Edito1': Hiro shi UJIIt
Associate editors : l kuwo OBATA, Yasuji SAlTO, Kazuhiko UEMURA

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Tatsuro MATSUMOTO

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Hiroshi UJIIt, Ikuw o OBATA, Yasuji SAITO, Kazuhiko UEMURA

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Kametoshi KANMERA, Itaru HAY AMI, Tomowo OZAWA" Fossils":

Yokichi T AKAY ANAGI, Toshiaki TAKAYAMA

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from the Late Permian A kasaka Series in Gifu Prefecture.

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Trans. Proc. Palaeont. Soc. Japan, N. S., No. 90, pp. 45-71, pis. 9-10, June 20, 1973

615. BIOSTRATIGRAPHIC STUDY OF
THE JURASSIC TOYORA GROUP'PART IIIHIROMICHI HIRANO
Department of Geology, Faculty of Science, Kyushu University-/:>. :7 *cf~!:iil;I'3m:0){t1]"r\'f1If~(I"Jl!JfJE --to) 3: :ll!l:illirl'Wf''EO) 7 :/.of: 7 1 r 10 Hpi!:nt!.·I&
l, i::. hfe J: IJ, -to) 1 J: IJ "Co' ~ {f.)f.v ,t:: 7:/.of: 71 r O)~c,nx::!:-1"A:-C *,~n L- t::.o :;f>:1\1f,fo)lI~frtf;):, 7:/'.of: 7 1 r tJ: G U'fe 1 I -t: :7 1, 7- J: I). Sinemurian j. G Bathonian fel*~ C~!Jii:~.:/l.,~o 7 :.(-t-71 Htl1::!:~JffT0jJSr:J:tLlJl\lif:l:. TH[J: I) Fontanellicerasfontanellense;:g:. Protogrammoceras nipponicum ;w,:. Dactylioceras helianthoides ;1!~:0) 3 ;:I~:iI~Ui\j}IJ ~:lc~o i::.:/cGf;):. f;11iJ:tUl!!lDxO)::jI:>'F-c'f:l:tL;*· IH} (1947) 0)3;:I~:f:::.i'rk*I'I~T~:d):. T~j.'j':""(
v:l:N;fe-tO)T~I'. nr)iI:~'}*ln iI'tJ: IJ >jH3tT ~ :::. C i.I: IVl G i.I< ji, ~o 19\1+1 t!g~JI!!J;j( C 'j:(if.~fiJ<~&-:5 ~ lU~-1" ~ C. F.'j. ':IHi Margaritatus *0) Stokesi ill!::WiI' G Spinatum ~i'':O)Tl'if\f:::',
P.ll. :,'IHi Spinatum ':g: J:1'i11i1' G Fa/cifer 1iH:::.. D. h. ;,'I7fi Falcifer 'lifO) Exaratum ill~
~1~:iJ' G Bifrons '1\fO) Fibulatum ill!~IHeMlt ~ :11-0 :;f>:fflUfO) 7 :/.of: 71 HiIJ~IlHi. ftll~
116H*~c "ide Hildoceratidae O)f&j@""('ffli~-:5lt Gh0:::.:ll::!: SIMPSO~ O)0-J'\::t:::.J: I) ft!l:rJll(O)bO)clt~;;:i-0 c. Domerian illip{1fO)JJJ~lIHi:/:/ ~ -,Ii.~O)bo)f::', -M1t::.fiJI!!r:J:tijijJ:t!l:h'O)bo)f:::.~1t'ViIJ;l,i'f£\!:"7f;To Whitbian -Cfil9\i+Ii'rJl!!c*L- < ?o1lil,'fl1jJ.)i'f£I!:"7f;lfij',i IJi.I:ts:v' 0 Yeovilian ""('vi::I - :h -tj- 7-tt!l:JjO) b 0) c O);z,., iI'tJ: I) ~1, ,'UjfJ.)!.t\!:"7f;T ::It:lj~jlEjl~F>iI' G:;f>:Mf,fO) Domerian c Whitbian O)bO)t:::'lU!Z~:ll0Ufl';5~ht.:to)fi. ~[/J~IlP: L--C;z,.
t::#/}1r~ t;i Ej11jjv' ~fiV;J.§(~7f;~ tJ: 1,'0 :;f>:lWnfB J: If::lI:;:lj:.:jJSj}[IO) 7:/'.of: 71 I- WJ17011Hi c t fC
JM~in}*0f<fi'l&~ b -JiI~. IV:'J+I""(JZ\ <;z,. Gh 0 J:: oj tJ: :G*~ C 'UI] O)-iE0) *rl';I-tt;;!:7f;~ f.

*t

0

0

0

~v7~*0)~m~J:IJ~T00~H~illspecies of Lytoceratidae. Nannolytoceratidae. Phylloceratidae and Juraphyl-'
litidae are systematically described.
Zonation and correlation is discussed.
by comparing the ammonoid assemblagesof the Toyora Group with European
standard. The characteristics of the
Toyora faunas are discussed by theinvestigation of assemblages. comparison
with other faunas in Japan and comparison with some faunas of other region.

Introduction

This article is Part III of the serial
biostratigraphic study of the Jurassic
Toyora Group. In the preceding Parts
lev II lithostratigraphy and 6 genera including 31 species of Domerian. Whitbian
and Yeovilian ammonites (Amaltheidae,
Dactylioceratidae. Hildoceratidae. andHammatoceratidae) were described. In
the present part comparatively uncommon 4 species of Hammatoceratidae,
Dactylioceratidae and Arietitidae and 6

Palaeontology (continued from Part II),
Subfamily Hammatoceratinae
BUCKMAN, 1887

* Received July 12, 1972; read Jan. 23, 1971.
at Tokyo.
45

46

Hiromichi HI RAND
Genus

Planamlllatoceras

BUCKMAN, 1922
Type-species :-Planammatoceras planiforme BUCKMAN, 1922
Planammatoceras sp. ct. P.
kitakamiense (SA TO)
PI. 9, Figs. 7a-b
Cf. 1934. Planammatoceras kitakamiense SI-IIMIZC; SHI:VIlZU in SI-II:'vIlZL: & 013ATA,
Cephalopoda, Iwanami book Co., vol.
32, no. 9, p. 119, fig. 58B (nom. nud.)1947. Hammatoceras sp.; MATSUMOTO in
MATSUMOTO & 01'0, Sci. Rep. Fac.
Sci., Kyushu Univ., Ceo!., vol. 2, no. 1,
p. 29, pI. 2, fig. 4.
Cf. 1954. Hammatoceras kitakamiense SI-11·\IIZU; SATO, Jap. Jour. Ceol. Ceogr.,
vol. 25, pp. 84-86, pI. 7, fig. 4, pI. 8,
figs. 3 & 5, pI. 9, fig. 4.
1956 Hammatoceras (Planammatoceras) d.
kitakamiense(SHIMIZU) ;ARKELL,
Jurassic Geology of the World, Oliver& Boyd Ltd., p. 421.
1962. Planammatoceras d. kitakamiense SHI\HZU; SATO, Mem. Soc. Ceol. France,
no. 92, p. 67.
1963. Hammatoceras (Planammatoceras) d.
kitakamiense (SHIMIZU) ; TAKAI, MATSUMOTO & TORIYA\IA ed., Geology ofJapan, Univ. Tokyo Press, p. 83.
Cf. 1969. Hammatoceras kitakamiense SATO;
TAKAHASHI, Sci. Rep. Tohoku Univ.,
2nd ser., vol. 41, no_ 1, pp. 53-54, pI.
4, figs. 13-16.

Material :-A fragmentary specimen,
GK. G. 2804.
Description :- The whorls enlarge slow1y and consequently the umbilicus is
proportionally wide. The venter has akeel. Ribs are nearly straight andradial. They spring at the umbilicalseam or on the umbilical wall and run
to a point one-fourth of the flank, where
they bifurcate. The primary ribs arestrong and swollen where the bifurcation arises. The secondary ribs are
weak on the middle of the flank andbecome coarse toward the ventral
shoulder. The intercalatory ribs occur
in the middle of the flank. The secondary and intercalatory ribs are nearly
equally weaker than the primary. All
the ribs are not much elevated. They
are weak 'in the) last 30· of the preserved
last whorl.
!vleasurements:- Whorl height of thepreserved last stage: ca. 50 (excluding
the height of keel). The maximum of
the radius: ca. 86 (excluding the heightof keel).
Comparison:- The present specimen isvery similar to the described specimensof Planammatoceras kitakamiense (SATO)(SA TO, 1954, pp. 84-86, pI. 7, fig. 4, pI. 8,
figs. 3 and 5, pI. 9, fig. 4, 1962, p. 67;
TAKAHASHI, 1969, pp. 53-54, pI. 4, figs.
13-16), from northeast Japan, in the modeof ribs, but it is too fragmentary to
identify it definitely with that species.
For the time being I treat it as Planammatoceras sp. ct. P. kitakamiense.
Occurrence :- Loc. 57: 1.
Family Dactylioceratidae HYATT, 1867
Genus Dactylioceras HYATT, 1867
communisType-species:- Ammonites
SOWERBY, 1815 (subsequent designationis pending in 1. C. Z. N.)

Subgenus Dactylioceras HYATT, 1867
Dactylioceras (Dactylioceras) sp. ct. D.
(D.) helianthoides YOKOYAMA
PI. 9, Fig. 91947. Dactylioceras aff. helianthoides YOKOYAMA forma ambiguus MATSUMOTO;
MATSUMOTO in MATSUMOTO & ONO,
Sci. Rep. Fac. Sci., Kyushu Univ., Ceol.,615.

.]u'rassic Toyora Group-Ill

vol. 2, no. 1, p. 26.

Material :-One specimen, GK. G. 2093.
Description : -The
whorls enlarge
slowly and consequently the umbilicus
is proportionally wide. The flank is.convexly rounded. The venter is notobservable, because of the ill preservation. The whorls are ornamented
with primary, secondary and intercalatory ribs. The primary ribs springat the umbilical seam and go on radially.
They are fine, straight and widely interspaced. The intercalatory ribs alternate
somewhat regularly with the primaryribs, and they spring on the middle or.a point inner two-thirds of the flank.
The secondary ribs arise on the middle·of the flank. All the ribs on the outerhalf of the flank are nearly equally
weak. The mode of ribs on the inner
whorls is not well known.
Measurements :No.
GK. G. 2093

D. U.
54.028.0

UjD
0.52

Rnz
30

Comparison:- The present specimen
is closley allied to those of Dactylioceras
helianthoides in the outline. The statistical data concerning the number of ribs
per half a whorl at the same diameter
is not obtained in D. helianthoides but
the number of ribs of the present
specimen may fall in the variation of
D. helianthoides. The present specimen
has secondary and intercalatory ribs on
the outer half of the flank, but D. helianIhoides has these ribs on the ventrolateral area.
The mode of ribs isvariable in D. helianthoides but no-specimen of that species has such longc-secondary and intercalatory ribs.
As only a fragmentary specimen is at
my hand and the difference between thepresent specimen and those of D. helian.thoides is not so dominant as a whole,47

I treat the present specimen underDactylioceras sp. d. D. helianthoides.
Occurrence :-Loc. 13: 1.
Genus Peronoceras HYATT, 1867
Type-species:- Ammonites fibulatus SowERBY, 1823 (subseq uently designated by
BUCKMAN, 1911).
Perolloce1'as subfibulatum (YOKOYAMA)
PI. 9, Figs. 1-6

1904. Coeloceras subfibulatum YOKOYAMA;YOKOYA;"IA, Jour. Coli. Sci., Imp. Univ.
Tokyo. vol. 19, art. 20, pp. 15-16, pI. 3,
Figs. 3-6 .
1947. Coeloceras (Peronoceras) subfibulatum
YOKOYA~IA.; MATSCMOTO in MATSl;,\OIOTO & 0'\0, Sci. Rep. Fac. Sci.,
Kyushu Univ., vol. 2, no. 1, p. 26.
1947. Coeloceras (Peronoceras) subfibulatum
var. illiermedia MATSC:\IOTO & 0'\0;
MATSDIOTO & OKO, ibid., p. 26.
1956 Peronoceras sUbfibulatum (YoKOYA:\IA);
ARKELL, Jurassic Geology of theWorld, Oliver & Boyd Ltd., p. 421.
1962. Peronoceras subfibulatum (YOKOYAMA);
SATO, Mhn. Soc. Ceol. France, no. 94,
p. 59.
1962. Perol1oceras subfibulatum var. intermedia
MATSl;,\IOTO; SATO, ibid., p. 59, sic.
1963. Peronoceras subfibulatum (YoKOYA:\IA) ;TAKAI, MATSU:VIOTO & TORIYA:\IA ed.,Geology of Japan, Univ. Tokyo Press,
p. 83.

Types:- Here one specimen, MM. 7066,
illustrated by YOKOYAMA (1904, pI. 3,
fig. 6) is designated as· the lectotype,which was obtained at loco 1. Threeother syntyypes, MM. 7067, 7068, 7069,
which were also illustrated by YOKOY AMA (1904, pI. 3, figs. 3, 4 and 5, respectively) and were obtained at loco 47,
are referred to the paralectotypes ofthe present species .
Diagnosis:-A species of Peronoc(!7'asHiromichi HIRANO

48

which has fine. somewhat widely interspaced and irregularly arranged ribs
and a comparatively small number oftubercles.
Description : - The whorls enlarge very
slowly and consequently the umbilicus
is proportionally wide. The lateral sideis rounded and the whorl-section is assumed to be elliptical. Ribs are fine, notmuch elevated and widely inters paced.
They spring at the umbilical seam andrun radially. At the middle or outer
one-third of the flank the two ribs arelooped by one tubercle. where two or
three secondary ribs spring and they
cross the venter. Sometimes at middle
or outer one-third of the flank thebifurcation arises without tubercles.
Simple ribs without tubercles are notrare and in some specimens such ribs
are numerous. In one specimen, GK. G.
2177, spines are preserved at the ventrolateral area.
A1easurements : -

No.

o.

MM. 7066
ca. 39.8
MM. 7067
41. 6
GK. G. 2171
36. 2
60. 1
GK. G. 2173
GK. G. 2i75
32.3.

U.

22. 9
23. 2
18. 2
33. 7
14.0

Rn,r (priUjO mary only)
ca. 31
/
0.56
/
O. 50
ca. 28
32
0.56
0.43
32

Remarks:-MATSUMOTO & ONO (1947,
p. 26) described a specimen as Peronoceras subfibulatunl var. inlerilledia, suggesting . that Peronoceras subfibulatumand Dactylioceras helianthoides are morphologically serial through the variety.
In fact one specimen labelled as Peronoceras . subfibulatu71i . var. intermedia issomewhat similar to some specimens ofD.helianthoides.
In P. subfibulatu1ll.
however, the ribs ate looped in pairs toa tubercle, which· is present on the
middle of the flank. and from the tubercle
two or three secondary ribs arise. On

the other hand in D. helian thoides the
tubercles are usually present on theventral shoulder and the ribs are neverlooped in pairs to a tubercle, thoughsuch a bifurcation sometimes occurs.
At least in these characters P. subfibulatum is distinguishable from D. helianthoides.
. Comparison : - The present species issimilar to Peronoceras fibula tum (SowERBY) (MONESTIER, 1931, pp. 43-44) inthe mode of furcation. But the present
species has not so many ribs and tubercles as P. fibulatum, though the rangeof the variations of those characters are
not precisely examined in the two
species. The mode of ribs of P. fibulalulIl seems to be more regular thanthat of the present species.
The present species is similar to
Peronoceras subarmatu17l (YOUNG & BIRD)(How ARTH, 1962, p. 117, MONESTIER. 1931,
pp. 46-47) in the mode of ribs. In P.
subarmalum, however, the ribs are wider
and the tubercles are usually more
dominant than in the present species.
Occurrence :-Loc. 47: 8, lac. 35: 5,
lac. 28": 4, lac. 3: 4, loco 13: 2, lac. 2: L
Superfamily Psilocerataceae
HYATT. 1867
Family Arietitidae HYATT, 1874
Subfamily Arietitinae HY ATT, 1874
Genus Arietites W AAGEN, 1869
Type-species: - Ammonites

bucklandi.

SOWERBY, 1816 (I. C. Z. N. Opinion 305).
Arietites sp.
PI. 9, Figs. 8a-b

Alaterial :-A
singlespecimen, GK. G. 11380.

fragmentary

615.

Jurassic Toyora Group-Ill

Description :- The venter is tricarinate:bisulcate. Two sulci are somewhat wide
:and shallow. The median keel is alittle higher than other two and rounded.
'Six ribs are preserved and are robust.
They are straight on the flank. curving-forward on the ventral shoulder andreach the lateral keel. The interspaceis wider than the space of a rib.
lVIeasurements:- Whorl-breadth:
4.8{inter costae), 5.8.
Comparison :- The present species is·similar to Coroniceras bisulcatum BRU'GUIERE by FREBOLD (1951, pp. 9-10) in
the mode of venter and ribs. Though
FREBOLD referred several specimens(1951, pI. 6. fig. 3, pI. 9, fig. 1. pI. 10. fig.
1, pI. 11, fig. 1, pI. 12, fig. 1, pI. 13, fig.
1) from British Columbia to Coroniceras,,1 think it better to refer them toArietites because of the presence of
two sulci on the venter.
The present species resembles Arietites.bucklandi (SOWERBY) (DONOVAN, 1952, pp.
718-719) in the mode of venter, but inthe former the ribs curve more strongly
forward than in the latter.
Because the present species is represented by only a small fragmentary
specimen, more detailed comparison.cannot be done.
Occurrence:- Loc. 51: 1.

Suborder Lytoceratina HYATT, 1889
Superfamily Lytocerataceae
NEUMA YR, 1875
Family Lytoceratidae NEUMA YR, 1875
Subfamily Lytoceratinae
NEUMAYR, 1875
Genus Lytoceras SUESS, 1865
Type-species:- Ammonites fimbriatus
SOWERBY, 1817 (1. C. Z. N. Opinion 130).

49

LJ'toceras sp. A
PI. 10, Figs. 2-3(Thysano/ytoceras ?)sp. ;in MATSC~-JOTO & O~o,Sci. Rep. Fac. Sci., Kyushu Univ., Ceo/.,vol. 2, no. 1, p. 25.
1956. Lytoceras sp. ; ARKELL, Jurassic Geologyof the World, Oliver & Boyd Ltd., p. 421.
1962. Thysanolytoceras sp.; SATO, Mem. Soc.
Ceol. France, no. 94, p. 58.
1947. Lytoceras

MATSC\IOTO

Material:-Eleven specimens GK. G.
2041-2044, 2049, 2051, 2061, 2064, 1133111333.
Diagnosis :-A species of Lytoceras
which has numerous fine ribs some ofwhich are associated with less elevatedcrinkled riblets. Constrictions are indiscernible or hardly discenible. The
umbilicus is usually wide proportionallyto the diameter.
Description :- The whorls enlarge very
rapidly or moderately but they are
evolute. The whorl-section is ellipticaland widest at the middle of the flank.
The fine ribs spring at the umbilicalseam and go on radially. They aremostly simple but sometimes bifurcationarises on the middle of the flank andintercalatory ribs are rarely present.
There are some ribs in the interval of
two crinkled rib lets. The adoral marginsof the crinkled rib lets are accompaniedby the ribs. Therefore the rib lets are
only crinkled adapically and their adoral
margins are smooth.
The crinkled
riblets are not so elevated but as highas the ribs and wider than the ribs. In
one specimen, GK. G. 11331, 6 weakspiral ribs are discernible in some part(40°).
}\1easurements : No.
GK.
GK.
GK.

D.
U.
G. 2043 35.6 14. 7
G. 2051 32.1 14.0
G. 2064 13. 9 5. 7

U/D H.
Rn~
0.24 12.1
I
O. 44 10.3 ca. 63
0.41
6. 0
I

Hiromichi HIRANO

50

Comparison :-The present species issimilar to Lytoceras eudesianum (D'ORBIGKY) (PUGIN, 1964, pp, 28-33) in theornamentation. but the value of UID islarger in the former than in the latter.
The crinkled riblets of the former are
more numerous than those of the latter.
I am observable only unfavourablypreserved specimens. and the diagnostic
characters are hot so well confirmed ascomparable with that species. Therefore I treat the present specimens under
Lytoceras· sp. A.
Occurrence :-Loc. 9: 5, loco 18E: 2,
loco 21 :. 1, loco 22: 1, loco 28" : 1, loco 30: 1.
Lytoceras sp. B
PI. 10, Fig. 4of the last whorl: ca. 23.
Comparison:- The present species issimilar to Lytoceras jimbriatus (SOWER BY)(ARKELL et al.. 1957. pp. L 194-196) inthe mode of ribs, crinkled rib lets andconstrictions. The present species, however, enlarge more rapidly and has more
numerous crinkled rib lets thanL. fimbriatus (SOWERBY).
The present species is distinguishedfrom Lytoceras sp. A by its absence ofconstrictions or rarity of them. The
whorls of the present species seems toenlarge more rapidly than those of
Lytoceras sp. A.
As the present species is represented
only by one fragmentary specimen, I
treat it tentatively under Lytoceras sp.

B.
Occurrence :-Loc. 18B: 1.

Material :-One fragmentary specimen,
GYU. M. 1019.
Description:- The
whorlsenlarge
rapidly and the umbilicus is proportionally narrow, but are evolute. Three
constrictions are visible in 100° of thepreserved whorl and they are parallelto the ribs. The angles between theconstrictions become small adorally andare 50° and 25°, though the data arepoor to be generalized. Eight ribs arepresent in the earlier interval of 50°
and four ribs in the later one of 25°.
They are radial and mostly accompaniedby the crinkled rib lets, which are alsoradial. The ribs become fine adorally
and the' interspace become narrowadorally. Sometimes bifurcation arises
on the ventral shoulder or at the umbilical periphery. Eleven crinkled riblets
are present in the interval of 50° andfive are in that of 25°. They are often
accompanied by the ribs and therefore
their adoral margins are smooth.
Measurements:- The preserved whorl :ca. 1000. The height of the last stage

Family N arrrrolytoceratidae SPATH, 1927
Genus Audaxlytoceras FUCINI, 1923

Type-species:- Lytoceras audax MENEGHINI, 1881 (subsequently designated by
ARKELL, 1957, p. L 199).
Audaxlytoceras? sp.
PI. 10, Fig. 91947. Lytoceras(Thysano/ytoceras ?)sp. ;in MATSUMOTO & ONO,
Sci. Rep. Fac. Sci., Kyushu Univ., Ceol.,
vol. 2, no. 1, p. 25 (pars).

MATSUMOTO

Material :-One fragmentary specimen,
GK. G. 2059.
Description :-This specimen is verysmall. The whorls enlarge somewhat
rapidly but they are little overlapping
and the umbilicus is somewhat narrow.
The umbilical periphery is abruptly
rounded and the wall is steep. The
surface of the whorl has no ribs but

615.

Jurassic Toyora Group-lIT

some constrictions, which are somewhat
inclined backward on the umbilical wall.
curve forward abruptly at the umbilicalperiphery. then go forward, and nearlyat the middle of the flank moderately
recurve backward. The angles between
the constrictions become smaller in accordance with growth, ca. 55° at diameters from 11.9 to 12.7 mm., ca. 50" atdiameters from 12.7 to ca. 14 mm. andca. 30° at diameters from ca. 14 to ca.
15 mm. No other ornamentations are
discernible on the surface of the whorls.
fl1easurements : No.
GK. G. 2059

D.
ca. 15

U.
ca. 4

UID
O. 25

H.
5. 5

Comparison :- The present species issomewhat similar to Audaxlytoceras
dorcadis MENEGHINI (MONESTIER. 1931,
pp. 10-11), from south France. in theevolute and smooth shell with someconstrictions. As far as the observablehalf a whorl is concerned, the frequencyof the constrictions is nearly equal toeach other. The former, however, isdistinguished from the latter by theconvex constrictions.
Occurrence:- Loc. 36?: 1.

Suborder Phylloceratina ARKELL. 1950
Superfamily Phyllocerataceae
ZITTEL, 1884
Family Phylloceratidae ZITTEL. 1884
Subfamily Calliphylloceratinae
SPATH, 1927
Genus Calliphylloceras SPATH. 1927
Type-species:- Phylloceras
ZITTEL. 1869.

disputabile

Calliphylloceras sp. A

51

PI. 10, Figs. 5-6

1947. Phylloceras(Calliphylloceras)
sp. ;in MATSUMOTO & 0:"0,Sci. Rep. Fac. Sci., Kyushu Univ., Ceol.,
vol. 2, no. 1. p. 25.
1956. Calliphylloceras d. nilssoni (HEBERT);
ARKELL, Jurassic Geology of the World,
Oliver & Boyd Ltd., p. 421.
1962. Calliphylloceras d. nilssoni (HEBERT) ;SATO, Mbn. Soc. Ceol. France, no. 94.
p. 58, [sic].
1963. Calliphylloceras sp.; TAKAI, MATSC'\IOTO & TORIYA~'IA ed., Geology ofJapan, Univ. Tokyo Press, pp. 83-84.
M.·\'TSL·~IOTO

Material:-Six specimens, GK. G. 2017,
2021, 2022, 2024. 2029, 2036.
Description:- The
whorlsenlarge
rapidly and consequently the umbilicus
is very narrow. They are involute_
Numerous fine ribs are discernible on
the whorls.
They are parallel withconstrictions.
The constrictions aremarked as furrows on the internal mould.
They are nearly straight or concave
adorally and somewhat prorsiradiate
but the last one at the diameter of 3556 mm. is very prorsiradiate. The angles
between constrictions slightly decreaseadorally. In one specimen, GK. G. 2029,
the angles are 60°, 60° and 50° at the
maximum diameter of 44.9 mm.
Inother specimen. GK. G. 2017, they are
60° and 50° of which the maximum
diameter is ca. 56 mm. Often both sidesof the furrows (=constrictions) areswollen as ridges. Suture is exposed atdiameter 21 mm.
The first lateral lobe is narrow, deep
and tripartite, and the second laterallobe also is tripartite. The first lateralsaddle seems to be triphyllic and thesecond lateral saddle is triphyllic.
Afeasurements : No.
D.
U.
H.
U/D
GK. G. 2021 35.8 ca. 6 ca. 19.8 ca. 0.17
GK. G. 2029 44.9
7. 1
19.7
O. 16

52

Hiromichi HIRANO

Comparison :- The present species issimilar to Calliphylloceras
nilssoni(HEBERT) (GURICH, 1933) in the mode of
volution and constriction. The former,
however, has a narrower first laterallobe and simpler suture than the latter.
As the described specimens are too
poorly preserved for exact comparison,for the time being I treat them as
Calliphylloceras sp. A.
Occurrence :-Loc. 18: 3, loco 53: 1, loco
55: 1, unknown loc.: 1.

weaker constrictions.
Calliphylloceras nilssoni (HEBERT) has
nearly straight but stronger constrictions
than the present species.
As the present species is represented
only by two fragmentary specimen, I
treat it tentatively under Calliphylloceras
sp. B.
Occurrence:- Loc. 4: 1, loco 27: 1.
Genus Holcophylloceras SPATH, 1927
Type-species:- Phylloceras
neum NEUMA YR, 1871.

Calliphylloceras sp. B

mediterra-

PI. 10, Fig. 7

Material:-Two specimens, GK. G.
11334, 11335.
Description:- The
whorlsenlarge
rapidly and are involute .. Consequently
the umbilicus is very narrow. Venteris assumed to be rounded. Umbilicalperiphery is rounded and the wall israther steep. Numerous fine lirae are
discernible on the surface of the shell.
They are fine, nearly straight and somewhat prorsiradiate. Constrictions arevery weak and obscure. They areparallel with the fine ribs. In one
specimen, GK. G. 11335, an angle between
constrictions is ca. 40 in the stage ahalf whorl younger than that withdiameter of 78 mm. Suture lines are
partly visible. Lateral saddle seems tobe triphyllic but the details of thesuture are unknown.
Measurements :0

No.
D.
GK. G. 11334 ca. 71
GK. G. 11335 ca. 89

Holcophylloceras sp.
PI. 10, Fig. 81947. Phylloceras(Holcophylloceras)
sp. ;in MATSUMOTO & ONO,
Sci. Rep. Fac. Sci., Kyushu Univ., Ceol.,
vol. 2, no. 1, p. 25.
1956. Holcophylloceras sp. ; ARKELL, Jurassic
Geology of the World, Oliver & BoydLtd., p. 421.
1962. Ho/cophylloceras sp. ; SATO, Mem. Soc.
Ceol. France, no. 94, p. 58.
1963. Holcophylloceras polyolcum (BENECKE) ;TAKAI, MATSUMOTO & TORIYAMA ed.,Geology of Japan, Univ., Tokyo Press,
p. 83.
MATSUMOTO

,

U.
ca. 6
ca. 9

H.
ca. 41
ca. 48

UjD
0. 09
0. 10

Comparison:- The present species issimilar to Calliphylloceras sp. A in themode of volution, but is distinguishedby the straight fine ribs and much

Material :-A specimen, GK. G. 2016.
Description :- The
whorls enlarge
rapidly and are involute. The umbilicus
is very narrow. Low ribs are present
on the outer half of the whorl. They
are weak and parallel with constrictions.
Six constrictions are present on the preserved 150 of the last whorl, of which
two are comparatively clearer and aremoderately biconcave. They start fromthe umbilical seam and proceed ada pically. At about inner one-third of theflank, they curve adorally and run
straightly. They recurve adapically again
0

615.

Jurassic Toyora Group-III

at about outer one-third of the flank andfurthermore they curve adorally near
the venter.
Two constrictions arevisible as furrows and their adoral sideor adapical side is swollen. Four constrictions are incompletely preserved
and are manifested as ridges.
Measurements :Height of the whorl of the preserved
last stage: 69.3 mm.
Comparison :- The present species issimilar to HOlcophylloceras aft. polyolcum(BENECKE) (SPATH, 1927, pp. 60-63), from
Cutch, and Holcophylloceras mediterraneum (NEUMAYR) (SPATH, 1927, pp. 5860), from Cutch, in the mode of vol uti on,
ribs and the abundance of constrictions,but is distinguished by its gentle curvature of constrictions.
The present species resembles Holcophylloceras guettardi (RASPALL) (ARKELL
et aI., 1957, p. L 190), from France, but
the constrictions occur more frequently
and curve more strongly in the former
than in the latter.
Occurrence :-Loc. 59: 1.
Family ]uraphyllitidae ARKELL, 1950
Genus Harpophylloceras SPATH, 1927
Type-species :-Ammonites eximius HAUER, 1854
Harpophylloceras? sp.
PI. 10, Fig. 1

1947. Rhacophyllites (Harpophylloceras ?) sp. ;MATSUMOTO in MATSUMOTO & 0]';0,Sci. Rep. Fac. Sci., Kyushu Univ., Ceol.,
vol. 2, no. 1, p. 25.
1956. juraphyllites sp.; ARKELL, Jurassic
Geology of the World, Oliver & BoydLtd., p. 421.
1962. juraphyllites sp.; SATO, Mem, Soc.
Ceol. France, no. 94, p. 58.

53

1963. juraphyllites sp. ; T AKAI, MATSt::>IOTO& TORIYAMA ed., Geology of Japan,
Univ. Tokyo Press, p. 84.

Material :-A small specimen, GK. G.
2020.
Description:- The
whorlsenlarge

rapidly and are involute. Consequently
the umbilicus is narrow. The ventral
shoulder is rounded, the flank is convex
and the umbilical periphery is rounded.
Therefore the whorl-section is assumed
to be elliptical. The venter has a thinand low keel. A sulcus is not present.
The surface of the shell seems to beornamented with numerous and radial
fine ribs. The fine ribs, however, areobscure because of the unfavourable
preservation. Two constrictions arenearly straight and rectiradiate. Lateralsaddle of the suture is diphyllic.
lv/easurements :No.
GK. G. 2020

D.

U.

H.

12.9

2.8

6.0

U/D
0.22

Comparison :-The present species issimilar to Harpophylloceras eximiwn(HAUER) (ARKELL. 1957, p. L 191) in themode of constrictions. The degree of
involution of the former seems to resemble that of the latter, but this iscompared between specimen of dissimilar size.
As only a small, unfavourably preserved specimen is at my disposal, moredetailed comparison is impossible.
Occurrence :- Loc. 52: 1.

Zonation and correlation
A. GeneralAmmonoid fossils are very abundantin the Nishinakayama Formation, lessabundant in the Utano Formation andrare in the Higashinagano Formation.
The Higashinagano Formation is incom-

54

Hiromichi HIRANO

petent, the Utano Formation is difficultfor precise zoning because of a small
number of specimens and only the Nishinakayama Formation is competent for
reliable zoning. The succession of ammonoid fossils in the Nishinakayama
Formation is well exposed along a small
stream, Sakuraguchi-dani, where theframework of zoning is established. The
zonation of the Nishinakayama Formation by MATSUMOTO & ONO (1947) in thenorthern part is acknowledged also byme but that in the southern part is revised (Fig. 4). The stratigraphic and~eographic distributions of ammonites
and some other characteristic fossils are
mentioned below in ascending order.
The stratigraphic position of each fossil
locality is shown in the columns (Fig.
2 in Part II).
The correlation between two regions
should originally be done by the same
species in strict sence but the same
species is rare between the Toyora andthe standard area of Europe. Therefore
I use the similar species to the Toyora
species and the ammonoid assemblages
for the correlation in this article.
The geographic variation is only able
to discuss based upon the study ofvariation in each population. No one
has studied on the variation of ammonoids in the standpoint of population
concept since the description of ammonoid species began. Therefore today
no one can distinguish or identify logically a Japanese ammonite from or as
a European one. Above all the variationof a local population should be clarified.
I could clarify the variation of thenumber of ribs in some species but I
could not treat other characters becauseof the unfavourable preservation of thematerial. Therefore the contents described and discussed in this article are
the record of the characteristics based

upon the appearance of material. At
first study of ammonites in the standpoint ·of population concept should bedone by the use of the favourably preserved material (In Japan favourablypreserved material cannot be obtained).

B. The Higashinagano Formation
No ammonites were collected from theMember Nbc and only Pentacrinus sp.
was collected from its upper part. Accordingly the age of the Member Nbc
is not precisely determined. The sedimentary features suggest that it did nottake so long time for the deposition ofthis member and therefore its geologicalage may be close to the superjacent
Member Ncs.
Various kinds of bivalves, gastropods,
scaphopods, ammonoids, brachiopods,
corals and crinoids have been reported.
Bivalvia and gastropods from Member
Ncs were described by HAYAMI, who
named them as Cardinia toriyamai faunule(1958, 1959, 1960a, 1961, 1962). As to theammonoids Arietites sp. and Harpophylloceras? sp. have been obtained fromthis member. The corals are Chomatoseris cyclolitoides (Y ABE & EGUCHI, 1933)
and an isastraeid, and the crinoid is
Pentacrinlls sp. (HAY AMI, 1961). As regards the age, it is said that several
pelecypods are identical with or closely
related to some Liassic (properly lower
Liassic) species hitherto known inEurope, northern Africa or Canada andthat no Triassic (inclusive of Rhaetic)
element is found in the fauna (HAY AMI,
1959, p. 37). On the basis of Arietites
sp. I regard this member as lower Sinemurian.
The geological age of the Member Nssvaries from place to place. At Higashinakayama, the age is referred to lower
Domerian by the occurrence of Amaltheus
sp. d. A. stokesi and Arieticeras sp. aff.

615.

Jurassic Toyora Group-III

A. apertum (Fig. 2d in Part II). In thenorthern area, e. g., Higashinagano and
Sakuraguchi-dani, the age of this member
is considered at least in part as upper
Sinemurian, because a Domerian ammonoid is known from the basal part of
the Member Nm and a lower Sinemurian
ammonoid is known from the lower partof the Member Ncs.
The age of the Member Nsh varies
locally.
In the northern area, e. g.,
Higashinagano and Sakuraguchi-dani,
this member is assumed to be uppermost Sinemurian stage. At Nishinakayama-Higashinakayama district, not only
the Nsh but also the lower part of the
Nss is referred to Domerian substage.
No fossil indicating an Carixian age has
been obtained. The sediments of thisage is regarded to have been eroded
away, because there is conglomerate at
the base of the Nishinakayama Formation in the southern district.
C.

The Nishinakayama Formation
Various kinds of ammonoids have beenobtained from the Member Nm andpartly from Member Na and Nss at
about fifty localities. Zonal frame isestablished in the sequence along the
Sakuraguchi-dani (Fig. 2a in Part II. Fig.
1) and three zones are confirmed by the
supplementary sequence along the Kogodani (Fig. 2c in Part II), the Anda -dani(Fig. 2b in Part II), the River Era, theRiver Motoyoku and the River Sakota.
The three zones are discernible in thenorthern two-thirds of the studied area.
They are the Fontanelliceras fontanellense Zone, the Protogrammoceras nipponicu/1l Zone and the Dactylioceras helianthoides Zone in ascending order as
mentioned below.
Fontanelliceras fontanellense Zone:
This zone is represented by Fontanelliceras fontanellense and about 25 to 50

55

m. in thickness. In addition, Canavariajapon ica. C. d. sicula. Arieticeras d.
pseudocanavarii, A. aff. apertu11l, Paltarpites toyoran us, P. paltus, P. aff. Platypleurus, Fuciniceras primordium, F. cL
llormanianum, Dactylioceras helianthoides
D. (Prodactylioceras) aff. italicum, Amaltheus d. stokesi and Calliphylloceras sp_
A are found from this zone. The lower
boundary of this zone is marked by theappearances of Ama/theus, Arieticeras.
Canavaria and/or D. (Prodactylioceras)
and is in oblique relation with lithostratigraphic unit (Fig. 4). The index, thefirst four genera and Amaltheus are
known as the indices of Domerian substage. Fuciniceras is usually known in
Domerian substage and questionably in
Whitbian substage (ARKELL, 1957, p. L
258). Dactylioceras has so far been knownin Toarcian and Calliphylloceras fromlower Jurassic to lower Cretaceous_
Accordingly, it can be said that the assemblage of this zone indicates Domerianage. and more detailed discussion is
mentioned below.
FOiltanelliceras fOlltanellense is known
from MONESTIER's subzone c (=theGiiJIJOSUS Subzone. DEAN et aI., 1961) inAveyron (MONESTIER, 1934) and known
from the equivalent of the Spinatumzone in Alta Brianza (VENZO, 1952)_
Arieticeras pseudocanavarii and A. apertum are known from MONESTIER's subzone c (=the GibboSliS Subzone, DEAN
et aI., 1961) in Aveyron (MONESTIER.
1934). A species is comparable with
A17laltheus stokesi. which is the index of
the lowest subzone of the Margaritatus
Zone. A species is comparable with
Fuciniceras Ilormanianum, which is
known from the Davoei Zone to the
J\![argaritatus Zone in Haut Atlas (DRESNA Y. 1963). from equivalent of the lower
Margaritatus Zone in Huescar (DUBAR
et aI., 1967) and from the Stokesi Zone

Hiromichi HIRANO56
o k~loe. 28

27

26

25

23
22

in'

~Ul

21

20
19

.
c
o

18

N

17

on

.\'!

16

u

~

10m.

~

"E

~

o
Nsh

Hildoceratidae

Oactyti~r~tidae' l:y'toceratidae
Phylloceratidae

Fig. 1. The zonal framework founded on the sequence in the Sakuraguchidani.
A black square corresponds to the locality number in the left side, which refers to
the number in systematic description. The number beside the black square indicatesthe number of individuals.

(GECZI, 1970) in

Hungary. A species isvery similar to Dactylioceras (Prodactyliocems) italicum, which is known fromthe equivalent of the Subnodosus Subzone in Aveyron (MONESTIER, 1934) andfrom the DaL'oei Zone in Hungary(GEczI, 1970).
On the basis of these correlation, theFon tanelliceras jontal1ellense Zone isnearly correlated with the Margaritatus
Zone and a part of the Spinatum Zone.
The basal part may be correlated withthe base of the Stokesi Subzone and its
upper part may be correlated with thelower Spinatum Zone.
Protogmmmoceras nipponicum Zone:
This zone is represented by Protogrammoceras nipponicum and about 50 m. in

615.

57

Jurassic ToyoTa Group-III

thickness. Protogrammoceras olloi. P.
yabei. Lioceratoides yokoyamai. L.
matsumotoi, Harpoceras chrysallthe~mum, H. olwdai, H. aff. exaratum, H.
(Harpoceratoides) nagatoensis. Fuciniceras nalwyamense, Dactylioceras heli~anthoides, D. ct. helianthoides. Lytoceras sp. A, L. sp. B and Caliiphyllo~
ceras sp. B are obtained from this zone.
Protogrammoceras, Fuciniceras, Dacty~
lioceras and Lioceratoides are known
in upper Pliensbachian and the first
three genera are known also in lower
Toarcian. Harpoceras and Harpoceratoides are known only in lower
Toarcian. Lytoceras and Caliiphylioceras are known not only in the lower
Jurassic but also in the lower Cretaceous. It can be roughly said that
this zone indicates from the upper
part of Domerian to the lower part of
Whitbian. The more detailed cor~
relation is discussed below
Protogrammoce1'as is known fromthe Stokesi Subzone and the Sub1/odosus
Subzone in Aveyron (DEAN et aI., 1961).
Protogrammoceras nipponicum, theindex of this zone, is very similar toP. celebratum, P. marianii and P. bo~
Ilareliii (see the description).
P.
celebratum, P. marianii and P. bonarellii
are known from Alta Brianza with
Amaltheus margaritatus (VENZO, 1952)
and P. celebratum is the index of theMargaritatus Zone in south Europe.
In Portugal, Protogrammoceras ismainly known from lower Domerian.
P. bonarellii is commonly known and.

~~--. . ..

u

c

<:i.

- a:
0

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.

~ c

<II

u

c

C

.~

u
.~

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-;;

u

c:

0

;;:, E

~
l:

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e

P

M

e

P

M

e P

P

u
0

0

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e P

P
P

P

<II

-.: -"c

c

u

.c: "

<:i.

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U

<!l

c

0

u

0

N

"'

~- - -- __I

P,M

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.!:

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0

Q

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-

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,.,

~

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I

P

<!l

-

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e A

E

-

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<II

-

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eo!

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0-

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,.,

e P M
e P M

e A

U

-

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5

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~

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u'"

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~

.c:

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(;

C

-.:
.
,;
".. ." '" ".
'"
" .
'" '"
.c: ,,; .,,;.,;'" '" ..
. '" >:. g.. .. " :;; i';' '"... ce- ~ ~ " 2"'"
3- .. ..
il:
'"
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<II

.'"

-.:'" i:·0"" CD -.: '"<:i. -.:'"-.:.c' c:

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-

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1- 111I

Fig. 2. The detailed mode of occurrence of fossils and lithofacies observed at the river mouth of theMotoyoku (loc. 4). The black squareindicates the part which each fossil
occurred. The number beside the blacksquare indicates the number of individuals.

100

em.

a

e P

P

e P
e A

P
P

~" 1-11
--

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<II

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58

Hiromichi HIRANO

restricted in the Margaritatus Zone inPortugal (MOUTERDE; 1967). P. celebratum and P. bonarellii are known fromthe Stokesi Zone in Hungary (GECZI,1970). P. d. nipponicum is known with
H. (Harpoceratoides) d. contectens. Cf.
Canavaria excellens, C. d. morosa, Cf. P.
bonarellii, P. d. marian ii, Arieticeras d.
domarense, Cf A. algovianum, Liparoceras
cf. bechei and Leptaleoceras dickinsoni
in Oregon (IMLAY, 1968).
Fuciniceras is known from the Stokesi
and the Subnodosus Subzone in Aveyron(DEAN et al., 1961). Fuciniceras nakayamense is abundant only in the P. nipponicum Zone and is also the useful index
of the zone. F. nakayamense is similar
to F. boscense and F. falciplicatum anda little to F. lavinianum (see the description). F. lavinianum is known fromthe lowermost part of Domerian in
Huescar, Spain (DUBAR et al., 1967). F.
falciplicatmn is known from the Stokesi
Subzone in Hungary (GECZI, 1970). F.
boscense is known from the Margaritatus
Zone in Aveyron (MONESTIER, 1934).
As mentioned above, the foreign
species to which the two species, P.
nippnicum and F. nakayamense, aresimilar are known in lower Domerian.
At the same time, however, Toarcian
genera such as Harpoceras and Dactylioceras are commonly known in this zone.
Harpoceras is the characteristic genusof the Falcifer Zone in Europe (DEAN
et al., 1961). Dactylioceras helianthoides
is similar to D. crassiusculosum and D.
gracile, which are known from the
Bifrons Zone in Aveyron (MONESTIER,
1931).
I think the Protogrammoceras nipponicum Zone could be correlated with theage from upper Domerian (the Spina tum
Zone) to lower Whitbian (the FalciferZone) on the basis of these comparison.
Dactylioceras helianthoides Zone: This

zone is characterized by the abundanceof Dactylioceras helianthoides, Harpoceras
chrysanthemum and H. inouyei, and thelower boundary being drawn immediately above the disappearances ofProtogrammoceras and Fuciniceras. The
upper boundary is drawn just below
the Member Na. Harpoceras chrysanthemum and H. inouyei appear from theuppermost part of the P. nipponicum
Zone but the occurrences in the partare very rare and usually appear after
the disppearances of Protogrammoceras
and Fuciniceras. H. d. mulgravium, H.
d. exaratum, L. yokoyamai, L. matsumotoi,
Hildoceras sp., Peronoceras subfibulatum
and Calliphylloceras sp. B are known inthis zone.
Harpoceras, Hildoceras, Peronoceras
and Dactylioceras (s. str.) are known as
the lower Toarcian genera (ARKELL,
1957) and Harpoceras is the characteristic genus of the Falcifer Zone (DEAN
et al., 1961). Hildoceras is known fromthe Bifrons Zone. Peronoceras subfibulatum is similar to P. fibulatum, whichis the index of the Fibulatum subzone.
No species which indicate the age later
than the Fibulatum subzone are known
from this zone and therefore I thinkthe uppermost part of this zone is correlated with a part of the Fibulatum
Zone. The basal part of the D. heliantho ides Zone is not clearly and precisely
correlated with the European standard.
No parts of this zone and the P. nipponicum Zone could be correlated with thestandard Tenuicostatum Zone. The basal
part of the zone could be correlatedwith a part of the Exaratum Subzone
in consideration of the assemblage as
mentioned above.
Dactylioceras helianthoides sporadicallyoccurs in the Member Na. This member
is assumed to be Whitbian considering
the occurrence of D. helianthoides and615.

.]~trassic

Toyora Group- [II59

Table 1. Range chart of Domerian and Whitbian ammonite species in the Toyora
Group and zonal correlation with the European standard zones and subzones.
- ____~u~tagel

Domerian~

Whitbian----1---- ____ ----------:--------1
European Standard
Zone and Subzone

:;:
;::<

'"
"

'"

;::<

''<;'
CI)

""
:::::-t-..""

k.

'"""

.",

~

"

::t::'"
F. fontane-

I llense Zone

P. nipponicum
Zone

"

....
...,

'"

"-l

.~

t:Q

~

....

""

~

"

~
k.

""

;::

":;:
:;:

Cl

c..J

:;:

t"

~
~

k:

D. helianthoides
Zone

:...

'";::<
.§
...."
'"

t:Q

Na I Up--- --------------------------1

Amaltheus cf. stokesi
Arieticeras d. pseudocanavarii
A. aff. apertum
Canavaria japonica
C. d. sicula
Fontanelliceras fontanellense
Paltarpites toyoranus
P. paltus
P. aff. platYPleurus
Fuciniceras primordium
F. nakayamense
F. cf. normanianum
Protogrammoceras
nipponicum
P. yabeiP. onoi
Lioceratoides yokoyamai
L. matsumotoi
liarpoceras okadai
li. d. exaratum
li. chrysanthemum
li. inouyei
li. d. mulgraviumli. (liarpoceratoides)
nagatoensis
liildoceras sp.
Dactylioceras (Prodactyliocer-as)· aff. italicum
D. (s. s.) halianthoides
D. d. helianthoides
Peronoceras subfibulatum~....Cl

~

~

:;:

2

'"
;::

'-'

"""....
'"'"

Species

....

;::<

.~

~

--I

---

60

Hiromichi HIRANO

the ammonite assemblage of the overlaying Member Up. These discussions
on correlation are concisely shown as arange chart in Table 1.

Geologicalage
Callovian

~j
\

Time
unit

Lithos tratigraphic
unit
Kwanmon Group-, ,The Utano Formation
Pseudolioceras sp., Grammoceras aff.
obesulIl, Phymatoceras toyoranum, Calliphyllocems sp. A and Bositra sp. are
known from the Member Up. The lower
limit of the Variabilis Zone is definedby the appearance of Phymatoceratinae
in abundance and the upper limit isdrawn immediately below the firstoccurrence of Grammoceras (DEAN et aI.,
1961). The lower limit of the Thouarsense Zone is defined by the sudden appearance of Grammocems and the upperboundary is marked by the appearanceof Phlyseogrammoceras.
In Toyora.
Grammoceras and Phymatoceras appear
simultaneously. The Member Up could
be roughly correlated with the Variabilis
and the Thouarsense Zones considering
the above mentioned ammonites assemblage.
Phymatoceras sp. is known from theMember Ub and its age is considered to
be Yeovilian.
Planammatoceras
d. kitakamiellse,
Dumortieria ? sp. and Calliphylloceras sp.
A are known from the Member Uh. In
addition to the discrepancy of appearance and disappearance of genera between Toyora and Europe, the contentsof ammonite assemblages in the Utano
Formation, especially in upper part thanthe Member Up, is poor. Consequently
the correlation in zonal level is unable
to be done. The age of the Member
Uh may be referred to a part of Yeovilian and a part of lower Bajocian (s. I.).
The discussions on correlation of thisgroup with European standard mentioned
above are concisely shown in Fig. 3.
Harpophylloceras sp. and Inocemmus
D.

BathonianUt
120-650m.
180mUhBajocian- - -,,,
90mUb
Aalenian,,,
120m.Up, , - - -IOOm. Na
c Yeovilian ,,
I

'"

D.h.

I

0

~

0
I-

!l

:J

&

'"

E

'"

Zone

Whitbian.0
III

Carixian

a:

""

V

Sinemurian,
Hettangian

Nm

Zone

120-150m.

Zone

-

~
~
50m

\
\

\

Paleozoic- P. n.
- F. f.

0

'c"

0

c

:>.

~
E Domerian

.~

EO
IL.

';Om.

Nbc

",.
.><

'c"

.c
III
Z
r--

E

IL.
0

c

'"
'"
'"

Cl

.!::
.c
III

.~
:I:

Sangu~o~k~amorphic .

Fig. 3.
Modified stratigraphic seQuence of the Toyora Group and its correlation with international stage andsubstage.

utanoensis are known III the upper
horion of the Member Ut. It is said.
that I. utanoensis is very similar toBathonian I. kystatymensis KOSCHELKINA r
1960 (HAY AMI, 1962). I also think thatI. utanoensis KOBAYASHI, 1926 is hardly
distinguishable from Retroceramus kyst-atymensis from the Bathonian of east
Siberia (KOSCHELKINA, 1963, pp. 150-151)_
This member is supposed to be Bathonianby this fact. but the accurate age ofthe top of this member is not determinable.

615.

Jurassic Toyora Group-III

Characteristics of the Toyora faunas
A. Assemblage
Ammonite fossils are rich in the
middleform ation and partly common in
the upper formation. The middle and theupper formations are somewhat monotonous black shale without any abruptchange of lithofacies and biofacies.
Among various ammonoid species of
the Toyora faunas, Dactylioceras helianthoides shows the longest vertical range
and is accompanied by many species of
Domerian and Whitbian.
Protogrammoceras nipponicu7Il is rarely
accompanied by P. onoi and the ratioof the numbers between them is 1: 4 to1 : 2 except the lowest part at the studied
outcrop (Fig. 2). P. yabei is accompaniedby P. nipponicum, but the number ofindividuals of the former is always small.
Canavaria japonica coexists with FOIltanelliceras fontanellense, and both arelarge in the number of individuals (e. g.,
51 of C. japonica, 30 of F. fontanellense).
Fuciniceras nalwyamense coexists with
P. nipponicul7l and both are large in thenumber of individuals (e. g., 11 of F.
nakayamense, 21 of P. nipponiculIl).
Generally speaking, in a bed with
Canavaria, Fontanelliceras and Fuciniceras, also Arieticeras occurs commonly
in many parts of the world. For somereasons Arieticeras is poor in the Toyora
Group. Harpoceras has hitherto been
known as a lower Toarcian genus but
Harpoceras okadai occurs with some
Domerian species.

B. Comparison with other faunas

of
japan
The Liassic ammonoids are known
from the Shizukawa Group of northeast
Japan and the Kuruma Group of central
Japan.
In the Shizukawa Group no
Pliensbachian ammonoids are known and61

the Toarcian is indicated by Harpoceras
okadai. Hosoureites ikianus, Grammoceras
sp. and Phymatoceras sp. (SATO. 1956,
1962; TAKAHASHI, 1969). Harpoceras,
Grammoceras and Phymatoceras are
genera occurring in the Toyor-a.,fauna,
but as regards the specific rank only
Harpoceras okadai is common to the
Toyora fauna. In the Bajocian Member
Hh of the Shizukawa Group, Planammatoceras kitalwmiense (SA TO) is known anda comparable species is known in theMember Vh of the Vtano Formation.
From the Kuruma Group, Amaltheus
sp. and Canavaria sp. are known as
Pliensbachian ammonoid. Toarcian isindicated by only Grammoceras sp.
(KOBA Y ASH! et aI., 1957). The Toyora
ammonoid faunas are characterized anddistinguished by the eminent Mediterranean elements in the Domerian substage from other fauna in Japan. The
common ammonoid species are veryrare between the Toyora faunas andother faunas of Japan for some reasons_
Palaeogeography, palaeocurrent and.
faunal province were discussed in detailby SA TO (1956, 1960). Amaltheus fromthe Toyora Group is newly described
and therefore the palaeocurrent drawn
by SA TO (1960) should be partly revised.
if palaeocurrent was really the principal
factor to control the distribution ofammonite fauna.

C. Comparison with some faunas of otherregionsC-1. The Toyora fauna in Domerian
substage
From the Nishinakayama Formation
the following 20 species of 11 genera
are ascribed to Domerian substage.
Arieticeras cf. pseudocanavarii, A. aff.
apertum, Canavaria japonica, C. cf. sicula,
Fontanelliceras fontanellense, Paltarpites
toyoranus, P. paltus, P. aff. platypleurus,

62

Hiromichi HIRANO

Lioceratoides yokoyamai, L. matsumotoi,
Fuciniceras primordium, F. nakayamense,
F. d. normanianum, Protogrammoceras
nipponicum, P. yabei, P. onoi, Harpoceras
okadai, Amaltheus d. stokesi, Dactylioceras helianthoides, D. (Prodactylioceras)aff. ita./icum. This assemblage is characterized by the predominance of Hildoceratidae in both number of species andthat of specimens. The fauna is characterized by the Tethyan elements, namely most of the species have close affinities to the species of the Tethyan
Realm as mentioned in the description.
According to HALLAM (1969), the northern boundary of the Tethyan Realmis roughly corresponds to the line fromthe Alpine fold belt, via eastern Siberia
and Japan to northern California. The
cause of the separation of ammonite
faunas between the Tethyan and the
Boreal Realm has not been clarified,though some speculations and regional
studies have been done by many students. I list up upper Pliensbachianammonite genera from the world, paying attention to localities of the Mediterranean region and compare themwith the Toyora fauna concerning thesimilarity by the method of SIMPSON'S

formula:N1~N2 100 (N1~N2, Numberof genera of each fauna; C, number ofcommon genera in two faunas).
The computed result (Table 2) indicates that the Toyora fauna has a similarity in the highest degree to theTaormina fauna of Sicily Is. On theother hand, the Taormina fauna hassimilarity to the Toyora fauna in higher
degree than to any other faunas. Huescar fauna in Spain is the second and
S. Pedro fauna in Portugal is the third
in the degree of similarity to the Toyora
fauna. These are said to be representative faunas in the Tethyan faunal

Table 2.

Faunal resemblance in Domerian.

!

6
i
9 401

Yorkshire Coast
Dorset Coast

! I!

I

I.

i

I

I

I

~~~~---=:~~W,:I=FFF:=I':.rl~tedicetOn!: -=-_il~:tHl~'042 ,\ _~[~l~':.~ ·l'-__:----=-, ~I~f' ~':~ :~'~~ ~~i601 T_-~
Taormina

S.PedroHaul Atlas

6

lo3i' 21 057 50 27 ! ' ! : ' 1---'-a 42 30 19 45 53 '0 38 52 76

.-

I .-

7 -'612520130 42103 53,50 33 48!. __ _

ill'

E.O •• goo, 9 24136 01564538521575349461
Sr. Columbia & s. ~u~~ -.!~g~~_ 20 13 25135 42 38i~
Toyora11 4713014158523371. 6064

:1-

62i5614a153"

province of Domerian substage. On thecontrary, in Yorkshire Coast, Dorset
Coast and Hebrides Is. the diversitiesof their faunas are low, and also thedegrees of similarity to the Toyora
are low, though Yorkshire Coast fauna
is somewhat higher than the other two.
Recently, as to the upper Pliensbachian faunas of North America, somestudies have been published. Amongthem eastern Oregon fauna (IMLAY, 1968)shows some affinity with the Toyora
fauna, and some species are actuallycompared with the Toyora species. In
the present quantitative treatment, however, the eastern Oregon fauna does
not indicate high similarity to the
Toyora fauna.
The eastern Oregon
fauna, however, has higher similarities
to the Aveyron, Alta Brianza and Huescar faunas. It is caused by the higher
diversity of eastern Oregon fauna than
the Toyora fauna. The British Columbia
to southern Yukon fauna (FREBOLD, 1970)
has some affinity with the Toyora fauna,though it has not high diversity andhas some boreal elements. The British
Columbia to southern Yukon fauna showsa high similarity to the Bou-Rharraf
fauna in Haut Atlas at the same time.

615.

Jurassic Toyora Group-III

There are various degrees of diffe-renee among the faunas of the Tethyan
Realm and a certain fauna is not always
similar to ·others. The difference isassumed to be caused by difference of
local condition besides palaeogeographical circumstances. Therefore I researched the lithography of the localities-in order to know a part of differenceof local condition. In general survey,
calcareous sediments such as limestone,marl and marly limestone are rich in
1:he Tethyan faunal Realm as HALLAM(1969) noted. As to Toyora, eastern-Oregon and British Columbia to southern
Yukon, however, calcareous matter israre or absent and clastics predominate.
·Some taxa which occur exclusively in
non-calcareous strata in the Tethyan
faunal Realm are some Liparoceratidae·(e. g., Liparoceras, Becheiceras, Metacymbites), Harpoceratinae(F ann inoceras,
Whitbyiceras), Arieticeratinae (Leptaleoceras) and Phylloceratidae (Tragophyl.loceras-with question. Holcophylloceras).
These data of faunas outside Japan
care based on the following references.
For the Brescia fauna BETTONI (1900),
the Haut Atlas oriental fauna DRESNA Y-(1963), Huescar fauna DUBAR et aL (1967).
British Columbia to southern Yukon
fauna FREBOLD (1970), Monte di Cetona
fauna FUCINI (1901, 1902), Taormina
fauna FUCINI (1923-28). Yorkshire fauna
HOWARTH (1955), Hebrides Is. fauna
HOWARTH (1957), eastern Oregon fauna
IMLA Y (1968), Aveyron fauna MONESTIER(1934), S. Pedro fauna MOUTERDE (1967)
and for the Alta Brianza fauna VENZO,(1952).

C-2. The Toyora fauna 111 Whitbian
substageIn the Toyora Group the following 15
species of 7 genera are assigned to the
Whitbian assemblage. Dactylioceras he·63

lianthoides, D. d. helianthoides, Perolloceras subfibulatum. Harpoceras chrysallthemum, H. inouyei, H. okadai, H. aff.
m ulgravium, H. aff. exaratum, Harpoceratoides nagatoensis, Hildoceras sp.,
Protogrammoceras nipponicum, P. yabei,
P. onoi, Lioceratoides yokoyamai and L.
matslIl1lotoi.
This fauna shows remarkably highsimilarities to the Alta Brianza fauna.
the Pyrenees fauna and the eastern partof the Paris Basin fauna (Table 3). The
Alta Brianza fauna shows the highest
similarity to the Valdorbia fauna, thePyrenees fauna and the eastern part of
the Paris Basin fauna. Alta Brianza
and Valdorbia are in the Mediterranean
region but the other two are not. The
Alta Brianza fauna, however, shows aconsiderably high similarity with theeastern part of the Paris Basin fauna.
The Toyora fauna shows somewhathigh similarities to the Dorset-Somerset
fauna, the Tage fauna, the eastern Caucasus fauna and the northern Alaska
Table 3. Faunal resemblance in Whitbian. Harpoceratoides is treated being independent of Harpoceras (Tables 3-4).

2L100
Nl+Nl

64

Hiromichi HIRANO

fauna.
The Dorset-Somerset faunashows the highest similarity to the northern Alaska fauna and a somewhathigh similarity to the eastern Caucasus
fauna but a low similarity to the Tagefauna. The eastern Caucasus faunashows a high similarity to the British
Columbia fauna, but the British Columbia fauna shows a low similarity to thenorthern Alaska fauna.
The Jebel
Tuwaiq and the Madagascar faunas are
peculiar and do not seem to have similarities to the Toyora fauna, as far as
the available evidence is concerned.
Hammatoceratidae and Bouleiceratidae
are regarded as the Tethyan elements
by HALLAM (1969), but Bouleiceras is
restricted to Jebel Tuwaiq, Madagascar,
related areas and is unknown from thewestern Mediterranean region. On thecontrary genera of Hammatoceratidae
are known as north as the Paris Basinand Britain, and their distribution is
wide. A few ammonites of Hammatoceratidae occur in the Toyora fauna but
it is difficult to say that they are of the
Tethyan Realm. In Europe, high similarity is shown between two adjacentfaunas and the longer the distance, thelower the similarity (e. g.. Dorset-E.
Paris Basin-Jura Mts., Dorset-E. Paris
Basin-pyrenees-Alta Brianza-ValdorbiaTage). In comparison with the Domerlan ones the Whitbian faunas show
higher similarity between the provinces.
The above data of the faunas outside
Japan are based on the following references.
For the Dorset-Somerset fauna ARK ELL(1933), Jebel Tuwaiq fauna ARKELL etal. (1952), Northants fauna ARKELL (1933),
eastern Caucasus, east of the Paris Basin,
Jura Mts., Madagascar and Pyrenees
faunas ARKELL (1956), Valdorbia fauna
DONOVAN (1958), British Columbia, Alberta and southern Yukon fauna FRE-BOLD (1970). northern Alaska fauna~
IMLA Y (1955), eastern Oregon and Cali-fornia IMLAY (1968) and for the Alta
Brianza fauna VENZO (1952).
C-3. The Toyora fauna in Yeovilian sub-stage
The Toyora fauna shows the highest:
similarity to the eastern Caucasus fauna.
and low similarities to other faunas(Table 4). In this substage, the Euro-pean faunas show very high similarities
between the subprovinces and the longer
the distance the lower the similarity'(e. g., Dorset-E. Paris Basin-PyreneesTage-Valdorbia) and they generally
show low similarities to faunas of otherregions. As regards North America, it
is noted that British Columbia, eastern
Oregon and northern Alaska show very'
low similarity mutually throughout
Domerian, Whitbian and Yeovilian.
The data of the faunas outside Japanare based on the following references.
For the Dorset-Somerset fauna ARKELL(1933), Jebel Tuwaiq fauna ARKELL etal. (1952), eastern Caucasus fauna, east
Table 4.

Faunal resemblance in Yeovilian.
c

.l1
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I I
ei
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~

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95371
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E. Paris Basin
792 5063
Tage
1267 476774
I
Pyrenees
777 6775 8674
886 4659 938080
Jura Mis.
344 2533 4040 4036
E. Caucasus
I
746 ~3 38 43 357 5340
E. OregonI
Sr. Columbia, Alberta & s.Vukon 440 4431 5550 3667 2936
N. Alaska
1 0 o 0 015 0 050 0 0
C. Arabia
1 0 0 0 o 0 0 0 0 o 0 0
344 017 4027 03633 000 0
Madagascar
44044 655 5055 5086 3650 40 0.29
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Valdorbia_Ll-+-

615.

Jurassic Toyora Group-lJI

65

'~f

the Paris Basin fauna. Jura Mts.
fauna, Madagascar fauna and Pyrenees
fauna ARKELL (1956), Valdorbia fauna:DONOVAN (1958), British Columbia fauna
FREBOLD (1970), northern Alaska fauna
IMLAY (1955), eastern Oregon and Cali-fornia fauna IMLAY (1968) and for the_Alta Brianza fauna VENZO (1952).

,

Conclusion
The Toyora Group is composed of. conglomerate, sandstone, shale and al·ternation of sandstone and shale and-shale and 1200 to 1900 m. in thickness.
The group represents a sedimentary
cycle and it is divided into three forma'tions, namely, the Higashinagano Forma-tion of the transgressive phase, theNishinakayama Formation of the inun·dative phase and the Utano Formation·-of the regressive phase.
23 genera including 42 species of ammonoids are identified and described.
-The age of the Toyora Group ranges
from Sinemurian to Bathonian as evidenced by these ammonoids and some·other fossils.
A diachronous situation of the lithos·tratigraphic unit is suggested from the-data in the Higashinakayama area.
Three zones are recognized in the
middle part of the Toyora Group on-the basis of ammonid assemblage. They-are correlated from the Stokesi Subzoneof the Margaritatus Zone to the FibI/_latum Subzone of the Bifrons Zone. The
Member Up of the Utan9 Formation isroughly correlated with the Variabilis,and the Thouarsense Zones.
The Toyora fauna in Domerian substage is characterized by elements of
the Mediterranean or Tethyan faunas.
It is restricted only to Whitbian that
the Toyora fanua shows a somewhathigh similarity to that of western•..• Boundary of zone..... B.
member

-

B.
Faull

formation

O,,"-===_~5_ _.....
1 Km.

Text-fig. 4. Map showing the zonation.
F: Fontanelliceras fontanellense Zone, P:
Protogrammoceras nipponicum Zone, D:
Dactyl ioceras helianthoides Zone.

Europe. The Toyora fauna shows asomewhat low similarity to the faunasof western and southern Europe in
Yeovilian substage. _There are some comparab:le species
between the Toyora fauna and the eastern Oregon fauna, but high similarity
is not recognized in the generic assemblage.
Stratigraphic guide of localities(loc. 1-59)
Member Ncs: Loc. 51, 52.
Member Nss: Loc. 50.
Fontanelliceras fontanellense Zone:

Loc. 11,

Hiromichi HIRANO

66

12, 12B, 14, 16, 17, 18, 19, 29,38,39,48,50.
Protogrammoceras nipponicum Zone: Loc. 4,9, 10, 13, 15, 18B, 18D, 18E, 20, 21, 22, 23,
24, 30,31, 32.
Dactylioceras helianthoides Zone: Loc. I, 2,
3,5,6,7,25,26,27,28,28'-28"",33,34,35,
36, 40, 41, 42, 43, 44, 45, 46, 47.
Member Na: Loc. 8, 37, 49.
Member Up: Loc. 53, 54, 55.
Member Ub: Loc. 56.
Member Uh: Loc. 57, 58.
Member Ut: Loc. 59.

References
ARK ELL, W. J. (1933): The Jurassic System
in Great Britain, Oxford Press, 681p.
- - (1956): Jurassic geology of the World,
Oliver & Boyd Ltd., 806p.
- - et al. (1957): Treatise on invertebrate
paleontology, Mollusca, pt. L4, Geol. Soc.
America & Univ. Kansas Press, 490p.
- - BRAMKAMP, R. A. and STEINEKE, M.
(1952): Jurassic ammonites from Jebel
Tuwaiq, central Arabia, Phil. Trans. Roy.
Soc. London, ser. B, vol. 633, pp. 241-313,
pis. 15-3l.
BETTONI, A. (1900): Fossil Domeriani della
Provincia di Brescia, Mem. Soc. Paleont.
Suisse (Abh. schweiz. palaont. Cesell.) ,vol. 27, pp. 1-88, pis. 1-9.
BUCKMAN, S. S. (1899): A monograph on theInferior Oolite ammonites of the British
Islands, Palaeontogr. Soc., pt. 11, supple.,
pp. 33-64, pis. 5-14.
- - (1904): Ditto, Ibid., pt. 12, supple., pp.
65-168, pis. 15-19.
- - (1905): Ditto, Ibid., pt. 13, supple., pp.
169-208, pis. 20-24.
- - (1909): Yorkshire Type Ammonites,
vol. 1, pts. 1-8, 80 pis.
- - (1921-1923): Type Ammonites, vol. 4,
pts. 25-42, 180 pis.
(1925-1927): Ditto, vol. 6, 192 pis.
DEAN, W. T., DONOVAN, D. T. and HOWARTH,
M. K. (1961): The Liassic ammonite
zones and subzones of the North-west
European province, BUll. Brit. Mus. (Nat.
Hist.), Ceol., vol. 4, no. 10, pp. 437-505.
DOKOVAN, D. T. (1952): The ammonites of

the Blue Lias of the British district, pt..
2, Arietitidae, Ann. Mag. Nat. Hist., ser.
12, vol. 5, pp. 717-752, pis. 27-29.
- - (1958): The Lower Liassic ammonite,
fauna from the fossil bed at Langeneckgrat, near Thun (Median Prealps),
Schweiz. Palaeont. Abh., vol. 74, pp. 158, pis. 1-7.
DRES):AY, R. (1963): Quelques ammonites
de la partie inferieure du Pliensbachien(Carixien et Domerien pro parte) du jbel
Bou-Rharraf (Haut Atlas oriental), Note'
Servo Ceol. Maroc, vol. 23, no. 172, pp.
141-164, pis. 1-2.
DeBAR, G., FOL:CAl7LT, A. and MOUTERDE,
R. (1967): Le Lias moyen des environs
de Huescar (province de Grenade,Espagne), Bull. Soc. Ceol. France, vol. 7,
no. 9, pp. 830-834.
DUMORTIER, E. (1867): Etudes paleontologiques sur les depots jurassiques duBasin du Rhone, pt. 2, 252 p., 50 pis.
FREBoLD, H. (1951): Contributions of thepalaeontology and stratigraphy of theJurassic System in Canada, Ceol. Surv.
Canada, Bull. 18, pp. 1-54, pis. 1-17.
(1957): The Jurassic Fernie Group in
the Canadian Rocky Mountains and foot-·
hills, Ceol. Surv. Canada, Mem. 287, no.
2531, pp. 1-197, pis. 1-44.
- - (1964a) :Illustrationof Canadianfossils, Jurassic of western and Arctic
Canada, Ceol. Surv. Canada, Paper 63-4,
pp. 1-106, pis. 1-5l.
- - (1964b): Lower Jurassic and Bajocian
ammonoid faunas of northwestern British
Columbia and southern Yukon, Ceol.
Surv. Canada, Bull. 116, pp. 1-31, pis. 1-8.
- - (1970): Pliensbachian ammonoids from
British Columbia and Southern Yukon,
Can. Jour. E. Sci., vol. 7, no. 2, pp. 435456, pis. 1-4.
- - and LITTLE, H. W. (1962): Palaeontology, stratigraphy and structure of theJurassic rocks in Salmo map-area,
British Columbia, Ceol. Surv. Canada,
Bull. 81, pp. 1-31, pis. 1-5.
- - , MOUNTJOY, E. W. and TEMPELMANKLUIT, D. J. (1967): New occurrencesof Jurassic rocks and fossils in central

615.

Jurassic Toyora Group-III

and northern Yukon Territory, Ceoi. Surv.
Canada, Paper 67-12, pp. 1-35, pis. 1-3.
FLTI'."I, A. (1900) :" Ammoniti del Lias mediodell' Appennino centrale esistenti nel
Museo di Pisa, Paiaeontogr. Italica, vol.
6, pp. 17-78, pis. 7-13.
- - (1901): Cefalopodi liassici del Montedi Cetona, pt. I, Ibid., vol. 7, pp. 1-89,
pis. 1-14.
(1902): Ditto, pt. 2, Ibid., vol. 8, pp.
131-217, pis. 12-26.
- " (1904): Ditto, pt. 4, Ibid., vol. 10, pp.
275-298, pis. 18-2l.
- - (1905): Ditto, pt. 5, Ibid., vol. 11, pp.
93-146, pis. 3-1l.
- - (1923-1928):
Fossili domeriani dei
Dintorni di Taormina, Ibid., vols. 29-30,
pp. 41-77, pis. 4-15.
(1931): Ditto, pt. 4, Ibid., vol. 31, pp.
93-149, pis. 5-21.
GECZI, B. (1970): Pliensbachi ammonites
zonak a Bakonyhegy.segben, Bull. Hung.
Ceo!. Soc., vol. 100, pp. 248-258.
GEMMELLARO, G. G. (1885): Sopra taluni
Harpoceratidi del Lias superiori dei
Taormina, Ciorn. Sci. Nat. Econ. Palermo.,
vol. 17, pp. 1-109, pis. 1-2.
GURICH, G. (1933): Leitfossilien, Cebruder
Borntreger, 272 p., 24 pis.
HAAS, O. (1913): Die Fauna des mittleren
Lias von Ballino in Siid tirol, Beitr.
Palliont. Ceol. Oster. Orient., Bd. 26, pp.
1-161, pis. 1-7.
HALLAM, A. (1969): Faunal realms andfacies in the Jurassic, Palaeontology, vol.
12, pt. I, pp. 1-18.
HAUG, E. (1885): Beitrae zu einer Mono·graphie der Ammoniten Gattung Har·
poceras, N. Jb. Min., B.·Bd. 3, pp. 585722, pis. 11-12.
HAYAMI, 1. (1958): Taxonomic notes on
Cardinia with description of a new
species from the Lias of western Japan,
Jour. Fac. Sci., Univ. Tokyo, sec. 2, vol.
11, pt. 2, pp. 115-130, pI. 11.
- - (1959): Lower Liassic Lamellibranchfauna of the Higashinagano Formationin West Japan, Ibid., vol. 12, pt. I, pp.
31-84, pIs. 5-8.
- - (1960a): Lower Liassic gastropods from67

the Higashinagano Formation in WestJapan, Jap. Jour. Ceol. Ceogr., vol. 31,
nos. 2-4, pp. 99-106, pI. 9.
- - (1960b): Jurassic inoceramids in Japan,
Jour. Fac. Sci., Univ. Tokyo, sec. 2, vol.
12, pt. 2, pp. 277-328, pis. 15-18.
- - (1961):
On the Jurassic pelecypod
faunas in Japan, Ibid., vol. 13, pt. 2, pp.
243-343, pI. 14.
- - (1962): Jurassic pelecypod faunas inJapan with special reference to theirstratigraphical distribution and biogeographical provinces, Jour. Ceol. Soc.
Japan, n!. 68, no. 797, pp. 96-108. (inJap:mes£ with English abstract].
HIRA'."O, H. (1971): Biostratigraphic studyof the Jurassic Toyora Group. Pt. I,
Mem. Fae. Sci., Kyushu Univ., ser. D,
vol. 21, no. I, pp. 93-128, pis. 14-20.
- - (1973): Ditto, pt. 2, Trans. Proc. Pa/aeont. Soc. Japan, N. S., no. 89, pp. 1-14,
pis. 1-4.
HOWARTH, M. K. (1955): Domerian of theYorkshire Coast, Proc. Yorkshire Ceo!.
Soc., vol. 30, pt. 2, no. 10, pp. 147-175,
pis. 10-12'- - (1956): The Scalpa Sandstone of theIsle of Raasy, Inner Hebrides, Ibid., vol.
30, pt. 4, no. 19, pp. 353-370, pI. 27.
- - (1957): The middle Lias of the Dorset
Coast, Q.]. C. S. London, vol. 113, pp.
185-203, pI. 17.
- - (1958): A Monograph of the ammonitesof the Liassic family Amatheidae in
Britain, pt. I, Pa/aeontogr. Soc., pp. 1-26,
pis. 1-4.
- - (1962): The Yorkshire type ammonites
and nautiloids of YOUNG and BIRD, PHIL·
LIPS, and Martin SIMPSON, Palaeontology,
vol. 5, pt. I, pp. 93-136, pIs. 13-19.
IMLAY, R. W. (1955): Characteristic Jurassic
Mollusks from northern Alaska, Ceol.
Surv. U. S. A., Prof. Paper 274-D, pp. 6996, pIs. 8-13.
- - (1968): Lower Jurassic (Pliensbachianand Toarcian) ammonites from eastern
Oregon and California, Ibid., 593-C, pp.
CI-C51, pis. 1-9.
KOBAYASHI, T. (1926): Note on the Mesozoic
Formation in Province Nagato, Chugoku,

68

Hiromichi HIRANO

Japan, Jour. Ceol. Soc. Japan, vol. 33,
pp. 1-9, pI. II.
- - (1935): Contributions to the Jurassic
Torinosu Series of Japan, Jap. Jour. Ceol.
Ceogr., vol. 12, nos. 3-4, pp. 69-92, pI. 12.
- - (1936): The geological structure ofSouthwest Japan and its Mesozoic palaeogeography, pt. 4, Jour. Ceol. Soc.
Japan, vol. 43, pp. 531-541 (in Japanese].
- - , KOl'ISHl, K., SATO, T., HAYA.:\II,1. andTOKUY AMA, A. (1957): On the Lower
Jurassic Kuruma Group, Ibid., vol. 63,
no. 738, pp. 182-194 (in Japanese].
- - and MORI, K. (1954): Studies on theJurassic trigonians in Japan, pt. 2,
Prosogyrotrigonia and the Trigoniinae,
Jap. Jour. Ceol. Ceogr., vol. 25, nos. 3-4,
pp. 155-175, pis. 15-16.
KOSCHELKINA, Z. V. (1953): Stratigraphy
and bivalve mollusks of the Jurassic
deposits of Viluysk syncline and nearVerkhojansk foredeep, Trans. East.
Siberia K{)m. Inst., vol. 5, ,pp. 1-219, pis.
1-25.
MATSUMOTO, T. (1949): The Late Mesozoic
geological history in the Nagato Province,
Southwest Japan, Jap. Jour. Ceol. Geogr.,
vol. 21, pp. 235-243.
- - ed. (1963): A survey of the fossils
from Japan illustrated in classicalmonographs (Primarily a nomenclatorial
revision), Palaeont. Soc. Japan, 55th

Anniversary Vol., 57 p., 68 pis.
- - et al. (1967): Historical geology, pt. 2,
Asakura Book Co., 683 p. (in Japanese].
- - in MAKIYAMA, J. et al. (1953): Historical geology, pt. 2, Asakura Book Co.,546 p. (in Japanese].
and ONO, A. (1947): A biostratigraphic
study of the Jurassic Toyora Group, withspecial reference to ammonites, Sci. Rep.
Fac. Sci., Kyushu Univ., Ceol., vol. 2, no.
1, pp. 20-31, pis. 1-2 (in Japanese].
MERLA, G. (1933): Ammoniti giuresi dell'Appennino centrale, 1. Hildoceratidae,
Palaeontogr. italica, vol. 33, n. ser. 3,
pp. 1-54, pis. 1-7.
MONESTIER, J. (1931): Ammonites rares ou
peu connues et ammonites nouvelles duToarcian moyen de la region de l'Aveyron,
Soc. Ceoi. France Mem., n. ser., vol. 7,
pt. 1, pp. 1-79, pis. 1-9.
- - (1934): Ammonites du Domerien de laregion sud-est de l'Aveyron et de quelques regions de las Lozere a l'exclusion
des Amaltheides, Ibid., vol. 10, pt. 3, pp.
1-102, pis. 1-11.
MouTERDE, 'R., (1967): Le Lias moyen de
Sao Pedro de Muel (Portugal) (Premiere
partie), Comun. Servo Ceol. Portugal, vol.
52, pp. 185-208.
NAUMANN, E. and NEUMAYR, M. (1890):
Zur Geologie und Palaontologie von Japan,
Denk. Mathern. Natur. Klasse Konig.

Explanation of Plate 9(All in natural size)
Figs. 1-6. Peronoceras subfibulatum (YOKOYA:\IA)
1. MM. 7068, Paralectotype, loc. 47; 2. GK. G. 2182, loc. 28"; 3. MM. 7069, Paralectotype, loc. 47; 4. GK. G. 2177, loco 35; 5. MM. 7067, Paralectotype, loc. 47; 6. MM. 7066,
Lectotype, loc. 1.
Figs. 7a-b. Planammatoceras sp. d. P. kitakamiense (SATO)
7a. Gypsum cast of GK. G. 2014, loco 57; 7b. Rubber cast of a part of GK. G.' 2014
Figs. Sa-b. Arietites sp.
8a. GK. G. 11380, external mOUld, loco 51; 8b. Rubber cast of GK. G. 11380
Fig. 9. Dactylioceras (s. str.) sp. d. D. helianthoides YOKOYAMA
GK. G. 2093, loco 13
Fig. 10. Hidoceras sp.
'GK. G. 11352, loco 44

HIRANO:

Jurassic Toyora Group-III

Plate 9

615.

Jurassic Toyora Group-III

Akad. Wissen., Bd. 57, p. 35, figs. 1-3.
NUTSCHUI3IDZJ, K. S. (1966): Lower Jurassic
fauna of Caucasus, 212 p., 41 pIs.
·OISHI, S. (1935): A new species of Zamites
from the Nishi-Nakayama Bed, Yamaguchi Prefecture, Jour. Fac. Sci., Hokkaido
Imp. Univ., ser. 4, vol. 3, no. 1, pp. 97100.
._- (1940): The Mesozoic floras of Japan,
Ibid., vol. 5, nos. 2-4, pp. 123-480, pIs.
1-48.
PUGIN, L. (1964):
Ammonites prealpines.
Etude critique des Lytoceratina duDogger, Schweiz. Palaeont. Abh., vol. 80,
pp. 1-67, pIs. 1-4.
SAra, T. (1954) : Hammatoceras de Kitakami,
Japon, Jap. Jour. Ceol. Ceogr., vol. 25.
nos. 1-2, pp. 81-100, pIs. 7-9.
- - (1955): Les ammonites recueillies dansIe groupe de Kuruma, nord du Japon
central, Trans. Proc. Palaeont. Soc. Japan,
N. S., no. 20, pp. 111-118, pI. 18.
- - (1956).: Correlation du Jurassique inferieur japonais en basant sur les ammonites fossils, Jour. Ceol. Soc. Japan,
vol. 62, no. 732, pp. 490-503 (in Japanesewith French abstract).
- - (1957): Biostratigraphie de la serie deShizukawa (jurassique inferieur) duJapon septentrional, Jour. Fac. Sc.,
U niv. Tokyo, sec. 2, vol. 10, pt. 3, pp.
131-350, pIs. 1-2.
- - (1960): A propos des courants oceaniques froids proves par I'existence desammonites d'origine arctique dans Ie
Jurassique japonais, Internat. Ceol. Congr.
Norden, Rep. 21 st., pt. 12, pp. 165-169.
- - (1962): Etudes biostratigraphiques desammonites du Jurassique du Japon, Mhn.
Soc. Ceol. France, no. 94, pp. 1-122, pIs.
1-10.
- - in ASA:-;O, K. et al. (1967): Historicalgeology, revised ed., pt. 2, 683 p.,
Asakura Book Co. (in Japanese).
SHIKA'"-'IA, T. and HIRA:'-IO, H. (1970): On
the mode of occurrence of ammonites
in the Nishinakayama Formation, Toyora
Group, Sci. Rep. Yokohama Natl. Univ.,
sec. 2, no. 16, pp. 61-71, pIs. 9-11.
SHIMIZU, S. (1928): Remarks on two am-

69

monites Harpoceras Japonicum NEUMAYR
and Arapadites sakawanus MOJslsovlcs
from the Sakawa basin in Shikoku, Jap.
Jour. Ceol. Ceogr., vol. 5, no. 4, pp. 219222.
- - and OUAT A, T. (1934): Cephalopoda,
Geol. Palaeont., vol.. 32, no. 9, pp. 1-137,
Iwanami Book Co. (in Japanese).
SPATH, L. F. (1919): Notes on ammonites,
Ceol. Mag., ser. 6, vol. 6, pp. 170-177.
- - (1923): Correlation of the Ibex andJamesoni Zones of the Lower Lias, Ibid.,
vol. 60, pp. 6-11.
- - (1927): Revision of the Jurassic cephalopod fauna of Kachh (Cutch), pt. 1,
Palaeontogr. Indica, n. ser. vol. 9, no. 2,
pp. 1-72, pIs. 1-7.
TAKAHASHI, E. (1951a): Descriptive notes
on some Mesozoic plants from Province
Nagato (Yamaguchi Pref.), Jour. Ceol.
Soc. Japan, vol. 57, no. 664,pp. 29-33.
- - (1951b): Some Cycadophyta from theJurassic Toyora Series, Province Nagato(Yamaguchi Pref.), Japan, Ibid., vol. 57,
no. 668, pp. 191-193.
- - (1954) : Stratigraphy of the fossil plantsof the Toyora Group, Ibid., vol. 60, no.
703, p. 169 (in Japanese).
- - et al. (1965): Palaeozoic and Mesozoic
formations of the eastern and thesouthern parts of the Tabe Basin,
Yamaguchi Prefecture, Sci. Rep. Yamaguchi Univ., v 01. 15, pp. 33-49, pIs. 1-3(in Japanese with English abstract).
- - et al. (1966): Mesozoic formations of
the northern and the eastern parts of
the Tabe Basin, Yamaguchi Prefecture,
Ibid., vol. 16, pp. 53-65, pIs. 1-2 (inJapanese with English abstract).
- - et al. (1968): Geology and structureof the Toyogadake-Nishiichi district of
the Nagato tectonic zone, Ibid., vol. 18,
pp. 9-25, pIs. 1-2 (in Japanese withEnglish abstract).
- - and NAITO, G. (1950): Dictyozamites
from the Jurassic Toyonishi Series of
Provo Nagato (Yamaguchi Pref.), Jour.
Ceol. Soc. Japan, vol. 56, no. 655, p. 188.
(in Japanese).
TAKAHASHI, H. (1969): Stratigraphy and70

Hiromichi HIRANO

ammonite fauna of the Jurassic systemof the southern Kitakami Massif, Northeast Honshu, Japan, Sci. Rep. Tohoku
U niv., 2nd ser. Ceol., vol. 41, no. 1, pp.
1-93, pis. 1-19.
TAKAI, F., MATSCMOTO, T. and TORIYAMA,
R. ed. (1963): Geology of Japan, 279 p.,
Univ. Tokyo Press.
TIIEVE:\I:\, A. (1908):
Paleontologie deMadagascar-5. Fossiles Liasiques, Ann.
Pateont., vol. 3, pp. 105-143, pis. 8-12.
TORIYA~IA,
R. (1S-38):
Geology of the
Toyora Group in Toyora county, Yamaguchi Prefecture, jour. Ceol. Soc. japan,
vol. 45, no. 533, pp. 247-258 (in Japanese).
VENZO, S. (1252): Nuove faune ad ammoniti del Domeriano-Aleniano dell'Alpeturati e dintorni (Alta Brianza), Atti
Soc. Ital. Sci. Nat., no. 91, pp. 95-123,
pis. A-B.
WRIGHT, T. (1882): Monograph on the Liasammonites of the British Islands, Palaeontogr. Soc., vol. 5, pp. 329-400, pis.
49-69.
(1883): Ditto, Ibid., vol., 6. pp. 401-440,
pis. 70-77.
(1884): Ditto, Ibid., vol. 7, pp. 441-480,
pis. 78-87.

YABE, H. (1920): On the so-called Mesozoic
formation of the Kiku Peninsula, Province Bizen, jour. Ceogr., vol. 32, no.
389, pp. 1-8 (in Japanese).
- - and EGGeIII, M. (1933):
Anabachia
cyclolitoides sp. nov. from Japan, withremarks of the genus Anabachia, jap.
jour. Ceol. Ceogr., vol. 10, nos. 3-4, pp.
119-124.
YEHARA, S. (1921): On some new speciesof Trigonia from the Lias of Provo ofNagato and the Cretaceous of Provo
Awa, jour. Ceol. Soc. Tokyo, vol. 28, pp_
7-11, pI. 5.
- - (1927): Faunal and stratigraphicalstudy of the Sakawa Basin, Shikoku,
jap. jour. Ceol. Ceogr., vol. 5, nos. 1-2,
pp. 1-40, pis. 1-5.
YOKOYAMA, M. (1904): Jurassic ammonites
from Echizen and Nagato, jour. Coil.
Sci. Imp. Univ. Takyo, vol. 19, art. 20,
pp. 1-17, pis. 1-4.
ZEISS, A. (1956): Hecticoceras and Reineckeia
im Mittel- und Ober-Callovien von Blumberg (Sud baden) , Bayer. Akad. Wiss.
Miinchen, pp. 1-101, pis. 1-4.
ZITTEL, K. A. (1885): Handbuch der Palaontologie, Bd. 2, 893 p, R. Oldenbourg.

Explanation of Plate 10(All in natural size)

Harpophylloceras? sp.
GK. G. 2020, loc. 52
Figs. 2-3. Lytoceras sp. A
2. GK. G. 2049, loc. 9; 3. GK. G. 2043, loc. 9
Fig. 4. Lytoceras sp. B
GYU. M. 1019, loc. 18B
Figs. 5-6. Calliphylloceras sp. A
5. GK. G. 2017, loc. 53; 6. GK. G. 2029, the Anda-daniFig. 7. Calliphylloceras sp. B
GK. G. 11335, loc. 23
Fig. 8. Holcophylloceras sp.
GK. G. 2016, loc. 59
Fig. 9. Audaxlytoceras? sp.
Rubber cast of GK. G. 2059, loc. 36 ?
Fig. 1.

HIRANO:

Jurassic ToyoTa G1'oup-III

Plate 10

1

9

3

4

615.
Higashinagano
Nishinakayama
Utano
Sakuraguchi·dani
Anda·dani

Jurassic Toyora Group-III

*

~

ft(

Q

*

III

i§

i=j:I

lilk

!b't
ill
!L'f
~
~

Higashinakayama
the River Era
the River Motoyoku
tne River Sakota

71

* laa
*
J:f:t

tt

ill
)II

)II

;g 13'1 III

Trans. Proc. Palaeont. Soc. Japan, N.S., No. 90, pp. 72-80, pIs. 11-13, June 30, 1972'<616.

EARLY PERMIAN PARAFUSULINA AND PSEUDOFUSULINELLAFROM THE CHILLIWACK GROUP, SOUTHWESTERNBRITISH COLUMBIA, CANADA *KIMIYOSHI SADA
Department of Geology, Faculty of General Education,
Hiroshima University, Hiroshima 730

and
WILBERT R. DANNER
Department of Geological Sciences, the University of
British Columbia, Vancouver, Canada

1J -j-!/ British Columbia im1§-It!,O) Chilliwack l7inf.O) Parafusulina c Pseudofusulinella: British Columbia jY,ji!§ii!> Chilliwack valley !l!!h.il(O) Chilliwack l\'Hl'f.I'j:lO):fii!k
~~i v:/ ;;(/.1' GIIMtIJ,:J'EC:m:Wt.d.\!:\'i'j ~!-li:t:-J- Parafusulina c Pseudofusulinella ~iiii\JJIJ 1.t:o)-CfIWf-J-{So :=.:=. f:::l1cji&~;jl,t:Hllfi Pseudofusulinella danneri SKINNER & WILDE,
Parafusulina mongeri SAD A & DA:\:\ER, sp. nov., P. laudoni SKIj';NER & WILDE OJ
3 It]-C:'J;,0, :=.;jl,GO)Hn:::J:: ·~-::-hYi)jx."6;j1-0 Chilliwack *JjkllEE.{tEtJJ~1llHi SKI0i0iER &WILDE (1966) f::: J:: "? -::- ¥!l15-"6 ;jlt: Washington HIO) Black Mountain M~1\lti'JtJJ~~f
J:: f) "t,-'{" ~ ffZWJO)tO)O)J:: -J f:::.\lU-:>1.l" California ')+10) McCloud Iii!k1:'iO)H;:g: (SKINNER& WILDE, 1965) 0)(tnilJ~11n:::;l'Ht"6;fl0, :::'1.lGO):::'C/.pG, :='(7)(Uiwi)17I)R'Hi Leonardian *JJlmO)"t,O)C~;tGh0o
itFI:Ii"dH' • W.R. DANNER

Introduction

DAL Y (1912) gave the name Chilliwack
Series to the Paleozoic rocks of theChilliwack valley but the term Groupwas substituted for Series on the 1944
Geologic Map of the Hope Sheet by
CAIRNES (Geological Survey of Canada
map 737 A) to bring the nomenclaturein line with modern usage of stratigraphic terminology. DALY (1912) foundlimestone containing bryozoa, brachiopods and the fusulinid Fusulina elongata
south of the border in Washington and
GIRTY (in DALY, 1912, p. 515) suggested
that this fauna probably correlated with

The Chilliwack Group is a thick se1luence of upper Paleozoic clastic, carbonate and volcanic rocks cropping out on
both sides of the International Border insouthwestern British Columbia, Canada
and northwestern Washington, U. S. A.
-South of the border it includes rocks as
old as Devonian but north of the border
only rocks of Pennsylvanian and Permian
age have been recogni2ied.

* Received Jan. 13, 1973; read Oct. 28, 1972
at Matsuyama.

72

616.

Fusulinids from Chilliwack, B. C.

73:

BRITISH/

OREGON

RIVER

S.c.
CANADA-._._oA-·.-.-.-.-.

,8 MILES
Text·fig. 1.

01

BLIcK MTN.

WASHINGTON

U.S.A.

Map showing Chilliwack fossil localities in southwestern British Columbia.

that of the Nosoni Formation of northern California. THOMPSON, WHEELER &HAZZAR (1946) regarded F. elongata
SHUMARD as probably belonging to thegenus Parafusulina. COOGAN (1960) andSKINNER & WILDE (1965) described theNosoni Formation fusulinids and foundthem to be advanced species of Parafuslliina which are younger than forms
found in the Chilliwack Group.
HILLHOUSE (1965) noted fusulinid-bearing limestone on the British Columbia
side of the border but they were too
poorly preserved for specific identification. Their large size, however, indicated a Permian age. In 1956 DANNER
started reconnaissance studies of theChilliwack area to continue field work
started several years earlier on the
Washington side of the border. DANNER(1957) listed an abundant fusulinid faunafrom the Black Mountain area in Wash-ington State which SKINNER (personalcommunication) considered to be of Wolfcampian age. Later the discovery of a_Parafusuli71a in these collections (SKIN-NER & WILDE, 1966) suggested a probable early Leonardian age for this samefauna which contains one species ofPselldofusulillelia, two species of Schwa-gerina and one species of Parafusulina ..
MONGER (1966) started field work in
the area in 1962 on his Ph. D. thesis andmade many fossil collections includingfusulinids. Specimens from one of his.
localities are included in the descriptionsin this paper. He made the most accu-rate geologic map that has yet been_
produced of the Chilliwack Group on the
Canadian side of the border and he recognized the probable diachronous nature:of the Permian limestone bodies.

74

Kimiyoshi SADA and Wilbert R. DANNER

Field work in the Chilliwack area by
W. R. DANNER and laboratory work carried on at the University of British
Columbia by K. SADA as a post-doctoral
fellow was financed by grants from the
National Research Council of Canada.
Further work on this project was carriedout while DANNER was visiting Professor
at Hiroshima University under the auspices of the japan Society for the Promotion of Science.
Geology

The Chilliwack Group is composed ofa sequence of argillites, fine- to coarsegrained volcanic arenites, rare conglomerates, large and small limestone bodies
and near the top a volcanic unit ofaltered basic to intermediate flows. tuffs
and silicified tuffs and chert. The baseis not exposed. The top is overlain
disconformably or is infault contact with
fine- to medium-grained volcanic arenites
and argillites of the late Triassic-earlyjurassic Cult us Formation.
In the Chilliwack area the maximum
total thickness of the Chilliwack Groupis estimated to be about 5700 feet
(MONGER, 1966). The sequence is complexly folded and faulted and in someinstances is inverted. Most of theChilliwack rocks, except for the limestones, are not distinctive enough thatthey can be easily defined as formations
and used for correlation. However, thelimestones are diachronous and theirbases and tops are not stratigraphic
horizons, a phenomena noted in otherwestern Cordilleran North American
limestones of similar environment (SKINNER & WILDE, 1965). Mostly it is only
fossils in the limestones that offer reliable indications. It is also very difficult
to identify whether the argillites andfine- to medium-grained volcanic arenites

belong to the Chilliwack Group or to asimilar lithology of the younger late
Triassic-early jurassic Cultus Formation.
Throughout the area of the Chilliwack
Group lower Permian and lower Pennsylvanian limestones form the two mostprominent marker units. Between themis a clastic seq uence ranging from fineto coarse-grained volcanic arenites andcoarse conglomerates. At several localities this clastic seq uence contains plantfragments. It is between 450 and 800
feet thick in the Chilliwack area but
may be 300 feet or less in parts ofnorthwestern Washington.
Lower Permian fusulinid-bearing limestone is found as large and small beds
and lenses. It is dark grey to lightgrey and buff in color. Locally it isdolomitized and contains a considerable
amount of black to grey secondary
chert. It is commonly cliff-forming andwhere internally folded has thicknessesof more than 2000 feet. The maximum
normal thickness found by MONGER is
300 feet. To the south in Washington
State it is generally thinner and may be
represented by two or more limestone
members separated by shales.
MONGER (196'6), noted fusulinids to be
the commonest fauna in the Permian
limestone and found them to be mostabundant at the top of the limestonebodies underlying the Chilliwack volcanic
unit. Associated with the fusulinids arebryozoans, crinoid columnals and rare
gastropod and brachiopod fragments.
Large corals (Dibunophyllum ?) are often
present. Many of the limestone bodies
in the Chilliwack Group are recrystallized and only outlines of the fossils arepreserved.
Recrystallization is mostcommon in the eastern part of the area
nearer the contact with the Cenozoic
Ch illi wack Batholith.

616.

Fusulinids from Chilliwack, B. C.

75

Discussion of the Fauna

Chilliwack Fossil Localities

The Chilliwack Group early Permian
fusulinid collections from the Chilliwack
area of British Columbia contain PseudoJusulinella danneri SKINNER & WILDE,
ParaJusulina laudoni SKINNER & WILDE,
and ParaJusulina mongeri, sp. nov. at the
top of the lower Permian limestone unit
or in numerous small limestone pods
underlying and interbedded with thevolcanic unit. A few schwagerinids occur in the larger limestone bodies but
our specimens are generally not wellenough preserved for description. ParaJusulina is very abundant and in somelocalities may be the only fusulinidpresent. In contrast, to the south inWashington at Black Mountain ParaJusuhna is rare at most localities andschwagerinids are abundant and wellpreserved.
PseudoJusulinella danneri
SKINNER & WILDE, is relatively abundant at both of our localities and at
Black Mountain.
It seems apparent, as suggested by
MONGER (1966) that the Washington
fusulinid fauna described by SKINNER &WILDE (1966) represents a slightly older
fauna than the fusulinids described here
from the Chilliwack area. However, we
do not have enough well preserved
schwagerinid material to describe andto see if they correlate with the Black
Mountain fauna of SKINNER & WILDE.
The Chilliwack area early Permian ParaJusulina zone seems to correlate mostclosely with zone H in the McCloud
Limestone of California (SKINNER &WILDE, 1965) and is of early Leonardianage. The Chilliwack fusulinid fauna
appears to be younger than most of theeastern facies of the Cache Creek Groupto the north in the Kamloops area of
British Columbia.

Locality Ml: (James MONGER thesis
locality No.5) Limestone on side of
logging road, just north of saddle, 2!
miles south of Bridal Falls, altitude 4,000
feet. South side of Fraser River valley.
Locality Dl: Talus blocks from hillside above lower forks of Liumchen
Creek. Along logging road and in creek
bed. Altitude about 2,000 feet. Manyof the fusulinids are silicified.
Systematic Paleontology

Subfamily Fusulininae von MOLLER, 1878
Genus PseudoJusulinella THOMPSON, 1951
Type-species :-NeoJusulinella occidentalis THOMPSON & WHEELER, 1946
PseudoJusulinella danneri
SKINNER & WILDE
PI. 11, figs. 1-13

1966. Pseudofusulinella danneri SKINNER &WILDE.
Pal. Contrib. Univ. Kansas,
Paper 4, pp. 42-43, pI. 34, figs. 1-5.

Description:-The shell of PseudoJusulinella danneri SKINNER & WILDE is small
and thickly fusiform, having a straightaxis of coiling and moderately pointed
poles. The lateral slopes are straightto slightly concave. The mature shellsof seven to nine volutions of eight specimens are 5.25 to 7.00 mm. in length and2.75 to 3.67 mm. in width. The form
ratio ranges from 1.81 to 2.32.
The outside diameter of the pro loculus
varies from 75 to 207 microns, commonly
113 to 188 microns. The shell is tightly
coiled in the inner three volutions andexpands rapidly and uniformly in theouter volutions. The radius vectors of

76

Kimiyoshi SADA and Wilbert R. DANNER

the 1st to the 9th volution of eight specimens are 94-132, 118-226, 245-321, 358491, 491-673, 675-887, 849-1170, 1435-1095
and 1748-1824 microns, respectively. The
heights of the chambers are about thesame throughout the length of the shell
excepting in the extreme polar regions.
There the chambers slightly increasein height.
The spirotheca is thin and composedof the upper and lower dense layers, atectum and a thin porous layer. The
thickness of the spirotheca of the 1st to
the 8th volution of eight specimens is16-50, 23-50, 29-69, 29-96, 34-98, 36-92,
59-105 and 46-121 microns, respectively.
The proloculus wall is thin and its average thickness measures 37 microns.
The septa are almost plane in theregion of the tunnel and closely fluted
in the extreme polar regions. The septal
counts of the 1st to the 7th volution ofa specimen illustrated as Fig. 11 on PI.
11 are 11, 15, 20, 22, 23, 32 and 32, respectively.
The chomata are well developed
throughout the growth of the shell,reaching nearly to the tops of thechambers. The tunnel angles are 18 to
23 degrees in the 8th volution.
Remarks and comparison:- The present specimens resemble Pseudofusu!inella danneri SKINNER & WILDE moreclosely than any other known speciesof the genus in the shell-shape, theinternal characters and the statistic

data. P. danneri was originally describedby SKINNER & WILDE (1966) from thePermian Chilliwack Group in the Black
Mountain area, northwester.n<Washing"ton. This species was mainly characterized by the thick fusiform shells, thelarge proloculus for a member of thisgenus, the well developed chomata andthe straight to slightly concave lateralslopes of the shells. The last one plays
an important role in the specific variation of this species. As shown by the
figures of the holotype and the paratypes, this reveals considerable variationin the shell shape. The holotype (SKINNER & WILDE, 1966, pI. 34, fig. 1) is thickfusiform with concave lateral slopes but
the paratypes (SKINNER & WILDE, 1966,
figs. 2 and 3) are thick fusiform withstraight lateral slopes. We here designate the holotype as a-form and theparatypes as j9-form.
The specimens we described are also
as variable in their shell-shape as the·original specimens of the species described by SKINNER & WILDE (1966). Thespecimens illustrated here as Figs. 1, 2"
and 4 on PI. 11 coincide with a-form and.
the other specimens illustrated as Figs.
5 to 10 on the same plate are referableto j9-form in the shell-shape. The lateral slopes of the former are concaveand the ones of the latter are straight ..
Of these specimens the forms illustrated as Figs. 8 to 10 on PI. 11, allbelonging to j9-form, are somewhat larger

Explanation of Plate 11
All x 10 except fig. 13
Figs. 1-13. Pseudo/usulinella dalllleri SKI,,""ER & WILDE
1-10. Axial sections; Rg. No. M44, M42, M34, M43, M49, M48, M41, M45, Dl and M46,.
respectively. 11-12. Sagittal sections: M50 and 07, respectively. 13. Enlargecf
figure of fig. 10 showing wall structure. x 123.
Photos by K. SADA.

SADA and DANNER : Fusulinids from Chilliwack, B. C.

Plate 11

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I:'<.0Type-species :-Parafusulina wordensis
DUNBAR & SKINNER, 1931.

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Subfamily Schwagerininae DUNBAR& HENBEST, 1930
Genus Parafusulina DUNBAR

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than the holotype and paratypes of P.
danneri in size. having 6.35 to 7.00 mm.
in length and 3.10 to 3.67 mm. in widthof the shells. However, these specimens
quite resemble the paratypes of thespecies in the shell-shape and .the otherinternal characters of the shells. Therefore we can hardly avoid the conclusionthat these should be the fully grownspecimens of Pseudofusulinella danneri.
The present specimens are somewhat
similar to Pseudofusulinella pinguis
SKINNER & WILDE (1965, p. 38, pI. 53,
figs. 6-10) from the upper part of the
McCloud Limestone of northern California and (1966, p. 12, pI. 9, figs. 2-5)
from Coyote Butte Limestone in Suplee
area, east-central Oregon. However,they can be easily distinguished by thesmaller form ratios, the smaller tunnel
angles, the convex lateral slopes of theshells and the weaker septal fluting of
the latter species.
Occurrence:-Abundant at Loc ... Ml "and Loc. " Dl " in Chilliwack area, southwestern British Columbia. The specimens illustrated as Figs. 1-8. 10-11 on
PI. 11 came from Loc ... Ml " and figs. 9
and 12 from Loc. " Dl ".

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Parafusulina 11l01zgeri SADA &DANNER, sp. nov.

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PI. 12, figs. 1-5; PI. 13, fig. 4

Description :-The shell of Parafusulina mongeri SADA & DANNER, sp. nov.

78

Kimiyoshi SADA and Wilbert R. DANNER

is large and elongate cylindrical, witha straight axis of coiling and bluntly
pointed to rounded poles. The lateralslopes are convex. The shell of theholotype (PI. 12, fig. 1) is 15.75 mm. in
length and 3.67 mm. in width. Its form
ratio is 4.29.
The outside diameter of the proloculus
is 250 to 450 microns. The proloculus
wall is 18 to 37 microns. The radius
vectors of the 1st to the 7th volution offour specimens are 50-250, 350-450, 450650,600-900,800-1250, 1050-1600 and 15002250 microns, respectively. The chamberis nearly the same in height throughout
the length of the shell except the polar
regions.
The spirotheca is composed of a tectumand coarsely alveolar keriotheca. The
thickness of the spirotheca is 18-56, 1837, 18-56, 56-75, 56-151 and 56-151 microns, respectively, for the 1st to the
6th volution.
The septa are thin, closely spaced,narrowly. highly and regularly fluted
throughout the shell. Cuniculi are present in the outer volutions. The septal
counts of a specimen are 14, 27, 29, 34,
41 and 40, respectively, for the 1st to
the 6th volution. The tunnel is very
narrow and less than 30 degrees in theouter volutions. The chambers along
the axial region of the inner four tofive volutions are filled with dense deposits.

Remarks :-Parafusulina mongeri SADA
& DANNER, sp. nov. resembles P. laudoni
SKINNER & WILDE from northwestern
Washington more closely than any otherknown American species belonging to
the genus. However, the former species
can be distinguished from the latter by
its cylindrical shell, the slower expansion of the shell, the smaller proloculus,
the weaker and more regular septal
fluting, the lighter axial fillings and thesmaller tunnel angle. Parafusulina mongeri. sp. nov. bears a certain similarity
to P. belcheri THORSTEINSSON (in HARKER& THORSTEINSSON, 1960, pp. 29-30, pI. 9,
figs. 1-5; pI. 10, figs ..1-5) from Grinnell
Peninsula, Arctic Archipelago. The major difference between these two species
is that P. belcheri is smaller at maturity,
has weaker septal fluting, a broad tunnel angle and no axial fillings.
Occurrence:- Abundant at Loc. "D1 "in Chilliwack valley, British Columbia.
All of the illustrated specimens (PI. 12,
figs. 1-4; PI. 13, fig. 4) came from Loc.
o. Dl".
Parafusulina laudoni SKINNER & WILDE
PI. -13, figs. 1-3, 5-6

1966. Parafusulina laudoni SKINNER & WILDE.
Pal. Contrib. Univ. Kansas, Paper 4, pp.
43-44, pI. 36, figs. 2-5.

Description :- The shell of Paraf2lsu-

Explanation of Plate 12
All x 10 except fig. 5
Figs. 1-4. Parafusulina mongeri SADA & DAN:-IER, sp. nov.
1. Axial section of holotype: Rg. No. D20. 2-3. Axial sections of para type: Rg. Nos.
D16 and DI4, respectively. 4. Sagittal section: Rg. No. DID.
Fig. 5. Tangential section of Parafusulina laudoni SKINNER & WILDE showing cuniculi.
x 66.6. Reg. No. M46.
Photos by K. SADA

SADA

and D ANNER:

F'/,~su linids j1"Om Chilliwack, B. C.

Plate 12

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79

lilla laudoni SKINNER & WILDE is large
and elongate subcylindrical, having astraight axis of coiling, bluntly pointed
poles and convex lateral slopes. The
shell of eight volutions of the typical
specimen (PI. 13, fig. 1) is 17.00 mm. longand 4.35 mm. wide, giving a form ratioof 3.90.
The proloculus is large and sphericalto subspherical. Its outside diameter
ranges from 350 to 550 microns. The
pro loculus wall is thin, measuring 37
microns. The radius vectors of the 1st
to the 8th volution are 264-350, 434-550,
661-800, 887-1100, 1208-1600, 1605, 1907
and 2304 microns, respectively. The
chamber is nearly the same in height
throughout the length of the shell except at the extreme polar regions .
The spirotheca consists of a tectumand coarsely alveolar keriotheca. The
thickness of the spirotheca of the 1st to
the 8th vol uti on of two specimens is 37,
37, 37-56, 56-94, 75-113, 94, 113 and 113
microns, respectively.
The septa are strongly fluted throughout the length of the shell. The phrenotheca are developed partly in the outer
volutions. The septal counts of a specimen (PI. 13, fig. 5) are 11, 22, 31, 40, 43
and 44, respectively, for the 1st to the
6th volution. Their number in the 7th
volution is unknown because of the incomplete test. Cuniculi are present in
the outer volutions. The tunnel angles
are 40 to 45 degrees in the 6th volutionof a typical specimen. Heavy dense deposits are present along the axial region.
Remarks:- In the shell-form, the internal biocharacters and the measured values, the present specimens show striking
similarities to the specimens describedunder the name of Parafusulina laudoni
by SKINNER & WILDE (1966) from thePermian Chilliwack Group on the northside of Black Mountain in Whatcom

80

Kimiyoshi SADA and· Wilbert R. DANNERCounty, Washington. They may be conspecific. The typical specimen (PI. 13,
fig. 1) is slightly larger in size. than theholotype (SKINNER & WILDE, 1966, pI. 36,
fig. 2) of P. laudoni. but this falls within
the limits of the individual variationof the species.
Occurrence:-Abundant at Loc. "M1"
in Chilliwack area, British Columbia.
All of the .illustrated specimens (PI. 13,
figs. 1-3, 5-6) came from Loc. "M1 ".
References
CAIRNES, C.E. (1944): Hope Sheet; Ceol.
Survey Canada Map 737A.
COOGAN, A.H. (1960): Stratigraphy and Paleontology of the Permian Nosoni and
Dekkas ·Formations (Bollibokka Group).
California Univ., Pub. Ceol. Sci., Vol. 36,
no. 5, pp. 243-316.
DALY, R.A. (1912): Geology of the North
American Cordillera at the forty-ninth
Parallel. Ceoi. Survey Canada Memoir 38.
DA)I:-;'ER, W.R. (1957): Stratigraphic reconnaissance in the Northwestern Cascade
Mountains and San Juan Islands of Wash-

ington State. Unpublished Ph. D. thesis"
Univ. of Washington.
HARKER, P. & THORSTEI:'<SSO:'<, R. (1960);Permian rocks and faunas of Grinnel Pe-·ninsula, Arctic Archipelago. Ceol. Surv ..
Canada Mem. 309, pp. 1-89.
HILLHOUSE, D.N. .(1965): Geology. of theVedder Mountain (Silver Lake) Area ..
Unpublished M. Sc. thesis, Univ. of Brit··
ish Columbia.
MO:"GER, ].W.H. (1966): The stratigraphy
and structure of the type-area of the:Chilliwack Group, Southwestern British
Columbia. Unpublished Ph. D. thesis,
Univ. of British Columbia.
SKI:"1\ER, ].W. & WILDE, G.L. (1965): Per-mian biostratigraphy and fusulinid fau-·
nas of the Shasta Lake area, northern
California. Pal. Contr. Univ. Kansas,.
Protozoa, Article 6, pp. 1-98.
SKI:'INER, J.W. & WILDE, G.L. (1966): Per··
mian fusulinids from Pacific Northwest.
and Alaska. Pal. Contr. Univ. Kansas ..
Paper 4, pp. 1-64.
THO:\1PSO:", M.L., WHEELER, H.E. & HAZ·
ZARD, ].C. (1946): Permian Fusulinids.
of California. Ceal. Soc. Amer;, Mem ..
17 p. 1-77.

Explanation of Plate 13
All x 10
Figs. 1-3, 5-6. Parafusulina laudoni SKINNER & WILDE
1-3. Axial sections: Rg. Nos. M52, M53 (the immature specimen) and M39, respectively._
5-6. Sagittal sections: Rg. Nos. M59b and M59a, respectively.
Fig. 4. Parafusulina mongeri SAD A & DANNER, sp. nov.
4. Axial section: Rg. No.. D23.
Photos by K. SAD A,

SADA and DANNER:

Fusulinids ft"om Chilliwack, B. C.

Plate 13

"Trans. Proc. Palaeont. Soc. Japan, N. S., No. 90, pp. 81-94, June 30, 1973

'617.

OMMA-MANGANJIAN MOLLUSCAN FAUNA IN THE
FUTATSUI AREA OF NORTHERN AKITA, JAPAN*
KIYOTAKA CHINZEI
Geological Institute, University of Tokyo, Hongo, Tokyo 113

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.saishuensis, Macoma tokyoensis, Mercenaria stimpsoni ;'".: c;:-t;r.il&-:5it Gh:Qll'f.!t, :to
J:.V::rf:I;:fl\O)/J'IKlljJU:.;l;.G~l,:Q Felaniella usta, Thracia kakumana O)II'f.~"C:·£>Qo !iHIi*1E
1~.;!F>O)rl:lf.!Lli'Hflf:'f1, Umbonium akitanum, Glycymeris yessoensis O)~\I'/tl!~:.ll'f.ill£> I),,,::,1,1,~(&1:.$*J[li:J;'i'tt~T Q, 5 'lI.H~ O)ll'f.~ c L- -C t&?, ..::.ll G O)llf~O) 5J::tnf'j: ~'t;;fBO)5J:.{rjc --f'il: L. -to)tJ1I1fi:fIlO)tQ c c t ::'II~nllITiP,r-IJJ:Q, -7j:' O)ffl_Hrr*1t}1~1* c VCrnill o i;Jt
ifiHI:O)(tTirliJ"""fI:.:t31t :Q:tIWWI) C '1!IJIl9i~;j1" tl'f.~0)1I!f]?7~::tn'1, 1,~*S~f:'f1i1tiO)i;JtIr., i1ti:h.ilto)

c 'v'? mj:;r~lr.f:'1:~c~ ~'l-o~~, ~llf~0)j:JH'j!.0)11'r.llit;1 ~"";;fI'lO)5J:.{fi::.j;;lIi.E~ h-Clt':Q ,!:",;t:Q, i- tJ: *:>'1,,' TII'[ip G _H"U'O)llf-lil~O)tJF7IH1, ~WfO)iltJllff:..:t;:t :Q i~jirril' Gi;Jtjijf",O)ll'f.
.~o)~,II:~£>QI',~gri:."C:-ff;I~T:Q t;l;.-C J:. 'v', ='/:J:j:"C:-,~G;/'lQ :'O)J:.?;,".: R'f.~~c-tO);fII
E:IVilllM1, *~~7}l~iW!jM7ljll'f'O) --?O)I\::~(l~;'"dIJ c ,'IT!.:bh, liT] r k:1l.11XOYII'f.~illtr-JI!!.I:'iWlO G
m~'

~l,Q,

~1!

j11:j

ii!t

ji1lj

He regarded the fauna as representative of the off-shore assemblages of the
Pliocene in Northeast japan, and compared it with the shallow sea assemblages of the Tatsunokuchian fauna.
In detail, however, the composition of
the fauna varies remarkably in different
areas and at different localities, even inareas typical of the Omma-Manganjian
fauna such as Kanazawa (HATAI andNISIY AMA, 1939; KASENO and MATSUURA,
1965) and Manganji in southern Akita(OTUKA, 1936). This suggests that thefauna includes assemblages representing
various types of environments, and thatthe fauna does not always represent anoff-shore community. Detailed analysis
has only been done by KASENO andIntroduction'The molluscan fauna in the marine
Pliocene of the japan Sea coast of Hon'shu has been generally called the Omma'Manganjian fauna. The name was pro1l0Sed by OTUKA (1939a) who described-the fauna as "a fauna of the japan Sea·during the Pliocene ". It has been;thought to be composed of cold deep
water inhabitants (OTUKA, 1939b; HATAI;and NISIY AMA, 1939 etc.). CHINZEI (1963)
noted that species characteristic to the:fauna are mostly dwellers of off-shore
muddy or fine sandy bottoms with elements intermingled from gravelly facies.

* Received Nov_ 17, 1972; read Jan. 16,..1973 ,at SendaL

81

82

Kiyotaka CHINZEIMA TSUURA (1965) on the fauna in the
Kanazawa area. KASENO and MATSUURA
concluded that the molluscan fauna of
the Omma formation is composed mainlyof upper sublittoral species, although
the shells are mostly transported andmixed with those of different habitats.
In this paper, the writer will presenta brief description of the molluscan
assemblages in the Pliocene deposits of
the Futatsui area, northern Akita Prefecture. This area is known as one
where molluscan fossils belonging to
the Omma-Manganjian fauna are foundabundantly.
Analysis is made of the modes offossil occurrence and the type of sediments that contain the fossils. Fivetypes of molluscan assemblages can be
distinguished when discussion is confined to the autochthonous individuals
or individuals transported only a shortdistance. Each type of assemblage ischaracterized by two or three predominant or common species, and is in aparticular sedimentary facies. In thisrespect, an assemblage may be regarded
as a unit whose constituents have aclose ecological relationship to eachother.
The combined occurrence of theseassemblages including the species composition of each assemblage is considered to be typical of the Omma-Manganjian type molluscan fauna.
Acknowledgements: Professor Tetsuro
BANAl and the writer's colleagues at the
Geological Insitute, University of Tokyo
made valuable suggestions during thecourse of the study. Comments on stratigraphical problems were made by Dr.
Jiro HIRAYAMA of the Geological Surveyof Japan. The manuscript was read byProfessor T. HANAI, and Mr. John
GRIMMER of the University of California, Los Angeles. The writer wishes toexpress his deep thanks to these persons_Outline of stratigraphy and descrip ..
tion of sedimentary facies

The Futatsui area is situated at thenortheastern corner of the Akita oilfield. The upper part of the marine
Neogene is exposed in this area forming gentle folds with a NNE-SSW trend.
The stratigraphy of the Neogene deposits in this area is similar to that in
the type-section of the oil-field in the
Akita area. In the study area the formations are dominated by marine clastic
deposits, while the Neogene deposits
exposed to the immediate east and thenorth of the study area are rich inaltered volcanic materials known as theGreen-Tuff.
The lowest horizon exposed in thearea is the Upper Nanakura tuff member of the Fujikotogawa formation (HIRAY AMA and SUMI, 1963). It is composedof fine acidic pumices containing large
numbers of pumice blocks and otherlithic fragments. The tuff is correlatedwith the top of the upper Miocene Funakawa formation of the Akita area.
The Upper Nanakura tuff is overlain
conformably by a grey massive siltstone
more than 450 m thick. This siltstone
is a part of the Kobinaizawa formation(HIRA Y AMA and SUMI, 1963). The mainpart of the siltstone is correlated with
the Tentokuji formation as judged fromthe stratigraphic position and lithology_
It is a coarse-grained homogeneous siltstone, and is tuffaceous, containing
small fragments of volcanic glass, plagioclase, hornblende and other crystals.
Thin layers of pumice-tuff and tuffaceous fine-grained sandstone are foundrarely. The upper part of the siltstone
becomes sandy. and is intercalated byvery fine-grained silty sandstone. Mol-

617.

Text-fig.!.

Omma-Manganjian fauna

83

Geologic map and fossil localities of the Futatsui area.

1-63: fossil localities; A-M: the locations where the columnar sections (Text-fig. 2) aremeasured. Symbols for geologic m:!!); 1: sands and gravels, 2: bedded pumice tuff,
3: fine- and medium-grained sandstone, 4: siltstone, 5: the Upper Nanakura tuff.

Kiyotaka CHINZEI

84

lu~can remain~ are found ~poradicallyin the upper horizon of the siltstone.
They are the assemblage of muddy
facies referred to in the following sections. Foraminifera are also found in
the siltstone.
Near the northeastern corner of thearea, between Locs. 49 and 51, a conglomerate lens 50 em to 2 m thick isintercalated between the siltstone andan overlying fine-grained sandstone.
It is composed of andesitic granules andpebbles, and contains abundant waterworn fragments of shells.
The siltstone is overlain conformably
by fine-grained sandstone. The sandstone probably corresponds to the Sasaoka formation of the Akita area although
the stratigraphic relationship between
the two is not possible to ascertain
directly because the sandstone is sepa-

rated from other areas of the oil-fieldby anticlinal highs of the underlying
formations. The lithology of the sandstone resembles the Tofuiwa facies(T AKA Y ASU, 1861) of the upper Sasaoka
formation at the type locality. The
sandstone is massive or very weakly
bedded with interbedded layers of pumice-tuff. It is mainly composed of wellsorted grains of volcanic rocks, crystals
and pumices. The sand fraction is 75 to
85 percent in general, and the modes ofthe frequency distributions of the grains
average approximately 3.5¢. Medium- tocoarse-grained strata are exceptionallyseen in the lower part of the sandstone
in the southeastern corner of the area
(columns Land M in Text-fig. 2). Thinlayers of siltstone are also seen in thesouthwest. The sandstone contains richmolluscan fauna. They are grouped in
J

G"
.'

A

M

.... :~.~ ...
L.. :-,. 6' H

B=_=c (0I~= =.

bJ . . .

........................ .

~--~

ft

~ ~
.."
... ---- ..~8E

p( =~- ~ :=: 331"~~
8:
=::==

- -..

D

-~-

'.'.

I-'!,\-.-~~-49- 4iJ

c
~~-

.

·34

3(

_-_

- 24

v

-.2,3

.

=-:- 3K

25:==-:;;
28-_-_ 2=-=- 4-.-. • 20::=::- 32 -::=- u=.

=-_=-_ q_-_ ·21~-."'[f'16"

"=/~

".

~

. yy

-=:- .22

0'1 ---

13

~,/~

1_-

~
" .. ,~

53sz-

Text·fig. 2.

Nanahura tuff

Columnar sections of the upper Neogene deposits in the Futatsui area,
indicating the stratigraphic horizon of fossil localities.

A-M correspond to the localities indicated in Text-fig. 1. Symbols for sedimentary
facies; a: medium-grained sandstone, b: fine-grained sandstone, c: siltstone, d:pumice tuff, e: thin tuff layer, f: conglomerate.

617.

Omma-Manganjian fauna

this paper as the assemblages of thefine-grained sand facies.
As shown in Text-fig. 2, the boundary
between the sandstone and the underlying siltstone obliquely crosses the interbedded pumice-tuff layers which are probably isochronous horizons. The sand~stone occurs at the lowest horizon in
the northeastern part of the area while
the uppermost horizon of the siltstone
is seen in the western part of the area.
The sandstone is thickest in the northeast where it is approximately 400 m
thick. It is 250 to 300 m thick in thewest.
The upper part of the sandstone
grades upward into a medium-grained
loose sandstone mineralogically similar
to the fine-grained part. This mediumgrained sandstone is poorly stratified
and rich in pumice grains. A clusterof molluscan shells was found in a lower
horizon of the medium-grained sandstone in the western part of the area
(Loc. 63 of Text-fig. 1). Median diameter of the grains of the sandstone at
Loc. 63 is 2.11> and the sand content isapproximately 65%.
The sandstone is overlain by wellbedded light grey pumice tuff beds.
The tuff beds are covered by thickalternating sands and gravels which
form the plateau of Oonotai. JUdging
from their sedimentary features thesetuff and gravel beds were consideredby HIRAYAMA and SUMI (1963) to be offresh water origin. As they are nearlyhorizontal, they probably cover the underlying slightly inclined sandstone unconformably.
Modes of fossil occurrence

The sediments in which fossil molluscs are found can be divided into fourtypes, mud, fine-grained sand, medium-85

grained sand, and gravels. The modesof fossil occurrence can be closely correlated with these sediment types.
1. Muddy facies. The muddy facies
fauna is most common in the siltstone
beds which correspond to the Tentokuji
formation. The fauna also occurs sporadically in silty layers interbedded in thelower part of the fine-grained sandstone.
Molluscs are scattered in the siltstone
with a frequency, in general, of 1 to 5
per square-meter of the outcrop. The
individuals usually do not have a particular orientation. At Locs. 14 and 40,
such flat shells as Nuculana and Pandora,
are found lying parallel to the bedding
planes of thin patches of very finegrained sandstone. Most of the bivalvesoccur with conjoined valves except forsome specimens of Serripes groenlandica.
Minute sculpture of the shell-surface
and even fragile protoconchs of somegastropods are well preserved. Thereis no indication of transportation.
2. Fine-grained sand facies. Fossils
can be seen at most of the exposuresof the fine-grained sandstone, and they
are especially abundant in the westernarea. In the usual case, they are scattered very densely, and do not form
particular fossil beds. Exceptions arefound at Locs. 22, 31, 36, 38, 39 and 43,
where the shells are clustered in beds.
The number of individuals varies from
6 (Loc. 62) to more than 400 (Loc. 45)
per square-meter of exposure surface.
Bivalves are mostly conjoined evenwhen occurring in clusters. They are
randomly oriented in the sandstone except for Mya cunei/armis which is nearlyvertical with the posterior upwards.
Gastropods, represented abundantly by
Turritella saishuensis, do not show any
marked orientation. The majority ofbivalves and gastropods do not show
evidence of transportation by water.

86

Kiyotaka CHlNZEI

3. Medium-grained sand facies. A
bed of shells was found at Loc. 63 in
the medium-grained sandstone. It is alens 20 cm in maximum thickness andmore than 6 m in length. Bivalves areinvariably represented by odd valves
which are arranged parallel to the bedding plane. Broken and fragmental
shells are abundant. Although the surface sculpture of the shells is well preserved, they were undoubtedly transported and accumulated by water. Testsof the flat echinoid, Echinarachnius d.
humilis Nisiyama. are found in the lower
part of the shell bed.
4. Gravel facies. The gravel facies
Table 1.

fauna is found in the lenticular conglomerate at the base of the fine-grainedsandstone. Molluscs are all worn andbroken. They are mixed with the gravels. The shells were probably transported by water from remote places.
Molluscan assemblages

Judging from the modes of occurrence
described above. the molluscs found in
the muddy and the fine sand facies canbe regarded as autochthonous, preservedat or near the place of their origin_
The species observed at an outcrop are
considered to have some ecological rela-

List of molluscan fossils found in muddy facies in the Futatsui area.
NuauZana - TurriteZZa nipponiaa
Locality

12 13 14 17 18 23 24 27 40 48 49 50 51 52 53 56 57

Species, TurriteZZa nipponiaa YOKOYAMA00
FuZgoraria prevostiana (CROSSE)
Buaainum tsubai KURODA
Neptunea sp.
Teatonatiaa tugaruana (NOMURA & RATAI)
Fusitriton oregonensis (REDFIELD)
PropebeZa op.
Admete tabatai (YOKOYAMA)
ReatipZanes sadoensis (YOKOYAMA)
TurriauZa kaderZeyi (LISCHKE)

.

0 0-·

.·
·•
0

--.

NuauZana robai KURODA
Maaoma aaZaarea (GMELIN)
Serripes groenZandiaa BRUGUIERE
Pandora puZaheZZa (YOKOYAMA)
AaiZa cf. insignis (GOULD)
Limopsis tokaiensis YOKOYAMA
LimatuZa kurodai OYAMA
Panomya beringiana DALL
Panomya simotomensis OTUKACZinoaardium sp.
PortZandia japoniaa (ADAMS et REEVE)
NuauZana sp.
EnnuauZa tenuis (MONTAGU)
NuauZana yokoyamai KURODA
Luainoma aautiZineatum (CONRAD)
Veneriaardia ferruginea (CLESSIN)
PeripZoma s,P.
PaZZioZum peakhami (GABB)
Astarte boreaZis (SCHUMACHER)
Thyasira biseata (CONRAD)
SiphonodentaZium sp.

0
•

---

•

0

-

0-0

•

0

0

·
·

.

--e

---

00 0 0 - · 0 - 0--· - - 0 - - 0 - 0--0

0-

0-_0

0

--0

.
0--

··

•

.

0

(!)

0

·

0

0-0

•

.

0

.

0

---0

,

0-0
0

.

-

0

,
I

!

0
0

0

•
--e--o

•

,

0

.-,

0

0

Individual number / m2 of outcrop;(!)

10 - 6, 05 - 3,

• < 2

617.

Omma-Manganjian faunationship to each other.
Molluscs found in the medium-grained
sand facies were apparently transported
as noted above. They are, however,treated here tentatively as an assemblageof the medium-grained sand facies since
they are thought to have lived not far
from the place of deposition jUdging
from the state of preservation. The
assemblage contained in the gravel
facies is a mixture of species from morethan one habitat.
1. Muddy facies
Molluscs found in the muddy facies
are listed in Table 1. The differencein species compositIOn by locality is
noticeable. This may result partly fromthe chance of observation because thedensity of individuals in the sedimentis extremely low.
The muddy facies fauna is characterized by a richness of gastropod
species compared with the assemblages
in the fine-grained sand facies. The
fauna may be called the NllculanaTllrritella nipponica* assemblage sinceNllculana robai and Turritella nipponica
a.re the species most commonly seen in
the muddy facies. Other characteristic
species of the assemblage are Rectiplanes sadoensis, Fulgoraria prevostiana,
Buccinum tsubai, Neptunea sp., Admetetabatai, Macoma calca/'ea, Pandora pulchella, Panomya beringiana, Thyasirabisecta, Portlandia japonica, etc. The
assemblage is typically seen at Loc. 24.
Tllrritella nipponica is relatively common in the upper part of the siltstone
and in the silty layers interbedded in
the fine-grained sandstone. In these* Because two species each of Turritella,
Macoma, and Acila are recognized in thisarea, the assemblages are termed by the
species names in order to discriminate between them.

87

lithologies the species associated with
T. nipponica are more or less different
from those found in the typical assemblage. Nuclliana robai and gastropods
are generally absent. In some localities.
e. g .. Locs. 17 and 18, T. nipponica is.
associated with Limopsis tokaiensis andno other molluscan species. Limopsis
tokaiensis is commonly found in the
Turritella- Limopsis- Acila assemblageof the fine-grained sand facies. These
facts suggest that the variety of assemblage characterized by T. nipponica andLimop5is tokaie11.sis is the transitional
between the typical muddy facies assemblage and the fine-grained sandfacies assemblage.

2.

Fine-grained sand facie3
The molluscan fauna contained in thefine-grained sand facies is characterized
by the predominant occurrence of Turritella saishllensis motidllkii, Mya cuneifonnis and A/acoma tokyoensis, except
in the northeastern part of the area
where the former two species are rare_
The fauna can be divided into two major
assemblages on the basis of the difference in species associated with the dominant three forms. The assemblages
are Turritella saishuensis- LimopsisAcila nakazimai, and Turritella saishllensis- Macoma tokyoensis- Mercenaria ..
Although no appreciable difference canbe detected between the sediments containing the two assemblages, the stratigraphic distribution of the faunas isdifferent. The Turritella - LimopsisAcila assemblage is concentrated in thelower part of the fine-grained ·sandstone,
whereas the Tllrritella-Macoma-Mercenaria assemblage is characteristic of
the middle part.
In addition to the two assemblages
above, an assemblage dominated by
Felaniella usta and Thracia kakumana

:88

Kiyotaka CHINZEJ
Table 2.

,;,

List of molluscan fossils found in fine-grained

l -.Thrac-z-a J
FeZanie~Za

TurriteZZa saishuensis Limopsis - AciZa nakazimai~eLocality
15 16 19 20 2526 28 29 30 31 33 34 41 42 45 35 36

1Species

TurriteZZa saishuensis
motidukii OTUKA
Mohnia sp.

® -•• - . ®

•® ® ® ®

-.

• ••.-- ·.
®

Macomo. tokyoensis t.ffiKIYA~lA• -e-eMercenaria stimpsoni (GOULD)CZinoca:t'dium sp.
Anada:t>a amicuZa (YOKOY~)•
Protothaca adamsi (REEVE)--e---e e
Mya cuneiformis (BOlm)• e
Thracia kakumana (YOKOY~)ei Serripes groenZandica BRUGUIERE, FeZanieZZa usta (GOULD)!, Dosinia japonica (REEVE), AciZa cf. insignis (GOULD)
GZycymeris yessoensis (JAY)
Patinopecten kuros~ensis (!OKOY~)
Peronidia protovenuZosa (NOMURA)
Lucinoma acutiZineatum (CONRAD)•i Thyasira bisecta (CONRAD)ee
Macomo. caZcarea (GMELIN)0
YoZdia notabiZis YOKOY~
SpisuZa voyi (GABB)
Astarte boreaZis (SCH~CHER)e
Panomya simotomensis OTUKAe
C!)
Venerica:t'dia ferruginea (CLESSIN)®--®
AciZa nakazimai OTUKA-0-- ••
0
Limopsis tokaiensis YOKOY~- - ® - • • ® ®@ ® • - - ®

•Individual number / m2 of outcrop: •'is found in the middle horizon of thefine-grained sandstone.
.a) Tunitella saishuensis-L im opsisAdla nalwzimai assemblage
This assemblage is characterized by·the abundant occurrence of Limopsis.tokaiensis and Acila nalwzimai associatedwith Turritella saishuensis motidukii. In.general 1\1ya cuneiformis, Vellericardia
Jerruginea and i\lJacoma tokyoensis arealso found commonly. Other subordinate
species and individuals are few in number. The associations simply composed-of Tunitella or Tunitella and 1\1ya are.included in this assemblage. This assemblage is concentrated in the lower.part of the fine-grained sandstone and.in the west.

> 10

o 10 - 6, 0®- ®
O - f--

.-

e
e

••
••
• • 0

f--

r--

e - r-e - r-e• r-0 r--

••

5 - 3

e < 2

Detailed study reveals that the association of species found on the same
bedding plane or within a single layer
is simple in composition, but varies withlocality or horizon. The following associations of species can be recognized;
species are arranged in the order ofabundance of individuals.

Turritella (monospecific)
Loc. 20
Tunitella-Mya
Locs. 26, 34
Turritella-Mya-Limopsis
Loc. 33
Turritella- i\lJya- Acila
Loc. 28
Turritella- L imopsis Locs. 26, 29, 31
Turritella-Limopsis- Venericardia
Locs. 30, 45
Tunitella- Acila-Limopsis
Loc. 42
Limopsis- Acila-TurritellaLoc. 26
Limopsis-Acila-Mya
Loc. 26

617.

Omma-J1anganjian fauna

89'sand facies in the Futatsui area.
Turritella saishuensis - Macoma tokyoensis - Mercenaria

I~

3

4

5

6

7

8

9 10 11 21 22 32 37 38 39 43 44 46 47 54 55 58 59 60 61 62• e e@ e e e e e e - - - e - - e e-- @-- 0 -- 0 -- 00. - 0 · ooo--@-@-e--e----o@-o-ooO ••@·--·o·o0-0.
.• • ---.-----. ---@----- • • - .
.- ••• ------.
e----- e - @ • • • - - . - - - - - e •0• 0.--o •• -----. •• 0 .-0 00---0----------•••- - - - - - - - •• -e------.
• • -a----------------------e - - - 0 0 ----------------------0--------0 - - - - - - - - - - •.-e ------------------- e ------------------. ----------- 0

. .

..
•

e

---------------------e--------------------------.----------------------.

.

- - - - - - - - - - - - - - - - - - - - - - - - - - - - . - - - e------- - - - - - - - - - - - - - - - - - - - - - --- - - -----------------------------------0------------------------. ------------------------------------------------------.------------ 0

Limopsis-- Venericardia
Li71l0psis-- Mya• • ---------- 00----------

Loc. 26
Loc. 19

The greatest number of associations arefound at Loc. 26, where five different
associations are observed repeatedly
within a 30 m sequence. The differencesin species associations probably indicate
minor environmental differences. Acila
and Venericardia do not occur together.
This may suggest that the two species
were in competition for the same ecological niche, as the modes of life of thesegenera are quite similar to each other.

Turritella saishuensis-i\;facoma tokyoensis--l\;fercenaria assemblage
This assemblage is characterized by
the common occurrence of lHacorna to-b)

Icyoensis and Afercenaria stimpsoni associated with Protothaca adamsi, Anadara
amicula, Clinocardiul11 sp., Dosinia ja-·ponica. and some other bivalves. Turritella saishuensis l110tidulcii is abundantat most of the localities, and Mya cuneijormis is also commonly found. Other'noteworthy species in this assemblage
are Tellina protovenulosa, Spisula voyi,
Mactra Icuri/wma, and Patinopecten kuro-sawensis although they are rare. These
species have been reported from several
areas of the Omma-Manganjian faunal
distribution as the important constituents of the fauna. A large and wellpreserved shell of Patinopecten kurosall'ensis was collected at Loc. 44. Shells.
of Serripes groenlandica and Glycymeris:
yes soens is were recognized at severaL

'90

Kiyotaka CHlNZEJ

localities. They are rare, ordinarily occurring as single valves, some of which.are broken. These species are probably
not indigenous to the assemblage.
The relative abundance of some of theassociated species is somewhat variable.
The assemblages of Locs. 2 and 21 aredominated by Acila insillnis, and thoseof Locs. 22 and 38 by Anadara amiczila.
In general, Anadara amicula becomesdominant toward the upper horizon of
the fine-grained sandstone. At Locs. 22.and 38, shells of Anadara amicula aremostly conjoined valves which are foundin shell beds 5 to 10 cm thick. Macoma
tokyoensis, Clinocardium sp., etc., arefound in the immediate upper and lower
horizons of the Anadara beds, but are
not seen within the beds.
At Loc. 43, the shells of Turritellasaishuensis, Protothaca adamsi. and 1'vJacoma tokyoensis form an indistinct zone·of shell cluster, while Mya cuneifonnis
specimens are found about 25 to 30 cm
below the Turritella zone in their living
position. These modes of occurrence
seem to compare closely with the life
habits of Recent allied forms. These
Mya probably lived at the same time as
Turritella and other molluscs, and theshell bed seems to have preserved thispart of the benthic community at thetime of deposition.

Macoma tokyoensis, i\lJercenaria stimpson I,
and Tellina protovenulosa are species
commonly associated with the dominant
forms. TZirritella saishuensis and M)'aclllJeljonnis which are abundant in otherassemblages of the fine-grained sandfacies are absent in the shell beds andthe surrounding sediments. A shell bed
composed exclusively of conjoined shellsof Felaniella usta occurs along with the
Felaniella-Thracia bed at Loc. 36.

3. Medium-grained sand facies
As mentioned, molluscs were foundin the medium-grained sand facies only
at Loc. 63 where they form a thin lenticular shell bed. The most abundantspecies in the bed is Umbonium akitanum. It is associated with Glycymeris
yessoensis and Dosinia japonica. Small
individuals of Mercenaria stimpsoni andClinocardium sp. are also found in theshell bed. The bivalves are all dissociated. Dosinia, Mercenaria, and Clinocardium are common in the TurritellaMa co 71la- Mercenaria assemblage of thefine-grained sand facies. The assemblage of the medium-grained sand facies
is named the Umboniu71l-Glycymeris assemblage, and tentatively regarded as
typical of the molluscan fauna in themedium-grained sand facies.
4.

c)Felaniella-Thracia assemblage
This assemblage is found only at
Locs. 35 and 36, both in the middle
horizon of the fine-grained sandstone in
the western part of the area. Loc. 35
is situated at a horizon about 3 m lower
than that of Loc. 36. The shells form
a loosely clustered shell bed at each
locality.
Felaniella usta and Thracia kakumana
are dominant at both localities. The
former species is extremely abundant.

Gravel facies
The assemblage found in the conglomerate is identified as a mixture derived
from two or more different habitats.
i\lJercenaria stimpsoni, Felaniella usta, etc.
are found commonly in the fine-grained
sand facies. while the rest of the species,
Glycymeris sp., Patinopecten sp., Swiftopecten sp., are not found from the otherfacies in the study area.

617.

The order of the assemblages corresponds in general to their stratigraphic
distribution as shown in Text-fig. 3.
The distribution of assemblages coincides well with the distribution of thesedimentary facies. The boundary between the muddy facies assemblage andthe fine-grained sand facies assemblage
coincides with the sedimentary boundary
which crosses the isochronous tuff beds
obliquely. Moreover, the muddy facies
mollusc Turritella nipponica and its associates, appear repeatedly in the silty
layers in the lower part of the finegrained sandstone.
Accordingly the
distribution of molluscs is seemingly
controlled by the distribution of sedi-

Discussion

The molluscan assemblages seen in
the upper Neogene deposits of the Futatsui area are summarized as follows:
Muddy facies
Nllculana- Turritell a 11 ippol1 ica assembage

Fine-grained sand facies
Turritella saishuel1sis- Limopsis- Acilanakazimai ass.
Turritella saishuensis-Macoma 10k·
yoensis- Atfercenari a ass.
Felaniella-Thracia ass.
Medium-grained sand facies
UmboniZlIll-Glycymeris ass.

o

ABC

I II

91

Omma-Yfanganjian fauna

E

F

G

H

I I I I I

J

L

K

I

M

I I

I

50Cf,..

o~=0=--0----=--vVvv V-

Text-fig. 3.

§mD~
abc
d

o

0

•

•

@

1

2

.3

4

5

Schematic stratigraphic section of the Futatsui area andthe distribution of the assemblages.

A-M correspond to the localities indicated in Text-fig. 1. Symbols for sedimentary
facies and assemblages; a: siltstone, b: fine-grained sandstone, c: mediumgrained sandstone, d: pumice tuff, 1: Nuculana-Turrilella nipponica assemblage,
2: Turrilella saishuensis-Limopsis-Acila nakazimai assemblage, 3: T. saishuensisMacoma lokyoensis-Mercenaria assemblage, 4: Felaniella-Thracia assemblage, 5:
Umbonium-Glycymeris assemblage.

92

Kiyotaka CHINZEI

mentary facies and not by the timestratigraphic horizon.
The sediments become generallycoarser in the upper horizons, and are
finally covered by fresh water deposits.
The distribution of formations in thearea surrounding Futatsui also indicates
the withdrawal of the marine environment towards the west and southwest
during the Pliocene as discussed andillustrated by UEDA (1965).
Thus the vertical changes in the molluscan assemblages are controlled fundamentally by the regressive change ofenvironment, and the limit of the distribution is defined by that of the sedimentary facies. The vertical successionof molluscan assemblages may also be
indicative of the horizontal or geographical relation of the assemblages. The
muddy facies assemblage probably represents an off-shore, deep water fauna,
while the Turritella-Macoma-Mercenaria or the Umbonium-Glycymeris
assemblages are the near shore andshallow water faunas. The ecologicalrelationship in terms of depth between
the latter two assemblages is not clear;
there is, of course, a difference in sedimentary facies.
This conclusion agrees well withprevious conclusion of the writer (CHINZEI. 1961) regarding the Pliocene molluscan fauna of the Sannohe group ineastern Aomori. In the middle andupper parts of the Sannohe group, theassemblages dominated by Turritellanipponica. Rectiplanes sadoensis, Venericardia ferruginea and other species common to the muddy facies assemblage of
the Futatsui area are found in the central and deeper part of the sedimentarybasin. The assemblages characterized
by Mercenaria, Peronidia, Anadara, Fortipecten and other bivalved species arein the marginal and shallow facies ofthe basin. Genera of the molluscan
fauna seen in the marginal facies of the
Sannohe group. the Togawa faunule, areallied with the genera of the Tun:itella,---;
Macoma- Mercenaria' 'assemblage. Anadam, Dosinia. and some important constituents of the Togawa assemblages
are represented by different species thanthose of the Futatsui assemblages. They
are the same as the shallow embayment
assemblages of the Tatsunokuchianfauna (CHINZEI and IWASAKI, 1967). Consequently, the shallow sea assemblages
seen in the Futatsui area are considered
to be ecologically parallel (THORSON.
1957) to those of the Sannohe area andthe Tatsunokuchian fauna.
Molluscan assemblages composed of
the specics found in the Futatsui area
occur commonly in Pliocene deposits
along the Japan Sea coast of Japan. The
assemblages described by Iw AI (1961)
from the Narusawa formation in the
Nishi-Tsugaru District, Aomori, are characterized by species common to the
Nuculana- Turritella nipponica assemblage and also contain species which
occur in the coarse-grained sand or gravelly facies which have not been recognized in the Futatsui area. The species,
found in the Nuculana- Turritella assemblage are the main constituents of the
mudstone fauna of the Pliocene Nishiyama and Haizume formations in the
Niigata oil-field (lTOIGAWA, 1958).
Among the molluscan assemblages,
reported by TAKA Y ASU (1961) from the'fine-grained sandstone of the Sasaoka,
formation in the Akita oil-field, the assemblage of his Loc. 6 dominated byLimopsis tokaiellsis is identical with oneof the associations seen in the Turritella- Limopsis- Acila assemblage of
the Futatsui area. Other assemblages.
of the Sasaoka formation are mixturesof elements belonging to two or three617.

Omma-l1<langanjian faunadifferent assemblages in the Futatsuiarea. This conclusion is supported by
the observation made by TAKA Y ASU(1961) that the shells of these assemblages are mostly odd valve~alld broken. The same is true for the assemblages contained in the Omma formationin Kanazawa.
Some of the species characteristic of
the Omma-Manganjian fauna in otherareas are absent or very rarely foundin the Futatsui assemblages. They aresuch gastropod as Epitonium spp., Cerastoderma spp., Trophonopsis spp., and thebivalve Astarte borealis and allied species, Chlamys spp. and other pectin ids,
etc. They are most likely constituentsof assemblage(s) whose habitats did
not exist in the Futatsui area.

References
CHI,\ZEI, K. (1961): Molluscan fauna of the
Pliocene Sannohe group of Northeast
Honshu, Japan. 2. The faunule of the
Togawa formation. jour. Fac. Sci., Univ.
Tokyo, Sec. 2, vol. 18, pt. 1, pp. 81-131,
pis. 1-4.
- - (1963): Notes on historical change of
Neogene molluscan assemblages in Northeast Japan. "Fossils", no. 5, pp. 2026 (in Japanese].
- - and IWASAKI, Y. (1967): Paleoecologyof shallow sea molluscan faunae in the
Neogene deposits of Northeast Honshu,
Japan. Trans. Proc. Palaeont. Soc. japan,
N. S., no. 67, pp. 93-113.
HATAI, K. and NISIYAMA, S. (1939) : Remarks
on certain fossils from the borderlandof the Japan Sea.
japan. jour. Ceol.
Ceogr., vol. 16, nos. 1-2, pp. 123-154, pI. 9.
HIRAYA:-IA, J. and SDH, K. (1963): Explanatory text of the geological map of

9'J9Japan, scale 1 : 50,000, "Takanosu". Ceol.
Surv. japan.
!TOIGA\\'A, J. (1955): Molluscan fossils fromthe Niitsu, Higashiyama and Takezawa
oil-fields, Niigata Prefecture', Japan.
Mem. Call. Sci., Univ.>Kyoto, Ser. B,
YOI. 24, no. 4, pp. 249-263, pis. 1, 2.
1\\",<\1, T. (1960): Pliocene Mollusca from the
Nishi-Tsugaru district, Aomori Prefecture, Japan. Saito Ho-on Kai Mus., Res.
Bull., no. 29, pp. 35-45, pI. 4.
KASE:\O, Y. and MATsccRA, N. (1965): Pliocene shells from the Omma formation
around Kanazawa City, Japan. Sci. Rep.,
Kanazawa Univ., vol. 10, no. I, pp. 2762, pis. 1-20.
OTl'KA, Y. (1936): Pliocene Mollusca from
Manganzi in Kotomo-mura, Akita Pref.,Japan. jour. Ceo!. Soc. japan (Trans.
Proc. Pa!aeont. Soc. japan), yol. 43, pp.
726-736, pI. 41.
- - (1939a): Mollusca from the Cainozoic
system of eastern Aomori Prefecture,
Japan. jour. Ceo!. Soc. japan, vol. 46,
no. 545, pp. 23-31, pI. 2.
- - (1939b): Tertiary crustal deformationsin Japan, with short remarks on Tertiary
palaeography. jubilee Publ., Comm. Prof.
H. Yabe, vol. 1, pp. 481-519.
TAKAYASL', T. (1961): On stratigraphy andfossil fauna in the environs of Tofuiwa rnorthern part of Akita City, Akita Prefecture; Study of Cenozoic fossil fauna,in the region of Akita oil-field (part 1).
Rept. Res. Inst. Undergr. Res., Mining'
Coil., Akita Univ., no. 25, pp. 1-14, pis.
1-3.
THORSO:\, G. (1957): Bottom communities(Sublittoral or shallow shelf). In Treatise on Marine Ecol. Paleoecol., Ceo!.
Soc. Amer., Mem. 67, vol. 1, pp. 461-534.
VEDA, R. (1965): Stratigraphy and tectogenesis of the Tertiary system of North
Akita Prefecture, Japan.
Rept. Res.
Insf. Undergr. Res., Mining Call., Akita
Univ., no. 32, pp. 1-71.

94

Kiyotaka CHINZEI
Fujikotogawa
Funakawa
Futatsui
HaizumeKanazawa
Kobinaizawa
Manganji
Nanakura
Narusawa[f!

zt JIIrun

JII:.J:I:

:'/

'*-

m

{t

iH
IJ' it rJ~ iR]J ~n 1i'
t

~

111"-

i[\

"."

Nishitsugaru
Nishiyama
Omma
SannoheSasaoka
Tatsunokuchi
Tentokuji
TogawaTofuiwa

i1§
i1§

if:

n
UJ

7-:.

~

fi

1ft
",

'Il.

rW]
(J)

1=1

X. 1I& 11'
)If
4
.R

/I',!J~.I~.

Explanation of Plate 14
Fig. 1. Anadara amicula (YOKOY A:'vfA) xl, Loc. 43, Reg. No. eM 8080.
Figs. 2a, b. Macoma calcarea (Gl'vIELlN) xl, Loc. 43, Reg. No. eM 8081.
Fig. 3. Acila (Truncacila) nakazimai OTljKA x 1.5, Loc. 28, Reg. No. eM 8082.
Fig. 4. Felaniella usta (GOULD) x 1.5, Loc. 36, Reg. No. eM 8083.
Fig. 5. Mercenaria stimpsoni (GOULD) xl, Loc. 44, Reg. No. eM 8084.
Fig. 6. Thracia kakumana (YOKOYA1-.1A) xl, Loc. 35, Reg. No. eM 8085.
Fig. 7. Rectiplanes sadoensis (YOKOYA:'vIA) x 1.5, Loc. 49, Reg. No. eM 8086.
Fig. 8. Limopsis tokaiensis YOKOYA~IA x 1.5, Loc. 30, Reg. No. eM 8087.
Figs. 9a, b. Tectonatica tugaruana NO:'vIURA and HATAI xl, Loc. 53, Reg. No. eM 8088.
Fig. 10. Nuculana robai (KURODA) x2, Loc. 24, Reg. No. eM 8089.
Fig. 11. Umbonium (Suchium) akitanum SUZUKI x 1.5, Loc. 63, Reg. No. eM 8090 ..
Fig. 12. Turritella saishuensis motidukii OTUKA x 1.5, Loc. 30, Reg. No. eM 8091.
Fig. 13. Turricula kaderleyi (LISCHKE) x 1.5, Loc. 24, Reg. No. eM 8092.
Fig. 14. Turritella nipponica YOKOYAMA x1.5, Loc. 53, Reg. No. eM 8093.
Fig. 15. Mya cunei/ormis (BOHl'vI) xl, Loc. 25, Reg. No. eM 8094.
(All specimens are stored at the Department of Historical Geology and Palaeontology,

University Museum, University of Tokyo)

C HI NZEI :Omma- Man ganjia fauna

Photo by lS I-! I B AS I-! I

Plate 14

Trans. Proc. Palaeont. Soc. Japan, N. S., No. 90, pp. 95-98, June 30, 1973

~18.

EARLY CARBONIFEROUS VISEAN FAUNAS.'DISCOVEEEDFROM MITSUZAWA, SOUTHEASTERN PARTOF THE KW ANTO MASSIFPART I. GASTROPODS*SUMIO SAKAGAM.I
Department of Geology, Faculty of Education, Ehime University

WJ}.IHIJ!l!!TriJl.[a!S'=: ~ iF{,mliljW)1lJ;)H2 ~ -ii -i!t1liJJrl)c¥. -CO) 1. IJJlJEJii: 1.\tl1t1ml'·iIbfflOi J]
mJltf:ltjj*"J 6km O)'=:'/iR""C'~!i!.(~q'1t:WiJEm, JlmJEHi, ~A.:.'m, .:.tt!1t~fl, ifija{i~fit.;:ell' l? t.;: -lS[ifJ!fj/JlI¥O)? tJ , Il!lJE1fl Hll: Mourlonia hayasakai SHlKAMA and NISHIDA ~~G,i!Q L t:, :: (7)f!fH:l:f:ktfTi IkE Millerella yobarensis ;:r.=!: Fusulinella biconica ;:I~:1.p l? fll~~ ~Lt.: t 0)"(' <Ii:> -lSiI:, .=: ,/ iRjffi(7) t O)t1 Millerella yobarensis ;:Ir-ilj;:O) t 0) c!f.lt::t <~J:ll:
T -lS .:. ~J!!!:A.:t.:o!lLI:Ut:*:iIntroduction and Acknowledgmentsshows N 15°E strike, 50 S dip, and has
been included in the Katsuboyama
Paleozoic zone by FUJIMOTO (HUZIMOTO,
1936). The Katsuboyama Paleozoic zone
consists mainly of greywacke and shalein alternation intercalated with clayslate,chert. quartzite, schalstein, conglomerate,
including the fusulinid limestones. The
geological age of this zone was considered to range from Lower to Upper
Permian by FUJIMOTO but the di~coveryof Fusulinella ct. pseudobocki by SAKAGAMI (1955, MS.) from a small limestone
cropping out in Hosoo-iri (valley), abput
3 km SSE from the Mitsuzawa limestone
haS proved the existence of Carbopiferous there .
In the present article on.e gastropod,
Mourlonia hayasakai SHIKAMA andNISHIDA, is described from the Mitsuzawa limestone. The brachiopod, coraland bryozoan faunas will be describedpaleontologic ally in forthcomiiig-papers
by Drs. J. YANAGIDA, N. Y AMAGIWA
and S. SAKA~AMI. Discussion of the0

It is well known that the Paleozoic-and Mesozoic belts are arranged alternately in about NW-SE trend in thesoutheastern part of the Kwanto massif.
'The Paleozoic System is mostly of
Permian age and includes the Upper
Carboniferous Fusulinella and Fusulina.zones in small areas. No Lower Carboniferous strata have been known todate but the recent discovery (SAKAGAMI,
1972) of a fossil fauna including gas·tropods, brachiopods, corals, bryozoans.and crinoidal stems from a limestone
cropping out in the Mitsuzawa valley,
Hinode-mura, Nishitama-gun, Tokyo-to,.about 6 km NW of Itsukaichi-machi-(town), points to the recognition of the
Early Carboni.ferous Visean age.
The fossil bearing limestone at Mitsuzawa is about 4 m thick, whitish grayin color, interbedded with chert and* Received Jan. 26, 1973; read JUI)e 3, 1972..at Utsunomiya.

95

96

Sum'io ' SllKAGAMI
Mow-ionia (Mow-ionia ) hayasakai
SHIKAMA and N rSHIDA
Text-figures 2 (1 - 5).
- 1968M oui-loni a (i'vfaurlonia ) hayas akai SHI -KA M A and N I S H I DA, p. 212, 213, pI. 24,,,
figs. i - 6.

She ll of moderate size conical, turbini form . coilin g dextral and consisting of '4 rapidly increasing w horls. Hei g ht of 'shell less than diameter. S pire angle ·about 100
Whorls expan ded , rather'
narrowly convex, ge ntl y curved, s uturefurrowed, base of shell more · or lessflatten ed. Seleni zone slightly concave"less tha n 1 mm in max imum width at ~outer whorl, delimited by two spiral Ii raea nd situated just above the suture ..
Um bilicus may be phan e romphalous. ,Shell ornamentation fine. growth lines
regularly spaced, numerous, stron g lyprosociine, slightl y convex forward
above the se leni zon e and orthocline,
below it.
Measurements : ~0•

Tex t-fig . 1. Map showing the lo ca li t y of
the Eady Carboniferous Mitsuzawa fau na

fauna and its geologic age will be presented in Part ' IV . . Bryozoans by
SAKAGAM I.
Here I would like to ex press my sincere
gratitude to Professor Kotora HAT Ar of
the Institute of Geology and Palaeontology, Facu lty of Science, Tohoku Unive r sity for his kind supervision and constantencouragement. Further, I w ish to ex press my cordial thanks to Drs. Juichi
YA NAGIDA of Ky ushu Unive rsit y andNobuo YAM AGIWA of the Osaka Uni ve rsity of Education for their kind cooperations in the present study.
Description of Species

Genus Mow-ionia DE KONINCK, 1883
Subgenus Mow-ionia
DE Ko ' INCK,1883

N umber of w horls

4.5 ?

Heig ht

22.5 mm

Diameter

28. 5 mm

HI D ratio

O. 79

Sp ire angle

100

0

R emarlls :-Although one of two speci mens at hand is deformed and incomplete,.
the other is we ll preserved and identicalw ith Mow-ionia (Mow-ionia) hayasa lwi'described originally by SHIKAMA and:
NrSHIDA (1968) f rom the Millerella sp. a 'zone (= Millenilla yobarensi s zone of 'TO RIYAMA and OTA, 1971) to the Fusui{nella biconica zone in the Akiyoshi
Limestone Group. Among the sevenspecimens referred to M. hayasakai by -Visean Faunas from Kwanto Massif. Gastropods

4.

2
T ext-fig. 2.

97

5

3

M ourlonia ( Mourl onia) haya saka i SH I K AM A and N I S H I D A
f rom the Mi tsuzawa Lim esto ne.
Latera l, ap ic a l and umbilic a l v iews of on e specimen

1- 3.
(Cat. No . EEG6001 ), x 2.
4,5. La te ral a nd a pica l views of the ot her specim e n(Cat. No. EEG6002), x 2.

·SHI KAMA and N ISHIDA measurements
were g iven of four, namel y the holot y pe,para t y pes A , D and E. The paratype
E was obtained from the I'vlillerella yo barensis zone and the other three from·the Fu sulin ella biconica zone. The specimens from the two fossil zones seem
to show different ratios of height todiameter; namely, the ratios in thespecimens including the holot y pe from-the Fu sulinell a biconica zone show 0.93
to 1.0, while that in paratype E from-the Millerella yo barensis zone is 0.78.
The ratio in the present specimen is'0.79 and in this feature , it is nearest to

SHIK AMA a nd NISH ID A' s Parat y pe E, but
the shell size is a lmost twice of thelatter. Further it is considered that
there is no chan ge in the ratio of height
to diameter through the growth of theshell, because the holotype and paratype
A ha ve different size in spite of having
the same ratios. If HI D ratio changes
phylo geneticall y, the present form andParat y pe E from Ak iyoshi should be
separated from lvl. hayasakai as independent species or subspecies. However,more detailed examination must be reser ved because of the few number of
specim ens at hand .

98

Sumio SAKACAMI

Geological age:~Probably Upper Visean of the Early Carboniferous.
Repository and Specimen No:- The
present specimees are preserved in theCollection of the Department of Geology,
Faculty of Eduction. Ehime University.
Nos. EEG6001 and EEG6002.
References
FUJIMOTO, H. (HUZIMOTO, H.) (1936) : Stratigraphical and palaeontological studiesof the Titibu System of the Kwantomountainland.
Part L Stratigraphy.
Sci. Rep. Tokyo Bunrika Daigaku, Sec.
C, No.4, pp. 157-188, pis. 27-29.
Sf..KAGAMI, S. (1955, MS): Stratigraphicaland palaeontological studies of the

Mitsuzawa
Hinode-mura
Nishi tama-gun:=:. '/ iR
13

O):mi

jl§ ~I"tjil:northern part of Itsukaichi and thenorthwestern part of Orne, Nishitama·gun, Tokyo-to.
Graduation Thesis ofTokyo Univ. Educ.
- - (1972): Discovery of the early Carboni·ferous Visean fauna from the Kwanto
massif. jour. Geol. Soc. japan, Vol. 78,
No.4, p. 216. (in Japanese)
SHIKAMA, T. and NISHIDA, T. (1968): On
some species of Carboniferous Pleuroto·
mariaceans from, Akiyoshi (Molluscan
paleontology of the Akiyoshi limestoneGroup-III). Trans. Proc. Palaeont. Soc.
japan, No. 69, pp. 211-217, pis. 24, 25.
TORIYA'-'IA, R. and OTA, M. -(1972): Akiyoshidai (Guide book for the -geologicalexcursion). Geol. Soc. Japan, 29 pp. [inJapanese)

Itsukaichi-machi
Katsuboyama
Hosoo-iri

Jil3mlllT

lEft ~ I.iJ
*111 ~}...

Trans. Proc. Palaeont. Soc. Japan, N.S., No. -gO, pp., 99-112, pIs. 15, 16, June 30, 1973'~' 1-

619.

EARLY CARBONIFEROUS VISEAN FAUNAS DISCOVEREDFROM MITSUZAWA, SOUTHEASTERN PARTOF THE KW ANTO MASSIF-l<
PART II.

BRACHIOPODS

lurCH! Y ANAGlDA
Department of Geology, Faculty of Science,
Kyushu University, Fukuoka, 812

1)[1*11 I JlliIyj}j:[ fiI\~ 'y i}~I)EB~J WJTcirk fc I! t - litlliJJ:/7I)n,.:cu) 2. lin! iEW: i,fi siU;I: 1,·)!:tl~V: 11: L1

rh'lIfr~ 'y in,,:: 711'riT .Qilijs 1\"1'iEk 'G'i' J: i) Il\iiiEl'(jO) ::; Hi:

Schizophoria resupinata (MARTI:-:), Rugicostella sakagamii YA:-:AGIDA, sp. nov., Undaria sp., Martinia sp., Spirijer<

sp. '.\:'ii,'~~IJ GJL:ii& Lt.:" c..h00)? t;;,J: i':: Rugicostella sakagc.mii YA[\;AGIDA, sp. nov.
fi1':k;'f:rII:k'GJl';,:I\!t Millerella yowarensis ;:fn~'Ek'G,ir:O) R. nysliana (DE KO:-:Ii\;CK) (.::;Ii
W'e il6 'J, 2: 0 i,:: ;,HiJ 0) 13&JI:l)j; ~. t' - ~J( ::Jl~ 0 h':;' .:. c. t.H::' lJ;'f ft C!) jtfj 7;-;,r.' c. L -C ill ;;;:: -C il6 Q"it.: Schizophoria resupinata (MARTI:") (=h0;lT611(j:;g.tJ:fJ;jjf)jc~~~iHt:ltIl~·t·-i!tQ) S.
resupinata '.::~t;mT .Q!f;lql&""C: il6.Q c.. c)j, 0, lI~ftU~H= lf~1}tJ: 'nfH:1XfJI<T.Q .:: c '.\:'O)A:..t.: o0

f~11

II! 1f --Mitsuzawa. The study on the species
assemblage of the brachiopods describedhere led to a conclusion that the geologic
age of them is assigned to the Late
Visean.
The writer is greatly indebted to Dr_
Sumio SAKAGAMI who gave him every
facility in the field work and provided
him many brachiopod specimens. His
sincere thanks are also due to Professor
Ryuzo TORIY AMA for kind reading themanuscript.

Introduction and acknowledgements

The discovery of the Early Carboni,ferous Visean faunas from a limestoneof Mitsuzawa in the southeastern partof the Kwanto massif was recently reported by SAKAGAMI (1972), who gave apreliminary discussion on the outline ofstratigraphy, the fossils obtained fromthe limestone, such as bryozoans, brachiopods, crinoids, corals and gastropods, andtheir geologic age. The writer was very
fortunate to have an occasion of visiting
the locality and to obtain a fair numberof brachiopods under the kind guidanceof Dr. SAKAGAMI.
This paper is a part of the palaeontological study of the Visean faunas from

Remarks on the brachiopod
species assemblage

The assemblage is characterized by
the following brachiopod species: Schizophoria resupinata (MARTIN), Rugicostellasakagamii YANAGIDA, sp. nov'., Undaria* Received Feb. 1, 1973; read October 28,
1972 at Matsuyama.

99

100

Juichi YANAGIDA"sp.. .o//artinia sp., Spirifer sp.. Amongthem the former two species are very
"important for discussing their geologic.age. Schizophoria resupinata is the typespecies of Schizophoria, showing the wide
-distribution in Eurasian continent andranging through the Tournaisian and Vi·"sean with the most abundant occurrencein the Upper Visean in the European
standard of the Lower Carboniferous.
As stated in the chapter of systematic palaeontology S. resupinata from
Mitsuzawa appears to be fairly variable
in its shape. It consists of four extreme
forms, with several intermediate ones
among them. If the four extreme forms
are compared with the Belgian Dinantian{lnes, S. resupinata var. pinguis, var. dorsosinuata and var. rotundata describedby DEMANET (1934) and S. resupinata s. s.
:arethe closest forms, respectively corresponding to each of them. Among the
Mitsuzawa forms those compared withvar. dorsosinuata and var. rotundata aresmall and rather doubtful in their discrimination. On the other hand thestrongly inflated form is undoubtedlyreferable to DEMANET'S var. pinguis in
its outline, mode of inflation and its
slightly uniplicate anterior commissure.
As far as our present knowledge isconcerned S. resupinata var. pinguis is
known from the Upper Tournaisian toUpper Visean and most abundant in theUpper Visean in the Lower Carboniferous of England and Belgium.
Rugicostella sakagamii, the newly established species in this genus, is closely
related to R. nystiana, the type speciesof this genus, which is only known fromthe Visean of Belgium, England andJapan. R. nystiana was originally described by DE KONINCK (1842) under thename of Productus nystianus from the
Visean of Vise, Belgium. In Englandthe same species was also described by

DAVIDSON (1861) from the Lower Scarlimestone of Settle, Yorkshire. The geology and the faunal succession of thisregion was shown in detail by GARWOOD
and GOODYEAR (1924). According to them
Rugicostella nystiana occurs in a limestone of D2 subzone with a fair kinds ofbrachiopods, corals and other fossils. In
Japan YANAGIDA (1965) discriminated R.
nystiana from the Millerella yowarensis
zone (TORIY AMA and OTA, 1971) of the
Akiyoshi limestone Group at Yowara(or Yobara) with many kinds of otherbrachiopods. The writer correlated theage of the limestone with the Late
Visean.
Undaria sp. externally strongly resembles U. erminea (DE KONINCK) which is
known from the Visean of Vise, Belgium.
The genus Undaria is known only in the
Visean.
Two indeterminable species of Martinia and Spirifer are rather difficult tocompare with" other distinct species ofthese genera. A special attention is
given to the existence of a weak fasciculation in Spirifer sp. In this characteristics with external configuration of
pedicle and brachial valves, it is considered that S. liangchowensis CHAO fromthe Visean of northwest China is highly
comparable with the present species.
Summarizing the above discussion thespecies assemblage of Mitsuzawa brachiopods is unique in its constitution andclosely related with the Upper Viseanbrachiopods of Europe and Asia.
Systematic Palaeontology

Superfamily Enteletacea W AAGEN, 1884
Family Enteletidae W AAGEN, 1884
Subfamily Schizophoriinae SCHUCHERTand LEVENE, 1929

619.

Visean faunas from Kwanto massif: Brachiopods

Genus Schizophoria KING, 1850
Type.species :-Conchyliolites (Anomites)
resupinatus MARTIN, 1809.
Schizophoria resupillata (MARTIN)
PI. 16, figs. 3-9] 809. Conchyliolites (Anomites) resupinatus
MARTIN, p. 12, pI. 49, figs. 13, 14.
1842-4. Orthis resupinata, DE KONINCK, p.
226, pI. 13, figs. 9, 10.
1863. - - - - , DAVIDSOi\", Palaeontogr. Soc.
Monogr., p. 130, pI. 29,figs. 1-7, pI. 30,
figs. 1-5.
1923. Schizophoria resupinata,
DElvIA:'-lET,
Mem. Inst. Geol. Univ. Louvain, vol.
2, p. 119, pI. 5, fig. 1.
1923. - - - - . var. lata DEMANET, Ibid.,
vol. 2, p. 122, pI. 5, fig. 4.
1934. Schizophoria resupinata,
DE:\IANET,
Mem. Mus. Roy. d'Hist. Nat. Belg., no.
61, p. 47, pI. 3, figs. 1-5.
1934. - - - - var. lata, DE '>1 Ai\" ET, Ibid.,no. 61, p. 50, pI. 3, figs. 6-8.
1934. - - - - var. gigantea DElvIANET, Ibid.,no. 61, p. 60, pI. 4, figs. 12, 13.
1934. - - - - var. rotundata DEMANET,
Ibid., no. 61, p. 51, pI. 3, figs. 9-13.
1934. - - - - var. dorsosinuata DElvIANET,
Ibid., no. 61, p. 53, pI. 3, figs. 14, 15.
- - var. pinguis DEMA1\ET, Ibid.,1934. no. 6, p. 59, pI. 4, figs. 9-11.
J941. Schizophoria resupillata, BOND, Geol.
Assoc., London, vol. 52, pt. 4, p. 289,
pI. 21, figs. A-C.
1954. - - --, PARKINS00", ]. Paleont., vol.
28, p. 368, figs. 1, 2a-e.
1957. Schizophoria d. S. resupinata, CA~IP­
BELL, Ibid., vol. 31, p. 48, pI. 12, figs.
1-5.
1962. Schizophoria aff. S. resupinata, YANAGIDA, Mem. Fac. Sci., Kyushu Univ., vol.
12, no. 1, p. 122, pI. 21, figs. 4-13.
1968. Schizophoria resupinata, POCOCK, Palaeontology, vol. 11, pt. 1, p. 80, pI.
18, fig. 7.
1968. - - - - var. dorsosilluata, BRUNTO)/,
Bull. Brit. Museum (Nat. Hist.), vol.
16, no. 1, p. 11, pI. 2, figs. 7-37.

101

1971. Schizophoria d. S. resupinata, ROBERTS,
Bur. Min. Res., Geol. Geophysics Australia, Bull., no. 122, pI. 1, figs. 6-32.

iVlaterial:- About thirty -five specimens
are available under the heading withtwenty-seven better preserved ones. Theinternal structures are shown by serial.

_ X. =0.99 ; Iypl!' olLl.J'---+ k.. =0.91 ; typl!' C {oj,~:::::::::

r'/

.
width

Text-fig. 1. Variations in size andform among four extreme forms of Schizophoria resuPinata. Average form ratioof type A (0.89) for twelve articulatedshells, one brachial and three pedicle
valves; type B (0.82) for three articulatedshells; type C (0.91) for three brachialvalves; type D (0.99) for two articulatedshells and a brachial valve.
lengthText-fig. 2. Proportional composition
among length, width and thickness ofbrachial valves of Schizophoria resupinata.

Jwichi YANAGIDA

102

sections of a specimen, GK-.D 31155.
Description:- The shell 1's small to
medium, biconvex to moderately dorsi b iconvex, wider than long to nearlyequi-dimensiona l, with the largest width
at the mid -length. Hinge line is variable in length , abo ut a half to two thirds
the s hell width. The pedicle va lv e isweak ly to very s lightly convex with thelargest convex ity near the umbo, nearlyflat on anterior ha lf. The brachial valve
is ve r y variab le in its convexity and thebroad median sulcus is developed in somespecimens. Both valves are ornamented
by fi ne costellae, usuall y four to five in
1 mm at 10 mm from beak. In well pre-o
0 °·6 -

u11"US'IS"
2.2

3.9

4.0

o,
4.6

em

Text-fig. 3. Transverse ser ia l sect ions of Sch izoplwria resupinata,
GK- D 31155, measuremen ts in mm from vent ral beak.

619.

Visean faunas from· Kwanto massif: Brachiopods

served specimen the coarser costellae
with anteriorly developed spine base areobserved. Tightly arranged growth lines
are scattered in some specimens. Anterior commissure is recti marginate tobroadly sulcate.
The pedicle valve interior is withstrong teeth supported by strong parallel dental plates, diverging anteriorly

103

and extending about a fifth length ofshell. The median septum is very low.
slightly increasing in height anteriorly.
The brachial valve interior is with deep
dental sockets, articulating teeth. Stoutbrachiophores extend anteriorly nearlysame length with dental plates and theinner extremities of them seem to beinterlocked with each other.

Dimension of 10 specimens in mm:I

specimen numberI
lengthI

GK-D 31134) .1mn"
tovar. rotun"

91133 data by.;J

DEMANET••p.~dto var. pmg" 31129) ,."31131 uis by
DEMANET"t.
var. dorso" 31137) .1mn"
"
"
"
"

"

31138 sinuata by
DEMANET

31155
31136
31151
31153

18.5

I

width

ped. v.

I

I

I hingethickness

I

I
5.5

18. 7

bra. v.

4.5

i

I
4.5

form
ratio
(l/w)

line

8.9

6. 0

!

O. ~~9

I

0.90

17.6

19.5

22.4

21. 0

11. 0

1. 07

18.0

22.0

9.5

0.82

17.5

20.5

4. 7

5.5

13. 7

0.85

14.5

18.3

3.4

4.8

10.5

O. 79

24.5
22.3
33.5
23.9

26.5
26.6
36.0
25.5

7.0

4. 0
6.8
12.5
7.3

14.5

0.92

21. 0
13. 0

0.93
0.94

Statistics of length (I), width (w). thickness (th) and form ratio (fr) of brachialvalves of Schizoplwria resupinata specimens are as follows:l(a)~21.98(4.95), W(a)=23.87(5.32). th(a)=7.49(2.56), fr(a) =0.90(0.07), n=26.

Remarks :-Comparing with the neotype chosen by GEORGE and PONSFORD(1938) the Japanese specimens are allvery small but the morphological characters are quite in harmony with eachother. It is already known that the neotype is much larger than the average inthis species.

I

i

I

17.0
5.0

It is well known that Schizophoria resupinata shows several variations in its
form. DEMANET (1923, 1934) establishedthe following varieties on the Belgian
Lower Carboniferous specimens: dorsosinuata, gigantea, lata, pinguis and rotundata. They were discussed in detail by
BOND (1941) and POCOCK (1968). The
available specimens at hand respectively
show the individual variation, and it ispossible to group them into four extreme
forms, type A, B, C and D. If the division by DEMANET is followed, they are
respectively named as follows: type A.
Schizophoria resupinata s. s. (19 speci-

Juichi YANAGIDA

104

Text-fig. 4. Variations in form of,Schizophoria resupinata, showing four ex"'treme forms, 1 for type A, 2 for type B,.3 for type C and 4 for type D.

mens); type B, ? var. dorsosinuata (2'specimens); type C, var. pinguis (3 spe'cimens); and type D, ? var. rotundata(3 specimens). Nevertheless, several intermediate forms are also discriminatedamong the specimens which are referred.to S. resupinata s. Soo The writer followed POCOCK (1968) who considered these"Varieties by DEMANET to be included
under S. resupinata because that they
represent the extreme individual varia·.tion.

by serial sections of a specimen representing the visceral disc, GK-D 31191,
and other two specimens, GK-D 31160
and 31161.
Description :-The shell is small andsubcircular. The hinge line is shorter
than the largest width of the shell. The
pedicle valve is moderately convex withslightly convex visceral disc and short
trail. The visceral disc is strongly geniculated with a very weak cincture between the trail. The cincture is remarkably emphasized by exfoliation of shellsurface. The short trail is nearly atright angles to visceral disc. The brachial valve is with slightly concave visceral disc and short trail. The geniculation is remarkable and the cincture is
weak. The pedicle valve is ornamented
by closely arranged rugae on the wholesurface of the visceral disc, about three
to four in the distance of 2 mm on central median part of the visceral disc,and posteriorly more remarkable thananterior surface. The trail is ornamented
by short irregular costeIlae, about fivelength"'m)

Yw = 1.03.Superfamily Productacea GRAY, 1840

Yw ... ,1

Family Institinidae MUIR-WOOD
and COOPER, 1960
Genus Rugicostella MUIR-WOOD
and COOPER, 1960"

Type-species:- Productus nystianus DE
KONINCK, 1842.
Rugicostella sakagamii

Y ANAGlDA, sp_ nov.
Pl. 15, figs. 1-8, "'".-------7.'5,---------(m-'"Material :-Holotype, GK-D 31168 (PI.
15, fig. 2). More than 30 specimens areavailable. Internal structures are shown

Text-fig. 5. Variations in size andform of pedicle valves of Rugicostellasakagamii Y A~AGJDA, sp. nov.

..... idth

619.

Visean faunas from Kwanto massif. Bmchiopods

105.

height (h), and form ratio (fr) of Rugicostella sakagami are as follows:
Pedicle valve: I (a)=14.94(1.61), Vi (a)=14.53(1.84), h (a) =7.79(1.92), fr (a)=1.03(0.09), n=21.
Visceral disc of pedicle valve: i (a)=12.20(1.18), Vi (a) =12.69(1.70). h (a)=4.29(0.95). n=30.

em

b~-"'-"--

Text-fig. 6. a, b. Ventral and dorsal
views of an incomplete visceral disc of
Rugicostella sakagamii YANAGIDA, sp. nov.,
GK-D 31191. c. Profile of the same specimen showing positions of transverse serial
sections. Each number respectively corresponds to that of Fig. 7.

in the distance of 5 mm on anterior part,and often with spine bases at their anterior extremities. Fine spines are scattered on the visceral disc. The brachialvalve is ornamented only by weak. evenrugae. The pedicle valve interior is withraised diductor scars. The brachial valve
interior is with a distinct, trilobate cardinal process having two lobes completely in contact near the posterior margin,
but anteriorly they are slightly separate
with each other. Myophore is considered to be more complex at the posterior
margin. Median septum is low and narrow, extending about two-thirds lengthof the visceral disc.
Dimension of the holotype (GK-D 31168)
is as follows (in mm) : length, 16.7 ; width,
15.2; height, 10.5; form ratio (i/w),
1.09. Statistics of length (I), width (w),Remarks :-Rugicostella sakagall1ii is.
the only species which is known otherthan R. nystiana, the type species ofthis genus. It is apparently distinguishedfrom the latter by its uniformly larger
size, more numerous and less remarkable rugae, weaker cincture on pediclevalve, and more numerous irregular costellae with spine bases often recognizable on the anterior margin of them. Thelast characteristic is very important inthis species. In R. nystiana most of thecostellae begin near the cincture and extend to the anterior margin of trail. In,
R. sakagamii the costellae are very shortcomparing with the length of trail andmany costellae appear on anterior surface of trail. When the spine base isrecognized it is always at the anterior
margin of the costella. Therefore inthis case the costella seems to be prostrate spine ridge. The cincture on thepedicle valve is very weak when theshell surface is well preserved. Whenthe surface of the visceral disc or trail
is more or less exfoliated the cincturebetween them is remarkably impressed_
The morphological character of the cardinal process is similar to R. nystiana,
which is clearly shown by MUIR-WOODand COOPER (1960). Three specimens
were serially sectioned to observe theinternal characters. Bilobed characterof the cardinal process is observed in a
specimen, GK-D 31191, which shows thedelicate' complex shape of the myophore
near the posterior extremity. This char-Juichi YANAGI.DA

106

12

~

o' -_ _ _ _ _ _ _ _ 5 mm
14

Text-fig. 7.

Transve rse se rial sections of Rugicostella sak agam ii
sp. nov ., GK- D 31191 (see Text-fig. 6).

Y ANAG IDA,

619.

Visean faunas from Kwanto massif. Brachiopods

\

\

\
\
\

l/~~J4,_.":: ____i

\

"
\

\

\
\
\

,
\

\

,
\

""idth"--_ _ _ _ _ _ _ _~_ ___.:,\~heighlText-fig. 8. Proportional composition
among length, width and height of thirtyone visceral discs of Rugicostella sakagamii
YA'-:AGIDA, sp. nov.

acter is not recognized in other two specimens.
YANAGIDA (1965) discriminated R. nystiana from the Millerella yowarensis
zone of the Akiyoshi limestone Group,
Southwest Japan_ The present specimens
are externally very similar to those of
the Akiyoshi specimens_ However, theformer is clearly distinguishable fromthe latter by the above stated characters.
Family Linoproductidae STEHLI, 1954
Subfamily Linoproductinae STEHLI, 1954
Genus Undaria MUIR-WOOD
and COOPER, 1960
Type-species:-Undaria manxensis MUIRWOOD and COOPER, 1960.
Undaria sp.
PI. 15, fig. 9

Material: ~ Incomplete pedicle valve.
GK-D 31245, is available under the head- ing with the following dimension: length,18mm+ ; width, 18.5mm ; height. approx.
15mm.

107

Descriptive remarks :-The shell is medium, weakly convex longitudinally withthe largest convexity at anterior to theumbo, and slightly longer than wide witha short hinge line and steep flanks. The
venter is rather flattened. The outlineof the pedicle valve is suggested to beoval and the trail is probably not preserved. The widest part may be slightly
posterior to the mid-length of the valve.
The surface of the valve is ornamented
by remarkable rugae and fine capillae.
The rugae are irregular in width. counting about five on the venter and distributed on the whole surface of the valve.
They are often intercalated or bifurcatedwith rounded crest. The capillae aremuch less remarkable comparing withthe rugae.
The rugose ornament with fine capillae,
steep flanks, elongate oval outline andslightly convex pedicle valve of the
Mitsuzawa specimen well represent thecharacters of Undaria. The specimen
is incomplete but slightly asymmetricaloutline is also suggested from its outline_ In these characters the Mitsuzawa
species is considered to be very closely
related with Undaria erminea (DE KONINCK) from the Visean of Vise, Belgium.
The Belgian species has a long trail.
The Mitsuzawa specimen represents only
a posterior part of trail and the detailed
comparison with the Belgian specimen
is difficult. But the remaining parts ofpedicle valves are well in harmony witheach other. It is probable that both
species are conspecific with each other.

Superfamily Reticulariacea
W AAGEN, 1883
Family Martiniidae W AAGEN, 1883
Genus Martinia M'CoY, 1884

108

Juichi YANAGIDA(1zJ 0.5. 2.5

loP_ _ _ _ _ _ _ _ _ _- - ' ,-.

emText-fig. 9. Ventral, posterior, lateral and dorsal views (a-d) of a small specimen of
Martinia sp., GK-D 31233, and transverse serial sections of the same specimen with.
measurements in mm from ventral beak.

619.

Visean faunas from, Kwanto massif Brachiopods

Type-species :-Spirifer glaber SOWERBY,
1820

109

rounded. The beak is strongly incurved
over the delthyrium. The delthyrium
may be open. The interarea is very
low and concave. The sulcus is very
faint and narrow, obscurely distinguishedon anterior third of the valve. The
surface of the valve is very smooth onlywith fine, tightly arranged growth lines
and sometimes with very fine radialstriae on anterior half. The brachialvalve is slightly swollen longitudinally
but no distinct fold is observed. The
beak is slightly convex and rather erectwith a short distance between the opposite bf!ak. The ornamentation of thevalve is same with the opposite valve.
The pedicle valve interior is without
dental plates and median septum. Radialvascular markings are partly observableon the mould of a pedicle valve. The
brachial valve interior is with small
sockets, receiving teeth.

Martinia sp.
PI. 15, figs. 10-14

Material :-About fourty specimens
are examined, of which complete ones
are very few and most of them arevery incomplete pedicle valves.
Descriptive remarks :-The shell issmall, equally biconvex with the pedicle
valve slightly more convex than thebrachial one, and transversely subroundto equal in length and width with thewidest part at the mid-length of theshell. The hinge line is about two-thirds
the width of the shell. The anterior
commissure is gently uniplicate.
The pedicle valve is uniformly convex
both transversely and longitudinally.
The cardinal extremities are wellDimensions of ten specimens in mm.
specimen number
GK-D 31218
II
31219
II
31215
II
31236 (ped. valve)
II
II

---

31204 (II)31216 (II)II

31213 (II)II

31220 (II)II

31217 (bra. valve)II31207 (II)length

width

13.5
13.9
14.9
14.3
9.8
9. 7
15.5
14.2
9.0
12. 7
11. 0
11. 0
11.8
11. 1
approx. 14
13.8
11.5
12.2
18.0 I approx. 18

I

thicknesslength of
I hinge
line

7.6
8.5
5.3
6.0
4.5
3.5
4.9
4.3
2.8
approx. 6

6. 7
8.9
5.8
approx. 8
6.0
6.3
9.25
8.3
approx. 8
14.0

--I

I

form ratio(length/width)
~~---

--

0.97
1. 04
1. 00
1. 09
O. 70
1. 00
0.94
0.98
0.94
1. 00

-------The Mitsuzawa specimens are characterized by uniformly small size, very
faint sulcus and no distinct fold. In
these points of views the Mitsuzawa
species is externally very similar toMartinia decora var. longa described by
GROBER (1908) and WANG, JING a.nd F1\NG(1964) from the Lower and Middle Carboniferous of the Sinkiang, western
China. The slight differences between
them are on the sulcus and fold, which
are much weaker in the Mitsuzaw<,\
specimens th<'\n the other,

.htichi YANAGIDA

110

Superfamily Spiriferacea KING, 1846
Family Spiriferidae KING. 1846
Genus Spirifer SOWERBY, 1816
Type-species :-Conchyliolithus (Anomia)
striatus MARTIN, 1793
Spirifer sp.
PI. 16, figs. 1, 2

Material:- Two incomplete specimens,
respectively slightly deformed pedicle
and brachial valve, are at hand. The
dimension of them is not given exactly.
Descriptive remarks :-The shell is
medium to large. The pedicle valve
outline is suggested to be transverse andslightly convex with the hinge line

nearly equal to the largest width of theshell. The sulcus is broad and roundbottomed, originating near the umbo.
The umbo is slightly incurved over thedelthyrium. The width of the basal
part of the delthyrium is about a sixth
length of the hinge line. The interarea
is slightly concave medianly, becoming
flat toward the cardinal extremities withvery fine denticle grooves on the exfoliated surface. The pedicle valve isornamented by simple rounded costae
with rare bifurcation. About eight costae
are counted on the sulcus. The brachialvalve is moderately convex transversely
and longitudinally with a prominent
rounded fold. The surface ornamentation is same with the opposite valve.
Very weak broad fasciculation is pos-

Explanation of Plate 15
All figures x 1.5
Fig. l-S. Rugicostella sakagamii YANAGIDA, sp. nov.
la.-d. Posterior, ventral, anterior and lateral views of an incomplete pedicle valve,
GK-D 31170.
2a-d. Posterior, ventral, anterior and lateral views of the holotype, GK-D 3116S.
3a-e. Dorsal, posterior, ventral, anterior and lateral views of an incomplete shell,
GK-D 31167.
4. Visceral disc of an incomplete pedicle valve, GK-D 31203.
5. Dorsal view of visceral disc of an incomplete brachial valve, GK-D 31303.
6a, b. Ventral and posterior views of visceral disc of an incomplete pedicle valve,
GK-D 31177.
7a-c. Anterior, posterior and lateral views of an incomplete pedicle valve, GK-D 3115S.
7d. Visceral disc of brachial valve of the same specimen.
Sa-c. Ventral, anterior and posterior views of an incomplete pedicle valve, GK-D 31156.
Fig. 9. Undaria sp.
9a, b. Ventral and lateral views of an incomplete pedicle valve, GK-D 31245.
Figs. 10-14. Martinia sp.
lOa-c. Dorsal, ventral and lateral views of a complete shell, GK-D 3121S.
11a, b. Dorsal and lateral views of an incomplete shell, GK-31220.
12a, b .. Posterior and ventral views of a small pedicle valve, GK-D 31204.
13 • .Incomplete pedicle valve showing the mould of radial vascular markings, GK-D
31206.
14. Incomplete pedicle valve, GK-D 31216,
Photos by YANAGIDA, with whitening,

YAN AGIDA:

Visean Faunas f?'om Kwanto Massif. Brachiopods

Plate 15

6.19.

111

Visean .f(L~m(LS f?'om J(wanto massif. Bra,chio1Jods

teriorly observab le on a wi ng.
The above stated cha racters of the
Mitsuzawa specimens, espec iall y thestrongly convex and slightly fasciculatebrachial val ve with prominent fo ld
strongly reca ll those of Spirifer liang·chowen sis CHAO from the Visean Choniukou Formation of Kansll, north weste rn China.
References
BO ND, G. ( 1941 ) : Species and va ri ation in
Br i tish a n d Be lg ia n Carbo ni ferous Schi ·zophoriidae. Pro c. Ceo l . As soc . Londoll,
52, 285- 303, pI s. 21 - 22.
BR UN TON , C. H . C. (1968) : Si li c ified brachi.
opods from t he V isean of County Fer.
managh ( II ). BUll. Brit. Mu se um (Na t.
His!. ), 16, (1 ) , 1- 70, p Is. 1- 9.
CA~ I PBELL, K. S. W. (1957): A Lo we r Carboniferous brac hi opod · cora l fa u n a f rom
New Sout h Wa les . ./our. Pa/ eon t., 31 , (1 ) ,34- 98, p Is . 11 - 17.
CH AO, Y. T. ( 1958):
Carbon iferous andPermi an sp iri ferids of Chi n a. Pala eon t.
S£nica, ser . B, 5, fasc. 2, 1- 24'1, p Is. 1- 16.
D AV IDSO ,T. (1857- 1863) : A monograph oft h e B ri tis h Carboniferous Brachiopoda.
Pata eon!g r. Soc . ( Monogr. ) , pt. 5, 1- 280,
p Is. 1- 55.
DEMANET, F. (1923): Le Wa ul sort ien deSosoye . ivUm. I ll S/. Ceol. Vlliv. LOll va in ,2, 36- 286, p Is. 3- 14.
- - (1934) : Les brac hi opodes du Dinantiende la Be lg iqu e.
Mbn. ivfusee Roya lD'Hist. Nal . B elgiqu e. ( 61), 1- 11 6, p Is. 1_

10.
G ARW OOD, E. J. a nd GO ODYE AR, E. (1924) :The Lower Ca r bo n iferous success ion in
the Sett le district a nd a lo ng the line ofth e C ra ve n fa ul ts. Quart . 10llr. Ceol.
So c. London . 80, 18'1- 273 .
GEORGE, T.N . a nd P OI SFORD, D. R. A. (1938) :Notes o n the morpholog y of Schizophoria.
Tran s. Leeds Ceo l . Assoc. 5, pr. 4, pp.
227- 245, p L 5.

GR onER, P. ( 1908) : Uebe r die Faunen desu n terca rb o ni sch e n Transgress ionsmeeresdes zentra len T ia n-Schan , die in der Um g eb un g des Sa r t- d sc holp asses gefu nden
worden si nd . N. Jahrb. f. Mi1l. CeDi.
Paia eon t. , B. B. , 26 , 213- 248, pIs. 25- 30 .
K ON INC K, L. G. DE. (1842- 1844): Description
des an im aux fossi les qui se trouve n tdans Ie ter rain carbonifere de Be lg ique.
iv + 650 pp., L iege.
M UIR·WOOD, H. M. a nd CO OPER, G. A. (1960) :Morpho logy , cl ass i fication and li fe h abitsof t h e Producto id ea (B rachiopoda ) . Mem.

C eo l . Soc. Amer., 81, 1- 447, pIs. 1-135.
P A.RKI NSON , D. (1954): Quantitative st ud iesof brachiopods fro m t he Lower Ca r boni.
fe r ous r eef lim estones of E n g land. j Oll1".
Pal eon!., 28 , (3) , 367- 38l.
P OCOCK, V. P. (196B) : Carbon ife rou s schi.
zop horiid brachiopods f rom
weste r n
Europe. Palaeonl. , 11 , 64- 93, pl. 18.
ROBERT S, J . (1971): Devonian and Carbo ni ferous brac hi opods from the Bo na parteg u lf basin, northwestern Austra li a. Bur .
ivlin . Res . Ceot . Ceophysics, Bull., ( 122) ,1- 319, p Is . 1- 59.
S AKAGA MI, S . (1972): Disco very of t he Ear l y
Ca r bon i ferous Visean fauna from [heKwanto m ass if. j Ollr. Ceol. Soc. japan,
78 , ( 4), 216 ( in Japanese].
T ORIY AMA , R. and OTA, M. (1971) : The
Ak i yosh i p latea u . Guide book fo r t h e
geo log ica l excursion of t he 78th Annua lMeeting of t h e Geo logica l Society 0Japan , 1- 29 ( in Japane se].
V AUG HAN, A . (19 15): Corre lat ion of Din,'t ia n and Avonian. Quart . ./our. Ceoi.
London, 71 , I -52, p Is . 1- 7.
W AN G, Y., JI NG, Y. G . and F ANG ,( ed it o r s ) ( 1961 ) : Chinese brac
foss il s pt. 2, 355- 777, pIs . 59C h i n ese].
Y ANA.G ID A, J. ( 1962) : Ca r bonife rou

Ipods f ro m Ak iyos h i, sou t7 W
pt. I. Mem. Fa c. Sci, J(y ush( 1), 87- 127, pIs. 14- 2l.
(1965) : Carbonife r ous brac
Ak iyos hi , Southwest Japan
16, ( 2), 11 3- 142, p is. 25 - 2s'

I

112

Juichi YANAGIDA
Kwanto massif B:1J/ifL/Jttl!

Mitsuzawa :::: ';/ iR.

YowaraiL

Explanation of Plate 16
Fig. 2 x 1.25; all others x 1.5
Figs. 1, 2. Spirifer sp.
la-c. Posterior, ventral and lateral views of an incomplete pedicle valve, GK-D 31250.
2. Incomplete brachial valve, GK-D 31248.
Figs. 3-9. Schizophoria resupinata (MARTIN)
3a-c. Lateral, posterior and ventral views of an incomplete brachial valve, GK-D 31129.
4. Incomplete brachial valve, GK-D 31140.
5. Incomplete brachial valve, GK-D 31136.
6a-d. Dorsal, anterior, lateral and ventral views of -an incomplete shell, GK-D 31139.
7a-d. Anterior, dorsal, ventral and lateral views of an incomplete shell, GK-D 31134.
8a-d. Ventral, dorsal, lateral and anterior views of an incomplete shell, GK-D 31133.
9a-c. Lateral, dorsal and ventral views of a plaster cast, GK-D 31155.
Photos by YANAGIDA, with whitening.

YANA GID A:

Visean Fauna s j 1'O?n J(wanto Massif. BmchioJJocls

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Transactions and Proceedings of the PalaeontologicalSociety of Japan

June 20, 1973

New Series No. 90

CONTENTS
TRANSACTIONS
615.

HIRANO, Hiromichi:

Biostratigraphic study of the Jurassic Toyora Group.

Part III . .. ....... .......... .... . .... . .. .. .. . ... ... ..... . . ............

45

616. SADA, Kimiyoshi and DANNER, Wilbert R.: Early Permian Parafusulina
and Pseudofusulin ella from the Chilliwack Group, southwestern British
Columbia ............................................................
617. CHINZEI, Kiyotaka:72

Omma-Manganjian molluscan fauna in the Futatsuiarea of nothern Akita, Japan. . ..... ..... . . ........ ...... ... . .... .. ..

81618. SAKAGAMI, Sumio: Early Carboniferous Visean faunas discovered from
Mitsuzawa, southeastern part of the Kwanto Massif. Part I. Gastropods
619.

95

YANAGIDA, Juichi : Early Carboniferous Visean faunas discovered from
Mitsuzawa, southeastern part of the Kwanto Massif. Part II. Brachiopods ..... .. .................... ... ... . ... . ........... . ... . . ... . .. ... 99