ISSN 0031 - 0204

Transactions and Proceedingsof thePalaeontological Society of Japan
New SeriesNo. 106

Palaeontological Society of Japan
June 30, 1977

EditorItaru HAYAMI

Associate editors Ikuwo OBATA and Tomowo OZAWA

Officers for 1977 -1978
Honorary President: Teiichi KOBAYASHI
President:

Ryuzo TORIY AMA

Councillors: Kazuo ASAMA, Kiyotaka CHINZEI, Takashi HAMADA, Tetsuro HAN AI,
Itaru HAY AMI, Syozo HAY ASAKA, Hisayoshi IGO, Tadao KAMEl, Kametoshi
KANMERA, Tamio KOTAKA, Tatsuro MATSUMOTO, Tsugio SHUTO, Yokichi
T AKAYANAGI, Toshimasa T ANAl, Hiroshi UJIIE
Members of Standing Committee: Kazuo ASAMA (Membership), Kiyotaka CHINZEI(General Affairs), Takashi HAMADA (Foreign Affairs), Tetsuro HANAI, Itaru HA YAMI (Transactions), Hisayoshi IGO (Planning), Kametoshi KANMERA(Special Papers), Yokichi TAKA YANAGI ("Fossils"), Hiroshi UJIIE (Finance),
Juichi YANAGIDA
Secretaries:

Ienori FUJIYAMA (Special Papers), Kunihiro ISHIZAKI ("Fossils"),

Ikuwo OBATA and Tomowo OZAWA (Transactions), Kazuhiko UEMURA(Membership), Toshiyuki YAMAGUCHI (General Affairs)
Auditor: Tatsuaki KIMURA

The fossil on the cover: Original figure of Podozamites Reinii GEYLER,
1877, from the Tetori group. GEYLER'S description marked the onset ofmodern palaeontology in Japan.

All communications relating to this Journal should be addressed to the
PALAEONTOLOGICAL SOCIETY OF ]AP AN,
c/o Business Center for Academic Societies,
Yayoi 2-4-16, Bunkyo-ku, Tokyo 113, Japan.
Sole agent:

University of Tokyo Press, Hongo 7-3-1, Tokyo, Japan.

Trans. Proc. Palaeont. Soc. Japan, N. S., No. 106, pp. 61-70, pIs. 7, 8, June 30, 1977

675. NUMMULITES BONINENSIS FROM THE AMAMI PLATEAUIN THE NORTHERN MARGIN OF THE PHILIPPINE SEA *ISAO KONDA
Nara Senior High School, Nara 630

KAZUMI MATSUOKA
Department of Biology, Osaka City University, Osaka 558

AKIRA NISHIMURA and TERUFUMI OHNO
Department of Geology and Mineralogy, Kyoto University, Kyoto 606m~~#aii'iJ' I? (J) Nummulites boninensis: ~~#aii'iJ' I? F' l/ -;I : / I;: J: IJ
I?nt-.: ?( ;/ A
Y T .7-. It, IH1:)jj(im~£3:~(J)9=tmlMl~*fti.J' l?i1itt" 7.J Nummulites boninensis HM,zAWA I;:~~~n, jlj§:~~lt?i-~l:~~, Ij -t~(J) 2 ~1;:5tiJ,n7.Jo ilfJ~tr' N. boninensis forma M,
1&~tr' N. boninensis forma S c L, k(J) 2 ~~;: ")\, '-C, ?i-ml~rrn, P'lmlfi\i';]!f, c ~;:lamellachamber (J)JE~~jl;;tr' ltt:c, ~c1t Lt-.:o

<

c

~ffi

m, ~~~~, ~M ~, *ff~x

Plateau in the northern margin of thePhilippine Sea is one of the most noticeable results of this cruise. Several
hundreds of microspheric nummulitids
and a large number of megalosphericones were obtained. These specimensof nummulitids are all identified to
Nummulites boninensis HANZA WA, described originally from the middle Eocene
strata of Haha- jima (Hillsborough Island),Ogasawara (Bonin) Islands (HANZA WA,
1947).
The microspheric specimens,
however, are divided into two forms
with thick test and thin test from theexternal views. Such a phenomenon
was first reported from Haha- jima by
YOSHIWARA (1902), who assigned thethicker form to Nummulites' java nus
VERBEEK described from the Eocene ofIntroduction
The eleventh research cruise of Japanese Geodynamics Project in the West
Pacific was carried out by the R/VTokaidaigaku-maru II in August, 1974.
During this cruise, in which the authors
participated, many traverses of echosounding and seismic reflection profilingand frequent sampling of bottom sediments were enforced~ A brief note anda paleontological preliminary report werealready made by the Research Members
of GDP-ll Cruise (1975) and KONDA etal. (1975).
Discovery of Eocene larger foraminifers
including nummulitids from the Amami* Received July 30, 1975: read January 26,
1975 in Tokyo.

61

62

Isao KONDA et al.

Java and the thinner one as a varietyof the same species or a different
species. HANZAWA (1947) distinguishednummulitids of Haha-jima from otherknown species and established a new
species, NummuLites boninensis. He mentioned briefly a wide morphologicalvariation of the microspheric specimens
but did not describe it in detail. Lately,
IWASAKI and AOSHIMA (1970) reported
that the flatter and irregularly undulated
form is more abundant in the fine-grained
rock, while the thicker form is contained
more abundantly in the coarse-grainedrock.
In the present article, the authors
describe the morphology of the twoforms of microspheric generation of
Nummulites boninensis HANZA WA obtained from the Amami Plateau. As theinformation about their mode of occurrence is relatively poor because of thedredge haul, the geological and paleonto-

logical significance of their coexistence
is not discussed. The morphologicalcriteria of the two forms, however, areshown in the present article.
Acknowledgements
First of all, the authors are deeply
indebted to Captain Magoshichi SATO
and the crew members of the Tokaidaigaku-maru II, who contributed to thesurvey by their excellent operation andnavigation during the GDP-ll cruise.
Thanks are due to Professor Tsunemasa
SHIKI (Chief scientist of the Cruise) and
Dr. Takao TOKUOKA of Kyoto University,
Professor Hitoshi AOKI and Dr. Yoshifumi MISAWA of Tokai University forvaluable suggestions on the geology ofAmami Plateau. Appreciation is expressed to students of the Tokai University who cooperated in the work on
board. The authors' grateful thanks are

132°E

132°30'Er-------------..;::::..:~-------~28°20'N

J'
JO~~~~~-~~Cl ~Om,"oOo~Oo.

d-2000m~ ~~-~500m7fl250Om~'a"""-LJ--V
2500m _
___
__

28°N
4000

---......
"",,--JOOOin~"-...:.3500m~

3000","",,-"--- ~3500m~
4000m____

' ,
AMAMI

PL·~~=TE=A""U-~·3O'N" X

Zl"40'N

rn~02~O~'E~---=======--------====~I~~~O~E~~2---~~--~~~

Fig. 1. Map showing the fossil locality (asterisk). Con tor is shownin meters, adapted from MISAWA and HOSHIZAWA (1975).

28°N

675. Nummulites from the Amami Platea'lt
due to Professor Emeritus Shoshiro
HANZAWA of Tohoku University, Professor Yokichi TAKAYANAGI of the same
university, Dr. Hiroshi U]IIE of National
Science Museum and Dr. Kuniteru MA TSUMARU of Saifama University for valuablesuggestions and discussions on the
paleontological problems.
Materials and Methods
The sampling locality is situated on
the Amami Plateau in the northern
margin of the Philippine Sea (Station
No. GDP-1l-9, 28°04.0'N, 131°37.8'E28°04.4'N, 131°37.8'E, 1390-1410 m indepth). About two hundred isolated
microspheric specimens of nummulitids
were obtained together with many ferromanganese nodules by a chain bag
dredge. In a cylindrical sampler employed at the same locality, several
hundreds of microspheric specimens, alarge number of megalospheric ones,
numerous specimens of other Eocene
larger foraminifers, a few ferromanganese
nodules, and limestone gravels were
contained together with a large quantityof Recent foraminiferal sand. The nummulitids are coated with thin ferromanganese oxide peel, and some of the
microspheric forms are bored by organisms.
HANZAWA (op. cit.) assigned the ageof Nummulites boninensis from Haha- jima
to the middle Eocene (Lutetian), and
SAITO (1962) also correlated the planktonic foraminiferal fauna accompaniedby the nummulitids from Haha-jima with
the Porticulasphaera beckmanni Zone of
Trinidad (=P. mexicana Zone of BOLLI,1957) considered to represent a part ofthe middle Eocene. KANEOKA et al. (1970)
reported that the pyroxene andesite
conformably overlain by a tuff layer
with abundant Nummulites boninensis

63

HANZAWA indicates a K-Ar age ofabout 40 m. y. which may be slightly
younger than the true age. Anyway,
the age of the nummulitids from Hahajima is now thought to be the middle
Eocene. As already mentioned, manylarger foraminifers are associated with
the nummulitid in the sample from theAmami Plateau. They are Asterocyclina
penuria COLE, Asterocyclina sp. and Discocyclina sp. Although these coexistinglarger foraminifers may have been
derived from some different horizons, allof them indicate the middle to late
Eocene age. Furthermore, because thenummulitids and these larger foraminifers
are well preserved, they are thought tohave been derived from the middle toupper Eocene strata in the adjacent areaof the sampling station. For the present
study about two hundred microspheric
and about fifty megalospheric specimens
were utilized. The observations weremade on the external views, thin sections
along the axial and sagittal planes, andartificial splits mentioned by HANZAWA(1947). And ARNY'S (1967) graphic presentation of the growth mode was adopted
to show the diagnostic features of thegrowth mode in the two forms of asingle species. The measurements along
the sagittal line and spiral axis weremade on 1) the height of chambers, 2)
the same height plus the thickness ofspiral lamella and 3) distance between
the outer side of spiral lamella in eachwhorl and the floor of chamber of thesecond whorl near the center of test(see Figs. 4 and 5).
Measured and illustrated specimens
are deposited in the paleontological collections of the Department of Geology
and Mineralogy, Faculty of Science,
Kyoto University, Kyoto.

Isao KONDA et al.

64
Systematic Descriptionx

Family Nummulitidae
DE BLANVILLE, 1825

X xxx

x xx)()()(. Genus Nummulites LAMARCK, 1801

X

x

x)(
xxxxx

xxx x

xx

xx xx
x xxxxx x

Nummulites boninensis HANZAWA, 1947x )()()/C
xx
x x
xx
x

PI. 7, figs. 1-9, PI. 8, figs. 1-4xx)(x)()(X

X

xx

Nummulites boninensis HANZAWA: HANZAWA,
1947, pp. 247-259, pI. 39, figs. 1-7, pI.
40, figs. 1-9.

Description.
Megarospheric form: Test lenticularwith an acute periphery, 3.5 mm inaverage diameter and 1.8 mm in average
thickness, rarely asymmetrical, with one
side more inflated than another; surface
smooth, septal filaments numerous, radial,
flush with the general surface ·of test;
heads of pillars embedded in spirallamellae, usually found on septal filaments as tiny spots, sometimes elevatedas granules on the surface of test; septa
a little inclined, slender and gently
curved; chambers generally higher thanbroad with their dimensions not changing much from central to outer whorls;
later chambers occasionally becoming
broad and low; thickness of spirallamellae fairly constant, 300 to 330
microns in sagittal section, and 125 to
250 microns in axial section, thoughbecoming thicker from central to peripheral part of test; development ofpillars variable, several narrow pillars
scattered in central part of test andtheir diameters attaining to 150 microns
in some sections, but scarcely developedin the other.
Microspheric form: Test discoidal withdiameter of 20 to 35 mm in general, of
41 mm in maximum, and consisting of aminute proloculus and closely coiled

2

3

4

~

5

Diameter in mm.

Fig. 2. Scatter diagram showing therelation between the diameter and thickness of the megalospheric tests.
Table 1. Number of chamber in theearlier stage of the microspheric specimens.
I, II······ : first whorl, second whorl, ...... :Whorls type specimen* forma M forma S
I

10

11

12

II

23

12-16

12-21

III

25

18-26

22-30

IV

31

21-23

29-37

V

35

.22-3433-40* Based on a figure illustrated in the original description (HANZAW A, 1947, pI. 40,
fig. 6).

whorls, usually more than 25 in number;thickness of test indicating bimodal frequency distribution with two peaks,
around 4 to 6 mm and 7 to 10 mm, sothat the sample is divided into two
types: thicker one with a rounded periphery and flatter one with an acuteperiphery; number of individuals of the
thicker type as twice as that of flatter
one; granulation invisible on surface oftest.

675. Nummulites from the Amami Platea1t
Numerous septal filaments clearlyvisible through semi-transparent spirothecal wall, meandriform and complicatedly anastomosing; three filaments
counted within 1 mm; septa diagonal,
gently curved and connected with outerlamella in a narrow angle; pillars numerous and starting from sagittal plane oftest up to 170 microns in diameter, but
their heads embedded in spiral lamellae
and not raised on general surface of test.
Rerwrks: Some important features ofpresent specimens of microspheric andmegalosperic generations such as septa,
septal filaments and pillars are quite
coincident to those of Nummulites
boninensis HANZA w A from Haha- jima.

65

In microspheric generation, however,two forms are distinguished mainly on
the basis of the thickness of test andthe acuteness of periphery.
In thepresent article, the thicker and thinner
forms are called henceforth forma M
and 5 respectively.
F.orma M shows thick test with broadly
rounded periphery and relatively small
form ratio (diameter/thickness proportion
ranging from 2.0 to 4.0. Because thetest shape resembles Manju (a Japanese
bean-jam bun), the initial of Manju isapplied for the name of this forma. In
sagittal section, the height of chamber
and the thickness of spiral lamella increase as far as fifth to eighth whorls,•

forma f.J+

forma S

•
•

15

•

~

•

•• •

.....

•

.....

10

••
••• ••• • • 4-:::- •

...

5
++

+

+ + ...

+!:.+++:.+

+

+

+ +

°1~0----~----~~~~--~----~30~----~----T.40~
Diameter in mm.

Fig. 3. Scatter diagram showing the relation between the diameterand thickness of the microspheric tests.

66

Isao KONDA et al.

where they attain about 350 and 250
microns respectively (see Fig. 4). From
there to outer whorls, the height ofchamber becomes variable. Its change

is greater and more frequent in the
middle whorls than in the inner and theouter ones. In the outer whorls of spire,
the height of chamber is fairly constant

Nummuli tes boninensis forma N

14lrnm

D/T = 2.1

12

10
8

800

6

600

4

400
\, /".\

2

\I

,
\,-

....... _------..

_--_ ...... -_ .. -0L-~~~------'1~0----~1~5~----~2nO----~2~5------3t.O~--~13~5----~4UOl
l6~

rnm

Number of whorls
Nummulites boninensis forma S

D/T = 9.6

14

12

10
8
6

600

4

400

2

200

o
Number of whorls
Fig. 4.

Graphic projections of the characteristics of the microspheric
form in sagittal sections.
Broken line and thick line show the height of chamber and the same height plus the
thickness of spiral lamella in each whorl, respectively (scale on the right side). The distance between these two lines, therefore, represents the thickness of spiral lamella.
Thin line connecting dots shows the distance between the outer side of spiral lamellae
in each whorl and the floor of chamber of the second whorl, and consequently, it corresponds to the well-known "winding curve". In the measurements of the height of chamber
and the same height plus the thickness of spiral lamella, the first whorl is omitted
because of difficulty in accurate measurements of them.

11

67

675. Nummulites from the Amami Plateau
and about 50 microns. Thus, the height/
length proportion of chamber varies
from the inner part to the outer, i. e.,
three to one in the inner, one to one in
the middle, and one to two in the outerpart. The thickness of spiral lamella
scarcely changes throughout the whole
spire except for the inner whorls, where
it is larger than in the outer. The meanvalue of thickness of spiral lamella isabout 140 microns, and the number ofJwhorls is about 43 on an average. In
axial section, the height of chamberincreases with test growth. The spirallamellae, on the other hand, are thicker
in the early stage of growth than in thelater (see Fig. 5).
Forma S is characterized by the thintest with a narrow and rounded to moreor less acute periphery and relatively
large form ratio ranging from 4.0 to
10.0. This type is similar in shape to

Nummuli tes boninensis forma M

D/T = 2.3
300

mm

]J

200

2

Number of whorls
Nummulites boninensis forma 5

D/T = 6.8

J

100

mm

o

10

]J

20
15
25
Number of whorls

Fig. 5. Graphic projection of the characteristics of the microspheric form inaxial sections. Broken line and thick line show the height of chamber along theaxis and the same height plus the thickness of spiral lamella in each whorl, respectively (scale on the right side). Thin line connecting dots represents theincrease of the thickness of test (scale on the left side).

68

Isao KONDA et al.

Senbei (a Japanese rice cracker), theinitial of which is used for this forma.
In sagittal section, the height of chamber
and the thickness of spiral lamella increase together with the test growth as
far as the seventh to eighth whorl,
where they attain to about 400 and 250
microns, respectively (see Fig. 4). From

there to the outer whorls, the height ofchamber decreases abruptly. In theouter whorls of spire, it is about 100
microns, and the chamber is slightly
higher than broad. The height/length
proportion of chamber is about two to
one in the inner several whorls andabout one to one in the major part.
+-+

forma S
forma

M

10

/t

5

/
/

/
/,. ...... ,
:to

.-

.,.~

......................................-......................

..... -........

+,".:~f-/... -...

....-....

-..........

O~----~5----~10~----~15~--~2~O----~25~--~~­
Ntunbei· of whorls

Fig. 6.

Changes of form ratio (diameter/thickness proportion) with test growth.

Explanation of Plate 7
Fig. 1. Lateral view of Nummulites boninensis forma M. Sample No. ]C 1001. xL 7
Fig. 2. Lateral view of Nummulites boninensis forma S. Sample No. ]C 1002. xL 7
Fig. 3. Peripheral view of the same specimen as. Fig. 1. xL 7
Fig. 4. Peripheral view of the same specimen as Fig. 2. x 1.7
Fig. 5. A part of lateral view. of the same specimen as Fig. 1. x 5
Fig. 6. A part of lateral view of the same specimen as Fig. 2. x 5
Fig. 7. Lateral view of megalospheric form of Nummulites boninensis HANZAWA. Sample No.
]C 1007. x 12
Fig. 8. Sagittal section of megalospheric form of Nummulites boninensis HANZAWA. Sample
No. ]C 1008. x 12
Fig. 9. Axial section of megalospheric form of Nummulitesboninensis HANZAWA. Sample No.
]C 1009. x 12

KO NDA et al.:Nummulites from the Amami Plateau

Plate 7

675.

Nttmmulites from the Amami Plateau

The thickness of spiral lamella scarcely
changes throughout the whole spire
except for the inner whorls. Its meanvalue is about 200 microns. The numberof whorls is about 30 on an average.
In axial section, the height of chamber
is generally smaller than in forma M
and furthermore, the thickness of spirallamella is smaller than a halt of that offorma M (see Fig. 5). Consequently, thetest of forma 5 becomes flatter with thegrowth in comparison with forma lvI.
The microspheric specimens of N.
boninensis illustrated by HANZA WA (1947,
PI. 39, figs. 1:"8, PI. 40, fig. 6) seem tobe assigned to forma 5 here described.
In conclusion, these two forms of
microspheric generation seem to represent a range of variation within a single
species, Nummulites boninensis HANZA w A,
because such essential characteristics asinternal structure and skeletal pattern
are the same, and because any difference
corresponding to this variation is notobserved in the megalospheric specimens.

69

References
ARNY, P. (1967): A comprehensive graph ofthe essential diagnostics of Nummulites.
Micropaleontology, vol. 13, no. 1, p. 41-54.
BOLLI, H. (1957): Planktonic Foraminiferafrom the Eocene Navet and San Fernand
formations of Trinidad, B. W. 1. U. S.
Nat. Mus., Bull., 215, p. 155-172, pIs. 3539.
HANZAWA, S. (1947): Eocene Foraminiferafrom Haha- jima (Hillsborough Island).
Jour. Paleollt., vol. 21, no. 3, p. 254-259,
pIs. 39, 40.
IWASAKI, Y. and AOSHIMA, M. (1970): Report on geology of the Bonin Islands.
The Nature of the Bonin and the Volcano
Islands (edit. Ministry of Education), p.
205-220, pIs. 1, 2, (in Japanese withEnglish abstract).
KANEOKA, 1., ISSI-IIKI, N., and ZASI-IU, S.
(1970): K-Ar age of Izu-Bonin Islands.
Geochem. Jour., vol. 4, p. 53-60.
KONDA, 1., HARADA, K., KITAZATO, H.,
MATSUOKA, K., NISHIDA, S., NISHIMURA,
A., Ol-INO, T. and TAKAYA~-IA, T. (1975):
Some paleontological results of the GDP1, 8, 11 Cruises. Geological problems ofTable 2. Statistics of megalospheric specimens.
I, II, ...... : first whorl, second whorl, .......
Diameter ofproloculus

Specimens

1
Number ofwhorls(I-'-)

1

783

2

696

Numbers ofchambers
in whorl

Height of whorls(mm)

rlrrlmlrv r -rr-~l~

3--.L
4

71~1~- 1. 46 2.54 3.38

3

fi

1_-

17

1. 42

28

I

-12.25 2.83

- - - - - -- - - - - -

3

826

-I

730

4~
2

1
i

1042

5

I

I

I

6

12

24

33

1. 92

3.63

4.33

- - i: - - -Ii 20 28 1. 71 2. 46 • 3. 17 l 4. 01

4--.L
4

7112

4~

7114122130 ! 2. 13

2

2.75

I

I

'

3.251~1~I

I

Isao KONDA et al.

70

the Philippine Sea (edit. Geol. Soc. Japan),p. 91-98, pIs. 1, 2. (in Japanese).
MISAWA, Y. and HOSlIIZAWA, M. (1975):
Submarine topography and results ofcontinuous seismic profiling studied in
the GDP-ll Cruise. Ibid., p. 75-81, (inJapanese) .
RESEARCH MEMBERS OF THE GDP-11 CRUISE(1975): Nummulites, and pebbles ofhornblende-tornalite and other igneousrocks, collected at the Amami Plateau,

Jour. Ceo!. Soc. Japan, vol. 81, no. 4, p.
269-271, (in Japanese).
SAITO, T. (1962): Eocene planktonic Foraminifera from Haha-jima (HillsboroughIsland).
Trans. Proc. Palaeont. Soc.
Japan, N. S., no. 45, p. 209-225, pIs. 32-34.
YOSHIWARA, S. (1902): Geological age of
the Ogasawara Group (Bonin Islands) as
indica ted by the occurrence of Nummulites.
Ceo!. Mag., Des. 4, vol. 9, pp. 296-303.

Amami Plateau 1it~$a, Ogasawara (Bonin) Islands 'J,j1:!JlCml1h, Haha-jima (HillsboroughIsland) fJ:l1h

Explanation of Plate 8
Sagittal section of Nummulites boninensis HANZAWA forma M.

Fig.!.

Sample No. JC 1003.

x2.5

Fig. 2.

Sagittal section of Nummulites boninensis HANZAWA forma S.

Sample No. JC 1004.

x2.5

Fig. 3.
Fig. 4.

Axial section of Nummulites boninensis HANZAWA forma M. Sample No. JC 1005.
Axial section of Nummulites boninensis HANZAWA forma S. Sample No. ]C 1006.

x8x8

KONDA et al. :Nummulites from the Amami Plateau

Plate 8Trans. Proc. Palaeont. Soc. Japan, N. S., No. 106, pp. 71-88, pIs. 9-12, June 30, 1977

676.

PALYNOLOGY OF THE LOWER TERTIARY CONCEPCIONFORMATION, CENTRAL CHILE'KIYOSHI TAKAHASHI
De;:>artment of Geology, Nagasaki University

CP~"f-Y -Ttfll~::::*c::z /-1::7'./3 /T@O)/{Y / P : ) - : JlJ*"f- Y -~II'~tfllo)::Z /-1:
:7 './ 3/0) f¥jt,'f,0) ::z P* ER 0)/l.-

EEl::z / -I: :7 './ 3 /?k:ERI~O) ::fiJ}{ ii' G ~ G h t;:{E~ • ill!Ff ltf~

It~/!§tj~· ~amO)Il?JT 62% (trilete 53.5%, monolete 8.5%), f!l!TM~:ft~ 4% (sac-cate 0.5%, inaperturate 3.5%), ~Tjjtl~i't~ 34% (monocolpate 1.5%, dicolpate c!::tricolporate1.5%, triporate 31%) J: I)t.r.Qo Il?JT-c'lt5;f[!~. 1E~-c'lt3;f[!~~;f[!c!:: L-c ~ct\( L, "i t..:/l?lT-C'lt 3 ;f[!iI;, :ftf5J-c-lt 12 ;f[!iI;Ttfll~::::~I:::.fJtl:::'%J Gh L\,' Q :m!m-c';!; Q.:. c!:: ~Ij)j GiI'l:::' Lt..:o Triorites minor COUPER ,t.:.h"i -C':;';:l. -:) - =7 / F', ?!- - 7- !- =7 Y70)l::tfll~:;lUcl:'%JGh -C~'Q ~O)-c-;!;Qo Myrtaceidites parvus COOKSON & PIKE It.:.
h"i-c'?!--7-!-=7 Y 70)Ml~1lt-f!lf~1ltI:::'9:i1GhL\,'Q ~O)-c';!; I), -*;f[!mO)t±lm.O)~f\;;~1;)!W-t Q c!:: ~::::~fJJJtIlt.r.~' L Ml~1ltI:.t±lm. L -C ~'Q ~ O)iI:iI't.r. I) J..
::z / -1::7 './ 3 / T@O)
~f\;;IHa~1lt c!:: :;If X. G h Q 0.:. O):ft~. Il?JTtW~~ B *0)15~::::~0) ~ 0) c!:: Jt~-t Q c!::, -to)mnli:0)!flfi'~7:1t ~ 1i<t.r.
"?-C:to I), c!:: 1:::.Il?JTO)t±lm.~iI;i\1Ii
f!l!Tjj!:t0{E~O)t±lm.~iI;{~~'o)lt!flf1i<-C·;!;Qo .:. 0)tW~lt 5 t ereispori t es-G I ei chenii d i t es-Tri poropoll en it es- M yrtacei d i t es-Su bt riporopol-

<,

<

<

<,

lenites O)mif-ltil::±'f*c!::t.r."?-C~'Qo;\1Ij~

ii1J

Introduction

Acknowledgements

The coal material investigated wasprovided by Prof. S. MAEDA, Department of Geology, Faculty of Science,
Chiba University, who collected it fromthe Eocene Concepcion Formation in theConcepcion area, central Chile.
The author has found many sporesand pollen grains in the coal material
from the Concepcion Formation. Thirtyfour species of plant microfossils consisting of micros pores and pollen grains,are described in this paper.
Eightspecies are instituted as new species.

The author expresses his gratitude toProf. Dr. S. MAEDA, Department of
Geology, Faculty of Science, Chiba
University, for supplying the sample
material upon which this study isbased. Thanks are also due to Prof. Dr.
T. KIMURA, Department of Earth Sciences, Tokyo Gakugei University, forproviding some literature on paleobotanyand palynology of South America.
Material and method

The examined coal sample was obtained from the Concepcion Formationin the Concepcion area, central Chile.
The sample is a bituminous coal.
The material was processed by me-* Received Feb. 12, 1977; read Jan. 21, 1977
in Tokyo.

71

Kiyoshi TAKAHASHI

72

mixture of solid paraffin and canadabalsam.
All specimens illustrated in this paper
and the sample from which they wereobtained are in the palynological collection of the Department of Geology,
Nagasaki University.

--11-------+----1'7=;:---+-- 0°

Palynological assemblage--+--i1--\---+-----I--200--~--~----~------~+----400

N

Concepcion.

+o, ' - - - - - -25km',
Coronel (coalfield)

Text.fig. 1. Index map showing thesampling locality (x) at Coronel· coalfieldnear Concepci6n.

chanical and chemical methods (maceration by KCI0 3 and cone. HN0 3 , treatment by 15%KOH and then by acetolysis method, centrifuging and .washingin pure water after each step). The
residues were mounted in glycerine
jelly. All slides were sealed with a

The plant microfossils recovered fromthe studied coal material indicate a total of
34 palynomorph types which appear to
be important for characterizing the Concepcion palynological assemblage. This
includes 17 arboreal angiosperms, 2 probable or known non-arboreal angiosperms,
4 gymnosperms, a moss and 11 ferns.
Approximate percentages of counted• specimens for the entire assemblage aremoss and ferns 62% (trilete-53.5%, monolete-8.5%),gymnosperms 4% (saccate0.5%,. inaperturate-3.5%), and angiosperms 34% (monocolpate-1.5%, dicolpate
and tricolporate-1.5%, triporate-31%).
The fossil genera and species foundare as follows;,.··· ,. ,.. ,. r.'oTrilete spores:
Deltoidospora -sp.
Leiotriletes minus n. sp.
Leiotriletes microadriennis KRUTZSCHStereisporites concepcionensis n. sp.
Conravisporites sp;
Triplanosporites minor n. sp.
,Triplanosporites sp.
? Punctatisporites sp.
Gleicheniidites spe.ciosus n. sp.
Glei.cheniidites circinidites (COOKSON) n.
comb.
l'v1;onolete spores:
Laevigatosporites ovulatus n. sp.
Laevigaiospor'itesC dehiscens T AKAHASI-l[
Pollen grains:
Dacrydiumites d. florinii COOKSOK & PIKE
Inaperturopollenites pseudodubius
TAKAHASHI

Inaperturopollenites laevigatus TAKAHASHI

676. Palynology of the Concepcion Formation, Chile
Ephedripites sp.
Monocolpopollenites cf. kyushuensis
TAKAHASHI

Liliacidites variegatus COUPER
Smilacipites setarius (R. POTONIE) R.
POTONIE

Triatriopollenites sp.
Triporopollenites festatus TAKAHASHI
Momipites sp.
Myrtaceidites parvus COOKSON & PiKE
forma anesus COOKSON & PIKE
Myrtaceidites Pdrvus COOKSON & PIKE
forma nesus COOKSON & PIKE
Myrtaceidites sp.
Triorites minor COUPER
Triorites cf. harrisii COUPER
Subtriporopollenites rotundus n. sp.
Sub triporopollenites falsus n. sp.
Subtriporopollenites levius TAKAI-IASHI
Dicolpopollis sp.
Tricolporopollenites sp.
Rhoipites bradleyi WODEHOUSE
Rhoipites sp.
Foveotricolporites foveolatus n. sp.

The microflora of the Concepcion Formation consists mainly of many species
appearing in Lower Tertiary: Leiotriletes microadriennis KRUTZSCH, Gleicheniidites circinidites (COOKSON) n. comb.,
Laevigatosporites dehiscens TAKAHASHI,
Dacrydiumites cf.jiorinii COOKSON & PIKE,
Inaperturopollenites pseudodubius T AKAHASHI, Inaperturopollenites laevigatus
TAKAHASHI,
lvIonocolpopollenites
cf.
kyushuensis
TAKAHASHI,
Liliacidites
variegatus COUPER, S71lilacipites setarius(R. POTONIE) R. POTONIE, Triporopollenites fesiatus TAKAHASHI, Subtriporopollenites levius TAKAHASHI, Tri01'ites d.
harrisii COUPER, Rhoipites bradleyi
WODEHOUSE, lvIyrtaceidites parvus COOKSON & PIKE forma anesus COOKSON &PIKE, and lvIyrtaceidites parvus COOKSON& PIKE forma nesus COOKSON & PIKE.
Of these species, Leiotl'iletes microadriennis KRUTZSCH, Gleicheniidites circinidites -(COOKSON) n. comb., Smilacipites
setarius -(R. POTONIE) R. POTONIE, - Sub-73

triporopollenites
levius
TAKAHASHI,
Triorites cf. harrisii COUPER, Rhoipites
bradleyi W ODEHOUSE, lvIyrtaceiri.ites parvus
COOKSON & PIKE forma anesus COOKSON& PIKE, and lvIyrtaceidites parvus COOKSON & PIKE forma nesus COOKSON &PIKE appear only in Paleogene or Tertiary.
Other species appear in both
Lower Tertiary and Upper Cretaceous.
Triorites minor COUPER is only an Upper
Cretaceous species from New Zealand.
Foveotricolporites foveolatus n. sp. issimilar to Foveotricolporites caldensis
GUZMAN from the pollen zone I(a)(Lower Eocene) of .Tibu area, Colombia.
All above-mentioned species except
Triorites minor COUPER appear commonly
in Paleogene or Eocene. Accordingly,
the Concepcion Formation indicates apossibility to be an Eocene age.
Stratigraphic and geographic distribution of all above-mentioned species issummariz·ed as follows.
Leiotriletes microadriennis KRUTZSCH
Eocene: Geiseltal, Germany.
Eocene: Dorog, Bakony, Hungary.
Gleicheniidites circinidites (COOKSON)
n. comb.
Early Tertiary: S. Australia, Victoria, Australia.
Laevigatosporites dehiscens TAKAHASHI
Paleogene-Miocene: W. Honshu, N.
Kyushu, Japan.
Carripanian-Maastrichtian: Hokkaido,
Japan.
Upper Cretaceous: Quiriquina Formation, Chile.
Dacrydiumites jiorinii COOKSON & PIKE
Paleocene-Pliocene: New Guinea,
N. S. Wales, Victoria, S. Australia,
W. Australia, Tasmania.
Maastrichtian-Paleocene:
Dorotea
Formation, -Argentina.
Inaperturopollenites pseudodubius T AKAHASHi
Paleogene-Miocene: W .. Honshu, N.

Kiyoshi TAKAHASHI

74
Kyushu, japan.
Cretaceous-Paleogene:NE. Honshu, japan.

Triorites minor COUPER
Hokkaido,

Inaperturopollenites laevigatus T AKAHASH!
Paleogene-Miocene: W. Honshu, N.
Kyushu, japan.
Cretaceous-Paleogene: Hokkaido, NE.
Honshu, japan.
Upper Cretaceous: Quiriquina Formation, Chile.
Monocolpopollenites kyushuensis T AKAHASH!
Paleogene-Miocene: W. Honshu, N.
Kyushu, japan.
Upper Cretaceous-Paleogene: Hokkaido, japan.
Liliacidites variegatus COUPER
Paleocene: Chubut Province, Argentina.
Maastrichtian-Paleocene:
Dorotea
Formation, Argentina.
Maastrichtian-Miocene,
Southland,
New Zealand.
Smilacipites setarius (R. POTONIE) R.
POTONIE
Eocene: Geiseltal, Germany.
Triporopollenites festatus T AKAHASH!
Paleogene-Miocene: W. Honshu, N.
Kyushu, japan.
Upper Cretaceous-Paleogene: Hokkaido, japan.
Turonian-Eocene: Sarawak, Malaysia.
Upper Cretaceous: Quiriquina Formation, Chile.
Myrtaceidites parvus COOKSON & PIKE
forma anesus COOKSON & PIKE
Eocene-Pliocene: W. Australia, S.
Australia, Victoria, New Guinea.
Upper Cretaceous: Quiriquina Formotion, Chile
Myrtaceidites parvus COOKSON & PIKE
forma nesus COOKSON & PIKE
Eocene-Pliocene: S. Australia, Victoria, N. S. Wales, Queensland, Austrat1.a.

Upper Cretaceous: Kaitangata coalfield, New Zealand.
Turonian: Port Campbell No.2,
Victoria, Australia.
Triorites harrisii COUPER
Early Tertiary: Wangerrip Group,
Victoria, Australia.
Oligocene: Southland, New Zealand.
Subtriporopollenites levius T AKAHASH!
Paleogene: N. Kyushu, japan.
Rhoipites bradleyi WODEHOUSE
Eocene: Green River Formation,
U.S.A.

Descriptive palynology
Anteturma Sporites H. POTONIE 1893.
Turma Triletes REINSH 1881 emend.
R. POTONIE & KREMP 1954.
Subturma Azonotriletes LUBER 1935.
Infraturma Laevigati BENNIE &KIDSTONE 1886 emend. R.
POTONIE 1956.
Genus Leiotriletes NAUMOVA 1937
emend. POTONIE & KREMP 1954.
Type species: Leiotriletes sphaerotriangulus (LOOSE 1932) POTONIE & KREMP
1954.

Leiotriletes minus n. sp.
PI. 9, figs. 19-21

Description: Spores trilete; outline
triangular in polar view, with slightly
concave sides and somewhat rounded
angles.
Trilete mark straight andreaching to the equator. Prominent
folds 1.5 fl. wide, often of unequal length,
accompany the trilete mark. Exine thin,chagrenate. Grain size 23.5-27.2 fl..

676.

Palynology of the Concepcion Formation, Chile

Holotype: PI. 9, fig. 20; grain size
27.2 p, exine thin; slide GN 2527.
Occurrence: Few; Concepcion Formation (Eocene) in the Concepcion area.
Remarks: The present specimens aresuperficially similar to Leiotriletes spp.
(G. M. BRATZEBA, 1969, pI. 8, fig. 3; pI.
20, fig. 4) from the Upper Cretaceous
formations, Far East.
Botanical affinity: ? Schizaeaceae.

Leiotriletes microadriennis KRUTZSCH
PI. 10, fig. 1

1959. Leiotriletes microadriennis KRUTZSCH,
Geologie, vol. 8, no. 21-22, p. 61, pI. 1,
figs. 3-7.

Dimensions: Grain size 51.7 p, exine
1.3 p thick, chagrenate.
Occurrence: Very rare; Concepcion
Formation (Eocene) in the Concepcion
area.
Remarks: This specimen is identified
with Leiotriletes 11licroadriennis describedby W. KRUTZSCH from the lower coalseams (middle Eocene) at Geiseltal.
Botanical affinity: Schizaeaceae, cf.

Lygodium.
Genus Stereisporites THOMSON &75

Arcuate thickening of the spore wall on
the proximal face subtent angles between
the laesurae. Exine psilate, less than
1 p thick; a thickend zone 2-3.5 p widesurrounds the equator Equatorial diameter 19.3-25.4 p.
Holotype: PI. 9, fig. 5; equatorial
diameter 22 p, laesurae about 1/2 spore
radius (5 p long), a thickened zone 3.5 p
wide; slide GN 2536.
Occurrence:
Frequent; Concepcion
Formation (Eocene) in the Concepcion
area.
Remarks: The present specimens arevery similar to Sphagnum antiquasporites
WILSON & WEBSTER (1946, p. 273, fig. 2)
from the Paleocene Fort Union Formation of Montana, but the Concepcion
specimens are different from the Montana
species in thickness of the thickened
zone.

Botanical affinitv: SPhagnum.
Genus Concavisporites PFLUG

1953 emend. DELCOURT &SPRUMONT 1955.
Types pecies: Concavisporites rugulatus
PFLUG 1953.

Concavisporites sp.

PFLUG 1953.

PI. 9, fig. 22

Type species: Stereisporites stereo ides
(POTONIE & VENITZ 1934) THOMSON &PFLUG 1953.

Description: Spore trilete. Amb triangular in polar view, with concave
sides and rounded angles. Trilete markstraight and reaching to the equator.
Exine thin, punctate or chagrenate.
Grain size 29 p.
Occurrence: Rare; Concepcion Formation (Eocene) in the Concepcion area.
Remarks: Only one specimen was
found. This is similar to Concavisporites
macellus TAKAHASHI (1964, p. 192-193,
pI. 23, figs. 18-19) from the Campanian

Stereisporites concepcionensis n. sp.
PI. 9, figs. 1-7

Description: Spores trilete, outline
triangular or subtriangular in polar
view, with convex sides and rounded
angles. The laesurae of the tetrad scar
simple, about 1/2-2/3 spore radius.

Kiyoshi TAKAHASHI

76

Hakobuchi Group, Hokkaido, Japan, but
is different from the latter in length of
Y-mark.
Botanical affinity: Unknowri.
Genus Triplanosporites PFLUG 1953.
Type species: Triplanosporites sinuosus
PFLUG 1953.

rounded.
Occurrence: Rare; Concepcion Formation (Eocene) in the Concepcion area.
. Remarks: Only one specimen was
found. This specimen differs from
Triplanosporites minor n. sp. in having
compressed rhombi~ form and roundeddistal pole.
Botanical affinity: Unknown.

Triplanosporites minor n. sp.
PI. 10, figs. 2-3

Description: Spores trilete, outline
in equatorial view rhombic; polar axis
longer than equatorial axis. Trilete
mark distinct, reaching almost to theperiphery. The proximal and distal
poles peaked. Exine thin, psilate. Grainsize: polar axis 20-27.3 p, equatorial axis
18.5-27 p.
Holotype: PI. 10, fig. 3; polar axis 27.3
p, equatorial axis 27 p; exine thin; slide
GN 2532.
Occurrence: Few; Concepcion Formation (Eocene) in the Concepcion area.
Remarks: The species differs from
Triplanosporites microsinuosus PFLANZL(F. MURRIGER & G. PFLANZL, 1955, p.
87, pI. 5, figs. 12a-b; pI. 6, figs. 21a-b;
W. KRUTZSCH, 1962, p. 42, figs. 1-16) inhaving extremely thin exine and smaller
size.
Botanical affinity: Unknown.
Triplanosporites sp.

Genus Punctatisporites IBRAHIM 1933
emend. POTONLE & KREMP 1954.
Type species: Punctatisporites punctatus IBRAHIM 1933.
? Punctatisporites sp.
PI. 10, fig. 5

Description:
Spore trilete; outline
circular in polar view. Trilete markstrong, straight and not reaching to theequator. Exine 5 p thick, fine punctate(?). Grain size 71 p in diameter.
Occurrence: Rare; Concepcion Formation (Eocene) in the Concepcion area.
Remarks: It is not accurately determined whether the present specimen belongs to Punctatisporites or not, becauseof its poor preservation.
Botanical affinity: Unknown.
Subturma Zonotriletes WALTZ 1935.
Infraturma Cingulati POTONIE &KLAUS 1954.

PI. 10, fig. 4

Description: Spore trilete; outline inequatorial view compressed rhombic;
polar axis shorter than equatorial axis.
Trilete mark distinct, reaching almost
to the periphery. Exine chagrenate,thin. Grain size: polar axis· 26.3 p,
equatorial axis 30 p. The distal pole

Genus Gleicheniidites Ross 1949 ex
DELCOURT & SPRUMONT 1955
emend. DETTMANN 1963.
Type species: Gleicheniidites senonicus
Ross 1949.

Gleicheniidites speciosus n. sp.

676.

Palynology of the Concepcion Formation, Chile

PI. 9, figs. 8-15

Description: Spores trilete; outline
triangular in polar view, with usuallysomewhat convex or concave sides andmore or less rounded angles.
The
proximal wall flattened. Exine 4-6 p.
thick at the sides and psilate or chagrenate (on a few spores a faint rugulate
was observed). Trilete mark straightor sometimes somewhat undulating andalways reaching to the equator. Grainsize 35-42.7 p. in diameter.
Holotype: Pl. 9, fig. 8, grain size 39 p.,
exine 5 p. thick at the sides; slide GN
2535.
Occurrence:
Frequent; Concepcion
Formation (Eocene) in the Concepci6n
area.
Remarks: The present specimens are
similar to Gleicheniidites marginatus
TAKAHASHI (1964, p. 191-192, pl. 23, figs.
4-17; pl. 40, fi. 1) from the Campanianand Maastrichtian Hakobuchi Group,
Hokkaido, Japan, but the former differsfrom the latter in size and in details ofform.
Botanical affinity:
GleicheniaceaeGleichenia.
Gleicheniidites circinidites(COOKSON) n. comb.
PI. 9, figs. 16-18

1953. Gleichenia circinidites COOKSON, Aust.
Jour. Bot., vol. 1, no. 3, p. 464, pI. 1,
figs. 5-6.

Dimensions: Grain size 32.8-40 p. indiameter, exine psilate, at the corners
2-2.5 p. thick and increasing to 3-4 f.l at
the sides.
Common; Concepci6n
Occurrence:
Formation (Eocene) in the Concepcion
area.
Remarks: The present specimens are

77

referable to Gleichenia circinidites COOK·
SON (1953) from the Early Tertiary coalat 619.6 feet of core at Comaum, South
Australia, Australia.
Botanical affinity: GleicheniaceaeGleichenia.

Turma Monoletes IBRAHIM 1933.
Subturma Azonomonoletes
LUBER 1935.
Infraturma Laevigatomonoleti
DYBOVA & JACHOWICZ 1957.
Genus Laevigatosporites IBRAHIM 1933.
Type
species:
Laevigatosporites
vulgaris IBRAHIM 1933.
Laevigatosporites ovulatus n. sp.
PI. 10, figs. 6-10

Description: Spores monolete; outline
in lateral view broadly bean-shaped, 2639x21-30 p. (ratio of width to length
0.7-0.9). Exine smooth, thin (less than
1 p.). Mo~olete mark straight or some·what convexly curved and not borderedby ridges. Sometimes folding along thedehiscence furrow.
Holotype: Pl. 10, fig. 7 ; grain size 39x28.2 p. in lateral view, exine thin; ratioof width to length 0.72; slide GN 2536.
Occurrence:
Common; Concepcion
Formation (Eocene) in the Concepcion
area.
Remarks: The present specimens areclosely similar to Laevigatosporites ova/us
WILSON & WEBSTER (1946, p. 273, fig. 5)
from the Paleocene Fort Union Formation of Montana and Laevigatosporites
major (COOKSON) KRUTZSCH (al. Monolites major COOKSON, p. 135, pl. 15, fig.
56) from the Tertiary lignites andcarbonaceous sandstone in Kerguelen

Kiyoshi TAKAHASHI

78

Island, but differ from the ovatus formin having a thin wall and from the major
form in having a small size and thin
wall.
Botanical affinity: Polypodiaceae.
Laevigatosporites dehiscens
TAKAHASHI
PI. 10, gg. 11

1961. Laevigatosporites dehiscens TAKAHASHI,
Mem Pac. Sci., Kyushu Univ., Ser. D,
Geol., vol. 9, no. 3, p. 290, pI. 16, figs.
4-8.

Dimensions:
Grain size in lateralview 31 X 19 f.1., exine thin.
Occurrence:
Few; Concepci6n Formation (Eocene) in the Concepci6n area.
Remarks: This specimen is identified
with Laevigatosporites dehiscens T AKAHASHI from the Paleogene and Miocene
formations of Japan.
Botanical affinity: Polypodiaceae.

Anteturma Pollenites R. POTONIE 1931.
Turma Saccites ERDTMAN 1947.
Subturma Disaccites COOKSON 1947.
Genus Dacrydiumites COOKSON

1953 ex HARRIS 1965.
Type species: Dacrydiumites jiorinii
COOKSON & PIKE 1953.
Dacrydiumites d. jiorinii
COOKSON & PIKE
PI. 10, figs. 18-20

1953. Dacrydiumites florinii COOKSON & PIKE,
Aust. Jour. Bot., vol. 1, no. 3, p. 479,
pl. 3, figs. 20-35.

Dimensions:

Total length of the grain

35.6-43 f.1., total height of the grain 30.737.4 f.1., width of the air sacs 24.2-26.3 f.1.,
height of the air sacs 14.5-23.3 f.1..
Occurrence:
Rare; Concepci6n Formation (Eocene) in the Concepci6n area.
Remarks: The present specimens arepoor in preservation, but they are barelyreferable to Dacrydiumites jiorinii COOKSON & PIKE, ranging from Paleocene to
Pliocene in Australia.
Botanical affinity: Dacrydium.
Turma Aletes IBRAHIM 1933.
Subturma Azonaletes LUBER 1935
emend. POTONIE & KREMP 1954.
Infraturma Psilonapiti ERDTMAN 1947.
Genus Inaperturopollenites PFLUG &THOMSON 1953 emend. R.
POTONIE 1958.
Type species:
Inaperturopollenites
dubius (POTONIE & VENITZ 1934) THOMSON & PFLUG 1953.
Inaperturopollenites pseudodubius
TAKAHASHI
1957. Inaperturopollenites pseudodubius TAKAI-IASHI, Mem. Pac. Sci., Kyushu Univ.,
Ser. D, Geol., vol. 5, no. 4, p. 216, pI.
38, figs. 11-17; pI. 39, figs. 13-14.

Occurrence:
Few; Concepci6n Formation (Eocene) in the Concepci6n area.
Remarks: This species appears in
Paleogene and Miocene of Japan. Thisis similar to Inaperturopollenites dubius(POTONIE & VENITZ) THOMSON & PFLUG,
but differs from the latter in having avery thin wall.
Botanical affinity: Taxodiaceae.
Inaperturopollenites laevigatus
TAKAHASHI

676.

Palynology of the Concepcion Formation, Chile

PI. 10, figs. 15-17

1957. Inaperturopollenites laevigatus TAKAHASHI, Mem. Fac. Sci., Kyushu Univ.,
Ser. D, GeoI., vol. 5, no. 4, p. 216217, pI. 38, fig. 18; pl. 39, fig. 16.

Dimensions:21-36.7 fl in diameter,
exine thin, laevigate.
Occurrence: Few; Concepci6n Formation (Eocene) in the Concepci6n area.
Remarks: The present pollen grains
fold very often. They are referable toInaperturopollenites laevigatusT AKAHASHI
from the Paleogene strata of westernJapan.
Botanical affinity: Taxodiaceae.

Illfraturma Subpilonapiti ERDTMAN
1947 emend. VIMAL 1952.
Genus Smilacipites WODEHOUSE 1933
emend. R. POTONIE 1960.
Type species: Smilacipites echinatus
WODEHOUSE 1933.

Similacipites setarius (POTONIE)

Botanical affinity:

79? Smilax.

Turma Plicates NAUMOVA 1939
emend. POTONIE 1960.
Subturma Polyplicates ERDTMAN 1952.
Genus Ephedripites BOLCHOVITINA 1953.
Type species:
Ephedripites mediolobatus BOLCHOVITINA 1953.

Ephedripites sp.
PI. 10, fig. 14

Description: Pollen grain ellipsoidal,
without a furrow, 24 fl long and 15.8 flbroad. Exine firm, smooth with about
15 longitudinal ridges. Width of ridge
1.1 fl.
Occurrence: Very rare; Concepci6n
Formation (Eocene) in the Concepci6n
area.
Remarks: Only one specimen was
found. This pollen grain belongs to theform-genus Ephedripites.
Botanical affinity: ? Ephedraceae.

POTONIE
Subturma Monocolpates IVERSEN &PI. 12, fig. 27

1934. Pollenites setarius POTONIE, Arb. Inst.
Palaevbot. Petrogr. Brennst., vol. 4, p.
93, tab. 5, fig. 24, 28.
1960. Smilacipites setarius (POTONIE), Po TONIE, Beih. Ceol. lb., no. 39, p. 86-87,
pI. 5, fig. 88.

TROELS-SMITH. 1950.
Genus Monocolpopollenites PFLUG &THOMSON 1953.
Type species: lvIonocolpopollenites tranquil/us (R. POTONIE 1934) THOMSON &PFLUG 1953.

Dimensions: Grain size 31.5 fl; lengthof spine 1.8-2.4 fl.
Occurrence: Very rare; Concepci6n
Formation (Eocene) in the Concepci6n
area.
Remarks: Only one specimen was
found. This specimen is identified with
Smilacipites setarius (POTONIE) POTONIE
from the Eocene lignite of Geiseltal.

lvIonocolpopollenites d. kyushuensis
TAKAHASHI
PI. 10, figs. 12-13

1961. Monocolpopollenites kyushuensis T AKAHASHI, Mem. Fac. Sci., Kyushu Univ.,
Ser. D, Geol., vol. ·11, no. 3, p. 292, pI.
16, figs. 17-23.

Kiyoshi TAKAHASHI

80

Dimensions: Pollen grain 32-33.5 X
17.7-22.5 fl.; exine less than 1 fl., chagrenate.
Occurrence: Rare; Concepcion Formation (Eocene) in the Concepcion area.
Remarks:
The present specimens
resemble Monocolpopollenites kyushuensis
TAKAHASHI from the Upper Cretaceousand Tertiary strata of Japan.
Botanical affinity: Palmae.

Genus Liliacidites COUPER 1953.
Type species: Liliacidites lwitangataensis COUPER 1953.

PI. 12, fig. 26

Description: Pollen grain dicolpate;outline in polar view circular. Colpus
not reaching to the pole. Exine thin,smooth. Grain size 42 fl..
Occurrence: Very rare; Concepcion
Formation (Eocene) in the Concepcion
area.
Remarks: Only one specimen was
found. This specimen belongs to theform-genus Dicolpopollis established by
G. PFLANZL (1956).
Botanical affinity : Unknown.

Liliacidites variegatus COUPER

Subturma Ptychotriporines
NAUMOVA 1939.

PI. 12, fig. 28

Infraturma Prolati ERDTMAN 1943.

1953. Liliacidites variegatus COUPER, New
Zealand Ceol. Surv., Paleont. Bull., vol.
22, p. 56, pI. 7, figs. 98-99.

Genus Rhoipites WODEHOUSE 1933.

Dimensions: Length of the grain 31.5
fl., breadth of the grain 18.4 fl.; exine
reticulate, muri baculate, 0.6 fl. high,lumen of reticulum 1 fl.±in diameter.
Occurrence: Very rare; Concepcion
Formation (Eocene) in the Concepcion
area.
Remarks: The present specimen isreferable to Liliacidites variegatus COUPER
from the Oligocene (Landonian) strata,
Mataura Valley, Southland, New Zealand.
Botanical affinity: Liliaceae.
Subturma Dicolpates ERDTMAN 1947.
Genus Dicolpopollis PFLANZL 1956
ex R. POTONIE 1966.
Type species:
PFLANZL 1956.

Dicolpopollis kockeli

Type species:
WODEHOUSE 1933.

Rhoipites

bmdleyiRhoipites bmdleyi WODEHOUSE
PI. 12, figs. 30-31, 33a-b

1933. Rhoipites bradleyi WODEHOUSE, Bull.
Torr. Bot. Club, vol. 60, p. 513, fig. 45.

Dimensions: Length of the grains 2025.8 fl., breadth of the grains 28.8-32 fl.;exine finely reticulate.
Occurrence: Few; Concepcion Formation (Eocene) in the Concepcion area.
Remarks: The present specimens are
identifiable with Rhoipites bradleyi WODEHOUSE from the Eocene Green River
Formation, U. S. A.
Botanical affinity: Unknown.
Rhoipites sp.
PI. 12, fig. 29

Dicolpopollis sp.
Description: Pollen grain tricolporate;676. Palynology of the Concepcion Formation, Chile
outline in lateral view elliptical. Colpi
narrow, with large ora, almost reaching
to the pole. Exine very finely reticulate.
Muri finely baculate. Grain size 15x25.6 p..
Occurrence: Very rare; Concepcion
Formation (Eocene) in the Concepcion
area.
Remarks: Only one specimen was
found. This specimen is similar to
Rhoipites bradleyi WODEHOUSE.
Botanical affinity: Unknown.

Genus Foveotricolporites PIERCE 1961.
Type species:
Foveotricolporites
rhombohedralis PIERCE 1961.
Foveotricolporites foveolatus n. sp.

81

Type species: Triatriopollenites rurensis
THOMSON & PFLUG 1953.
Triatriopollenites sp.
PI. 11, figs. 10a-b

Description: Triporate pollen. Equatorial contour triangular-convex. Pores
small, equatorial, sometimes one or two
pores subequatorial. Exine thin, 0.7 p.
thick, chagrenate, without annulus andtumenscens, but with distinctly developed
atrium in the pore areas. Grain size
30 p. in diameter.
Occurrence: Rare; Concepcion Formation (Eocene) in the Concepcion area.
Remarks: The present speCimen with
developed atrium is identified with theform-genus Triatriopllenites.
Botanical affinity: Myricaceae.

PI. 12, figs. 32a-b

Description: Pollen grain tricolporate,
subprolate. Col pus with rounded pore
relatively narrow. Exine thin, foveolate;lumina less than 1 p. in diameter. Grainsize 30 X 35 p..
Holotype: PI. 12, figs. 32a-b; grain
size 30x35 p.; slide GN 2527.
Occurrence: Rare; Concepcion Formation (Eocene) in the Concepcion area.
Remarks: The present specimen issimilar to Foveotricolporites voluminosus
GUZMAN from the Lower and Middle
Eocene of the Tibu area, Colombia, butdiffers from the latter in having thinwall and smaller lumina.
Botanical affinity: Unknown.

Turma Poroses NAUMOVA 1937
emend. R. POTONIE 1960
Subturma Triporines NAUMOVA 1939
emend. R. POTONIE 1960.
Genus Triatriopollenites PFLUG 1953.

Genus Triporopollenites PFLUG &THOMSON 1953 emend.
R. POTONIE 1960.
Type species: Triporopollenites coryloides PFLUG 1953.
Triporopollenites festatus TAKAHASHI
PI. 11, figs. 1-8
1961. Triporopollenites festatus TAKAHASHI,
Mem. Pac. Sci., Kyushu Univ., Ser. D,
Geol., vol. 11, no. 3, p. 301, pI. 19,
figs. 29-37.
1968. Trioritesfestatus (TAKAHASHI) MULLER,
Micropaleontology, vol. 14, no. 1, p. 15,
pI. 3, fig. 10.

Dimensions: Grain size 26-32.8 p. inequatorial diameter; exine 0.6-1.4 p. thick,forming annulus in the pore areas.
Occurrence: Common; Concepcion Formation (Eocene) in the Concepcion area.
Remarks: The present specimens areKiyoshi TAKAHASHI

82

identified with Triporopollenites festatus
TAKAHASHI from the Paleogene andUpper Cretaceous formations of Japan.
Botanical affinity: Betulaceae.
Genus NIomipiles WODEHOUSE 1933.
Type species:

Momipites coryloides

Myrtaceidites parvus COOKSON & PIKE
forma anesus COOKSON & PIKEPI.

12, figs. 7-11

1954. Myrtaceidites parvus COOKSON & PIKE
forma anesus COOKSON & PIKE, Austra·lian Jour. Bot., vol. 2, llO. 2, p. 206,
pI. 1, figs. 27-28.

WODEHOUSE 1933.

Momipites sp.
PI.

12, figs. 5-6

Description: Triporate pollen grains.
Equatorial contour triangular-convex.
Pore small, equatorial. Exine without
atrium, annulus and labrum in the poreareas, thin, 1 p. thick, chagrenate. Grainsize 16-19.5 p. in diameter.
Occurrence: Rare; Concepcion Formation (Eocene) in the Concepcion area.
Remarlls: Only two specimens were
found.
These specimens belong undoubtedly to the form-genus Momipites.
Botanical affinity: Betulaceae.
Genus lvIyrtaceidites COOKSON & PIKE

Dimensions: Grain size 12-13.6 p. III
equatorial diameter; exine smooth orchagrenate; polar islands absent.
Occurrence: Common; Concepcion Formation (Eocene) in the Concepcion area.
Remarks: The present specimens are
identical with the species Myrtaceidites
parvus COOKSON & PIKE forma anesus
COOKSON & PIKE described by 1. C.
COOKSON and K. M. PIKE (1954) from the
Eocene to Pliocene sediments in Australia.
Botanical affinity: Unknown.
Known range in Australia: Eocene to
Pliocene.
Myrtaceidites parVlls COOKSON & PIKE
forma nesus COOKSON & PIKE

1954 ex R. POTONIE 1960.

Type species: Myrtaceidites mesonesus
COOKSON & PIKE 1954.

PI.

12 figs. 12-24

Explanation of Plate 9(All figures x 1000)
Figs. 1-7. Stereispo1'ites concepcionensis ll. sp.
Figs. 1, 2: slide GN 2531; fig. 3: slide GN 2533; fig. 4: slide GN 2534; fig. 5: holotype,slide GN 2536; fig. 6: slide GN 2541; fig. 7: slide GN 2548.
Figs. 8-15. Gleicheniidites speciosus ll. sp.
Fig. 8: holotype, slide GN 2535; figs. 9, 10: slide GN 2532; fig. 11: slide GN 2540; fig.
12: slide GN 2548; fig. 13: slide GN 2533; fig. 14: slide GN 2508; fig. 15: slide GN 2536.
Figs. 16-18. Gleicheniidites circinidites (COOKSON) n. comb.
Fg. 16: slide GN 2507; fig. 17: slide GN 2508; fig. 18: slide GN 2537.
Eigs. 19-21. Leiotriletes minus ll. sp.
Fig. 19: slide GN 2528; fig. 20: holotype; figs. 20, 21: slide GN 2G27.
Fig. 22. Concavisporites sp.
Slide GN 2535.

TAKAHASHI:

Palynology of Concepcion Formation

Plate 922

676.

Palynology of the Concepcion Formation, Chile

195-1. Myrtaceidites parvus COOKSON & PJI<E
forma nesus COOKSON & PIKE, Austra·lian Jour. Bot., vol. 2, no. 2, p. 206,
pI. 1, figs. 29-31.

Dimensions: Grain size 10.7-12.5 fl inequatorial diameter; exine smooth or
faintly patterned; polar islands distinct.
Occurrence:
Abundant; Concepcion
Formation (Eocene) in the Concepcion
area.
Remarks: The specimens are referable
to lvlyrtaceidites paruus COOKSON & PIKE
forma nesus COOKSON & PIKE describedby 1. C. COOKSON K. M. PIKE (1954) fromthe Eocene to Pliocene formations inAustralia.
Botanical affinity: Unknown.
Known range in Australia: Eocene to
Pliocene.
Myrtaceidites sp.
PI. 12, fig. 25

Description: Grain size 17.5 fl in equatorial diameter. Amb with straight orslightly convex sides. Arci prominent,
polar islands absent. Exine thin, chagrenate or faintly pUnctate.
Occurrence: Very rare; Concepcion
Formation (Eocene) in the Concepcion
area.
Remark s: Only one specimen was
found. This specimen coincides with thecharacteristics of the form-genus Myrtaceidites.
Botanical affinity:

Unknown.

Genus Triorites ERDTMAN 1947
ex COUPER 1953 emend.
R. POTONIE 1960.
Type species:
COOKSON 1950.

Triorites magnificlls

83

Triorites minor COUPER
PI. 11, fig. 11

1953. Triorites minor COUPER, N. Z. Ceol.
Surv., Paleont. Bull., vo\. 22, p. 61, p\.
7, figs. 112-113.

Dimensions:
Grain size 19.7 fl inequatorial diameter. Exine thin, punctate or chagrenate.
Occurrence: Very rare; Concepcion
Formation (Eocene) in the Concepcion
area.
Remarks: Only one specimen was
found. This specimen coincides withthe characteristics of Triorites minor
COUPER (1953) from the Upper Cretaceous (Sub-Wangaloan) of the Kaitangata
coalfield (New Zealand).
Botanical affinity: Unknown.
Triorites ct. hG1Tisii COOPER
P\. 11, figs. 21a-b

1953. Triorites harrisii COUPER, N. Z. Ceol.
Surv., Paleont. Bull., vo\. 22, p. 61, p\.
7, fig. 111.

Dimensions:
Grain size 20.8 fl inequatorial diameter. Ora 3.2-4.8 fl indiameter.
Exine thin, annulus andlabrum around ora, chagrenate.
Occurrence: Very rare; Concepcion
Formation (Eocene) in the Concepcion
area.
Remark s: Only one specimen was
found. This specimen is closely similar
to Triorites harrisii COUPER describedby R. A. COUPER (1953) from the Oligocene sediments in the Ford's Old Lignite
Mine, Southland (New Zealand).
Botanical affinity: Unknown.
Genus Subtriporopollenites PFLUG &THOMSON 1933.

Kiyoshi TAKAHASHI

84
Type species:

plex (R.
PFLUG

Sub triporopollenites sim-

POTONIE

1931)

THOMSON

&1953.

subtriporopollenites rotundulus n. sp.

(1961, p. 305-306, pI. 20, figs. 35-37; pI.
21, figs. 1-10), but the former differsfrom the latter in structure of exine in
the pore areas (annulus).
Botanical affinity:
Juglandaceae-?

Carya.
PI. 11, figs. 9, 12-13; pI. 12, fig. 4

Description:

Pollen grain trip orate.
Grain circular to sub triangular in polar
view. Pores circular, 2.4 f1 in diameter;
one or two pores subequatorial. Exine
0.8-1.5 f1 thick, chagrenate, annulus III
the areas. Grain size 30.6-36.6 f1 III
equatorial diameter.
Holotype: PI. 11, fig. 12; grain size 32
fl in equatorial diameter; exine 1 f1
thick, chagrenate; slide GN 2530.
Occurrence: Few ; Concepcion Formation (Eocene) in the Concepcion area.
Remarks: The present specimens are
similar to the Japanese species subtri-

poropollenites

kyushuensis

TAKAHASHI

sllbtriporopollenites falslls n. sp.
PI. 11, figs. lLl-20; pI. 12, figs. 2-3

Description: Pollen grain triporate.
Grain circular to subtriangular withrounded sides in polar view. Pores
small, circular to elliptical; all pores
subequatorial, sometimes one pore equatorial. Exine sometimes with weakannulus and labrum, less than 1.5 f1
thick, chagrenate or faintly pUnctate.
Grain size 21.5-29 f1 in equatorial diameter.
Ho lo type : PI. 11, fig. 19; grain size
26.5 f1 in equatorial diameter; pore 1.7 f1

Explanation of Plate 10(All figures x 1000)
Fig. 1. Leiotriletes microadriennis KRUTZSCIISlide GN 2530.
Figs. 2-3. Triplanosporites minor n. sp.
Fig. 2: slide GN 2533; fig. 3: 'holotype, slide GN 2532.
Fig. 4. Triplanosporites sp.
Slide GN 2532.
Eig. 5. ? Punctatisporites sp.
Slide GN 2526.
Figs. 6-10. Laevigatosporites ovulatus n. sp.
Figs. 6, 7: slide GN 2536; fig. 7: holotype; fig. 8: slide GN 2534; fig. 9: slide GN 2537;
fig. 10: slide GN 2535.
Fig. 11. Laevigatosporites dehiscens TAKAHASHI
Slide GN 2507.
Figs. 12-13. Monocolpopollenites d. kyushuensis TAKAHASHI
Fig. 12: slide GN 2533; fig. 13: slide GN 2540.
Fig. 14. Ephedripites sp.
Slide GN 2508.
Figs. 15-17. Inaperturopollenites laevigatus TAKAHASHI
Figs. 15, 16: slide GN 2532; fig. 17: slide GN 2533.
Figs. 18-20. Dacrydiumites d. florinii COOKSON & PIKE
Figs. 18, 19: slide GN 2530; fig. 20: slide GN 2539.

TAKAHASHI:

Palynology of Concepcion Formation

Plate 10

676.

Palynology of the Concepcion Formation, Chile

diameter; exine thin, chagrenate;slide GN 2536.
Occurrence:
Abundant; Concepcion
Formation (Eocene) in the Concepcion
area.
Remarks: The Japanese species Subtriporopollenites kyushuensis TAKAHASHI(1961, p. 305-306, pI. 20, figs. 35-37; pI.
21, figs. 1-10) is compared with thepresent specimens.
Botanical affinity:
J uglandaceae-?
III

Carya.
Sllbtriporopollenites levius TAKAHASHI
PI. 12, fig. 1

1961. Subtriporopollenites levi us TAKAIIASHI
Mem. Fac. Sci., Kyushu Univ., Ser. D,
Geol., vol. 11, no. 3, p. 306, pI. 21, fig.
12.

Dimensions: Grain size 20 f.1 in eq uatroial diameter; exine thin, roughly
rugulate.
Occurrence: Very rare; Concepcion
Formation (Eocene) in the Concepcion
area.
Remarks: Only one specimen was
found. The present specimen belongs to
the species Subtriporopollenites levius
TAKAHASHI (1961) from the Lower
Oligocene formations of the Kasuya
and Karatsu coalfields in north Kyushu,
Japan. The former is smaller in size
than the latter.
Botanical affinity: ? Juglandaceae.
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spores and pollen grains that extend thegeological and geographical distributionof living genera. Proc. Roy. Soc. Victoria, vol. 69, p. 41-53, pIs. 8-10.
- - and PIKE, K. M. (1954): Some dicotyledonous pollen type from Cainozoic deposits in the Australian region. Aust. J.
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COUPER, R. A. (1953): Upper Mesozoic andCainozoic spores and pollen grains fromNew Zealand. N. Z.,Ceol. Surv., Paleont.

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Kiyoshi TAKAHASHI

Bull., vol. 22, p. 1-77.
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New Zealand Mesozoic andCainozoic plant microfossils. N. Z. Geo!.
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Explanation of Plate 11 .
(All figures x 1000)
Figs. 1-8. Triporopollenites festatus TAKAHASHI
Fig. 1 : slide GN 2532; fig. 2: slide GN 2508; figs. 3, 4: slide GN 2507; fig. 5: slide GN
2528; fig. 6: slide GN 2538; fig. 7: slide GN 2530; fig. 8: slide GN 2536.
Figs. 9, 12, 13. Subtriporopollenites rotundulus n. sp.
Fig. 9: slide GN 2528; fig. 12: holotype, slide GN 2530; fig. 13: slide GN 2508.
Figs. lOa-b. Triatriopollellites sp.
Slide GN 2529.
Fig. 11. Triorites minor COCPER
Slide GN 2536.
Figs. \.!-20. Subtriporopollenites falsus n. sp.
Fig. 14: slide GN 2535; fig. 15: slide GN 2532; fig. 16: slide GN 2538; fig. 17: slide GN
2534; fig. 18: slide GN 2537; fig. 19: holotype, slide GN 2536; fig. 20: slide GN 2527.
Figs. 21a-b. Triorites d. harrisii COUPER
Slide GJ-.~ 2531':

TAKAHASHI:

Palynology of Concepcion Formation

Plate 11

9

11

21a

676.

Palynology of the Concepcion Formation, Chile

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tigraphische Untersuchung der tertiaren

87

Schichten im Kasuya and Fukuoka
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- - (1970): Distribution and change ofUpper Cretaceous and Lower Paleogene
microfloras in circum·Pacific regions andSiberia.
Fossils, nos. 19-20, p. 31-39,
tabs. 1-3.
- - (1971): Stratigraphic and geographic
distribution of the Cretaceous pollenspore assemblage. Prof. H. MatsushitaMem. Vol., p. 31-48.
- - (1973): Distribution and change of theUpper Cretaceous and Paleogene palynofloras and their problem. Fossiis, nos.
25-26, p. 65-73.
- - (1977): Upper Cretaceous palynoflora
from Quiriquina Island, Chile. BUll.

Fac. Liberai Arts, Nagasaki Univ., Nat.
Sci., vol. 17, p. 29-53, pis. 1-4.
THOMSON, P. W. und PFLUG, H. D. (1953):
Pollen und Sporen des mitteleuropaischen
Tertiars. Palaeontographica, Abt. B, Bd.
94, p. 1-138, pis. 1-15.
WODEHOUSE, R. P. (1933): Tertiary pollen-II. The oil shales of the Eocene Green
River Formation. Bull. Torr. Bot. Club,
vol. 60, p. 479-524, text-figs. 1-56.

88

Kiyoshi TAKAHASHI

Explanation of Plate 12(All figures x 1000)
Fig. 1. Subtriporopollenites levius TAKAHASHI
Slid!:! GN 2536.
Figs. 2-3. Subtriporopollenites falsusn. sp.
Fig. 2: slide GN 2539; fig. 3: slide GN 2532.
Fig. 4. Subtriporopollenites rotundulus n. sp.
SlideGN 2528.
Figs. 5-6. Momipites sp.
Fig. 5: slide GN 2533; fig. 6: slide GN 2536.
Figs. 7-11. Myrtaceidites parvus COOKSON & PIKE forma aneslls. COOKSON & PIKE
Fig. 7: slide GN 2538; figs. 8, 11: slide GN 2535; fig. 9: slide GN 2532; fig. 10: slide
GN 2533.
Fgs. 12-24. Myrtaceidites parvus COOKSON & PIKE forma neSllS COOKSON & PIKE
Fig. 12: slide GN 2534; figs. 13-17, 21: slide GN 2535; figs. 18, 24: slide GN 2539; figs.
·19, 20;· 23 : slide GN 2536; fig. 22: slide GN 2508.
Fig. 25. Myrtaceidites sp.
Slide GN 2534.
Fig. 26. Dicolpopollis sp.
Slide GN 2536.
Fig. 27. Smilacipites setarius (POTONIE) POTONIE
Slide GN 2530.
Fig. 28. Liliacidites variegatus COUPER
Slide GN 2532.
Fig. 29. Rhoipites sp.
Slide GN 2525.
Figs. 30-31, 33a-b. Rhoipites bradleyi WODEHOUSE
Fig. 30: slide GN 2530: fig. 31: slide GN 2529; fig. 33: slide GN 2532.
Figs. 32a-b. Foveotricolporites foveolatlls n. sp.
Holotype, slide GN 2527.

TAKAHASHI:

Palynology of Concepcion Formation

6

5

1

11

Plate 12

12

3

14

8

9

15

16

18

10

21

25

24

29

23

22

Trans. Proc. Palaeont. Soc. Japan, N. S., No. 106, pp. 89-99, pI. 13, 14, June 30, 1977

677.

UPPER PERMIAN FUSULINACEANS CONTAINED IN THE
PEBBLES OF THE BASAL CONGLOMERATE OF THE
ADOY AMA FORMATION, KUZU, TOCHIGI
PREFECTURE, JAPANHISA YOSHI IGO
Institute of Geoscience, The University of Tsukuba, Ibaraki 300-31

and
HISAHARU IGO
Department of Astronomy and Earth Sciences, Tokyo Gakugei University, Tokyo 184

W*!JiU~1=.f.fjIi0)7 nlJ~£I1t.~;J50)~tc~£.nQl:mC~*0)7;(!! TtC'?\"L: 7 r
Jl.I~li=~*"'C, £11t.$tC1:lJ.jl(;J5~;J5;O;ge:8'! L q:r$=~*O)~Jl.I~~""~{'JIC:to:to? 0 ~ 0)~;J50)~Kl:$=~*~m~~Q7;(UT~~£.n, ~Jl.I~~*~<m~~.nk~~~~~~.nG7;(!!T~&~~Q~~K, ",,~{'JO).~~.C~• • ~~· • • ~M

which overlies unconformably the Nabeyama Formation. Thus the stratigraphy
and geochronology of the Aso and Tochigi
Groups in this district were considerably
revised by KOIKE, IGO, IGO and KINOSHITA(1974). The purpose of this paper is to
discuss the geological significance of theunconformity between the Permian Nabe . .
yama and Triassic Adoyama Formations
and to describe some Upper Permian
fusulinaceans contained. in the pebbles
of basal conglomerate of the Adoyama
Formation. To date, this fusulinacean
faunule rarely occurs in Japan. Fusu. .
linaceans treated herein are Codonofusiellasp., Paradoxiella sp., Dunbarula suzukii
IGO and IGo, n. sp., Reichelina changhsing. .
ensis SHENG and CHANG, Nankinella
kuzuensis IGO and IGO, n. sp., Yabeina
globosa (Y ABE) and Yabeina kanmerae
IGo.

Introduction
Upper Paleozoic and Lower Mesozoic
rocks are widely distributed in the Kuzu
district, Tochigi Prefecture, about 80 km
north of Tokyo. YOSHIDA (1956, 1957),
FUJIMOTO (1961), WATANABE et al. (1957),
HATORI (1965), SHOJI (1967), YANAGIMOTO (1973) and others have contributed
to geology and sedimentology of this
district. Although no comprehensive
paleontological works have been published, MORIKAWA and HORIGUCHI (1956),
MORIKAWA and T AKAOKA (1961), IGO(1964a) and several others describedsome Middle Permian fusulinaceans fromthe Nabeyama Formation.
Recently, Triassic conodonts wererecovered from the Adoyama Formation* Received Feb. 22, 1977; read Jan. 16, 1973
at Sendai.

89

Hisayoshi IGO and Hisaharu IGO

90

Geologic Setting
We revised the stratigraphy of thePermian and Triassic rocks in this
district as shown in Fig. 1. The Aso
Group of our definition is subdivided
into two formations, namely, the Izuru
and Nabeyama Formations in ascendingorder.
The Izuru Formation consists mainlyof dark green, dark gray and partly
variegated basic tuff, agglomerate andlava. These volcanoclastic and volcanic
series are 500 m in maximum thickness,but vary their thickness by the thrustfault. The Nabeyama Formation overlies conformably the Izuru and consists
mainly of limestone and dolostone. This
formation is subdivided into the lower
Yamasuge Limestone, middle Hanezuru
Dolostone and upper Karasawa Limestone
Members. This calcareous facies attains
about 300 m in maximum thickness.
Parafusulina and other Middle Permian

.~
".
u

Mak! Formation

~

~~

00

c.z

f--

~

go
B

r-- "
0

z

~

~

Adoyama Formation(= ~ika9ura~Aisawa. Formation

Formation)

~
~
~

.g

(=

.
H1roto Formatl.on )Ohi(!Y:=a~~rmation
I1\~~aFormation)

r-".
,S;
I,'t!
....
il

I--

....

~

" ..
Ii

~

go

f

~

:S
"

:

Nabeyama Formation

0

Izuru Formation

Fig. 1. Stratigraphy and Geochronologyof the Aso and Tochigi Groups.

fusulinaceans are very abundant at
various levels and localities. They represent almost entire part of the Zoneof Parafusulina.
The Tochigi Group of our sense canbe subdivided into the following four
lithologic units, such as, Adoyama,
Aisawa, Ohirayama and Maki Formations
and these lithologic units are mostly
Triassic in age. The Hiroto, Mikagura
and Nakazuma Formations proposed by
the previous authors are contemporaneous with the Aisawa, Adoyama andOhirayama Formations, respectively.
The Adoyama Formation consists mainlyof chert and shale and about 80 to 450.
m in thickness. The basal part of thisformation is locally limestone conglomerate and unconformably overlies the
Nabeyama Formation. There can beobserved very interesting features ofthe buried karst topography, crevices,
shafts or wells sinkhole and caves atthe base of the Adoyama. The basal
part of the Adoyama is typically exposed at the northern part of thequarry of Miyata Lime Industry Co. Ltd
at Semba, north of Kuzu Town.
The following succession is exposed at
this quarry in descending order.
Chert; red to green, thin-bedded, iIitercalating thin layers of siliceous shale,radiolarian remains, conodonts, sponge
spicules, arenaceous foraminifers andmany other microfossils ............... .
· ................. more than 50 m thick;
Shale; dark gray, occasionally red andgreen, intercalating bedded chert, radiolarian remains and conodonts ......... .
· ....................... about 6 m thick .
Limestone conglomerate; consisting ofvarious shaped and sized pebbles oflimestone, dolostone and chert cemented
by calcarenite and calcilutite ......... .
· . variable in thickness, 0 to 10 m thick.
---unconformity·---677.

Upper Permian Fusulinacea

Limestone; massive, pale gray towhite, partly silicified and dolomitized ..
· . . . . . . . . . . . . . . . . . . . . . .. 0 to 4 m thick.
Limestone; coquinoidal, composed ofsilicified shells of Parafusulina and otherfragments of invertebrate fossils ..... .
· ....................... about 9 m thick.
Limestone; gray, massive or thickly
bedded, highly fossiliferous and containing black chert concretions ........... .
· ................. more than 80 m thick.
Upper Permian fusulinaceans describedherein were collected from the boulderof the basal conglomerate of the Adoyama Formation.
The Aisa wa Formation was once considered as Permian, but it yields Triassic
conodonts, such as Epigondolella abneptis,
E. postera and others. It consists mainlyof shale and sandstone and intercalating
thin layers of chert and chert breccia.
Thickness of this formation was estimated as 1500 m by FUJIMOTO (1961).
According to our recent observation,
however, this formation is repeated byfolding and the true thickness is thinnerthan 500 m.
The Ohirayama and Nakazuma Formations are also composed of chert.
The former unit attains approximately
800 m and the latter is about 700 m in
They yield Epigondolella
thickness.
nodosa, Gladigondolella tethydis, Neogondolella polygnathiformis, Neospathodus
sp. and are considered to be Carnian.
From the above mentioned revised
stratigraphy, the geologic history in this
district during the Permian and Triassic
is summarized as follow. The Nabeyama
Formation started its calcareous deposition on the elevated submarine volcanic
rise consisting of the Izuru Formationin Middle Permian and continued up to
the end of Permian. The upper part ofthese carbonate deposits apparently

91

comprises the Neoschwagerina, Yabeina,
Codonofusiella-Reichelina and Palaeofusulina-Reichelina Zones. However, theNabeyama Formation was deeply denuded
and more than two-thirds of this formation was eroded away. The Upper
Triassic Adoyama overlies unconformably this etched surface of carbonate
rocks.
The lime-sand and lime-silt
consisting of the matrix of the basal
conglomerate of. the Adoyama yield
Upper Scythian species of conodontsintermingled with Middle to Upper
Triassic conodonts.
Therefore, thedenudation before the deposition of the
Adoyama was first started in Early
Scythian and repeated calcareous condensed deposition and subsequent denudation until late Carnian or Norian.
The mixed reworked conodonts ranging
from the Upper Scythian to Norianshow the mentioned sedimentation anderosion. Chert-rich facies of the Norian
Adoyama Formation laterally changed
into shale and sandstone facies of the
Aisawa and Hiroto Formations. The
Ohirayama and Nakazuma Formations
consisting mainly of chert represent theCarnian off-shore sediments and areoverlain by the Aisawa and Hiroto
Formations.
The Maki Formation consisting mainlyof sandstone is probably Jurassic in age
and overlies Triassic formations. However, the stratigraphic relationship between the Upper Triassic formations andthe Maki Formation stilI remains unknown.
Fusulinacean faunule contained in thepebbles of the Aisawa Formation andits geological significance

FUJIMOTO (1961) reported the occurrence of Yabeina columbiana (DAWSON)
and Neoschwagerina spp. from the92

Hisayoshi Jeo and Hisaharu Jeo

Karasawa Limestone Member. Therefore, the upper part of the Karasawa
Limestone Member was correlated with
the Upper Permian by several subsequentauthors. However, it is evident thatthese Upper Permian fusulinaceans areapparently derived fossils by the remarkable denudation before the deposition of the Adoyama Formation.
Upper Permian fusulinacean-bearing
limestone boulders in the basal conglomerate of the Adoyama show two typesof lithic character. One is algal-biosparitic gray limestone and more than
2 m in diameter. The other is microcrystalline black limestone and morethan 1 m in diameter. The former isnumbered 4052A and the latter is 4052B.
Fusulinacean faunule contained in 4052A
is as follows; namely:Dunbarula suzukii IGO and IGo, n. sp. . ..
................................ common
Reichelina changhsingensis SHENG and
CHA:-;G ..•••.......••.•••.• ; •.... common
Nankinella Il1lzuensis IGO and IGO .... rare

The following species are yielded from
4052B, such as:
Yabeina kanmerae IGo ............ abundantYabeina globosa (Y ABE) . . . . . . . . . . . . . . rare
Codonofusiella sp. . ................... rare
Paradoxiella sp. . ..................... rare
Dunbarula sp. . ....................... rare

Dunbarula suzukii is similar to Dunbarula paleofusulinaefonnis SHENG described from the W uchiaping Limestone
in South China. Nanl,inella ',uzuensis issimilar to Nankinella quasihunanensis
SHENG and N. hunanensis (CHEN) described from the uppermost Permian ofSouth and Northwest China. Therefore,
the faunule contained in 4052A can becorrela~ed with the Upper Permian faunaof the Wuchiaping or Changhsing Limestone.
Fusulinacean faunule came from 4052A
is characterized by Yabeina lwnmerae

IGO which was originally described fromthe Kono Formation of the Nyukawa
Group in Hida Massif, Central Japan.
Although the occurrence is rare, theassociation of Paradoxiella sp., Codonofusiella sp. and Dunbarula sp. is also
worthy to note. This faunule can becorrelated with the upper part of theYabeina Zone in Japan and slightly older
than the faunule contained in 4052A.
To date, the uppermost Permian
Lopingian fusulinacean fauna is rather
poorly known in Japan. The Mitai
Formation in Miyazaki Prefecture andthe uppermost part of the Tsukumi
Limestone in Oita Prefecture, both inKyushu contain rather prolific Codonofusiella-Reichelina and PalaeofusulinaR eichelina faunas(KANMERA, in KANMERA
and NAKAZAWA, 1973). The upper partof the Maizuru Group distributed in the
Maizuru Belt also contains the Palaeofusulina fauna (NOGAMI, 1958). SAITO
and KA TO (1971) briefly reported theoccurrence of Reichelina and other upper
Permian foraminifers from Umeki,slightly north of the present area.
Recently, KOBA YASHI (1975) described
the Palaeofusulina-Reichelina fauna fromthe pebbles of the Triassic conglomerate
in the Itsukaichi district, west of Tokyo.
The present discovery of the R eichelinaDunbarula faunule from the Triassic
conglomerate and KOBA YASHI'S (1975)
observation show considerable denudation
took place in certain areas in Japanafter the end of Permian and before thedeposition of the Upper Scythian. There
are positive possibilities that the uppermost Permian fusulinacean fauna will befound from the Triassic pebbly facies invarious regions in Japan.
Description of Species

Genus Reichelina ERK, 1941

677.

Uppe1" Permian Fusulinacea

93

Occurrence :-Commonly yielded from
4052A, Semba, Kuzu Town, Aso County,
Tochigi Prefecture.
Reg. nos: 5000, 5001, 5002, 5003, 5004,
5005.

Reichelina changhsingensis
SHENG and CHANG
PI. 13, figs. 21-24
Reichelina changhsingensis SHENG and CHANG,
1958, p. 211, pI. 1, figs. 1-11 ; SHEKG 1963,
p. 150-151, pI. 1, figs. 23-29.

Genus Nankinella LEE, 1933
Nankinella kuzuensis IGO and IGo, n. sp.

Shell lenticular, minute, planispiral andinvolute with slightly convex polar
regions, short axis of coiling and uncoiled
last volution. Inner one or two volutions
with rounded periphery. Axial length
0.13 to 0.20 mm, median width 0.80 to
2.08 mm with uncoiled portion and form
ratio 1 : 0.03 to 1 : 0.25. Proloculus minute,spherical and about 25 to 45 fl in outside
diameter.
Spirotheca thin, composed of twolayers of thin tectum and diaphanotheca.
Septa also thin, almost plane and arcuate anteriorly in outer volutions.
Chomata low, extending to polar regions
and slightly asymmetrical. Tunnel low
and slit-like. Axial filling weak andrestricted to axial region.
Remarks:-The present material isvery similar to the Chinese specimens
described by SHENG and CHANG fromthe Changhsing and Wuchiaping Limestones. Reichelina matsushitai NOGAMI
is also allied species to 'our specimens,
but the former has rather thin uncoiled
part in the axial section.

PI. 13, figs. 1-6

Shell minute, thickly discoidal withnarrowly angular to bluntly pointed
periphery and convex polar regions.
The holotype specimen consists of 5 1/2
volutions and attains 0.83 mm in length,1.68 mm in median diameter, giving aform ratio 1: 0.5. Proloculus minute,spherical and about 45 fl in outside
diameter.
Spiro theca relatively thin and composed of tectum and lower less dense
layer, but secondary mineralization obliterates detailed structure of spirotheca.
Septa numerous, not fluted and plane.
Chomata low, asymmetrical and extending laterally to polar regions. Tunnel
narrow, low and having rather irregularpath.
Remarks:-This new species resembles
Nankinella quasihunanensis SHENG andNankinella hunanensis (CHEN) describedfrom the Wuchiaping Limestone andChinghsichung Limestone of South China,

Table 1. Measurements of Reichelina changhsingensis SHENG & CHANG (in mm.)Thickness of spiro theca

Height of volutions
Specimen

L.

10
12
13
15
16

0.13
0.20
0.18
0.20
0.13

W.

F.R.

2.08
0.80
0.50
1.13
0.75

0.06
0.25
0.35
0.18
0.17

D.P.
0.03
0.04
0.02
0.04
0.03

1

2

3

4

1

2

3

4

0.03
0.02
0.02
0.02
0.02

0.04
0.03
0.02
0.03
0.05

0.07
0.06
0.07
0.10
0.06

0.87
0.50
0.20
0.55
0.50

0.005
0.005
0.003
0.003

0.008
0.018
0.005
0.005
0.003

0.008
0.010
0.010
0.010
0.003

0.008
0.020
0.005
0.003
0.003

-

Hisayoshi IGO and Hisaharu IGO

94
Table 2.
Specimen

20
21
22
23
24

L.

w.

Measurements of Nankinella kuzuensis leo & lCD, n. sp. (in mm.)Thickness of spirotheca

Height of volutions

F.R. D.P.

- -- 0.83 1. 68 0.49 0.04
0.88 1. 30 0.67 0.03
1. 08 1. 75 0.61 0.07
0.50 1. 20 0.42 0.05
0.38 0.73 0.51 0.02

1

2

3

0.06
0.03
0.06
0.05
0.05

0.15
0.04
0.12
0.10
0.07

0.17
0.07
0.15
0.12
0.10

respectively. It can be easily distinguished from the latters by less numerous
and smaller shell at maturity.
Occurrence :-Rare in 4052A, Semba,
Kuzu Town, Aso County, Tochigi
Prefecture.
Reg. nos. 5006 (Holotype), 5007, 5008,
5009, 5010, 5011, 5012 (Paratypes)
Genus Dllnbarllla CIRY, 1948
Dllnbarula sllzukii IGO and IGo, n. sp.
PI. 13, figs. 7-20

Shell small, short fusiform with inflated
median part and bluntly pointed poles.
Mature shells having 5 to 51/2 volutions.
Axial length 1.60 to 2.00 mm, median
diameter 0.88 to 1.25 mm, and from ratio
1 : 1.7 to 1: 2.4 in well-oriented mature
specimens.
Inner two to three volutions discoidal
or lenticular and coiled almost rightangle to the later volutions. Spiro thecacomposed of thin tectum and underlying
thicker diaphanothecal layer. Spiro thecathin, 5 to 20 p in inner juvenile volutions.
Proloculus minute, spherical and its outside diameter 30 to 50 p.
Septa
numerous, more or less strongly andrather irregularly fluted throughout shell.
Chomata rather distinct in outer volutions
and asymmetrical.
Tunnel low andrather narrow and having irregular

4

5

6

0.20 0.18
0.10 0.17 0.22
0.17 0.27
0.25
0.12

1

2

3

4

5

0.02 0.02 0.03 0.03 0.03
0.02 0.02 0.03 0.05 0.03
0.02 0.02 0.02 0.02 0.02
0.02 0.02
0.01 0.02 0.02

path.
Remarks:-The present new species isvery similar to Dunbarula paleo/usulinae/ormis SHENG described from theWuchiaping Limestone, Kueichou, South
China in many respects.
However,Dunbarllla suzukii has weaker septal
fluting, smaller proloculus and more distinct chomata than the Chinese species.
Occurrence :-Common in 4052A, Semba,
Kuzu Town, Aso County, Tochigi Prefecture.
Reg. nos. 5013 (Holotype), 5014, 5015,
5016, 5017, 5018, 5019, 5020, 5021, 5022,
5023, 5024, 5025 (Paratypes)
Genus Paradoxiella SKINNER
and WILDE, 1955
Paradoxiella sp.
PI. 13, figs. 25, 26

Remarks :-Several incomplete specimens were obtained. Minute shell consists of 3 to 31/2 volutions and with
uncoiled disc-shaped flare. General biocharacters are identical with those of
Paradoxiella SKINNER and WILDE. However, we could not obtain any completehorizontal axial section and specific
ISHII andidentification is reserved.
TAKAHASHI (1960) described Paradoxiellajaponica from the Ogamata Formation
distributed in the Kanto Massif. The

677.

Upper Permian Fusulinacea

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LI>

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c:-.i ,....; ,....; ,....; ,....;

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Genus Yabeina DEPRAT, 1914
Yabeina kannzerae IGO
PI. 14, fig. 2-7

0
0

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-

co

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present material resembles Paradoxiellajaponica in several respects.
Occurrence ;- Very rare in 4052B, Semba,
Kuzu Town, Aso County, Tochigi Prefecture.
Reg. nos. 5026, 5027, 5028.

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l1'>
N

0 0 0 0 0 0

0 0 0

<0

o(l

::s

0

0 0 0 0 0

I::
.!<:

Ul

l1'>
N

M
N

- -- ---

0

....o

M

0

0 0 0

Ul

....

"

-

l1'>

.".
0

95

0

M

0

co

0

M

"1'

LI>

<0

t-

co

0>

t-

o

t- O> l1'> 00 <0 <0I ,....;,....; ,....; ,....; ,....; ,....;

-

N

M

Yabeina kanmerae leo, 1964b, p. 647, pI. 106,
figs. 1-4.

Shell large, highly inflated fusiformwith convex lateral slopes and bluntly
rounded poles. Mature specimens have
21 to 25 volutions. The largest specimen 13.20 mm in axial length, 8.40 mm
in median diameter and 1: 1.57 in form
ratio. Inner one or two volutions commonly discoidal and coiled askew tolater volutions. Pro loculus very small,
spherical and 33 to 80 p in outside diameter.
Spiro theca thin, consists of tectum andfine alveolar keriotheca. Thickness of
spiro theca about 10 p in juvenile volutions, 50 to 80 p in outer volutions.
Septa also thin, numerous, rather widely spaced and unfluted throughout .
Septal counts 30 to 35 in 20th and later
volutions. Axial septula variable both inshape and numbers per chamber. One
axial septulum developed in inner fourth
to sixth volutions, commonly 2 or 4 in
8th to outer volutions, 4 to 10 in 20th
volution. Primary transverse septulathin, appear throughout shell, unite withthin and rather high delicate parachomata and about one half of height ofvolutions in younger stages, but about
one third in adult stages. Secondarytransverse septula also thin, short and·delicate. They first appear in· 8th or

96

Hisayoshi leo and Hisaharu leo

9th volutions and regularly alternatewith primary transverse septula in 10thor 11thvolution and outerward.
Twosecondary transverse septula
rarely appear between adjacent primary
septula in outer volutions.
Remarks:- Yabeina kanmerae was firstdescribed from the Kono Formation of
the Nyukawa Group. Hisayoshi IGO
pointed out that this species resembles
Yabeina columbiana (DAWSON) in many
respects, but it differs from the latterin slightly larger shell, higher chambersin the adult stage and small proloculus.
Yabeina syrtalis (DOUVILLE) which was
fully redescribed by SKINNER and WILDE(1967) from Tunisia is also an allied
species.
Occurrence :-Abundant in4052B, Semba,
Kuzu Town, Aso County, Tochigi Prefecture.
Reg. nos. 5029, 5030, 5031, 5032, 5033,
5034.
Yabeina globo::a (Y ABE)
PI. 14, fig. 1

Neoschwagerina globosa YABE, 1906, p. 4, pI.
1, fig. 5, pI. 3, fig. 1; OZAWA, 1927, p.
159-160, pI. 41, figs. 2, 9, pI. 42, figs. 1,
2, 4, 6, pI. 43, figs. 1b, 4; Yabeilla globosa,
MORIKAWA and SUZUKI, 1961, p. 67-68,
pI. 10, fig. 2, pI. 16, fig. 8, pI. 21, fig. 1.

[For further synonymy refer(1966, p. 818-819).J

KAHLER

Remarks:-We have obtained several
sectioned specimens associated with
Yabeina kanmerae. They have 18 to 21
volutions measuring 11.4 to 11.8 mm inlength and 7.3 to 8.2 mm in median
diameter. Primary transverse septula
developed throughout, united with thickand high parachomata especially inouter volutions. Secondary transverse
septula first appear in 6th or 7th volution. General biocharacters are very
similar to the topotype specimens camefrom the Akasaka Limestone.
Occurrence :-Rare in 4052B, Semba,
Kuzu Town, Aso County, Tochigi Prefecture.
Reg. nos. 5035, 5036.
Acknowledgements:-We wish to express our sincere gratitude to Dr. Toshio
KOIKE of Yokohama National University,
Mr. Fumio KOBAYASHI of Tokyo University of Education and Mr. Shigeru
TAKIZAWA of the University of Tsukuba,Miss Sachie HOSOI and Miss Rieko AOKI
formerly of the students of TOkY~
Gakugei University, for their kind assistance in the field. Sincere thanks also
go to Mr. Yoichi SUZUKI of the Miyata
Lime Industry Co. Ltd., for his kindfacility in the field and to Miss Shuko

Explanation of Plate 13
Figs. 1-6. Nankillella kuzllellsis lGO and lGo, n. sp.
1, Axial section of the holotype; 2, 4-6, axial sections of para types; 3, tangential sectionof paratype; x 30.
Figs. 7-20. Dunbarula suzukii lGO and lGo, n. sp.
7, Axial section of the holotype; 8-18, axial sections of paratypes; 19, 20, sagittal
sections of para types; x 25.
Figs. 21~24. Reichelilla changhsillgellsis SHENG and CHANG
Axial sections, x 30.
Figs. 25, 26. Paradoxiella sp ..
Sagittal sections,. x 30.

H . lco and H. lCO:

Upper Permian Fu,sulinaceans

Pla,te 13677.

Upper Permian F1ts?,£linaceaof the Universitv of Tsukuba
for typing this manuscript.
Repository :-All specimens describedin this paper are preserved at theInstitute of Geoscience, the Universityof Tsukuba.
ADACHI

97

References cited
CHEN, S. (1956): Fusulinidae of South China,
Part 2. Pal. Sinica, N. S., B, no. 6, p. In, pIs. 1-14.
FUJIl\IOTO, H. (1961): Explanatory text ofthe geological map of Japan, Scale
1 : 50000, Tochigi. Ceol. Surv. Japan.

Table 4. Measurements of Yabeina kanmerae IGO (in mm.)
Specimen
34567Height of volutions

w. F.R. D.P.

L.

11. 20 8.60 1.38 0.05
13.20 8.40 1. 57 0.08
11.60 9.10 1. 27 0.03
10.30 7.07 1. 46 0.04
7.63
0.05

1

2

3

0.05
0.01
0.02
0.04
0.03

0.05
0.07
0.03
0.02
0.06

0.07
0.07
0.03
0.15
0.05

4

5

6

7

0.07 0.12 0.11
0.15 0.16 0.16
0.07 0.10 0.10
0.09 0.12 0.13
0.08 0.18 0.12

8

0.13 0.16
0.17 0.19
0.12 0.14
0.15 0.17
0.14 0.15

910

0.17 0.20
0.18 0.45
0.16 0.17
0.21 0.21
0.17 0.16

Height of volutions
11

12

13

14

15

16

17

18

19

20

21

0.20
0.19
0.17
0.21
0.18

0.20
0.24
0.21
0.24
0.21

0.20
0.24
0.25
0.24
0.24

0.26
0.12
0.30
0.24
0.21

0.31
0.39
0.25
0.31
0.23

0.25
0.29
0.27
0.21
0.26

0.27
0.30
0.27
0.21
0.24

0.32
0.31
0.30
0.31
0.18

0.32

0.30

0.32

0.27

0.27

0.27 0.27 0.30 0.28 0.27

0.27

0.21

22

23

24

25

Thickness of spiro theca
Specimen
3
4
5
6
7

1

2

3

4

5

6

7

8

9

10

11

12

0.01
0.01
0.01

0.01
0.01
0.01

0.01

0.01

0.02
0.01
0.01
0.02
0.02

0.02
0.02
0.02
0.02
0.02

0.02
0.02
0.02
0.02
0.02

0.02
0.05
0.03
0.02
0.02

0.05
0.03
0.05
0.02
0.02

0.08
0.03
0.04
0.02
0.02

0.05
0.03
0.04
0.02
0.02

0.02
0.02
0.03
0.02
0.02

0.02
0.03
0.02
0.02
0.02

0.02
0.03
0.02
0.02
0.02

23

24

25

0.03

0.03

Thickness of spirotheca
13

14

15

16

17

18

19

20

21

22

0.02
0.03
0.02
0.02
0.02

0.02
0.03
0.03
0.02
0.02

0.02
0.03
0.02

0.02
0.03
0.02

0.02
0.03
0.02

0.02
0.03
0.02

0.02
0.02
0.02

0.02
0.02
0.02

0.02

0.02

0.02

0.02

0.03

0.03

0.02

0.02

0.02

0.02

0.02

0.02

0.02

0.02

98

Hisayoshi IGO and Hisaharu IGO

HATORI, H. (1965): Stratigraphic studies inthe southeastern part of the Ashio
Massif, Tochigi Prefecture. jour. Geol.
Soc. japan, vol. 71, p. 247-256.
IGo, H. (1964a): Fusulinids from the Kabe·yama Formation (Permian) Kuzu, Tochigi
Prefecture, Japan. Mem. Mejiro Gakuen
Women's junior Coli., vol. 1, p. 1-28, pis.
1-10.
- - (1964b): Permian fusulinids of Nyu.
kawa, central Japan, Part 1. jour. Pal.,
vol. 38, p. 637-649, pis. 103-106.
ISHII, A. and TAKAHASHI, H. (1960): Fusu·
linids from the upper Permian Ogamata
Formation, central part of the Kwanto
Massif, Japan. Sci. Rep. Tokyo Univ.
Education, sec. C, vol. 7, no. 66, p. 205216, pis. 4, 5.
KAHLER, F. and KAHLER, G. (1966): Fossi·
lium Catalogus, Part 113, Fusulinida.
Teil 3, p. 818-819, junk.
KANMERA, K. and NAKAZAWA, K. (1973):
Permian· Triassic relationship and faunalchanges in the eastern Tethys. Mem.
Canada Soc. Petrol. Geol., 2, p. 100-119.
KOBAYASHI, F. (1975): Palaeofusulina.Rei.
chelina fauna contained in the pebbles
of intraformational conglomerate dis·tributed in the Okutama district, WestTokyo. Trans. Proc. Pal. Soc. japan,
vol. 80, no. 7, p. 293-306.
KOIKE, T., IGo, H., IGo, H. and KINOSHITA,
T. (1974): Geological significance of theunconformity between the Permian Nabe·
yama and Triassic Adoyama Formationsin the vicinity of Kuzuu, Tochigi Pre·
fecture. jour. Geol. Soc. japan, vol. 80,
no. 7, p. 293-306.
MORIKAWA, R. and HORIGUCHI, M. (1956):
Parafusulina nakamigawai n. sp. from the
Adoyama Formation in the neighborhoodof Kuzu City, Tochigi Prefecture. Sci.

Rep. Saitama Univ., ser. B, vol. 2, p.
261-264, pl. 35.
- - and SUZUKI, Y. (1961): Fusulinids fromthe Akasaka Limestone (Part 2). Sci.
Rep. Saitama Univ., ser. B, vol. 4, p. 4374, pis. 4-22.
- - and TAKAOKA, Y. (1961): Two new
species of the Parafusulina yabei typefrom Tomuro, Tochigi Prefecture, Cent·ral Japan. Trans. Proc. Pal. Soc. japan,
N.S., no. 41, p. 33-40, pis. 7-9.
NOGAMI, Y. (1958): Fusulinids from the
Maizuru Zone, Southwest Japan, Part 1.
Mem. Coll. Sci., Kyoto Univ., ser. B, vol.
25, p. 97-109, pis. 1-3.
OZAWA, Y. (1927): Stratigraphical studiesof the Fusulina Limestone of Akasaka,
Province of Mino. jour. Fac. Sci., Imp.
Univ. Tokyo, sec. 2, vol. 2, p. 121-164,
pis. 34-45.
SAITO, Y. and KATO, A. (1971): Smaller
foraminifers from limestone lenses in
the West of Umenoki, Kuzuu.machi,
Ashio Mountainland. jour. Geol. Soc.
japan, vol. 77, p. 675-676.
SHENG, J. C. (1958): Some fusulinids from the
Maokou Limestone of Chinghai Province,
northwestern China. Acta Pal. Sinica,
vol. 6, no. 3, p. 268-291, pis. 1-4.
- - (1963): Permian fusulinids of Kwangsi,
Kueichow and Szechuan.
Pal. Sinica,
N.S., no. 10, p. 1-247, pis. 1-36.
- - and CHANG, L. H. (1958): Fusulinids
from the type.locality of the Changhsing
Lime~tone.
Acta Pal. Sillica, vol. 6, no.
2, p. 205-214, pI. 1.
SHOJI, R. (1967): Occurrence and petro·logical studies of Paleozoic chert of thewestern Ashio·Mountain.
jubilee Pub.
Commem. Prof. Sasa, 60th Birthday, p.
171-183.
SKINNER, J. W. and WILDE, G. L. (1955):

Explanation of Plate 14
Fig. 1. Yabeina g/obosa (YABE)
Axial section, x 8.
Figs. 2-7. Yabeina IWllmcrae IGO
2, Axial section; 3, slightly oblique axial section; 4-6, sagittal sections; 7, tangential
section, x 8.

H. leo and H. leo:Upper Permian Fusulinaceans

Plate 14

677.

Upper Permian Fusulinacea

New fusulinids from the Permian ofWest Texas. jour. Pal., vol. 29, no. 6,
p. 927-940, pIs. 91-95.
- - and - - (1967): Permian foraminiferafrom Tunisia. Univ. Kansas Pal. Contr.,
no. 30, p. 1-22, pIs. 1-32.
WATA;\"ABE, T. et al. (1957): Geologicalmap of the Ashio Massif and explanatory
text. Tochig Pre!.
Y ABE, H. (1906):
A contribution to thegenus Fusulina, with notes on a Fusulinalimestone from Korea. jour. CoIl. Sci.

99

Imp. Univ. Tokyo, vol. 21, p. 1-36, pIs.
1-3.
YANAGIMOTO, Y. (1973): Stratigraphical andgeological structure of the Paleozoic andMesozoic formations in the vicinity ofKuzu, Tochigi Prefecture. jour. Ceol.
Soc. japan, vol. 79, p. 441-451.
YOSHIDA, S. (1956, 1957): Stratigraphicaland tectoni cal studies in the districtneighboring Kuzu Machi, Tochigi Prefecture, Part 1, 2. Bull. Ceol. Comm.
Hokkaido, no. 32, p. 1-10, no. 33, p. 1-5.

Trans. Proc. Palaeont. Soc. Japan, N. S., No. 106, pp. 100-105, pl. 15, June 30, 1977

678.

MIDDLE JURASSIC AMMONITES FROM BISHO,KUMAMOTO PREFECTURE, KYUSHU*HIROMICHI HIRANO** and HIROYOSHI SANO
Department of Geology, Kyushu University, Fukuoka 812

j'j~*9f<~1:'@:<f1:lt1J s/ "- "7 *,C 7 / -'C 7 l' ~: ~*9f<i\ ~!lli*~:fj~1:iJ' GIi, iJ, -:> "O'h'i!:t'~*~R~~:. J: f) ~:lt!!.IliX~uPJm s/ "- "7 *O):ff:::fE-t;o ;: .!::
iJ:~i~~n""( \, ,t-::o JiiJli, f!i:'llffi~~:lt!!.IliXO)ilH!l1Ez.rr\' " r"'~.!:: ~ n""(\, ,t-:::lt!!~O):B-:;(Pfllliltll.!::A'tilfz.1!!l GiJ'i:' Lt-::o i tdli't-::I:'-" l/.L.. 7 l' ~ 1 ffiliJ;~Gnt-::o ;: nO)ftEfH 'fn {, ItIfJti3<J

1fl!~:. J: f) 7 / -'£- 7 "'t ~ 3 lIliJ:l*:!* ~n,-Clii5;oiJ:, ·~W10)*6:ll~:7 /-'£-71' ~ 0) 111lfi Cadomites sp., fmO) 111lft Planisphinctes?
sp. .!:: ~t<E ~ nt-::o -" l/ .L.. 7 l' Hi s/ '" l/ '/4'- - P$±O)llili~i:' J: f) Parahastites? sp. .!:: \"*-;00 tJl:O)=~O)~jjO){E:ff::ltIJr"jfi<f1:lt1Js/ "- "7f.C-Ci5 i), ~1E~nt-:::lt!!~O)±Jmft<f1Jms/ "-<"7*z.'@;trbl~·*-Gnoo ~Gnt-::ltEO)f*miJ: tt.\"iJ:, ltE'@:I±l~O):!6ffiIk.(:ftl"H~l:O)&~z.i5b~~*-;o.!:::lt!!~~.l:• • ~.M.!::~;oO)~ ~~L~.Lko
3f'llf5l.~ • ft'llf5l.tff-

sequence of the formation in question(SANO, 1977), with acquisition of abelemnite; the other of us (H. H.) endeavoured to identify the ammonites
collected by Mr. AKA TSU. This paper
is to describe briefly the results of ourstudy.
We thank Prof. MATSUMOTO for thepertinent supervision, Dr. K. KANMERA
and Dr. K. TANABE for their help in thefield work, Mr. K. AKA TSU for his
generosity to provide the specimens forthe study, Dr. J. A. JELETZKY for theidentification of a belemnite, and Messers
MURASAKI and INOUE of Toyo .. mura for
their offer of facilities in the field work.

Introduction

The Bisho area in Toyo .. mura (pre ..
viously called Ka wamata .. mura), Yatsu ..
shiro .. gun, Kumamoto Prefecture was
geologically studied by Ken AKA TSU forthe graduation thesis of Kyushu University in 1957 under the supervision ofProf. T. MATSUMOTO. He collected a
few ammonite specimens at Bisho in thearea but did not describe them. MATSUMOTO (1962, p. 235) briefly recorded thisfact, mentioning that the ammonite
bearing formation could be Middle
Jurassic.
At the suggestion of Prof. MATSUMOTO
one of us (H. S.) restudied the geologyof the same area in 1974 and clarified
the distribution and the stratigraphic* Received March 22, 1977; read June 27,
1976 at Hiroshima.
** Present address: Institute of Earth Science,

Geological setting

The localities of ammonites and abelemnite are near a small village called
Bisho in the tributary of the River
Hikawa and are geologically in the Hinagu
belt of the Chichibu terrain (MATSUMOTO

School of Education, Waseda University,
Tokyo 160.

100

678.

Middle Jurassic Ammonites from Kyushu

and KANMERA, 1952; KANMERA, 1953),
where sediments from the upper Permianto the lower Cretaceous are complicatedly
distributed (Fig. 1). The Jurassic Bisho
Formation is narrowly distributed andsurrounded with faults by the Norian in
the north, the Albian Yatsushiro Formation in the south and east and theNorian and the Aptian Hinagu Formation in the west (Fig. 2). The Jurassic
strata trend from NEE to SWW, dipping
steeply to the south. They are composedof massive shale and alternation ofsandstone and shale. The conformableseries is stratigraphically divided into
three parts, the upper, the middle andthe lower. The ammonites are presumed
to have come from the shale of the
middle part (Fig. 3).

5,
Fig. 1.

101

Palaeontographic description

Family Stephanoceratidae
NEUMAYR, 1875
Genus Cadomites MUNIER-CHALMAS, 1892
Type-species.--Ammonites deslongchampsi
DEFRANCE in D'ORBIGNY, 1846 (rCZN
Opinion 324).
Cadomites sp.
PI. 15, Fig. 2

Material.-An internal mould (rightside) of a quarter whorl, GK. G. 11432.
Description.-The whorl is of moderate
involution. The primary rib is rectiradiate and generally strong with some-

10km,

Map showing the studied area and the Hinagu and Sakamoto belts.

102

Hi1'omichi HIRANO and Hiroyoshi SANO

N

t

x

(Hn)
...::;.~, "/ , / / / / ,/ / /[ill] a~;~// (Ys);" ~:/ /;~ // /

"

, /

/ /

/

7

//
/////
///
,//,,//,,//// /////'""''''/'''////'" '" '" 0

\-y

lkm

~b

==

c

~d
~e

I

Fig. 2. Geological map of the Bisho area. a: Kuma Formatiom, b: Upper Triassic
Formation (Tr), c: Middle Jurassic Formation, d: Hinagu Formation (Hn), e: Yatsushiro
Formation (Ys).

~ 10c.C"!< loc, B................

. ................ .. .
~o~.::.-.-:::: :: .../o......

'·':::::::::::·1

what sharp crest. It starts from theumbilical seam, becoming stronger outward and bifurcates or trifurcates at
the middle of the flank, where it isswollen if not tuberculate. The swell
is fairly high in the earlier part but becomes weaker on the later part. The
secondary rib is much finer and much
lower than the primary. The interspaceof the primary ribs is about two times
as wide as the primary rib, and theinterspace of the secondary ribs is as
narrow as the secondary rib.
Theventer, cross section, early whorls andFig. 3. Columnar section of the Jurassic
near Bisho. Fossil localities, A: ammonite,
B: belemnite, C: bivalve. Solid line: shale,
dot: sandstone, alternating line and dots:
alternation of sandstone and shale.

678.

Middle Jurassic Arnrnonites frorn Kyusln~

suture are not seen.
Comparison.-The present specimen issimilar to the specimens of C. deslollgchampsi (d'ORBIGNY) (ARKELL, 1952,
text-fig. 21). from England, and C.
psilacanthus (WERMBTER) (WESTERMANN
and RrouL T, 1975, p. 871, pI. 105), from
Normandy, in the strength of primaryrib, the mode of fur cation, the weaknessof secondary rib, and the mode of coilingbut is distinguished by the absence oftubercle at the point of furcation.
The present specimen also resembles
MAUBEUGE'S (1969. p. 76) specimen of C.
septicostatusiformis (MAUBEUGE), fromBale-Campagne, in the general charactersbut has much stronger primary ribs
which show clearer furcation.
It is distinguished from a specimen of
C. seplicostatus BUCKMAN (1923, part 42,
pis. 422a-b) by the wider interspace ofribs, that is, the interspace in the latter
is as narrow as the width of the rib,
although both two lack a distinct tubercle at the point of fur cation.
Only C. bandoi TAKAHASHI (1969, p. 61,
pI. 5, figs. 4, 6-8, 13) has been hitherto
known from Kitakami as a species ofCadomites in the Japanese Jurassic but
the present specimen is not allied to any
specimen of C. bandoi in that it has
stronger primary ribs and no tubercles
at the points of furcation.
Locality.-Locality A in the route map(Fig. 4). It is a small tributary of theRiver Hikawa, running near Bisho, Toyomura, Yatsushiro-gun, Kumamoto Pre-

Fig. 4.

Route map of the fossil localities.

103.fecture, Kyushu.
Family Perisphinctidae
STEINMANN, 1890
Subfamily Pseudoperisphinctinae
SCHINDEWOLF, 1925
Genus Planisphinctes BUCKMAN, 1922
Type-species.-Planisphinctes planilobus
BUCKMAN, 1922
Planisphinctes (?) sp.
PI. 15, Figs. la-b

Material.-A left external mould of afragmentary specimen, GK. G. 11433.
Description.-The whorl is fairly evolute. The primary rib radially runs
from the umbilical seam. Its crest is
sharp at the umbilical shoulder and becomes fiat and low outward. The interspace of the ribs is nearly as wide asor somewhat broader than ,the rib.
Several ribs show bifurcation immediately below the umbilical seam of thenext whorl. The ventral area is so incompletely preserved that its characters
are not observable.
Comparison.-Because the presentspecimen is fragmentary and because its outerpart is not observable, it is hardly identified. The described characters, however,suggest that it may be a species ofPlanisphinctes. It is indeed similar to
Planisphinctes planilobus BUCKMAN (1922,

Symbols are the same as those in Fig. 3.

104

Hiromichi HIRANO and Hiroyoshi SAND

pI. 327; ARKELL, 1958, p. 230, pI. 33, figs.
7a-c) in the widely separated somewhat
sharp primary ribs and evolute whorls
but exact comparison should be done on
better preserved specimens.
Locality.-Locality A in the route map(Fig. 4), Bisho, Toyo-mura, Yatsushirogun, Kumamoto Prefecture, Kyushu.
Concluding remarks

In Europe C. d(lslongchampsi ranges
from the Parkinsoni Zone to the Zigzag
Zone, and C. psilacanthus is restricted
to the Parkinsoni Zone. Genus Cadomites
is said to range from the upper Bajocian
to the Bathonian or to the lower Callovian with question. The age of Genus
Planisphinctes is the lower Bathonian.
One unfavourably preserved specimen,of which characters suggest that it may
belong to a middle or upper Jurassic
ammonite, illustrated in the plate (PI. 15,
Fig. 3) also was obtained at loco A by
AKATSU.
A belemnite, collected at loco B by
TANABE, is similar to Parahastites (personal comm. by Dr. JELETZKY) whichranges from Pliensbachian to Bajocian.
At loco C an unfavourably preserved
bivalve was obtained, but is too incomplete to be identified.
From these facts the main part of thestudied succession is regarded as the
middle Jurassic, especially from Bajocian
to Bathonian.
Hitherto known middle Jurassic in the
Chichibu terrain is the Naradani Formation in Sakawa, Shikoku and the
Tsurubami Formation in the Kuma
mountains, Kyushu.
These two formations are shale and sandstone withlenticular, partly oolitic limestones containing brachiopoda, echinoid spines etc.
(TAMURA, 1960), but the studied middle
Jurassic sequence is shale and alternation of sandstone and shale without
limestone. Furthermore, it should be
noted that the middle Jurassic formationof Bisho is distributed in the Hinagu belt
whereas the upper and middle Jurassic
Torinosll and Tsurubami formations arein the Sakamoto belt to the south of the
Hinagu belt (Fig. 1).

References
ARKELL, W.]. (1952): Monograph of the
English Bathonian Ammonites. Palaeontogr. Soc. pt. 3, p. 73-102, pIs. 9-11.
- - (1958): Ditto, Ibid., pt. 8, p. 209-264,
pIs. 30-33.
BL"cK:VIAN, S. S. (1922):
Type Ammonites.
vol. 4, pt. 35, pI. 327.
- - (1923): Ditto, vol. 5, pt. 42, pIs. 422A-

B.

Explanation of Plate 15(All in natural size)
Fig. 1. Planisphinctes? sp.
la. External mould, GK. G. lU33, loc. A. lb. Rubber cast of lao
Fig. 2. Cadomites sp.
2. GK. q. 11432, loc .. A.
Fig. 3. Gen. et sp. indet.
3. GK. G. 11435, loc. A.
Fig. 4. Parahastites? sp.
<la. Late;al view of rubber cast, GK. G. 11434, IDe. C. ·lb. Dorsal view of rubher cast.
4c. Ventral view of rubber cast.

HIRANO and SANO: Jurassic ammonites from Kyushu

Plate 15

678. Middle Jumssic Ammonites from Kyushu
KANMERA, K. (1953): The Kuma Formation,with special references to the Upper
Permian of Japan.
Jour. Geol. Soc.
Japan, vol. 59, no. 697, p. 449-468.
MATSU1..,!OTO, T. (1962): Regional geologyof Japan-Kyushu region. MATSUMOTO,NODA and M!YAHISA (eds.), 423p., Asakura Publishing Co. Tokyo.
MATSUlI'!OTO, T. and KANMERA, K. (1952):
A guide book for field trip: The area ofthe lower stream of the River Kuma. 71
p., 6pls., Dept. Geol., Kyushu Univ.,
Fukuoka.
MAUBEUGE, P. L. (1969):
Catalogue desAmmonites du Jurassique inferieur etmoyen (Hettangien a Bathonien) duMusee cantonal del Bale.Campagne.
Tiitigkeits. Natur. Gesell. Baselland, Bd.
26, p. 65-79.

SANO, H. (1977): Middle Jurassic Formationin the Kuma Mountains, Kyushu. Jour.
Geol. Soc. Japan, vol. 83, no. 2, p. 135137.
TAKAHASHI, H. (1969): Stratigraphy andammonite fauna of the Jurassic systemof the southern Kitakami Massif, north·east Honshu, Japan. Sci. Rept. Tohoku
Univ., 2nd ser. (Geol.), yol. 41, no. 1, p.
1-93, pIs. 1-19.
TAMURA, M. (1960): Stratigraphic study on
the Sakamoto Group in Kyushu. Jour.
Geol. Soc. Japan, vol. 66, no. 777, p.371383.
WESTERMANN, G. E. G. and R!OULT, M.
(1975): The lectotype of the ammonite
Cadomites psilacanthus(WERMBTER).
Palaeont., vol. 18, pt. 4, p. 871-877, pI. 105.

Bisho ~1:, Naradani -t~1:l-, Hikawa 7tJII, Sakamoto 1&*, Hinagu S~~.
*~tt, Kawamata foJ~, Tsurubami
Kuma ;ej(f!, Yatsushiro·gun /\ftW

tIj*.

105

Toyo.muraTrans. Proc. Palaeont. Soc. Japan, N. S., No. 106, pp. 106-121, pI. 16, June 30, 1977

679. A MOLLUSCAN ASSEMBLAGE OF THE SETOGAWA GROUPYASUHIDE IWASAKI
Department of Geology, Faculty of Science, Kumamoto University,
Kumamoto 860

and
SUSUMU ONO
Japan Petroleum Exploration Co. Ltd. Tokyo

iflip)II~~£:O)JHI::E~: iflipJllm~ltfl::El::'z L.

<, ;:nt::.~-t7.>~1!i-lt~ <tt.~'iJ;,'}!Ilflt:lt!fl~1tO)-m i?, j'iiJ~~9=rf!BO)lm1R.~rlftt::.a.; 7.> ;y':Ji!:;!5ffi!5O)@:J:.iJ' i?~+/~0)fJi!::ff:0)a.; i I) J: <tt.\" Jl,fl::Ez.l*~ L.t':o ;: 0) <PiJ' i?~ JI, 6~, =fXJI, 8 ~z.IDlt'i]IJ L.t.:0)L'~1!i--t 7.>0;: O)fT-I, :A 'J '\'- v ;11'1 MO)-~lt¥r~c~6? i?nt.:O)L' Emarginuia tokuyamai C ~~ L.
1l21ltL.t.:o ;:O)fl::E~~lt, iJ'"0-C7.K!Ilf (1956) iJ:1!il1jtt::.llciillL.t.:;: ciJ~a.;7.>o ~JI,~t::.-gtr;: C. *!t. fT-I!t0)='?0)9bt.:~~~O)imfrz.jf--t;: cz.~~c-t7.>o ~,@,~lt:}.;:}.;trt2r
iiBl:li:iia1ff cm~~n, iia!1£ffi!5 c ~niJ' i?iJR1=. L.t.:~li!ttt. C'iJ;mnlt-t 7.> Ift'lI::' {f ? *1=.~~1it~~~."0~~mO)~~Ift~#?fT-I1=.~~~imftL.~~O)c~~i?n7.>o~JI,.#.~=aJl,
fT-Ij:.O)=fXJI, z.±: c -t 7.> j'iiJ~f;;ft!JJt!!~O) JI, ft:E~~ c;il<JI-t7.>flltjn'iJ:, M(ci] c L. -Clti5~=*cO)l:li:JI,-~fT-I~lfJb~~c O)Jli{J;J,~iJ'~~6?
7.>0
oEf~~~ • 'J'!Ilf ~tt. c· O)*1=.O)~~iJ~1j!.~-t 7.> t':6?iJ',

5t*.

i?n

structural geology were already reported(ONO, 1973). In the course of his fieldsurvey, ONO collected molluscan fossils
at several localities. The majority ofnearly fifty fossil specimens for thepresent study were derived from a single
outcrop at Ashikubo, northern part of
Shizuoka city. Fossil collection wasmade several times at this outcrop andadjacent areas in order to obtain better
specimens for identification. The molluscan fossils, especially the fossil assemblage, were studied mainly by IWASAKI. 16 species were discriminated in
the total collection, although 12 of them
are specifically indeterminable owing to
the poor preservation. The results oftaxonomic study are summarized in thisIntroduction
The Setogawa Group, widely distributed in Shizuoka and Yamanashi Prefectures, central Japan, is a series ofthick clastic sediments of Paleogene age.
Our biostratigraphical and paleontologicalknowledge on this group, however, remains quite insufficient owing to its poor
fossil occurrence, compared with other
Cenozoic deposits of Japan. From 1967
to 1972, one of the writers, ONO surveyed
this group in almost all the distributed
area for the structural analysis.
Soine results on the stratigraphy and* Received April 9, 1977; read January 31,
1976 at Kawatabi.

106

679.

Setogawa Molluscs

article with some notes on the fossil
occurrence and on the upper Paleogene
molluscan faunas. All specimens numbered with prefix eM are deposited in
the Department of Geology and Palaeontology, University Museum, University ofTokyo.

On the occurrence of fossils
Fossil molluscs here treated were collected from one outcrop in a small
valley on the northern slope of Mt.
Takayama, about 500 m south from the
Ashikubo river, at Yazawa, AshikuboOkugumi, Shizuoka city, which is locatedin the central part of the distribution

107

area of the Setogawa group (Text-fig. 1).
There expose layers of titan-augite
bearing alkali basalt flow, and tuffaceousand calcareous lithic sandstone steeply
dipping to ESE. They make up a coreof an anticline of NNE-SSW trend.
Fossil bearing rock is a thin lithic sandstone overlying the lava flow. Fossils
are found close to the basalt as if they
were contained in volcanic rocks. Molluscs occur rather sporadically in association with corals and algal fragments
except for some shell clusters of Lima
sameshimai. As almost all the shellmaterials are dissolved, only outer andinner molds can be obtained. However,
the tests of Lima, Brachidontes and~ II 0.. ~ t

5 km

Text-fig. 1. Map showing fossil collecting location at Ashikubo,
Shizuoka City. Explanation of geological map; 1. basalt lava, 2. lower
calcareous member of the Takizawa Formation, 3. upper sandstone andshale member of the Takizawa Formation, 4. Tentokuji Formation, 5.
conglomerate of the Tentokuji Formation, 6. picrite.

108

Yasuhide IWASAKI and Susumu ONO"Minolia" species remain unsolved inpart. The preserved material of theformer two bivalves seems to be recrystallized calcite which primarilv formed
the outermost calcite layer. Similar
partial preservation of the calcite shelllayer was also found in the Eocene molluscs in the nummulite-bearing sandstoneof Hahajima OW ASAKI, 1975). Most
A
bivalve shells are disarticulated.
muddy limestone layer is found above
the lithic sandstone, and silicified shelllike fragments are contained. But nogenerically determinable molluscan fossils
are found (Text-fig. 2). Thick argillaceous sedimentary rocks successive to thelimestone scarcely yield molluscan fossils
in the neighborhood of Ashikubo.
Among the fossils from Ashikubo, six
gastropod and eight bivalve species are
discriminated. They are:Emarginula tokuyamai IWASAKI and ONO,
n. sp.
" Minolia" ikebei (OZAKI, 1958)
Tonna? sp.
Fusitriton sp.
Mitra (Tiara) sp.
Hemiconus sp. [=? Conus sameshimai MIZU.
NO, MS]Brachidontes (Hormomya) sp.
Lima (Plicacesta) sameshimai OYA!l1A andMIZL'KO, 1958
Thyasira (Axinopsida) sp.
Trapezium d. jobanicu1Il RATAI and NISIYAMA,
Crassatella sp.
Crassatina (Chattonia) sr.
Nemocardium d. iwakiense (MAKIYAMA,
1934)

Cadella sp.
Two other bivalves were foundIchinose.
Chlamvs d. irregularis (SOWERBY)
Lucinoma annulata (REEVE)

fromFossil occurrence from Ashikubo wasonce briefly reported by MIZUNO (1956)
in a paper on biostratigraphy of the

?

-."
E

::::::::::: 5S

sh

-"

a

-;

..."

1

T

E

D
~

~

I

~

...
D

Text·Fig. 2. Columnar section of
mapped area in Text-fig. 1. Scale bar
indicates 10 m.

Japanese Paleogene.
Among several
molluscan species listed by him, Lima
(Acesta) sameshimai and Minolia tsuchii
were later described by OYAMA andMIZUNO (1958).
Among eight bivalve species, Lima
sameshimai, Brachidontes sp. and Trapezium cf. jobanicum are epifaunal, andthey may have attached themselves tosome hard objects. On the contrary,
Nemocardium d. iwakiense, Thyasira sp.
and Crassatella sp. are infaunal and presumed to have inhabited in fine sandbottom. Most of the gastropod species
listed above are epifaunal and probably
dwellers on hard, gravelly bottom orsand bottom. Dominant species of thisassemblage are Lima sameshimai among
bivalves, and "Minolia" ikebei among
gastropods, whereas Nemocardiu11l cf.
iwakiense is the most abundant among
the infaunal species. Thus, this assemblage is predominated by epifaunal

679.

Set ogawa Molluscs

species which inhabited on rocky or
gravelly bottom made up of the basalt
pillow lava and its breccia. ' The living
places of these epifaunal and infaunal
species do not seem to be far from eachother. The two ecologically inconsistentgroups of molluscs were most likely
mixed in the course of deposition.
Remarks on the stratigraphy andcomparison with othermolluscan faunas
Stratigraphically, the Ashikubo fauna
occurs from the lower part of the Takizawa Formation, and two other bivalvesof Ichinose occur from the Tentokuji
Formation of ONO (1973). The Setogawa
Group in the neighborhood of Ashikubo
is subdivided into the following fiveformations in descending order:
Domoto Formation
Tentokuji Formation
Takizawa Formation
Sangozawa Formation
Oyakuzure Formation- - - - fault - - - The Takizawa Formation is mainlycomposed of sandstone and siltstone.
Limestone and conglomerate are intercalated in the lower part. Titan-augite
bearing alkali basalt lava and basaltic
breccia including lithic sandstone arefound at the basal part of this formation.
The basalt shows pillow structure in
part. The fossils are contained in thelower part of the formation. No significant unconformity is observable in thesequence of these formations. The
Takizawa Formation occupies the middle
part of the group indicating the stageof basic volcanic activity. According to109

TOKUYAMA (1974), the Setogawa Groupis a series of eugeosynclinal sediments
accumulated in the outer belt of theSouthwest Japan. The Setogawa Groupis said to be geotectonically distinguishable from the Shimantogawa Group andthe Oigawa Group, both of which are
adjacent to the Setogawa Group withfaults.
ONO'S stratigraphic subdivision of the
Setogawa Group is remarkably different
from the results by TOKUOKA (1964),
MATSUMOTO (1966) and MAKIYAMA in
MAKIY AMA et al. (1975), owing to different interpretation of the complicatedgeological structure. However, the fossilbearing horizon at Ashikubo seems,
anyhow, to belong to the Takizawa
Subgroup or Formation, the middle
division of the Setogawa Group, of theseauthors, because the basic volcanic layer,
a key bed, is included in the named formation.
Molluscs comprising the Ashikubo assemblage have no useful indicator ofwater depth. Most genera of the assemblage show remarkably wide bathymetrical distribution judging from theoccurrence of living related species.
The suggested depth from the assemblage
is between 30 and 200 m, likely somewhere from outer sublittoral zone tothe bathyal slope. Judging from thevertical and lateral change of sedimentary facies, the living place of these
species was probably on the top of amound or bank on the sea floor formedby the volcanic activity.
Occurrences of molluscan fossils werereported by ICHIKAWA (1946), MA TSUMOTO (1964, 1971) and MATSUMOTO andHIRATA (1972) from the Setogawa Group
at some other localities. All of themwere recorded from the southwesternarea, and from calcareous or noncalcareous sandstone and mudstone of

110

Yasuhide IWASAKI and Susumu OND

younger members than the present fossil
bed. The species composition is characterized by the predominance of bivalves,especially by soft bottom burrowing
species. No common species with the
Ashikubo fauna is found. MATSUMOTO(1964, 1971), described two different typesof molluscan fauna from the Oga andWappazawa Formations, the uppermost
and the lowermost parts of the Setogawa Group of his division. The former
is represented by Yoidia iaudabiiis YOKOYAMA, Venericardia tokudai TAKEDA andPhaxas izumoensis jobanicus (KANNO),
and is to be correlative to the Oligocene
Asagai-Poronai type fauna of Northeast
Japan. On the contrary, the latter ispredominated by Callista matsuraensis(NAGAO) which is an Oligocene species
common to the lower Miocene formations
in northern Kyushu, Southwest Japan.
MATSUMOTO and HIRATA (1972) reported
the occurrence of Aduiomya uchimuraensis
KURODA which was originally describedfrom the Miocene Bessho Formation.
MA TSUMOTO estimated the geologicalage of the Setogawa Group to be Oligocene to younger Miocene on the basisof these molluscan fossils.
On the other hand, HONJO and MINOURA (1968) reported a Discoaster species
from the calcareous rocks of the "Takizawa" Formation and correlated the formation with the Eocene of U. S. A. andEurope. NAKAZAWA (1973) considered
the geological age of the Setogawa
Group as Eocene to Oligocene on thebasis of regional stratigraphic correlationof the Shimanto terrain of Southwest
Japan.
Useful index fossils are scarcely included in the Ashikubo fauna, although
MIZUNO (1956) once attempted to correlate lvIoropophoius aff. effingeri WEAVER
from the present locality with M. effingeriof the Lincoln stage of U. S. West Coast.

In the present collection, there are comparable specimens with Ne11locardium
iwakiense of the Asagai Formation andTrapezium jobanicum of the Iwaki Formation in the Joban coal-field. Brachidontes sp. morphologically resembles B.
matchgarensis reported by MAKIY AMA(1934) from the Oligocene formation at
the northern end of Sachalien. These
evidences suggest that the Ashikubo
fauna is somewhat allied to the AsagaiPoronai fauna which is a cold water
representative mainly distributed in thenortheastern part of Japan, as alreadymentioned by MATSUMOTO (1964) in thecase of the molluscan fossils of his Oga
formation.
Most species comprising the Ashikubo
assemblage are, however, endemic to the
Setogawa Group. It may be partly due
to the predominance of epifaunal species
in the assemblage, which are generally
minor elements in the Japanese Cenozoic
molluscan faunas, and partly due totheir peculiar habitat, submarine bank,as shown in Text-fig. 3. In the molluscan
fossils of the Setogawa Group reported
by MATSUMOTO, bivalve species of soft
bottom dwellers are main constituents.
Among rich molluscan faunas in thelower Miocene of Japan, the Ogurui
faunule (KOBAYASHI and HORIKOSHI, 1958)
shows peculiar association of species
which is characterized by such gastropodsof rocky substrate Turbo and Tectus, andhas few common elements to the speciesof shallow sand bottom typified by the
Kadonosawa fauna. The relationshipbetween the Ogurui faunule and theKadonosawa type fauna seems to be
similar to that between the Ashikubo
assemblage and the Japanese Oligocene
molluscan faunas.
Lima sameshimai,
Emarginuia tokuyamai and some othermolluscs are recorded only from one
locality, although the individual number

679.

Setogawa Molluscs

111

I
A

M

30

B'

100
200

B

-c
mud

sand

B

30
-100

M

2

A

8

Callista matsurarmsis
Venericardia nipponica
Tellina umedairensis
Chlamys d. ashiyaensis

Brachidontes sp.
Lima sameshimai"Minolia" ikebei
Conus (Conolithus) sp.
8~

Nemocardium
cf. iwakiensecPortlandia watasei
Yoldia laudabilis
Venericardia tokunagai
Ancis trolepis japonicus
Fulgoraria praevos tiana

Text·fig. 3. Sea bottom profile showing estimated habitat of the Ashikubo assemblage,
and relation with other molluscan assemblages during the Setogawa stage. Upper diagram
showing relation of molluscan assemblage· type with water depth and bottom sediments. Ada·
pted from !TOIGAWA and SHIBATA (1973).

of these species is not small. Their dis·tribution may not be restricted to asmall area near Ashikubo, but presumably
they had no chance to be preserved at
any places where the similar environment to Ashikubo was prevailed.
ITOIGAWA and SHIBATA (1973), in their
paleoecological study of Miocene molluscsof the Setouchi district, recognized morethan 20 types of molluscan assemblages.
They attempted to plot these assemblages in a diagram of grain size of sediments in abscissa and water depth inordinate. The Ashikubo assemblage appears to be different from any assemblage types of their work, i. e., it represents
sand-gravel bottom of 30 to 100 m deepin the diagram, where no corresponding
assemblage is found in the Setouchi
district. Two molluscan assemblages

described by MATSUMOTO (1964, 1971)
seem to correspond either to ITOIGAWA
and SHIBATA'S Saccella-Cultellus or
Macoma-Lllcinoma assemblage.
No molluscan assemblage representing
littoral or near-shore facies has beenfound in the Setogawa Group. The
representative of near-shore type molluscan assemblage from the group is
likely similar to what once reported by
SHIKAMA (1951) from the southernmost
area of Nagano Prefecture. Callista(NAGAO),
Venel'icardia
matsllraensis
nipponica YOKOY AMA, Tellina umedairensis
SHIKAMA, Chlamys d. ashiyaensis(NAGAO)
and some other species were describedfrom the Wada Formation, and this assemblage has been regarded as allied to
the Ashiya fauna of northern Kyushu.
Although the Wada Formation is situated112

Yasuhide IWASAKI and Susumu ONO

beyond the Chichibu terrain about 50 km
nohhwesterly distant from Ashikubo, it
is one of the nearly distributed fossil-bearing
Paleogene sediments. Paleogeographicalrelationship between the Wada Formationand the Setogawa Group can presumably
be compared with that between the
Nakaoku Formation of SHUDA (1962)
and the Muro Group in the Kii Peninsula.
The Muro Group, which is stratigraphically correlative with the Setogawa
Group (NAKAZAWA, 1973), is characterized by thick and deeper water finegrained clastic sediments. On the other
hand, the approximately contemporaneous Nakaoku Formation is comparatively
thin and composed of shallow watercoarse-grained sediments, and its distribution is restricted to the pre-Cenozoic
Chichibu terrain. Molluscan fossils occurring from the Muro Group were summarized by MIZUNO (1973). Most species
belong to two assemblage types. One isequivalent to those described by MATSUMOTO (1964), and the other is a deeper
water dwelling group comparable withmuddy bottom species from the HotaGroup of the Boso Peninsula describedby HAT AI and KOIKE (1957), including
Solemya bosoana HATAI and Acila vigilia
SCHRENCK, Porilandia watasei (KANEHARA), Periploma besshoense(YoKOYAMA),
Ancistrolepis bicordata HAT AI and KOIKE.
The latter seems to correspond to the
Nuculana- Yoldia or Neilonella-Palliolul1l
assemblage of ITOIGAWA and SHIBATA(1973).
Thus, in Text-fig. 3 is shown a topographic section, bottom sediments andcorresponding molluscan species groups
at the discussed area during the Setogawa stage, presumably of Eocene toearly Miocene ·age. The annexed diagram in Text-fig. 3 is adapted fromITOIGAWAand SHIBATA (1973).
As MIZUNO (1956, 1973) and MA TSU-

MOTO (1964) stated, the molluscan faunaof the Setogawa Group, particularly the
deeper elements, has apparent relationship to the northern Asagai-Poronai type
fauna. These deeper elements seem tobe extensively distributed to the area ofthe Muro Group. The Asagai-Poronai
type fauna appears to extend its distribution southward, gradually changing
its optimal habitat to deeper domainsof bathymetry.
The shallow waterelements are, on the other hand, havemuch alliance to the southern Ashiya
type fauna, and this area seems to benear the northern extremity of the- warm
water elements. As the Setogawa Groupis distributed geographically in the
middle part of the Japanese Islands, its
molluscan fauna is characterized by two
different Paleogene faunal elements developing typically in Kyushu and Hokkaido, southern and northern extremities ofJapan respectively. Thus, the Setogawa
Group containing both types of faunas
is likely situated in the transitional areaof the two zoogeographical provinces inlate Paleogene times.

Systematic description
Family Fissurellidae FLEMING, 1822
Subfamily Emarginulinae GRAY, 1834
Genus Emarginula LAMARCK, 1801
Emarginula tokuyamai IWASAKI

and ONO, new species
Pl. 16, figs. 3-5; Text-figs. 4, 5

Diagnosis.-Small.
antero-posteriorly
elongated patelliform gastropod, with
distinct anterior slit and with cancellated
surface ornamentation.
Description. - Shell
small, conical,
moderately elevated. Apertural shape679.

Setogawa Moll~~scs

113

anteriorly elongated elliptical, but somewhat quadrate like that of Scutu s. Apex
located at about two -thi rd back ofanterior margin pointing to rear. Shellalmost symmetrical bilaterally. Anterior
slope gently convex, but posterior slopeconcave near apex.
Slit present atanterior margin and distinctl y emarginated. Its length and width moderate
for the genus. Selenizone weakly depressed but distinct. Shell surface ornamented with fine radial ribs, cancellated with growth lines that regu larly
spaced and less elevated than the radialribs. No septal structure found on innersurface.
Muscle scar discontinuous
anteriorly, brancning pattern imperfectly
preserved (Text-fig. 5).
Measurements.-(in mm)
CM 8446
CM 8447
CM 84485mm

Text-fig. 4. Emarginula tokuyamai
I WASAK I and ONO, n. sp.

aText-fig. 5. Muscle sca r of Emal-ginula
tokuyamai I WASAKI and ONO. lIIustration
method by M AC CLI NTOCK (1963) .

Leng th
16.8
16.9
14.8

Width
9. 6
10. 2+
10.7

Hei ght
6.5 paratype/I
6. 1
6.5 ho]ot ype

R emark s.- Three specimens are examined for the description. They aremostly mold specimens, but original
surface ornamentation seems to be wellpreserved on their surface. This is thefirst record of Emm-ginula species fromthe Japanese Paleogene. Thus no comparable species is found in contemporaneous faunas. Emarginula hiranoae O ZAKI,1958 of th e Pliocene Na-arai Formation
is similar in shell size to the present
species, but is taller, more conical in outline, finer in surface ornamentation andnarrower in slit shape than the present
species. Moreover, the shell of E.
hiranoae is asymmetrica l, because theslit and the sculpture of seleni zone arebiased rightward from midline of shelllik e Loxotoma.
Two recent species,
Emm-ginula frag ilis YOKOY AlI;IA, 1920
which also occurs as fossils and E_
crassicosta SOWER BY, are distinguishable

114

Yasuhide IWASAKI and Susumu ONDfrom the present species in more posteriorly situated apex and round shell outline. Emarginula variegata A. ADAMS is
distinguishable from the present species
by its depressed shell height and rounder
outline.
The muscle scar of the present species
is open anteriorly, a fissurellid form of
MACCLINTOCK (1963), and narrow bridging scar is not observable partly due tothe ill preservation.
Judging from the impression of surface sculpture, the original shell of thepresent species seems to be thin likethat of E. fragilis. The species nametokuyamai is dedicated to Prof. A.
TOKUYAMA of the Shizuoka University
to whom the writers, especially ONO, areindebted for his useful suggestion on thegeology of the Setogawa Group.
Family Trochidae RAFINESQUE, 1815
Subfamily Solariellinae POWELL, 1951

5mm
Text-fig. 6.

"Minolia" ikebei (OZAKI, 1958).

not large in diameter. No callus developing on parietal region. Operculum unknown.
Measurements.-(in mm)

eM 8449eM 8450eM 8451eM 8452eM 8453eM 8454eM 8455
eM 8456

Height
7.5
7.1
9.0
8.5
7.9
8. 1
7.0+
8.3

Diameter
8.0
7.8
8.4
9.0
8.0
8.4
7.8
9.9

Numberof spires
4
5
5
5
4
4
3
4

Genus Minolia A. ADAMS, 1860

" ivlinolia" ikebei (OZAKI, 1958)
PI. 16, figs. 8-10; Text-fig. 6

Calliostoma ikebei OZAKI; OZAKI, 1958 March,p. 140-141, pI. 8, figs. 14, 15.

Minolia tsuchii OYAMA and MIZUNO; OYAMA
and MIZUNO, 1958 September, p. 2, pI. 1,
fig. 1.
Minolia tsuchii: OYAMA, MIZUNO and SAKAMOTO, 1960, p. 27, pI. 1, fig. 9.

Description.-A small turbiniform gastropod having four to five spires ofmoderate height. Six to eight distinct
spiral rib:; on roundly shouldered spire.
Body whorl having ten to forteen spiralribs that also distribute near umbilicus.
Suture distinct. No axial ribs observable.
Growth lines slightly prosoclinal. Aperture roun1~shaped. Umbilicus deep but

Remarks.-More than ten specimens
were collected, but eighCafe examined
and measured for the present study.
This gastropod from Ashikubo wasformerly named Minolia tsuchii by OYAMA
and MIZUNO. In the original descriptionof M. tsuchii, which was also subsequently reproduced by OYAMA, MIZUNO andSAKAMOTO (1960), measurerilents of shellwere given in error. The correct values
should be ten times of the figures.
Calliostoma ikebei OZAKI wa:s originallydescribed from the Plioce,ne Na-arai
Formation. It is very similar in outline
to M. tsuchii and its type . specimen isornamented with spiral ribs which areseven in number on each spire and 17
on the body whorl. Calliostoma ikebei
has an umbilicus and turbinate base.
Thus, it is certainly congeneric with M.

679.

Setogawa Molluscs

tsuchii. Genus "Minolia" is more appropriate for that shell than genus
Calliostoma.
lvlinolia tsuchii is virtually indistinguishable from "Minolia" ikebei in shellmorphology except for slight large sizeof the latter.
Minolia tukiyosiensis(OYAMA and SAKA, 1944) in ITOIGAWA,SHIBATA and NISHIMOTO (1974) from the
Miocene Togari Formation of the Mizunami basin is one of the morphologicallyallied species, but is distinguishable insparsely spaced spiral ribs especially on
its base. "Lirularia" condoni (DALL,
1909) distributed on the opposite side of
the Pacific coast seems to resemble thepresent species.
The living species
Minolia punctata A. ADAMS is distinguishable from the present species in angularshoulder and in large and deep umbilicus.
.. Millolia" ikebei is traditionally regarded as a trochid species without description of operculum. Some paleontologists still consider it as a turbinid,
Homalopoma species, based on its overall shell outline. Further examination
will be required for the generic assignment.

Family Mitridae SWAINSON, 1831
Genus Mitra MARTYN, 1784
Subgenus Tiara Sw AINSON, 1831
Mitra (Tiara) sp. indet.
PI. 16, fig. 6; Text·fig. 7

Description.-Shell small for the genus,
fusiform in outline. Spire high. Suture
not depressed. Spire slope almost straight.
Body whorl large, more than a half ofshell height. Aperture narrow, somewhat broadened abapically. Siphonal
canal straight. Shell surface sculptured
with spiral threads without axial ribs.

115

Text·fig. 7. Mitra (Tiara) sp.
bar indicates 5 mm.

ScaleThree columellar folds apparent on the
inner lip. Crenulations on inner surfaceof outer lip unknown.
Measurements.-(in mm)
eM 8457
eM 8458
eM 8469

Height
13.0+
13.2+

9. 7

Maximum diameter

5.5
5.0
4.3

Rel7larks.- Three specimens were col·lected. They are mostly molds withpartially preserved surface sculpture.
Apical part of all specimens are broken.
The shell shape, fine spiral costae andcolumellar folds are characteristic andsuggest that this species belongs to Mitra(Tiara).
It resembles .Mitra Cfiara) isabella
Sw AINSON in surface sculpture, but ismore swollen in shell outline and muchsmaller in size than the latter. Specificidentification will be made when better
preserved specimens are obtained. It
resembles Mitra (Tiara) sp. from theNojima Formation (SHIKAMA and MAsuJIMA, 1969), but is less slender than thelatter.

Ya8'/,~hide IWASAKI and SU8umu OND

116

Family Conidae RAFINESQUE, 1815
Genus Hemiconus Co SSM ANN, 1889

Hemiconus sp. indet.
PI. 16, figs. 19, 20; Text·fig. 8

Description."-Shell small for the genus.
Conispiral in outline, with moderately
elevated spires. Five or six spires
observable, slightly coeloconoid. Spiredistinctly shouldered, without ornamentation on the shouider. Body whorl
more or less convex, without surface
sculpture. Aperture narrow, straight.
Test seems to be· thin.
Measurements.-(in mm)
eM 8460
eM 8461eM 8462eM 8463Height
15.0
17.0+
7.0
8.5

Maximum diameter
7.8
8.4 inner mold
4.5
4.6

"
"

Remarks.-Four specimens are at hand.
One specimen is external cast and therest are inner molds.
The present species is regarded as thesame with what was once listed as

5mm
Text.fig. 8. Hemiconus sp.

Conus sameshimai MIZUNO, MS (MIZUNO,1956), because one specimen with thatname stored in the Geological Surveyof Japan (MIZUNO'S specimen) is identicalwith the present materials. It is characterized by small shell and moderately
slender outline with no distinct surface
ornamentation. It is distinguishable from
Conus tuberculosus SOWERBY by its
smooth shoulder. Specific identification
is suspended until more completely preserved specimens are available.
Family Mytilidae RAFINESQUE, 1815
Subfamily Mytilinae RAFINESQUE, 1815
Genus Brachidontes Sw AINSON, 1840
Subgenus Hormomya MORCH, 1853

Brachidontes (Hormomya) sp.
PI. 16, figs. 16, 17; Text·fig. 9

Description.-Shell medium to small insize, mytiliform, posteriorly elongatedand more or less slender. Umbo notsituated at anterior terminal. Hinge line
short and weakly arcuated. Anterior
margin straight in young shell but slightly
concave in adult.
Lunule indistinct.
Anterior periphery almost vertical to thecommissure plane. Surface sculptured

Text-fig. 9.

Brachidontes (Hormomya) sp.

679.

Setogawa Molluscs

with fine radial striae bifurcated atmedian part of the shell. No septum
found on inner side of anterior terminal.
Hinge teeth unknown, presumably very
weak. Inner ventral margin finely crenulated.
Measllrements.-(in mm)
eM 8468
eM 8469

Length44.6
20.7

Height21. 8
11. 9

Inflation Valve
13.4
Left
7.5
Right

Remar/,s.-In addition to two specimens at hand, three more specimens in
the collection of the Geological Surveyof Japan were examined. The latter
seems to be the material as once listed
as Septifer sp. by MIZUNO (1956).
The smaller specimen, in which shellmaterial is preserved, has no internal
septum. The remainders including thosestored in the Geological Survey are moldspecimens without shell materials, andhave only weak impression of radial
riblets. The larger specimen (PI. 16 fig.
16) is deformed longitudinally, and shows
more slender outline. Text-fig. 9 is a
restored shell based on above mentioned
five specimens. Shell outline, surface
sculpture and absence of internal septum
suggests Brachidontes. The shell outlineof the present specimens, especially the
concavity of the antero-ventral side, resembles that of Brachidontes matchgarensis MAKIYAMA, 1934, though the size
is much smaller than B. matchgarensis.
The present species is also similar to B.
matchgarensis in the fine radial sculptureof shell surface, but the sculpture of theformer shows frequent bifurcation. This
sculpture is finer than that of B. (Hormomya) mutabilis (GOULD) which is aeM 8464eM 8465
eM 8466eM 8467

Length
52.4
54.2
26. 7
29.4

Height
70.0
56.3
30.1
40.5+

117

living species in the shore of the JapaneseIslands.
Modiolus (Braclzidontes) eleqllalzensis
WEA VER and PALMER, 1922 and M. (B.)
cowlitzensis WEAVER and PAL~IER, 1922
from the west coast of U. S. A .. and otherallied fossil forms to the present one
have coarser radial sculpture. Specificassignment is difficult, because the specimens are not in good state of preservation.
Family Limidae RAFINESQUE, 1815
Genus Lima BRUGUIERE. 1797
Subgenus Plicacesta VOKES. 1963
Lima (Plicacesta) sameshimai OYAMA

and MIZUNO, 1958
PI. 16, figs. 1, 15
Lima (Acesta) sameshimai OYA~IA and MIZU·NO; OYAMA and MIZUNO, 1958, p. 10, pI.
1, figs. 11, 12.
Lima (Acesta) sameshimai: OYA~IA, Mlzu:-,;oand SAKA:VIOTO, 1960, p. 126, pI. 35, fig.
1.

Description.-Shell moderate in size forAcesta group, subauricular and more orless ventricose. Anterior auricle almost
completely reduced and slight anterior
gape at antero-dorsal margin. Posteriorauricle ill defined, continuous to posterior shell. Radial ribs strong and wellelevated. Ribs round-topped in someindividuals but more or less sharply
ridged in others. Number of ribs 17 and18. Ribs distributed also on posteriorauricle. Inner surface undulated radiallyowing to strong elevation of ribs. Shell
presumably not thick.
Measllrements.-(in mm)
Inflation
9.0+
8.8
4.0
4.6

Number of ribs
17
17
18
17

-/alve
Right
1/

Left
Right

118

Yasuhide IWASAKI and Susum'u OND

Remarks.-More than ten specimens
were collected from several fossil aggregations. Among them, four specimens
were used for observations and measurements.
This species is characterized by coarse
and strong radial ribs which make adiagnostic feature.
Other Cenozoic
species of Plicacesta in the West Pacificarea have rather finely ribbed shells.
The present material is mostly moldspecimens. In some individuals, however, thin calcareous shell is preserved
and shows an apparent surface sculptureof original shell such as weak concentric
growth lines and imblications, but thehingement structure is not observed. In
comparison with other limid species,
this shell material appears to be theouter layer which is originally made up
of foliated structure of calcite. The
inner surface of this shell probably represents the boundary surface between
the outer foliated layer and the middle
crossed-lamellar layer. Neither muscle
scar nor hingement sculpture is therefore observable.
Family Cardiidae LA1VIARCK. 1809
Subfamily Protocardiinae KEEN, 1951
Genus ,Vemocardium MEEK, 1876
Nemocardiu71l d. iwafliense(MAKIY AMA, 1934)
PI. 16, figs. 2, 18

Description.-Shell moderate to smallin size for the genus, subcircular in outline, ventricose. Beak somewhat prominent. Posterior one third of shellsurface sculptured by fine distinct radial
riblets with numerous faint imblications.
Remainder of the surface smooth or
faintly sculpture with radial and growthlines. Hinge plate narrow. Inner ventral
margin finely crenulated.
Measurements.-(in mm)
Length Height InflationeM 8470
eM 8471

17.1
30.2

16.1
29.2

4.8
8.6

eM 8472eM 8473

18.8
18.2

17.6
18.0

5.6
5.8

Valve
Right
Right
+Left
Left
Right

Remarfls.-Four mold specimens andseveral fragmental external molds werecollected. The present specimens seemto have very thin shells. The shellmorphology and surface ornamentation
indicate the genus Nemocardium. They
are similar to Nemocardium samarangae(MAKIY AMA, 1934), a living species of
the Northwest Pacific, in the shell outline as well as thin test, but the former
has coarser sculpture on the posterior
slope. In comparison with N. iwakiensedescribed by MAKIY AMA (1934), thepresent specimens are smaller in size andless inflated. Specific identification isdeferred in the present study because of
the poor state of preservation.
Family Trapeziidae LANY, 1920
Genus Trapezium MEGERLE
von MVHLFELD, 1811
Trapezium d. jobanicum HATAI
and NISIYAMA, 1949
PI. 16, fig. 12

Description.-Shell sub trigonal in outline. Anterior border narrowly arcuated,and posterior border truncated. Ventral
margin broadly rounded. Lunule andescutcheon indistinct.
Shell surface
characterized by a ridge from umbo topostero-ventral corner. Surface has faintconcentric striations, but has neither
concentric lamellae nor radial ribs.

679.

Setogaw a jlt[oll1,~s cs

119Hinge teeth presumably of arcticoid
type, but not confirmable. Test moderately thick.
Measllremen ts.-(in mm)
CM 847-1
CM 8475

Length18. 6
16.-!

Hei g ht
15. 3
12.1

In fla tion Val ve
5. 0
Ri ght3.6
1/

Remar/,s.- Two specimens were collected, and two more alli ed ones arefound in the co llection of the Geological
Survey of Japan. The present specimens are di ff erent from T mpezium
bicarinatum (SCH UMACHER) in absence ofdistinct s urface sculpture and median
depression . It r esembles T . jobanicum
HATAI and NISIY AMA in shell outline,
but cannot be id entified because of thepoor state of preservation. T. modiolaeforme OYAMA and SAKi), 1944 from the
Tsukiyoshi Formation Q·f the Mizunami
basin di ffers from it in larger shell size
and more trapezifo rm shell outline.
Remarks on the other illustrated
specimens

Th yasira (Axinopsida) sp. PI. 16, fig. 7.
One small mold specimen \-vas collected.
U mbonal part is broken. Shell is somewha t fiat , round in outline. Height is
sli g htl y larger than length. Lunule isunkno 'vvn. Posterior area and ridge fromumbo to postero-ventral margin are
distinct. This shell is most likely tobelong to the genus Th yasira. Further,
the shell morphology coincides well withthe characteristics of Axinopsida KEE N
and CHAVA N, 1951, but specific identification cannot be made because of thepoorly preser ved specimen.
J\lJeasuremen ts in mm .- CM 8476, length,13.2; height, 14.7; inflation, 2.6; rightval ve.
Cms satina (Chattonia ) sp. , pI. 16, fig.
13 ; Text-fig . 10.

5mm

Te x t-fi g . 10.

Crassatina (Chattonia) sp .

One small specimen of suboval shape
was collected. It is characterized byfine and well defined concentric sculpture,a nd distinct posterior area. Posterior
end is somewhat truncated . Shell outline is of veneroid t y pe. Lunule andescutcheon are indistinct. Hinge structure cannot be confirmed.
Measurements in mm.-CM 8477, length,15.1 ; heig ht, 12.0 ; infiation, 4.1; right valve.

Cmssatella sp., pI. 16, fig. 11.
One small mo ld specimen of left va lve
was collected. Shell is subtrigonal in
outline with orthogyrate beak, acutely
round at anterior margin but somewhat
rostra ted posteriorl y and truncated at
posterior end. Hinge plate is triang ular
in shape, but dentition is indistinct.
Surface scu lpture is unkno wn.
Thegeneric assignment is based on shell
outline. Its specific position remains
indetermined.
Measurements in mm. - CM 8478, length,14.1 ; height, 10.5; inflation, 3.4; left va lve.
Cadella sp., pI. 16, fi g . 14.
One small mold specimen was collected.
Shell is elongated ovate in outline, notventricose. Beak is situated at one thirdfrom posterior end. Anterior margin issomewhat produced . Surface seems to
be weakl y sculptured \-vith concentric

120

Ya8uhide IWASAKI and SU8um't£ OND

striations. Hinge plate is narrow. The
present specimen is similar in shell outline to Cadella sp. of the Nadaki Formation of the Mizunami basin reported
by ITOIGAWA and others (1974).
Measurements in mm.-CM 8479, length,10.5; height, 7.6; inflation, 2.0+; left
valve.

Acknowledgments.- The writers are
greatly indebted to Prof. Toshio KIMURA,
Dr. Shizuo YOSHIDA of the Geological
Institute, University of Tokyo, and Prof.
Akira TOKUYAMA of the Faculty of
Education, Shizuoka University in thecourse of the geological study of the
Setogawa Group. They are also indebted
to Prof. Tetsuro HAN AI, Prof. Kiyotaka
CHINZEI of the Geological Institute, Prof.
Itaru HAYAMI of the University Museum,
both of the University of Tokyo for thepalaeontological study.
The senior
writer is thankful to Dr. Atsuyuki MIZUNO of the Geological Survey of Japan,
Dr. Ienori FUJIYAMA of the National
Science Museum, Tokyo, Mr. Minoru
NAKAMURA, director of the Mizunami
Fossil Museum, Gifu Prefecture for per-mission in examination of fossil specimens stored in their institutions.

References cited
H,HAI, K. and KOIKE, K. (1957): On somefossil Mollusca from Chiba Prefecture,
Japan. Japan. Jour. Geol. Geogr., vol. 28,
nos. 1-3, p. 77-90, pI. 4.
HONJO, S. and MINOURA, N. (1968): Discoaster barbadiensis TAN Sin Hok and thegeologic age of the Set ogawa group.
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ICHIKAWA, K. (1946): New fossil locality
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environs of Setogawa, Shida-gun, Shizuoka
Prefecture. Jour. Geol. Soc. Japan, vol.
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ITOIGAWA, J. and SHIBATA, H. (1973): Paleoenvironmental change and correlation
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---, - - and NISHIMOTO, H. (1974): Molluscan fossils of the Mizunami group.
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IWASAKI, Y. (1975): On two fossil molluscan
species from the Eocene of the Bonin

Explanation of Plate 16
Figs. 1, 15. Lima (Plicacesta) sameshimai OYAMA and MIZ(;:-;O, 1958, xl; fig. 1, CM 8465, fig.
15, CM 8464.
Figs. 2, 18. Nemocardium ct. iwakiense (MAKIYA:VIA, 1934), x 1.5; fig. 2, CM 8472, fig. 18, CM
8473.
Figs. 3-5. Emarginula tokuyamai IWASAKI and 01'0, n. sp., x 2; fig. 3, CM 8446, fig. 4, CM
8447, paratypes; fig. 5, CM 8448, holotype.
Fig. 6. Mitra (Tiara) sp., x 2; CM 8457.
Fig. 7. Thyasira (Axinopsida) sp., x 1.5; CM 8476.
Figs. 8-10. "Minolia" ikebei (OZAKI, 1958), x 2; fig. 8, eM 8450, fig. 9, C.rA 8449, fig. 10, CM
8451.
Fig. 11. Crassatella sp., x 2; CM 8478.
Fig. 12. Trapezium ct. jobanicum HATAI and NISIYAMA, 1949, x 1.5; CM 8474.
Fig. 13. Crassatina (Chattonia) sp., x 2; CM 8477.
Fig. 14. Cadell a sp., x 2; CM 8479.
Figs. 16, 17. Brachidontes (Hormomya) sp., xl; fig. 16, CM 8468, fig. 17, CM 8469.
Figs. 19, 20. Hemiconus sp., x 2; fig. 19, CM 8460, fig. 20, CM 8461.

IWASAKI and ONO:

Setogawa molluscs

Plate 16

14

679.

Setogawa Molluscs

Islands.
Trans. Proc. Palaeont. Soc.
Japan, N. S., no. 99, p. 143-155, pI. 13.
KOBAYASHI, T. and HORIKOSHI, M. (1958);
Indigeneous Aturia and some tropicalgastropods from the Miocene of Wakasa
in West Japan. Japan. Jour. Ceol. Ceogr.,
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MACCLINTOCK, C. (1963); Reclassification ofgastropod Proscutus FISCHER based onscars and shell structure. Jour. Pale.
ontol., vol. 37, no. 1, p. 141-156, pI. 20.
MAKIY AMA, J. (1934): The Asagai molluscs
of Yotukura and Matchgar. Mem. Coli.
Sci., Kyoto Imp. Univ., Ser. B, vol. 10,
no. 2, art. 6, p. 121-167, pIs. 3-7.
- - , MORISHITA, A. and ITOIGAWA, J. (1975):
Nihon.Chiho·Chishitsushi, Chubu·Chiho.
(Regional geology of Japan) Revised ed.,451 p., Asakura Shoten, Tokyo. (inJapanese)
MATSUMOTO, E. (1964): The Asagai.Poro.
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fecture, central Japan. Mem. Coli. Sci.,
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- - (1971): Oligocene molluscs from Seto·
gawa group in central Japan. Bull. Nat'l.
Sci. Mus., vol. 14, no. 4, p. 661-669, pIs.
1-3.
- - and HIRATA, M. (1972): Akebiconcha
uchimuraensis (KURODA) from the Oligo.
cene formation of the Shimanto terrain.
Ibid., vol. 15, no. 4, p. 753-760, pIs. 1, 2.
MIZUNO, A. (1956): A preliminary note on
the megafaunal zones of the Paleogene
in northwestern Kyushu, Japan. (Forcorrelation of the Paleogene formationsin Japan). Bull. Ceol. Surv. Japan, vol.
7, no. 6, p. 25-34, pIs. 1, 2.
. - (1973): Molluscan fossils of the Murogroup.-Present status of the study-.
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NAKAZAWA, K. (1973): Problems on the

Ashikubo (Okugumi)
Yazawa i:t-tR

121

Shimanto geosyncline. Ibid., o. 32-36. (inJapanese)
ONO, S. (1973): Slaty cleavages in the Paleo·
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OYAMA, K. and MIZUNO, A. (1958): On the
new forms of Paleogene molluscs fromJapan. Bull. Ceol. Surv. Japan, vol. 9,
no. 9, p. 1-18, pIs. 1-4.
- - , - - and SAKAMOTO, T. (1960): IIIus·
trated handbook of Japanese Paleogene
molluscs. 244p., 71pls., Ceol. Surv. Japan.
OZAKI, H. (1958): Stratigraphical and pale·
ontological studies on the Neogene andPleistocene formations of the Tyosi
district. Bull. Nat'l. Sci. Mus. Tokyo,
no. 42, 182+ 6 p., 24 pIs.
SHIIDA, 1. (1962): Stratigraphical and geotec.
tonic studies of the Paleozoic Chichibu
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terrains in the central part of the Kii
mountainland, southern Kinki, Japan.
Res. Bull., Dept. Ceneral Educ., Nagoya
Univ., no. 6, separate vol. 1, 58p., 10pls.
SHIKAMA, T. (1951): Paleogene Mollusca
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Trans. Proc.
Palaeont. Soc. Japan, N. S., no. 1, p. 13-16.
- - and MASUJIMA, A. (1969): Quantitative
studies of the molluscan assemblages in
the Ikego·Nojima formations. Sci. Repts.,
Yokohama Nat'l. Univ., Sec. 2, no. 15, p.
61-94, pIs. 5-7.
TOKUOKA, T. (1964): Preliminary report on
the Cenozoic Setogawa and Oigawa groups
in the central part of Shizuoka Pre·
fecture, Japan. Jour. Ceol. Soc. Japan,
vol. 70, no. 820, p. 1-11.
TOKUYAMA, A. (1974):
The Palaeogene
System, (Setogawa terrain). In TSUCHl,
R. ed., Geology of Shizuoka Prefecture,(Explanatory text, 1: 200,000 geologicalmap of Shizuoka Prefecture) p. 27-34.
(in Japanese)

J'5RfJf;: (~kd3'), Hahajima i#:ih, Takayama ii1IiJlJ, Ichinose mZifJi,

122

PROCEEDINGS OF THE PALAEONTOLOGICALSOCIETY OF JAPAN1m A ~ ~............................................ g§B3.~M~1:.:fiW<.Jtj-:// 7' =j :/ tl ~ :/Q)7};fp Cft.:fi1t.

Biostratigraphy, paleomagnetism and sedimentology of late Cenozoic sediments innorthwestern Hokkaido, Japan .................................... UJIIE, H., SAITO, T. et al.
Cenomanian foraminifera from northernmost Madagascar ............................ UJIlE, H.
Distribution of planktonic foraminifera in the Gulf of Mexico and Caribbean Sea· .......................... ... . ....... UJIIE, H. and HATTA, A.

mJII@ff."F$Q)ft.1t.:fiff.cnmtl:~:fL;g@Ff·.····································± ~.i-. ~*~TfjI"}!ft'f JII Lepidocyclina jlittt!!Q)nmtl:~:fL;g.................................... rx*~T . ±JIi-

g§~~ijl~~¥i9PQ)7c~~:fL~t~~~,<c ................................................. ···r~1L~~

The ecology of ostracod faunas in the Hamana Lake region ................... .
........................ IKEYA, N., HANAI, T. and SEKIGCCHI, Y.
Denticula nicobarica Group Q) 3 ~fil! (D. ikebei, D. kanayae :to J: Lr D. paranicobarica)c Denticula kanayae Zone t~~~'<C ................................................. ·f:Jc~Jttil
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tt~Jttil~tna~~~tJ:$~~~~g[~~IE~~~}(idoa ............................................ ~,*1~Palynological study of the deposits in Lake Biwa, Central Japan. 1: Pollen analysis
on the samples selected at 5 m interval of a 200 m core ..................... .
· ........................... FUJI, N., HORIE, S. and KAXEDA, K.
-,¥Jjj(~ili!!~ff.t~g[1±l L.t.: St!xegothaea !:in (.... =\'-";fl/-) Q)t:!i~t~~~'<C ......................... ·r~~3'i1*B
Some coniferous remains from the Palaeogene Noda Group, Iwate Prefecture, Japan(Part 2) ...................................................... KIMURA, T. and HORIUCHI, J .
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A calcitic sclerosponge from the Ishigakishima coast, Ryukyu Islands, Japan andits fossil relatives ........ , ....... , ............... , .. " ..................... , ....... MORI, K.
Stromatoporoids from the Silurian of the Oslo Region, Norway ...................... MORI, K.
fOr.rxlll!!jH~~!1!!~t~7};fp-:fo~m@g[I±lQ)~MJlllJlMt~~~'<C('f¥ll) ..................... .

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9P'ilIl.:x.1"@ff.Q) Scaphites ffll~~~'<C--t:-Q)7};fpc~~ff.~IH;IlnX:- , ......................... jjJ)J$-nX:

Note on Anagaudryceras sacya form the Diego.Suarez area Madagascar ............ HIRANO, H.
A new texanitine ammonite from Hokkaido .............. MATsu~1oTo, T. and HARAGUCHI, Y.

123
An occurrence of Ordosoceras in Jehol and a note on the Polydesmiidae ...... KOBAYASHI, T.
New Tertiary Sepiid from Chichibu Basin, Japan ........ OBATA, I., OGAWA, Y. and OISHI, T.
Living specimens of Nautilus macromphalus SOWERBY from New Caledonia ......... .
...................................... OBATA, I. and MIKA~"', S.
Nine month.rearing procedures of Nautilus macromphalus SOWERBY in the Yomiuri
Land Marine Aquarium, Tokyo ...... KANIE, Y., DEGUCHI, Y., OKUTANI, T. and MIKA:\H, S.
A juvenile macromphalus shell drifted on the shore of I. Amedee off Noumea,
New Caledonia ...................................... HAMADA, T., HABE, T. and MIKA~I1, S.
A fundamental assumption on Nautilus habitat condition and its application to
the rearing of N. macromphalus ............................... . HAMADA, T. and MIKA;\.JI, S.
Distribution and some possibly ecological barriers of Nautilus species ............ HAi\IADA, T.
SEM observation on the cirri of Nautilus macromphalus ... ........................ .
............. ..' ..... FUKUDA, Y., OBATA, I. and KA,,"A~IOTO, N.
Oral and digestive systems of some cephalopods with special reference to thoseof N. macromphalus ......................... . FUKUDA, Y., KAWA~WTO', N. and OKl'TA:\"I, T.
l/iI\f4;lIW¥J.JftE~~IH;c. J: 7.> tl~~f¥ffJT(7)-f9iJ .............................................. *#.tJlli¥=*1IE:~(7)""fmOi~t7) ¥!.ftEt;c. "?~ '-C..................................................... ·t~,!lI;~~...............'............................. ·~tt ft't
Vicarya Hii(7)1=.RRff:~I¥.J~W ................................................. ·tf!l!f=:J'li>· !l!fEE~R]
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Some late Triassic Bivalvia and Gastropoda from the' Domeyko Range of north Chile...................... HAYAMI, I.,MAEDA, S. and FULLER, C.R.
,!lI;:&w.i1!'i$t1iiI=l~g€(7)""f'illW "- 7*C=ttm;c.,,?~,-c .......... · ... · ....... J!71\. fI}. =J::.~. '8J11~W""f$B:!II!*'8tlJi2'1~g€(7)~ffi!.ftEt;c."?~'-C(-tt7) 1. Neritacea, Amberleyacea) .............. tmif/i:l;(:lfInoceramus schmidti t;c.~1=.-t 7.>~JW~ ffi!. AnisomYdn giganteus (7)1=.rg~* ...... ~iIJJJt:J'f: • J!71\. fI}
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the Otadai Formation, Chiba Prefecture .......................... HATTA, A. and MAEDA, S.

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Palaeontological Society of Japan

Special Papers No. 20

Devonian Trilobites of Japanin comparison with Asian, Pacific and Other Faunas
By Teiichi KOBAYASHI and Takashi HAMADA
Issued January 31, 1977; 202 pp., 13 pIs.

Price (postage and handling included) U. S. $. 24.00
This is the second outcome of a series of studies on the trilobites from Japan, following"Silurian Trilobites of Japan" (Spec. Pap. No. 18, 1974) by the same authors.

It contains thesystematic descriptions of Devonian trilobites from Japan, based mainly on new collections,consisting of 28 species of 18 genera in 9 families, of which 13 species and 2 subspecies arenew.

Certain families and genera are discussed at length, with the establishment of a new

genus in the Scutelluidae and a new subgenus in the Cheiruridae.
Notes are given of the age and correlation of the trilobite-bearing beds.

Furthermore, theknown Devonian trilobite faunas of Eastern Asia, South Asia, Siberia, Turkestan, Australia
and the Americas are extensively discussed in comparison with those of Japan.

As a result

a new scheme is proposed for the Devonian trilobite biogeographic provinces.

Palaeontological Society of Japan

Special Papers No. 21

Mid-Cretaceous Events-Hokkaido Symposium, 1976
By Tatsuro MATSUMOTO et al.
Issued May 10, 1977, vi+251 pp., 3 pIs.

Price (postage and handling included) U. S. $. 20.00
This is the proceeding volume of the second international conference of "Mid-Cretaceous
Events" held in Hokkaido from August 29th to September 6th, 1976 as an activity of the
IGCP [International Geological Correlation Program] project.
Altogether 18 papers of 20 authors are assembled.

The contributors are R. A. REYMENT,N. A. MORNER, M. COLLIGNON, J.A. JELETZKY, M.A. PERGAMENT, C. W. WRIGHT, J.M.
HANCOCK, W.J. KENNEDY, P. JUIGNET, E.G. KAUFFMAN, A.A. KURESHY, Y. TAKAYANAGI, S.
MAIYA, M. OKAMURA, I. OBATA, M. FUTAKAMI, Y. KANIE, H. HIRANO, K. TANABE and T.
MATSUMOTO.

Each of these papers has concentrated on one of the following three major

problems: (1) Cretaceous micro- or macro-biostratigraphy or history of the areas around thenorthern Pacific; (2) interregional correlation; (3) the problem of Cretaceous transgressions
and regressions.

This volume is, thus, indispensable for geological libraries as well as persons

who may have interests either in academic or applied aspects of the Cretaceous events andrelevant affairs.

The Special Papers are on sale at the Society.

Orders must be accompanied by remittancemade payable to Dr. Kametoshi KANMERA, Editor of the Special Papers, PalaeontologicalSociety of Japan, c/o Department of Geology, Faculty of Science, Kyushu University, 33,
Fukuoka (Hakata) 812, Japan.

The following backnumbers are also purchasable from the sameoffice as mentioned above.
Number 9 (Issued Dec. 15, 1962) Bibliography of Japanese Palaeontology and
Related Sciences, 1951-1960. Compiled by Fuyuji TAKA! .................. U.S. S. 18.00
Number 11 (Issued Feb. 20, 1966): The Echinoid Fauna from Japan and AdjacentRegions. Part I. By Syozo NISIYAMA ...................................... U. S. S. 33.00
Number 12 (Issued Sept. 20, 1966): Postcranial Skeletons of Japanese Desmostylia.
By Tokio SHIKAMA.. ... .. .. .. .. .. . ......................................... U. S. S. 17.00
Number 13 (Issued March 16, 1968): The Echinoid Fauna from Japan and
Adjacent Regions. Part II. By Syozo NISIYAMA ............................ U. S. S. 26.00
Number 15 (Issued Feb. 25, 1971): Early Devonian Brachiopods from the Lesser
Khingan District of Northeast China. By Takashi HAMADA ................ U. S. S. 17.00
Number 16 (Issued Dec. 25, 1971): Tertiary Molluscan Fauna from the Yakataga
District and Adjacent Areas of Southern Alaska. By Saburo KA:,\NO ...... U. S. S. 18.00
Number 17 (Issued Nov. 30, 1973): Revision of Matajiro YOKOYAMA'S Type
Mollusca from the Tertiary and Quaternary of the Kanto Area.
By Katura OyAMA .......................................................... U.S. S. 20.00
Number 18 (Issued Nov. 30, 1974): Silurian Trilobites of Japan in Comparison
with Asian, Pacific and Other Faunas. By Teiichi KOBAYASHI and
Takashi HAMADA .......................................................... U.S. S. 17.00
Number 19 (Issued Feb. 10, 1976): Bivalve Faunas of the Cretaceolls Himenoura
Group in Kyushu. By Masayuki TASHIRO .................................. U.S. S. 14.00(Numbers I, 2, 3, 4, 5, 6, 7, 8, 10 and 14 are out of stock.)

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Transactions and Proceedings of the PalaeontologicalSociety of Japan

New Series No. 106

June 30, 1977

CONTENTS
TRANSACTIONS
675.

KaNDA, Isao, MATSUOKA, Kazumi, NISHIMURA, Akira and OHNO, Terufumi:
Nummulites boninensis HANZAWA from the Amami Plateau in thenorthern margin of the Philippine Sea.. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 61

676. TAKAHASHI, Kiyoshi: Palynology of the Lower Tertiary Concepcion Formation, central Chile.................................................. 71677. IGo, Hisayoshi and IGo, Hisaharu: Upper Permian Fusulinaceans containedin the pebbles of the basal conglomerate of the Adoyama Formation,
Kuzu, Tochigi Prefecture, Japan...................................... 89678. HIRANO, Hiromichi and SANa, Hiroyoshi: Middle Jurassic ammonites from
Bisho, Kumamoto Prefecture, Kyushu ................................ 100
679. IWASAKI, Yasuhide and ON 0, Susumu: A molluscan assemblage of the
Setogawa Group ...................................................... 106
PROCEEDINGS ................................................................ 122