Transactions and P roceedingsof thePalaeontological Society of Japan
New Series

No. 73

Palaeontological Society of japan
A pril 30th, 1969

Editor : Tokio SHIKAMA
A ssociate Editor: Ki yotaka CHI NZE l and Nori y uki IKEY A

Officers for 1969- 1970
Honorary President :President :Hisakatsu YABEFuy uji T AKAICouncillors (*E xecuti ves ) :Ki y oshi ASA NO*, Tetsuro H ANA!';' (Secr etary ), Kotara

H ATAI, Ita ru H AY AMI, Koichiro ICHIK AWA, Taro K ANAYA , Kametoshi KA N·
MERA, T e iichi KOBAYASHI, Kenji KONISH I, Tamio KOTAKA, T a tsuro MATSU·
MOTO*, Masa o MrNATO, Hiros hi OZAKI* (T reasurer ), Tokio S HIKAMA*, Fu y uji
T AKA!*
Exec uti ve Committee (Cha irman:
Gen eral Affa irs:

F uy uji TAKA!)

T etsuro H ANAI, T a kashi HAMADA , Yasuhid e IwASAKIMembership : T akashi HAl\'lADA
F ina nce :Hiroshi OzA KI , Saburo KANN O

Planning:

Hiros hi OZAKI, Hiroshi U]ll E

Publications
Transac tions:

To k io S r-l!KAMA , K iyotaka Cr-II NZEI, Nori yuki IK EY A

S pecial Papers : T a tsuro MATSUMOTO, T omo wo OZA WA" Fossils " :K iyoshi ASAN O, Yokichi T AKAYANAG I

F ossils on t he cove r is Globo rotalia lruncatulinoides (o'ORBIG NY , 1839).
The photog r a ph was ta ken on a scannin g electron microscope, ]EOL- ]SM- 2, X 100.

A ll communications r elating to this journal should be a ddressed to the
PALAEONTOLOGICAL SOCIETY OF JAPAN
Geological Institute, Faculty of Science, University of Tol<y o, Tokyo 113, japan

Trans. Proc. Palaeont. Soc. Japan, N.S., No. 73, pp. 1-25, pls. 1-2, April 30, 1969

548. FOSSIL SPORES AND POLLEN GRAINS FROM THE
NEOGENE DEPOSITS IN NOTO PENINSULA, CENTRAL JAPAN-I
A PALYNOLOGICAL STUDY OF THE LATE MIOCENE
WAKURA MEMBER*
NORIO FUJI
Institute of Earth Science, Kanazawa University, Kanazawa

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Suzu, Wajima areas.
The present writer has been studying
the fossil pollen grains and spores foundfrom the diatomaceous deposits of Neogene age in the Hokuriku region since1960. The present article is the firstreport on the palynological researchesof the diatomaceous deposits and treats
the pollen grains and spores collectedfrom the Late Miocene Wakura Member
near Nanao City in the central part ofNoto Peninsula.
The scope of the investigation basedon the microfossils is the systematic
determination of the microfossils, thepalaeoclimatic condition and palaeogeographical environment under which the
Wakura Member was deposited in the
Late Miocene. Further, correlation andcomparison of the conditions and environment of the Wakura Member with
the Hijirikawa, Tsukada and I'izuka
diatomaceous Members distributed in thecentral and northern parts of Noto Peninsula are also undertaken.

Introduction
Some diatomaceous deposits occur atdifferent stratigraphical horizons in the
Tertiary (Neogene) System distributedin the northern and central parts ofNoto Peninsula, Ishikawa Prefecture,
Central Japan.
The diatomaceous deposits of Noto
Peninsula are classified into four hori. zons, ranging from the Middle to Late
Miocene in age. These four horizons
differ from one another in their environmental conditions, namely, one is nonmarine in origin, whereas the otherthree are marine. The most conspicuous
horizon is represented by the marine
diatomaceous mudstone of the Late
Miocene age. The diatomaceous deposits
in Noto Peninsula are distributed inmain three areas of Nanao-Nakajima,* Received Sept. 30, 1968; read November
18, 1961, at the 80th Meeting, the Kyushu University, Fukuoka; contribution from the Institute of Earth Science, Faculty of Education,
Kanazawa University, New series No. 7.
1Norio FUJI

2

Acknowledgements

The writer takes this opportunity to
express his deepest gratitude to Professor
Kotora HAT AI of the Institute of Geology
and Paleontology, Faculty of Science,
Tohoku University, for his advice during
the course of the writer's palynologicalinvestigation and for reading the manuscript. Appreciation is expressed to Professor Yoshio KASENO of the Instituteof Earth Sciences, Faculty of Science,
Kanazawa University, for his suggestions
and informations on the stratigraphy
and tectonic movements in the Nanao
area during the Late Miocene stage.
Thanks are due to Mr. Tomohide NOHARAof the University of Ryukyu and Yukio
KITAMURA for their suggestions on thestratigraphy and sampling. Finally, thewriter expresses his appreciation to the
Ministry of Education of the Japanese
Government for grants from the Science
Expenditure Funds.
Outline of the Geology

Many diatomaceous mudstones of Neogones age are distributed widely in thecentral and northern parts of Noto
Peninsula. They are mainly composedof homogeneous silty mudstone characterized with the dominance of fossil
microorganisms. In the central part ofthe peninsula, the diatomaceous deposits
are distributed locally, and their rockfacies are variable, especially around Mt.
Sekid6-san near Nanao City. In thenorthern part of Nanao the Neogene
deposits which overlie the Anamizu
Andesite Group with unconformity areclassified into six members in ascendingorder as follows : the Akaura sandstone,
Nanao calcareous sandstone, glauconitic
sandstone, Wakura diatomaceous mud-stone and Kojima sandstone Members
overlain with unconformity by Pleistocene deposits.
These strata are distributed in andaround Wakura and in the adjacent areasof Nanao City in the central part ofNoto Peninsula. Each stratigraphic units
is below, in ascending order.
The Anamizu Formation: This formation is distributed locally along thewestern coast near Wakura and also in
the area south of Okuhara. It is generally clas~ified into two parts, namely,
one is of pyroxyne andesite or hornblende pyroxyne andesite, and the otherconsists of andesitic pyroclastic rocks
intercalated with dacitic tuff layers.
This formation may be Early Miocene
in geological age.
- -- unconformity
The Akaura s;;tndstone Member: In
areas of Nanao, Takahama and Mt. Bij6zan, an arkose sandstone derived from
granite, which may be correlated with
the Hida metamorphic complex, is distributed widely. It is named the Akaura
sandstone Member near Nanao City.
This member consists of a yellowish
gray coarse-grained sandstone with
granule sandstone showing remarkablecross lamination structures. The member has yielded a fossil mollusc as
Patinopecten kagamianus pennirus. The
thickness of this member is about 200
meters.
- - interfigering with the upper
part of the Akaura Member-The Nanao calcareous sandstone Member: The upper part of the Akaura
Member interfigers with the calcareous
sandstone, which is named the Nanao
calcareous sandstone Member. Thismember occurs locally at I waya, Hosoguchi and Osugi-zaki in the limits ofWAitUftA

-f-

spj,

•

37"N

(
0
·'
ICANAbWA

I37"E0<:.>.,
-~--

?a

1000
M

~
0
4

LEGENDo~~~r_,.,

~2
L~
~

§_d3

,--J

I

~4

[Z]
~

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R.

~

"';;s

~
0
;::1

.,....

;:::,...

5"'>
rn++ls ~t±ti:±J "';;s0<Q[[]} "'~01~~]9Fig. 1. Geological map of the Nanao area, central part of Noto Peninsula, Japan (Compiled by Y. KAsE;--;o, 1963; after N. Ft.:JI,
T. AoKI, Y. KITAMURA and I-IoKuHIKU QuATEI<NARY RESEARCII GROUP). 1: Holocene deposiL;, 2: Pleistocene deposits, 3: Kojima
siltstone Member, 4: Wakura diatomaceous mudstone Member, 5: glauconitic sandstone, 6: Nanao calcareous sandstone Member, 7:
Akaura sandstone Member, 8: Andesite and andesitic pyroclastic rocks, 9: sampling localities.

~~0.,....
0I.......

c".::..

Table 1.

.----

Correlation table of the Neogene Tertiary diatomaceous deposits distributed in Noto Peninsula, Central Japan.
"· diatomaceous deposits.
--

GeologicalAge-----,

Standard stratigraphic
stratigraphic
division indivision of the oilfields in
Hokuriku Region
North Japan
Standard

Shibikowo

Honyu

Wokimoto

Himi

Hijirikawo

Nakajima

area

area

11111111 [ llllliiTllllll

Pliocene

Wokura -Notojimo

area

Suzu

area

I

1111111111111111111111111

OgijimaKojimaOginoyoAkosoki

KitouraI

Otogowa"Hijirikawo

Middler----EarlyI

Higoshibessho

Hareglauconite

glauconite

Tonokumo~noo calcareous"lido diotomoeeous
mudstonemember"

Doijimosandst.

~Kurosedoni"Hojuji

Hamadadiet. mst. m."

AkauroHigoshHnnoi

Araya

Kusold'bro1odci

Nonohora

l.ill
lwoineAnamizu

0"':lShingu--~-----~-~--

Miocene~"lizuko""Kososhio"

MioceneNishikurosowo.,,"Wokura"Funakowo

Onnogowa

~

\

!
Late
MioceneAnomizu\

Yanagida
1-----Anomizu
--~

~
.....

548.

Spores and Pollen from the Neogene of Nota-lNanao City. Most of the sandstone
member consists of granule and coarsegrained sandstone.
Fossils are very
abundant, namely, sponge spicules, bryozoa, smaller foraminifers as Nonion pompilioides, Angulogerina hughesi, Cassidulina margareta, Cibicides sp., Fissulina
sp., Lagena apiopleura, Nonion nicobarense, Rotalia sp., Uvigerina sp. etc., molluscs as Patinopecten kagamianus permints,
lv!iyagipecten
matsumoriensis,
Nanaochlamys notoensis, Chlamys crassivenia, brachiopods as Terebratella cor.eanica, T. gouldi, Terebratulina japonica,
T. crossei, T. peculiaris, Terebratella nipponensis, Laqueus rubellus, Coptothyris
grayi, and Hemithyris psittacea etc. are
known to occur.
--conformity-The glauconitic sandstone Member:This member is distributed in the Sakiyama, Nanao and Noto-jima areas. It
represents the earlist phase of the Otokawa stage of which age is considered
to be the Middle Miocene generally consists of a glauconitic sandstone, in which
flinty shale is intercalated and this suggests an interruption of sedimentation
or a diastem. These glauconitic sandstones or shales are thought to have been
deposited on a shallow sea bottom andthey have yielded abundant remains ofa silicisponge such as Aphrocallistes sp.
and a mollusc called Chlamys crassivenia.
--conformity-The Wakura diatomaceous mudstone
Member: This member has been studied
by Takuji OGAWA (1908), Yanosuke
0TUKA (1935) and Yoshio KASENO (1963)
from the viewpoint of stratigraphy.
The Wakura Member is distributed locally in the areas of Wakura, Okuhara
and Ishizaki in the northern part of
Nanao City. The Entsunagi mudstone
Member, which is rlistributed at Han'no-5ura, Suso, Sanami and Koda of Notojima Island near Nanao City, coresponds
to this member. The rock-facies is generally a homogeneous yellowish brown
on a weathered surface and a bluishgray on a fresh surface diatomaceous
mudstone. The fossils from the member
are diatoms as Actinocyclus fios, Actin aptychus senarius, Arachnoidiscus ehrenbergii, Coscinodiscus subtilis, C. lineatus,
C. marginatus, and Stephanopyxis turris,sponge spicules and pollen grains. Thismember is about 80 meters in thickness .
The member developed in the Wakuraarea forms a small basin structure.
---unconformity--The Kojima sandstone Member: The
member is developed locally in the mapped area, that is, it is distributed fromnear Kojima and Iwaya to the northwestof the Nanao Station. This sandstone
member overlies with unconformity the
Akaura sandstone and Nanao calcareous
sandstone Members, and is a light bluishgray or grayish yellow silty sandstone
containing abundant remains.
Fossilmolluscs from the member are such as
Turritella saishuensis motidukii, Neptunea sp., Epitonium angulatosimile, Denlatium sp., Pecten spp., Astarte halwdatensis, Cardium, sp., and foraminifers as
Angulogerina hugesi. This member attains about 100 meters in thickness.
---unconformity- -The Quaternary deposits of this district are classified into five units, namely, the Takashina, Okuhara, Nishiminato,
Tokuda gravel Members and Holocene
deposits in ascending order.
The Takashina Member which yieldedsuch marine molluscs as Cerilbideo psillacingulata, C. djadjariensis and Tegillarca
granosa var. in its middle horizon may
be correlated with the Kamitako Member(Middle Pleistocene) in the Himi district

Norio FU]l6of Toyama Prefecture. It is noteworthy
that the marine environment during the
Middle Pleistocene along the japan Sea
coast is well represented in the Takashina Member.
The Okuhara Member including the
Wakura-eki shell bed is classified into
two members, that is, the lower or mud
submember and the upper or sand submember. Marine molluscs as Scapharca
satowi, Dosinella penicillata and Paphia
undulata, and marine diatoms such as
Coscinodiscus were found from the lower
submember. A study of the deposits
reveals that there occurred cme major
marine transgression which attained amaximum rise of 50 meters above thepresent sealevel during the Late Pleistocene, probably due to the glacial eustatic
movement called the Hiradoko phase in
the Hokuriku region. This phase can becorrelated with the Shimosueyoshi phaseof the Kwanto region, Central japan.
The Nishiminato Member is divided
into two submembers: the lower or mud
and upper or sand submembers. The
lower part of the mud submember preserves wood stumps and plant remains
as Trapa macropoda, Alnus japonica andjuglans mandshurica, which indicate amarsh environment. Molluscs and diatoms of marine origin are found in theupper part of the mud submember, which
may be correlated with the lower partof the Okuhara Member.
The Tokuda ·gravel Member is a nonmarine deposit, the age of which is
judged to be the Latest Pleistocene(Wiirm glacial age).
Palynological Research(1) Foreword
As already stated different ki,nds ofdiatomaceous deposits occur in the Noto
Peninsula, and there have yielded abun-dant microfossils as diatoms, flagellates,
foraminiferes, pollen grains and spores_
Although several papers have been published on the deposits, there were concentrated to stratigraphical investigations, and no literature has appeared
concerning the fossil pollen grains andspores until comparatively recently. The
writer has been studying the diatomaceous mudstone members, and previous works have been summarized(FUJI, 1964, 1966 & 1968) on the Early
Miocene Yamatoda, Middle Miocene Hojuji and l'ida, and Late Miocene Hijirikawa, l'izuka and Nakayama-toge Members.
The purpose of the present study is
to interpret the significance of the pollen
grains and spores from the samples collected from the Late Miocene Wakura
Member, mainly in· terms of palaeoclimatic condition and palaeogeographicalenvironment. These records, which arethought to reflect, in a relative mannerin general, the fluctuation of atomospheric temperature in the southernpart of Noto Peninsula during the Late
Miocene to Pliocene, is based on thecriteria gained by the writer during his
about ten years palynological researches_
The samples taken by the writer incollaboration with NOHARA and KITAMURA, serve as an example for the application of the criteria for the pollen
grains analysis of the samples fromCentral Japan.
(2) Sampling, Preparation of Materials
and Method of Study
Among the samples analysed six (Sample nos. 1-6) were collected by the writer,.
KITAMURA and NOHARA in the summer
season of 1961. . The other samples (7a7c and 8a-8g, ten samples in total) wereobtained from two wells drilled for the
research of the diatom earth distributed

548.

Spores and Pollen from the Neogene of Noto-I

7

D
[[]]
~

•rn
•

2
3
4

5
6

0

7

0

10

km
20

Fig. 2. Geological outline of Noto Peninsula and distribution of diatomaceous deposits (After W. IcHIKAWA & Y. KAsENO, 1963). 1: (denotedby a few spot) Pliocene series, 2: Upper Miocene series, 3: Middle Miocene
series (sedimentary rocks), 4: Middle Miocene series (pyroclastic rocks),
5: Lower Miocene series, 6: Pre-Tertiary system (granite & gneiss), 7:
diatomaceous deposits: Z: l'izuka Member, T: Tsukada Member, W:
Wakura Member, D: !'ida Member, H: Hojuji Member, Y: Yamatoda Member.

widely in Noto Peninsula. The sampling
localities and stratigraphical horizons in
the Wakura Member are shown in Figs.
1 and 3.
Of the sample collected from outcrops,
one sample consisted of three to fivepieces of rock ever collected at random
along the length of one meter, measured
parallel to the stratification of the member. These rock pieces were mixed
together to form a composite sample,
which is taken here to represent the8

Norio FUJI··············humus..... coarse Okuhara Mem.

grained sand.. ·_:.- ··· ···-··· medium - grained sand..... ---Lebensspuren
bluish gray mud intercalatedwith thin fine-g. sandand fossil beds
Sample6

Sample5

Sample 8odark greenish

gray diatomaceous

mudstone

Sample 4
Sample Bb
Sample Be
Sample 7a
Sample 3·Bd
SampleSampleSampleSample

7b
Be
7c
Bf

Sample Bg
Sample 2

SampleI

Glauconitic
Akaura Mem.

Fig. 3.

Columnar section showing the sampling horizons of the Wakura
diatomaceous mudstone Member.

outcrop. The present study is based on
the composite samples. Many rock samples and separate specimens for refer·ence at the writer's disposal, materiallyfacilitated the present work in checking
the distribution and confirming the identification of the pollen grains and spores.
The analytical procedure of the sam-pies is the same as was stated previously
by the writer (FUJI, 1965). The composite samples were treated by the
NaOH-HF-acetolysis method.
To record the position of a specimen
in the slide for taxonomical and biostratigraphical studies, Maltwood's finder orEngland finder were used to register the548.

Spores and Pollen from the Neogene of Noto-I

necessary specimens in this investigation.
The specimen registered in this study
can be easily brought under the microscopic field whenever necessary by placing the slide which includes the specimen registered with the finder. The
counting is made along the chosen lines
with use of a mechanical stage andfinder. All of the specimens which appeared while traversing the slide along
the chosen line are observed and counted. The counting is continued until 200
specimens are identified and counted.
When the specimens counted from one
slide are less than 200, the counting is
proceeded on another slide preparedfrom the same sample to count a total
number of 200. Therefore, more than
10 slides must be prepared from eachsample to count 200 specimens.
The frequency of each genus obtainedby the count of 200 specimens fromevery sample is recorded on the distributed diagram. All of the stream slides
are examined under the same magnification of 600 times in counting.
The slides counting the registeredspecimens are deposited in the collectionof the Institute of Earth Science, Faculty·Of Education, Kanaza wa University (register abbreviation: EKZJ), Kanazawa
City, Ishikawa Prefecture, japan.
{3) Description of the Pollen and Spore
Assemblages(a) General Statement
The present flora is composed of thespecies which are adapted to the physical phenomena which constitute theenvironment. But the fossil assemblageof any locality may be the total accumulation composed of a biocoenosis
andjor a thanatocoenosis. Therefore, tointerpret the geological and palaeoeco-

9

logical significances of the fossil assemblage it is necessary to make an analysisof the fossil composition from the viewpoint of the presence or absence, abundancy and distribution of every climaticelement to know the palaeoclimatic condition and palaeogeographical environment at the time of deposition.
(b) Stratigraphical Relations of the
Samples
The localities of the samples studied
are widely distributed in the present
field and the depths from the surface inthe wells drilled may be correlated tothe exposures on the surface. They canbe illustrated as a columnar section andfor the sake of convenience are calledhorizons in this work. Here, the termhorizon is used to denote the same ornearly same stratigraphic position orlevel within the stratigraphic unit.
The samples analysed in the present
work can be classified into 13 horizons
shown as the columnar! section (Fig. 3).
(c) Description of Assemblages
The assemblage of the fossil pollen
grains and spores found from the analysed 16 samples is shown in Figs. 4-8,
and is explained as follows in ascendingorder.
Sample 1: This sample which belongs
to the lowermost horizon of the W akura
Member. It yielded, Gymnosperm-fourgenera and one family; Dicotyledon-12
genera and two subgenera; Monocotyle·don-two families and one genus; and 4
genera of spores. Among them, Pinus
and Gramineae are abundant, 11% in
frequency, being the highest concentration in this composite sample. Quercus(evergreen), this genus includes two
types, one is of large size and the otherof small size based on the diameter ofgrain, the latter belongs to the evergreen

Norio FUJI

10

6%. Gymnosperm appers with a highrate of 23%, and Dicotyledon, Monocotyledon and Pteridophyta are respectively
type, and attains 6%. juglans and Myriophyllum are common, both being about

46%, 14% and 29%. Metasequoia, Cunninghamia, Glyptostrobus, Taiwania, theevergreen Quercus and Liquidambar are
the representative plants of a warm
temperate and subtropical region and

Larix
Talodioceoe

Fagus

50/ix

Celtis

Bi:'iUia
Juglans
Pterocoryo
Cary/usAcer·casianea
Coryo
Zelkovo
Menyonlhes

Styrax. "iiyri0Phyllum
Carpinus
Tilio

Fig. 4.

Pollen diagram (1) of the Wakura diatomaceous mudstone
Member. Numbers refer to Figs. 1 and 3.

-

~

...

Fig. 5.

=-""-=-:Pollen diagram (2) of the Wakura diatomaceous mudstone Member.
Numbers refer to Figs. 1 and 3.

548.

Spores and Pollen from the Neogene of Nota-l

are denoted by " B " in Fig. 6. Pinus,
Tsuga, Taxodiaceae without the warm
elements mentioned above, the deciduous
Quercus, Zelkova, Fagus, Salix, juglans,
Castanea, Tilia and !lex are the repre-

sentative plants of the temperate to cooltemperate regions analogous with the
Hokuriku region (indicated by "C" inFig. 6). Also admixed in the composite
sample are Abies, Picea, Fagus, Betula
etc., the representative plants of thecooler to cold regions (indicated by" A"
in Fig. 6!. According to the result, "A "appeared with a very low frequencyof 7'}{; in total. On the contrary, theplants of the warmer type denoted as" B " and the cool temperate type "C"
are respectively 16'}{; and 77% in frequency. The frequency of the spore
which certainly belongs to Pteridophyta
is as high as that of an originary marine
deposit, being 10%. The frequency ofthe plants of the warm temperate andsubtropical regions gives the highest
ratio in the treated sample. The phenomena seem in the composite sample will
be explained in later pages on the discussion on the palaeoclimatic conditionand palaeogeographical environment.
To facilitate considerations on theecological environments under whichsome ancient plants lived, the modern
equivalents of the fossil species aregrouped into four habitats, namely upland, mixed-slope, stream-side or riparian,and lake or marshy elements. From theviewpoint of the above mentioned significant statistics the fossil pollen grains
and spores from this composite sample
can be classified into upland, mixed-slope
and stream-side elements, occupying respectively 18%, 38% and 44% of thetotal.
Sample 2: The composite sample yielded one genus and one family of the

11

Gymnosperm (23%), 17 genera and two
subgenera of the Dicotyledon (60%), one
genus and two families of the Monocotyledon (9%), three genera of thePteridophyta and two genera of theother groups (1.% and 7% respectively).
Among them, Pinus and Taxodiaceae
are abundant (13.% and 10% respectively).
Ulmus, juglans, Zellwva and Carpinus
are common (5% to 6,%). The othergenera and families are rare in frequency. The boreal dements attain 5%,
the temperate ones 87.% and the others
indicated by "B" in Fig. 6 about 8%.
The fossil pollen grains and sporesfound from the composite sample are
divided into three groups based on the
habitat as follows;
upland element. ................ . 20%
mixed-slope element ............ 52%
stream-side andjor riparianelement ...................... 28%
Sample 8g: The sample was takenfrom the well drilled at Locality No. 8
situated about 150 meters northwest of
the Wakura Station. A depth of thesample is about 35 meters below thepresent ground surface. The analysedsample contains three genera and one
family of the Gymnosperm (16.%), 17
genera and two subgenera of the Dicotyledon (66%), two genera and one
family of the Monocotyledon (8%), andthree genera of the Pteridophyta andtwo genera of plants lower than Pteridophyta (respectively 8% and 10%).
Among the pollen grains and sporesfound from the sample, Pinus is abundant (10%). It is noteworthy that Liquidambar and evergreen Quercus as therepresentative plants of warm elements
are 8% and 7% respectively in frequency.
The other genera and families are few,
ranging from 1'% to 6%. The boreal(indicated by "A"), warm (indicated by12

Norio FUJI

"B ") and temperate (indicated by "C ")elements are respectively 4%, 21% and75%. As the mentioned previous in thedescription, the relative frequency of thewarm climatic elements obtained fromthis sample is higher than those from
Samples 1 and 2. On the other hand,the upland, mixed-slope, and stream-side
andjor riparian elements are 17%, 38%
and 45% respectively.
Sample 8/: Although the locality ofthis sample is similar to that of Sample
8g, its depth is about 30 meters below
the present ground surface. This sample
yielded three genera and one family of
Gymnosperm (16%), 12 genera and two
subgenera of the Monocotyledon (12%),and three genera of the Pteridophyta
and two genera belonging to anothergroup (8% and 13% respectively). Pinus,
Taxodiaceae and evergreen Quercus areabundant (respectively 10%, 8% and7.5,%). Liquidambar is the representativeplant of warm element (7%). For thissample the relative frequency of warmcomponents is higher than those fromsome higher horizons.
Namely, theboreal, warm and cooler temperate elements are 9%, 19% and 72% respectively. The upland, mixed-slope andstream-side elements are 21%, 42% and
37% respectively.
Sample 7c: This sample is from thewell drilled at Locality No. 7 situatedabout 100 meters north of the Wakura
Station. The depth of the sample is14.50-14.77 meters below the present
ground surface. The sample yielded
three genera and one family of Gymnosperm (15%), 13 genera and two subgenera of Dicotyledon (38%), two genera
and one family of Monocotyledon (12%),three genera of Pteridophyta and two
genera belonging to the plants lower

than Pteridophyta which shows 12% and
6% respectively. Among them, Pinus isabundant (10%).
Alnus, Liquidambar
and Osmunda are common, being 6% inevery genus. The other genera andfamilies are rare (1% to 4%). Liquidambar is the representative plant ofwarm component but amounts to 3%.
The cold or subalpine, warm and temperate elements are respectively 13.%,13% and 74%. The upland, mixed-slope
and stream-side andjor riparian elementsare 23%, 54% and 23% respectively.
Sample 8e: The sample is from thewell drilled at Locality No. 8, and its
depth is 25 meters below the present
ground surface. The sample yielded
four genera and one family to the Gymnosperm (20%), 18 genera and two subgenera of Dicotyledon (54%), two genera
and one family of Monocotyledon (10%),three genera of Pteridophyta and two
genera belonging to the plants lower than
Pteridophyta, attaining respectively 6%
and 10%.
The relative frequency of Pinus, Taxodiaceae and Polyadosporites are 10%, 7%
and 6.5,% respectively.
Evergreen
Quercus, Gramin~ae, Nympaceae, Lycopodium and Osmunda are common (5%to 6%).
The boreal, warm and temperate elements are respectively 9%, 16% and75%. In connection with the palaeogeographical environment the stream-side
andjor riparian, upland and mixed-slope
elements are 34%, 52% and 14% respectively.
Sample 7b:
From this sample, of
which the locality is similar to Lolality
No. 7, Pinus is abundant; being 10%.
The genera of common frequency are
Taxodiaceae, Alnus, Gramineae, Pte1·idium
and Polyadosporites, being about 6% to548.

Spores and Pollen from the Neogene of Noto-I

7'}6. Picea, Abies, Fagus, Salix, deciduous
Quercus, Betula, Acer, Liquidambar, Persicaria, Nuphar,Lycopodium and Osmunda
are of rare frequency, and the othergenera are very few. Gymnosperm includes Pinus, Picea, Abies, Larix andTaxodiaceae (about 20%). Dicotyledon
containing mainly Alnus, Myriophyllum
and Liquidambar etc., Monocotyledon andPteridophyta respectively 44'}6, 10% and
8;'6. The boreal, temperate and warm
elements are respectively 16%, 8'}6 and76%.
The upland, mixed-slope and streamside components are 18%, 50% and 32%
respectively.
It is noteworthy that the relative frequency of the warm climatic elements
such as Liquidambar and evergreen
Quercus which occurred from the horizons higher than that of Sample 7b islower than that of the other horizons.
In the horizon lower than that Sample
7b the warm climatic elements show
frequency higher than that of the cold
andjor cooler climatic elements.
Sample 3: The composite sample isfrom Locality No. 3, situated at about
500 meters northerneast of the Wakure
Station.
Pinus and deciduous Quercus areabundant (10% to 12.5%). Taxodiaceae,
Ulmus, Zelkova, Carpinus and Tilia areof common (5%) without Carpinus which
is about 6% in frequency. The othergenera and families are rare (less than3%).
The cold, temperate and warm climaticelements are 11.7% and 82% respectively.
The upland, mixed-slope and riparian
andjor stream-side components are respectively 17%, 55'}6 and 28'}6.
Sample 8d: The stratigraphical horizon of this sample is similar probably

13

to that of Sample 3.
Tilia, Pinus, deciduous Quercus, Carpinus and Pleuricelloesporites are abundant in relative frequency. The boreal,temperate and warm climatic elements
are 11%, 11% and 78% in relative frequency.
In the connection with the palaeoecological environment the stream-side
andjor riparian, upland and mixed-slope
components are 35'}6, 10% and 55% respectively.
Sample 7a: This sample, of which
the locality is similar to Locality No. 7,yielded: Pinus is abundant (10'}6). The
other genera showing a high frequency
except for Pinus are Alnus and Polyadosporites (9%). All of the Taxodiaceae,
Salix and Nuphar are common (4';6 to6%). Liquidambar (2%) represents awarm climate together with the evergreen Quercus. All of Picea, Abies,
Fagus and Betula, which grow under aclimate cooler than that of the present
day Hokuriku region, are 2'}6 in relative
frequency. Gymnosperm contains three
genera and one family (17';6), Monocotyledon has one genus and two families(11%), Dicotyledon comprises 11 genera
and two subgenera (57';6), Pteridophyta
and five other genera, amount to about
15%. The warm, temperate and cold
climatic elements are respectively 7%,
83% and 10%. In respect to the palaeoecological environment, the upland,
mixed-slope and stream-side components
are 21%, 51% and 28% respectively.
Sample 8c: With respect to the assemblage of specimens found from thissample which is from about 15 meters
below the present ground surface in
Locality No. 8, the Gymnosperm containing four genera and one family (20%);
the Dicotyledon 20 genera and two sub-

14

Norio FUJI

genera (61%), the Monocotyledon one
genera and two families (8%), and the. Pteridophyta and the others amount to
11%.
The warm, temperate and cold climaticcomponents are 9%, 81% and 10;?6 respectively, and the upland, stream-side
andjor riparian and mixed:slope elements
respectively 14%, 32% .and 54.%.
Sample 8b:This. sample yielded
twenty two genera, two subgenera andthree families; namely, four genera andone family of Gymnosperm (20%); Monocotyledon one genera and two families-(15%); Dicotyledon 16 genera and two
subgenera (43%); Pteridophyta three
genera (10%) and the other group gavea frequency of 12%. The boreal climatic plants such as Picea, Abies, Larix
cand Betula amounted to 16%, the plants
which grow in the temperate climatic
region 76% and the warm climatic elements 8%. With respect to the palaeoecological environment the upland,
mixed-slope and stream-side or riparianelements are respectively 17%, 58% and25%.
Sample 4: The mixed sample from
Locality No.4, where situated about 1 km
north of the Wakura Station, belongs to
the middle horizon of the Wakura
Member.
This sample yielded four genera andone family of the Gymnosperm (27% in
total frequency), 19 genera and two subgenera of Dicotyledon (46%), one genusof Monocotyledon (5%), three genera of
Pteridophyta (4%) and two genera of
the other lower plants.
Among the pollen grains and spores
from the sample, Pinus is abundant·(13%), deciduous Quercus and Carpinus
are common (7% and 6% respectively),.and the others ar~ rare or f~w (1% to 5%).

The boreal (A), warm (B) and temperate (C) climatic elements are respectively 24%, 7% and 69%. And also, theupland, mixed-slope and stream-side
components are respectively 19%, 55%
and 26%.
San~ple Sa: The sample is from thewell drilled at Locality No. 8 situatednorthwest of the Wakura Station. The
depth of the sample is some 5 meters
below the present ground surface.
Among the pollen grains and sporesfound from the sample, Gymnosperm
attains 18%, Monocotyledon 12%, Dicotyledon 54%, Pteridophyta 12% and theothers 4%. Pinus, Gramineae and Carpinus are abundant (8% to 10%); juglans,
Castanea, Stylax and Persicaria are common (6% to 8%); the boreal, warm andtemperate elements are respectively 8%,
7% and 85%, and the stream-side andjor
riparian, mixed-slope and upland elements are 44;?6, 42;?6 and 14%. It isnoteworthy that the stream-side andjor
riparian components such as Salix, Celtis,
juglans, Pterocarya, Styrax and Liquidambar etc. are more common than themixed-slope and upland elements.
Sample 5: The mixed sample is collected from Locality No. 5 at about 200
metres south of the Wakura Station.
This sample belongs to the middle partof the upper horizon of the Wakura
Member.
The upland, mixed-slope andstre amside elements are respectively 20%, 35%
and 45%. The cold, warm and temperate
climatic elements contain 18%, 7% and
75% respectively.
The Gymnosperm including Pinus,
Picea, Abies and Larix (23% in relative
frequency), Monocotyledon (18%), Dicotyledon (42%), Pteridophyta (10%) andothers (7%) are found. Pinus, Taxo-

548.

15

Spores and Pollen from the Neogene of Noto-I

analysed for a palynological research.
The Wakura-eki shell bed (NI'INO &YAMADA, 1946) occupies the lower part(mudstone in rock-facies) of the Okuhara
Member. The horizon of this Sample 6
is just under to the unconformity separating member mention ed above.
The pollen-flora of Sample 6 is represented by Pinus, Gramineae, Taxodiaceae
and Salix (11%, 10%, 8.5% and 8% re-diaceae, Salix, Persicaria and Gramineae
represent the pollen-flora of Sample 5.
Sample 6: The mixed sample from
Locality No. 6, where situated at about
500 meters west of the Wakura Station,
belongs to the uppermost horizon of the
Wakura Member. At this locality the
Pleistocene Okuhara Member overlies
with unconformity the Wakura diatomaceous mudstone Member and was
A

IX

50%

50%
k '

•5

7c

.,;,ab• Bdac

~·

I

B

•I

. '7;;•Sa
·2

5o%

\

\

c

Fig. 6. Pollen diagram (3) : Triangular diagram showing the relationship between
cold & cool climatic, temperate climatic and warm climatic elements found from several
samples of the Wakura diatomaceous mudstone Member. Numbers refer to Figs. 1 and 3.
a: Yamatoda Member, b: Sunagozaka Member, e: Hojuji Member, f: l'ida Member, h:present deposit of Lagoon Hojozu.gata, i: Nakayama-toge Member, j: Hijirikawa Member,k: Takakubo Member, 1: Omma Member. A: cold & cool climatic element, B: warm
climatic element, C: temperate climatic element.

16

Norio FUJ/

spectively).
The Gymnosperm (onefamily and four genera in this sample)
attains 24.5%, Monocotyledon (twofamilies 18%, Dicotyledon (ten genera
and one family) 43.5%, Pteridophyta(three genera) 10% and the other (twogenera) 4%.
In respect to the palaeoecological environment, the upland, mixed-slope andstream-side andjor riparian elements arerespectively 18%, 42% and 40% in relative frequency.
(4) Discussion
From analysis of the pollen grains andspores a general interpretation can bemade of the physical conditions prevailing during growth of the sedimentarybasin in which they were found. In thissection, the writer will discuss on thepalaeoclimatic condition, palaeographicalenvironment and geological age of thestratigraphical units based upon the
microfossils.
(a) Palaeoclimatic Condition
The pollen grain and spore assemblages have been analysed and from theresults the general characters of thepalaeoclimatic condition can be presented. The methods for analysing assemblages for palaeoclimatic interpretation
have been developed by ERDTMAN,
F AEGRI and IVERSEN, besides palynologists, and the writer has used anothermethod for palaeoclimatic analysis of
his palynological researches on the Neogene Tertiary and Holocene deposits
developed along the coastal region ofJapan Sea, and reported that the results
agreed well with the climatic indications
deduced by the other methods (Fun,1964 & 1966). The methods used by thepresent writer are classified into a
warmth index, triangular andjor quadrilateral diagrams.

100%

\

0

\

0

100%

Fig. 7. Pollen diagram (4): Quadrilateral diagram showing the palaeoclimaticcondition and palaeoecological environment
during the sedimentation of the Wakura
diatomaceous mudstone Member. Numbers
refer to Figs. 1 and 3. a: Yamatoda Member, b: Sunagozaka Member, c: Higashiin'nai Member, d: Najimi Member, e: Hojuji Member, f: l'ida Member, g: Wakura
Member, h: I•izuka Member, i: Nakayamatoge Member, j: Hijirikawa Member, k:
Takakubo Member, 1: Omma Member.

According to the writer's investigation,
as shown in the triangular diagram (Fig.
6), the warm and subtropical plants suchas Liquidambar and Metasequoia fromthe Wakura Member is far less in number of specimens than from the Yamatoda and Sunagozaka Members whichcorrespond to the Daijima stage, namely,

548.

Spores and Pollen from the Neogene of Nota-l

the latter yielded 61% to 85% in averagefor the total specimens, and the former
8% to 16%. The present result is closely
similar to the analytical results on thepollen and spore assemblages from the
Hojuji and l'ida Members studied previously (Fun, 1966). With respect tothe relative frequency of warm and subtropical elements found throughout thismember, the higher the horizon is, theJess the frequency becomes. However,on the contrary in respect to the cooland cold elements, the higher the horizon is, the more the frequency becomes.
The relationship between the temperate,
warm and cold elements is illustrated inFig. 9.
Comparison between the fossil plants
and similar living equivalents whose
climatic requirements are known is frequently used for climatic analysis of a
fossil flora. Where the modern relationships are known definitely, this method
is probably useful for accurate information. The Neogene Tertiary species arecomparatively modernized in morphological features, so it is not difficult tocompare them with Jiving equivalentswith some exceptions. The genera comprising the Neogene flora in Japan aremostly distributed now in East Asia,and nearly all of the temperate Dicotyledonous genera in the fossil flora are
now growing in Japanese Islands. However, exotic genera are sometimes commonly contained in the fossil flora. The
exotic coniferous genera such as Jo.;fetasequoia, Glyptostrobus, Sequoia, Pseudolarix and Keteleeria are found throughout the Neogene flora of Japan, andthey are mostly living now in China,
and some of them are known in thewestern part of North America. The
nearest living equivalents of the pollen
floras from thd Wakura Member andtheir modern distribution in East Asia

17

are shown in Table 2. According to thistable, the Wakura pollen flora consists
mainly of temperate genera, with warm
climatic elements commonly associated.
The dominant genera among the temperate ones are Alnus, Fagus, Castanea,
Quercus, Ulmus, Zelkova, Acer and Tilia.
The modern species equivalent to them,according to TANAI (1961), are mostly
distributed in Japan proper, especiallyfrom Central Japan to Kyushu. However, some of them are rather luxuriantly
distributed in Northern Honshu andHokkaido. Further, the pollen flora sometimes contains many exotic conifers suchas Cunninghamia, Taiwania, Metasequoia,
Glyptostrobus and Liquidambar of the
Dicotyledons, though they are not abundant in number of specimens and arerather relicts which survived from theprevious Yamatoda and Sunagozaka
pollen floras. Such presumption regardingthe climatic conditions is supported by
the fact that the pollen flora frequently
contains the warm climatic elements.
Thus, according to the writer's researches, the pollen flora of the W akura
Member comprises temperate and warm
climatic elements mingled in floristic
composition as already described in theprevious part of this work. From theviewpoint of leaf character analysis reported on the Late Miocene floras fromvarious localities by T ANAl (1961) the
Wakura pollen flora is related to thepresent temperate or somewhat temperate forest in Central and Southern
Japan, and they seem to have grownunder a warm temperate climatic condition. However, the reduction of warmand subtropical plants evidently indicatesthat the temperature had lowered incomparison with that of the Daijima stage.
(b) Palaeogeographical Environment
To facilitate the considerations on the

1-l
00

Table 2. Modern equivalents o£ the fossil microplants from the Wakura diatomaceous mudstone Member.
Modern equivalentmacroplants

Near fossil macroplants

Pinus
Abies
Pice aP. palaeopentaphylla
A. protojirma
P. kaneharai
P. jessoensis
P. koribai

P. parviflora
A. firma
P. polita
P. jessoensis
P. excelsa

Cun. protokonishii
Gly. europaeus
Met. occidentalis
Seq. afjinis
Tai. japonica
Tax. dubium
F. palaeocrenata
F. protojaponica
U. protojaponica
U. protolaciniata
U. subparvifolia
S. k-suzukii

C. konish!i
G. pensilis
M. glyptostroboides
S. sempervirens
T. cryptomeroides
T. distichum
F. crenata
F. serrata
U. japonica
U. laciniata
U. parvifolia
S. jessoensis

Q. protosalicina

Q. salicina

Q. miocrispula

Q. crispula

X

Q. protodentata
Q. protoserrata
A. miojaponica
A. protohirsuta
A. protomaximowicziana]. nipponica
C. nathorsti
C. nordenskioldii
B. miomaximowicziana
B. onbaraensis
B. protoermanni
B. protoglobispica

Q. dentata
Q. serrata
A. japonica
A. hirsuta
A. maximowicziana]. ailanthifolia
C. jessoensis
C. occidentalis
B. maximowicziana
B. grossa
B. ermanni
B. globispica

X
X

Larix
Taxodiaceae

Fagus
Ulmus
Salix
Quercus(evergre.)
Quercus(non e.g.)Alnus]uglans
CeltisBetula

I

China

Japan

Fossilmicroplants

1_:_j__3__ 4
X

X

5

7 1 8

6

9

----

X

X

X

X

X

X

X

X

X

Habitat

~~~

13

12
~-

-

-

-

u
M

u

X

X

X

M
M

u
u

X

R
M
M

X
X

I

X

X

u

X

R
X

X

X

X

M~U

X

X

X

X

X

X

X

X

X

X

X

X

M
R
M
M
R

X

X
X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X

X
X

X
! X
I X

X

I X

X

! X

X

X

X

X

X

X

X
X

X

X

I

X
X

X

X

X

X

X

X

X

X

X

X
X

M

X
X

M
M
M~R

X
X

X

X
X

X

R

I M~R
U
u

X

M
M

X

M~U

i

I

: X

i

I

M

I

I
1

I

I i

M~U

I

M

~

"'!

~·

':tj

~
......

1

Pterocarya

B. protojaponica

i P. nipponica
P. asymmetrosaP. protostenoptera

Cory! usAcer

Castanea
Cary aZelkova
Menyanthes
Styrax
Carpinus

Tilia

Liquidambar----

A. nordenskiiildi
A. palaeodiabolicum
A. palaeorujinerve
A. protojaponicum
A. protosieboldianum
A. prototrijidium
A. pseudocarpinifolium
A. submayri
A. svbpictum
C. miocrnata
C. miocathayensis
Z. ungeri
S. protoobassia
S. japonica
I C. miocenica
C. nipponica
C. stenophylla
C. subcordata
C. subyedoensis
I T. distans
T. miohenryana
T. protojaponica
1i3. japon!ca
P. rhoifolia
P. paliurusP. stenoptera

X

X
X

X
X

S. obassia
S. japonica
C. laxiflora! C. lanceolata
1 C. carpinoides
C. cordata
C. tchonoskii
T. amuraensis
T. henryana
T. japonica

X

X

X
X

I A. palmatum
A. diabolicum
A. rujinerve
A. japonicum
A. sieboldianum
A. trijidium
A. carpinifolium
A. monoA. monoC. crenata
C. cathayensis
Z. serrata

I
X

X
X

! X
j

X

X
X

X

! X

X
X
X

X
X

I X
X

l

X
X
X
X

X

I
1

i

X
X
X : X

X
X
X

X

X

X
X
X

X i X

X
X

X
X

I

I

X
X

X

X

X I
X

: X
X
X

X

j

X
X

X
X

X

X

I

X
X
X
X

X
X

X
X

X
X

X

X I X

I

X

1 X

I X

X

X

I

X

I

X

X

X '
X
X

, X

X

X

L. miofor:osana .. ______ __!_/~rm~~!:_~ _____ ---··- -·· _____

X

X

X

i X

1

I X

I

j

X

I X

I

M~R

X
X

X
X
~.

X

I

-- ..

R
R
M
M
M
M
M
M
M
M
M
M
M
M
M
R
M
M
M
M
M

I M~R

X
X

1

X

X

X
X

I

' X

! X

I

X

X
X

X
X

I

X
X

X
X I X
X ; X

I
I

'
X II
,
I X I
X
X

x~~~~

i X

X

M

'M~R

I

X

X

-

Member and their modern distribution
Modern Distribution
1: Saghalien and Kurile Is., 2 : Hokkaido, 3: Northern Honshu, 4 : Central Honshu, 5: Southwe:otern Honshu,
6: Kyushu and Shikoku, 7: Formosa and Loochoo Is., 8: Korea, 9: North China, 10 : Central China,
11: Southeastern China, 12: Southwestern China, 13: Manchuria and Primorskaya Prov.
HabitatU: upland, M : mixed-slope, R : riparian and stream-side

I

M
M
M
R
--·

~
..__

Co

~
0

"'""
<:':>

~

~

R.

~
.,.....
.,.....
<:':>

~

~
0
~

.,....
~
<:':>

~

<:':>

0
<Q
<:':>

~

<:':>

~
~
0
No

0

I

'-<

......
'-020

Norio FUJI
100%

I
0

0

!
100%

Fig. 8. Pollen diagram (5) : Quadrilateral diagram showing the relationshipbetween cold & temperate climatic andwarm climatic elements, stream & riparianand upland & mixed-slope elements foundfrom several samples of the Wakura diatomaceous mudstone Member. Numbers refer
to Figs. 1 and 3.

probable ecological environments underwhich some ancient plants lived, themodern equivalents of the fossil species
are grouped according to their habitats,namely; four types of upland, mixedslope, stream-side or riparian, and lakeor marshy elements.
The Wakura p·ollen flora is mainlycomprised of mixed-slope or mixedslope-riparian plants in number of
specimens, and also contains uplandmixed-slope plants. Namely, this flora

seems to represent a mixed-slope toriparian forest. For instance, the mixedslope plants amount to 44% in frequency
on average, stream-side and riparianplants 30% and the remainder of upland
plants. On the other hand, judging fromthe lithofacies, poor contents of planktonic foraminifers, fossil diatom assemblages and diversity in the thickness ofthe deposits, the sea under which the
Wakura Member was deposited during
the Neogene Tertiary seems to havebeen a more or less closed embayment
in the Wakura area 6f central part ofNoto Peninsula, though the sea insouthern part of Noto Peninsula widened
during the Late Miocene age. The
spread of this semi-opened sea is shownin Fig. 10.
The friq uency of grass-pollen grains.
and spores have been generally accepted
to be related to the geographical environments. Accordingly, such presumption on the marine terrain is supportedby that the frequency of the grass-pollen
grains and spores ranges from 36% to
50% in the Wakura Member, thoughfrom 26% in the Hijirikawa to 46% in
the l'izuka Members.
(c) Geological Age
In the japanese Islands the correlation
and age determination of the Tertiary
floras have been frequently made by theuse of several characteristic fossils andassemblages. The Neogene flora ofjapan has been described by Y ABE and
ENDO, SUZUKI, T ANAl and many otherauthors, and consequently the floristic
composition of each flora is comparatively well known at present. On thebasis of these researches, TANAI (1961}
classified the Neogene floras of japan
into six types, considering the floristic
composition and components, along withthe geological ages indicated by them.

548.

21

Spores and Pollen from the Neogene of Noto-I

r

I
)

; )

~

\

\
30

o:A,

X

:B, o:C,

40

50

60

70

80%

10

20

30

40

•:Upland, o:mixed-slope, "'Stream-side

50

60%

a riparianFig. 9. Pollen diagram (6) : Figure showing the relationship between cold & coolclimatic, temperate climatic, warm climatic, upland, mixed-slope and riparian elements
found from several samples of the Wakura diatomaceous mudstone Member. Numbers
refer to Figs. 1 and 3.

These types are in ascending order the
Ainoura (Earliest Miocene), Aniai (Early
Miocene), Daijima (Middle Miocene),
Mitoku (Late Miocene to Mio-Pliocene),
Shinjo (Early Pliocene) and Akashi (Late
Pliocene) types.
The Wakura pollen flora is very
similar in generic composition to the
Mitoku-type flora. It contains a few
exotic elements which are found abupdantly in the Noroshi and Yama:i:oda

floras. It is commonly found in the Late
Miocene floras of Europe and in thewestern part of the United States where
the modernized plants are dominant.
Thus, in comparison with various florasof the Neogene in japan and from theviewpoint of its stratigraphical evidences
the Wakura pollen flora can be nearlycorrelated with the Mitoku-type flora, andthe geochronological position of the W'akura Member seems to be Late Miocene.

22

Norio FUJI
References Cited-37"N._ __ 1_______ .... -/137" E

Fig. 10. The Palaeogeographical map
during the sedimentation of the Wakura
diatomaceous mudstone Member (the Otogawa stage of Late Miocene age) (After
Y. KASENO, 1963).

AoKI, T. (1956) : Geological Study of the
Nanao-Tatsuruhama District, Ishikawa
Prefecture (MS). Graduation Thesis of
the Kanazawa Univ., 46 p., 7 text-figs.,.
2 tabs., 8 pis.
BAcHMAi'::-.:, A. (1962) : The Silicoftagellides.
in the Wakura Beds, Nanao City, Prefecture Ishikawa, Japan. Sci. Rept., Kanazawa Univ., 8, 1, pp. 161-175, 4 figs., 10·
pis.
CouPER, R. A. (1953) : Upper Mesozoic andCainozoic Spores and Pollen Grains fromNew Zealand. New Zealand Geol. Surv.
Paleont. Bull. 22, 77 p., 3 text-figs., 3tabs., 9 pis.
ERDTMAi':, G. (1954) : An Introduction to·Pollen Analysis. 239 p., 15 text-figs., 10tabs., 28 pis., Chronica Botanica Comp.
FAEGRI, K. and IvERSEN, T. (1964) : Text-

Explanation of Plate 1
Fig. 1:
Fig. 2:
Fig. 3:Fig. 4:
Fig. 5:
Fig. 6:
Fig. 7:
Fig. 8:Fig. 9:Fig. 10:
Fig. 11:
Fig. 12:Fig. 13:
Fig. 14:
Fig. 15:
Fig. 16:
Fig. 17:
Fig. 18:
Fig. 19:
Fig. 20:
Fig. 21:
Fig. 22:
Fig. 23:
Fig. 24:
Fig. 25:
Fig. 26:
Fig. 27:
Fig. 28:

Pice a; Locality 3; EKZJ coil. cat. no. 20019.
Abies; Locality 8, Horizon b; EKZJ coli. cat. no. 20020.
Taxodiaceae; Locality 7, Horizon a; EKZJ coli. cat. no. 20021.
Podocarpus; Locality 7, Horizon d; EKZJ coli. cat. no. 20022.
Tsuga; Locality 6; EKZJ coil. cat. no. 20023.
Tilia; Locality 8, Horizon d; EKZJ coli. cat. no. 20024
Betula; Locality 4; EKZJ coli. cat. no. 20025.
Podocarpus; Locality 6; EKZJ coli. cat. no. 20026.
Zelkova; Locality 8, Horizon c; EKZJ coli. cat. no. 20027.
Cfr. Zelkova; Locality 7, Horizon b; EKZJ coli. cat. no. 20028.
Cary a; Locality 8, Horizon g; EKZJ coil. cat. no. 20029.
Cary a; Locality 8, Horizon d; EKZJ coli. cat. no. 20030.
Aff. Cary a; Locality 3; EKZJ coli. cat. no. 20031.
Carya; Locality 3; EKZJ coli. cat. no. 20032.
Carya; Locality 4; EKZJ coil. cat. no. 20033.
Alnus; Locality 1; EKZJ coli. cat. no. 20034.
Pterocarya; Locality 5; EKZJ coli. cat. no. 20035.
Salix; Locality 8, Horizon c; EKZJ coli. cat. no. 20036.
Salix; Locality 7, Horizon b; EKZJ coli. cat. no. 20037.
Salix; Locality 8, Horizon g; EKZJ coli. cat. no. 20038.
Castanea; Locality 7, Horizon a; EKZJ coli. cat. no. 20039.
Quercus (small), evergreen Quercus; Locality 4; EKZJ coil. cat. no. 20040.
Fagus; Locality 7, Horizon a; EKZJ coli. cat. no. 20041.
Nyssa; Locality 2; EKZJ coil. cat. no. 20042.
Nyssa; Locality 4; EKZJ coli. cat. no. 20043.
Quercus (large), deciduous Quercus; Locality 6; EKZJ coli. cat. no. 20044.
Quercus (large), deciduous Quercus; LocaJity 6; EKZJ coli. cat. no. 20045.
Quercus (large), deciduous Quercus; Locality 5; EKZJ .coli. cat. no. 20046.

fi'VJJ:

Fossil Spo1·es a~(l Poll(!?'/, Gmi?~s fro?n the Neogene of Noto I

2

Plate 1

3

0
7

G

5

10
11

12

15

13

e
.

16

.

18

19

21

20

22

17

aae~w
~·[II
26

23

24
'~!1 51·'

27

28

548.

Spores and Pollen from the Neogene of Noto-I

book of Pollen Analysis. 237 p., 23 textfigs., 8 pis., Munksgaard.
FUJI, N., IcHIKAWA, W. and BACHMANN, A.
(1964) : Fossil Diatoms, Pollen Grains
and Spores, Silicoflagellates and Arachaeomonads in the Miocene Hojuji Diatomaceous Mudstone, Noto Peninsula, Central Japan. Sci. Rept. Kanazawa Univ.,
9, 1, pp. 25-118, 30 text-figs., 3 tabs., 15pis.
- - (1965) : Palynological Studies on the
Late Tertiary and Quaternary Systems
in Hokuriku District, Central Japan.
Quaternary Research, 4, 3-4, pp. 183-190,
5 text-figs., 1 tab.
- - and BAcHMANN, A. (1968) : Fossile
Pollen, Sporen und Silicofiagellaten aus
den Hijirikawa-Schichten (Obermiozlin)der Halbinsel Noto, Zentral-Japan. Bull.
Fac. Educat. Kanazawa Univ., 17, S. 4156, 7 Abb., 2 Tab.
HoKuRIKu QuATERNARY RESEARCH GROUP(1967) : Quaternary Deposits in the Vicinity of Nanao, Noto Peninsula, Central
Japan. jour. Geol. Soc. japan, 73, 1, pp.
495-510, 13 text-figs., 5 tabs.
IcHIKAWA, W. (1960): On the Fossil Marine
Diatoms in the Wakura Beds, Noto Peninsula, Japan. Sci. Rept. Kanazawa Univ.,
7, 1, pp. 175-214, 1 text-fig., 1 tab., 9 pis.
- - and KAsENO, Y. (1963) : Diatomaceous
Deposits of Noto, Japan. 45 p., 5 textfigs., 3 pis., 4 geol. maps, Ishikawa-ken.
KAsENo, Y. (1963) : Geology of Southern
Noto Peninsula, Central Japan, with Reference to the Cenozoic History. Sci.
Rept. Kanazawa Univ., 8, 2, pp. 541-568,
11 text-figs., 1 tab., 4 pis.
MAcKo, S. (1957) : Pollen Grains and Spores
from Miocene Brown Coals in Lower
Silesia -I-. Prace Wroclawskiego To-

AinouraAkashiAkauraAnamizu
Aniai
DaijimaHijirikawa

m

im

a}!
'i)f;

1::i

im

ll•if t*......
1'A

{'i

n

1ih

~

Jll

23

warzystwa Naukowego, Trauaux de laSocietie des Sciences at des Lettres deWroclaw, Ser. B, 96, pp. 1-108, 5 textfigs., 3 tabs., 57 pis.
NIINO, H. and YAMADA, M. (1949): On the
Wakura-eki and Amadani Shell Beds in
Noto Peninsula. Miscellaneous Inst. Nat_Res., 27, pp. 37-41, 8 text-figs.
NISHIJIMA, T. (1958): The Geological Studyof the Sakiyama District, Noto Peninsula,
Central Japan (MS). Graduation Thesis.
of the Kanazawa Univ., 75 p., 11 textfig., 7 tabs., 5 pis., 12 photos.
SHIMAKURA, M. (1956) : PollenstratigraphicalStudies of the Japanese Cenozoic Formation-!-. Bull. Nara Gakugei Univ., 6,2, pp. 57-64, 7 text-figs.
- - (1957) : Pollenstratigraphical Studies of
the Japanese Cenozoic Formations -II-.
The Harakawa Formation of the Nijo
Group. Ibid., 1, 2, pp. 35-42, 3 text-figs.,
1 tab., 1 pl.
- - (1959) : Pollenstratigraphical Studies of
the Japanese Cenozoic Formations -III-.
The Kobe Group and the Akashi Group.
Ibid., 8, 2, pp. 65-75, 4 text-figs., 4 tabs .•2 pis.
- - (1960) : Pollenstratigraphical Studies of
the Japanese Cenozoic Formations -IV-The Nishigawa Oil Field, Niigata Prefecture and the Ningyotoge Uranium Mine,
Chugoku District. Ibid., 9, 2, pp. 33-42,
2 text-figs., 2 tabs., 2 pis.
- - (1963) : Pollenstratigraphical Studies of
the Japanese Cenozoic Formations-VI-.
The Jigokudani Formation. Ibid., II 1, 2.
text-figs., 3 tabs., 2 pis.
TANAI, T. (1961): Neogene Floral Change·
in Japan. jour. Fac. Sci. Hokkaido Univ.,
Series IV, II, 2, pp. 119-398, 7 text-figs.,
15 tabs., 32 pis.

Himi
Hiradoko
Hojuji
HosoguchiI•izukaIshizaki
Iwaya

:7](

~

-o/·

*

r.tH.± ;;'f

*Ill

r:l

fiJi

J.j

{:i

·~lft1~~

Norio FUJI

24
Kamitako
K6da
KojimaMitokuMt. Bij6-zan

J: ru .:r
(o]

LU

+

!Ih
t'lr.

}§

Jt LIJ

Mt. Sekid6-sanNakayama-toge
Nanao
Nishiminato
Noto

i::i !WJ LiJ
f:j:ILIJilif;

-t

~

l§

~

Explanation of Plate 2
Fig. 29:
Fig. 30:
Fig. 31 :Fig. 32:
Fig. 33:
Fig. 34:
Fig. 35:
Fig. 36:
Fig. 37:
Fig. 38:
Fig. 39:
Fig. 40:
Fig. 41:
Fig. 42:
Fig. 43:
Fig. 44:
Fig. 45:
Fig. 46:
Fig. 47:
Fig. 48:
Fig. 49:
Fig. 50:
Fig. 51:
Fig. 52:
Fig. 53:
Fig. 54:
Fig. 55:
Fig. 56:
Fig. 57:
Fig. 58:
Fig. 59:
Fig. 60:
Fig. 61:
Fig. 62:
Fig. 63:
Fig. 64:
Fig. 65:
Fig. 66:

Pinus; Locality 6; EKZJ coli. cat. no. 20047.
Pinus; Locality 8; Horizon b; EKZJ coli. cat. no. 20048.
Pinus; Locality 2; EKZJ coli. cat. no. 20049.
Pinus; Locality 7, Horizon c; EKZJ coli. cat. no. 20050.
Pinus; Locality 8, Horizon e; EKZJ coli. cat. no. 20051.
Pinus; Locality 4; EKZJ coli. cat. no. 20052.
Pinus; Locality 7, Horizon c; EKZJ coli. cat. no. 20053.
Pinus; Locality 2; EKZJ coli. cat. no. 20054.
Abies; Locality 3; EKZJ coli. cat. no. 20055.
Pinus; Locality 8, Horizon d; EKZJ coli. cat. no. 20056.
Pinus; Locality 7, Horizon c; EKZJ coli. cat. no. 20053.
Pinus; Locality 2; EKZJ coli. cat. no. 20054.
Pinus; Locality 7, Horizon a; EKZJ coli. cat. no. 20057.
Persicaria; Locality 4; EKZJ coli. cat. no. 20058.
Spore, gen. indet. ; Locality 4; EKZJ coli. cat. no. 20059.
Monosulcopollenites; Locality 4; EKZJ coli. cat. no. 20060.
PleuricellaesPorites; Locality 7, Horizon c; EKZJ coli. cat. no. 20061.
Monosulcopollenites; Locality 5; EKZJ coli. cat. no. 20062.
Triadosporites; Locality 8, Horizon c; EKZJ coli. cat. no. 20063.
Pleuricellaesporites; Locality 5; EKZJ coli. cat. no. 20064.
Jnapertisporites; Locality 3; EKZJ coli. cat. no. 20065.
Pleuricellaesporites; Locality 6; EKZJ coli. cat. no. 20066.
Trilate type spore, gen. indet.; Locality 6; EKZJ coli. cat. no. 20067.
Trilate type spore, gen. indet.; Locality 5; EKZJ coli. cat. no. 20068.
Lycopodium; Locality 3; EKZJ coli. cat. no. 20069.
Tricolporopollenites; Locality 8, Horizon d; EKZJ coli. cat. no. 20070.
Tricolporopollenites; Locality 7, Horizon c; EKZJ coli. cat. no. 20071.
Tricolporopollenites; Locality 8, Horizon d; EKZJ coli. cat. no. 20072.
Castanea; Locality 4; EKZJ coli. cat. no. 20073.
Tricolporopollenites; Locality 1; EKZJ coli. cat. no. 20074.
Tricolporopollenites; Locality 4; EKZJ coli. cat. no. 20075.
Tricolporopollenites; Locality 8, Horizon d; EKZJ coli. cat. no. 20076.
Acer; Locality 7, Horizon e; EKZJ coli. can. no. 20077.
Castanea; Locality 6; EKZJ coli. cat. no. 20078.
Pollen grain ( ?) ; Locality 8, Horizon c; EKZJ coli. cat. no. 20079.
Cory ius; Locality 6; EKZJ coli. cat. no. 20080.
Tilia; Locality 8, Horizon a; EKZJ coli. cat. no. 20081.
Cary a; Locality 6; EKZJ coli. cat. no. 20082.

(Figs. 30-32, 37-38, 41-44, 47, 49, 51-53, 64-65 are measured by a right scale, 20 p, and the-other figs. by a left scale, 15 p. All specimens illustrated are kept in the Institute of Earth
Science, Kanazawa University)

FUJI : Fo ssil Spores a1~d Polle1~ Grains fro?n the Neo oe1~e of Nato I

32

31

"

36

35

34

33

Plate 2

tlO

39
38

41

47

54

18

1

•

'
'

55

Sl

49

{j
:)6

:i7

58

62

6l

,_ _

,1 51'

53

52

50

·~·--

1

20 "
'

S~l

60

548.

25

Spores and Pollen from the Neogene of Noto-I

Noto-jimaOkuhara6sugi-zaki
Otogawa
Sakiyama
SanamiShinjoSunagozaka

ii~ ~ Jfb~}]{*~~ill~""'13 ill

"'~
1ti:
mr

ill
r&:
/£

fl') -T~

Suso
Takashina
TokudaTsukadaWakuraWakura-eki
Yamatoda

~
~

f!lij
~

lit
Jli!1
Ill
Ill
J§r

;fr:J
;fr:J J§r ~ill? IIITrans. Proc. Palaeont. Soc. Japan, N. S., No. 73, pp. 26-31, pl. 3, April 30, 1969

549.

OCCURRENCE OF TUTCHERIA FROM THE LOWERJURASSIC OF WEST JAPAN*

ITARU HAYAMI
Department of Geology, Kyushu University® [] :;{Cf}m /"'" 7 *cJil iJ, G Tutcheria (.7) 1}1;:/±', : Tutcheria Cox, 1946 v'i Carditidae
c Astartidae (.7)~il&~3lfth.(illf;t.Q::::. c -c·f.a!l'*<b.Q=tx&-c·<b.Q. 4'-@l, :l!IJ:im/illlfllH~lllcfl\lti!.li@;iillil' G*~ (.))f{rf!l!iJ":f*~ ~ ht..:(.))"C·lJe•l&i" .Q, ::::. (.7)#1!~1:: Tutcheria /m(.)) 57~11*~-I:V?wlli:
rc-::>&:~Nt~IJPX.t-.::*11-lr:, Astartidae J: IJ t Carditidae r:f';-Cl:l.Q)iiJ":~~-c·<b.Q c(.))*lfffi,ij
rei~ !A.:,;)£ 7Jc
til-

Tutcheria is an interesting bivalve
genus, because it has both the charactersof the Carditidae and the Astartidae. It
was proposed by Cox (1946) for nine
European species, some of which had
been referred to Cardium, Cardita, !so·cardia or Anisocardia. Its known distribution is almost restricted strati·
graphically to the Lower Jurassic(mainly Hettangian to Pliensbachian)and geographically to western Europe,
although an Upper Triassic carditid
from east Siberia, Cardita cloacina sibirica
KIPARISOVA, 1966, may belong to thisgenus.
In the course of his geologic survey
for the graduation thesis Mr. Masataka
ITO, a student of the Kyushu University
1962-1966, collected many fossil bivalvesfrom the Higashinagano formation of
the Toyora group in the Ishimachi areaof Yamaguchi Prefecture. Most of thembelong to the already described species
by YEHARA (1921) and HAY AMI (1958,
1959), but some seem to represent unde·scribed species. Recently I have found a

new species of Tutcheria in his collection, and the result of examination is.
reported here. An interpretation on thesystematic position of Tutcheria is alsopresented. This is probably. the firstreport for the occurrence of this genus.
in a region outside western Europe.
Before going further, I wish to record
my sincere thanks to Prof. TatsuroMATSUMOTO of the Kyushu University
for his kind instruction and supervisionof this manuscript and to the late Dr.
Leslie Reginald Cox of the British
Museum (Natural History) for his kind
information about European Jurassic
bivalves including the genus in question.
Acknowledgements are also due to Mr.
Masataka ITo of the Bulldozer Engineering Company of Osaka for his kind
supply of the material and some unpublished data.

* Received Oct. 18, 1968; read Nov. 30,
1968 at Shizuoka.

Family Carditidae FLEMING, 1829

Description and discussions

Order Veneroida
Superfamily Carditoidea

Genus Tutcheria Cox, 1946
26

549.

Tutcheria from the Jurassic

Type-species.-Cardium
submulticostatum D'ORBIGNY, 1850 (=Cardium multicostatum PHILIPS, 1829, non BROCCHI),
Middle Lias, western Europe. (original
designation)
Discussions.- The genus Tutcheria is,
as defined clearly in the original diagnosis,
characterized by the small size, numerous radial riblets (or threads) interrupted by some widely spaced imbricating
growth lamellae, denticulate ventral
margin in accordance with the radial
ornament and Astarte-like dentition as
AI 3b PI (Pill)
formulated: AICZ4 b- -:PlC' The absence of the teeth 3a and Alii and thetubercular shape of both lateral teeth
are noteworthy.
Notwithstanding the fact that the external morphology of this genus recalls
strongly that of the Carditidae such as
Palaeocardita, Pseudocardia, Glans andVenericardia, the hinge structure, especially the presence of anterior lateral
teeth, is similar to that of the Astartidae.
Cox (1946, pp. 36-37) laid stress on theresemblance of hinge structure between
Tutcheria and astartids, suggesting thederivation of the former from the sameancestral stock which gave rise also to
the latter. He did not mention whichfamily Tutcheria should be referred to,
but from his discussion this genus wasevidently regarded as more closely related
to the Astartidae than to the Carditidae.
In relation to the taxonomic and phylogenetic problem of Tutcheria, I thinkthat the following facts and acknowledged
opinions should be taken into consideration.
1l Such a strong radial ornamentationis very common in the Carditidae but
unknown at all in any described speciesof the Astartidae. Although some speciesof the genus Ensio Cox, 1962 (typespecies: Ptychomya agasszzi LYCETT,

271850) of the Astartidae have peculiar
divaricated sculpture, they are certainly
unrelated to Tutcheria. The sculpture of
Ensio does not correspond with the·marginal crenulation but is probably a
modification of concentric ribs.
2) In view of the presence of distinct
marginal crenulation in the adult shells.
of many astartids, it might be presumed
that certain radial shell structure related to the crenulation would be concealed in the interior of shells. WRIGLEY(1946, pp. 11, 18), however, denying thetruth of this presumption, clarified thatno radial shell structure is visible inseveral species of fossil Astarte from the
Eocene London Clay, though such astructure was said to be common in the
Crassatellidae. It is probably the samewith the Mesozoic species of Astarte andmany genera of the Astartidae. I havesometimes etched the test of fossil
astartids with dilute HCI in order tO·
observe the internal structure, but havenever seen any radial structure in thecourse of etching. It may be, therefore,
concluded that Tutcheria is fundamentarily different from the Astartidae not
only in the surface ornamentation but
also in the structure of shell.
3) Anterior and posterior lateral teeth
are commonly well developed in the
Astartidae, especially in the Mesozoic
species, although in some species theytend to be weakened through the growth.
On the other hand they are scarcely
seen in the adult individuals of Cardita
and V enericardia from the Cenozoic andRecent. However, the absence of lateral
teeth does not necessarily serve as adiagnostic criterion for the· Carditidae_
For example, many species of the genus.
Palaeocardita CONRAD, 1867, from theTriassic (BITTNER, 1895) and an aberrant
species of "Pseudocardia " from theLower Cretaceous (HAY AMI, 1965, p. 79}

28

Itaru HAYAMI

have distinct posterior lateral teeth.
Furthermore, ·in some Cenozoic andRecent species of the genus Glans
MEGERLE VON MUHLFELD, 1811 (typespecies: Chama trapezia LINNAEUS, 1758)
there are weak traces of anterior lateral
teeth AI and All.
BERNARD (1895) and DOUVILLE (1913,
1921) explained successfully the evolutionof heterodont hinge teeth on the basisof ontogenetical development of someliving and fossil species; According tothem, the cardinal teeth of .. heterodont
bivalves are nothing but the.products by
the terminal thickening of anterior lateral
teeth. It is rather reasonable to interpretthat in early . ontogenetical stage there
are anterior lateral teeth in all the speciesof heterodont bivalves. The cardinalteeth 3a and 2 of the Carditidae andAstartidae are, of course, considered to
be originated from the. anterior lateral
teeth Alii and All respectively, regardless the condition that the anterior laterals
may or may not be persistent in theadult shells. Anyhow, the strength andpersistence of anterior lateral teeth are
regarded as changeable from species tospecies in these· families. In Tutcheria
the cardinal tooth 3a aml.. the lateral
tooth Alii are actually ·not· demarcatedfrom the valve margin. Such a state is,however, commonly metwith both in the
Astartidae and the Carditidae.
4) The combinatio'n of, radial sculpture
and anterior lateral teeth is known in
the Condylocardiidae which .are repre.sented by Condylowrdia BERNARD, 1896,
Carditella SMITH, 1881, · and a few othergenera in the Cenozoic and Recent. Although little has ·been known about theirMesozoic ancestors, it is possible thatfossil representatives of· this family havebeen overlooked, .because the shell-size i,sgenerally very small . in the known
species. In some characterS!·Tutcheria issimilar to Carditella, but the former
differs from the latter in the worse
developed cardinal tooth 3a and moreprosogyrous umbo.
Eventually I am inclined to conclude.that Tutcheria may have been derived
from a certain common root of the
Carditidae and the Astartidae but thatit had better be referred, if anything, to
the Carditidae as done by some previous
authors and recently by VoKES (1967,
p. 257). It is interesting to see that
Cardita cloacina sibirica KIPARISOVA,
1966, from the Norian of east Siberia has
Tutcheria-iike concentric rings on thesurface. Further discovery of the direct
ancestors of Tutcheria in the Triassic
would make its systematic position more
distinct.

Tutcheria itoi sp. nov.
Pl. 3. figs. 1-5

Material.-The holotype (GK. G6882) isan external mould of left valve from thelower part of the Higashinagano formation at Joe. It. 108, Higashinagano.
Six paratypes (GK:· G6860-GK. G6865)
from the same locality.
Diagnosis.-Medium-sized and noncarinated species of Tutcheria, characterized by the subor-bicular outline,
prosogyrous and comparatively narrowumbo, narrow lunule, strongly impressed
adductor scars and about 45 radial ribs
which are interrupted by a few widely
spaced and strong imbrications of growthstages on the middle-ventral surface.
Description.-Shell medium-sized forthe genus, ·about 12mm long in thelargest specimen,. suborbicular in outline,
nearly as high as long; strongly inflated,never carinated; test moderate in thickness; antero-dorsal. margin . concave infront of umbo, fairly long, passing

549.

Tutcheria from the Jurassic

gradually into the anterior. margin;postero-dorsal margin comparatively
short, gently arcuate; ventral margin
evenly rounded; umbo comparatively
narrow, prosogyrous, rising a little above
the hinge marg\n, placed at about threesevenths of length from the anterior
end; lunule narrow but deep,. delimited
by a weak ridge; escutcheon probably
not demarcated ; ligament opisthodetic,
external; surface-ornamented with about
45 fine regular radial ribs which arenearly as wide as their interspaces; afew strong and widely spaced imbrications, which indicate some growthstages, interrupting the radials on the
middle-ventral surface, although their
number and interval are quite irregular;
ventral margin finely crenulated internally in accordance with the radial ribs;
hinge plate moderate in breadth, com-29

paratively short; ,dentition typical of
Tutcheria, ..generally as formulated:
AI 3b PI (Pili).
.
.
Ali. 2 - 4b-PIC- , cardmal teeth dtvergent
from the beak; 3a undeveloped at all; 2vertical, thin; 3b very large, triangular,
rounded at top ; 4b thin, adjacent to thenymph; lateral .teeth of both sides in
two valves short, clearly separated fromthe cardinal te,eth; .AI tuberculiform,
stronger than All; Alii not separated
from the antero-dorsal margin ; PI and Pilirelatively weak, separated from eachother by an oblong recess for the reception of the tubercular lateral tooth
PII; Pili not clearly separated from thepostero-dorsal margin ; adductor scars
subequal in size, oblong, strongly impressed; pallial line simple; umbonal
cavity moderate in depth.

l\1easurements in mm.Specimen
Holotype (GK. G6859) left ex. mould
Paratype (GK. G6860) left ex. mould
Paratype (GK. G6861) left ex. mould
Paratype (GK. G6862) left ex. mould
Paratype (GK. G6863) right in. mould
Paratype (GK. G6864) left in. mould
Paratype (GK. G6865) right in. mould

Observations and comparisons.-Four
external moulds including the holotype
reveal the characteristic surface ornamentation, though none of them arecomplete. Three internal moulds, fromwhich silicone rubber casts were taken
successfully, show a dentition of typical Tutcheria. The test is not preservedat all. Owing to the arenaceous matrix,
these specimens are almost free fromsecondary deformation, but further
biometrical studies seem to be difficult.
The present species may be closely
allied to Tutcheria nor:tonensis Cox, 1946,
from the Middle Lias of England. How-

Length
10. 2+
11.8
11.4+
11. 4+
12.4
10.8
12.6

Height11.4
11. 0+
11. 2+
12.6
12.2
10.8
11.8

Thicknessca. 3. 0
2. 8+
2.8+
ca. 3. 4
3.2+
2. 8+
3. 2+

ever, apart from its much larger size
the present species differs from the
British one in the more tuberculiform
anterior lateral tooth AI, less elongatedposterior lateral tooth PII and narrower
hinge plate. ·Tutcheria cingulata (GOLDFUSS, 1837) from the Lower Lias ofWi.irtemberg and England (Cox, 1946)
also resembles the present species, but
the ratio of length/height is distinctly
larger in the former than in the latter.
Tutcheria heberti (TERQUEM, 1855) fromthe Lower Lias of France (DUMORTIER,
1864) and England (Cox, 1946) shows
comparable size and number of radials

:30

ltaru HAYAMI

with the present· species. The radials.and concentric imbrications, however,are apparently much weaker than in any.of the present specimens.
Cox (1946) proposed at the same time
the genus Pseudo pis (type-species: Pseu.dopis astonensis Cox, 1946) for three
Lower Jurassic · species which have
Tutcheria-like structure and more or less:sharp carina. According to Cox there.are some species intermediate between
Tutcheria and Pseudopis, and the derivation of the latter from the former is:suggested. The present species, how-ever, has no affinity with Pseudopis.
Occurrence.-All the present specimens were collected by M. ITO from aweathered sandstone of the basal memberof the Higashinagano formation (Nbs
bed by MATSUMOTO and ONO, 1947, or
Cardinia toriyamai bed by HAY AMI, 1959)
at loc. It. 108, a small valley, about 500
m southeast of Narusebashi, Higashinagano, Toyoda town, Toyora County,
Yamaguchi Prefecture. The present
species is accompanied by Oxvtoma(Oxytoma) inequivalvis (SOWERBY), Meleagrinella japonica HAY AMI, Chlamys
textoria (SCHLOTHEIM), Entolium sp. cf.
E. calvum (GOLDFUSS), Plagiostoma
matsumotoi
HAY AMI,(Plagiostoma)Sphaeriola nipponica HAY AMI and Pholadomya sp. The age is probably Sinemurian, because an Arietites-like ammo----~~~-~--·~~~~-~~~-

Explanation of Plate 3
Figs. 1- 5. Tutcheria itoi sp. nov ....................................................... p. 28
1. Left external mould, GK. G6862 (la) and its rubber cast (lb), paratype, x2.
2. Left external mould, GK. G6859 (2a) and its rubber cast (2b), holotype, x2.
3. Rubber cast of two left external moulds, GK. G6860 (lower) and GK. G6861 (upper),para types, x 2.
4. Right internal mould, GK. G6863 (4a) and its rubber cast (4b), paratype, x2.
5. Left (lower) internal mould, GK. G6864 and right (upper) internal mould, GK. G6865,(5a), and their respective rubber casts (5b, 5c), paratypes, x2.
All the specimens were collected by M. ITo from the basal part of the Higashinagano formation at It. 108, Higashinagano, Toyoda town, Toyoda County, Yamaguchi Prefecture.
Figs. 6-11. Oxytoma (Oxytoma) mojsisovicsi TELLER .................................... p. 35
6. Left valve, GK. F6887, x 1.5.
7. Rubber cast of a left external mould, GK. F6888, x 2.
8. Left internal mould, GK. F6889, x 2.
9. Left valve, GK. H6890, x 2.
10. Left external mould, GK. F6885 (lOa) and its rubber cast (lOb), x 1.
11. Rubber cast of a right external mould, GK. F6886, x 1.5.
Fig. 12. Chlamys (?) sp. indet. . ....................................................... p. 36
12. Right valve, GK. F6891, x 2.
Fig. 13. Pseudolimea naumanni (KoBAYASHI and IcHIKAWA) .......................... p. 37
13. Left valve, GK. F6892, x 2.
Fig. 14. Astarte sp. indet ............................................................... p. 38
14. Right valve, GK. F6894, x 2.
The specimens illustrated in Figs. 6, 9, 12, 13, 14 were collected by OzAWA from lenticular limestone of the Tachigaya formation at Tachigaya, Orne City, Tokyo Prefecture, those'in Figs. 7, 8, 10, 11 by OzAWA and HAYAMI from the adjacent calcareous sandstone at the.same locality.

I-!A YAM T :Plate 3T~itche1·ia jr01n0Zf\ WA cmd }[AYAMJ :the Jurassic
Triassic Oxytoma bed f1·o 11~ J(wa%to

4a

5b

Sa

549.

Tutcheria from the Jurassic

nite was collected from thesandstone at another locality.

same

References
BERNARD, F. (1895) : Premiere note sur ledevelopment et Ia morphologie de Ia
coquille chez les lamellibranches. Bull.
Soc. geol. France, [3], 23, (3), 104-154.
BITTNER, A. von (1895) : Lamellibranchiaten
der alpinen Trias. I. Revision der Lamellibranchiaten von St. Cassian. Abhandl.
Geol. Reichsanst., 18, (1), 1-236, pis. 1-24.
Cox. L. R. (1947) : Tutcheria and Pseudopis,
new lamellibranch genera from the Lias.
Proc. Malac. Soc. London, 27, (1), 34-48,
pl. 3.
- - (1962) : New genera and subgenera of
Mesozoic Bivalvia. Palaeontology, 4, (4),592-598.
DouVILLE, H. (1913) : Classification deslamellibranches. Bull. Soc. geol. France,[4], 12, (4), 419-467.
- - (1921) : La charniere dans les lamellibranches heterodontes et son evolution.
Ibid., [ 4], 21, 116-124.
GoLDFuss, A. (1833-1840) : Petrefacta Germaniae. Bd. II. 312 pp., pis. 72-165.
HAY AMI, I. (1958) : Taxonomic notes on
Cardinia with description of a new species
from the Lias of western Japan. jour.

Higashinagano
Ishimachi
Toyoda town

31

Fac. Sci., Univ. Tokyo. [2], 11, (2), 115130, pl. 11.
- - (1959) : Lower Liassic Lamellibranchfauna of the Higashinagano formation inwest Japan. Ibid., (2), 12, (1), 31-84,
pis. 5-8.
- - (1965) : Lower Cretaceous marine pelecypods of Japan. Part II. Mem. Fac.
Sci., Kyushu Univ., [DJ, 17, (2), 73-150,
pis. 7-21.
KIPARISOVA, L. D., BYCIIKOV, J. M. and
PoLUBOTKO, I. V. (1966) : Late Triassic
Bivalvian Mollusca from east Siberia,
USSR. 312 pp. (40 pis. incl.) All Soviet
Union Geol. Inst. (VSEGEI) (in Russian)
MATSUMoTo, T. and O:xo, A. (1947): A
biostratigraphic study of the Jurassic
Toyora group, with special reference toammonites. Sci. Rep. Fac. Sci., Kyushu
Univ., Geol., 2, (1), 20-33 (pis. 1-2 incl.)(in Japanese).
Vor<Es, H. E. (1967) : Genera of the Bivalvia:
a systematic and bibliographic catalogue.
Bull. A mer. Paleont., 51, (232), 111-394.
WRIGLEY, A. (1946) : Observations on the
structure of lamellibranch shells. Proc.
Malac. Soc. London, 27, (1), 7-19.
YEHARA, S. (1921) : On some new speciesof Trigonia from the Lias of Prov.
Nagata and the Cretaceous of Prov. Awa.
jour. Geol. Soc. Tokyo, 28, (329), 7-12,
pl. 1.

cw: ·& !J!f)
Ui

IIIJ)

c~~J:

1n IIIJ)

Trans. Proc. Palaeont. Soc. Japan, N. S., No. 73, pp. 32-40, pl. 3, April 30, 1969

550.

TRIASSIC OXYTOMA BED IN THE SUBURBS OF
OME CITY, KW ANTO MOUNTAINS*TOMOWO OZAWA and IT ARU HAY AMI
Department of Geology, Kyushu Universitym:'Pffiifip';(~?'H:::.§e~~ht..::=:i:Hc Oxytoma}l:[~ffll""f-FH~rtJ~tl§)j*':J 4 km OJ:i'l.-7~
iWiM1i!I~:::.J:It~tl$.f1:;0)J:il!.Jiiv:::.JfJi/i't"l'i ~ 7;.1: 'Hot..::=:JlH'F-O)f~'Ht 5J;ffi"iit9<n Ght..:. ~Jli[f:':J110m ~:::.~ l , :s'l.-T~Ji.'i c O}'!v"C·tJ$,/Wii>I~:>IK]}I]T Q 0 ::;j;::N/f'i::Ec VCli'}!E · 'W!Gii' Gt.J: f),
9=> tfflfCti" Jj)(!GO),j\1./ :/ 7--'l!:'ffi" Q o 4-@1, I: O);p" Ek!G :to J:: t:Pt 0) J:ilz: v:::.t,Jt 1Ci Ek 'W:u;P'Eiii' G<

Oxytoma (Oxytoma) mojsisovicsi, Pseudolimea naumanni 1!:'15-tr=t~~ll'fi.l~§e~ ~ hf-::o
I: O)WiilX:v:t:=:\lHcf&JtJJ (:to-1:- G 7J- =- T :/) ~!:'~ l, ::;j;::JW'd::'il.§i¥l 13 ::;j;::?'\-11\'0)JIIi*J-7~ffilf,¥""f<i~~~:::.xtrti"Q c. u~nrtJ8--c·<bQo,J, iR ~ ±·ill! 7Jc

Hi

Pseudolimea naumanni (KOBAYASHI andICHIKAWA)
Astarte sp. indet.
Because the first and third species have

TAKAGI (1944) reported the occurrenceof a specimen of Monotis (Entomonotis)
ochotica from a conglomeratic sandstone
exposed near the jNR station of Ishigamimae (formerly called Rakurakuen)
in the Orne area, Tokyo Prefecture.
However, little has been known about
the exact distribution of Triassic strata·in this area, because no more fossil occurrence prevents ones from discriminating them from the surrounding Carboniferous-Permian strata of the Chichibu
terrain.
In the field survey of the Upper Paleozoic strata one of us (T. 0.) discovered
unexpectedly a characteristic limestonelens bearing fossil bivalves and someother marine organisms near the hamletof Tachigaya, about 4 km northwest of
the center of Orne City (Fig. 1). The
other of us (I. H.) jointly examined thecollection and identified the following
bivalves:
Oxytoma (Oxytoma) mojsisovicsi TELLER
Chlamys (?) sp. indet.

140"'· .......... ·f ...... "".

Hinodeyama0._.........

2km

902

Fig. 1. Map showing the locality offossils and the distribution of the Tachigaya
formation.

* Received Oct. 18, 1968; read Nov. 30,
1968 at Shizuoka.

32

550.

Triassic Oxytoma becl from Kwanto

been known on ly from the Upper Triassic (mainly Carnian ) in japan and East
Siberia, we regard the fossil bed inquestion as Upper Triassic (Carnian if
not Norian ). The fossil bearing strata
is denominated here the Tachigaya formation. The aim of this paper is todescribe the stratigraphy and fossi ls of
this formation in some detail.
Before going into description, we express our sincere thanks to Prof. Tatsuro
MATSUMOTO and Prof. Ryuzo TORIYAMAof the Ky ushu University for their kindness in reading the manuscript. Acknowledgements are also due to Prof.

33

Emeritus Teiichi KOBAYASHI of the
University of Tokyo for his generous
advice in the Triassic stratigraphy andpaleontology, to Dr. Kametoshi KANMERA of the Ky ushu University for his
valuable suggestion on the fie ld workand also to Miss Seiko HAYAKAWA for
her assistance in drafting.

Stratigraphic notes

In the Orne area of southeast Kwanto
mountains Upper Pa leozoic rocks arewidely distributed, showing a general

L egend)<:'--,____,___
L.O m

m

Fossil occurrence
Fa u l t
Limestone

30

~

20

J::: >\ Sandstone

Mudstone0

Fig. 2. Idea lized columnar section of
the Tachigaya formation.

Fig . 3. Limestone (bivalve biosparudite) of the Tachiga ya formation at
the southern bank of Kitaosoki river,
Tachigaya ( x 10). Numerous bi val vi anshell fragments cemented by sparrycalcite.

:34

Tomowo OZAWA and ltaru HAYAMI:strike of NW -SE or NWW -SSE. Several
striking thrust faults are developed inparallel to the general trend and divide
these rocks into many belts. Zonal distribution of formations is well recogniz·ed in this area as usual in the Kwanto
mountains and also in the Outer Zone·of Southwest Japan. The newly discovered Triassic strata are situated in abelt of Carboniferous and Permian formations, which is here called the Raidenyama belt. As shown in Fig. 1, theTriassic strata, denominated the Tachigaya formation in this paper, are narrowly distributed along the Kitaosoki
river in the environs of Tachigaya.
The Tachigaya formation itself forms
a synclinal structure with a generalstrike of NW-SE dipping to the north·or south at angles as high as 70 or 80
degrees. The northern and southernborders are cut by faults, and the Trias·sic strata are in contact with the Upper
Carboniferous Kitaosoki formation on
the north and with the Lower-Middle
Permian Raidenyama formation on thesouth.
The Tachigaya formation is composed·of black shale with subordinate fine- tomedium-grained sandstone in the lower
part (ca. 45 m) and of thickly bedded
medium- to coarse-grained sandstone
with occasional granule conglomerate
and thick black shale in the upper part(ca. 65 m). A small lens of dark grayshell limestone (ca. 1.5 m) with sparrycalcite cement occurs in the lower portion of the upper (Figs. 2 and 3). It
gradually becomes sandy and passes
into calcareous sandstone. The fossil
beds are best seen on the southern bank·of the Kitaosoki river at Tachigaya, thetype locality of this formation.
Oxytoma (Oxytoma) mo)stsoVtcst is
especially abundant in the limestone andcalcareous sandstone, although most of

the individuals are fragmentary andprobably immature. In the same limestone Pseudolimea naumanni, Chlamys (?)
sp., Astarte sp., and indeterminablespecies of brachiopod and echinoid arealso contained. Incidentally, such ashelly limestone has never been foundin the Upper Paleozoic formations of
this area.

Description of fossils

Class Bivalvia
Order Pterioida
Family Oxytomidae IcHIKAwA, 1958
(nom. trans!. by Cox, 1962,
ex Oxytominae ICHIKAwA, 1958)

Genus Oxytoma MEEK, 1864
Subgenus Oxytoma s. str.
The generic diagnosis of Oxytoma wasclearly given by ICHIKAWA (1958) andCox (1962). This genus is composed ofthree subgenera, Oxytoma (s. str.), Hypoxytoma ICHIKAWA, 1958, and Palmoxytoma Cox, 1962. All the Triassic speciesof Oxytoma from Japan seem to belong
to Oxytoma (s. str.).
Oxytoma (Oxytoma) mojsisovicsi TELLER
Pl. 3, figs. 6-11
1886. Oxytoma mojsisovicsi TELLER in MOJSIsovics, Mem. Sci. St. Petersbourg, ser.
7, vol. 33, no. 6, p. 129, pl. 19, figs. 7, 8.
1927. Pseudomonotis zitteli: YEHARA, japan.
jour. Geol. Geogr., vol. 5, nos. 1-2, p.
30, pl. 4, figs. 7, 8.
1927. Oxytoma zitteli: YEHARA, Ibid., vol. 5,
nos. 1-2, p. 32, pl. 4, figs. 9, 10.
1950. Oxytoma zitteli: KoBAYASHI and lciii-

550.

1950.

1950.

1957.

1959.

1959.
1963.

1964.

1966.

Triassic Oxytoma bed from Kwanto

KAWA, jour. Fac. Sci., Univ. Tokyo,
ser. 2, vol. 7, pts. 3-5, p. 220, pl. 2,
figs. 3-6.
Oxytoma subzitteli KoBA YASI-II and IcH I·
KAWA, Ibid., sec. 2, vol. 7, pts. 3-5, p.
221, pl. 2, figs. 7, 8.
Oxytoma yeharai KoBAYASHI and lcHI·
KAWA, Ibid., sec. 2, vol. 7, pts. 3-5, p.
222, pl. 2, figs. 1, 2, pl. 3, fig. 13.
Oxytoma subzitteli: NAKANO, jour. Sci.,
Hiroshima Univ., sec. C, vol. 2, no. 1,
p. 64, pl. 9, fig. l.
Oxytoma zitteli: ToKcYAC>.IA, japan.
jour. Geol. Geogr., val. 30, p. 7, pl. 1,
figs. 19-21.
Oxytoma subzitteli: ToKUY AMA, Ibid.,
vol. 30, p. 8, pl. 1, figs. 23, 24.
Oxytoma cf. subzitteli: NAKAZAWA,
Mem. Coli. Sci., Kyoto Univ., ser. B,
vol. 30, no. 2, p. 54, pl. 2, figs. 10-12.
Oxytoma cf. subzittel: NAKAZAWA,
Ibid., ser. B, vol. 30, no. 4, p. 36, pl. 5,
figs. 6-8.
Oxytoma mojsisovicsi: KIPARISOVA in
KIPARISOVA, Buciii<ov and PoLU·
BOTKO, Late Triassic Bivalve Moll. Fast
Siberia, p. 31, pl. 2, figs. 14, 15, pl. 3,
fig. 2 (with a list of complete synonymy
in USSR)

Material.-Although most of the specimens are fragmentary, the external features of adult valves are shown in two
external moulds (GK. F6885, GK. F6886).
In addition four other smaller specimens{GK. F6887-GK. F6890) are available forthe descriptive study.
Description.-Shell moderate or rather
large for the genus, highly inequivalve.

35

The left valve moderately inflated, pteriform, prosocline, provided with ten to
twelve prominent primary radial ribs,
which are highly elevated and sometimes slightly spinose; each interspaceof primary ribs divided subequally into
two parts by a secondary rib which isclearly discriminated in prominence fromnumerous fine tertiary ribs; ribs slightly
curved outwards in the anterior and posterior areas; anterior wing comparatively
small; posterior wing flattened, as
broad as the main part, provided withnumerous weak radial riblets of the tertiary strength, pointed backwards; umbo
nearly orthogyrous, comparatively narrow, rising a little above the hinge line,
placed at about one-fifth of hinge linefrom the anterior end. Right valve, on
the contrary, nearly fiat except for theslightly convex umbonal area; byssal
auricle of moderate size, clearly demarcated by a deeply incised subauricularnotch; ctenolium not observed; surface
marked with numerous fine radial ribletsof a single order of prominence; posterior wing not clearly defined, provided
with one or two blunt oblique ridges
near the dorsal periphery. Hinge, ligament and musculature not observable in
the present material.
Observations and comparisons.-As theavailable specimens are mostly fragmentary and poorly preserved, it is not readily realized that they belong actually
to one species. However, we think so,-----------------------

JV!easurements in mm.
Specimen
Left ex. mould (GK. F6885)
Right ex. mould (GK. F6886)
Left valve (GK. F6887)
Left ex. mould (GK. F6888)
Left in. mould (GK. F6889)
Left in. mould (GK. F6890)

LengthHeightThickness

48.5
27.5
10.5
9.0+
14.5
8.5+

53.5
25.0
6. 5+
9.5
11. 5+
8.5+

ca. 11. 0
ca. 3.5
ca. 2.5
ca. 2.0
ca. 3.5
ca. 2.5

36

Tomowo OZAWA and Itaru HAYAMI

because the mode of radial ornamentation of the left valves is essentially thesame and because they were extracted
from crowded fossil banks in a limestone lens and adjacent calcareous sandstone at the same locality.
The present specimens, especially thetwo larger ones (GK. F6885, GK. F6886),
are quite similar to Oxytoma mojsisovicsi
TELLER, 1886, from the Upper Triassicof East Siberia. Int he Sakawa basinof Shikoku and other areas of Japan
similar specimens were described by
KOBAYASHI and ICHIKAWA (1950) andothers under the name of Oxytoma zitteli(TELLER), Oxytoma subzitteli KOBAYASHI
and ICHIKAWA or Oxytoma yeharai KOBAYASHI and ICHIKAWA. As NAKAZAWA(1963, 1964) suggested already, Oxytoma
zitteli (TELLER) (=Pseudomonotis zitteli
TELLER) from Siberia may be specificallydistinct from "Oxytoma zitteli" fromJapan, which is probably conspecificwith Oxytoma subzitteli. Furthermore,
KIPARISOVA in KIPARISOVA, BUCHKOV
and POLUBOTKO (1966) regarded "0. zitteli" and 0. yeharai by KOBAYASHI andICHIKAWA respectively as a synonym
and a variety of 0. mojsisovicsi. Accepting her opinion, we refer the present specimens to Oxytoma ino/sisovicsi,
which actually includes "0. zitteli ", 0.
subzitteli and 0. yeharai. The' numberof radial ribs and the form ratio are
general}y fairly variable in one speciesof pt'eri'oids, and the insignificant difference between these nominal species
may not serve even as a subspecificcriterion.
Another problem has arisen for many
years as to the relationship between
Oxytoma mojsisovicsi and Pseudomonotis
zitteli, since TELLER (1886) described
originally the former species on thebasis of left valves and the latter on
the basis of a right valve. We agreewith KOBAYASHI and ICHIKAWA (1950)
in considering that the specimens fromthe Sakawa basin, which YEHARA (1927)
described under these two specific names,
are actually conspecific. However, weare not in a position to discuss thisproblem on the basis of their typespecimens.
Occurrence.- Lenticular limestone andsuperjacent calcareous sandstone of theTachigaya formation at the southernbank of Kitaosoki river, near the hamletof Tachigaya, Orne City, Tokyo Prefecture. OzAwA and HAY AMI coiL
Family Pectinidae RAFINESQUE, 1815
Genus Chlamys RoDING, 1798
Chlamys (?) sp. indet.
Pl. 3, fig. 12This species is represented only by asmall left valve (GK. F6891, 7.5 mm long,
8.5 mm high) from the same lenticular
limestone as the preceding species. The
anterior wing is much larger than theposterior, suggesting the development of
a byssal auricle in the counter valve.
The surface is marked with numerous
faint radial riblets. It belongs to thesubfamily Chlamydinae, but at present
the generic assignment is uncertain andthe specific identification impossible. The
general outline is somewhat similar tothat of Chlamys mojsisovicsi KoBAYASHI
and ICHIKAWA, 1949, from the Carnianof Shikoku. The present species, however, differs from that in the larger
apical angle and more delicate radial
rib lets.
Family Limidae RAFINESQUE, 1815
Genus Pseudolimea ARKELL, 1932
Pseudolimea naumanni (KoBAYASHI

550.

Triassic Oxytoma bed from Kwanto

and ICHIKAWA)
Pl. 3, fig. 13
1939. Lima naumanni lata KATAYAMA, jour.
Ceo!. Soc. Japan, val. 46, no. 546, p. 135(nom. nud.).
1939. Lima naumanni obliqua KATAYA~IA,
Ibid., val. 46, no. 546, p. 135, pl. 8, fig.
6 (nom. nud.).
1949. Lima naumanni KoBAYASHI and IcHIKAWA, japan. jour. Ceo!. Ceogr., val.
21, nos. 1-4, p. 177, pl. 6, figs. 13-15.
1949. Lima naumanni var. obliqua KoBAYASHI
and IcHIKAWA, Ibid., val. 21, nos. 1-4,
p. 178, pl. 6, figs. 16, 17.
1952. Lima (Pseudolimea?) naumanni: NAKAZAWA, Mem. Coil. Sci., Univ. Kyoto,ser. B, val. 20, no. 2, p. 102, pl. 9,
figs. 7, 8, pl. 10, fig. 3.
1954. Pseudolimea? naumanni: lcH!KA ,,.A,
jour. Inst. Polytec. Osaka City Univ.,
ser. G, val. 2, p. 55, pl. 3, fig. 12.
1954. Pseudolimea? naumanni var. obliqua:
lciiiKAWA, Ibid., val. 2, p. 56, pl. 3,

37

fig. 11.

Material.-A left valve (GK. F6892)
and an internal mould of right valve( GK. F7893).
Description.-Shell medium in size, inequilateral, opisthocline, trigonally ovate,higher than long, strongly inflated ; testcomparatively thin; umbo placed posteriorly from the mid-length of shell, notprominent, with an apical angle of about
75 degrees; auricles depressed, probably
of moderate size; anterior umbonal ridge
absent; no "lunule"; surface of main
body ornamented with about 19 straight,
roof-shaped, plicated and non-bifurcatedradial ribs, interspaces of which aremarked respectively with a faint secondary rib; growth-lines crossing theradial ribs, distinct especially near theventral periphery, giving rise to serration in accordance to the radial ribs;
internal structure not observed.

A1easurements in mm.
Specimen
Left valve (GK. F6892)
Right in. mould (GK. F6893)

Observations and comparisons.- Theleft valve is well preserved and shows
the characteristic ornament in detail,though both auricles are incomplete. It
is quite similar to the holotype andpara types of Lima naumanni KoBAYASHI
and ICHIKAwA, 1949, from the Carnianof the Sakawa basin of Shikoku. The
right internal mould (GK. F6893) is rather
similar to the specimens called Lima
naumanni var. obliqua KOBA YASH! andICHIKAWA, 1949, in view of the somewhat
obliquely elongated outline. Because of
the suggested sympatric relation at
many localities (KATAYAMA, 1939; KoBAYASHI and ICHIKAWA, 1949; ICHIKAWA,

Length17.5
17.5

Height19.0
19.5

Thicknessca. 5. 0
ca. 4. 0

1954; etc.), the "variety" may not constitute a distinct subspecies.
The reference of the present species
to the genus Pseudolimea has been suggested by NAKAZAWA (1952) and ICHIKAWA (1954). As pointed out by IC:HI·
KA w A (1954) on a specimen from the
Sakuradani area of Shikoku, many important characters of the present species
agree with the diagnosis of Pseudolimea
given by ARKELL in DOUGLAS and
ARKELL (1932) and Cox (1944). However,
the resilifer appears to be much narrower and more prosocline in the present species than in many Jurassic
species of Pseudolimea. It is an inter-38

Tomowo OZAWA and !tarn HAYAMI·

esting fact that Triassic Mysidioptera
has similarly a narrow and prosocline
resilifer in comparison with Jurassic
Plagiostoma. Because Plagiostoma is believed to have been derived from Mysidioptera (Cox, 1943, 1952), it is probablethat a comparable transformation ofligament structure occurred in the evolutionary history of Pseudolimea. Fromthe present material, however, no further
knowledge could be obtained about theligament structure, and we regard provisionally the present species as an early
member of Pseudolimea.
Occurrence.-Lenticular limestone of
the Tachigaya formation at the southernbank of Kitaosoki river near the hamletof Tachigaya, Orne City, Tokyo Prefecture. OzAwA coli.

Order Veneroida
Family Astartidae D'ORBIGNY, 1843
Genus Astarte SOWERBY, 1816
Astarte sp. indet.
Pl. 3, fig. 14

This species is represented by fiveminute specimens (GK. F6894-GK. F6898)
from the same lenticular limestone as
the preceding. The length of the largest
specimen scarcely exceeds 7 mm. Although the hinge structure is not observable, it belongs undoubtedly to the genus
Astarte of wide sense, judging from thegeneral outline, clearly excavated lunuleand the distinct concentric ribs on theumbonal area. This species differs from
Astarte? iwayai IcHIKAwA, 1954, fromthe Carnian of Shikoku in the smallersize, less triangular outline and more
densely spaced and narrowly restrictedconcentric ribs. So far as we are aware,
there is no comparable species of Astartein the Triassic, while the present species.
looks somewhat similar to some small
Jurassic and Cretaceous species ofAstarte (s. str.) such as Astarte (Astarte}semicostata NAGAO, 1934, from theAptian-Albian of north Japan.
Concluding remarks
In the northwestern suburbs of Orne
City, Tokyo Prefecture, there is a narrow distribution of Triassic strata, which
are denominated here the Tachigaya
formation. As described above, thisformation is partly calcareous and contain some fossil bivalves and otherorganisms in a lenticular limestone and.
superjacent calcareous sandstone. Thisfaunule comprising Oxytoma (Oxytoma)mojsisovicsi and Pseudolimea naumanni
indicates an Upper Triassic (probably
Carnian) age at least for the fossiliferous
part.
Incidentally, the genus Oxytoma ranges.
widely from the Lower Triassic to theUpper Cretaceous, but Lower and Middle
Triassic species seem quite rare. In
Eastern Asia such large specimens as.
the present ones have been known only
from the Upper Triassic. Oxytoma(Oxytoma) mojsisovicsi itself has beenreported from the lower part of the
Kochigatani group at Sakawa and Sakuradani-Kito areas, the Kyowa formation of the Nariwa area and the lower
part of the Mine group of the Ominearea. Although some identifiable specimens with this species were described
also from such Norian Monotis-bearing
strata as the ]ito formation of the
Nariwa area (NAKAZAWA, 1963) and theupper part of the Saragai group of the
Shizukawa area (NAKAZAWA, 1964), it iscertain that 0. (0.) mojsisovicsi shows anacmaeic prosperity in the Carnian stage
in japan as well as in East Siberia ..

550.

Triassic Oxytoma bed from Kwanto

As pointed out by lcHIKA w A (1958, p.
163), "Oxytoma sp. aff. 0. mojsisovicsi"
described by CHEN (1950) from the Lower
Triassic of southeast China is probablyreferable to Eumorphotis.
The occurrence of Pseudolimea naumanni also supports the assignment of
the fossiliferous part to the Carnian,because this species has been known
only from the Carnian such as the lower
part of the Kochigatani group in the
S:ikawa and Sakuradani-Kito areas, thelower part of the Mine group of the
Omine area and the Nabae group of the
Maizuru area. NAKAZA w A (1956) suggested that this species characterizes theupper part of the Sakawan ( ·. Carnian)sediments in the Maizuru area.
Although the constituent species ofthis faunule is few, the assemblage isundoubtedly of the lower Kochigatani
fauna. It has been known that the
Kochigatani group in the Outer Zone ofSouthwest Japan is partly calcareous.
For instances, the "Oxytoma-Mytilus
beds" at Okunominetani of the Sakawa
area are fairly calcareous (KOBAYASHI
and ICHIKAWA in Geol. Surv. Japan, 1951,
p. 101), and, moreover, the "Proarcestes
beds" at Yoshinosakadani of the Taho(=Tao) area and the Tanoura formationof the Tanoura area bear occasionallysome lenses of impure limestone (IcHIKAWA in Geol. Surv. Japan, 1951, p. 109;
MATSUMOTO and KANMERA, 1964, p. 57).
In the Kwanto mountains the Arai formation of the ltsukaichi area, which is
generally regarded as Carnian if not
Norian, has also some impure limestonelenses (ICHIKAWA and Kuoo in Geol.
Surv. Japan, 1951, p. 29), although its
bivalvian assemblage is quite different
from that of the Kochigatani fauna(ICHIKAWA, 1954a).
To sum up we have come to the conclusion that the Tachigaya formation

39>

is a representative of the lower part of
the Kochigatani series in the southern
Kwanto mountains. We have, however,.
on positive evidence to determine its
stratigraphic relation to the Monotisbearing formation of the present area
and to the Arai formation of the ltsukaichi area, because they are distributed
separately in narrow areas.
References
Works cited only in the lists of synonymy
are omitted here.
CHEN, P.-Y. (1950): On the marine Triassic
fauna of Lungyen and Ningyang, Fukien.
Quart. jour. Taiwan Mus., 3, (2), 82-97.
Cox, L. R. (1943) : The English Upper Lias.
and Inferior Oolite species of Lima. Proc.
Malac. Soc. London, 25, (5-6), 151-187,
pis. 6-29.
- - (1944) : On Pseudolimea ARKELL. Ibid .•26, (2-3), 74-88, pls. 2, 3.
- - (1952) : The
Jurassiclamellibranchfauna of Cutch (Kachh).
Palaeont ..
Indica, [9], 3, (4), 1-128, pis. 1-12.
- - (1962) : New genera and subgenera of
Mesozoic Bivalvia. Palaeontology, 4, (4),592-598.
DouGLAs, J. A. and ARK ELL, W. J. (1932) :The stratigraphical distribution of the
Cornbrash : 2. The north-eastern area.
Quart. jour. Geol. Soc. London, 88, 112170, pls. 10-12.
Geological Survey of Japan (1951) : Triassic
stratigraphy of japan.
Rept. Special
Number, Geol. Surv. Japan. 148 pp., 8
maps. [in Japanese]
lci-IIKA\VA, K. (1954): Late Triassic pelecypods from the Kochigatani Group in the
Sakuradani and Kito areas, Tokushima
Prefecture, Shikoku, Japan. Part 2. jour.
I nsf. Polytec. Osaka City U niv., [ G], 2,53-75 (pis. 3, 4 incl.)- - (1954a) : Triassic Mollusca from the
Arai Formation at Iwai near Itsukaichi,
Tokyo Prefecture. japan. jour. Geol.
Geogr., 24, 45-70, pl. 7.
- - (1958) : Zur Taxionomie und Phylogenie

40

Tomowo OZAWA and ltaru HAYAMI

der triadischen " Pteriidae" (Lamellibranch.) mit besonderer Beriicksichtgung
der Gattungen Claraia, Eumorphotis, Oxytoma und M onotis.
Palaeontographica,
111, (A), 131-212, pls. 21-24.
KIPARISOVA, L. D., BvcHKov, ]. M. and
POLUBOTKO, I. V. (1966) : Late Triassic
bivalvian Mollusca from east Siberia,
USSR. All Soviet Union, Geol. Inst.
(VSEGEI) · 312 pp. (40 pls. incl.). [inRussian]
KoBAYASHI, T. and IcHIKAWA, K. (1949):
Tosapecten gen. nov. and other Upper
Triassic Pectinidae from the Sakawa
basin in Shiko:w, Japan. japan. jour.
Ceo!. Ceogr., 21, 163-171, pl. 5.
- - and - - (1949a) : Myophoria and other
Upper Triassic pelecypods from the Sakawa basin in Shikoku, Japan. Ibid., 21,
177-187, pl. 6.
- - and - - (1950) : Triassic Oxytoma fromthe Sakawa basin in Shikoku, Japan.
jour. Fac. Sci., Univ. Tokyo, [2], 7, (35), 217-229, pls. 2, 3.
MATSUMOTO, T. and KANMERA, K. (1964):
Hinagu: Explanatory text of the geological map of Japan, scale 1:50,000.
Geol. Surv. Japan. 147+27 pp. [in Jap-

anese with an English abstract]
NAKAZAWA, K. (1952): A study on thepelecypod-fauna of the Upper Triassic
Nabae group in the northern part of
Kyoto Prefecture. Part 1. Pectinids andlimids. Mem. Coli. Sci., Univ. Kyoto,[BJ, 20, (2), 95-106, pls. 7-10.
(1956) : Op. cit. Part 4. Ibid., [BJ, 23,(2), 231-253, pls. 1-4.
- - (1963) : Norian pelecypod-fossils from}ito, Okayama Prefecture, west Japan.
Ibid., [B], 30, (2), 47-58, pls. 1, 2.
- - (1964) : On the Monotis typica zone inJapan. Ibid., [BJ, 30, (4), 21-39, pls. 3-5.
TAKAGI, Z. (1944) : On the discovery of
Pseudomonotis ochotica in the vicinity ofOrne town and a note on the geology ofthis area. jour. Ceo!. Soc. japan, 51,(609), 196-198. [in Japanese]
TELLER, F. (1886): Die Pelecypoden-Fauna
von Werchojansk in Ostsibirien.
In
MoJSisovics, E. v.: Arktische Triasfaunen. Mem. Acad. Imp. Sci. St. Petersbourg, [7], 33, (6), 103-137, pls. 17-20.
YEHARA, S. (1927) : Faunal and stratigraphical study of the Sakawa basin, Shikoku. japan. jour. Ceo!. Ceogr., 5, (1-2),
1-40, pls. 1-5.
----~----

lshigamimae
Kitaosoki

1:j

t1!1

;Jt.'l' ~

AIJ

*

Orne
Tachigaya

,[];

r'J'
:lL

till:
?-

1§-

Trans. Proc. Palaeont. Soc. Japan, N.S., No. 73, pp. 41-:48, pls. 4-6, April 30, 1969

551. PLANT MICROFOSSILS FROM THE PERMIANSANDSTONE IN THE SOUTHERN MARGINAL
AREA OF THE TANBA BELT*KIYOSHI TAKAHASHI
Department of Geology, Nagasaki University

and
AKIRA YAO
Department of Geosciences, Osaka City University:Pti&:;:g=l{'i¥¥<$0)-";t.-A r.cuY:Ei~li!l~f~Jfti:J: ~if G0 ) - A., i\P§f:J:."),Cr;[IJH1-II~'iL'f>;fi13RIUJ
C:t t.:f:J:.jR1~dW Jt.O)i,/ifrfMr/1) 0)-" IvA $cireti~ <i=' 0) v :/ 7-'ikJi;J;'fi:.p G
M&O)Hti!!Jf.lii~ft::fi~tn:±l u.:, ~:'JYGO)ffuo)-A., i'hit~f:J:.c.;f1.,GO)iWJit::&H.\li$~L-. :rnHc. L"L f:l:. ?Araucariacites gloria sus n. sp., ?Florinites sp. (?Cordaitales), Reticulatasporites joraminulatus n. sp. ~. T£ t.:: -cr 1 !! 1=1 7" 7 / !1 r :/C. !...- "C Tasmanites tanbaensis
n. sp. ~~f&)JrJL.-t:O)'"C'~cli&L $JF6-t0,~t,TI; ii!i · AP§ Sr3
m:Ll.i~t);O)J'Ji&:1ll'Nmn"fll

Introduction

Education]. Consequently, the authors
have here reported and described three
species of sporomorphs and one speciesof phytoplankton. This paper is thefirst report on the Paleozoic sporomorphs
and phytomicroplankton in japan.
The authors wish to thank Professor
Dr. Koichiro ICHIKAwA, Department ofGeosciences, Osaka City University, for
his suggestion and valuable advice on
the stratigraphic relation and geologic
age, Professor Dr. Misaburo SHIMAKURA,
Nara Univeraity of Education, for hiskind direction of analytical method, andProfessor
Dr. Hermann
WEYLAND,
Wuppertal-Elberfeld (West-Germany), for
his kind suggestion on botanical speciesof the epidermal cell.

The junior author, A. Y AO, has collected samples from lenticular sandstonesin the Permian mudstone member inthe southern marginal area of the Tanba
belt. Mechanical and chemical treatment of the samples were carried out
by him under the direction of Professor
M. SHIMAKURA, Nara University of Education and he has found many plantmicrofossils under the microscope.
The senior author, K. TAKAHASHI, has
minutely observed some sections which
the junior author has provided and preliminarily studied [Y AO, 1966 (MS) Graduation Thesis, Nara University of* Received October 28, 1968; read June 22,1968 at Sendai.

41

Kiyoshi TAKAHASHI and Akira YAO

42

Geologic setting

The strata distributing in the Jubusen(Mt. Jubu) area, Kyoto Prefecture, aredivided into three formations, A, B, and134°

C, which are conformable each other(Y AO, 1968). The A formation is apparently lowermost and the C formation
is uppermost.
The A formation lies in the southern138°

Text-fig. la-b.
Index map(1a) and Geological map of Mt. Jubuarea, Kyoto prefecture (1b).
Text-fi;r. la.

3Ms[ill]

sB 10G 11[TI'::';::xt-fig. lb.

1. Equivalent of the Osaka Group(Plio-Pleistocene)
2. Tsuzuki Group (Miocene)
3. Granitic rocks (pre-Cenozoic)
4-8. Permian (divided into the Bandthe C formation)
4. Pelitic rocks
5. Cherts
6. Psammitic rocks
7. Submarine basic volcanics
8. Limestones
9. Fault
10. Boundary between the B andi
the C formation
11. Fossil localities
P: Plant microfossils, described in this paper.
F: Neoschwagerinids, reported by YAo (1968).

551.

Plant Microfossils from the Permianpart of this area and consists mainlyof mudstone intercalating chert andsandstone. The B formation is distributed in the central part of the area
and composed predominantly of mudstone
and chert with some sandstone beds, butbasic pyroclastic rocks and limestones
are very rare. Many spore-pollen grains
and phytoplankton were found from thefine to medium lenticular sandstone (3050 em in thickness) of this formation,
about 500m north of Harayama, Watsukacho. The C formation occupies the northern part of the area and mainly consistsof mudstone and sandstone with basic
pyroclastic rocks, limestones, and cherts.
Fusulinid fossil, Yabeina (or Neoschwagerina) sp., was found from the limestoneof this formation. Consequently, it isestimated that its geologic age will be
upper Middle Permian. As the B formation is seemingly lower than the Cformation, the geologic age of the former
will be naturally before upper Middle
Permian.
Preparation of material andmicrofossils
After crushing, the samples weremacerated in mixed solution with HNO.
and HCl, rinsed with water and thenboiled for a few minutes with 10% KOH
solution. The samples were then rinsed
repeatedly with water. Organic residue
in upper part of the precipitates wasconcentrated and subsequent oxidation(HNO.+HCl) and alkali (5% KOH) treatment were usually used. Finally concentrated HF was used for the purpose of
excluding minerals. The preparations
were mounted in glycerine jelly.
A number of specimens were foundunder the microscope. Above all, pollen
grains of ? Araucariacites gloriosus areabundant. They are similar to Florinites

43

belonging to Cordaitales from the Permian and Carboniferous, but they possess
no morphologic character which is recpgnized as air-sacs. On the other hand,
they are very similar to pollen grainsof Araucariaceae, but the latter is granulate in. ornamentation of exine. For thetime being, the authors report the present
specimens as ?Araucariacites gloriosus.
Only one pollen grain of ?Florinites
was found.
This is morphologicallysimilar to ? Araucariacites gloriosus, but
this has central body which is surrounded with air-sac ( ?).
Many species of Reticulatasporites
were reported from the Carboniferousof Germany and U.S. A. The present
Permian specimens belong certainly to
R eticulatasporites.
About Tasmanites there are some reports of A. EISENACK and others. The
present specimens are closely similar to
Tasmanites cf. tardus Eisenack which
was reported by S. MANUM (1964) fromthe Cretaceous of Graham Island andEllef Ringes Island of Arctic Canada.
The shell wall of Tasmanites tardus
Eisenack is far thicker than that of thejapanese species.
The epidermal cells illustrated in textfigure 2, coexisting with spores andpollEn grain::, cannot be exactly determined, because of the insufficient materials for reliable decision. However, thesematerials remine us of gymnospermous
plant.
Many
undeterminable microfossils
were also found, but these microfossils
are not dealt with in this paper.
All preparations are kept in the
Department of geosciences, Osaka City
University.
Systematic description
Anteturm:l:Pollenites

44

Kiyoshi TAKAHASHI and Aki1·a YAO

ab

Text-fig. 2a- b.

Epidermal cell ( lo wer cuticle) of gymnospermous plant ( ?) . x 420 .

R. POTONIE, l931
Turma:"S ubturma:

Aletes IBRAHIM, 1933
Azonaletes (LUBER 1935)

POTONIE & KREMP, 1954
Infraturma:

Granu lonapiti

COOKSO 1, 1947
Genus:

Araucariacites COOKSON, 1947

Type species:

A nzu c(l1'iacites

australis COOKSON, 1947
? Araucariacites gloriosus n. sp.
Pl. '1, figs. 1- 9; text-fig. 3a, b

Holotype :- Slide 66041104-13 ; Pl. 4,
fig. 3 ; size 133 x 100 ,u.
Type locality :-500 m north of Harayama, Watsuka-cho, Soraku-gun, Kyoto
Prefecture.
Type horizon :-Sandstone in the mudstone member of the B formation in the]ubusen area of the Tanba belt.
D escription :- Inaperturat e pollen
gra ins; shape ori g inally spheroidal oroval w ith diameter of 100 to 160,u.
Exine about 0.8 to 1.7,u thick w ith bothendexine and ektexi ne app roximately ofequal thickness, sculptured with rod-likeelements in optical section of the exine(see text-fig. 3a) an d w ith fine rugulate

Explanation of Plate 4
Figs. 1- 9. ?.4raucariacite s gloriosus n . s p .
Fig. 3: Holotype, s lide 66041104-13.

x 420.

TAJ\f1 JfASI{I a~d Yl\0 ;Plant Microfossils ,f1·on" (;h f3 P<3rmian

551.

Plant Mic?·ofossils from the Pe1·mian

45-

by its size and ornamentation.
Bota nica l affinity:- ? Araucariaceae.
Infraturma :Reticulorapiti (ERDT -MAN, 1947) VIMAL, 1952
Genus: R eticu lata spm·ites (IBRAHIM,.
1933) POTO NIE & KREMP, 1954
Type species: R eticulata spori tes
facetus IBRAHIM, 1933
Text-fig. 3a- b. Enlargement of the ornamen ta tion of ? Araucariacites gloriosus . x 1050.
3a : optica l section; 3b: s urfa ce of the ex ine.

arrangement on the surface of the ex in e(see text-fig. 3b) : rod-like (baculate orclavate) elements 1.3 to 1.7f-1 long. On
account of excessive folds the shape andsize vary greatly.
R emarks:- The present specimens are
similar to Inaperturopo llenites insignis
MA NUM (S . MA NUM, 1962, p. 39, pl. 6,
figs . 3, 4) from the lower light sandstoneseries (Tertiary) S,,, Spitsbergen, in the
shape and ornamentation, but differ inthe form size and the composition of theexine.
B. E. BALME (1957) described the similar species, Jnaperturopollenites Limbatus
BALME (B. E. BALME, 1957, p. 31, pl. 7,
figs. 83, 84) and I naperturopollenites
ht1·batus BALME (B. E. BALM E, 1957, p.
31, pl. 7 figs . 85, 86; pl. 8, fig. 87), from
the Mesozoic of Western Austra li a .
The former has smaller si ze and thicker
exine and the latter has sma ller size
and a differetially thickened circularpolar area about 40f-1 in diameter.
The present species is distinguishedfrom Araucariacites australi s COOKSON
from Tertiary lignites and carbonaceous
sandstone of Kerguelen Island (I. C.
COOKSON, 1947, p. 130, pl. 13, figs. 1-4)

R eticula ta sporites foraminulatus n. sp.
Pl. 5, figs. 1-8

Hol otype :- Slide 66041104- 10; Pl. 5,
figs. 4a, b ; size 73f-1.
Type Locality :- 500 m north of Harayama, Watsuka-cho, Soraku-gun, Kyoto
Prefecture.
TyjJe horizon :-Sandstone in the mudstone member of the B formation in the
Jubusen area of the Tanba belt.
Description:- Tetrad mark not v isible,
circular to oval in outline, exine thinwalled, ·w ith many circular to ellipti ca lpores of diameter 3.9 to 6.5f-1. Exinecolour colourless. Size range : length 68.
to 103/-1; breadth 50 to 75f-1.
Rematlz s :- The present specimens do·
not closely resemble any known species.
of R eticulata spm·ites.
A ll species of
R eticulata sporites were described by F.
LOOSE (1934) (R . mediapudens ), A. C.
IBRAHIM (1933) (R. facetus, R. viscendus,
and R. spongiosus ), R. POTONIE & G.
KREMP (1955) (R . facetus and R . taciturnus ) and D. C. BHARDWAJ (1957) (R ..
novicu s and R. teichmiillerii ) from theUpper Carboniferous of Germany, R.
KRii.USEL & G. LESCI-IIK (1955) (R. aduncu s.and R. densus) from the Upper Triassicof Switzerland, and C. J. FELIX & P. P.
BuRBRIDGE (1967) (R. lacunosus ) from

Kiyoshi T A K AHASHI and Akira YA O

46

the Springer Formation (Carboniferous)·Of southern Oklahoma, U. S. A. The
mesh-like network of the present j apa nese species is r ela ti vely s imilar to that
·Of the Amer ican species R . lacunosu s,
but the latter ha s very large muri .
Botanical affinity :- Unknown.
Turma:

Saccites ERDTMAN, 1947

.S ubturma:

Monosaccites (CI-IIT ALEY ,1951) POTONIE & KREMP, 1954

lnfraturma:

Aletesa cciti

Text-fig . 4

Description :- Monosaccate pollen g ra in? ; circula r or bread elliptica l in outline,
diameter of grain 152 x 127 f.l· Body wallver y thin , ver y fine rug ul ate or punctate.
Central body somewhat indistinct, 96 x
87 f.l in diameter, roughly r eticulate ?, no
tetrad ma rk recogni zable.
Occurrence :- Sandstone in the mudstone member of the B fo rmation in thejubusen a rea of the T a nba belt; 500 m
nor th of
Harayama,
Watsuka-cho,
SiSrak u-g un, Kyo to Pref ecture.
B otanical affinity :- ?Corda itales.

LESCHIK, 1955
Microplan kton

Florinites SCHOPF,
vVILSON & BENTALL, 1944

Genus:

ln certae Sedi s

Type species : Fl orinites antiquus

Acritarcha EviTT, 1963

Group:Class:SCHOPF, 1944
F a mily:?Florinites sp.

Chlorophyceae

Tasmanaceae SOMMER, 1956

Genus:Ta smanites Newton, 1875

Ta smanites tanbaensis n. sp.
Pl. 6, fig s . 1- 8

Te x t-fig. 4.

? Florinites s p.

x 420 .

J-!olotyjJe :-Slide 660Lll104-13; Pl.
6, fig. 2; size 128 x 119p in diameter;
wall 6.7 f1 in thickness.
Ty pe locality :- 500 m north ofHarayama, Wats uk a-cho, SiSr ak ug un , Kyoto Prefect ure.
Type horizon :- Sandston e in the
mudstone memb er of the B for mation in t he jubusen area of theTanba belt.
DescrijJtion :- Gra ins circ ular or
somewhat elliptical in outlin e, range
ofdiameter
107 - 152(-l x 82- 144(-l.

Expla nation of Plate 5
Figs. 1- 8. R eticulatdsporites foraminulatus n. sp .
Figs. 4a- b: Holotype, s lide 66041104- 10 ;Figs. 1- 7: x 420; F igs. 8a- b: x 1050.

TAKAHASHI ancl YAO:

Plant MicTofossils .from the Pennian

Plate 5

551.

Plant Microfossils from the Permian

Wall dark brown or reddish brown, 5 to
6.7 p. in thickness. Very small pores of
the wall are found here and there, espe-cially by fig. 8 remarkable.
Remarks:- The present specimens are
similar to the specimen from the Creta·Ceous of the Graham Island and Ellef
Ringes Island, Arctic Canada which wastreated by S. MANUM (1964) as Tasmanites cf. tardus EISENACK (S. MANUM,
1964, p. 22, pl. 7, fig. 9). The shell wall-of the present species is far thinner thanthat of Tasmanites tardus EISENACK.

References
BALME, B.E. (1957): Spores and pollen
grains from the Mesozoic of Western
Australia. Commonwealth Sci. Ind. Res.

Organization, coal Res.

Sec., T.C.

25

(Catalog of fossil spores and pollen, 13)
BALME, B.E. and HENNELLY, J.P.F. (1955):
Bisaccate sporomorphs from Australian
Permian coale. Austr. jour. Bot., 3, 1,
89-98, pls. 1-6. (Catalog of fossil sporesand pollen, 13)- - a n d - - (1956): Monolete, monocolpate,
and alete sporomorphs from Australian
Permian sediments. Ibid., 4, 1, 54-67, pls.
1-3 (Catalog of fossil spores and pollen,
13)
BHARDWAJ, D.C. (1957): The spore flora ofVelener Schichten (Lower Westphalian D)
in the Ruhr coal Measures. Palaeontographica, 102, B, 110-138, pls. 23-26.
CooKsON, I.C. (1947) :Plant microfossils
from the lignites of Kerguelen Archipelago. B.A.N.Z. Antarctic Research Expedition 1927-31, Rpts., Ser. A, 2, 8, 127142, pls. 13-17 (Catalog of fossil sporesand pollen, 15)•CooKsoN, I.C. and DETTMANN, M.E. (1959) :On Schizosporis a new form genus from
Australian Cretaceous deposits. Micropaleontology, 5, 2, 213-216, pl. 1.
DowNIE, C. (1967): The geological historyof the microplankton. Rev. Palaeobotan.
Palynol., I, 269-281.

47

DowNIE, C., EviTT, W.R., and SARJEANT,
W.A.S. (1963) : Dinoflagellates, hystrichospheres and the classification of theAcritarchs. Stanford Univ. publ. Geol.
Sci., 1, 3, 1-16.
EisE~ACK, A. (1958) :Tasmanites Newton
und Leiosphaeridia n. g. als Gattungender Hystrichosphaeridea. Palaeontographica, A, II 0, 1-19.
- - (1962) : Mitteilungen iiber Leiospharen
und iiber das Pylom bei Hystrichospharen.
N. ]b. Geol. Paliiont., Abh., 114, 1, 58-80,
Taf. 2-4.
- - (1963) : Hystrichospharen. Biol. Rev.,38, 107-139, Taf. 1-2.
EviTT, William R. (1963): A discussion andproposals concerning fossil dinoflagellates,
hystrichospheres, and acritarchs. I, II.
Proc. National Acad. Sci., 49, 2, 3, 158164, 298-302.
E!j>peMOBa, r .
(1967) : OaJIHHOJIQrHqecKoe.n:.

H3yqeHHe

HH)I{HerrepMCKHXOTJIO)I{eHHH

paiioHe acTpaxaHCKoro IIO.llHHTHH.

B

Tpy .llhi

MHHHCTepcTBO reoJIOrHH CCCP, BHHTHH,

52,

58-62, pls. 1-2.
FELIX, C.J. and BuRBRIDGE, P.P. (1967) :Palynology of the Springer Formation ofsouthern Oklahoma, U.S.A. Palaeontology, I 0, 3, 349-425, pls. 53-66.
GoTHAN, W. und WEYLA:-.:o, H. (1964) :Lehrbuch der Palaobotanik. Akademie-

Verlag, Berlin.
GRIGNAI'\I, Daria (1967) : Paleozoic spores
and Triassic pollen grains from some
Tunesian well samples. Rev. Palaeobotan.
Palynol., I, 155-159.
IBRAHIJvi, A.C. (1933) : Sporenformen desRuhr-Reviers (Dissertation, Berlin), 1-46,
Taf. 8, Triltsch, Wiirzburg (Catalog offossil spores and pollen, 6).
KRA.USEL, R. und LEsCHIK, G. (1955) : Die
Keuperflora von Neuewelt bei Basel, II.
Die !so- und Mikrosporen. Schweizerische
Paliiont. Ab., 12, 1-70, Taf. 1-10.
LESCHIK, G. (1956): Sporen aus dem Salzton
des Zechsteins von Neuhof (bei Fulda).
Palaeontographica, I 00, B, 122-142, Taf.
1-3.
MANUM, Svein (1962) : Studies in the Tertiary flora of Spitsbergen, with notes on

Kiyoshi TAKAHASHI and Akira YAO

48

Tertiary floras of Ellesmere Island, Greenland, and Iceland. A palynological investigation. Norsk Polarinstitutt Skrifter,
125, 1-127, pis. 1-20.
MANUM, S. and CooKsoN, I. C. (1964) : Cretaceous microplankton in a sample from
Graham Island, Arctic Canada, collectedduring the second " Fram '•-Expedition(1898-1902), with notes on microplankton
from the Hassel Formation, Ellef Ringes
Island. Skrifter utgitt av Det Norske
Videnskaps-Akademi i Oslo I Mat.-Naturv.
Klasse, N.S., 17, 1-36, pis. 1-7.
MuLLER, Jan (1968) : Palynology of thePedawan and Plateau Sandstone Formations (Cretaceous-Eocene) in Sarawak,
Malaysia. Micropaleontology, 14, 1, 1-37,
pis. 1-5.
nerywesa, JI. M. (1967) : CrropOBO·IIbiJ!b~eBbie
KOMIIJieKCbi cpe.llHe H sepxHeKaMeHHoyrOJib·
HbiX

OT JIOlKeHHH

JOr0·3aiia.llHOH

BOJirOrpa.llCKOH 06JiaCTH.

'laCTH

Tpy .llbi MHHHC·

TepcTso reoJiomH CCCP. BHl1fHl1. 52,
48-57, pis. 1-9.
PococK, S. A.}. (1962) : Microfioral analysis
and age determination of strata at theJurassic-Cretaceous boundary in theWestern Canada plains. Palaeontographica, 111, B, 1-95, Taf. 1-15.
PoTONIE, R. (1958) : Synopsis der Gattungender Sporae dispersae. II. Teil. Beih.
Geol. ]b., 31, 1-114, Taf. 1-11.
- - (1960) : Synopsis der Gattungen derSporae dispersae. III. Teil. Ibid., 39, 1189, Taf. 1-9.

Harayama
JubusenS6raku-gun---~-

DR Lll
~i$LlJ;f~~:mPoTONIE, R. und KREMP, G. (1954) : Die
Gattungen der palaozoischen Sporae dispersae und ihre Stratigraphie. Geol. ]b.,69, 11-194, Taf. 4-20.
- - und - - (1955) : Die Sporae dispersae
des Ruhrkarbons, ihre Morphographie undStratigraphie mit Ausblicken auf Arten
anderer Gebiete und Zeitabschnitte, Teil
I. Palaeontographica, 98, B, 1-136, Taf.
1-16; (1956) Teil II. 99, B, 85-191, Taf.
17-22.
RousE, G. E. (1959) : Plant microfossils from
Kootenay coalmeasures strata of British
Columbia. Micropaleontology, 5, 3, 303324, pis. 1-2.
SMITH, A. H. V. and BuTTERWORTH, M.A.
(1967) : Miospores in the coal seams of
the Carboniferous of Great Britain.
Special papers in Palaeontology No. 1.
STAPLIN, F. L., PococK, S. A. J. and JANsoNius, J. (1967): Relationships among
Gymnospermous pollen.
Rev. Palaeobotan. Palynol., 3, 297-310.
TAKAHASHI, Kiyoshi (1964): Sporen undPollen der oberkretazeischen Hakobuchi
Schichtengruppe, Hokkaido. Mem. Fac.
Sci., Kyushu univ., Ser. D, Geol., 14, 3,
159-271, Taf. 23-44.
WoDEHOUSE, R. P. (1935) : Pollen grains.
Hafner Publ. Co. 1965.
Y AO, Akira (1968) : Discovery of Fusulinids
from Ujitawara-mati, Kyoto Prefecture(Short note). Jour. Geol. Soc. japan, 14,
7, 399-400.

Tanba
Watsuka-cho- -------"----------------------------

Explanation of Plate 6
Figs. 1-8. Tasmanites tanbaensis n. sp. x 420.
Fig. 2. : Holotype, slide 66041104-13.

T A KAHASF-{I aJLd YJ\0:

Pla?~tMioTofossils from the Perrniam

Plate 6

49

PROCEEDINGS OF THE PALAEONTOLOGICAL SOCIETY
OF JAPAN~I *'-IJ:'E~Of:~~ 101 @]f9~~f:l:,1968 ,q:_ 11 fl
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Lepidocyclina ........ ± ~ft- · **'Jit=fTriassic Oxytoma bed in the Environs ofOrne City, Kwanto mountains ......... .
..... Tomowo OzAwA and Itaru HAY AMI
Occurrence of Tutcheria from the Lower
Jurassic of west Japan .... Itaru HAY AMI!7 1 7- :fj 1-lf"JL-;f-'r/' 0)~®.'!!2~1~-?v'"C · · · · · ·c. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 'Sw;(f*~ti
Review of the Philippine Palaeontology ..
...................... Wataru HAsHI:v1oTo
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Two Interesting Fossil Specimens from theUpper Paleozoic System in Japan ..... .
.................... R. ENoo & R. MoRI,
Mesozoic Filicales of Japan ............. .
. . . . . . . . . . . . . . . . T. KIMURA & S. SEKIDO
Mesozoic Plants from the Yatsushiro Formation, Kyushu, Japan ...... T. KIMURA
Addition to the Mesozoic Plants from the
Iwamuro Formation, Gumma Prefecture,
Japan ........................ T. KIMURA::PJII- tffi#~'F;tjl~Jilt; 1- /;f.!L-{>j"i!J:O):;)(Jli~t@~ll'i'IC"?v'""C ....................... -~tf!,~:f!lfllJ-&i;~s/1€~ r:j:l 0)

Braarudosphaera bigelowi(GRAN & BRAARUD) fC"?v'L .... jl!i]Ll.J(:!J:IIf'3

1'hfiH'i.Ek'6El"f}rH:Ji;JHcO) :1/ r:,- 1- fC-?v'-c· · · · · · · · · · · · .. ·. ·. · · · · · -illWH:Iti£! • ;J,tt!l~~On the Genus Thecosphaera from the Neogene Formation, Japan .... K. NAKASEKO
Phylogeny and Classification of the Fusulinacean Family Verbeekin.idae .. T. OzAWA
Lepidolina multiseptata (DEPRAT), the typespecies of the Verbeekinid Genus Lepidolina LEE, 1933 .............. T. OzAWA;t.Jft~~l!lmJ:nc "?v'-c................ LLJF>mll:1~;t,)f.;t'-e§EQ-2' ~1L Yabeina shiraiwensisLepidolina toriyamai ft::Pli¥ ~~ "? v '-c ....

........................ wr.;;u!l~ · J;JS[ ~H~

Analysis of the Recent Foraminiferal Faunas
from Miyako and Yamada Bays, Northeastern Japan ......................... .
. . . . . . . . . . . . . . H. UJIIE & T. KusuKAWA
Four New Species of Foraminifera from
Miyako and Yamada Bays ........... .
.............. H. UJIIE & T. KusuKAWA
iJH.t 'I\~ 1:.:t-o It 0 Globorotalia tosaensisGloborotalia truncatulinoides O)rJEI±',~rjf;~~"?v'L('f$11) .................. j\'ljj]J{t:nr,

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from the Environs of Sendai, Japan ....
. ................. K. MAsuDA & H. NooA
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Lower Cretaceous Ammonites from the
Miyako Group. Pt. 3. Some Douvilleiceratids from the Miyako Group ..... .
................................ I. OBATA
Selected Acanthoceratids from Hokkaido ..
............................ T. MATSUMOTO, T. MuRAMOTO & T. TAKAHASHIsoCalyptogena ~]':qH:-:::>v'-c. -lilm~lhJ~ · ±(~ii<'J·:~t-=r­:fl~/\l:~1t::fi, !f;'ff;: Turcicula f;:-:::>v'-c ....

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The 3rd International Conference on Palynology;):, 197lif., Novosibirsk, USSR ;:_;t;v'TIJiJ
fill'0~l.;~o if*/jJUd:, Professor M. I. NEUSTADT, Institute of Geography of the Academy of
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Transactions and Proceedings of the PalaeontologicalSociety of Japan

Apr il 30, 1969

New Series No. 73

CONTENTS
TRANSACTIONS
548. FUJI, Norio:

Fossil Spores and Pollen Grains from the Neogene Deposits

in Noto Peninsula, Central Japan - I A Pal ynological Study of the Late
Miocene Wakura Member
549.

1

HAYAM I, ltaru : Occurrence of Tul cheria from th e Lower Jurassic ofWest japan . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .

26

OZAWA , Tomowo and HAY AM I, ltaru: Triass ic Oxy loma Bed in the Suburbs of Ome City, Kwanto Mountains . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .

32

T AKA HASHI, Kiyoshi and YAO, Akira: Plant Microfossils from the Permian Sandstone in the Southern Marginal Area of the Tanba Belt. . . . . .

41

PROCEEDINGS . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .

49

550.

551.