.lr.ilcl!lXT .Qo :::.. hvinl<:f*~O)fE:Q~ 2 em JE.l?:>fO)'J''!!'t', JLI:l~v'ijWiWTrilfi~ "b t:,, mi»EEIB~Jl!:Q~y L. fh LV' .Qo ~~ilfilr.li~am77~f'I C. k C.?J:v'o ~~lifT U~v' < v~~'Li7~mltt,gl]".)lr.lJ.gU.) l?:>~'L.Q o ~-8- ~.~lii7'tJ: f) lJ!*-4ifl:: L. LV' .Q:Q~, fimf*~~i3"JICiJi! .Q C. 7':7. .:C -e 7 :A O)~!j't"C:· £> .Q o :!9J~fi-:l: .Q:::.. "'o ;:.0)~? tJ:!I;t~~~~ff-T'l'J!!O)tO)fi 7 :..-'.:C-;1-1 ~ 0))1fdl::'ii:'.J:v'ov'~:dJ::f.;J.fc.iE)J!i7' !?:> -t":tLf.:,HJ':t1( C. L. L~glib t?:>tL.Q o fl!!f1UC. Fol~iJ~-t'O)iJ1iJZ!~iLU~ .iE1i1iHciJi!tLf, Ji!Jif J:::r:i!!!m ~I%:Ji!.v't.:~~'LLv'.Qo ;::O)"bO)fitcfi!Ji0)7:A.:C-e7:Aill!:fJI.O) .;( /'/~-lr.li::.A:L, £>-:1: fJi! 9E'l:"tJ:v'1:.ffitJtr.\':~"b"" Lv'f.:O)'t'vitl:v'i7'ctiH~~tL.Qo r~ : for one of them, belonging to the sub Introduction family Desmoceratinae, is T. MATSU In this paper descriptions and remarks MOTO and T. MURAMOTO and that for are given on two small, peculiar ammo the other, belonging to the subfamily nite species which are assignable to the Puzosiinae, is T. MATSUMOTO and A. family Desmoceratidae. The authorship !NOMA. Before going further we thank Dr. Itaru HAYAMI, Miss Yuko WADA and * Received Jan. 23, 1972; read Jan. 20, 1972 at Chiba. Miss Seiko HAY AKA w A in their kind 1) Department of Geology, Kyushu Univer assistance in preparing the plates and sity, Fukuoka 812. typescript. For the study of the second 2) Yayoi, Mikasa, Hokkaido 068-22. species we thank the Japan Petroleum 3) Japan Petroleum Exploration Co., Ote Exploration Company and Professor Wa machi, Tokyo 100. taru HASHIMOTO for their kind support. 377 378 Tatsuro MATSUMOTO, Tatsuo MURAMOTO & Akitoshi !NOMA Systematic description from the Lower Cenomanian of Hokkai do. Its comparisons· and affinities with Family Desmoceratidae other genera are to be given after the description of the species. Subfamily Desmoceratinae* Several years ago when we were con Microdesmoceras tetragonum MATSU centrated in a field work to obtain fossils MOTO and MURAMOTO, sp. nov. from the Cenomanian of the Ikushum bets area, central Hokkaido, one of us Pl. 47, Figs. 1-4; Text-figs. 1-4 (T. MURAMOTO) was successful to find four small, peculiar ammonite specimens. Material.-Holotype, GK. H5653, from They show very distinctive characters of loc. Ik 1101, Kami-Katsurazawa, Ikushum one and the same species, which requires bets. Three paratypes, of which one a new genus in the Desmoceratinae. from loc. Ik 1101 and another from Ik 1051b are preserved in the MuRAMOTO Genus llficrodesmoceras MATSUMOTO Museum and the last from loc. Ik 1067bp and MURAMOTO, nov. is in Kyushu University (GK.) with re Type-species.-Microdesmoceras tetrago gister number H5650. The last one has num sp. nov., to be described below. been cut into two main parts and a few Generic diagnosis.-A small desmocera minute pieces (of the first whorl) to ex tid, with somewhat simplified pattern of amine the characters of the inner whorls. sutural elements, showing a broad and Specific characters.-The shell is small. trifid lateral lobe (L) and somewhat phyl The holotype, which is regarded as re loid terminals of saddles aligned on a presenting an adult stage, is 18 mm in descending line. Coiling of moderate involution; slight ly deviated from normal spire in the last whorl. The body-whorl and the c preceding part of the late, septate whorl characterized by somewhat tetragonal outline in cross-section. The surface of the shell nearly smooth, only with flexu ous weak lirae, which show a moderate ly projected ct~rve on the venter and another on the middle part of the flank. Gently sigmoid, periodic constrictions marked on the internal mould of late whorls, but not accompanied with a Text-fig. 1. Microdesmoceras tetragonum perceptible elevation on the surface of sp. nov. Diagrammatic sketch of the halo the shell. type in two lateral and an apertural views Remarks.-This genus is at present (above). A part of the !irate surface (left) represented by only a single species and constriction on the internal mould (center) are shown. The external part of * The authorship of the description under the second last suture (below) exposed at subfamily Desmoceratinae is Tatsuro MATsu s. u.s. =umbilical seam; u.sh. =umbilical MOTO and Tatsuo MURAMOTO. shoulder. · (T. MAT. delin.) 601. Two small desmocemtid ammonites 379 E c U2 U3 U4= 5 U.Jh. t.!.S', Text-fig. 2. Microdesmoceras tetragonum sp. nov. Diagrammatic sketch of a para· Text-fig. 3. Microdesmoceras tetragonum type, from Joe. Ik 1101, in lateral and sp. nov. Diagrammatic sketch of a para apertural views (above) and the suture type, from Joe. Ik 105lb, in lateral and exposed at s. (T. MAT. delin.) apertural views (above) and the external part of the last suture exposed at s. (T. MAT. delin.) diameter. The involution is moderate and the umbilicus is of moderate width, about 34(±1) percent of the shell diame flank and then recurved at the ventro ter. The mode of coiling of the adult lateral part passing to a moderate ven whorl, as seen in the holotype, is slightly tral projection. The lateral and the deviated from the normal spire, i.e. ventral projections are rounded. The slightly scaphitoid. outline of the apertural margin is not The body-whorl occupies about three precisely known. quarters of the last volution. It is· nearly There are three or four constrictions as high as broad and approximately per whorl in the late growth-stages. tetragonal in cross-section, having flat They are roughly sigmoid on the flank and parallel flanks, a broadly arched but not so much projected as the lirae venter and vertical umbilical walls. The on the venter. They are impressed only preceding septate part of at least a half on the internal mould and the corn~s volution has also flat and parallel flanks ponding elevations on the test are but is somewhat broader than high. Still hardly discernible. The constrictions of inner whorls are much broader than high the body-whorl is very faint on the and rounded to reniform in cross-section. flanks but better marked on the venter. They are more evolute than the outer Generally speaking the suture is of whorls. The above mentioned change of desmoceratid type, but is particular in shell-form with growth may be illus· its more simple pattern as compared trated by a cross-section (Text-fig. 4). with those of the nearly contemporary The surface of the shell looks nearly Desmoceras (Pseudouhligella) and Puzosia. smooth, having only weak lirae. As far The external suture of the last whorl as the observed outer whorls (of 10 to (at the whorl height of 4 or 5 mm) is 20 mm in diameter) are concerned, the characterized by a somewhat narrowed lirae show a sigmoid curvature, running stem of the external lobe, asymmetrically fairly strongly forward from the umbili divided first lateral saddle, broad and cal edge to the mid-flank, curved some trifid first lateral lobe (L), which is situ what backward on the outer half of the ated on the ventrolateral shoulder, much 380 Tatsuro MATSUMOTO, Tatsuo MURAMOTO & Akitoshi !NOMA Measurements.- Specimen Diameter Umbilicus Height Breadth B./H. GK. H5653 18. 0(1) 6. 2(. 34) 6. 0(. 33) 6. 0(. 33) 1.0 Paratype from 9. 8(1) 3. 3(. 33) 4. 0(. 41) 4. 0(. 41) 1.0 Ik 1101 Paratype from 11. 2(1) 3. 8(. 34) 4. 2(. 37) 4. 2(. 37) 1.0 Ik 1051b GK. H5650 12. 5(1) 4. 4(. 35) 4. 8(. 38) 5.1(. 41) 1.0 smaller and narrower second lateral lobe ence in the details of the suture, such (U2) and gradually descending auxilia as the mode of subdivision of the first ries. Minor incisions are less numerous lateral saddle, even among the four spe and shallower than in the typical Desmo cimens, although the fundamental pat ceras or Puzosia and each of the saddles tern of the suture is the same. and folioles show a rather entire outline, Comparison.-At first sight this species resulting in a· somewhat phylloid aspect looks like a certain species of Tetragonites in the sutural pattern. in shell-form, but it is not related with The development of the suture with the Tetragonitidae, because its suture is growth has not been completely traced, fundamentally different from those of because of unfavourable state of preser the Tetragonitidae. In the latter the first vation. So far as the observation on the lateral saddle is tripartite, the lateral available material is concerned, the for lobes [L and U2] are bipartite and the mula is probably E, L, U2, U3, U4 =S, internal lobe forms a septal lobe [Is]. ulV• uld, I, but could be interpreted In its simplicity of suture (or better otherwise. The saddle between E and to say simplified suture), small size and L is bipartite in early stages (from a smooth shell the present species reminds certain stage of the second whorl) and us of such species as Flickia simplex then modified in late stages, normally by PERVINQUIERE, 1907, but it differs from subdivision of the larger dorsal branch. them by its rather desmoceratid basic The protoconch is comparatively large pattern of sutures, different shell-form as in other examined examples of the and the existence of constrictions. Cer desmoceratids. tainly it has no affinity with the Flicki Remarks.-The holotype and the third idae which, in turn, are apparently re paratype (GK. H5650) are regarded as lated. to Mojsisoviczia or Falloticeras of representing an adult shell, because the the Brancoceratidae (see WRIGHT, 1957, last two septa are approximated and p. L409), hence provisionally placed in because the last whorl presents a parti the Acanthocerataceae. cular shape as compared with earlier On account of its phylloid aspect of whorls. sutures, smooth shell with sigmoid lirae · The variation in shell-form between and more or less evolute whorls, this individuals seems to be little, as is indi species is apparently similar to certain cated by the above measurements, but early representatives of the Phyllocera the number of the examined specimens taceae, such as Eopsilocems planorboides is by no means· enough to lead a con (GUMBEL) (see WIEDMANN, . 1970) and clusion. There is some extent of differ- W opji.ngites krystyni WIEDMANN, 1970, 601. Two small desmoceratid ammonites 381 /,...---....., II ' \ I I I I \ ) pr. 5 O.Smm ....---...< 30 U3 U2 L E .~2° u.s. O.Smm ,.····-I Ul U2 E Text-fig. 4. Microdesmoceras tetragonum MATSUMOTO and MuRAMOTO, sp. nov. Diagrammatic illustration of a paratype, GK. H5650, showing growth of whorls in cross-section and lateral view (above) and also that of sutures (below). pr= proto conch, !•=the first whorl, z·=the second whorl, 3•=the third whorl, 4•=the fourth whorl, b=early part of the body-whorl [living-chamber]- s=the last second suture. A concealed but presumed part of a suture is drawn with a broken line, with the aid of the observed feature in cross-section. (T. MAT. delin.) from the Upper Triassic of Europe. The because its geological age is much sepa· similarity is regarded again as homeo rated from them. morphy, because it has no lituid internal This species is somewhat allied to lobe of the phylloceratacean type and Desmoceras (Pseudouhligella) japonicum 382 Tatsuro MATSUMOTO, Tatsuo MURAMOTO & Akitoshi !NOMA Y ABE (see MATSUMOTO, 1954a), from the bed belongs to the zone of Mantelliceras Cenomanian of the northern Pacific re japonicum, Lower. Cenomanian. The third gion, in the flattened flanks, perpendicu paratype was found in a rolled calcare lar walls and sigmoidal constrictions of ous nodule collected at Joe. lk 1067bp, an adult shell, although the shell of the which was probably derived from the latter species is more compressed, much same zone exposed on the southern wall more involute and about six times as of the Shimo-ichino-sawa [locally called large as the former in diameter. The Tori-sawa], a tributary of the Ikushum suture of the former resembles that of betsu near an electric power station, an immature shell of the latter (see because Zelandites injiatus, Hypoturilites MATSUMOTO, 1954, text-fig. 6 [52]), in sp. and Eogunnarites sp., among many the general pattern and probably also in other mollusks, were found in the same the mode of development with growth, nodule. although much broader L and more sim Discussions.-On the basis of the pre ple, phylloid outline of the saddles are ceding description it can be concluded characteristic of the former. D. (P.) ja that the genus 1\1icrodesmoceras, as re ponicum and other species of Desmoceras presented by M. tetragonum, should be have more finely and deeply incised, ascribed to the family Desmoceratidae. complex sutures in late growth-stages. M. tetragonum is, however, so peculiar The present species resembles certain that it is not directly connected with species of Puzosia [e.g. P. mayoriana any known species of the Desmocerati (n'ORBIGNY)] in the degree of involution, dae. In other words the origin of the width of umbilicus and sigmoid constric species is obscure. tions. The suture of immature Puzosia Microdesmoceras is not so closely con or its allies (see SCHINDEWOLF, 1966, nected with main representatives of the text-figs. 373-377) is fairly similar to that Desmoceratinae or those of the Puzosii of the present species, but the former is nae that it could possibly be accomodated more incised and the auxiliaries are in a new subfamily. However, we still strongly descending* even if the shells hesitate to propose a new subfamily of the same size are compared. Species name, because we have not yet discov of Puzosia have generally more distinctly ered any descendants or relatives which marked constriction and numerous ribs. could be closely grouped with Microdes They are evidently larger than the pre moceras under the same subfamily. It sent species in the adult stage. is indeed a particular offshoot of the Occurrence.-The holotype and a para Desmoceratidae, in view of its small size, type came from Joe. Ik 1101 and another simplified suture, less prominent con paratype from Joe. Ik 1051b on the north strictions and tetragonal, smooth, slight ern wall of the V -shaped valley of the ly scaphitoid outer whorl. For the time lkushumbets (see MATSUMOTO et al., being we have to assign it to either the 1969, text-fig. 9). They were contained subfamily Puzosiinae or to the subfamily in calcareous nodules from the lower Desmoceratinae. Someone might prefer part of unit lib, Mikasa Formation. The the former assignement on account of its less involute coiling, but we are rather * This character is not well shown in inclined to the latter assignement, though SctiiNDE\\'OLF's text-figs. See MATSUMOTO, provisionally, on the grounds of the pat 1954b, text-figs. 2-4 for this point. tern of its suture. .(iO 1. Two small desmoceratid ammonites 383 It is interesting to see the appearance Subfamily Puzosiinae* of peculiar micromorphic offshoots in the evolutional history of various branches The subfamily Puzosiinae include many of the Ammonoidea. The Upper Albian species which have a large shell. A giant to Cenomanian Flickiidae, which are pro example, which is more than a meter in visionally ascribed to the Acanthocera shell-diameter, was reported by MILLER taceae (see WRIGHT, 1957, p. L409), are and YouNGQUIST (1946) from the Seno good examples. Lower Cenomanian genus nian of Montana under the specific name Neosaynoceras, which is included at pre of Parapuzosia bradyi. A specimen of sent in the family Acanthoceratidae may Pachydesmoceras denisoni (STOLICZKA) be another minor example which consid (1865, pl. 66a), GSI. No. 208, which one of erably deviates from the principal genera us (T.M.) examined in the Museum of the of the family in many characters. Micro Geological Survey of India, Calcutta, is desmoceras can be taken as another ex nearly as large as 100 em in diameter at ample of a special, dwarfish derivative the middle of the coarsely ribbed body which appeared in the course of the whorl. The holotype of Lytodiscoides evolutional history of the Cretaceous conduciaensis (CHOFFAT, 1903) and that great family Desmoceratidae. of L. [ =" Achileoceras "] erasmusi (vAN Aside from the Cretaceous examples, HOEPEN, 1951), which have magnificently Cymbites and Paracymbites in the Arieti ornate body-whorl, are likewise large. tidae, Protocymbites in the Psiloceratidae In the Cretaceous deposits of Hokkaido and Metacymbites in the Liparoceratidae, and Saghalien large ammonites are not Primelites and Diaphorites, provisional infrequently found at various strati members of the Eoderoceratidae, and graphic levels. Some of them certainly Oecoptychius and Protophites in the Ste belong to the subfamily Puzosiinae. Thus phanocerataceae are examples of peculiar an example of Mesopuzosia sp., which dwarfs or degenerated, simplified (or came from the Upper Turonian (upper specialized) derivatives in several fami most part of the Mikasa Sandstone) of lies or superfamilies of Jurassic ammo the Yubari area, now exhibited in the nites (see ARKELL, 1957, p. L240, L248, National Science Museum, and two other L296). examples of Pachydesmoceras cf. pachy The origin of this kind of ammonites discoide MATSUMOTO, from the Turonian is more or less obscure and they are Saku Formation of the Saku area, one often called cryptogenic. In other words of which was presented to the Akiyoshi the peculiar character appeared seem dai Science Museum (from T.M.) and the ingly suddenly, with little evidence of other in the possession of Kyushu Uni intermediate forms. Why this is so is versity (T.M. Coll.), are about 70 to 80 em one of the problems of evolution in in diameter. They are, however, nearly palaeontology. How were the habitats wholly septate and, accordingly rriust or ecological conditions of these ammo have exceeded a meter, if their body nites may be another problem to be whorls were completely preserved. Aside worked out in the future. We generally from these giant examples, we see more presume that they may have been less aggressive animals. * The authorship of the description under the subfamily Puzosiinae is Tatsuro MATSU MOTO and Akitoshi !NOMA. 384 Tatsuro MATSUMOTO, Tatsuo MURAMOTO & Akitoshi [NOMA frequently pu:~;osiine arnmop.ites of about smallest form. 30 to 40 em in diameter. In contrast to the above mentioned Kitchinites (Neopuzosia) haboroensis large ammonites of the Puzosiinae there are very small specimens which repre MATSUMOTO and INOMA, sp. nov. sent a species of the !)ame family. They Pl. 47, Figs. 5-6; Text-figs. 5-9 were collected by one of us (A.I.) from the Upper Cretaceous of the Haboro area, Material.-Holotype, GK. H5654, from northwest Hokkaido, preliminarily stu Joe. IA-1564. Paratypes, GK. H5655, from died by A. !NOMA, then sent to T. MA Joe. IA-1562; GK. H5656; from Joe. IA- TSUMOTO of Kyushu University for fur 1561; GK. H5657, from Joe. IA-1599; GK. ther study and now preserved in the H5660, from Joe. IA-1557; GK. H5661, Type-Specimen Room, Department of from Joe. IA-1570; GK. H5658, from Joe. Geology, Kyu::;hu University. They are IA-1577, Haboro area. Probably refer assigned to a new species of Kitchinites able specimens, GK. H5659, from Joe. described below, with some discussions. IA-1536, Haboro area; IGPS. 57746, lku shumbets area. Specific characters.-Shell is small, Genus Kitchinites SPATH, 1922 about or slightly less than 30 mm in Subgenus Neopuzosia MATSUMOTO, 1954 diameter at the adult stage. It is mod erately evolute, about a half of the in Type-species.-Kitchinites (Neopuzosia) ner whorl being embraced by the outer japonicus SPATH, 1922. one. Its umbilicus is also fairly wide, Remarks.-Neopuzosia was proposed as occupying about 34-38 percent of a di an independent genus, because the clis ameter in the holotype and measurable tinction between the type-species of Neo paratype. The umbilicus is shallow and puzosia and that of Kitchinites [K. pondi encircled by a very low but nearly ver cherryanus] was very clear. There are, tical or steeply inclined wall. however, certain species which show The outer whorl is compressed, show apparently intermediate or even mixed ing about 0.7 to 0.8 in the proportion of characters (see MATSUMOTO, 1954b, p. 89; breadth to height. Its flanks are, how HOWARTH, 1965, p. 387). At present we ever, gently convex, passing to a rather would agree with WRIGHT (1957) and narrowly arched venter. Its cross-section HowARTH (1965) in admitting Neopuzosia is, therefore, subelliptical. The inner as a subgenus of Kitchinites. whorls are less compressed and sub Species of Kitchinites, including those rounded ; the innermost one is depressed. of the subgenera Neopuzosia and Kitchi Constrictions are well marked (i.e. deep nites (s.s.), have a shell of moderate to and moderately broad on the internal small size even at the mature stage, mould) and fairly frequent, about five to being generally smaller than many other six per whorl. They are gently sigmoid species of the Puzosiinae. This point on the flank and projected on the venter. was mentioned by MATSUMOTO (1954b, p. On the body-whorl the linguiform ven 90) and has been ascertained by subse tral projection is remarkable, being ac quent descriptions of HOWARTH (1965) companied with the notable elevation and HENDERSON (1970). The species to behind the constriction. be described below may exemplify the The inner whorls are nearly smoothish. 601. Two small desmoceratid ammonites 385 a Smm L--J Text-fig. 5. Kitchinites (Neopuzosia) haboroensis MATSUMOTO and !NOMA, sp. nov. Diagrammatic sketch of the holotype, GK. H5655, in lateral view and its front view, with body-whorl cut at Q (above); external part of the second last suture at S (below). m =internal mould; t =test preserved; a= line of demarcation showing the apertural margin at an earlier growth-stage; u.s. =umbilical seam, u.sh. = umbilical shoulder. (T. MAT. delin.) The septate part of the outer whorl has tral projection. Aside from the eleva fine and weak, sigmoidal ribs. The body tions which are accompanied with the whorl has more distinct, but fairly fine two constrictions, ribs are very faint, and dense, ribs, which are more or less whereas fine, sigmoid lirae are discerni sigmoidal on the flank and projected on ble on the shell-surface of the interval the venter. The ribs which are situated between these two· constrictions. In front at some distance in front of the con of the last constriction there are elon striction are normally more sigmoid than gated lappets which are situated at about the others, although there may be a the inner one third of the flank. The variation in the details. ventral part of the peristrome is mod Near the apertural margin of the adult erately projected. shell there are two approximated con· A distinct line of demarcation which strictions which show a very strong ven- probably marks the apertural margin of 386 Tatsuro MATSUMOTO, Tatsuo MURAMOTO & Akitoshi !NOMA St U.!;, Text-fig. 6. Kitchinites (Neopuzosia) haboroensis MATSUMOTO and !NOMA, sp. nov. Diagrammatic sketch of an immature shell, paratype no. 5, GK. H5658, in lateral and frontal view (above); the other side, in part (center); internal suture, with adjacent portion of external suture, at S2; external suture at Sl (below). symbols m, t, a, and u.s. same as in Text-fig. 5, j =injured part of the apertural margin at an early growth-stage. (T. MAT. delin.) the immature shell is sometimes pre Sutures are of Puzosia pattern. Those served at some distance in front of the in the late part of the septate whorl constriction, showing a moderate flexuo have a somewhat asymmetrically tripar sity on the flank and a ventral projection. tite first lateral lobe (L) which is deeper Its convexity on the lower part of the than the external lobe (E). The aux flank is somewhat stronger than the ribs iliary elements beyond the second lateral or lirae on the adjacent parts (Text-figs. lobe (U 2) are aligned on a strongly_:ctes 5-7). cending line. 601. . Two small desmoceratid ammonites 387 Measw-ements.- Specimen Diameter Umbilicus Height Breadth B./H. GK. H5654 29. 0(1) 11. 2(. 38) 11. 5(. 40) 8. 9(. 31) (c) 0 77 8. 7 (. 29) (ic) " ( -180°) 7.2 6.2 0 86 GK. H5655 28. 0(1) 10. 4(. 37) 11. 2(. 40) 7. 3(sec. compr.) GK. H5656 29. 5(1) 10. 2(. 34) 12. 2(. 41) 8. 7(. 29) .71 GK. H5658 14. 3(1) 4. 3(. 30) 5. 5(. 38) 5. 5(. 38) 1.0 ·~--·-~ The saddles are bipartite and their lateral projection. stems tend to be narrowed by deep in The distinction in the succeeding later cision of the branches of the lobes. The whorls of the two species is unmistaka sutural formula is probably E, L, U2 , U3, ble. The adult shell of K. (N.) habaro U4 =S, U,v, U,d, I, but could be interpreted ensis is much smaller and more widely otherwise [E, L, U2 , U3 =S, U1, I, as one umbilicate than that of K. (N.) ishikawai of us (T.M., 1954b, text-fig. 3) thought so and ends at the peristome which is char on K. (N.) ishikawai] (see also ScHINDE acterized by pronounced lateral lappets~ WOLF, 1966, text-fig. 377). The mode of curvature of the ribs on Remarks.-There is some extent of the body-whorl of K. (N.) haboroensis is variation in the relative width of umbili more sigmoid than those of K. (N.) ishi cus and the proportion between breadth kawai. The ribs are remarkably strong and height of the whorl, even if the on the ventral part of the adult body shells of corresponding size are com whorl of K. (N.) ishikawai, except for pared. The details in the rib curvature the faintly ribbed apertural part. Such may also vary as shown in the illustra a sudden increase in the rib-intensity tion. does not occur in K. (N.) haboroensis, Comparison.-The shell of this species although the ribs gradually become dis closely resembles the small immature tinct on its outer whorl. The probably one of Kitchinites (Neopuzosia) ishikawai adult shell of K. (N.) ishikawai has at (JIMBO, 1894) (see also MATSUMOTO, 1954b). least two more whorls, attaining to about In fact the two species are apparently 120 or 130 mm in diameter, as repre indistinguishable up to the shell diame sented by GK. H5663 (Y. UEDA Coli.) from ter of about 20 mm, if we ignore the the generally same Haboro-Chikubetsu minor variation. One point which may area (UEDA et al., 1962). Its very aper serve as a distinction even in this im tural margin is not completely preserved, mature shell is that a remarkably sig but there are two, fairly approximated moidal line of demarcation, probably the constrictions which are prorsiradiate and peristome of the immature shell, is dis very gently sigmoid on the flank and tinct at some distance ahead of the con strongly projected on the venter. The striction on a well preserved shell of K. weak ribs and lirae on the interval of (N.) haboroensis. A similar line may be the two constrictions and immediately in discernible in front of the constriction front of the last one show a similar on some well preserved inner whorl of curvature. Although the very margin K. (N.) ishikawai, but its curvature seems is not completely preserved, judging to be more gentle, with a less pronounced from the curvature of the lirae in the 388 Tatsuro MAL-UMOTO, Tatsuo MURAMOTO & Akitoshi !NOMA strictions are stronger in K. (N.) haboro ensis. Unfortunately the peristome of the adult shell has not been clearly described in K. (K.) angolaensis nor in K. (K.) pondi cherryanus (KOSSMAT), the type-species from India. The neotype of K. (K.) an gustus (MARSHALL), proposed by HENDER SON (1970, p. 34, pl. 14, fig. 1), from the Text-fig. 7. Kitchinites (Neopuzosia) ha Campanian of New Zealand, shows dense boroensis MATSCMOTO and !NOMA, sp. nov. lirae at the preserved last part (diame Diagrammatic sketch of a part of an im ter about 130 mm), which show a very mature shell, paratype no. 6, GK. H5661, gently sinuous curvature on the flank in, Jateral view (test preserved). and are considerably projected on the (T. MAT. de/in.) venter as in the above mentioned speci men of K. (N,) ishikawai. However, it preserved last part, it does not seem to is not certain whether or not the last have long lateral lappets. part of that New Zealand species marks K. (N.) haboroensis is somewhat similar the very apertural margin. to Yokoyamaoceras jimboi MATSUMOTO In view of the gentle inflation of the:: (1955, pl. 9, figs. 4, 5 ; text-fig. 13) in the flanks and the gradual strengthening of small size, presence of lateral lappets the ribs in the adult shell, this species and other general appearance. The could be referred to Mesopuzosia, but latter has ventrolateral tubercles on we are inclined to assign it to Kitchi a limited part of the body-whorl and nites (Neopuzosia) because of its small prorsiradiate constrictions which cut ob size and its close resemblance to K. (N.) liquely numerous ribs behind them. The ishikawai in immature stages. suture of the former species is of puzo Occurrence.-The type-locality is Joe. siine type, with remarkably descending IA-1564, in unit B (siltstone) of the San auxiliaries, whereas that of the latter is tonian sequence exposed in the area of of Kossmaticeras type. the Haboro dome, Rumoi district, Teshio Kitchinites (Kitchinites) angolaensis provine, northwest Hokkaido. Paratypes HOWARTH, 1965 (p. 386, pl. 11, figs. 4-6), came from Joe. IA-1599, Deto-Futamata, from the Campanian of Angola, is con a tributary of the Haboro, upper part siderably small. Its probably adult shell, of unit A (siltstone), and rolled or fallen as represented by the holotype, is 64 mm nodules obtained at Joe. lA -1557, lA-1561, in diameter. Therefore it is twice as lA-1562, lA-1577 (Haboro dome), IA-1570 large as K. (N.) haboroensis. K. (K.) an (Sakasa-gawa), and IA-1536 (Ainu-sawa). golaensis has somewhat less flexuous ribs The possible sources of the rolled or and more involute and more compressed fallen nodules are from unit A to D whorls than K. (N.) ishikawai and K. (N.) within the Santonian sequence (zone of haboroensis, if the shells are compared Inoceramus naumanni) of the Haboro at corresponding size. Rather rapid area (Text-fig. 8). They are all from strentghening of the ribs on the ventral calcareous nodules in siltstone and often part of the probably adult whorl is evi associated with Inoceramus naumanni. dent in K. (K.) angolaensis, whereas con- Thus in the Haboro area, which repre- 601. Two small desmoceratid ammonites 389 N + 0 Text-fig. 8. Geological map of the upper reaches of the Haboro. A-F= Upper Cretaceous (Santonian) sequence in ascending order, A: dark grey siltstone, with tuffaceous sandstone at the top (indicated by black band), B: dark grey siltstone, C: glauconitic sandstone (coarsely dotted), D: dark grey siltstone, E: green sand stone, F: black mudstone. T=Tertiary (Miocene) conglomerate, sandstone, shale and tuff (finely dotted). x =Locality where the described ammonites were obtained (in situ) ; + Ditto (in fallen or rolled nodules). (Geol. Surv. by A. !NOMA) sents a northwestern part of the Yezo bets area, central Hokkaido. geosyncline and probably belongs to a Discussions.-The fact that Kitchinites less off-shore facies, the species seems (Neopuzosia) haboroensis shows almost to occur not uncommonly. In other areas the same stratigraphical range as K. (N.) the occurrence of the species has not ishikawai (JIMBO) and that the former is been well ascertained, except for a rare closely similar to the latter in the im occurrence of a probable example from mature stages but much smaller in the the Santonian of Kikume-zawa, lkushum- mature stage, having a particular type 390 Tatsuro MATSUMOTO, Tatsuo MURAMOTO & Akitoshi !NOMA of peristome, recalls us of the possibility·· - is smoothish and unusually inflated be- of sexual dimorphism between the two hind the last constriction, with the "nominal species". The situation ap- breadth of 225 mm (about 0.98 of the parently seems to be analogous with the height). The shell in front of the last cases in certain Jurassic ammonites as constriction is not completely preserved; exemplified by Cosmoceras spinosum the ventral linguiform projection is pre- (SOWERBY) and Quenstedtoceras mariae sent but the presence or absence of lat- (D'ORBIGNY), which were discussed by era! lappets is not know. If we assume MAKOWSKI (1962), and by Creniceras that there were no lateral lappets, this renggeri (OPPEL), Distichoceras bicosta- specimen could possibly be regarded as tum (STAHL), and ? Hecticoceras brightii representing a female form of Puzosia (PRATT), which were ontogenetically ex- sp. by analogy with the cases of Juras- amined by P ALFRAMAN (1966, 67, 69). sic ammonites. However, the evidence We do appreciate these and other auth- to conclude so is by no means sufficient ors who took into consideration the and no corresponding male form (some- problem of sexual dimorphism in the what smaller one with lateral lappets) study of ammonites, but it seems to us has been confirmed to occur in the same fairly difficult to present the necessary formation. and sufficient evidence for concluding In the recent collection of one of us that A is the female and B is the male (T.M.) there is an interesting specimen, of one and the same species. GK. H5665 (Text-fig. 9), from Joe. T 1021p Aside from the Jurassic ammonites, of the Turonian Saku formation, in with which we are not well acquainted, which the peristome is almost completely let us consider the problem in the case preserved. Based on the general char- of the Puzosiinae. Although numerous acters of the shell it is probably refer- species of the subfamily have been able to Mesopuzosia pacifica MATSUMOTO, monographed by various authors, little 1954. It is of moderate size, only some- has been mentioned about the peristome what larger than the holotype. On the of mature shells. In our experience of last part of its body-whorl the ribs are field work we observe that the smooth- much weakened between two, rather ap- ish body-whorl of a large shell of Puzosia, proximated, strong constrictions (eleva- Mesopuzosia or Pachydesmoceras is often tions on the shell), which are very gently squashed probably because of its weaker sigmoidal on the flank and projected on condition as compared with the septate the venter. In front of the last con- whorls. striction there is a remarkable ventral One of a few examples in which the rostrum, which approximately continues apertural margin was described is a the spiral line of coiling, and remark- very large specimen of " Ammonites able lateral lappets, which are as long as planulatus " in STOLICZKA (1865, p. 134, the rostrum but somewhat bent inward pl. 68). One of us (T.M.) fortunately at their terminal portion. The lirae are had an opportunity to examine this spe- gently sigmoidal on the part immediate- cimen in the museum of the Geological ly in front of the last constriction but Survey of India, Calcutta. There is a become more and more strongly flexu- broad, deep, concave constriction near ous so as to follow the outline of the the preserved last part of the shell (about very apertural margin. Whether every 805 mm in diameter). The body-whorl shell of Mesopuzosia pacifica has always 601. Two small clesmoce?'"atid ammonites 391 Tex t-fig. 9. Mesopuzosia sp. cfr. M. pacifica M ATSUMOT O . GK. H5665, from Joe. Tl02lp2, Saku Formation, x 0.9. Note the w ill preserved apertural margin and a marked contribution behind it. (I.H. jJhotos) this kind of peristome in the mature species, inasmuch as we observe a dif· shell or not is not clear. One of the terence even in the immature stage (see paratypes of this species, GK. I-!1571 (see description under the heading of com· MATSUMOTO, 1954b, pl. 15, fig. 2) has a parison). The said difference, however, larger outer whorl than the holotype and should be examined more precisely by the above specimen (GK. H5665), but its treating more specimens with respect to outer whorl is so incompletely preserved ontogeny and variation. that its apertural margin is not shown. Another point which is unfavorable Thus we cannot yet settle the problem for concluding the sex ual dimorphism of sexual dimorphism in this species. in this case is the occurrence. Although Be that as it may, it is interesting to there would be some collection failure, see a similarity between the well pre· the specimens of K. (N.) haboroensis have served peristome of the above mentioned been known only in a limited area of a iVIesopuzosia jJacifica and that of Kitchi particular facies and are not always as· nites (Neopuzosia) haboroensis. On these sociated with K. (N.) ishilwwai, which, in grounds it can be stated that at least turn, is more widely distributed. We some, if not all, of the Puzosiinae have rather consider that smaller ammonites an apertural margin which is character· which possess lappets at the peristome ized by a rostrum and lateral lappets. of the shell should have particular habi· We would not completely deny the tats and mode of life which are different possibility that Kitchinites (Neopuzosia) from larger ammonites without lappets. haboroensis might represent the male Presumably the former may have been form of K (N.) ishilwwai. So far as less active and less rapidly locomotive the available material is concerned, we than the latter and have taken different should regard them as two different kinds of food. Too much difference in 392 Tatsuro MATSUMOTO, Tatsuo MURAMOTO & Akitoshi [NOMA these respects between male and female aperture, stressing that the Puzosiinae seems to be unnatural, if not impossible. include various species from a gigantic In other words, the difference in size and size to a very small one. It is noted apertural character of the adult shell that the Puzosiinae show a considerable may not imply sexual dimorphism but diversity in the character of the adult may be concerned with taxonomic dif body-whorl. There would be some di ference or morphological diversity in versity in the character of its apertural evolution, which in turn, is connected margin in the same subfamily, although with diversity in habitats and mode of the actual features have not yet been life. It is, furthermore, noted that the thoroughly known on account of the un megaform is about two whorls larger favourable preservation. The species and has much more numerous septa than described in this paper presents a rare the compared microform. This implies but good example. a considerable gap in age between the two forms. In spite of a large number of speci References cited mens which have been monographed under the subfamily Puzosiinae, exam ARKELL, ].W. (1957) : In MooRE, R.C. (ed.) : ples which have lappets are very few. Treatise on Invertebrate Paleontology, Part L (Mollusca 4, Cephalopoda, Am Smaller shells with lappets should occur monoidea) L1-L490, Geol. Soc. Amer. & more frequently in association with Univ. Kansas Press. numerous, larger shells, if such sexual CHOFFAT, P. (1903) : Contributions a Ia con dimorphism as analogous to that stated naissance geol. des colonies portugaises in Jurassic ammonites existed in the d'Afrique. I. Le Cretacique de Conducia, Puzosiinae. We would rather expect a pp. 1-29, 7 pis., 1 folded pl., Cornmiss. SeriJ. different type of sexual dimorphism in Geol. Portugal. the Puzosiinae, such as more inflation of HENDERSON, R.A. (1970) : Ammonoidea from the adult body-whorl or broader aper· the Mata series (Santonian-Maastrichtian) ture and somewhat (but not extremely) of New Zealand. Special Papers in Palae larger size of the male shell than the ontology, (6), pp. 1-82, pis. 1-15. HoEPEN, Ir. E.C.N. VAN (1951) : A remark female, as suggested by the· living spe able desmoceratid from the South African cies of Nautilus, or difference in fineness Albian. Paleont. Navor. Nas. Mus. Bloem or intensity of the ornamentation of the fontein, D!. 1, St. 10, pp. 345-349. adult shell as suggested by REYMENT HowARTH, M.K. (1965) : Cretaceous ammo (1971) for dimorphic pairs of Cretaceous nites and nautiloids from Angola. Bull. Benueites species. Brit. Mus. (Nat. Hist.), Geol., Vol. 10, To sum up, we have considered a (no. 10), pp. 337-412, pis. 1-13. possibility of sexual dimorphism in the KossMAT, Frantz (1895) : Untersuchungen Puzosiinae but are rather inclined to iiber die Siidindische Kreide-formation, I. think that the available evidence is yet Beitr. Paliiont. Geol. Osterr.-Ungarns u.d. Orients, Bd. 9, pp. 97-203 [1-107], pis. 15- insufficient to support it, leaving the 25 [1-11]. problem in the future. In this paper MAKOWSKI, Henryk (1962) : Problem of sex we describe Kitchinites (Neopuzosia) ha ual dimorphism in ammonites. Palaeont boroensis as a new species of the Puzo ologia Polonica, No. 12, 92p., 20 pis. siinae which is characterized by a very MATSUMOTO, Tatsuro (1954a) : Selected Cre small size and a particular type of shell- taceous leading ammonites in Hokkaido 601. Two small desmooerat __id ammonites 393 and Saghalien. In MATSUMOTO, T. (ed.) : No. 1, pp. 126-154, pis. 6-8. The Cretaceous System in the japanese PERVINQUIERE, L. (1907) : Etudes de pale Islands, Appendix, pp. 243-313, pis. 17 ontologie tunisienne. I. Cephalopodes des [1]-36 [20]. terrains secondaires. Carte Ceol. Tunisie, -- (1954b) : Family Puzosiidae from Hok 428p., 27 pis. kaido and Saghalien. Mem. Fac. Sci., REYMENT, R.A. (1971) : Vermuteter Dimor Kyushu Univ., Ser. D, Ceol., Vol. 5, No. phismus bei der Ammonitengattung Be 2, pp. 69-118, pis. 9-23. nueites. Bull. Ceol. Inst. Univ. Uppsala, -- (1955) : Family Kossmaticeratidae from [N.S.], Vol. 3, art. 1, pp. 1-18, pis. 1-10. Hokkaido and Saghalien. japan. jour. Ceo/. ScHINDEWOLF, O.H. (1966) : Studien zur Ceogr., Vol. 26, nos. 1-2, pp. 115-164, pis. Stammesgeschichte der Ammoniten. V, 8-10. Akad. Wiss. Liter., Abh. Math.-Naturw. Kl., --, Tatsuo MuRAMOTO and Takemi TAKA· Jahr. 1966, No. 3, pp. 321-454. HASH! (1969) : Selected acanthoceratids STOLICZKA, Ferdinand (1863-66) : Ammo from Hokkaido. Mem. Fac. Sci., Kyushu nitidae, with revision of the Nautilidae, Univ., Ser. D, Ceol., Vol. 19, No. 2, pp. etc. In BLANFORD, M.F. and STOLICZKA, 251-296, pis. 25-38. F., 1861-66. The fossil Cephalopoda of MILLER, A.K. and YouNGQUIST, Walter the Cretaceous rocks of southern India. (1946) : A giant ammonite from the Cre Mem. Ceol. Surv. India, Pa/aeont. Indica, taceous of Montana. jour. Paleont., Vol. Ser. 3, 216p., 95 pis. [pp. 41-56, pis. 26-31, 20, no. 5, pp. 479-484, pis. 73-75. 1863; pp. 57-106, pis. 32-54, 1864; pp. 107- PALFRAMAN, D.F.B. (1966): Variation and 154, pis. 55-80, pl. 66a, 1865; pp. 155-216, ontogeny of some Oxfordian ammonites; pis. 81-94, 1866]. Taramelliceras__ richei (DE LoRIOL) and UEDA, Yoshiro, Tatsuro MATSUMOTO and Ken Creniceras renggeri (OPPEL), from Wood AKATSU (1962) : The Cretaceous deposits ham, Buckinghamshire. Palaeontology, in the Chikubetsu area, Hokkaido. Sci. Vol. 9, pt. 2, pp. 290-311, pis. 48-52. Rept. Dept. Ceo!. Kyushu Univ., Vol. 6, -- (1967) : Variation and ontogeny of some no. 1, pp. 15-32, with 3 folded chart and Oxford Clay ammonites: Distichoceras maps [in Japanese with English abstract]. bicostatum (STAHL) and Horioceras bau WIEDMANN, Jost (1970) : Ober den Ursprung gieri (D'0RI3IGNY), from England. Ibid., der Neoammonoideen-Das Problem einer Vol. 10, pt. 1, pp. 60-94, pis. 9-13. Typogenese. Eclogae Ceologicae Helve -- (1969) : Taxonomy of sexual dimorphism tiae, Vol. 63, no. 3, pp. 923-1020, pis. 1-10. in ammonites: morphogenetic evidence in WRIGHT, C.W. (1957) : In MooRE, R.C. Hecticoceras brightii (PRATT). In G.E.G. [Editor]: Treatise on Invertebrate Pale WEsTER:VIANN (Ed.). Sexual dimorphism ontology, Part L, Mollusca, Cephalopoda, in fossil Metazoa and taxonomic impli Ammonoidea, L1-L490, Geol. Soc. Amer. cations. Internal. Union Ceol. Sci., Ser. A, & Univ. Kansas Press. ------ Ainu-sawa ~ ffJ. iR Mikasa Chikubetsu Rumoi j;.l] * )Jlj Ell Deto-Futamata ---f' r =!Ysl Sakasa-gawa )!E Jll Ikushumbets ~;,ff}}lj Saku {:ti !A Kikume-zawa %J 00 iR Shimo-ichino-sawa T-O)iR Haboro ~~ ~1)\\ Tori-sawa .~ tR 394 Tatsuro MATSUMOTO, Tatsuo MURAMOTO & Akitoshi [NOMA Explanation of Plate 47 Figs. 1-4. Microdesmoceras tetragonum MATsUMOTO and MURAMOTO, sp. nov ...... Page 378 1. Holotype, GK. H5653, from Joe. Ik 1101, zone of Mantelliceras japonicum, Ikushum bets area. Two lateral (a, b), apertural (c) and external (d) views, approximately x2. 2. Paratype no. 2, immature specimen, from Joe. lk 1051b, MuRAMOTO Museum coli. Lateral (a) and external (b) views, approximately x 2. 3. Paratype no. 1, immature specimen, from Joe. Ik 1101, MuRAMOTO Museum coli. Two lateral (a, b) and external (c) views, x 2. 4. A half of paratype no. 3, GK. H5650, from Joe. Ik 1067bp. Two lateral (a, b) and sectional (c) views, x 2. Figs. 5-6. Kitchinites (Neopuzosia) haboroensis MATsUMOTO and !NOMA, sp. nov .... Page 384 5. Holotype, GK. H5654, from Joe. IA-1564, unit B of the Santonian sequence, Haboro area. Two lateral (a, b-e) and external (d) views, xl.5. To show the ribbing and other features b and c are taken under the light of somewhat different orientation. 6. Para type no. 1, GK. H5655, from Joe. IA-1562. Two lateral view (a. b), x 1.5. Kyushu University [I. HAYAMI] photos, with whitening. • MATSUMOTO, MURAMONO & !NOMA: Two small desrnocemticls Plate 47 lc ld 3c 3b 2b 4b Trans. Proc. Palaeont. Soc. Japan, N.S., No. 87, pp. 395-408, pis. 48, 49, September 30, 1972 602. SWIFTOPECTEN OF THE NORTHERN PACIFIC·~ KOICHIRO MASUDA Department of Geology, Miyagi University of Education, Sendai ~t.i:>fi.'Ni!!ll..)i(O) Swiftopecten: Swiftopecten fi, ~t.ll Jj(ip Gricif&~ ht.:3}1.j:_O) Pecten swijtii BERNARDI 1!: {l,"i:t\:filU: !..- "(, HERTLEIN (1935) fC J:: -:> L"tJ!':III§ ~ ll.J.: ob 0)'"(· Ji:, 0 0 * :7ff;l:l:'Jj]iy, B::;j\:OJ1tT:i:t-'J:: lf331.1:0J Pecten swijtii fc-::n,,-cfi]fl\:L-. -'tOJ:li!!'W:~I'I'{E.i:¥'li:fC"? v'-c;;-~~HTfJ:-:> t.: (MASUDA, 1959, 1960) o -'COJ[ifi~, *:'tHi~t.T ;< 0 ;t.J ®ifiJ!¥OJ'fi[r1:!fi!.i.i• G\illf!r~h'Lv'0, v'bfiJ:>0 Swiftopecten c B::;j\:OJ Swiftopecten 1!:'J:Ut!.<:tJ!F.i-t0·.1Z·~ii~Ji:> 0 c. c 1!: Hitiii L-t.: o 4'@1, ~11Hi;[t.T ;< 0 hiii:iifiJW=ii,G¥11'15~ht.:-jA:-cOJ Swiftopecten fC"?v''Lt'!\!il•J-L-t.: t!f:!if!:, T 7 A t.J ii' GF.c![\1( ~ ht.: Pecten (Chlamys) kindlei DALL, Chlamys (Swiftopecten) donmi lleri MAcNEIL :ts J:: lf, ~t. :iJ 0 7 ;t 1v =- T i.i' G ARNOLD (1906) il;\iR'ff L-t.: Pecten (Chlamys) parmeleei DALL fi, swijtii c :// =- J, -r· &.:> 0 C. c iJ;Q)l GiPfC tJ:-:> t.:iii.l', J:j:l 11~-m~~h 0 7;tlv=-TiPGioGh'Lv'0 parmeleei ii swiftii OJill.!tlc;;-.:Z0-"2:<::·&.:>0 :::.cil~ft)JGiPfCfJ:-:>f.:o l-7.1'!..-, J1§iiiJi¥fC:Gft0C.hGL:H~OJ Among the Northern Pacific Recent Introduction and fossil pectinids Swiftopecten is of in Pecten swijtii, a common Recent scal terest because of its characters, exten lop of Northern Japan, was first described sive geographical distribution and rather short geological range, as discussed in by BERNARDI (1858), and subsequently it and its varieties were recorded from the the following pages. seas of Northern Japan and also from the From the study of the Tertiary Pecti Neogene and Pleistocene deposits of Ja nidae of Japan the writer doubted whe pan, the West Coast of North America ther Swijtopecten of the West Coast of North America is identical with the true and eastern Soviet Russia. In 1935 HERT LEIN proposed Swijtopecten for the pre Swijtopecten of Japan. To clarify this sent species as a subgenus of the genus problem MASUDA (1959a, 1960) examined Pecten. numerous fossil specimens of Swiftopecten swiftii (BERNARDI) collected from the * Received January 22, 1972; read January Neogene and Pleistocene formations in 23, 1972 at Chiba. Northern Japan and Recent speci~ens 395 396 Koichiro MASUDA from the Northern Pacific and Japan Sea. Stanford University, Professor J. Wyatt At that time he supposed that the North DURHAM of the Department of Paleon American Pecten kindlei DALL and Pecten tology, University of California at Ber parmeleei DALL might be descendants of keley and late Dr. Leo G. HERTLEIN of the swijtii, and that they migrated from California Academy of Sciences in San East Asia to the West Coast of North Francisco, for their continuous encour America. MASUDA also pointed out that agement and help in various ways during the interrelationship between the Japa the course of the present work. Acknow nese fossil and Recent Swiftopecten and ledgments are due to Professor Kotora the so-called North American Swift a pecten HATAI of the Institute of Geology and should be studied comparatively. Paleontology, Faculty of Science, Tohoku Many specimens of Swiftopecten from University, for reading the manuscript. the West Coast of North America were The writer received support from the studied in connection with the problems following persons during the course of mentioned above. The specimens studied the present work, and takes this oppor are now in the collections of the Depart tunity to express his deep gratitude to ment of Geology, Stanford University, them : Drs. David M. HOPKINS, George U.S. Geological Survey in Menlo Park, PLAFKER and Warren 0. ADDICOTT of Museum of Paleontology, University of the U.S. Geological Survey, Menlo Park, California in Berkeley, California Acade Mr. Joseph H. PECK of the Department my of Sciences in San Francisco, Smith of Paleontology, University of California, sonian Institution in Washington, D.C., Berkeley, Dr. James H. McLEAN of the and County Museum of Natural History County Museum of Natural History in in Los Angeles. Los Angeles, and Drs. Wendell P. WooD The examination of those specimens RING, Harald A. REHDER and Thomas R. revealed that Pecten kindlei DALL from WALLER of the Smithsonian Institution the Pleistocene of Alaska, some of Pecten in Washington, D.C., Mr. Kenji SAKAMO panneleei DALL from the Pliocene of TO of the U.S. Geological Survey in Menlo northern California and Chlamys (Swifto Park prepared most of the photographic pecten) donmilleri MACNEIL from the work. Miocene of Alaska are synonyms of Thanks are due to the Department of Swiftopecten swiftii (BERNARDI), and that Geology, Stanford University, Museum several western North American species of Paleontology, University of California, or subspecies referred to Swiftopecten Berkeley, U.S. Geological Survey, Menlo differ from the true Swiftopecten. Park, Smithsonian Institution, California In the present article the morphological Academy of Sciences and Los Angeles characters of Swiftopecten are described County Museum of Natural History, for and the paleontological significances of permission to study their collections. the so-called Swiftopecten of the West Acknowledgments are also made to the Coast of North America are discussed. Ministry of Education of the Japanese Government, for the scholarship of study Acknowledgments abroad. The writer expresses his deep grati Historical review of Swiftopecten tude to Dr. A. Myra KEEN, Professor Emeritus of the Department of Geology, In the West Coast of North America 602. Swiftopecten 397 the species or subspecies hitherto been etchegoini and heteroglyptus into nutteri. referred to Swiftopecten or described as Among the species treated by them both a variety of swiftii are: Pecten (Chlamys) Pecten cosibensis YoKOYAMA, 1911 and P. parmeleei DALL, 1898, Pecten etchegoini heteroglyptus YOKOYAMA, 1926 had been ANDERSON, 1905, Pecten (Chlamys) nut described from the Pliocene formations teri ARNOLD, 1906, Pecten (Chlamys) wat in Japan. tsi ARNOLD, 1906, Pecten (Chlamys) wat MACNEIL (1943) described Pecten kindlei tsi morani ARNOLD, 1906, Pecten (Chla DALL under the subgenus Manupecten mys) kindlei DALL, 1920, Chlamys (Swifto from the Intermediate Beach, Center pecten) donmilleri MACNEIL, 1967, Chla Creek near Nome in Alaska, but subse mys (Swiftopecten) sp., MACNEIL, (1967), quently from the same locality he (MAC Swiftopecten sp., ADEGOKE, (1967), Swifto NEIL, 1967) recorded kindlei as a subspe pecten adekunbiana ADEGOKE, 1969 and cies of swiftii under the subgenus Swifto Chlamys (Swiftopecten) leohertleini MAC pecten. At the same time he described NEIL, 1970. However, no Recent species Chlamys (Swiftopecten) donmilleri, n. sp. of Swiftopecten is known from the West from the Miocene Yakataga Formation, Coast of North America. Yakataga district, Alaska, and Chlamys Pecten (Chlamys) panneleei first de (Swiftopecten) cf. donmilleri and Chlamys scribed by DALL (1898) from the Pliocene (Swiftopecten) sp. from the Unga Con formation at San Diego, Southern Cali glomerate at Alaska Peninsula. Further fornia, was distinguished from swiftii. In more, very lately he also described 1906 ARNOLD illustrated parmeleei from Chlamys (Swiftopecten) leohertleini, n. sp., the Pliocene formation at Pacific Beach from the Pliocene Tachilni Formation near San Diego and also from the Plio at the western end of Alaska Peninsula eene formation at Crescent City in North (MACNEIL, 1970). ern California. ELDRIDGE and ARNOLD In 1956 GLEN illustrated Pecten (Pallium) (1907) also reported the species from the swiftii var. etchegoini and swiftii var. Pliocene Fernando Formation at Else nutteri from the Pliocene "Merced" For mare Canyon, Southern California. Sub mation near San Francisco, California. sequently GRANT and GALE (1931) con F AUSTMAN (1964) recorded Pecten (Swifto sidered parmeleei a synonym of swiftii pecten) etchegoini wattsi and Pecten with the statement that the morphologi (Swiftopecten) sp. from the " Wildcat" cal characteristics pointed by DALL are Formation in Northern California. the same as those of swiftii. WOODRING Recently ADEGOKE (1967) described and BRAMLETTE (1950) illustrated parme Swiftopecten sp. from the Miocene Santa leei from the Pliocene Careaga Sandstone Margarita Formation, California and dis of the Santa Maria district, Southern cussed its paleontological significance, California. and he also (ADEGOKE, 1969) described In 1920 DALL described Pecten (Chlamys) from the same formation, Swiftopecten kindlei based upon the specimens from adekunbiana, n. sp. and Swiftopecten n. the Pleistocene deposits of Center Creek sp. and included etchegoini, wattsi and Mines near Nome, Alaska. GRANT and nutteri from the Pliocene Etchegoin and GALE (1931) included kindlei, nutteri and San Juaquin Formation, California, in the etchegoini into the variety of swiftii of genus Swiftopecten. the subgenus Pallium, and wattsi, wattsi On the other hand, in Soviet Russia, morani and cosibensis were included into KHOMENKO (1934) recorded swiftii under 398 KOichiro MASUDA the subgenus Pallium from the Pliocene genus Pecten (GRANT and GALE, 1931, formation of Schmidt Peninsula, North MACNEIL, 1943) and to the subgenus ern Sakhalin. Subsequently SLODKE Swiftopecten of the genus Pecten, but WITSCH (1938) illustrated Pecten (Pallium) subsequently MACNEIL (1967) referred swiftii from the Pliocene Pomyr Series them to the subgenus Swiftopecten of of Sakhalin and considered nutteri, et the genus Chlamys and ADEGOKE (1967) chegoini, heteroglyptus and pilutukensis raised Swiftopecten to generic rank. In as varieties of swiftii. Lately IL YINA eastern Soviet Russia swiftii and its (1963) figured etchegoini as a variety of varieties were referred to the subgenus swiftii under the genus Swiftopecten Pallium of the genus Pecten (SLODKE from the Pliocene of Kamchatka and WITSCH, 1938), but IL YINA (1963) raised KRISHTOFOVICH (1964) illustrated swiftii, Swiftopecten to generic rank and KRI nutteri and pilutukensis as varieties of SHTOFOVICH (1964) considered Swiftopec swiftii under the subgenus Swiftopecten ten as a subgenus of the genus Chlamys. of the genus Chlamys from the Pliocene From the remarks given above the of Sakhalin. Swiftopecten group is a confusing one in Since the historical review of the the Northern Pacific area. Therefore, swiftii group in Japan by the writer to clarify the confusion the writer de (MASUDA, 19o9a, 1960, 1962a), SAWADA scribes the type species from Japan and (1962), IWAI (1965) and UOZUMI, FUJIE presents discussions concerning it. and MATSUI (1966) figured swiftii under the genus Swiftopecten from the Pliocene formations in Northern Japan and also Description KASENO and MATSUURA (1965) figured Family Pectinidae swiftii under the genus Chlamys from the Pliocene of Ishikawa Prefecture. Subfamily Chlamyinae V. TEPPNER, 1918 As mentioned already HERTLEIN (1935) proposed Swiftopecten as a subgenus of Genus Swiftopecten HERTLEIN, 1935 the genus Pecten and designated switii Swiftopecten HERTLEIN, 1935, p. 319. BERNARDI as the type species, but gave Type-species :~Pecten swiftii BERNARDI, 1858. no diagnosis of his new subgenus. Recent, Northern Japan. Although swijtii had been described under the genus Pecten, the genus or Geological and geographical distribu subgenus Chlamys or as the subgenus tions :-Middle Miocene to Recent. North Pallium, HABE (1958) first used Swifto Pacific. pecten as a subgenus of the genus Chla Remarks :-As pointed out on the ear mys in Japan. The writer referred lier lines the Swiftopecten group has swiftii to the subgenus Swiftopecten of been considered a subgenus Pallium or the genus Chlamys (MASUDA, 1959a). But Manupecten. However, Pallium (SCHU because of its distinct morphological MACHER, 1817, fide GRANT and GALE, characters the writer raised Swiftopecten 1931) is distinguishable from Swiftopecten to generic rank (MASUDA, 1960). by its small shell, nearly equal auricles On the other hand, on the West Coast and well-marked cardinal crura, and of North America this species and its Manupecten (MONTEROSATO, 1889, fide varieties had been referred to the sub COSSMAN and PEYROT, 1914) differs from genus Pallium or Manupecten of the Swiftopecten by its right valve being 602. Swiftopecten 399 nearly equal to the left one in convexity, GRANT and GALE, Ibid., p. 174, pl. 10, both valves having equal sctJlpture, radial fig. 7. ribs which are nearly equal to their in 1934. Chlamys swijtii (BERNARDI) : KINOSHI terspaces in width, and by the left valve TA and IsAHAYA, Rept. Fish. Surv. Hok with np constricted radial ribs. Manu kaido Fish. Exp. Stat., No. 33, p. 14, pl. 10, fig. 74. pecten is considered to be closely related 1934. Pecten swijtii BERNARDI: KHOMENKO, with Swiftopecten as pointed out by Trans. Geol. Oil Inst., Ser. A, Fasc. 40, PHILIPPI (1900), GRANT and GALE (1931) p. 31, pl. 2, figs. 3, 4, pl. 3, figs. 2, 3. and MACNEIL (1967). Therefore, further 1935. Pecten (Pallium) swijtii BERNARDI: studies are necessary to settle the rela NoMURA and HATAI, Saito Ho-on Kai tionship between them. Mus., Res. Bull., No. 6, p. 98, pl. 9, fig. 8, pl. 10, figs. 3, 4, pl. 11, fig. 8, pl. 13. fig. 3. Swiftopecten swiftii (BERNARDI, 1858) 1938. Pecten (Pallium) swijtii BERNARDI: Pl. 48, figs. 1-5, Pl. 49, figs. 1-5 SLODKEWITSCH, Acad. Sci. USSR, Pal eont. Inst. Paleont. USSR, Vol. 10, pt. 1858. Pecten swijtii BERNARDI, jour. de Con 3, fasc. 18, p. 169, pi 22, fig. 2, pl. 23, ch., Vol. 7, 2nd Ser. Tome 3, p. 90, pl. figs. 1, 1a, 2, 3. 1, fig. 1, pl. 2, fig. 2. 1943. Pecten (Manupecten) kindlei DALL: 1867. Pecten swijtii BERNARDI: SCHRENCK, MAcNEIL in MAcNEIL, MERTlE and Moll. Amurl. Nordjap. Meeres, p. 487, PILSBRY, jour. Paleont., Vol. 17, no. 1, pl. 21, figs. 1-3. p. 87, pl. 12, figs. 7, 8. 1882. Pecten swijtii BERNARDI : KOCHIBE, 1950. Chlamys islandicus var. swiftii (BER Rika Kai-shi, Tokyo Univ. Press, No. 4, NARDI): KuBOTA, Cenozoic Res., No. 6, p. 75, pl. 5, fig. 2. p. 12, pl. 9, figs. 66, 67. 1888. Pecten swijtii BERNARDI: KOsTER und 1955. Chlamys swijti (BERNARDI) : HABE, KOBEL T in MARTINI und CHEMNITZ, Pub!. Akkeshi Mar. Biol. Stat., No. 4, Syst. Conch. Cab., Vol. 7, pt. 2, p. 142, p. 6, pl. 2, fig. 7. pl. 40, fig. 3. 1958. Chlamys (Swiftopecten) swifti (BER 1902. Pecten swijtii BERNARDI: YOSHIWARA, NARDI) : HABE, Publ. Seta Mar. Biol. Zool. Mag. Tokyo, Vol. 14, no. 162, p. Lab., Vol. 6,.no. 3, p. 263, pl. 12, fig. 18. 144, pl. 2, figs. 6a-b. 1958. Chlamys (Swiftopecten) swijti (BER 1906. Pecten (Chlamys) parmeleei DALL: AR NARDI) : YAMAMOTO and flAB!', Mar. NOLD, U.S. Geol. Surv. Prof. Paper No. Biol. Stat. Asamushi, Tohoku Univ., 47, p. 119, pl. 41, figs. 5, 5a. Bull., No. 9, pt. 1, p. 15, pl. 3, fig. 4, 1920. Pecten (Chlamys) kindlei DALL, U.S. pl. 5, figs. 4, 7. Geol. Surv. Prof. Paper 125-C, p. 30, pl. 1958. Chlamys swiftii (BERNARDI) : ToMIZA 6, figs. 2, 7. WA in T. and K. YAGI, Geol. Kami 1925. Pecten swijtii BERNARDI: YoKOYAMA, Minochi, p. 326, pl. 3, figs. 5a-b. jour. Colt. Sci., Imp. Univ. Tokyo, Vol. 1958. Chlamys swifti (BERI\:ARDI) : FUJIE, 45, art. 5, p. 27, pl. 2, fig. 1. Cenozoic Res., No. 28, p. 668, pl. 27, 1926. Pecten swiftii BERNARDI: YoKOYAMA, figs. 29, 30. jour. Fac. Sci., Imp. Univ. Tokyo, Vol. 1959. Chlamys (Swiftopecten) swiftii (BER 1, pt. 8, p. 303, pl. 37, figs. 5, 6. NARDI) : MAsUDA, Trans. Proc. Palae 1931. Pecten (Pallium) swijtii BERNARDI: ont. Soc. japan, N.S., No. 34, p. 87, pl. GRANT and GALE, Mem. San Diego Soc. 9, figs. 1-7. Nat. Hist., Vol. 1, p. 171, pl. 10, figs. 1959. Chlamys swiftii (BERNARDI): OYAMA, la-b, 4a-b. Sci. Photogr. Club, Tokyo, II, Chlamys Hi31. Pecten (Pallium) swiftii kindlei DALL: (5) , figs. 6-8. 400 Koichiro MASUDA 1960. Swiftopecten swiftii (BERNARDI) : MA its large and thick, posteriorly contorted SUDA, Sci. Rept., Tohoku Univ., 2nd Ser. shell which forms an angle of about 70• (Geol.), Spec. Vol. No. 4, p. 380, pl. 39, at apex and is much higher than long, figs. 9, 10. four prominent round-topped radial ribs l 960. Chlamys (Swiftopecten) swifti (BER· with several, fine radial threads, two i'>ARDI) : HABE, Shirikishinai Mar. Bioi. Inst., Hokkaido Gakugei Univ., Pub!., subordinate radial ribs near submargins, No. 2, p. 4, pl. 1, fig. 16, pl. 5, figs. fine intercalary threads. rather conspi· 7, 8. cuous concentric constrictions, very large 1962. Swiftopecten swiftii (BERNARDI) : MA triangular anterior auricle and flat hinge SUDA, Sci. Rept., Tohoku Univ., 2nd plate in the right valve. The left valve Ser. (Geol.), Vol. 33, no. 3, p. 196. is characterized by its five prominent, 1962. Swiftopecten swiftii (BERNARDI) : SA round-topped radial ribs which are usu WADA, Mem. Muroran Inst. Techno/., ally nodose and by its young shell which Vol. 4, no. 1, p. 73, pl. 1, fig. 3, pl. 2, is nearly flat or rarely a little concave fig. 3, pl. 3, fig. 4. upwards. 1964. Chlamys (Swiftopecten) swiftii (BER· NARDI) : KRISHTOFOVICH, Soviet Petrol. By the re-examination of the type spe· Sci.-Res. Geol., Expl. Inst., 232, p. 143, cimen (U.S. Nat!. Mus., No. 499058) and pl. 20, figs. 1, 2. numerous topotype specimens, it is con 1965. Swiftopecten swiftii (BERNARDI) : l\\"AI, sidered that Pecten (Chlamys) kindlei DALL Bull. Educ. Fac., Hirosaki Univ., No. 5, is a synonym of swiftii, because the con· p. 29, pl. 15, figs. 9, 10. vexity of the valves, low radial ribs and 1966. Swiftopecten swiftii (BERNARDI) : Uo concentric constrictions observed in kind ZUMI, FUJIE and MATSUI, jour. Fac. lei are quite similar with those of swijtii. Sci., Hokkaido Univ., Ser. 4 (Geol. Similarly the hypotype specimen (U.S. Mineral.), Vol. 13, no. 2, p. 175, pl. 14, Nat!. Mus., No. 164842) and the specimens fig. 2. 1967. Chlamys (Swiftopecten) donmilleri MAc labelled as parmeleei (Dept. Geol., Stan· NEIL, U.S. Geol. Surv. Prof. Paper 553, ford Univ., No. 4838) from the" Wildcat" p. 12, pl. 3, figs. 1, 4, 6. Formation in the vicinity of Crescent 1967. Chlamys (Swiftopecten) swiftii kindlei City, Northern California, are synonyms (DALL) : MAcNEIL, Ibid., p. 13, pl. 3, of swijtii. figs. 5, 7-9. Chlamys (Swijtopecten) donmilleri was described by MACNEIL (1967) from the Remarks:-The original description is Miocene Yakataga Formation, Alaska, quoted below for the sake of persons to based upon rubber casts. The morpho· whom the original work is inaccessible. logical characters of the type specimens "Testa maxima, utrinque convexa, so (U.S. Nat!. Mus., No. 644882, 644883, lidiuscula, nitida, elongata, valva supe 644884) as observed by the writer coin rore costis nodosis, majoribus 5, munita; cide with those of Swiftopecten swijtii, nodis distantibus concentrice dispositis; therefore, MACNEIL's donmilleri is a syno· interstiis longitudinaliter radiatis, minu nym of Swiftopecten swiftii. But Chlamys tissime granularis, costis concentricis 5 (Swijtopecten) cf. donmilleri described by graditim dispositis; valva inferiore vix MACNEIL (1967) from the Miocene Unga nodosa, regulariter radiatum sulcata; Conglomerate, Alaska Peninsula can not auriculis valde inaequilateralibus; supra be identified with swijtii but with Chla nodosis, infra sulcatis." mys cosibensis (YOKOYAMA) which is The present species is characterized by known from the Miocene to Pliocene 602. Swiftopecten 401 formations in Japan. For the Chlamys ont. Soc. japan, N.S., No. 34, p. 93. cosibensis group another paper is expect ed to be written. Remarks:-The original description is Swijtopecten swijtii resembles Chlamys " This species is close to P. Swiftii BER· cosibensis (YOKOYAMA) and has been con NARDI of Japan (J. de Conchyl., vii, plates fused with it (MASUDA, 1959b). Also Chla 1 and 2, 1858) but smaller, and differs mys etchegoini (ANDERSON), Chlamys nut by the smooth top surface of the ribs, teri (ARNOLD), Chlamys wattsi (ARNOLD) which in P. Swiftii are more or less and Chlamys wattsi morani (ARNOLD) de striated or coarsely threaded, and by scribed from the Pliocene deposits of the not alternated radial riblets on the California resemble swiftii, which can be right posterior ear; also, especially, by distinguished from those species and cosi the profuse coalescent microscopically bensis by its large, higher, posteriorly checkered squamation, which makes a contorted shell, smaller apical angle, tri complete external coating to the valve. angular large anterior auricle and nearly Alt. 45, lat. 38 mm ". flat left valve in younger stage. Parmeleei is characterized by its small Type locality :-Northern Japan. Re shell which is contorted posteriorly in cent. the younger stage but tends to become Geographical distribution :-Living in rounded with growth, four prominent Northern Japan, Sea of Okhotsk and but rather low, round-topped radial ribs along East Korea. which are broader than their interspaces Geological distribution:-Middle Mio with several, fine radial threads, two cene to Recent in Japan, Pliocene to subordinate radial ribs near submargins, Recent in Sakhalin and Kamchatka, and rather conspicuous concentric constric Middle (?) to Late Miocene to Middle tions, very large triangular auricle in Pleistocene along the West Coast of the right valve, and by the left valve North .America. having five round-topped radial ribs. Parmeleei differs from the closely re lated Swiftopecten swiftii in having small Swiftopecten swiftii parmeleei er shell which tends to become rounded (DALL, 1898) with growth and somewhat larger apical angle. Thus, morphologically, parmeleei Pl. 48, figs. 6, 7, Pl. 49, figs. 6-8. may have descended from swiftii and is 1898. Pecten (Chlamys) parmeleei DALL, Trans. considered a subspecies of swiftii. Wagner Free Inst. Sci., Philadelphia, From Chlamys cosibensis (YOKOYAMA) Vol. 3, pt. 4, p. 708, pl. 37, figs. 14, a. parmeleei differs by its higher shell which 1906. Pecten (Chlamys) parmeleei DALL: AR is posteriorly contorted in the younger NOLD, U.S. Geol. Surv. Prof. Paper, No. stage and triangular anterior auricle. 47, p. 119, pl. 41, figs. 1, 1a. GRANT and GALE (1931) figured par 1907. Pecten (Chlamys) parmeleei DALL: ELD· meleei from the Middle Pliocene deposits RIDGE and ARNOLD, U.S. Geo[. Surv., at Holser Canyon, Los Angeles, California, Bull., No. 309, p. 25, pl. 36, fig. 7. but their specimens should be identified 1959. Pecten (Pallium) swiftii etchegoini AN DERSON: GLEN, Univ. Calif. Publ., Geol. probably with Chlamys species. In 1950 Sci., Vol. 36, no. 2, p. 167, pl. 15, fig. 6. WOODRING and BRAMLETTE illustrated 1959. Chlamys (Swiftopecten) swiftii parmeleei Chlamys parmeleei from the Pliocene (DALL) : MAsUDA, Trans. Proc. Palae- Careaga Sandstone, Santa Maria district, 402 Koichiro MASUDA California. However, according to the scribed as the varieties of swijtii from writer's study of the hypotype specimen the Pliocene deposits of Sakhalin and (U.S. Nat!. Mus., No. 560101) their par Kamchatka but considering from their meleei should be identified with Chlamys descriptions and figures Swijtopecten in etchegoini (ANDERSON). GLEN (1959) de Sakhalin and Kamchatka is represented scribed Pecten (Pallium) swijtii etchegoini only by swijtii (s.s.). from the "Merced" Formation, San Mateo, As already pointed out (MASUDA, 1959a) California, but the writer considers that some morphological differences such as GLEN's specimen (Mus. Paleont., Univ. concentric constrictions or natures of the Calif. Berkeley, No. 37614) should be radial ribs of the left valve are observed identified with parmeleei. In 1966 STAN in the specimens living in the northern TON recorded parmeleei from the Late areas and those living in more southern Miocene Castaic Formation, Los Angeles, areas. These morphological features California, but STANTON's specimen has may suggest that the specimens living not been authenticated. in the northern areas are somewhat less Type locality:-Pacific Beach, San Diego, influenced by the water temperature California. than those living in more southern areas. Distribution:-Middle to Southern Cali And, the morphological differences ob fornia. Middle Pliocene. served between the fossil specimens and Recent ones may be the reflection of the Remarks environmental conditions such as ther mal conditions. Such inference may be As already pointed several species or interpreted that the so-called kindlei re subspecies of the West Coast of North presents the northern type of swiftii and America have been referred to Swifto that some of the so-called parmeleei from pecten. However, among those species northern California the rather southern the true Swijtopecten is represented only type of swijtii. Also the so-called don by the so-called kindlei and donmilleri milleri may represent the southern type from Alaska, some of the so-called par of swiftii. meleei from northern California, and par As known at present the oldest occur meleei from middle to southern Califor rence of swiftii is the Middle Miocene nia, whereas the other species hitherto Otsutsumi Formation in the environs of referred to Swiftopecten should be refer Sendai, Northeast Honshu, Japan, where red to Chlamys or some other genera. it is rather rare, and its associated mollus According to the writer's study of the can fauna mainly consists of what we type specimen (Mus. Paleont., Univ. Calif. now call temperate water elements, such Berkeley, No. 36639) of Swijtopecten ade as Miyagipecten matsumoriensis MASUDA, kunbiana ADEGOKE, 1969 which was first Chlamys kaneharai (YOKOYAMA), Dosinia described as Swiftopecten sp. (ADEGOKE, lwneharai YOKOYAMA, Mercenaria chi 1967) and subsequently named adekun taniana (YOKOYAMA), Spisula voyi GABB, biana, n. sp. from the Miocene Santa etc. But with the progress of geologi Margarita Formation, California is dif cal age swijtii gradually increased its ferent from Swiftopecten, because its dominancy in association with the in hinge area is characteristic to the genus crease of cooler water molluscs, bryo Lyropecten. zoans, barnacles, foraminifers, etc. from Also several species have been de- the Miocene through Pliocene to Recent. 602. Swiftopecten 403 From the morphological differences ob Middle Pliocene and it became extinct served between the Recent and fossil at the end of Middle Pliocene. On the specimens it is inferred that Swiftopecten other hand, Swiftopecten swiftii extended swiftii acquired its stability as a species its distribution to northern California in during the Middle Miocene and survived the Early Pliocene but ~ith the progress to the Recent with little morphological of geological age it retreated· to Alaska variation (MASUDA, 1959a, 1960). and became extinct in the Middle Pleis On the other hand, the first appear tocene. Therefore, it is expected that ance of Swiftopecten along the West swiftii will be found from the Pliocene Coast of North America is the Miocene or Pleistocene formations of the north Yakataga Formation in Alaska, which ern part of the West Coast of North yielded donmilleri; it is believed to be America and also from the Pliocene of Middle to Late Miocene in American Kamchatka. The geographical distribu chronology (MACNEIL, 1967). As the tion of swiftii and parmeleei is shown in morphological characteristics of donmil Text-fig. 1. leri can be interpreted to represent the MACNEIL (1943, 1967) reported Forti southern type of swiftii (MASUDA, 1959a), pecten from Alaska and the writer and it is inferred that the Yakataga Forma ADDICOTT (MASUDA and ADDICOTT, 1970) tion may have been deposited under the recorded Yabepecten from the Early Plio influence of moderate to rather cool cene Montesano Formation in Washing water environmental conditions. This ton, and from the same formation the view is also supported by the associated writer described Mizuhopecten warreni, fauna (ADDICOTT et al., 1971). n. sp. (MASUDA, 1971). Therefore, the It is thought that the occurrence of occurrences of Swiftopecten, Fortipecten, Swiftopecten along the West Coast of Yabepecten and Mizuhopecten in theW est North America is a result of its migra Coast of North America may be signifi tion from East Asia to North America. cant for interregional correlation between Therefore, the writer considers that the Asia and North America. Those genera Yakataga Formation is at least not older are all known from the Cenozoic forma than the Otsutsumi Formation in Japan. tion of Japan. The changes of the environmental con The occurrence of Swiftopecten swiftii ditions from the Miocene to Recent from the Middle Miocene formation in (DURHAM, 1950, MASUDA, 1962b) probably Alaska suggests that the first Bering land have greatly influenced the marine fauna. bridge connecting North America and As swiftii had acquired its stability as Asia was in the Middle Miocene. On a species in the Middle Miocene (MASU the other hand, MACNEIL (1967) consid DA, 1959a), it could survive to the Recent ered that the Unga Conglomerate yield in the northwestern Pacific region but ing Chlamys (Swiftopecten) cf. donmilleri in the northeastern Pacific region it be in the Alaska Peninsula represents the came extinct in the Middle Pleistocene. Middle Miocene in American chronology, As the results of the gradual changing but according to the writer's study MAC environmental conditions, it is inferred NEIL's cf. donmilleri is a synonym of that Swiftopecten parmeleei branched off Chlamys cosibensis (YOKOYAMA) and is from the Swiftopecten swiftii stock as a morphologically a Pliocene type of cosi result of its southward migration follow bensis. Therefore, the geological age of ed by localization and adaptation in the the Yakataga Formation is open toques- 404 K8ichir6 MASUDA Pacific Ocean \ . "' 150E 150W '"'12cfw Text-fig. 1. Geographical distribution of Recent and fossil Swiftopecten. e--Swiftopecten swiftii (BERNARDI) (Recent) 0--Swiftopecten swiftii (BERNARDI) (Fossil) x --Swiftopecten swiftii panneleei (DALL) tion. Although further studies on the Prof. Paper 750-C, pp. Cl.8-C33, figs. 1-6. stratigraphy and paleontology of the ANDERSON, F.M. (1.905) : A stratigraphic Yakataga Formation are necessary to study of the Mount Diablo Range of Cali settle this problem, the writer is inclined fornia. Proc. Calif. Acad. Sci., Ser. 3, Vol. 2, pp. 155-248, pis. 1.3-35. to consider that a part of the formation ARNOLD, R. (1906) : Tertiary and Quater with donmilleri may represent the Late nary pectens of California. U.S. Ceo!. Miocene or Early Pliocene. Considering Surv. Prof. Paper 47, pp. 7-146, pis. 1-53. from the occurrences of Y abepecten, Mi BERNARDI, M. (1858) : Description d'especes zuhopecten and Fortipecten from the Early nouvelles. jour. de Conch., Vol. 7, 2nd Pliocene formations of the northern West Ser., T. 3, pp. 90-94, pis. 1-2. Coast of North America, it may be that CossMAN, M. and PEYROT, A. (1914) : Con the Bering strait was closed by a land chologieNeogenique deL'Aquitaine. Tome bridge during the Late Miocene or very II, Pelecypodes. Act. Soc. Linn. Bord., Early Pliocene. pp. 1-496, pis. 1-26. DALL, W.H. (1898) : Contributions to the Tertiary fauna of Tampa and the Plio References cene beds of the Caloosahahatchie River. Trans. Wagner Free Inst. Sci., Philadel ADEGOKE, O.S. (1967) : California Late Mio phia, Vol. 3, pt. 4, pp. 571-947, pis. 26-37. cene records of Swiftopecten HERTLEIN, -- (1920) : Pliocene and Pleistocene fossils 1935. Veliger, Vol. 9, no. 3, pp. 337-339, from the Arctic Coast of Alaska and the pl. 47. Auriferous Beaches of N orne, Norton -- (1969) : Stratigraphy and paleontology Sound, Alaska. U.S. Ceo/. Surv. Prof. of the marine Neogene formations of the Paper 125-C, pp. 23-37, pis. 4-5. Coalinga region, California. Univ. Calif. DuRHAM, J.W. (1950) : Cenozoic marine cli Pub!., Ceo!. Sci., Vol. 80, pp. 1-241, pis. mate of the Pacific coast. Bull. Ceo!. 1-13, 6 text-figs., 3 maps. Soc. Amer., Vol. 61, pp. 1243-1264, 3 text ADDICOTT, W.O., KANNO, S., SAKAMOTO, K. figs. and MILLER, D.]. (1971) : CLARK's Ter -- (1961) : Palaeogeographic conclusions in tiary molluscan types from the Yakataga light of biological data. "Symposium, district, Gulf of Alaska. U.S. Ceol. Surv. Pacific basin biogeography". 1Oth Pacific 602. Swiftopecten 405 Congress, pp. 355-365, 4 text-figs. Academy of Sciences, 1932. Proc. Calif. -- and MAcNEIL, F.S. (1967) : Cenozoic mi Acad. Sci., Ser. 4, Vol. 21, no. 25, pp. grations of marine invertebrates through 301-328, pis. 18-19. the· Bering Strait region, in HOPKINs, ILYINA, A.P. (1963): Mollusks in the Neo D.M., The Bering land bridge, pp. 326-349, gene of Kamchatka. Soviet Petrol. Sci. . 4 tables, Stanford Univ. Press. Res. Geol. Expl. lnst., 202, pp. 1-242, pis. ·ELDRIDGE, G.H. and ARNOLD, R. (1907) : The 1-54. Santa Clara Valley, Puente Hills and Los IWAI, T. (1965) : The geological and pale Angeles Oil districts, southern California. ontological studies in the marginal area Bull. U.S. Geol. Surv., No. 309, pp. 1-266, of the Tsugaru Basin, Aomori Prefecture, pis. 1-41, 17 text-figs. Japan. Bull. Educ. Fac., Hirosaki Univ., FAUSTMAN, W.F. (1964) : Paleontology of the No. 15, pp. 1-68; pis. 12-20, 3 text-figs., Wildcat Group at Scotia and Centerville 10 tables. . Beach, California. Univ. Calif. Publ., Geol. KASENO, Y. and MATSUURA, N. (1965) : Plio Sci., Vol. 41, pp. 97-151, pis. 1-3, 7 text cene shells from the Omma. Formation figs. around Kanazawa City, Japan. Sci. Rept. FUJIE, T. (1958) : Pleistocene molluscan fos Kanazawa Univ., Vol. 10, no. 1, pp. 27-62, sils (Pelecypoda) from the Shikonai For pis. 1-20, 3 text-figs., 5 tables. mation, Hokkaido. Cenozoic Res., No. 28, KEEN, A.M. and BENTSON, H. (1944) : Check pp. 663-679, pis. 27-28. list of California Tertiary marine Mol GLEN, W. (1959) : Pliocene and Lower Pleis lusca. Geol. Soc. Amer., Spec. Paper, No. tocene of the western part of the San 56, pp. 1-280, 4 text-figs. Francisco Peninsula. Univ. Calif. Publ., KHOMENKO, l.P. (1934) : The stratigraphy of Geol. Sci., Vol. 36, no. 2, pp. 147-198, pis. the Tertiary beds of the south-western 15-17, 5 text-figs. coast of the Schmidt Peninsula (Northern GRANT, U.S., IV, and GALE, H. (1931) : Cata Sakhalin). Trans. Geol. Oil Inst., Ser. A, logue of the marine Pliocene and Pleis Fasc. 40, pp. 12-86, pis. 1-19. tocene Mollusca of California and adjacent KINOSHITA, T. and IsAHAYA, T. (1934): Cata regions. Mem. San Diego Soc., Nat. Hist., logue of marine Mollusca from Hokkaido. Vol. 1, pp. 1-1036, pis. 1-32, 15 text-figs. Rept. Fish. Surv. Hokkaido Fish. Exp. Stat., HABE, T. (1955) : Fauna of Akkeshi Bay, 21, No. 33, pp. 1-19, pis. 1-15. Pelecypoda and Scaphopoda. Pub!. Akke KocHIBE, T. (1882) : Johoku Chishitsu Hen shi Mar. Bioi. Stat., No. 4, pp. 1-31, pis. (Geology of Northern Hitachi), Rika Kai 1-7. shi, Tokyo Univ. Press, No. 4, pp. 1-153, -- (1958) : Report on the Mollusca chiefly pis. 1-9. collected by the S.S. Soyo-maru of the KRISHTOFOVICH, L.V. (1964) : Mollusks in Imperial Fisheries Experimental Station the Tertiary sediments of Sakhalin .. Soviet on the continental shelf bordering Japan Petrol. Sci.-Res. Geol. Expl. lnst., 232, pp. during the years 1922-1930. Part 3. Lamel 1-343, pis. 1-55. libranchia (1). Pub!. Seto Mar. Bioi. Lab., KuLJOTA, K. (1950) : Explanation of Cenozoic Vol. 6, no. 3, pp. 241-279, pis. 11-13. fossils from northern Japan, 9. Fossil -- (1960) : Fauna of shell-bearing mollusks Pectinidae from the Setana Series. Ceno of the sea around Shirikishinai, Hokkai zoic Res., No. 6, pp. 12-18, pis. 8-9. do. 1. Pelecypoda. Fauna and flora of the KUsTER, H.C. and KoBELT, W. (1882): Die sea around the Shirikishinai Marine Sta Gattungen Spondylus und Pecten in MAR tion. Shirikishinai Mar. Stat. Bioi. lnstr., TINI und CHEMNITZ, Syst. Conch. Cab., Hokkaido Gakugei Univ., No. 4, pp. 1-10, Vol. 7, pt. 2, pp. 1-296, 72 pis. pis. 1-5. MAcNEIL, F.S. (1967) : . Cenozoic pectinids of HERTLEIN, L.G. (1935) : The Templeton Alaska, Iceland and other northern re Crocker Expedition of the California gions. U.S. Geol. Surv. Prof. Paper 553, 406 Koichiro MASUDA pp. 1-57, pis. 1-25. -- (1960) : On morphogenesis of Nanao -- (1970) : New Pliocene Chlamys (Swifto chlamys. Sci. Rept., Tohoku Univ., 2nd pecten) and Beringius from the Alaska Ser. (Geol.), Spec. Vol. No. 4, pp. 371- Peninsula. Nautilus, Vol. 84, no. 2, pp. 383, pl. 39, 10 text-figs. 69-74, 1 pl. -- (1962a) : Tertiary Pectinidae of Japan. --, MERTlE, ].B. Jr. and PILSBRY, H.A. Ibid., Vol. 33, no. 2, pp. 117-238, pis. 18- (1943) : Marine invertebrate faunas of 27, 11 text-figs. the buried beaches near Nome, Alaska. -- (1962b) : Note on the Tertiary Pectini jour. Paleont., Vol. 17, no. 1, pp. 69-96, dae of Japan. Ibid., Spec. Vol. No.5, pp. pis. 10-16. 159-193, 9 text-figs., 9 tables. --, WoLFE, ].A., MILLER, D.]. and HoP -- (1971a) : On some PatinDpecten from KINS, D.M. (1961) : Correlation of Ter North America. Trans. Proc. Palaeont. tiary formations of Alaska. Bull. Amer. Soc: japan, N.S., No. 83, pp. 166-178, pis. Assoc. Petrol. Geol., Vol. 45, no. ll, pp. 19-21, 2 text-figs. 1801-1809, 2 text-figs. -- (1971b) : Amussiopecten from North A MASUDA, K. (1959a) : On the Miocene Pecti merica and northern South America. Ibid., nidae from the environs of Sendai: Part No. 84, pp. 205-223, pis. 25-26, 4 text-figs. 14, On Pecten swiftii BERNARDI. Trans. -- and ADDICOTT, W.O. (1970) : On Pecten Proc. Palaeont. Soc. japan, N.S., No. 34, (Amusium) condoni HERTLEIN from the pp. 101-111, pl. 9, 1 text-fig. West Coast of North America. Veliger, -- (1959b) : On the Miocene Pectinidae from Vol. 13, no. 2, pp. 153-156, 1 pl. the environs of Sendai : Part 15, Pecten NoMLAND, ].C. (1917) : The Etchegoin Plio cosibensis YoKOYAMA and its related spe cene of Middle California. Univ. Calif. cies. Ibid., No. 35, pp. 130-141, pl. 13, 1 Pub!., Geol. Sci., Vol. 10, no. 14, pp. 109- text-fig. 254, pis. 1-12, 2 text-figs. ------···-~------ Explanation of Plate 48 (Natural size) Right valve Figs. 1-5. Swiftopecten swijtii (BERNARDI). 1, Dept. Geol., Stanford Univ., No. 4846. Loc.: Intermediate Beach, Nome, Alaska. Middle Pleistocene. 2, IGPS*, coli. cat. no. 90593. Loc.: About 300m NW of Kurosawa, Akita City, Akita Prefecture. Sasaoka Pliocene. 3, 4, Saito Ho-on Kai Mus., Reg. no. 21266. Loc.: Tayazawa, Wakimoto-machi, Oga City, Akita Prefecture. Shibikawa Pliocene. 5, Dept. Geol. Stanford Univ., No. 4838. Loc.: Crescent City wharf, Del Monte County, California. "Wildcat" Pliocene. Figs. 6, 7. Swiftopecten swiftii parmeleei (DALL). 6, Dept. Geol., Stanford Univ., No. 47210. Loc.: East of Capitola, Santa Cruz County, California. Purisima Pliocene. 7, Los Angeles County Museum. Loc. : South central part of San Diego County, California. San Diego Pliocene. *-Institute of Geology and Paleontology, Tohoku University, Sendai, Japan. MASUDA: Sw1}'topecten Plate 48 7 602. Swijtopecten 407 NOMURA, S. and HATAI, K. (1935) : Pliocene ToMIZAWA, T. (1958) : Studies on fossils Mollusca from the Daishaka shell beds in from the Kami-Minochi district, Nagano the vicinity of Daishaka, Aomori-ken, Prefecture, in T. and K. YAGI, Geology Northeast Honshu, Japan. Saito Ho-on of Kami-Minochi-gun, Nagano Prefecture. Kai Mus., Res. Bull., No. 6, pp. 83-137, pp. 317-347, pis. 1-14, 5 text-figs., 2 tables. pis. 9-13. UozuMI, S., FuJIE, T. and MATSUI, M. (1966) : OYAMA, K. (1959) : The molluscan shells, II, Neogene molluscan fauna in Hokkaido. Chlamys (5). Sci. Photogr. Club, Tokyo. Part 3, Description of the Ainonai fauna PHILIPPI, H.A. (1900) : Beitrage zur Morpho associated with Desmostylus cf. minor logie und Phylogenie der Lamellibran NAGAO, from Kitami district, East Hok chier. II. Zur Stammesgeschichte der Pec kaido. jour. Fac. Sci., Hokkaido Univ., tiniden. Zeit. Deutsch. Ceo/. Cesellsch., Ser. 4 (Ceo/. Mineral.), Vol. 13, no. 2, Bd. 52, pp. 64-117, 24 text-figs. pp. 119-183, pis. 14-15, 3 text-figs. SAWADA, Y. (1962): The geology and pale WooDRING, W.P. and BRAMLETTE, M.N. ontology of the Setana and Kuromatsunai (1950) : Geology and paleontology of the areas in southwest Hokkaido, Japan. Mem. Santa Maria district, California. U.S. Muroran lnst. Techno!., Vol. 4, no. 1, pp. Ceo/. Surv. Prof. Paper 222, pp. 1-185, pis. 1-110, pis. 1-8, 9 text-figs., 13 tables. 1-23, 9 text-figs. SCHRENCK, L. (1867) : Mollusken des Amur YAMA:v!OTO, G. and HABE, T. (1959) : Fauna Iandes und des nordjapanischen Meeres. of shell-bearing mollusks in Mutsu Bay. Reisen und Forshung Amurlande in dem Lamellibranchiata (1). Mar. Biol. Station 1854-1856. Vol. 2, pt. 3, pp. 259-976, pis. Asamushi, Tohoku Univ., Bull., Vol. 9, no. 12-28, 1 map. 1, pp. 1-20, pis. 1-5. SLODKEWITSCH, W.S. (1938) : Tertiary Pele YoKOYAMA, M. (1911) : Pectens from Koshi cypoda from the Far East. Pts. 1 & 2. ba Neogene. Ceo!. Soc. Tokyo, jour., Vol. USSR Acad. Sci., Paleont. Inst., Paleont. 18, no. 208, pp. 1-5, pl. 1. of USSR, Vol. 10, pt. 2, fasc. 19, pp. 1- -- (1926) : Fossil shells from Sado. jour. 275, pis. 1-106. Fac. Sci., Imp. Univ. Tokyo, Vol. 1, pt. 8, STANTON, R.J. (1966) : Megafauna of the pp. 249-312, pis. 32-37. Upper Miocene Castaic Formation, Los YosiiiWARA, S. (1902) : Japanese shells. Zoo/. Angeles County, California. jour. Paleont., Mag. Tokyo, Vol. 14, n0. 162, pp. 141-145, Vol. 40, no. 1, pp. 21-40, pis. 5-7, 2 text pis. 1-5. figs. Akita :f:k ~LI Sawada-machi iH~IliiBJ Kaidateno-sawa fl Jr. iR Sa wane iR tR Kurosawa !R. iR Shibikawa fi.ffl Jll Oga lJ3 UE Tayazawa III :t:l- iR Otsutsumi -j( ~ Tomizawa rn iR Sa do-gun t!r. 'lf~ Wakimoto-machi n.;pt: IBJ ,..,,. i/Jf. Sasaoka ·w: fliU 408 K6ichiro MASUDA Explanation of Plate 49 (Natural size) Left valve Figs. 1-5. Swiftopecten swiftii (BERNARDI). 1, Dept. Geol., Stanford Univ., No. 4846. Loc.: Intermediate Beach, Center Creek, Nome, Alaska. 2, Saito Ho-on Kai Mus., Reg. no. 16827. Loc.: Tomizawa, Wakimoto-machi, Oga City, Akita Prefecture. Shibikawa Pliocene. 3, 4, Dept. Geol., Stanford Univ., No. 4838. Loc. : Crescent City wharf, Del Monte County, California. "Wildcat" Pliocene. 5, IGPS, coli. cat. no. 90597. Loc. : Kaidate-no-sawa, Sawada-machi, Sado-gun, Niigata Prefecture. Sawane Pliocene. Figs. 6-8. · Swiftopecten swiftii parmeleei (DALL). 6, 8, Los Angeles County Museum. Loc.: 305 A. South central part of San Diego County, California. San Diego Pliocene. 7, IGPS, coli. cat. no. 92043. Loc. : Tijuana River south western San Diego County, California. San Diego Pliocene. MASUDA: Swijtopecten Plate 49 Trans. Proc. Palaeont. Soc. Japan, N.S., No. 87, pp. 409-413, September 30, 1972 603. SCAPHOPODA-LIKE FOSSILS FROM THE UDO FORMATION (MIOCENE) OF MIYAZAKI PREFECTURE, JAPAN* KOTORA HATAI, HIROSHI NODA and KENSHIRO OGASAHARA Institute o~ Geology and Paleontology, Faculty of Science, Tohoku University, Sendai, Japan 'E'(~eyl!,~ 9=JW!illl:!l\~Ff 1'.'1 iiU1~1JEJ'Ltoldl::t:dc -:>v' -c : 'll~f.i y;uc a:; <3Ei~T sociate Professors Takehiko Iw AI, Biro Introduction and acknowledgements saki University, Taisuke TAKAY ASU, Aki During the excursion for observations, ta University, Tamio KOTAKA, Tohoku discussions and collection of the inverte University, Saburo KANNO, Tokyo Uni brate marine fossils of different strati versity of Education, Hiroyuki OTSUKA, graphic units of Mizuho age distributed Kagoshima University; Junji ITOIGAWA, in Miyazaki Prefecture, Kyushu, Japan Nagoya University, Kiyotaka CHINZEI, in the latter part of October, 1971, abun Tokyo University, and Sakae OHARA, dant scaphopod-like fossils were collected Chiba University, Drs. Yasuhide IWA and brought back to the laboratory for SAKI, Tokyo University, Kazuo OKAMOTO, study. These form the subject of the Hiroshima University, and Mr. Kimihiko present article. OKI, Kagoshima University. Here the writers express their deep appreciation to the undermentioned per sons for their kind cooperation in the Fossil locality and stratigraphic field and talks during the evening, name position ly ; Professors Tokio SHIKAMA, Yokohama National University, Koichiro MASUDA, The abundant scaphopod or Dentalium Miyagi College of Education, and Shozo like specimens were collected from a HAYASAKA, Kagoshima University; As- siltstone of a road cliff south of Uzu tsumi near the Kagamisu-toge (pass) on * Received Jan. 23, 1972; read June 3, 1972 the road leading from Nagayama to Ko at Utsunomiya. gochi, south of Kiyotake, Kiyotake-cho, 409 410 Kotora HATAI, Hiroshi NODA and Kenshiro OGAS'AHARA Miyazaki-gun, Miyazaki Prefecture. The fossils, although from most probably the siltstone is a part of the Boroishi Mem same cliff from where SHUTO recorded ber of the Udo Formation (Miocene) and the fossil molluscs mentioned above, did also of the Aoshima facies of the Miya not occur in association with the mol zaki Group of SHUTO (1961). luscs. Although from the same litho The fossil locality of the scaphopod facies as the molluscs, the scaphopod or Dentalium-like fossils nearly corre like fossils were found forming a close sponds to locality no. 12 or 13 of SHUTO assemblage separated from the nearest (1961). SHUTO (op. cit.) recorded from molluscan fossil both vertically and lat the locality (no. 12 and no. 13) such fos erally by a distance of more than sev sil molluscs as, Acila (Acila) submirabilis eral ten centimeters. MAKIY AMA, Saccella confusa kongiensis The stratigraphic subdivision of the OTUKA, Yoldia (Tepidoleda) naganumana Miyazaki Group according to SHUTO (OTUKA), n. subsp., Paliolum (Delecto~ (1961) is reproduced in Table 1, for the pecten) peckhami (GABB), Amussiopecten sake of the readers. iitomiensis (OTUKA), ]oanisiella cumingii (HANLEY), Laevicardium pigmaea SHUTO, The scaphopod-like fossils V epricardium kyushuense SHUTO, V en tricoloidea foveolata miyazakiensis (SHU The scaphopod-like fossils were found TO), Pitar sp., Paphia (Paphia) exilis taka in the siltstone facies of the Boroishi okaensis SHUTO, Clementia (Clementia) Member of the Udo Formation. The papyracea (GRAY). tubular fossils were found in a position These fossils, all marine in origin, almost parallel with the bedding plane were considered to be Miocene in age of the stratum preserving them. None by SHUTO (op. cit.) and to characterize of the calcareous tubular structures were the Boroishi Member, the lowest part of found to be either vertical or oblique to the Udo Formation. The scaphopod-like the bedding plane at least where they Table 1. Stratigraphic subdivision of the Miyazaki Group according to SHUTo (1961). Tozakibana M. Kibana Togo ·M. I I I I .---'t---1..----.....L--..,L::------\-- ...... : ..L- - --- ~ ~' Gonobaru "4"o:', ""1,. ' ' l\L +.';. __ 603. Scaphopod-like fossils 411 Text-figs. 1, 2. Ditrupa miyazakiensis HATAI, No DA and 0 GASA HARA. Natural size. Tex t-fig. 1- weathered specimens. Tex t-fig. 2- well preserved specimen showing annular growth, other showing irregular growth. could be determined as buried in their ter, gently curved, both ends open, the original position, which is parallel with surface rather smooth, irregulary wrink the sea bottom on which they li ved, and led or more or less annular, all brownish on which they crawled over. In this colored, consisting of calcium carbonate, respect they may be of value in deter and none were found to be straight or mination of the inclination and top or entirely smooth throughout their length. bottom of the strata in which they occur. In general curvature the present speci The non-association of the scaphopod mens resemble Dentalium (L aevidenta like or annelid tubes with other kinds lium) C01"USCU1n PILSBRY, described and of invertebrate fossils may be due to illustrated by KURODA and KIKUCHI (1933, that the larvae of molluscs, foraminifers p. 10, pl. 1, fig. 1) from Toyama Bay, and other kinds of marine life form a Toyama Prefecture, but the curvature is part of their food chain. stronger and the shell is more strongly The tubular specimens showed random polished in coruscum compared with the orientation of their shells, but all that present fossil. The fossi l also resembles could be observed were preserved hori Dentalium ( L aevidentalium) toyamense zontall y throughout a thickness of about KUROD A and KIKUCHI (1933, p. 11, pl. 1, ten to fifteen centimeters of siltstone, figs. 5, 6) from Toyama Bay, but the shell the state of preservation was different is smaller, more strongly curved and the according to whether exposed or embed growth is more irregular than the Recent ded, none were seen lying across one an species of KURODA and KIKUCHI. other a lthough many were in close posi In general size and shape, the present tion, none so far as observed exceeded fossil resembles Dentaliwn ophiodon DALL 25 mm in length, andn one were found in (HE NDERSON, 1920, p. 84, pl. 14, fig. 2) but association with fossils of bivalves, gas differs in having stronger and less ob tropods or scaphopods or other inverte lique annulations on the shell. brates. All of the tubular structures are The Miyazaki specimen also resem short, measuring up to about 20- 25 mm bles the worm tube from Proctor Creek, in length and about 1- 1.3 mm in diame- Snohomish County, Washington, illus- 412 Kotora HATAI, Hiroshi NODA and Kenshiro OGASAHARA trated by DANNER (1955, fig. 3), but is FELS, 1955, p. E39; MAKIY AMA, 1931, p. more strongly curved and shorter in 5, figs. 1, 2). Makiyama is widely dis· length. It is also similar to Tereb1·ellina tributed in the Miocene and Pliocene shikokuensis KA TTO (1960, p. 328, pl. 34, marine deposits of Japan, and wherever, figs. 1, 3, pl. 35, fig. 7) from the Eocene it occurs, it is always found as isolated, Naharigawa Formation at Kannoura, sporadic rods with squarely rounded ter Toyo-cho, Aki-gun, Kochi Prefecture, and minals, generally more or Jess flattened also the same species (KA TTO, op. cit.) and often creased longitudinally along from the Eocene Muroto Formation at its middle part. The terminal parts of Nabae, Muroto City, Kochi Prefecture, the Makiyama short rods never taper but differs from them in the smaller size, towards one end, never consist of cal Jess curvature of the tube and more careous material, and usually do not prominent external sculptu•re of the shell. occur in clusters, although the rods are Hyalinoecia tubicola illustrated by HER usually found in a position parallel with SEY (1967, p. 239, figs. 22-23, p. 240, figs. the bedding plane of the strata in which 22-24) from Dalaware Bay in 450 m depth they occur. Under the microscope Maki (former) and from Chesapeak Bay in 365 yama is spiculate. The just mentioned m depth (latter), also resembles the pre characters serve to easily distinguish sent fossil specimens but the Recent Ditrupa miyazakiensis from Makiyama species· is longer and straighter than the chitanii. Also since the genus Dentalium fossil one. or Siphonodentalium consists of shells The genus Ditrupa BERKELEY, 1835, made of aragonite (SHROCK and TWEN figured by HOWELL (1962, p. W156, fig. HOFEL, 1953, p. 362), they will not be 97-4) is very closely similar to the pre misidentified for the shells of an annelid sent fossil, which has stronger concen tube, which consist of calcium carbonate. tric wrinkles or annulations on the sur face. The type species of Ditrupa, D. cornea (LINNE) is stated to come from References cited the Pliocene of Italy (HOWELL, op. cit.) DANNER, W.R. (1955) : Some fossil worm tubes and to contain Dentalium corneaum LINNE of western Washington. Rocks and Min and Dentalium subulatum DESHA YES as erals, pp. 451-457, 7 figs. its synonyms. The characters distin DELAUBENFELs, M. W. (1955) : Treatise on guishing the present fossil from Ditrupa invertebrate paleontology, Edited by R.C. cornea (LINNE) illustrated by HOWELL MooRE, Geol. Soc. America and Univ. (op. cit.) are considered sufficient for the Kansas Press, Part E, Archaeocyatha and proposal of a news pecies, which is here Porifera, pp. 1-122, 89 figs. named miyazakiensis, after the geogra HENDERSON, J.B. (1920) : A monograph of phic name of its occurrence. Miyazaki the East American scaphopod mollusks. ensis can be distinguished from the dif U.S. Nat. Mus., Bull., no. 111, pp. 1-177, pis. 1-20. ferent kinds of fossils mentioned above HERSEY, }.B. (1967) : Deep sea photography. which show resemblance with it by the johns Hopkins Press, 310 pp. features already mentioned. There seems HowELL, B.F. (1962) : Treatise on inverte to be little chance for the present fossils brate paleontology, Edited by R.C. MooRE, being mistaken from detached parts of Geol. Soc. America and Univ. Kansas Press, the sponge known as Makiyama chitanii Part W, Worms, pp. 144-177, figs. 85-108. (MAKIYAMA) (=Sagarites) (DELAUBEN- KATTO, J. (1960) : Some Problematica from 603. Scaphopod-like fossils 413 the so-called unknown Mesozoic strata of Colt. Sci., Kyoto Imp. Univ., Ser. B, vol. the southern part of Shikoku, Japan. Sci. 1, art. 1, pp. 1-53, pis. 1-3, figs. 1-4. Repts., Tohoku Univ., 2nd Ser., Geol., SHROCK, R.R. and TwENHOFEL, W.H. (1953) : Spec. Vol., no. 4, pp. 323-334, pis. 34-35. Principles of invertebrate paleontology. KuRODA, T. and KIKUCHI, K. (1933) : Studies MacGraw-Hill Book. Co. Inc., New York, on the molluscan fauna of Toyama Bay Toronto, London, pp. 1-816. (1). Venus (Japan. jour. Malac.), vol. 4, SHUTO, T. (1961) : Palaeontological study of no. 1, pp. 1-14, pl. 1. (in Japanese with the Miyazaki Group-A general account English Resume). of the faunas-. Mem. Fac. Sci., Kyushu MAKIYAMA, J. (1931) : Stratigraphy of the Univ., Ser. D, Geol., vol. 10, no. 2, pp. Kakegawa Pliocene in Totomi. Mem., 73-206, figs. 1-23, tabs. 1-5, pis. 11-13. Aki-gun Muroto p * 1;; nil :4?: Aoshima -l'l IIh Nabae ;w~ 1:. Boroishi )l)( :fi Nagayama 7k iJJ Kannoura Ffl iill Naharigawa *~ifljJII Kagamisu-toge ~ iJ« lhii Toyo-cho Jti:illliT Kiyotake iflt J1t Udo ~ [=i Kogochi ,J, iiiJ r"J Tr_ans. Proc. Palaeont. Soc. Japan, N.S., No. 87, pp. 414-428, pis. 50, 51, September 30, 1972 604. PERMO-CARBONIFEROUS ENDOTHYRACEANS FROM JAPAN* PART 1. BISERIAMMINIDAE YU JI OKIMURA Institute of Geology and Mineralogy, Hiroshima University :;1s:#'i)r1R Endothyraceans O)jiJB'E : Endothyracean foraminifera Vi l.l HiP G ts. IJ, tlj:,f-tf&!\IJO) m'}l:.fs_7];iflft1"1 c ~ ~v-c "' .Q ;?;, I;' ':l: t.:l::: :;js:;!'J;::::.:t;:t .Q.f:O)J'5~~l'i1f c;;, ['Joll ?;Jl,"t'i;'fS.v'o Jf,;:'}.[);?>GO) biseriamminids O)f,[{f!ffir'i tl/)"t'"(:·(li;,IJ, i:O)f4-0)~;icil&!ID:a: lf:Hli L- "t' itTl!fiFP¥:s'{'®~R :a:-41H*1F.;!, Lt.:o =E c L- "t' rN~JJ:t!r1;0)::l::W:EEk:EJii'i (lliiJ~·. ·,'i'i~R • 'f:k i'O iP G, ~lobivalvulina 1:::/,'il-t .Q (ftl!.O) 21m Biseriammina, Olympina f;J:*§£ 5',!) 7f!ll; G. kamenszs, G. granulosa compressa, G. mosquensis, G. sp. cf. G. kantharensis, G. sp. cf. G. gracea, G. regularis n. sp., G. sp. A, G. sp. B l2~~llix L- "(', ;tjs:;/'[)O)J_:. Ttff> E~*O)!JE:3'\'-, ;: c f:::_i:.~II:W!R*Tl~llf:::.:t;lt 0 itE~Ji"·"NI''Jts.Mf.RHR G;?,f;:: L- t.:o ':l: t.:, r~lfl±'ri\"i tjfL;fo' J: Lf1:11Jd':-O)~~i1'1: U'U.l\~JU.Jtf;:: "?I;'"(' 1(, li}f)'E Lt.:o jrp .H ift = the Biseriamminidae from Japan treat Introduction ing mainly the Carboniferous specimens It is well known that some of the from the thick limestones of Taishaku endothyracean foraminifera have been Akiyoshi, Atetsu and Koyama of th~ accepted valuable index fossil in the late Chugoku Region, the Kakisako forma Paleozoic. According to Treatise on tion of the Kuma Massif, Kyushu Region, Invertebrate Paleontology (Edit. MOORE, and the Nagaiwa formation of the Kita 1964, pp. 329-358), the superfamily Endo kami Massif, Tohoku Region. The Per thyracea is organized by eleven families; mian specimens are also examined from Nodosinellidae, Colaniellidae, Ptychocla the Taishaku and Atetsu limestones in diidae, Palaeotextulariidae, Semitestula order to compare with Carboniferous riidae, Tetrataxidae, Biseriamminidae, ones morphologically and to make clear Tournayellidae, Endothyridae, Archae the stratigraphic distribution. discidae and Lasiodiscidae. Among them, All the specimens from the above lime the biostratigraphical significance of stones belong to Globivalvulina, a genus Endothyridae and Palaeotextulariidae of the Biseriamminidae. As is shown by has been passably established on the RAUSER-CHERNOUSSOVA and REITLINGER basis of their paleontological study. (1957), Globivalvulina appears in the upper However, the study of the other families Lower Carboniferous and becomes extinct may be said to be insufficient, especially in the Upper Permian, thriving extremely in the lower Upper Carboniferous. Ac in Japan. This report is the first description of cordingly the frequency of globivalvu linid foraminifera may offer some im * Received Jan. 24, 1972; read Jan. 23, 1972 portant data to the boundary problem at Chiba. between the Lower and Upper Carboni- 414 604. Permo-Carboniferous endothyraceans 415 ferous of Japan. spiral shell and two-layered wall. Ac Acknowledgements:-The writer wishes cording to Osnovy Paleontologii (Edit. to express his sincere thanks to Profes RAUSER-CHERNOUSSOV A and FURSENKO, sor Akira HASE of Hiroshima University 1959) Globivalvulina is again attached to who constructively advised him and the Biseriamminidae. kindly revised the manuscript. Thanks Such confusion on the taxonomy of are due to the research members of Globivalvulina is chiefly caused by some stratigraphy and paleontology of the difference of worker's subjective ·view same university for their helpful dis· with regard to the coiling form and wall cussions. Financial aids for this study structure; that is to say, it is a question were partly granted by the Ministry of whether the test is planispiral or trocho Education. spiral, and whether the wall is aggluti Repository:-All the specimens de nate or undifferentiated microgranular scribed and figured in this paper are or layered. In this paper the writer kept in the Institute of Geology and follows the classification of Treatise on Mineralogy, Hiroshima University, Japan. Invertebrate Paleontology. According to Their register numbers are indicated it, the diagnosis of Biseriamminidae within the brackets in the explanation (synonymous with Globivalvulinae REIT of plates. LINGER, 1950; and Globivalvulininae PoKORNY, 1958) is as follows: Test en rolled planispirally to slightly trocho Paleontological and biostratigraphical spirally, chambers biserially arranged, notes on the family Biseriamminidae involute, aperture opens. at inner border and the genus Globivalvulina of septal face. The family Biseriamminidae consists The family Biseriamminidae was first of three genera; Biseriammina from the proposed by CHERNYSHEVA (1941) with middle Tournaisian of South Ural (CHER the type-genus Globivalvulina, but his NYSHEVA, 1941), Olympina from the Per classification is not always followed after mian of Cyprus (REICHEL, 1945) and the that. For instance, PLUMMER (1948) stud type-genus Globivalvulina. The first and ied in detail the morphology of Globi the second are monotypic, and there is valvulina, and said that it would be nothing to be mentioned on their bio placed in the family Cassiduliniidae by stratigraphical significance. the nature of a biserial arrangement of SCHUBERT (1921) proposed Globivalvu chambers in a planispiral coiling, even lina for the " Globigerina-like" Paleozoic though the aperture of this Paleozoic foraminifera, designating briefly V alvu form is not harmonious with those of lina bulloides BRADY as the type-species, the rest of the family. CusHMAN and but he did not defined it in detail. Ac ]ONES (1950) followed BRADY's classifi cording to the emended definition of cation (1876) which placed this genus in Treatise on Invertebrate Paleontology, the the Trochamminidae characterized with basic characters of the genus are sum a trochospiral coiling. REITLINGER (1950) marized as follows: Subglobular to hemi newly established the subfamily Globi spherical test, planispirally to slightly valvulinae, and included it in the family trochospirally coiled ; biserially arranged Tetrataxidae by the characteristics of chambers; microgranular calcareous wall biserial chamber arrangement, trocho- with some inner fibrous layers ; aperture 416 Yuji OKIMURA Table 1. Stratigraphic distribution of the species of Globivalvulina previously described. Up. Carbon. Low Perm. Car b. I low. mid. up. I I : G. biserialis CusH. & WATERS X G. bristolensis REITLINGER X G. bulloides (BRADY) x? X X X x? ! *G. cora HARLTON X I G. cyprica REICHEL : X : G. donbassica POTIEVSKAYA I X i G. eogranulosa REITLINGER X X *G. gaptankensis HARL TON X I : G. gracea REICHEL X G. granulosa REITLINGER : X : G. granulosa complicata REIT. X G. granulosa compressa REIT. X I G. granulosa multiseptata REIT. X G. kamensis REITLINGER X G. kantharensis REICHEL X G. minima REITLINGER X ; G. moderata REITLINGER X X G. mosquensis REITLINGER : X *•G. ovaia CusHMAN & WATERS X G. parva CHERNYSHEVA X I ; G. pulchra REITLINGER X G. rauserae REITLINGER X G. scaphoides MoRozovA X X +G. shikhanensis MoRozovA X +G. spiralis MoROZOVA X G. syzranica REITLINGER X I G. vonderschmitti REICHEL X I +G. vulgaris MOROZOV A X x? I * Described only by the external characters of free specimens; + described by line drawing without microphotograph; • identified with G. biserialis by thin section study. interiomarginal, opens into vestibule near from the upper Lower Carboniferous, middle of apertural face. twenty-one from the Upper Carbonifer Twenty-eight species of Globivalvulina ous and five from the Permian (see Table have been previously described ; two 1). Generally the species from the Lower 604. Permo-Carboniferous endothyraceans 417 A B c D E Text-fig. 1. Various sections of Globivalvulina (partly figured after REICHEL, 1964). A, sagittal section; B, nearly sagittal section; C, apertural section ; D, parallel section; E, external view. Lines under capital letters A, B, C and D correspond sectional lines shown in E. Carboniferous are small in size (0.25 mm section carrying the helicoid axis of more or less in maximum length of biseriality (in other words perpendicular sagittal section) and subspherical in to the coiling axis) and passing through shape, while the Permian species are the proloc!J.lus best reveals internal fea characterized with larger size (more than tures of the shell, as is known from the 0.6 mm) and rapidly expanding chambers morphological study of REICHEL (1946, in adult stage. The Upper Carbonifer text-figure 36) and PLUMMER (1948). The ous species are commonly 0.3 mm to 0.6 present writer makes use of the term mm in size and intermediate in shell of sagittal section to this orientation. shape between the Lower Carboniferous The apertural section, which is sliced and Permian types. with the face of lobata opening, is in The re-examination is required with dispensable for the purpose of observing three species which have been only stud the feature of aperture, for it can not ied by the external appearance without be seen in sagittal section. Such others taking notice of the inner microstruc as axial, parallel and nearly saggital ture by thin section. St. ]EAN (1957, p. sections are also necessary to investigate 36) regards both species of Globivalvu in. detail the characteristics of test (Text lina biserialis and G. ovata as the same fig. 1). one from the common characteristics of the inner structure. Three species which Systematic description were defined with the vague figures by line drawing are also insufficient in order Family Biseriamminidae to compare exactly with other species. CHERNYSHEV A, 1941 With regard to the orientation of thin section in this genus, the terms of trans Genus Globivalvulina SCHUBERT, 1921 verse and longitudinal sections have Type-species:-Valvulina bulloides BRADY, hitherto been mainly used, but there is 1876, Palaeont. Soc., London, Monograph, vol. such disorder that REITLINGER's trans 30, p. 89, pl. 4, figs. 12-15. verse section (1950) is the same as St. ]EAN's longitudinal one (1957). In any It was reported from the upper Penn case, it admits of no doubt that the sylvanian of Iowa, U.S.A., but according 418 Yuji OKIMURA to PLUMMER (1948, p. 169), the exact geo graphic position of the type-locality for Globivalvulina kamensis REITLINGER the species is questionable. Pl. 50, figs. 1-8 Diagnosis:-Test small, sub globular to hemispherical, planispirally to slightly 1950. Globivalvulina kamensis REITLINGER, trochospirally coiled, comprises a biserial Akad. Nauk. USSR, Inst. Geol. Nauk, succession of chambers arranged along Trudy, Moscow, fasc. 126 (Ceo!. Ser. no. 47), p. 78, pl. 16, figs. 5-6. an axis of biseriality that draws an open 1962. G. kamensis: BocusH and }uFEREV, helicoid curve. Apertural face (ventral Akad. Nauk, USSR, Dep. Siberian Inst. side) more or less concave. Wall cal Ceo!. Geogr., p. 197, pl. 8, fig. 14. careous, microgranular, may have an inner fibrous or porous layer particularly Types :-So far as the type-specimens well developed along septa. Aperture photomicrographed by REITLINGER are single, lobate, and opens into near the concerned, they are not good enough to center of a little flattened part of some describe the species definitely, because what concave apertural face, with a the one is a nearly apertural section valvular projection. (fig. 5) and the other (holotype) a nearly Remarks:-This genus is clearly dis sagittal, slightly oblique section (fig. 6). tinguished from the others of Endothy They were obtained from the Kashira racea by a lobate aperture and chambers formation (lower Moscovian), southern biserially arranged along the helicoid part of the region around the Timan axis of biseriality. In parallel section, Upland, Komi, U.S.S.R. the chamber arrangement closely resem Material.·-Five sections almost per bles that of palaeotextulariids seen in pendicular to the coiling axis, three 0/co/co section, but the shell of Globi parallel to the plane of ventral side of valuulina is not tapering, being obtuse test, and seven others were examined. triangular in shape. The apertural char The majority came from the Millerella acter can be defined in detail only by sp. ArvPseudostaffella antiqua zones of the external observation of isolated spe the Akiyoshi and Taishaku limestone cimens, though examined partly in aper groups. tural section. Description:-Test moderate in size, Geological age:-The upper Lower Car hemi-ellipsoid, slightly trochospiral with boniferous to the upper Permian; mainly a very weakly curved helicoid axis of the lower Upper Carboniferous. Occur biseriality, consisting usually of one to rences of the upper Lower Carbonifer one and a half volutions with biserial ous and Permian species are geographi chambers. Chambers six to seven in cally restricted. That is to say, only number in each row, fairly overlapped; two Visean species have been recorded the last two rapidly expanding, occupy from the central part of Bashkiria, ing about two-thirds of the total outer U.S.S.R., and Permian ones, except G. whorl, and especially the last chamber donbassica from Donbass region, from highly inflated ; inner half of the whorl Chatzimanoli, Ile de Chio, Greece and consists. of small chambers tightly coil Cyprus. All the other species occur ed. The last chamber has a valvular from the Pennsylvanian of the U.S.A. projection on the floor, which takes and European Russia. about a half of the chamber height and generally parallels the " antetheca of 604. Permo-Carboniferous endothyraceans 419 Fusulinacea". Wall relatively thin, cal of the Moscow Basin, U.S.S.R. The careous and microgranular, partially holotype (fig. 1) is described as trans with inner fibrous layer. Aperture lo verse section, but it may be a slightly bate, opening at the central part of oblique, nearly sagittal section, and the somewhat flattened apertural face; its paratype (fig. 2) is a parallel one. There true character is indistinct, though ob fore, the apertural feature and the val served as dark part in Pl. 50, fig. 8 vular projection are unable to be seen (nearly a pert ural section). in detail in these figures. Dimensions:-The longest diameter Material:-The writer obtained four 0.34 mm in the figured sagittal section teen specimens in all, but there is no (Pl. 50, fig. 1), and the maximum width precisely sagittal section. Three nearly 0.25 mm in the figured parallel section sagittal sections slightly oblique to the with apertural face (Pl. 50, fig. 7). coiling axis, two sections parallel to the Remarks:-The last chamber of this apertural face, and nine other were ex specieJ is more inflated than in any amined. The occurrence is limited to other species of Globivalvulina. It also the Profusulinella"" Fusulinella zones of differs from others except for G. gracea the Akiyoshi and Atetsu limestones and REICHEL in its long valvular projection. the Nagaiwa formation (Profusulinella This projection is apparently short in zone) of the Kitakami Massif. the photomicrograph of the holotype, Description:-Test moderate in size, for it is a slightly oblique section. G. subglobular, slightly trochospiral, and liamensis closely resembles G. granulosa slightly compressed laterally; apertural REITLINGER including its three subspe face very weakly concave. Number of cies, but the former is distinguished whorls not more than one and a half. from the latter in its plane or very Chambers increasing gradually in size, slightly arcuate apertural face. especially slowly in juvenile stage, hi Horizon:-The present species was seriality that describes an open helicoid obtained from the Millerella sp. A"" curve, but the last chamber swerves Pseudostatfella antiqua zones of the Aki from the axis; seven chambers in each yoshi limestone, the Millerella sp. A row interlocked very shallowly. The zone of the Taishaku and the Koyama valvular projection may be present on limestone, and the upper part of the the floor of the last chamber, as shown Kakisako formation (Millerella zone) of in Pl. 50, fig. 10 (slightly oblique, nearly the Kuma Massif. sagittal section); the identical hook shaped projection is also recognized on floors of the last three chambers in the Globivalvulina mosquensis REITLINGER figure of the holotype. Wall relatively Pl. 50, figs. 9-12 thin, microgranular, calcareous, with in ner fibrous layer partially. Aperture 1950. Globivalvulina mosquensis REITLII\GER, probably lobate, opening on some what Akad. Nauk, USSR, Inst. Geol. Nauk, concave apertural face; but its precise Trudy, Moscow, fasc. 126 (Geol. Ser. no. 47), p. 79, pl. 16, figs. 1-4. character obscure because of a lack of apertural section. Types :-This species was first found Dimension:-The longest diameter 0.38 from the middle Upper Carboniferous mm in the nearly sagittal section (Pl. Podolsk formation in the eastern part 50, fig. 10), and the maximum width 0.35 420 Yuji OKIMURA mm in the parallel section with aper yoshi limestone and the Millerella""Pro tural face (Pl. 50, fig. 12). fusulinella zones of the Taishaku lime Remarks :-Such characters as low stone. There is no section precisely spire and inner fibrous layer described perpendicular to the coiling axis and on the type-specimens are not always passing through the proloculus. special ones of this species. The pre Description:-Test moderate in size, sent species resembles more closely G. hemispherical, fairly concave in aper bulloides (BRADY) than any other spe tural face, composed of one to one and cies,· but differs in its small size and a quarter whorls with six or seven regularly expanding chambers through chambers biserially arranged. almost the growth stage. It is also distin planispiral, but its helicoid axis weakly guished from G. lwmensis REITLINGER curved in later stage. Chambers deeply in its more deeply concave apertural overlapped, rapidly expanding except face. those in juvenile stage which are tight Horizon:-Although this species was ly coiled ; the last chamber relatively originally recorded from the upper Mos inflated, slightly swerving from the heli covian, it may range down to the lower coid axis of biseriality. Valvular pro Moscovian or Bashkirian by reason of jection indistinct owing to a lack of occurring from the Profusulinella bep sagittal section, but a small hook-shaped pensis zone of the Akiyoshi limestone projection may be present on the floor and its equivalents. of the last chamber. Wall thin, micro granular, calcareous, inner fibrous layer Globivalvulina granulosa compressa poorly developed. Aperture lobate, fair ly large, opening at the central part of REITLINGER concave apertural face; there are five PI. 51, figs. 1-6 lobations, among which one is acute and the rest are obtuse. 1950. Clobivalvulina granulosa REITLII\GER Dimension:-The longest diameter 0.39 var. compressa REITLINGER, Akad. mm and the maximum width 0.26 mm Nauk, USSR, Inst. Ceo!. Nauk, Trudy, in the nearly sagittal section (Pl. 51, fig. Moscow, fasc. 126 (Ceo!. Ser. no. 47), 2). The length along the axis of biseri p. 81, pl. 16, figs. 10-ll. ality 0.34 mm and the maximum width Types:-The holotype specimen (fig. 0.32 mm in the apertural section (Pl. 51, 10) is not a transverse section but a fig. 5). nearly sagittal one, and also the para Remarks:-The present species is allied type specimen (fig. 11) is a nearly aper to G. mosquensis REITLINGER in respect tural section (not a longitudinal one). that the last chamber swerves from the They were described from the lowermost helicoid axis of biseriality, but the form Moscovian V ereia formation, southern er is clearly distinguished from the latter part of the region around the Timan by its strongly concave apertural face. Upland, Komi, U.S.S.R. This species closely resembles G. bulloi Material.·-Nine specimens were ex des (BRADY), but it differs in its aper amined. They consists of four nearly tural feature with five lobations and sagittal, a just apertural and four other curved helicoid axis of biseriality. sections from the Millerella sp. A"' Horizon:-Although the type-species Pseudostaffella antiqua zone of the Aki- of this species were originally described 604. Permo-Carboniferous endothyraceans 421 from the lowermost Moscovian, its range acters the material here dealt with is should be set down to the Bashkirian comparable with C. kantharensis REICHEL, owing to the occurrence from the Mil though the writer avoids the exact iden lerella zone. tification owing to insufficiency of the material. The species is closely allied to C. bulloides (BRADY) and G. granulosa Globivalvulina sp. cf. G. kantharensis compressa REITLINGER, but it can be REICHEL distinguished in its strongly depressed Pl. 50, figs. 13-14 ventral side and gradually expanded chambers. Compare: Horizon:-In Cyprus G. kantharensis 1946. Clobivalvulina kantharensis REICHEL, Eclogae Ceo!. Helv., Lausanne, vol. 38, was accompanied by Pseudoschwagerina no. 2, pp. 554-555, text.figs. 40a-d. sp., and in Taishaku, too, occurred only from the lower Pseudoschwagerina zone. Types :-G. kantharensis was described Very recently, Mr. TAKEDA, who is from the lower Permian of Cyprus. The engaging in studying the geology of the holotype (text-fig. 40b) is a sagittal sec southwestern Atetsu limestone plateau, tiion and the paratype? (text-fig. 40c) is found three specimens belonging to this a section nearly parallel to the coiling species from the Pseudoschwagerina zone. axis and apertural face. Other two spe Therefore, the species may be effective cimens are oblique. Therefore, the aper as a horizon marker. tural feature is unknown even through out all figured specimens. Material:-Two nearly sagittal sec Globivalvulina sp. cf. G. gracea tions from the lower part of the Pseudo REICHEL schwagerina zone of the Taishaku lime stone. Pl. 51, figs. 7-10 Description:-Test small, sub globular, Compare comprising a compact biserial succession 1946. Clobivalvulina gracea REICHEL, Eclogae of gradually enlarging chambers, almost Ceo/. Helv., Lausanne, vol. 38, no. 2, p. 550, pl. 19, figs. 15-17, text-figs. 36A-F planispirally coiled with an axis of hi and 38a-f. seriality that describes an open helicoid 1970. Clobivalvulina gracea: KociiANSKY-DE curve. Apertural side strongly concaved. VIDE, Ceo!. Razpr. Por., vol. 38, p. 185, Valvular projection is present on the pl. 9, fig. 6, pl. 18, figs. 1-2. floor of the last chamber, fairly long, hook-shaped; Its length attains to half Types :-REICHEL established G. gracea of the chamber height. In sagittal sec from the Permian of Chio Island, Greece. tion, a single aperture is recognized as The holotype photomicrographed with a low slit-like opening. Wall thin, mi pl. 19, fig. 15 is a nearly sagittal section. crogranular, calcareous; inner fibrous The test-figs. 36A-F given as "cotype" layer very poorly developed. (paratype ?) are the most important Dimension:-The maximum length 0.32 figures requisite for thin section study mm and the maximum width 0.23 mm of the genus Globivalvulina. in the nearly sagittal section figured Material:-Three nearly sagittal, a with Pl. 50, fig. 13. parallel and two oblique specimens were Comparison :-In many important char- examined from the Fusulinella and Para- 422 Yu}i OKIMURA fusulina zones of the Taishaku limestone. Description:-Test relatively large, Globivalvulina regularis sp. nov. subglobular, weakly depressed on aper Pl. 50, figs. 15-19 tural side, consisting of one and a half whorls with eight chambers biserially iVIaterial :-A sagittal section (holotype, arranged through the growth stage. YONG6-15), a nearly apertural section Chambers gradually enlarging, but the (paratype, YONG6-14), two parallel sec last and penultimate ones fairly inflated. tions with apertural face, two nearly A valvular projection is present on the sagittal sections and others were exam floor of the last chamber, long, tapering, ined. The majority came from the Na and parallels the "antetheca of Fusuli- · gaiwa formation of the Kitakami Massif. nacea ". Wall relatively thick, composed Description:-Test relatively large, of outer microgranular and inner fibrous subglobular, planispiral, weakly depres layers. In sagittal section the aperture sed on both lateral sides of the boundary is recognized as a slit-like opening. between the juvenile and the adult, con Dimension:-The maximum length 0.59 sisting of one volution with seven cham mm and the maximum width 0.39 mm bers of adult stage fairly inflated as in the sagittal section (Pl. 51, fig. 9). The compared with four small, gradually en length along the axis of biserity 0.52 mm larging and tightly coiled chambers of and the maximum width 0.39 mm in the the juvenile. On each floor of the adult parallel section (Pl. 51, fig. 10). chambers there is a hook-shaped projec Comparison :-Almost all characters tion, while the axial part of early stage stated above are comparable with those filled with calcareous microgranular sec of G. gracea, though the apertural nature ondary deposits. Wall composed of outer is indistinct because of lack of apertural thick microgranular and inner thin de section. This species and G. kantharensis fective fibrous layers. Aperture lobate, REICHEL are closely alike in their sub with five shallow lobations, opening on globular shell, but the former is distin the concave apertural side. guished from the latter in its larger Dimension:-The maximum length 0.48 size and more depressed ventral side. mm and the maximum width 0.38 mm The species is also distinguished from in the holotype (sagittal section) figured G. mosquensis REITLINGER by that the with Pl. 50, fig. 19. The maximum length last chamber of the latter swerves out 0.42 mm and the maximum width 0.41 of the axis of biseriality. mm in the paratype (apertural section) Horizon :-According to the original figured with Pl. 51, fig. 18. description of G. gracea from Chio Island, Remarks:-This new species can be the species coexists with such Permian distinguished from other species of Globi foraminifers as Agathammina pusilla valvulina in its depression on both lat (GEINITZ), Hemigordius aff. schlunbergi eral sides of test that is caused by (SCHUBERT) and Geinitzina postcarbonica abrupt expanding of chambers in adult SPANDEL, but there is no evidence on stage. the precise age. The specimens dealt Horizon:-Almost all specimens were with in this paper occurred from the obtained from the Ng-6 horizon (ONUKI, Moscovian and Middle Permian parts of 1955) of the Nagaiwa formation (Profu the Taishaku limestone. sulinella zone), Kitakami Massif. A few came from the Millerella sp. A zone of 604. Permo-Carboniferous endothyraceans 423 the Akiyoshi limestone and from the Hor·izon :-The occurrence of the pre same zone of the Kobatake limestone, sent species is limited to the Millerella Jinseki-gun, to the south of Taishaku sp. A zone of the Akiyoshi limestone. district, Hiroshima Prefecture. Some specimens comparable with this species were found from the same zone of the Taishaku limestone. Globivalvulina sp. A Pl. 50, figs. 20-22 Globivalvulina sp. B Material :-Six specimens were exam Pl. 51, figs. 11-13 ined; a nearly sagittal, a parallel, a nearly apertural and other sections from Material:-Two nearly sagittal and the lower Upper Carboniferous part of other oblique sections were examined the Akiyoshi and Taishaku limestones. from the Upper Permian of Taishaku. Description:-Test moderate in size, Descriptive remarks:-Test large, hemi subglobular, very slightly trochospiral. ellipsoid, planispiral, composed of one Number of whorls not over one and a and a half whorls with nine or ten half. Commonly seven chambers biseri chambers biserially arranged along the ally arranged ; chambers of an inner helicoid axis of biseriality. The helicoid half whorl small and tightly coiled, while axis becomes very loosely coiled or un those of later stage increase in size coiled in later stage, and this is the rapidly but not uniformly, and the last most important character of the .species. chamber fairly swerves from the heli Chambers deeply overlapped as those of coid axis of biseriality. Secondary de palaeotextulariids. The characters of posits remarkably developed on floors valvular projection and aperture are in of the chambers. Wall relatively thin, distinct because of an absence of avail consisting of outer microgranular and ably oriented section. Owing to the in inner fibrous layers. Aperture lobate, sufficiency of the material, the definite with two or more acuate lobations, open designation is postponed. ing at the central part of apertural face. Dimension:-The maximum length 0.57 Dimensions:-The maximum length mm and the maximum width 0.33 mm 0.27 mm and the maximum width 0.21 in the sagittal section figured with Pl. mm in the sagittal section (Pl. 50, fig. 51, fig. 11. 22). The length along the axis of hi Horizon:-All the specimens referable seriality 0.31 mm and the maximum to this species were obtained only from width 0.33 mm in the nearly apertural the locality TKSH-1, Yabeina zone of section (PI. 50, fig. 21). the Taishaku limestone. Remarks:-This species is remarkably characterized with secondary deposits, inflated chambers of the adult stage, and Notes on the occurrence a considerable swerve of the last cham of Globivalvulina ber. Accordingly, it may be a new spe cies, but the writer hesitates to conclude In this chapter, the biostratigraphical so, because there is no sagittal section significance of Globivalvulina is noted, enough to designate as the type-speci and the frequency of it is related with men. the petrographical character of lime- 424 stone. The writer (1966) has already than fusulinaceans in frequency. Espe divided the Carboniferous limestones of cially speaking, the occurrence of three the Chugoku Region into the following species of G. kamensis REITLINGER, G. zones in descending order. granulosa compressa REITLINGER and G. sp. A is limited to this zone. Moreover, Fusulinella imamurai-F. biconica zone the writer did not find any species of Profusulinella toriyamai-P. beppensis zone Globivalvulina from the underlying zones. Pseudostaffella antiqua zone Eostaffella sp. A-Millerella sp. A zone Such being the case, it may be con --- Disconformity -- cluded that Globivalvulina is an impor Mediocris sp. A-M. mediocris zone tant faunal element of the Eostaffella Endostaffella delicata zone sp. A-Millerella sp. A zone of the Chu Endothyra sp. A zone goku Region, and that the frequency of it offers an available datum to the prob The upper four zones are characteri lem concerning the boundary between zed with primitive fusulinaceans, while the Lower and Upper Carboniferous in the lower three with smaller foramini Japan. RAUSER-CHERNOUSSOVA and REIT fers. The writer (1963, 1966) also em LINGER (1957, p. 113) has already stated phasized that Globivalvulina is one of that the age of prosperity of the genus the characteristic genera in the Millerella is in the lower Upper Carboniferous. zone. Table 3 shows the distribution of Globi Table 2 shows the biostratigraphic dis valvulina with regard to the lithologic tribution of Globivaluulina in the Tai types of limestone. As understood from shaku, Atetsu and Akiyoshi limestones. this table, globivalvulinid foraminifera Among 239 specimens in 64 thin sections occur more abundantly from micritic (a section 30 X 20 mm in area) examined, limestones, especially such limestones as 151 one (about 67.3%) were obtained from foraminiferal or crinoidal biomicrite, than the Eostaffella sp. A-Millerella sp. A zone, from sparitic ones. Such occurrence may where the genus is occassionally greater be related to the paleoecology of the Table 2. Frequency of Globivalvulina with relation to the divisions of the Permo-Carboniferous limestones in Chugoku Region. Numerals fn and out of brackets indicate the number of thin sections containing Globivalvulina and that of specimens of the genus respectively. Taishaku Atetsu Akiyoshi Total l.s. l.s. l.s. Y abe ina zone 20 (2) 34 (9) Pseudoschwagerina zone 19 (3) ~: ~~~ .1 ...... not exam ... . 1... 32 (5) Fusulinella zone 4 (3) 0 2 (1) 6 (4) Profusulinella zone 1 (1) 7 (2) 1 (1) 9 (4) Pseudostaffella antiqua zone 0 3 (1) 4 (1) 7 (2) Eostaffella sp. A- 67 (13) 151 (40) Millerella sp. A zone 41 (18) 43 (9) Total 85 (27) 80 (21) 74 (16) 239 (64) - I • '' ~ ;·. • 604. Permo-Carboniferous endothyraceans 425 Table 3. Frequency of Globivalvulina with relation to the petrographical divisions of limestones. Numerals show the number of thin sections containing Globivalvulina. In each box the number of the Carboniferous sections is set below and that of the Permian ones above. Taishaku Atetsu Akiyoshi Total l.s. l.s. I l.s. I Sparite 4 5 2 15 1 3 _J I Sparudite 0 0 1 6 0 5 I I Micrite 1 4 2 24 17 0 I I Micrudite 0 0 10 15 1 4 I I Biolithite 0 0 1 4 3 0 I I Total 5 9 16 64 22 12 I I genus. However, it is difficult to make References clear the pa:leoecological environment, because what factors influence the frequ BocusH, O.I. and JuFEREV, O.V. (1962) : Fo ency of Paleozoic smaller foraminifera raminifers and stratigraphy of the Car is not well known. boniferous deposits in Karatau and Talas In this respect, the study of CRONEIS skii Alatau. Alzad. Nauk, USSR, Rept. and TOOMEY (1965) is worth appending, Siberian Inst.G eo!. Geograph., p. 1-234, which reported the composition of the pis. 9 (in Russian). BRADY, H.B. (1876) : A monograph of Car foraminiferal population on four thin boniferous and Permian Foraminifera (the sections (a section 30x30 mm. in area) genus Fusulina excepted). Pal. Soc. Lon from the Gunsight limestones (Virgilian). don, Monograph, no. 30, p. 1-166, pis. 12. According to it, 200 specimens of globi CIIERNYSI-IEVA, N.E. (1941) : A new genus of valvulinids on an average are counted Foraminifera from the Tournaisian de from the foraminiferal-brachiopoda! bio posits of the Urals. Akad. Nauk, USSR, micrudite (coral horizon) accompanied Doklady, val. 32, no. 1, p. 69-70. with a few sessile foraminifera, while -- (1948) : Some new species of. Foramini only 3 specimens from the algal-forami fera from the Visean of the Makarov dis niferal biomicrudite in which the remains trict (South Urals). Akad. Nauk, USSR, !nsf. Geol. Nauk, Trudy, no. 62 (Geol. Ser. of calcareous algae and sessile forami no. 19), p. 246-250, pl. 1 (in Russian). nifera are the dominant faunal elements. CRONEis, C. and TooMEY, D.F. (1965) : Gun It was supposed by them that the de sight (Virgilian) Wewokellid sponges and positional environment of the former their depositional environment~ ]o.ur. Pal was under normal marine, clear, shallow eont., vol. 39, no. 1, p. 1-16, pis. 7. water, and that of the latter under very CUSHMAN, J.A. and WATERS, J.A. (1928) : Ad shallow, marine, quiet water. ditional Cisco Foraminifera from Texas. 426 Yuji OKIMURA Contrib. Cushman Lab. Foram. Research, Oklahoma. Oklahoma Geol. Survey, Circ., vol. 4, no. 3, p. 1-16, pis. 8. no. 21, p. 1-27, pis. 5. -- and -- (1930) : Foraminifera of the. HARL TON, B.H. (1928) : Pennsylvanian Fo Cisco group of Texas. Univ. Texas Bull., raminifera of Oklahoma and Texas. jour. no. 3016, p. 22-81, pis. 11.. Paleont., vol. 1, p. 305-310, pis. 2. GALLOWAY, J.J. and RYNIKER, C. (1930): Fo KocHANSKY-DEVIDE, V. (1970) : Permski Mi raminifera from the Atoka Formation of krofosili Zahodnih Karavank. Geol. Razpr. Explanation of Plate 50 (All figures x 100) Globivalvulina kamensis REITLINGER Figs. 1 and 3. Nearly sagittal section (1, YOTM40; 3, YOTM109) from the Mediocris mediocris zone of the Taishaku limestone. Fig. 2. Tangential section (YOAD17) from the upper part of the Millerella sp. A zone of the Akiyoshi limestone. Fig. 4. Nearly sagittal section (YOAD13-2) from the upper part of the Millerella sp. A zone of the Akiyoshi limestone. Fig. 5. Nearly sagittal section (YOA3-l) from the lower part of the Millerella sp. A zcne of the Akiyoshi limestone. Fig. 6. Nearly sagittal section (YOAD26-2) from the Pseudostaffella antiqua zone of the Akiyoshi limestone. Fig. 7. Parallel section (YOAD24-1) from the upper part of the Millerella sp. A zone of the Akiyoshi limestone. Fig. 8. Nearly apertural section (YOTM109-2) from the Mediocris mediocris zone of the Taishaku limestone. Globivalvulina mosquensis REITLINGER Figs. 9-11. Nearly sagittal sections (9, YOADll-1; 10, YOAD24-2; 11, YOAD24-3) from the upper part of the Millerella sp. A zone of the Akiyoshi limestone. Fig. 12. Parallel section (YOAKJ2-1) from the lower part of the Millerella sp. A zone of the Akiyoshi limestone. Globivalvulina sp. cf. G. kantharensis REICHEL Figs. 13 and 14. Nearly sagittal section (13, YOTUYM18-1; 14, YOTUYM18-2) from the Pseudoschwagerina zone of the Taishaku limestone. Globivalvulina regularis sp. nov. All specimens from the Nagaiwa formation (Projusulinella zone) of the Kitakami Massif. Figs. 15 and 16. Nearly sagittal sections (15, YONG6-ll; 16, YONG6-12). Fig. 17. Parallel section (YONG6-13). Fig. 18. Neaaly apertural section (YONG6-14), Para type. Fig. 19. Sagittal section (YONG6-15), Holotype. Globivalvulina sp. A Fig. 20. Parallel section (YOAD28-2) from the Profusulinella beppensis zone of the Aki yoshi limestone. Fig. 21. Nearly apertural section (YOAD3) from the lower part of the Millerella sp. A zone of the Akiyoshi limestone. Fig. 22. Nearly sagittal section (YOAD14) from the upper part of the Millerella sp. A zone of the Akiyoshi limestone. GKIMURA: Permo-Carboniferous endothyraceans Plate 50 4 11 604. Permo-Carboniferous endothyraceans 427 Por., vol. 13, p. 175-250, pis. 26 (in Jugosla Ser. Strati, and Paleont., no. 44, p. 49- vian). 94, pis. 8 (in Russian). LIE Bus, A. (1932) : Die Foraminiferen In: RAUSER-CHERNOUSSOVA, D.M. and REITLIN· Die Fauna des Deutschen Unterkarbons. GER, E.A. (1957) : Phylogeny of Paleozoic Pt. 3. Preuss. Geol. Landesanst., Bah., n.s., Foraminifera and its stratigraphical sig no. 141, p. 133-175, pis. 2 (in German). nificance. Izvest. Akad. Nauk, USSR, Ser. MooRE, R.C., edit. (1964) : Treatise on In Geol., vol. 11, p. 103-124 (in Russian). vertebrate Paleontology. Geol. Soc. Amer. --and FuLSENKO, A.B., edit. (1959) : Osnovy and Univ. Kansas Press. Paleontologii. Izdat. Akad. Nauk, USSR, MOROZOVA, V.G. (1949) : Representatives of Moskva (in Russian). the Families Lituolidae and Textulariidae REICHEL, M. (1946) : Sur Queleques Forami from the Upper Carboniferous and Artin niferes nouveaux du Permien Mediterra skian Deposits of the Bashkiria; Pre-Ural. nean. Eclog. Geol. Helvetiae, vol. 38, p. Akad. Nauk, USSR, Inst. Geol. Nauk, 524-560, pis. 19. Trudy, no. 105 (Geol. Ser. no. 35), p. 244- REITLINGER, E.A. (1950) : Foraminifera of 275, pis. 5 (in Russian). the Middle Carboniferous Formations of 0KIMURA, Y. (1963) : Characteristics of the the Central part of the Russian Platform Smaller Foraminiferal Assemblage from (Exclusive of the family Fusulinidae). the Carboniferous limestone of the Chu Akad. Nauk, USSR, Inst. Geol. Nauk, goku Province. Kaseki (Fossils), no. 6, Trudy, no. 126 (Geol. Ser. no. 47), p. 1- p. 1-6 (in ] apanese). 127, pis. 22 (in Russian). -- (1966) : Microbiostratigraphical Studies ScHUBERT, R. (1921) : Paleontologische Daten on the Foraminiferal Faunas of the Lower zur Stammesgeschichte der Protozoen. Carboniferous Formations of the Chugoku Pal. Zeitschr., Berlin, vol. 3, no. 2, 1-153. Region, Southwest Japan. Geol. Rep. Hi St. ]EAN, ]. (1957) : A Middle Pennsylvanian roshima Univ., no. 15, p. 1-46, pl. 1 (in Fauna from Dubois County, Indiana. In Japanese). diana Geol. Survey, Bull., no. 10, p. 1- PLUMMER, H.]. (1948) : Morphology of Globi 66, pis. 5. valvulina. Amer. Mid. Naturalist, vol. WARTHIN, A.S. (1930) : Micropaleontology of 39, p. 166-173. the Wetumka, Wewoka, and Holdenville POTIEVSKAYA, P.D. (1962): Representatives Formations. Oklahoma Geol. Survey, Bull., of certain Families of small Foraminifera. no. 53, p. 1-95, pis. 7. Akad. USSR, Kiev, Inst. Geol. Sci., Trudy, Akiyoshi f:k s Kobatake 1]' ...13 Atetsu [\iif 'ill Koyama il1li w Jinseki-gun f411:ilNI Kuma l'Jt Ill Kakisako :till i.E! Nagaiwa .ffi: !6 Kitakami ~1:; J: Taishaku 'iff fR 428 Yuji OKIMURA Explanation of Plate 51 (All figures x 100) Globivalvulina granulosa compressa REITLINGER Fig. 1. Nearly apertural section (YOAD22-1) from the upper part of the Millerella sp. A . zone of the Akiyoshi limestone. Figs. 2 and 3. Nearly sagittal sections (2, YOAKJ4; 3, YOAKJ2-2) from the lower part of the Millerella sp. A zone of the Akiyoshi limestone. Fig. 4. Sagittal section (YOADll-2) from the upper part of the Millerella sp. A zone of the Akiyoshi limestone. Fig. 5. Apertural section (YOAD22-2) from the same horizon as the above. Fig. 6. Parallel section (YOA3-2) from the lower part of the Millerella sp. A zone of the Akiyoshi limestone. Globivalvulina sp. cf. G. gracea REICHEL Fig. 7. Nearly sagittal section (YOTUYM51) from the Parafusulina zone of the Taishaku limestone. Fig. 8. Nearly sagittal section (YOTNDA4) from the Pseudoschwagerina zone of the Tai shaku limestone. Fig. 9. Sagittal section (YOTUYM18-3) from the Pseudoschwagerina zone of the Taishaku limestone. Fig. 10. Parallel section (YOTG27) from the Fusulinella zone of the Taishaku limestone_ Globivalvulina sp. B All specimens from the Yabeina zone of the Taishaku limestone. Fig. 11. Sagittal section (YOTKSH1). Fig. 12. Nearly sagittal section (YOTKSH2). Fig. 13. Tangentially oblique section (YOTKSH3). OKIMURA: Permo-Carboniferous endothymceans Plate 51 Trans. Proc. Palaeont. Soc. Japan, N.S., No. 87, pp. 429-435, September 30, 1972 605. A NOTE ON THE DISTRIBUTION OF BRAARUDOSPHAERA BIGELOW! (GRAN AND BRAARUD) DEFLANDRE IN THE BOTTOM SEDIMENTS OF SENDAI BAY, JAPAN* TOSHIAKI TAKAYAMA Institute of Geology and Paleontology, Faculty of Science, Tohoku University, Sendai, Japan fiJIT:fi;~Jm.l]'ifr:pO) Braarudosphaera bige/owi (GRAN and BRAARUD) DEFLANDRE [C. "?v'"C : flili:i'i~ J:: fJ };;(~ LJ-:: 18 jlli]O)!ii'&1i\Jtrfr:J:1 O)::p'g(f~-;1- Y I 7" 7 Y ~ r Y]\t~fC "?v' "C t~ ilt L-, )XO)*t;* ::!::j~t:o Braarudosphaera bigelowi fi7Ki~ 24m .L:.l,i~O)±!Etfl!fi;J"i" fC:~rli\r:::.~ IL', ~ h 0 0) feli L-, Cyclococcolithus leptoporus fi.:C O)!>'Hl!IJO) J:: fJ iA~v '±iEh't!f!JJ rj" rc ~ iflii' 0, jilijf.Ti0)5~;{fiO)rx:Jl:*ri, MARTINI (1967) ;?;----:,~.- Y'7iPJr:::..t>v'-c :r;-~~ L t.:f:;'i* c -rxi' 0 0 !l'li iJJ {~ A[l Introduction:-The living calcareous mation in California (BRAMLETTE and nannoplankton species Braarudosphaera SULLIVAN, 1961), the Middle Oligocene bigelowi (GRAN and BRAARUD) DEFLAN "Rupelton" of the Mainz Basin (MAR DRE has twelve regular pentagonal cal TINI, 1960) and the Sarmatian of the careous skeletal elements around the cell Vienna Basin (STRADNER, 1960). MAX which make a dodecahedral form (Text WELL et al. (1970) studied the deep sea fig. 1-a). Each pentagonal skeletal ele cores taken from the South Atlantic ment consists of five segments of crys Ocean and found several layers of Bra tallographic units which are joined along arudosphaera chalk of the kind that straight sutures that radiate from the occur most frequently in the Oligocene. center of the plate (Text-fig. 1-b). This According to them these layers of chalk species was first described by GRAN and consist almost exclusively of Braarudo BRAARUD in 1935 as Pontosphaera bigelowi sphaera rosa and are distributed widely and since then it has been reported from in the South Atlantic. They considered the sediments of the Jurassic to the Re that these chalk layers originated at cent by many investigators from many bathyal depths on the basis of the floral parts of the world. and faunal evidences associated with Abundant occurrences of fossil Bra Braarudosphaera rosa and they proposed arudosphaera bigelowi have been report two hypotheses to explain the origin, ed from various stratigraphic horizons: i.e. either unusual oceanographic condi the Danian of south-west France (MAR tions such as the so-called •· red-tide " TINI, 1961), the Lower Eocene Lodo For- bloom must have prevailed in this region for a short interval of geologic time or * Received Feb. 25, 1972; read Jan. 25, 1969 currents carried these shallow water at Tokyo. deposits into deep water. 429 430 Toshiaki TAKAYAMA Text-fig. l. Braarudosphaera bigelowi (GRAN and BRAARUD) DEFLANDRE; coccosphere (a) and its single plate (b). It is generally accepted that modern sis like other plants, they are mainly Braarudosphaera bigelowi occurs in abun concentrated in the upper layers of the dance only from the near shore water ocean within the reach of sunlight. and that it is very rare or absent in the Therefore it seems probable that such typical pelagic sediments despite a few factors as salinity and the temperature exceptions (GRAN and BRAARUD, 1935; of the surface water are more signifi GAARDER, 1954). MARTINI (1967) investi cant in the control of their distribution, gated the distribution pattern of Braaru than the depth of water. Their distri dosphaera bigelowi and Cyclococcolithus bution patterns are considered to be leptoporus in the recent sediments of the closely related to the present current Persian Gulf, the Gulf of Oman and the systems. Nevertheless, Braarudosphaera northern part of the Arabian Sea and bigelowi is assumed as a species that reported as follows ; Braarudosphaera inhabits coastal waters and through its bigelowi which is fairly abundant in the life-history the free-swimming genera Persian Gulf drastically reduces its num tion appears to alternate with filamen ber at the Strait of Hormz, becomes few tous or other sessile forms that colonize in the northwestern part of the Gulf of on rocks or other solid foundations. Oman and almost absent in the greater It is considered that the detailed stud part of the Gulf of Oman and northern ies of the modern Braarudosphaera bige Arabian Sea; on the other hand the lowi may afford some solution to the number of specimens of Cyclococcolithus origin of the spectacular burst of fossil leptoporus which is abundant in all sam Braarudosphaera at these stratigraphical ples from the Gulf of Oman, decreases horizons. However, these data are still abruptly at the Strait of Hormz, becomes incomplete and fragmentary, and the rare in the eastern part of the Persian origin is still a mystery. With this view Gulf and almost absent in the central in mind the present writer contributes part of the same Gulf. ·some data on the distribution pattern of As the calcareous nannoplankton uses Braarudosp!wera bigelowi in the bottom the energy of sunlight for photosynthe- sediments of Sendai Bay. 605. Distribution of Braarudosphaera bigelowt 431 Materials :-Sendai Bay is located on samples were taken from the bottom of the eastern side of Miyagi Prefecture; Sendai Bay in November, 1966, extend approximately at 38.30' to 37.50'N. Lat. ing from shallow water (19m) to the and 141.00' to 142.20'E. Long. and is upper part of the continental slope (203 surrounded by the Ojika Peninsula at m). The sampling localities are shown the north and by a gentle concave coast in Text-fig. 2. The samples were taken line at the west (Text-fig. 2). The coast by the Phleger sampler (PHLEGER, 1951, line between Ishinomaki and Soma Cities 1960) and the uppermost one centimeter is interrupted by the recently submerged in thickness, comprising approximately Matsushima Bay. On the land area sur 10 cc of wet sediment, was cut off from rounding Sendai Bay, the Miyagino each core and examined for the present coastal plain is headed at the north by study. At the time of sampling, meas the southern part of the Paleozoic and urements were made of the depth of Mesozoic systems of the Kitakami Massif. water and the surface and bottom water The main drainages into Sendai Bay are temperatures. The bottom water tem the Kitakami, Naruse, Nanakita, Natori perature was measured on board the and the Abukuma rivers. A total of 18 ship from the water obtained by the Text-fig. 2. Chart of Sendai Bay, showing locations of the samples. 432 Toshiaki TAKAYAMA Phleger sampler before removing the the suspension with a drinking straw sediment. These data are as follows: and settled out on a microscopic cover glass and dried on an electric hot-plate Water depth Temperature oc carefully. Caedax (n=l.55) was then Site No. (m) Surface Bottom spread over it,· dried and a large deck 127 19 15.8 12.5 glass was pressed on it. This was ex 128 22 16. 1 14.0 amined under a Nikon binocular polar 130 24 16.4 14.5 izing microscope with phase contrast 137 87 17.9 15.5 equipment. A magnification of 1,500X 138 109 17.8 15.5 with oil-immersion objective lens was 139 130 17.8 14.0 necessary. 140 143 17.6 14.0 Distribution pattern:-In each sample 17.7 12.5 141 142 two hundred specimens of coccoliths 142 203 17.9 12.4 were counted. The relative frequencies 143 144 17.9 13.5 144 147 18.7 13.5 of the species obtained are listed in 145 126 19.3 14.8 Table 1. Under the light microscope 146 103 19.5 15. 1 nearly half of the total specimens were 147 76 19. 7 16.0 too small (less than 3p) for precise iden~ 148 55 19. 7 16.0 _ tification, though they _were considered 153 34 18.9 15.5 to belong to Emiliania huxleyi, "Cocco 154 28 18.9 15.5 lithus doronicoides" and broken speci 174 130 18.5 14.5 mens of Gephyrocapsa oceanica. There fore they are lumped together under The present materials were processed miscellaneous in Table 1. Among the and examined according to the following remaining ones the fairly dominant spe methods outlined by STRADNER and P APP cies is Gephyrocapsa oceanica. In addi (1961). Disintegration of a very small tion, Coccolithus pelagicus, Braarudo quantity of the samples was placed in a sphaera bigelowi, Helicopontosphaera small glass. Water was added until a kamptneri, Cyclococcolithus leptoporus, depth of 3-4 em was obtained. The glass Rhabdosphaera clavigera and Syraco was placed in a ultrasonic equipment at sphaera pulchra were found, though rare moderate vibration level. After settling and sporadic in occurrence. Of the dis of the heavier particles, a few drops tribution patterns the following are re were sucked from the upper layer of cognized : 1) Braarudosphaera bigelowi Table 1. Abundance in counted specimen; 200 in each sample. Sample 1~1~1~1~1~1~1~1~1~1~1~1~1~1~1~1~1~1~ Species ------Braarudosphaera bigelowi 4 8 2 0 2 1 0 1 0 0 0 0 0 0 0 0 0 0 Coccolithus pelagicus 8 3 3 2 2 2 3 2 7 2 3 2 9 1 3 9 7 6 f!eclococcolithus leptoporus 0 0 0 2 0 0 2 0 3 2 6 3 5 1 7 8 5 3 eP.hyrocatsa oceanica , 85 42 62 100109 ~ 50 90 47 28 30 25 88 33 58 ~ 31 57 Helicopon osphaera kamptneri 1 1 1 3 0 0 0 0 1 1 0 0 0 3 0 0 1 0 1 Rhabdosphaera clavigera . 1 1 1 1 0 1 1 0 0 0 0 3 0 0 0 0 2 0 ~racosphaera pulchra 3 2 0 0 1 3 2 3 0 1 0 4 0 0 0 0 0 0 iscellaneous I 98 1~ 129 95 86 165 142 103 142 167 161 163 95 165 132 139 155 133 I M~ IDDDDD~D~DDDDDDDD~~ I - De_Pth (_lllL__ _ _, 19_E___3_4_ 28 34 55- 76 87 103 109 126 130_E_O 142 ~1,;3__1_44 ~ 605. Distribution of Braarudosphaera bigelowi 433 Table 2. Abundance in counted specimen ; 200 in each sample (Gephyrocapsa oceanica and miscellaneous excluded). ~=;=~<~, s~~~~ T127128130 15415314a1471371-4G138145139 174141l~o 1~3_144142_ 1 BraarUf}osphaera ~tgelowt I 90 99 82 - - 17 - 8 15 7 3 3 4 1 2 5 6 6 Coccoltthus.pelagtcus 1 54 28 45 - - 48 - 53 76 66 63 52 64 75 86 59 61 93 I Cyc(ococcoltfhus leptoporus . . 4 5 10 - - 52 - 41 90 77 118 86 64 89 101 107 100 95 Reltcopontosphgera kamptnert 7 2 7 - - 21 - 10 8 8 3 15 6 15 2 24 9 7 ! i Ooltthotus anttllarum. ' 0 0 0 - - 0 - 0 1 0 1 3 1 4 0 2 2 1 ' Rhabdosphaera clavtgera 4 8 8 - - 17 - 14 2 8 3 10 20 3 0 2 15 o Syracosphaera pulchra 41 58 48 - - 45 - 74 8 34 9 31 41 13 9 1 7 4 Total 200 200 200 - - 200 - 200 200 200 200 200 200 200 200 200 200 200 Depth(m) 19 22 24 28 34 55 76 S7103 109126 130130 142 143144147 203 is found only from the sediments less number of specimens were found from than 87 m in water depth and it is the these cores and also in some part of the characteristic species of the inner part sea floor of this area bed-rocks are ex of the bay; 2) Cyclococcolithus leptoporus posed. Table 2 shows that the near shore is rare or almost absent in the near sediments shallower than 24 m are char shore sediments; 3) Syracosphaera pul acterized by the abundant occurrence of chra occurs from the sediments less Braarudosphaera bigelowi compnsmg than 130 m in water depth. nearly 50 percent of the assemblage. On To reveal the distribution patterns of the contrary Cyclococcolithus leptoporus these species more clearly, in each sam is almost absent in this area. The dis ple 200 coccoliths specimens except Ge tribution patterns of these two species, phyrocapsa oceanica and miscellaneous which are substantially the same as specimens were counted at random again MARTINI's (1967), are shown in Text-fig. and identified. The relative frequencies 3 and Text-fig. 4. Judging from the of the species obtained are listed in Table present data, the distribution of Braaru 2. On this occasion station nos. 147, 153 dosphaera bigelowi is apparently control and 154 were excluded because only a led only by the depth of water. To small number of minute specimens of obtain a clear understanding of the real coccoliths were found from these sam factors involved, it is also necessary to ples. During the cruise several boring assume other factors such as fresh water were made in the area between station and nutrients provided by the drainages nos. 130 and 137 and between 148 and like the Kitakami River. At present no 152, but no cores could be taken because data concerning these factors are avail of the distribution of bedrocks. HATTORI able, and there is room for further in (1967) studied the bottom sediments of vestigation. Sendai Bay and divided them into thre~ Acknowledgements:-The author wishes units on the basis of texture, composi to acknowledge his grateful thanks to tion, minor structures of the sediments Professor Kiyoshi ASANO of the Institute and their presumed historical ages, i.e. of Geology and Paleontology, Tohoku Younger Suites, Older Sands A and Older University and Dr. Herbert STRADNER Sands B. Sample nos. 147, 153 and 154 of the Geological Survey of Austria for were obtained from the area of his Older their interest and encouragement. Deep Sands B, which were considered by him appreciation is due to Professor Kotara to be in the non-depositional area. This HATAI and Dr. Yokichi TAKAYANAGI of may be the reason why only a small the Institute of Geology and Paleontolo- 434 Toshiaki T AKAYAM A .0 ' ~ •t. of B~aarudosphaera bigelowi in total assemblage Text-fig. 3. Percentage distribut ion map of Braarudosphaera bigelowi. ~ "!. of Cyc/ococco/ithus /eptoporus in total assemblage Text-fig. 4. Percentage distribution map of Cyclococcolithus leptoporus. 605. Distribution of Braarudosphaera bigelowi 435 gy, Tohoku University for their critical coasteriden und verwandte Formen aus reading of the manuscript. The bottom dem Rupelton des Mainzer Beckens. No sediments were obtained by the research tizbl. hess. L..-Amt Bodenforsch., vol. 88, vessel Tansei-maru of the Oceanographic pp. 65-87, pls. 8-11. -- (1961) : Ein Kalkflagellat in den Meeren Institute, University of Tokyo; acknow der Gegenwart und Vorzeit. Natur u. ledgements ar'e expressed to the crew Volk, vol. 91, no. 9, pp. 335-339. of this ship for their kind assistance in -- (1967) : Nannoplankton und Umlager collecting the samples. ungserscheinungen im Persischen Golf und im nordlichen ArabischenM eer. Neus jahrb. Ceo!. Paliiont. Monatsh., vol. 10, pp. References 597-607. MAXWELL, A.E., HERZEN, R.P. von, HsU, BRAMLETTE, M.N. & SULLIVAN, F.R. (1961): K.]., Al'DREWS, ].E., SAITO, T., PERCI Coccolithophorids and related nannoplank VAL, S.F., MrLow, E.D., Jr. & BoYCE, ton of the early Tertiary in California. R.E. (1970) : Deep sea drilling in the Micropaleontology, vol. 7, no. 2, pp. 129- South Atlantic. Science, vol. 168, no. 3:?35, 188, 14 pls. pp. 1047-1059. GAARDER, K.R. (1954) : Coccolithineae, Silico PHLEGER, F.B. (1951) : Ecology of Foramini flagellatae, Pterospermataceae and other fera, northwest Gulf of Mexico, Pt. I., Fo forms from the "Michael Sars" North raminifera distribution. Ceo!. Soc. Amer., Atlantic Deep Sea Expedition 1910. Rep. Mem., 46, pp. 1-88, pls. 1, 2. Sars N. All. Deep Sea Exped. 1910, vol. --· (1960) ·: Ecology and distribution of 2, no. 4, pp. 1-20. Recent Foraminifera. The john Hopkins GRAN, H.H. & BRAARUD, T. (1935) : A quanti Press, Baltimore, viii+297p, pls. 1-ll. tative study of the phytoplankton in the STRADNER, H. (1960) : Dber Nannoplankton Bay of Fundy and the Gulf of Maine. Invasionen im Sarmat des Wiener Beckens. jour. Bioi. Board Canada, vol. 1, pp. 279- Erdoe!zeitschr. vol. 76, no. 12, pp. 430-432. 467. -- & PAPP, A. (1961): Tertiare Discoas HATTORI, M. (1967) : Recent sediments of teriden aus Osterreich und deren strati Sendai Bay, Miyagi Prefecture, Japan. Sci. graphische Bedeutung mit Hinweisen auf Rept. Tohoku Unip., 2nd Ser. (Ceo!.), vol. Mexico, Rumanien und Italien. jahrb. 39, no. 1, pp. 1-61. Ceo!. Bundesanst. [Wien], Sonderband, MARTINI, E. (1960) : Braarudosphaeriden, Dis- vol. 7, pp. 1-159, pls. 1-42. ------. -----·-----·---- Abukuma [liiffi\:flN Nanakita -t::ltl!l III'!. Ishinomaki T=i ~ Naruse ... '] i~hi Kitakami ;It; _L: Natori :f=, lf:'i Matsushima t~ llh Ojika u lk ,L, Miyagi fr tl!\ Sendai frlJ r::t Miyagino 7;•;JJN.'J!f Soma 1'11 ...If' ..; Trans. Proc. "Palaeont. Soc. Japan, N.S., No. 87, pp. 436-445, pis. 52, 53, September 30, 1972 606. FUSULINIDS OF THE PROFUSULINELLA ZONE OF THE TAISHAKU LIMESTONE (STUDIES OF THE STRATIGRAPHY AND THE MICROFOSSIL FAUNAS OF THE CARBONIFEROUS AND PERMIAN TAISHAKU LIMESTONE IN WEST JAPAN, NO.2)"' KIMIYOSHI SADA Department of Geology, Faculty of General Education, Hiroshima University ~iHREEk~~O) Profusulinella 11\'0)f;/jiil!!i\ C:fim • =:lll:~7iHR::fifk;{'50)/\"i/J; c IJ~it:.:fillilr.Jf1 f.FIC"?It''LO)lijfy"E, No. 2): ~~viiff,'~R:Pfk~O) Profusulinella ;fW (1'!.:133, 1967) IC:."?It' 'LO)/i}f~il'~ 2 fi]O) Profusulinella c 4 fi.J!O)~tHm~~}]lj L.. ;I::O)"""C", ;: ;: !;:~~!Ill( • i!H5·T .Q. il~lllX~nt.:f'!IHi Projusulinella fusijormis SADA, sp. nov., P. toriyamai SADA, Millerella sp. B, Pseudostaffella taishakuensis SADA, sp. nov., Nankinella yokoyamai SADA, sp. nov., Staffella akagoensis ToRIYAMA """C"~.Q, ;:tt,~O)f)j~!i\f<::.J:: -:>'L!f.\'~ -::3ft ~tt,.Q'ffr~R:r-i/.1(~0) Profusulinella 11Hi, F>iiftFG/.1(~0) Profusulinella toriyamai Tif (f!i:III, 1961, 1964, 1965), f:XE.f:fi/.1(~0) Profusulinella beppensis ;lW (.~LIJ. 1954, 1958), rliitl!!O) Profusulinella /ukujiensis * (~~J!II. 1957) f<::.M!t~n. ~ ~~;:::, ~1::.*0) Early Atokan 0) Profusulinella it:.=F-illi!J~ll'ff::.IH£~i'L.Q. ft.: Ill /];; ~i- to say, the Profusulinella beppensis zone Introduction (TORIY AMA, 1958) of the Akiyoshi Lime Having a very short stratigraphic stone, the Profusulinella fukujiensis zone range, the genus Profusulinella RAUSER (IGo, 1957) of the Ichinotani formation in CHERNOUSSOV A and BELJ AEV is regarded Gifu Prefecture and Profusulinella tori as being one of the best index fossils in yamai zone (SADA, 1961) of the Atetsu the lower part of the Middle Pennsyl Limestone in Okayama Prefecture. And vanian. The Profusulinella zones in Ja these zones are mostly characterized by such genera as Profusulinella, Pseudo pan have been reported from several staffella, Millerella, Nankinella, Staffella, areas since the first discovery of this Eoschubertella and Akiyoshiella, all rather zone (TORIY AMA, 1954) in the Akiyoshi primitive genera except for the last one. Limestone in Yamaguchi Prefecture but Recently, the Atetsuan was proposed by the Profusulinella zones whose zone fos TORIYAMA (1967) for the time strati sils had been described and illustrated graphic unit equivalent to the zone of are very few. As far as our knowledge Profusulinella in Japan based on the goes, they are only three zones, that is Profusulinella toriyamai zone in the * Received May 17, 1972; read Jan. 21, 1967 middle part of the Kodani formation of at Tokyo. the Atetsu Limestone (SADA, 1961). 436 606. Fusulinids of Taishaku Limestone 437 The Carboniferous and Permian Tai shaku Limestone about 30 km to the Systematic Paleontology west of the Atetsu Limestone, having Family Ozawainellidae THOMPSON been studied by me since 1965, comprizes in its lower part the Profusulinella zone & FOSTER, 1937 designated in my preceding paper (1967). Genus Millerella THOMPSON, 1942 The Profusulinella zone in this area, as I described before, conformably overlies Type species.-Millerella marblensis the Lower Pennsylvanian Millerella zone THOMPSON, 1942. and also is covered by the Fusulinella zone, while the species identified from Millerella sp. B the zone are Profusulinella toriyamai Pl. 53, figs. 13-14 SADA, P. fusiformis SADA, sp. nov., Mil lerella sp. B, Pseudostaffella taishakuensis Descriptive remarks.-The present spe SADA, sp. nov., Nankinella yokoyamai cimens are poorly preserved but the shell SADA, sp. nov. and Staffella akagoensis shape and some internai characters sug TORIY AMA. The present fauna consist gest that the present forms are ascri ing of them closely resembles in specific bable to genus Millerella. The shell of or generic composition the Profusulinella the present species is small and discoidal toriyamai fauna of the Atetsu Limestone. in shape. The periphery of the outer For example, Profusulinella toriyamai volution is broadly rounded to subangu SADA is a representative species in both lar and the shell has a short axis of Profusulinella faunas of the Taishaku coiling, possessing the umbilicate poles. and the Atetsu Limestone. Pseudostaf The specimen illustrated as fig. 14 on fella taishakuensis SADA, sp. nov. is simi Pl. 53 is 188,u long and 566,u wide. Its lar to P. kanumai IGO from the Ichino form ratio is 0.3. tani formation and the Atetsu Limestone The present species resembles some in some respects and they are almost of what Millerella ? sp. A (SADA, 1969, p. the same stage in the evolutional de 120, pl. 12, figs. 20-21) from the Cheste velopment of the shell. Accordingly, the rian Eostaffella zone of the lower part paleontological similarities between these of the Taishaku Limestone. The former two faunas indicate that the Profusuli species, however, can be distinguished nella fauna of the Taishaku Limestone from the latter one in having a longer is, to be sure, of the Atetsuan age. And axis of coiling, a larger form ratio and also the present fauna may be consid an incomplete evolute form in the outer ered to be of the equivalent age to the volutions. Profusulinella faunas in the lower part of the Middle Pennsylvanian in North America. In this paper are given six Table 1. Measurements of Millerella sp. B. species of fusulinids cited above from the Profusulinella zone of the Taishaku Specimen A12801D2e A12801D10g Limestone. Pl. fig. 53-13 53-14 Financial aid for this work was given Length 0.226 0.188 by the Ministry of Education and Ma Width 0. 660 0.566 tsunaga Science Foundation. Form ratio 0.3 0.3 (Measurements in mm) 438 Kimiyoshi SADA Occurrence.-Rare in the Profusulinella Description.-The shell is small and zone of the Taishaku Limestone. Asso ellipsoidal in shape. The mature speci ciated fusulinids are Profusulinella tori men of five volutions illustrated as fig. yamai SADA, P. fusiformis SADA, sp. nov., 1 on Pl. 52 is 1151,u long and 944,u wide, Pseudostaffella taishakuensis SADA, sp. having a form ratio of 1.2. The lateral nov., Nankinella yokoyamai SADA, sp. slopes are straight to convex. The ratios nov. and Staffella akagoensis TORIY AMA. of the half length to the radius vector Type locality is Loc. No. A12801D. of the 1st to the 5th volution are 1.0, 0.8, 1.5, 1.4 and 1.2, respectively. The proloculus is minute and its out side diameter is 37 ,u. The expansion of Family Fusulinidae VON MOLLER, 1878 the shell is slow. The radius vectors of Subfamily Fusulininae VON MOLLER, 1878 the 1st to the 5th volution in a specimen are 56, 113, 188, 302 and 510,u, respec Genus Profusulinella RAUSER tively. The spirotheca is thin and con CHERNOUSSOV A and sists of a tectum and inner and outer tectoria in all volutions. The thickness BELJAEV, 1936 of the spirotheca of the 1st to the 5th Type species.-Profusulinella aljutovica volution at the central part of the shell RAUSER-CHERNOUSSOVA, 1938. is 23, 23, 23, 39 and 50 ,u. respectively. The septa are unfiuted throughout the Profusulinella toriyamai SADA length of the shell. The tunnel is low and broad. The chomata are massive Pl. 52, figs. 1-4 in the outer volutions. 1958. Profusulinella sp. A, ToRIYAMA. Mem. Remarks.-In the shell shape, the in Fac. Sci. Kyushu Univ., Ser. D, Geol., ternal character and the measured values, vol. 7, pp. 35-36, pl. 1, figs. 20-21. the present species agrees closely with 1961. Profusulinella toriyamai SADA. jour. Profusulinella toriyamai SADA (1961, pp. Sci. Hiroshima Univ., Ser. C, vol. 4, no. 97-99, pl. 9, figs. 1-13) from the Atetsu 1, pp. 97-99, pl. 9, figs. 1-13. Limestone in Okayama Prefecture, West Table 2. Measurements of Profusulinella toriyamai SADA Specimen A12801D2a: Pl. 52, fig. 1. Length Width Form ratio Pro!. 1. 151 0. 944 1.2 0.037 Radius vector Ratio of HI. to Rv. Thickness of spirotheca Vol. Vol. Vol. 0 0. 009 1 0.056 1 1.0 1 0.023 2 0.113 2 0.8 2 0.023 3 0.188 3 1.5 3 0.023 4 0.302 4 1.4 4 0.039 5 0.510 5 1.2 5 0.050 (Measurements in mm) 606. Fusulinids of Taishaku Limestone 439 Japan. The holotype of four volutions (Rg. No. Occurrence.-Abundant in the Profusu A12801D13b) illustrated as fig. 8 on Pl. linella zone of the Taishaku Limestone. 52 is 1227 p long and 528p wide, giving Associated fusulinids are Millerella sp. a form ratio of 2.3. The fully grown B, Profusulinella fusiformis SADA, sp. specimen of five volutions (Rg. No. nov., Pseudostaffella taishakuensis SADA, A12801D13a) (Pl. 52, fig. 5) is 1567 p long sp. nov., Nankinella yokoyamai SADA, sp. and 755p wide and its form ratio is 2.1. nov. and Staffella akagoensis TORIY AMA. The inner two volutions are tightly coil Type locality is Loc. No. A12801D. ed and spherical to ellipsoidal, and be yond the 3rd volution the shell attains its mature shape. The ratios of the half Profusulinella fusiformis SADA, sp. nov. length to the radius vector in the 1st to Pl. 52, figs. 5-12 the 5th volution of four specimens are 1.0-1.7, 1.0-3.0, 1.6-2.9, 1.9-2.2 and 2.3, Description.-The shell is small and respectively. fusiform in shape, having a straight The proloculus is small. The outside axis of coiling and bluntly pointed poles. diameter of the holotype is 75p. The The lateral slopes are slightly concave. radius vectors of the 1st to the 5th Table 3. Measurements of Profusulinella jusijormis SADA, sp. nov. Specimen A12801D13a A12801D14b A12801D13b A12801D8d Pl. fig. 52-5 52-6 52-8 52-10 Length 1. 567 1. 511 1. 227 1.038 Width 0. 755 0. 736 0.528 0.547 Form ratio 2.1 2.0 2·3 1.9 Pro!. 0.037 0.056 0.075 0.056 Vol. Radius vector 1 0.056 0.056 0.056 0.075 2 0.094 0.094 0.094 0.113 3 0.151 0.188 0.151 0.188 4 0.264 0.321 0.283 0. 302 5 0.377 Ratio of HI. to Rv. 1 1.7 1.7 1. 7 1.0 2 2.0 2.4 3.0 1.0 3 2.4 2.6 2.9 1.6 4 2.2 2.2 2.1 1.9 5 2.3 Thickness of 0 0.013 0.011 0.018 0.016 spirotheca 1 0.016 0.021 0.011 0.025 2 0.016 0.021 0.009 0.016 3 0.023 0.018 0.018 0.021 4 0.025 0.032 0.027 0.011 5 0.039 (Measurements in mm) 440 Kimiyoshi SADA volution of four specimens are 56-75, proloculus. 94-113, 151-188, 264-321 and 377 p, respec Occurrence.-Commonly found in the tively. The spirotheca is thin and com Profusulinella zone of the Taishaku posed of a tectum and inner and outer . Limestone. Associated fusulinids are tectoria. The spirothecal thickness of Millerella sp. B, Profusulinella toriyamai the 1st to the 5th volution of four spe SADA, Pseudostaffella taishakuensis SADA, cimens is 11-25, 9-21, 18-23, 11-32 and sp. nov., Nankinella yokoyamai SADA, sp. 39p, respectively. The septa are almost nov. and Staffella akagoensis TORIY AMA. plane and closely spaced. The septal Type locality is Loc. No. A12801D. counts of the 1st to the 6th volution of a specimen illustrated as fig. 12 on Pl. 52 are 5, 11, 13, 15, 15 and 20, respec Genus Pseudostaffella THOMPSON, 1942 tively. The chomata are well developed and massive in the outer volutions. The Type species.-Pseudostaffella needhami tunnel path is almost straight. The THOMPSON, 1942. tunnel angle of the 3rd volution of the Pseudostaffella taishakuensis holotype is 32°. Remarks.-ln the shell size, the shell SADA, sp. nov. shape, the number of volutions, the Pl. 52, figs. 13-21; Pl. 53, fig. 12 rate of expansion, the spirothecal struc ture, and the mould of chomata, Pro Description.-The shell of the present fusulinella fusiformis SADA, sp. nov. is species is small and spherical to sub closely allied to Profusulinella sp. B de spherical in shape. The specimens of scribed by SADA (1961, pp. 105-107, pl. five volutions are 679 to 830p in length 10, figs. 4-8) from the Profusulinella and 660p in width, giving the form ratio zone in the middle part of the Kodani of 1.0 to 1.3. The shells of four volu formation of the Atetsu Limestone. The tions are 528 to 660p long and 528 to 622p striking similarities between these two wide, having form ratio of 0.9 to 1.3. species indicate that they are indubit The inner one to two volutions are tight ably conspecific each other. The present ly coiled and they show commonly endo species differs from Profusulinella tori thyroid coiling. yamai SADA (1961, pp. 97-99, pl. 9, figs. The outside diameter of the proloculus 1-13 and figs. 1-4 on Pl. 52 in this paper) is 75p in the illustrated specimens. The from the Atetsu Limestone and the Tai radius vectors of the 1st to the 5th volu shaku Limestone in that the former spe tion of four specimens are 75, 94-132, cies is fusiform in the shell shape and 170-188, 207-321 and 358-396p, respec has the larger form ratio and the slower tively. The spirotheca is thin and con expansion of the shell. Profusulinella sists of a tectum and inner and outer fusiformis SADA, sp. nov. somewhat re tectoria. The thickness of the spirotheca sembles P. beppensis TORIY AMA (1958, of the 1st to the 5th volution is 16-27, pp. 31-33, pl. 2, figs. 1-6) from the Aki 16-23, 13-27, 23-29 and 25-34p, respec yoshi Limestone. However, P. fusiformis tively. The chomata are well developed can be easily distinguished from P. bep and massive and asymmetrical in the pensis by its shape of the· shell, its outer volutions. longer axis of coiling, its slower expan Remarks.-Pseudostaffella taishakuensis sion, its larger form ratio and its larger SADA, sp. nov. is somewhat similar to 606. Fusulinids of Taishaku Limestone 441 Table 4. Measurements of Pseudostaf/ella taishakuensis SADA, sp. nov. Specimen Al2801D5b A12801D10c A12801D7c A12801D4d Pl. fig. 52-13 53-12 52-21 52-20 Length 0.660 0.528 0.830 0.679 Width. 0.528 0.622 .0. 660 0.660 Form ratia 1.3 0.9 1.3 1.0 Pro!. 0.075 0.075 0.075 Vol. Radius vector 1 0.075 0.075 2 0.113 0.132 0.094 0.094 3 0.170 0. 188 0.188 0.188 4 0.207 0.321 0.283 0.245 5 0.396 0.358 Thickness of 0 0.034 0.013 spirotheca 1 0.027 0.016 0.018 0.023 2 0.021 0.016 0.021 0.023 3 0.021 0.013 0.016 0.027 4 0.025 0.029 0.025 0.023 5 0.025 0.034 (Measurements in mm) Pseudostaffella kanumai IGO (1957, pp. Associated fusulinids are Millerella sp. 194-196, pl. 4, fig. 26, pl. 5, figs. 1-5) and B, Profusulinella toriyamai SADA, P. P. kanumai pauciseptata IGO (1957, pp. fusiformis SADA, sp. nov., Nankinella 196-197, pl. 5, figs. 6-8) from the Ichino yokoyamai SADA, sp. nov., Staffella aka tani formation in the Fukuji area, Gifu goensis TORIY AMA. The type locality is Prefecture, Central Japan. The former, Loc. No. A12801D. however, can be distinguished from the latter two by its smaller shell, rather Family Staffellidae MIKLUKHO larger form ratio and larger proloculus. Pseudostaffella taishakuensis, sp. nov. can MAKLAY, 1949 · be recognized from P. rotunda DoUGLASS Genus Nankinella. LEE, 1931 (1971, pp. 6-9, pl. 2, figs. 4-21), which was described from Peratovich Island Type species.-Staffella discoides LEE, near Prince of Wales Island, Southeast 1931. ern Alaska, by its smaller size of the shell, the smaller chomata and the nar Nankinella yokoyamai SADA, sp. nov. rower tunnel angles. Pseudostaffella tai Pl. 52, fig. 22; Pl. 53, figs. 1-2, 4-11 shakuensis, sp. nov. differs from P. sand ersoni THOMPSON (1965, p. 227, pl. 33, Description.-The shell of Nankinella figs. 10-18) from British Columbia in yokoyamai SADA, sp. nov. is discoidal having a larger shell and thicker spiro and planispiral throughout growth and theca. has umbilicate to partial umbilicate poles Occurrence.-Common in the Profusu and angular periphery in general. The linella zone of the Taishaku Limestone. axial length and median width of the 442 Kimiyoshi SADA Table 5. Measurements of Nankinella yokoyamai SADA, sp. nov. Specimen A53112704 A12S01D4c A12801D6c A12801D6d A12801D15b A12801D14c Pl. fig. 53-1 53-9 53-10 53-11 53-4 53-6 Length 0.453 0.377 0.415 0.245 0.510 0.340 Width 1. 473 0.849 0.849 0.698 1. 208 1. 085 Form ratio 0.3 0.4 0.5 0.4 0.4 0.3 Pro!. 0.075 0.056 0.075 0.075 0.037 0. 056 ~ Vol. Radius 1 0.075 0.075 0.075 0.056 0.094 0.056 vector 2 0.132 0.132 0. 132 0.113 0. 188 0.113 3 0.207 0. 188 0. 188 0.170 0.283 0. 188 4 0.283 0.283 0.321 0.264 0.415 0.283 5 0.396 0.472 0.472 0.396 0.566 0.415 6 0. 566 0.603 7 0. 755 Thickness 0 0.025 0.034 0. 011. 0.018 0. 011 0. 018 of 1 0.018 0.011 0.025 0.032 0.018 spirotheca 2 0.018 0.013 0.018 0.023 0.013 3 0.018 0.011 0.023 0.023 0.021 4 0.013 0.025 0.016 0.023 0.021 0.021 5 0.025 0.023 0.023 0.021 0.025 0.023 6 0.046 0.029 7 0.023 -~~-~---~ ~-----·------(Measurements in mm) Explanation of Plate 52 Figs. 1-4. Profusulinella toriyamai SADA 1-2. Axial sections: Rg. No. A12801D2a (x22) and A12801D10a (x22), respectively. 3-4. Sagittal sections: Rg. No. A12801D6a ( x 22) and A12801D8f ( x 22), respectively. Figs. 5-12. Profusulinella fusijormis SADA, sp. nov. 8. Axial section of the holotype: Rg. No. A12801D13b ( x 22). 9. Enlarged figure of Fig. 8 ( x 50). 5-6, 10-11. Axial sections of paratypes: Rg. No. A12801D13a ( x 22), A12801D14b (x 22), A12801D8d (x22) and A12801D2b (x22), respectively. 7, 12. Sagittal sections of para types: Rg. No. A12801D8c ( x 22) and A12801D10a ( x 22), respectively. Figs. 13-21. Pseudostaf[ella taishakuensis SADA, sp. nov. 20. Axial section of the holotype : Rg. No. A12801D4d ( x 63). 13-17,21. Axial sections of paratypes: Rg. No. A12801D5b (x63), A12801Dla (x63), A12801D4b (x63), A12801D1b (x63), A12801D4e (x63) and Al2801D7c (x63), respec tively. 18-19. Sagittal sections of paratypes: Rg. No. A12801D9c (x63) and A12801D5a (x63). Fig. 22. Nankinella yokoyamai SADA, sp. nov. 22. Sagittal section of a paratype: Rg. No. A12801D6b (x63). 606. Fusulinids of Taishaku Limestone 443 holotype of the species (A53112704) illus stone. trated as fig. 1 on Pl. 53, are 453 and Occurrence.-Commonly found in the 1473p, respectively. Its form ratio is 0.3. Profusulinella zone of the Taishaku The specimens of five to six volutions Limestone. Associated fusulinids are are 245 to SlOp long and 698 to 1208p Millerella sp. B, Profusulinella toriyamai wide. Their form ratios range from 0.3 SADA, P. fusiformis SADA, sp. nov., and to 0.5. Staffella akagoensis TORIY AMA. The type The proloculus has the outside diame locality is Loc. No. A12801D. ter of 37 to 75p in six specimens. The radius vectors of the 1st to the 7th volu tion are 56-94, 113-188, 170-283, 264-415, Genus Staffella OzAWA, 1925 396-566, 566-603 and 755p, respectively. Type species.-Staffella sphaerica VON The spirotheca is partly replaced by the MOLLER, 1878. secondary mineralization and it seems to be composed of three layers in the Staffella akagoensis ToRrY AMA inner volutions and four layers consist ing of a tectum, diaphanotheca and inner Pl. 53, fig. 3 and outer tectoria in the outer two volu 1958. Staffella akagoensis ToRIYAMA. Mem. tions. The septa are unfluted and ex Fac. Sci., Kyushu Univ., Ser. D, Geol., tend forward slightly. The septal counts vol. 7, pp. 22-24, pl. 1, figs. 6-8. of the specimen illustrated as fig. 7 on Pl. 53 are 7, 9, 11 and 15, respectively, Description.-The shell of Staffella aka for the 1st to the 4th volution. The goensis TORIY AMA is small, subspherical chomata are low. The tunnel angles of and planispiral, having a broadly round the 3rd to 5th volutions of the holotype ed periphery. The specimen of six vo are 14, 14 and 12 degrees, respectively. lution (Pl. 53, fig. 3) is 566p long and Remarks.-Nankinella yokoyamai SADA, lOOO,u wide, possessing a form ratio of sp. nov. resembles in some respects Nan 0.5. kinella plummeri THOMPSON (1947, pp. The proloculus is small and its outside 155-157, pl. 32, figs. 11-16, pl. 33, figs. diameter is 56p. The radius vectors of 10-11) from the Pennsylvanian rocks of the 1st to the 6th volution of a specimen the Llano Uplift in Texas. However, are 56, 94, 188, 283, 377 and 528p, respec the mature form of the former species tively. The spirotheca is thin and seems has a longer axis of coiling, generally to consist of four layers such as a tectum, larger proloculus and fairly thicker a lighter layer seemingly like a diaphano spirotheca. Nankinella yokoyamai SADA, theca and inner and outer tectoria. The sp. nov. is similar to Nankinella sp. A thickness of the spirotheca of the outer by KOCHANSKY-DEVIDE (1965, p. 118, pl. three volutions of a specimen is 18 to 2, figs. 14-18). The former species, how 25p. The chomata are low and asym ever, can be distinguished from the lat metrical. ter one by the larger shell, the larger Remarlzs.-The present species resem proloculus and the umbilicate form of bles closely Staffella akagoensis TORIY A the former species. The species name MA (TORIY AMA, 1958) from the Profusu is dedicated to Dr. Tsuruo YoKOYAMA linella zone of the Akiyoshi Limestone who formerly carried on the study of in all respects except for the length of the stratigraphy of the Taishaku Lime- the shell and the form ratio. The pre- 444 Kimiyoshi SADA Table 6. Measurements of Stafjella References akagoensis TORIYAMA. Specimen A53112704Jb: Pl. 53, fig. 3. (See also the references cited in the preced ing papers by SADA (1967, 1969 and 1970)) Length Width Form ratio Prol. 0.566 1. 000 0.5 0.056 DouGLAss, R.C. (1971) : Pennsylvanian Fusu linids from Southeastern Alaska. Geol. Radius vector Thickness of spirotheca Surv. Prof. Paper 706, pp. 1-20, pls. 1-7. Vol. Vol. KocHANSKY-DEVIDE, V. (1965) : Die Fusu 1 0.056 0 liniden Foraminiferen aus dem Karbon 2 0.094 1 und Perm im Velebit und in der Lika 3 0. 188 2 (Kroatien) Mittleres und Oberes Perm. 4 0.283 3 jugoslavenska Akademija znanosti i Um 5 0.377 4 0.018 jetnosti Odjel za Prirodne Nauke, Acta 6 0.528 5 0.018 geologica v, str. pp. 101-150, pls. 1-13. 6 0.025 SADA, K. (1961) : Profusulinella of Atetsu Limestone. jour. Sci. Hiroshima Univ., (Measurements in mm) Ser. C, val. 4, no. 1, pp. 95-116, pls. 9-10. -- (1964) : Carboniferous and Lower Per sent form has the slightly shorter length mian Fusulines of the Atetsu Limestone of the shell and the smaller form ratio. in West. Japan. Ibid., val. 4, no. 3, pp. However, it seems that such a difference 225-269, pls. 21-28. between these two forms falls within -- (1965) : Carboniferous and Permian the specifk variation of Staffella akago Stratigraphy of the Atetsu Limestone in ensis TORIYAMA. West Japan. Ibid., val. 5, no. 1, pp. 21- Occurrence.-Abundant in the Profusu 80. linella zone of the Taishaku Limestone. -- (1967) : Fusulinids of the Millerella Zone of the. Taishaku Limestone (Stud Associated fusulinids are Millerella sp. ies of the Stratigraphy and the Micro B, Profusulinella toriyamai SADA, P. fusi fossil Faunas of the Carboniferous and jormis SADA, sp. nov., Pseudostaf!ella tai Permian Taishaku Limestone in West shakuensis SADA, sp. nov. and Nankinella Japan, No.1). Trans. Proc. Palaeont. Soc. yokoyamai SADA, sp. nov. Type locality japan, N.S. no. 67, pp. 139-147, pls. 12-13. is Loc. No. Al2801D. - (1969) : Microfossils of the Lowest Part Explanation of Plate 53 Figs. 1-2, 4-11. Nankinella yokoyamai SADA, sp. nov. 1. Axial section of the holotype: Rg. No. A53112704 (x55). 2, 4-6, 9-11. Axial sections of paratypes: Rg. No. A12801D7a (x60), A12801D15b (x60), A12801D13c ( x 60), A12801D14c ( x 60), A12801D4c ( x 65), A12801D6c ( x 60) and A12801D6d (x60), respectively. 7-8. Sagittal sections of para types: Rg. No. A53112704Ja ( x 60) and A12801D8a ( x 60), respectively. Fig. 3. Stafjera akagoensis TORIYAMA 3. Axial section : Reg. No. A53112704Jb ( x 60). Fig. 12. Pseudostafjella taishakuensis SADA, sp .. nov. 12. Axial section of a paratype: Rg. No. A12801D10c (x60). Figs. 13-14. Millerella sp. B 13-14. Axial sections: Rg. No. A12801D2e ( x 91) and A12801D10g ( x 100). SADA : Fusulinids of Taishaku Limestone Plate 52 ·~~2 ~,_~ 3 ·~4 8 • 12 .,~ 18 Plate 53 SADA: Fusulinids of Taishalc~~ Limestone 606. Fusulinids of Taishaku Limestone 445 of the Taishaku Limestone (Ditto, No. 4). 31-33. Ibid., no. 75, pp. 119-129, pis. 12-13. - (1965) : Pennsylvanian and Early Per - & YoKOYAMA, T. (1970): Fusulinids of mian Fusulinids from Fort St. James Fusulinella Zone of the Taishaku Lime Area, British Columbia, Canada. Ibid., stone (Ditto, No: 3). Mem. Fac. General vol. 39, no. 2, pp. 224-234, pis. 33-35. Educ. Hiroshima Univ. II I, vol. 4, pp. 45- ToRIYAMA, R. (1954) : Geology of Akiyoshi. 54, pl. 1. Pt. 1. Study of the Akiyoshi Limestone THOMPSON, M.L. (1947) : Stratigraphy and Group. Mem. Fac. Sci., Kyushu Univ., Ser. Fusulinids of Pre-Desmoinesian Pennsyl D, Geol., vol. 4, no. 1, pp. 40-97. vanian Rocks, Llano Uplift, Texas. jour. - (1967) : The Fusulinacean Zones of Ja· Paleont., vol. 21, no. 2, pp. 147-164, pis. pan. Ibid., vol. 18, no. 1, pp. 35-260. Akiyoshi Limestone 1':k2f:r:ifk:'G Ichinotani Atetsu Limestone lliiJtf:r:ifk:'G Kodani Fukuji rffi J:lli Taishaku Limestone ','i'HI'rfifk~~;· 446 PROCEEDINGS OF THE PALAEONTOLOGICAL SOCIETY OF JAPAN B;tJ!l·~fu~:~~ 109 @1-f?~:iHJ:, 1972 it: 6 H 3 Some fossil Pteropoda from Miyazaki and B ~tii'I;I::k"lt~i!l'tillfc.iJv•"CfJf.JHli~ ht-::0 (iJ::IJn~ Okinawa Prefectures, Japan .... NooA, H. ro~)~k~6H4s~n. ~**~~~. *~* ~-- v '/ '/ · - A .!H- 110 @] i7IJ = ~ !l}1 * "[- 1972 1:['. 10 FJ 28· 29 13 1972 1¥- 9 FJ 20 13 19731¥- ~S; ·l,f-S; ;II:. 7c ¥ 1973 1f:. 1 JJ 16·17 13 197 21¥- 11 FJ 20 B* * 1973 if. 6 JJ 23 .24 13 111 @] ~ lj A iliff if.!~ 197 31¥- 4 JJ 20 13* = * ~ (7 ~ ) • ~~ jl?iv.J 8 f:t. , 7. ~" ~7" 7 Af-O!i\lj0)\"i[lf;"C4"1& C. M~ fiJi O) ~ 2 'r Fl 'M velt't..: L ;J: -r o ~~~~ ~ jjl("f~ v'o o ~ 110 IElf0JS; · !ilHtiili~ c1oFJ 29 s)-i:J:t :9c Wi. i1H,~. &....nma:r. = ,g.~t,r.c - c ~P'l1f :ik:;tt-~:=:) 0 1972 1¥- 6 JJ J: f:J O)J.. S;c.\f (1972 if. 6 fl 2 13 O)i\'f.r.n~ S;-z:· jjl([;?c! ) f:HMf ilf!~~ 8 15 :tE?>tS;~ 1 15 (1~1' jii'], 1i\(#Jimf'T) o J:.i1!3/ii~:l~~. sfr: :J:~i$~ . P91li:h=- . fJiii~ ill. iZ§III!AHr. lli'ilti ill, ;ji;:ik=:=:~B . iHti=~B . ~ ~ 0 0 1972 1f. 6Jl 213 0)~~~~S;t:::.;fov'-c , {;;:O)f,'lf~O) ifl: ~n;~:z,llJG:M..: (lffjf,Ji rof'T ) o :Eiti: :=:~~ . ~!ilrtvFf . ~)(.;fiJ- , *8 !ilt~ ~. ill11 * t..: lt ;Fo , 't\PJ!Xi~rzWJ, l~ilJ []i\] i\'\ «:) 1972 iJ'. 5 J'l Jl tE 3t H<~~~j:{l-fj [ · 473 ::f6o 0 il\itici\~~&&S;ICBv'"'C r5' 1:~;J ~ liJf )b±t:~~N~~~O)fl~iJ+fi il;~ I:L\~h t..: (1Ui'i1'1i\1 , 1SX#!iW5-) o ~lilt li!i ( ~~~fj~~) . 7c ~$ ~iili ( ~ f,\ij ~f.:/'0 , iJ7:t:HI!i\:JTI: OfVJ ~!J~~ ). JliTJ II)i::!~ CHEi~;J~S; ), ;ji;::;f;:i!~B. llliFa,Jey ~ . TE ;tt: 'Uf~~. 1 hl'li §: ~ . illlil~Pf.¥:5, fJ~i1!3i~liGi . l~lll~ffr± . l\1l i :Ji'~ =. miii~-~Bo 0 il\iflcil~i\~&S;ICHv'-cf41iJf!lJtffiL5-!~~S;~&O)®tr~M ;lJ,:O)J:? IC~I±\~ ~1.-f..:o illli:fVPt$6, [§[fi {);:!Jg , iti'.ii.'ii lE ((J.: .. ~, Bi: ~ 7'.2> 0 NEWS o 1972 1¥- 8 fl 11 13 1:::~ 9 W li!:i 1:171.J~ rvt Jt.iillt~~&S;O)AA 1 IEl4:.'iln;r,rJn> t'1 , ~~:J¥:~ c~!ilt m. **1::: 7c~--RI§ i !li . 1 ] ';l1lj §;~ , 1H~'W~ fl , ~lii i i~ ±. t!':::;f;:i!~!IO) 5 ;ft t; ;;~~l\ ~ tot..: o «:) Hciillt~~&S;Ic ;Fov' -c , JXO) J: ? IC%1ffi~&iJ ; ~I:I:'. ~ ht..: (ll ~i1'1iil , IJX#r; Wf'T) o ttl!.~ it~ • ~"=83 ft ~ }illi;'1 J ' ~& S; ( ' l 'i1!3~= ), I]!~JiU I!l :£'1\r/Il ! iHII%;lJIJ~&S; (r~~l'l*c ;;f; ), f.<;:.iflcPM ! fJ' liJ!Y'Giillt~~~ 4:.: (;ji; ::;f;: i!~~ ). [W ~ 1 9 7 2 1¥- 9 JJ 25 13 ~p li\U §'Efi:li a;;t;:·J5~tJ~~ 1 9 7 2 if. 9 Fl 30 13 9E fJ )[ 5l'\ 1R siF ~ 2-4-16 13 * ~ 4:.: * f:t t :/ !1 - P'l (ji ~ r:J ~ * * 8 4 7 8 0 ';=) Efl ± w lilO :%f * * $ ~ .~ IK ~ .:E ;It 2 I 13 900 p:j ~~~~]:flfGIJ!*:rt:4:.'t± "II Ill :7[; Transactions and Proceedings of the Palaeontological Society of Japan New Ser ies No. 87 September 30, 1972 CONTENTS TRANSACTIONS 601. MATSUMOTO, Tatsuro, MU RAM OTO, Tatsuo and !NOMA, Akitoshi: Two small desmoceratid ammonites from Hokkaido (Studies of the Creta- ceous ammonites from Hokkaido and Saghalien-XXIV) ...... 377 602. MASUDA, K6ichir6: Swiftopecten of the Northern Pacific ...... 395 603. HAT AI, Kotora, NODA, Hiroshi and OGASAHARA, Kenshiro: Scaphopoda like fossils from the Udo formation (Miocene) of Miyazaki Prefecture, Japan ...... 409 604. OKIMURA, Yuji: Permo-Carboniferous endothyraceans from Japan, Part 1. Biseriamminidae ...... 414 605. TAKAYAMA, Toshiaki: A note on the distribution of Braarudosphaera bigelowi (GRAN & BRAARUD) DEFLANDRE in the bottom sediments of Sendai Bay, Japan ...... 429 606. SADA, Kimiyoshi : Fusulinids of the Profusulinella zone of the Taishaku Limestone. (Studies of the stratigraphy and microfossil faunas of the Carboniferous and Permian Taishaku Limestone in West japan, No.2) . . 436 PROCEEDINGS ...... 446 -?%iC:·JPtt.~: fJ, tr L 0, Ditrupa lC~Jift( L, J::)!tO) ~~N&f'J: 7-.Xllfillf~fflifif!i.J> Ditrupa vcl,li;-9