ISSN 0031-0204

Transactions and Proceedingsof thePalaeontological Society of Japan
New SeriesNo. 133

Palaeontological Society of Japan
April 30, 1984

Itaru HAY AMI and Ikuwo OBATA

Co-Editors

Officers for 1983-1984
President: Yokichi TAKAYANAGI
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Kiyotaka CHINZEI, Takashi HAMADA, Tetsuro HAN AI, Yoshikazu HASEGAWA,

ltaru HAYAMI, Hisayoshi IGo, Junji ITOIGAWA, Tadao KAMEl, Tatsuaki KIMURA,
Tamio KOTAKA, Ikuwo OBATA, Tsunemasa SAITO, Tsugio SHUTO, Yokichi TAKAYANAGI, Toshimasa TANAIMembers of Standing Committee: Kiyotaka CHINZEI (General Affairs, Co-Editor of "Fossils"),
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Trans. Proc. Palaeont. Soc. Japan, N.S., No. 133, pp. 265-287, pis. 54-56, April 30, 1984

773. EARLY JURASSIC PLANTS IN JAPAN. PART 6*
TATSUAKI KIMURA and MASANORI TSUJIITokyo Gakugei University, Koganei, Tokyo 184

Abstract. This is the sixth of our serial papers on the early Jurassic plants inJapan. In this paper we describe Ginkgo ex gr. sibirica, Sphenobaiera cfr. eurybasis, S. nipponica sp. nov., S. cfr. ophioglossum and Ginkgoidium? sp. belonging
to Ginkgoales, Czekanowskia ex gr. rigida and Phoenicopsis ex gr. angustifolia
belonging to Czekanowskiales, and Elatocladus sp. A, E. sp. B, Storgaardia spectabilis, Podozamites ex gr. distans, P. sp. A, P. sp. B, P. (Cycadocarpidium?) sp. C
and Swedenborgia sp. A belonging to Coniferales, together with the supplementary
description of Neocalamites sp. A (Equisetales), Marattia asiatica (Marattiaceae)
again and Coniopteris sp. A (Dicksoniaceae) based on our additional material. This
paper gives the first record of Sphenobaiera in the older Mesozoic floras in Japan.
As our specimens are mostly poorly preserved impression, it is difficult to give clear
specific names but they are all characteristic constitutional elements of the earlyJurassic flora in Japan.

We express our sincere gratitude to Professor
Emeritus Thomas M. Harris, F.R.S. of the
University of Reading for his helpful suggestions
and critical reading over the present manuscript.
We also give our thanks to Mr. Gumpei Mori,
Mr. Noriyuki Sasaki, Mr. Akihiro Kobayashi
and many students of the Tokyo Gakugei University for their kind help in collecting thefossils here described.

Introduction and Acknowledgements
In continuation of our previous papers(Kimura and Tsujii, 1980a, b, '81, '82, '83), we
here describe the fossil plants belonging to
Ginkgoales, Czekanowskiales and Coniferales
from the Lower Jurassic Kuruma Group andIwamuro Formation. In addition we also describe three forms belonging to Pteridophyte
as a supplement based on our additional material
newly obtained.
The details of stratigraphy of plant-bearing
formations and localities were already given in
our first paper (Kimura and Tsujii, 1980a).
The characteristics of the early Jurassic flora inJapan and its significance for stratigraphy andphytogeography will be discussed in detail inthe last (Part 7) of our serial papers, together
with the detailed correlation between the earlyJurassic flora in Japan and the coeval floras
in East Asia and other regions.

Systematic Description
Ginkgoales
Genus Ginkgo Linnaeus
Ginkgo ex gr. sibirica Heer
PI. 54, Figs. 1-3; PI. 56, Figs. 1-2;
Text-figs. 1a-j

Ginkgoites digitata (Brongniart) var. huttoni
Seward: Oishi, 1931, p. 247, pI. 18, figs. 1B, 4(Tsuchizawa, Kuruma Group): 1940, p. 378(pars) (ditto).
Ginkgoites ? sp.: Kimura, 1959a, p. 25, pI. 10,
fig. 7 (Iwamuro).

*Received Jan. 10, 1983: Read Oct. 4, 1981 at
Hiroshima and June 26, 1982 at Hokkaido.
265

Tatsuaki KIMURA and Masanori TSUJII

266

Baiera? sp.: Kimura, 1959a, p. 25, pl. 10, fig. 5,

Ginkgo lepida Heer: Heer, 1876, p. 62, pl. 12,
figs. 1-10 (Ust-Balei).

text-fig. 14 (ditto).

Comparable specimens:
Ginkgo sibirica Heer: Heer, 1876, p. 61, pl. 7,

Comparable Japanese specimens:
Ginkgo sibirica Heer: Geyler, 1877, p. 231, pl.

fig. 6; pl. 9, fig. 5B; pl. 11; pl. 20, fig. 36;
pl. 22, fig. 3 (Ust-Balei and River Amur).

31, fig. 6 (Kuwashima) ?: Yokoyama, 1889,
p. 60 (remarks).

1j
1f

~~

1\\\\\\lfl

~b..
,
1i'~

1b

.

3cm
Text-figs. 1a-j. Ginkgo ex gr. sibirica Heer: Showing varied leaf-forms (all natural size).
la, b (A-0406, Pl. 54, Fig. 2), 1c (Kr-060, Pl. 54, Fig. 1), 1d (Kr-062), 1e (NNW-053), 1f (Kr064), 19 (A-0420), 1h, j (A-0354, Pl. 56, Figs. 1-2), 1i (A-2045, redrawn from Kimura, 1959a, pl.
10, fig. 5).

773. Early Jurassic plants in Japan. Part 6
Ginkgoites sibirica (Heer) Seward: Oishi, 1932ap. 347, pI. 49, figs. 4-5 (Upper Triassic Nariw~
Group): 1940, p. 380, pI. 38, fig. 11 (Upper
Jurassic Kiyosu~ Formation); pI. 39, fig. 1(Kuwashima): Kimura and Sekido, 1976, p.
365, text-fig. 22 (Lower Cretaceous Akaiwa
Formation ).
Ginkgo cfr. lepida Heer: Yokoyama, 1889, p. 60,
pI. 14, fig. 10 (Hakogase, Upper Jurassic
Kuzuryu Group)?
References of other regions, see Harris andMillington (in Harris et aI., 1974, pp. 20-21) andSamylina (in Vakhrameev et aI., 1980, pp. 109110).
Material: A-035 (0420, counterpart), 0395,
0406, 0425, 2046, 2059 (Iwamuro), Kr-016,
051, 055, 060, 062, 064, 127 (Tsuchizawa),
NNW-053 (Nishi-Neiridani), 4980804-7 (Kotaki
Coal-Field ).
Description: The leaves are long petiolate;the longest petiole is more than 1.6 cm long
(Text-fig. If). The laminae are nearly semicircular, forming angle of 145-225 degrees,
variable in size, with radius up to 6.5 cm (thesmallest one, 1.8 cm) from the first dichotomy(the top of petiole)_ The lamina is divided into
two parts by the median sinus reaching at ornear the top· of petiole. Typically the second
dichotomy in each part sends off the inner lobe
and an outer branch which sends further off the
middle and outer lobes at the third dichotomy.
Thus the typical number of lobes in a leaf is six.
The lobes are mostly simple, but often shallowly
lobed at the fourth dichotomy. Generally the
distance between adjacent dichotomies is small
except that between the third and fourth dichotomies. The lobes are fairly varied in form,
elongate-oblong, lanceolate, oblanceolate orsometimes linear with rounded apex. The veinsare 3-5 in number at the base of lobe, then dichotomously forking 2-3 times at all levels in thelower half of lobe, thus the number of veins is10-16 (12-19 per cm) at the distal portion of
lobe. Cuticle is not preserved.
Distribution and occurrence: Rather rare, but
locally common in the Iwamuro Formation andTsuchizawa of the Kuruma Group (Kr2)' A single
specimen was collected from the Negoya Formation.

267

Remarks: Our leaves are similar in form andbranching habit of lobes to original leaves described by Heer from the Irkutsk Basin andAmur Region, but somewhat differ from them inthe following: In our leaves the lobes are broader
than those of the original leaves and the veins are
more crowded (10-16 at the distal portion oflobe) than those of the original leaves (5-9 at thecorresponding portion of lobe). If the differences
between ·our and Siberian leaves mentioned
above be due to the specific difference, the number of Ginkgo species would increase enormously. Thus we at present regard our leaves asGinkgo ex gr. sibirica owing to the general resemblance of their form and branching habit oflobes to Heer's Ginkgo sibirica.
We think Heer's species from Ust-Balei
Ginkgo sibirica, G. lepida, G. schmidtiana, G:
flabellata and G. pusilla are conspecific andought to be included into G. sibirica, because
in their leaves, the branching habit of lobes andvenation are fundamentally the same. In UstBalei and some other regions, Ginkgo sibirica
leaves are in close association with G. concinna
leaves in which laminae are further divided by
the dichotomies of four times into slender orfiliform ultimate segments each with a few veins.
But from our localities, Ginkgo concinna-type
leaves have not been found.
Oishi (1931) described Ginkgo leaves from
Tsuchizawa as Ginkgoites digitata var. huttoni.
But his leaves are more deeply dissected into
lobes than those of Ginkgo digitata and are very
close in broader lobes and venation to some of
our leaves as shown in Text-figs. 19 and 1h.
We distinguished our leaves from the leaves ofGinkgo digitata and G. huttoni, as interpreted
by Harris and Millington (in Harris et al., 1974),
because in G. digitata laminae are less deeply
dissected and in G. huttoni lobes are irregularly
truncated or notched.
In Japan, several Ginkgo leaves were describedunder the names of Ginkgoites sibirica and G.
cfr. lepida as listed above, among which theleaves described by Geyler (1877) and Yokoyama (1889) were doubtful in specific identity
because they were all represented by broken

268

Tatsuaki KIMURA and Masanori TSUJllleaves. Other Japanese leaves are rather similar
in form and number of veins to ours than Heen
original leaves.
The Yorkshire leaves described in detail by
Harris and Millington (in Harris et al., 1974)
as Ginkgo sp. cfr. sibirica ar~ also similar in form
and venation to ours.
The leaves described by Takahasi and Okafuji(1967, '68) from the Carnic Momonoki Formation, Yamaguchi Prefecture as Ginkgoitessibirica,
may belong to Baiera furcata-group including B.
lindleyana-type leaves.
Genus Sphenobaiera Florin, 1936: 105
Sphenobaiera cfr. eurybasis Sze

PI. 54, Figs. 4-5; Text-figs. 2a-e
Pityophyllum (Pityocladus) sp.: Kimura, 1959a,
p. 27, pI. 9, fig. 5 (A-2050) (Iwamuro).
Comparable specimen:
Sphenobaiera eurybasis Sze: Sze, 1959, pp. 12,28, pI. 6, fig. 8; text-fig. 3 (Chaidamu, Qinghai, China): Sze et aI., 1963, p. 241, pI. 83,
fig. 4, 4a (Sze's specimen).
Material: NEE-207 (232, counterpart) (Higashi-Neiridani), NNW-053 (772) (Nishi-Neiridani),
NEG-151 (Negoya), DAI-069 (Dairagawa), SHI89 (099) (Shinadani), A-2050 (Iwamuro).
Description: The leaves are long and narrowly
wedge-shaped, more than 7 cm long, divided by
the first dichotomy into uneven parts and eachby as many as three successive dichotomies into
narrow ultimate segments. The basal undivided
portion of leaf is at least half as long as divided
part of leaf and 2-2.5 mm wide, gradually widening upwards to up to 0.8 cm wide below the firstdichotomy. In Text-fig. 2e [Kimura (1959a) misidentified it as Pityophyllum (Pityocladus) sp.],the leaf appears to be attached to the axis whichis 3 mm wide and at an angle of about 40 degrees. The basal angle of divided part of leaf is304>5 degrees, the angle of branching is 5-15
degrees. The dichotomies are at intervals of 0.71.3 cm. The leaf-segments are 1-3 mm wide,
mostly contracted at their base, gradually increasing in width upwards, and at their maximum
width immediately below the dichotomy. The
apices of lobes are all missing. The veins are notvisible. Cuticle is not preserved.
Distribution and occurrence: Sphenobaiera cfr.
eurybasis is rarely known from the Kuruma
Group and Iwamuro Formation.
Remarks: Our leaves are characterized bytheir narrowly wedge-shaped divided part andlong undivided part. Their general feature ismost similar to Sphenobaiera eurybasis originallydescribed by Sze (1959) from the Lower-Middle
Jurassic of Chaidamu Basin, Qinghai, China. But
we determined our leaves as Sphenobaiera cfr.
eurybasis, because Sze's species was based on asingle imperfect specimen with rather broader
undivided part.
Sphenobaiera pecten Harris (1945) from
Yorkshire is another allied form to ours, but isdistinguished by its narrower or filiform segments.
Sphenobaiera nipponica
Kimura and Tsujii sp. nov.

PI. 54, Fig. 6; PI. 55, Figs. 1-4;
PI. 56, Figs. 3-4; Text-figs. 3a-j
Material: Holotype: NNW-627 (Nishi-Neiridani). Paratypes: NNW-616, 632, 639 (NishiNeiridani) (Divided leaves), NNW-217, 602,345,
NEE-283 (Higashi-Neiridani) (Undivided leaves).
Other specimens: NNW-230, 449, 565, 567,
609, 617 (divided leaves), NNW-172, 320, 334,
340, 386, 535, 746, 864, NEG-127 (Negoya)(undivided leaves).
Stra~m typicum: Negoya Formation, Kururna Group. Locus typicus: The Nishi-Neiridani,
Asahi-machi, Shimo-Niikawa·Jun, Toyama Prefecture.
Derivatio nominis: After Nippon meaning
Japan in Japanese.
Diagnosis: Leaf dimorphic, entire or deeply
lobed. Entire leaf oblanceolate in outline, up to
12 cm long and 1.5-2 cm wide at the widest portion, gradually narrowing towards the petiole.
Petiole narrow, about 1-1.2 mm wide, length atleast 1.5 cm. Apex shallowly emarginated. Bilobed (divided) leaf variable in size, length 3."
cm or more, sinus reaching the basal narrow part,
each lobe oblanceolate in outline, up to 1.5 cm
wide at the widest portion. Apex rounded. Vein

773. Early Jurassic plants in Japan. Part 6

269

3a

~\1'1~\~

2b

3d

3g

3f
3cm

Text-figs. 2-3 (all natural size).
2q-e. Sphenobaiera cfr. eurybasis Sze: 2a (NNW-053, PI. 54, Fig. 4), 2b (DAI-069), 2c (NEE207, PI. 54, Fig. 5), 2d (NNW-053, PI. 54, Fig. 4), 2e. A leaf attached obliquely to the axis (A-2050,
drawn from Kimura, 1959a, pI. 9, fig. 5).
3a-j. Sphenobaiera nipponica Kimura and Tsujii sp. nov.: 3a-e; undivided (entire) leaves.
3f-j; divided (bilobed) leaves. 3a (NNW-602, Paratype, PI. 55, Fig. 1), 3b (NNW-851), 3c (NNW334), 3d (NNW-345, Paratype, PI. 55, Fig. 2), 3e (NEE-283, Paratype, PI. 55, Fig. 3), 3f (NNW627, Holotype, PI. 56, Fig. 3), 3g (NNW-616, Paratype), 3h (NNW-639, Paratype), 3i (NNW·632,
Paratype, PI. 56, Fig. 4), 3j (NNW-230).

270

Tatsuaki KIMURA and Masanori TSUJIIin the narrow basal part or petiole being single
and thick, bifurcating at or near the top ofnarrow basal part, each branch giving off repeatedly forking parallel veins; 13-16 in number(8-9 per cm) at the middle of entire leaf; veins
not converging at apex. (Cuticle not preserved.
Reproductive organs not known.)
Distribution and occurrence: Locally common
in the Negoya Formation.
Discussion and comparison: We think ourentire and bilobed leaves belong to a single
species, because the venation of both types ofleaves agrees with each other and the leaves ofboth types occur in close association.
Sphenobaiera gyron originally described byHarris and Millington (in Harris et aI., 1974)
from Yorkshire also has dimorphic leaves,simple (entire) and bilobed. In Sphenobaiera
gyron the leaf apex appears truncate (e.g. theirtext-fig. 18D) and not rounded and its veinsbranch lower in the lamina. The vein concentrations are so similar that they scarcely constitutea specific difference.
The entire leaf of Sphenobaiera nipponica issimilar in form to those of Eretmophyllum,
but no forked Eretmophyllum leaves have beenreported. The leaves of Eretmophyllum glandulosum (Samylina) Krassilov are distinguished fromour entire leaves by its well marked marginalveins from which the others arise.
Our bilobed leaves are similar in form to somebilobed Ginkgoidium leaves (e.g. Ginkgoidium
nathorsti Yokoyama). The leaves described as
Ginkgoidium nathorsti (Yokoyama, 1889: Oishi,
1940: Kimura and Sekido, 1965, '76) from theLower Cretaceous Itoshiro Group, in the Inner
Zone of Japan, consist of both entire and bilobed
ones. But they differ from ours in that they havestrong marginal veins from which all other veinsarise and these veins are parallel, very crowded
and forked near their marginal origin. Similarbilobed Sphenobaiera leaves to ours are thoseof S. huangi (Sze) Hsu and S. pulchella (Heer)
Florin. But they are represented only by bilobed
leaves and no entire leaf has been known. Leavesof Sphenobaiera huangi are often larger in size
than ours.

Ginkgoidium (1) longilobatum originally described by Lebedev (1965) from the Upper
Jurassic of the Zeia River area is represented bybilobed leaves. It is distinguished from our bilobed leaves by its longer lobes each with small
number of branched veins (7 in each lobe).
Although there is no direct evidence, we
think our bilobed leaves might have been attached singly to the long shoot and our entire
ones spirally to the top of short shoot with very
short internode, like those of extant Ginkgo
biloba.
Similar thought was mentioned by Kimura
and Sekido (1965). They described both entire
and bilobed leaves as Eretmophyllum tetorienseand Ginkgoidium nathorsti respectively from theLower Cretaceous Ishoshiro Group in close
association in occurrence. Their Eretmophyllum
leaves were still attached to the top of a fairly
long short shoot. Both types of leaves havesuch similar venation that they supposed that
their Eretmophyllum tetoriense and Ginkgoidium nathorsti may be conspecific, and theirbilobed leaves may have been attached singly tothe supposed long shoots.
Sphenobaiera cfr. ophioglossum
Harris and Millington
PI. 54, Fig. 7; PI. 55, Figs. 5-6;
PI. 56, Fig. 5A; Text-figs. 4a-dComparable specimens:
Sphenobaiera ophioglossum Harris and Millington: Harris and Millington, in Harris et aI.,
1974, p. 4B, pI. 2, figs. 1-5; text-figs. 16-17(Yor kshire ).
Material: NEG-005, 012, 021, 029, 072, OB4,
095, lOB, 112, 123, 137, 146, 149, 254, 263,
279 (Negoya), NNW-652, 664 (Nishi-Neiridani),
NEE-041 (123, counterpart) (Higashi-Neiridani),
NE-135 (Neiridani).

Description: The leaves are narrowly wedgeshaped with broad leaf-base and without marked
petiole, varied in form and size; the basal angle
is typically 40 degrees. The leaves are divided
into two nearly equal or unequal lobes by the
deep median sinus; the lobes are often divided
once more. The largest leaf at hand is more than773. Early Jurassic plants in Japan. Part 6

14 cm long and its undivided basal part is atleast 3.3 cm long.
The primary lobes are contracted at base,gradually widening upwards to 1-1.9 cm wide
just below the second dichotomy, while theultimate lobes (or segments) are narrowing
gradually towards the apex; the dichotomies
are at intervals of 1.9-3.9 cm and the branchingangle is 20 degrees at the first dichotomy and12-20 degrees at the second dichotomy. The
apex of lobe is not known.
The veins are bifurcating from the base ofundivided lamina, then repeatedly bifurcating
at all levels except the distal portion of lobes,
parallel and not converging at apex; the number of veins is 9-10 (4-5 per cm) in primary
lobe. Cuticle is not preserved.
Distribution and occurrence: Locally common
in the Negoya Formation.
Remarks: Although none of our leaves iscomplete, our leaves are macroscopically close to
those of Sphenobaiera ophioglossum, but do not
fully agree with Yorkshire leaves. Differences
are: In our leaves they are mostly divided twice
and with veins of 4-5 per cm in primary lobe,
but mostly once and with veins of 20 per cm inSphenobaiera ophioglossum. We therefore determined our leaves as Sphenobaiera cfr. ophioglossum.
Sphenobaiera longifolia (Pomel) Florin is ananother allied form, but it is distinguished byits leaves typically forking four times and withslender lobes. However, some of the less divided
leaves described as Sphenobaiera longifolia aremacroscopically indistinguishable from ours.
The following species of Sphenobaiera also
resemble our leaves but each has a distinguishingfeature:Sphenobaiera huangi (Sze) Hsii: Sze, 1949
(as Baiera huangi): Hsii, in Sze and Hsii,
1954 (name): Sze et aI., 1963 (Sze's
specimen) (Lower-Middle Jurassic Xiangxi
Formation): Krassilov, 1972 (Upper Jurassic of Bureja Basin): Krassilov and Schorochova, 1973 (Lower Jurassic of Primorye):
Leaves mostly bilobed.
Sphenobaiera ikorfatensis (Seward) Florin:

271

Seward, 1926 (Lower Cretaceous of Greenland): Samylina, 1963 (S. ikorfatensis f.
papillata) (Upper Jurassic of Aldan Riverarea): Krassilov, 1972 (ditto) (Lower
Cretaceous of Bureja Basin): Leaves onceor twice forked but rather small-sized.

Sphenobaiera pulchella (Heer) Florin: Heer,
1876 and many others (known mainly
from Jurassic-Lower Cretaceous of Siberia): Leaves mostly bilobed.
Sphenobaiera spectabilis (Nathorst) Florin:
Nathorst, 1906 and others (mainly Lower
Liassic of Sweden and Greenland): Leaves
often further divided (five times).

Genus Ginkgoidium Yokoyama, 1889: 56
Ginkgoidium ? sp. A
Text-fig. 5

Material: A-75154 (Iwamuro).
Description: Only a single broken leaf asshown in Text-fig. 5 was obtained. The leaf ispossibly entire, oblong in outline, more than
4.5 cm long, nearly parallel-sided for the mostpart, 1.8 cm wide, abruptly narrowing near base.
Its apical half is missing. The venation is characterized by marked marginal veins from which
all other veins arise; these veins are parallel,dichotomously once forked near their origin
except median ones which are simple, 27 in
number (15 per cm) at the middle of leaf. Cuticle
is not preserved.
Distribution and occurrence: A single specimen from the Iwamuro Formation.
Remarks: As mentioned above, this leaf ischaracterized by its marginal veins from which
all other veins arise. From this our leaf would
possibly be included in the category of Ginkgoidium, and we regard it as Ginkgoidium ? sp. A.
However, as the apex is missing we cannot exclude the possibility that the veins might converge as in Podozamites.
Ginkgoidium ? sp. A is distinguished from
Sphenobaiera nipponica here described together
by its marked marginal veins and more crowded
veins.
Ginkgoidium ? sp. A is also distinguished fromG. nathorsti Yokoyama known abundantly

272

Tatsuaki KIMURA and Masanori TSUJII

from the Lower Cretaceous Itoshiro Group by
its small number of veins (20-40 in each leaf in
G. nathorsti).

preserved cuticles we cannot compare themfully with description of leaves in which detailsof cuticles are important.

Czekanowskiales

Genus Czekanowskia Heer, 1876: 65

In this order, two genera, Czekanowskia andPhoenicopsis are represented in our collection,
but no specimen of their reproductive organs
has yet been found. As our specimens lackCzekanowskia ex gr. rigida Heer

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4a
Text-figs. 4-5 (all natural size).
4a-d. Sphenobaiera cfr. ophioglossum Harris and Millington: 4a (NEG-095, PI. 54, Fig. 7),
4b (NEE-123, PI. 55, Fig. 6), 4c (NEG-lOB), 4d (NEG-279, PI. 56, Fig. 5A).
5. Ginkgoidium? sp. (A-75154).

773. Early Jurassic plants in Japan. Part 6
pI. 18, figs. 5--6 (Tsuchizawa, Kuruma Group):
1932a, p. 355, pI. 32, fig. 8, 8a (Nariwa
Group): 1940, p. 384, pI. 39, figs. 6-7(Upper
Jurassic Kiyosue Formation): Kimura, 1959a,
p. 25, pI. 11 (Iwamuro, good leaves, though
impression ).

Comparable specimens:Czekanowskia rigida Heer: Heer, 1876, p. 70, pI.
5, figs. 8-11; pI. 6, fig. 7; pI. 10, fig. 2a (UstBalei).
Czekanowskia setacea Heer: Heer, 1876, p. 68,
pI. 5, figs. 1-7; pI. 6, figs. 1--6 (Ust-Balei).
Oishi (1931) gave the list similar in macroscopical form to our leaves.
Material: A-2097 (4001, counterpart), 4004,
8001, AA·052 (053) (Iwamuro), Kr-045 (Tsuchi·zawa), NEE-279 (360) (Higashi-Neiridani), NNW·
396 (Nishi-Neiridani).

Description: The short shoot is very small,covered by several rounded or rectangular scaleleaves which appear to be easily lost. The foliage
leaves are in a bundle of more than four, eachdichotomously forking four times or more, morethan 13 cm long and 1 mm wide below and 0.5
mm wide above; their apices are unknown. The
halves of dichotomy diverge at small angle. The
veins are not visible. Cuticle is not preserved.
Distribution and occurrence: Locally common
in the Iwamuro Formation, but rather rare in
the Negoya Formation and the Alternation ofsandstone and shale (Kr2), Kuruma Group.
Remarks: Many Czekanowskia species havebeen described from the older Mesozoic plantbeds in the Northern Hemisphere and also fromthe younger Mesozoic plant.beds in the Siberian
Palaeofloristic Area (Vakhrameev, 1964 and hisother papers), including the Inner Zone ofJapan. Most of these species are not only basedon their macroscopic features but also on theircuticles. However, our leaves are macroscopicallyclose to the well-known species Czekanowskia
rigida shown in detail by Doludenko and
Rasskazova (1972). According to them Heer's
Czekanowskia setacea is conspecific with C.
rigida.

The following species resemble ours but are
distinguished macroscopically by the features
briefly mentioned below:

273

Czekanowskia blacki Harris and Miller:
Harris and Miller, in Harris et al., 1974 (Yorkshire): Leaves forked twice.
Czekanowskia furcata Harris and Miller andC. thomasi Harris and Miller: Ditto: Leaves
forked only once.
Our leaves are macroscopically indistinguishable in leaf·form and number of dichotomies
from both microscopically defined leaves ofCzekanowskia hartzi Harris (1926) and C.
nathorsti Harris (1935) both from the Liassicof Greenland. Had the cuticles of these species
not been preserved, they would have been
identified as Czekanowskia rigida.
Under the circumstances, our present
designation of our leaves to Czekanowskia
ex gr. rigida is comprehensive. Similar leaves
were described in Japan by Oishi from theKuruma and Nariwa Groups and the Kiyosue
Formation as Czekanowskia rigida as cited above.

Genus Phoenicopsis Heer, 1876: 51
Phoenicopsis ex gr. angustifolia Heer
PI. 54, Figs. 8--9; PI. 55, Figs. 7-8;
PI. 56, Fig. 6; Text-figs. 7a~

Phoenicopsis ? sp.: Oishi, 1931, p. 252, pI. 17,
fig. 5; pI. 18, fig. 7 (Tsuchizawa).

Phoenicopsis sp.: Kimura, 1959b, p. 73, pI. 1,
fig. 8 (Kotaki Coal-Field).

Comparable specimens:
Phoenicopsis angustifolia Heer: Heer, 1876, pp.
51, 113, pI. 1, fig. 1d; pI. 2, fig. 3b (UstBalei); pI. 31, figs. 7-8 (Amur River area):
Krasser, 1906, p. 22 (610), pI. 3, figs. 3-4(Lower Cretaceous of Jiaohe, Jilin, NEChina): Sze et aI., 1963, p. 252, pI. 87, figs.
4-5 [Seward's (1911) specimens], fig. 6 [Sze's(1959) specimen]; pI. 88, fig. 2 [Sze's (1933)
specimen], fig. 3 (Lower-Middle Jurassic of
Xinjiang); pI. 89, fig. 5 (ditto).
Phoenicopsis angustifolia Heer, f. media Krasser:
Yabe, 1922, p. 27, pI. 4, figs. 4-5 (Daanshan,
Lower-Middle Jurassic mentougou Group).
For Russian references, see Kiritchkova (inVakhrameev et aI., 1980), pp. 128-130.
Material: SHI-046, 060, 063 (070, counterpart), 106 (120), 131, 134, 140, 144, 151, 171(Shinadani), TOB-013C (Tobiiwadani), NEE-

Tatsuaki KIMURA and Masanori TSUJII

274

3cm

6a

Text-figs. 6-7 (all n atural size) .
6a-b. Czekanowskia ex gr. rigida Heer: 6a (NEE-279, Pl. 56, Fig. 5B), 6b (A-800l, drawn
partly from Kimura, 1959a, pI. 11).
7a---€ . Phoenicopsis ex gr. angustifolia Heer : 7a, c (SHI-060, Pl. 54 , Fig. 8; PI. 55, Fig . 7), 7b(SHI-120, Pl. 54, Fig. 9), 7d (SHI-070) , 7e. A detached leaf and its venation (NEE-035) .

773. Early Jurassic plants in Japan. Part 6035 (Higashi-Neiridani), 4962501-4 and other 2
specimens (Kotaki Coal-Field).
Description: The short shoot is caducous,
small, 0.35-0.4 mm long, covered with roundedscale-leaves and gives off a bundle of foliage
leaves. None of our specimen is complete, thus
the number of fOliage leaves and scale·leaves ona short shoot is uncertain. The foliage·leaves
appear to be easily broken near base or easily
shed at base, and are variable in size and form,
linear and nearly parallel·sided for the mostpart or elongate.oblanceolate in outline, narrow·ing gradually towards the base, but the leaf·apices
are all missing; the longest one is more than 15.8
cm long (Text·fig_ 7a) and 0.6-0.7 cm wide at
the middle. The veins are mostly simple, 11 in
number at the apical half of each leaf, but some·times dichotomously forking once on the basal
half of leaf as shown in Text·fig. 7e. No inter·stitials between veins are found. Cuticle is notpreserved.
Distibution and occurrence: Phoenicopsis ex
gr. angustifolia is locally common in the Shina·
dani Formation, but is rather rare in the Negoya
Formation, Alternation of sandstone and shale(Kr2) and the Kotaki Coal·Field.
Remarks: The original leaves of this species
are about 4-5 mm wide and each leaf has 6-10
veins without interstitials. We think that ourleaves belong to this well· known species, Phoenicopsis angustifolia, although our leaves are some·what broader and have more crowded veins thanoriginal leaves. However, we here regard ourleaves as Phoenicopsis ex gr. angustifolia becauseof lacking cuticle in them.
Phoenicopsis speciosa Heer is distinguishedfrom our P. ex gr. angustifolia by its compara·tively broad leaves with crowded veins (15-23
in each leaf), a leaf·bundle consisting of 20 leaves
and by having interstitials between veins.
Phoenicopsis sp. described by Oishi (1932a)from the Nariwa Group resembles ours, butaccording to Oishi, his leaves have faint inter·stitials between veins. The leaf·fragments from
Tsuchizawa and the Kotaki Coal·Field regarded
by Oishi (1931) and Kimura (1959b) as Phoenicops is ? sp. and P. ~p. respectively, are referable
to P. ex gr. angustifolia.

275
Coniferales

Form-Genus Elatocladus
Halle em. Harris, 1979: 104
Elatocladus sp. A

PI. 56, Fig. 8; Text-figs. 8a-c
Material: SHI·018, 026, 029, 043, 048 (Shinadani).
Description: Five broken leafy shoots wereobtained.. They are represented' possibly byultimate part of twigs, and are simple, slender,
dropped with their leaves still attached. The
axis is slender, up to 1 mm wide, bearing closely
set alternate leaves on all sides, but the leaf·
bases bend and twist to bring each lamina into
the horizontal plane at a wide angle. The leaves
are elongate·oblong or oblanceolate in outline
with rounded apex, typically 0.7 cm long and 1·
1.5 mm wide at the widest portion. The con·tracted leaf·base is continued as a decurrent leaf·cushion onto the axis as shown in Text·fig. Be.
The leaf·margins are entire. The midrib is promi·
nent and persisting to the tip. Cuticle is notpreserved.
Distribution and occurrence: Elatocladus sp.
A is rarely known only from the Shinadani For·mation.
Remarks: Our leafy shoots cannot be placedin a natural genus on the present evidence. We
place them in Elatocladus sp. A, as used byHarris (1979). No similar leafy shoot to ours
has been recorded from the Mesozoic plant·beds
in Japan, Korea and China, nor are any of thespecies described by Harris (1935).

Elatocladus sp. B
Elatocladus sp.: Oishi, 1931, p. 253, pI. 18,
fig. 8.
Distribution and occurrence: Only a single

leafy shoot. Its exact locality is uncertain.
Remarks: Oishi (1931) described a single
broken leafy shoot as Elatocladus sp. from anerratic at the upper course of the Dairagawa(belonging possibly to the Negoya Formation).
It differs from our Elatocladus sp. A in its
thick axis (2 mm wide) bearing the leaves which
are falcate and broadest at the base.

Tatsuaki KIMURA and Masanori TSUJII

276

10f

10c

"\

~
Text-figs. 8-11 (all natural size except 8c).
8a-c. Elatocladus sp. A: 8a (SHI-018, PI. 56, Fig. 8), 8b (SHI-029), 8c. Showing the leafbases and decurrent leaf-cushions, drawn partly from 8a.
9a-b. Storgaardia spectabilis Harris: 9a (NEE-070, PI. 56, Fig. 7), 9b (NNW-238).
lOa-f. Podozamites ex gr. distans «Presl) Braun: lOa (TOB-048A, PI. 56, Fig. 9), lOb (TOB017B, PI. 56, Fig. 10), 10c (NEE-188), 10d (Kr-073, PI. 55, Fig. 9), 10e (NEE-105), 10f(NEG-188).
11. Sweden borgia sp. A: (A-2040, redrawn from Kimura, 1959a, pI. 8, fig. 5).

773. Early Jurassic plants in Japan. Part 6

Genus Storgaardia Harris, 1935: 58
Storgaardia spectabilis Harris

PI. 54, Fig. 10; PI. 56, Fig. 7; Text-figs. 9a-b
Storgaardia spectabilis Harris: Harris, 1935, p.
58, pI. 11, fig. 17; pI. 12, figs. 7-8; pI. 16, figs.
1-2; text-figs. 24-26 (Liassic of Greenland):
1937, p. 60 (ditto): Doludenko and Orlovskaja, 1976, p. 82, pI. 38, fig. 1; text-figs. 48,
49a_ (Upper Liassic of Karatau).
Cfr. Storgaardia spectabilis Harris: Oishi and
Huzioka, 1938, p. 96, pI. 12, fig. 3; text-fig.
7 (Upper Triassic Nariwa Group: Oishi, 1940,
p. 412 (remarks).
?Pityophyllum longifolium (Nathorst): Oishi,
1931, p. 252, pI. 17, fig. 7 (Tsuchizawa etaI., Kuruma Group).
Material: NEE-070 (Higashi-Neiridani), NNW237, 318, 385 (Nishi-Neiridani).
Description: The shoots are more than 14 cm
long, bearing the leaves oppositely at intervalsof 0.5-1.3 cm and at an angle of 45-60 degrees
to the slender rachis. The leaves are very shortly
st~ked, elongate-Ianceolate in outline, typically
4.5-6.5 cm long and about 1 cm wide at middle
portion, narrowing abruptly at base and gradually towards the acute apex; margins are entire.
The leaf-pairs are possibly decussate but allleaves are brought into the horizontal plane andsome show twisting of the basal stalk. The midrib
is prominent, but no other veins are present.
Cuticle is not preserved.
Distribution and occurrence: Rather rare.
The specimens safely referable to this species
are at present known only from the Negoya
Formation.
Remarks: Our shoots agree closely with theoriginal ones described by Harris (1935) fromthe Liassic of Greenland in all macroscopic
features.
Oishi and Huzioka (1938) described similar
shoots from the Upper Triassic Nariwa Group.
But they refrained from its full identity withStorgaardia spectabilis because their shoots
had more crowded leaves which contracted
at base less abruptly and some leaf-pairs appeared
to be subopposite. However, so far as the macroscopical form of them is concerned, we think277

their shoots are conspecific with Harris' species
and their mode of insertion of leaves to therachis appearing to be subopposite is due tothe twisting of the basal stalk like those of ours.
Storgaardia hissarensis originally described byGomolitzky (1963) based mainly on its leafcuticle from the Middle Jurassic of the southwestern branches of Gissar Range, is an anotherknown species of the genus. But it is difficult
to makp its macroscopical comparison withours, because Storgaardia hissarensis is represented by several detached leaf-fragments.
'Podocarpites' mentoukouensis Stockmans
and Mathieu (in Sze et al., 1963) from theLower-Middle Jurassic Mentougou Group near
Peking (Beijing), China is similar in leaf-form
to ours. But according to Sze et al. (1963, p.
307), its leaves are said to be not decussate
but distichous or looking so and to be opposite
or subopposite and occasionally alternate.
Several detached leaves described by Oishi(1931) as Pityophyllum longifolium (Nathorst)from Tsuchizawa, Shimodera and south of
Kuruma (all belonging to the Kuruma Group)
may belong to Storgaardia spectabilis. If so,
Oishi's figure (pI. 17, fig. 7) is upside down.
Genus Podozamites Braunin MUnster, 1843: 36
Podozamites ex gr. dis tans (Presl) Braun

PI. 55, Fig. 9; PI. 56, Figs. 9-10; Text-figs.10a-f
Japanese specimens:
Podozamites lanceolatus (Lindley and Hutton):
Yokoyama, 1891, p. 245, pI. 34, figs. 3-4(Yamanoi): 1905, pp. 8, 13, pI. 1, fig. 6(ditto); pI. 3, fig. 5 (Nariwa): Oishi, 1931,
p. 254, pI. 17, fig. 6 (Tsuchizawa, Shimodera
and Kuruma, Kuruma Group): 1932a, p. 363,
pI. 32, fig. 2; pI. 52, figs. 6-9 (Nariwa): 1932b,
p. 13, pI. 3, fig. 13; text-fig. 1 (Shitaka):
1932c, p. 66 (Kusaigawa, Momonoki, Yamanoi and Michiichi): Kimura, 1959a, p. 27, pI.
11 (in association with Czekanowskia ex gr.
rigida; Iwamuro): 1959b, p. 74, pI. 2, fig. 8(Kotaki Coal-Field).
Podozamites sp. cfr. P. griesbachi Seward:
Kimura, 1959b, p. 74, text-fig. 1 (Kotaki
Coal-Field ).

278

Tatsuaki KIMURA and Masanori TSUJI!

Material: A-0411 and other 29 specimens(Iwamuro), Kr-072 and other 3 (Tsuchizawa),
NEE-116 and other 9 (Higashi-Neiridani), NNW267 and other 3 (Nishi-Neiridani), NEG-013 andother 3 (Negoya), TOB-017 A and other 3 (Tobi~
iwadani), SS-lA, 4982305 and other 2 (Kotakl
Coal-Field ).
Description: Many leafy shoots and detachedleaves were obtained, but none of our shoots iscomplete. The axis is 0.5-3 mm wide, not hairy,
bearing spirally arranged leaves. The leaves areevidently twisted so as to lie in the horizontal
plane except a shoot shown in Text-fig. 10d.
The ieaves are elongate-oblong in outline, withobtuse or rounded apex, varied in form and size;
the thick axis bears large leaves, 9.6 cm long and1.5 cm wide at middle (Text-fig. lOa) and thethin axis bears small leaves. The ratio of leaflength to maximum leaf-width (L/W) is 2.56.8. The large leaves are shortly petiolate but thesmall leaves are sessile. The proximal leaves on ashoot are often oblong or oval in outline withrounded or obtusely pointed apex as shown in
Text-fig. 10d. The veins are slender, simple oronce forked in the basal half of leaf to give
about 11-20 in number (6-10 per cm) in eachleaf, converging slightly towards the apex, butsome of them ending in the distal margins. No
interstitial is visible. Cuticle is not preserved.
Distribution and occurrence: Podozamites
ex gr. dis tans is common in the Kuruma Groupand Iwamuro Formation.
Remarks: It is difficult to classify Podozamites leafy shoots and detached leaves specifically on macroscopic features. Most of ourleaves are elongate-oblong in form, but a few arelanceolate. Our leaves differ from those ofLindleycladus lanceolatus (Lindley and Hutton)
Harris (formerly Podozamites lanceolatus) of
Yorkshire (Harris, 1979) in the ratio (L/W);
the ratio (L/W) in ours is 2.5-6.8 as mentioned
above , but that in Yorkshire species is 9-16.4
measured on the leaves illustrated by Harris(1979).
In the Japanese specimens having regarded
as Podozamites lanceolatus from the Upper
Triassic-Lower Jurassic plant-beds as cited
above, this ratio (L/W) is 2.8-7.1 and is quite

similar in numerical value to ours.
This ratio (L/W) is rather similar to that ofPodozamites distans known extensively fromthe older Mesozoic plant-beds in Europe. Thus
we here separate these Japanese leaves from
Lindleycladus lanceolatus and in the meantime
regard them as Podozamites ex gr. dis tans. But
it would be most probable that our Podozamites
ex gr. distans is a mixture consisting of morethan one natural species.
So far as we know, there is no leaf referable
in form to Lindleycladus lanceolatus in thelate Triassic-early Jurassic floras in Japan. In
Korea many Podozamites leafy shoots anddetached leaves were described by Kawasaki(1925, '26, '39) from the Daedong Supergroup(mainly Upper Triassic) as P. schenki, Cfr. P.
gracilis, P. reinii, P. distans and P. lanceolatus.
Apart from his Podozamites schenki, P. reinii,
Cfr. P. gracilis and a particular example (his1925, pI. 33, fig. 92), the ratio (L/W) is 3.38.3 which is quite similar in numerical value tothat of ours and other Japanese leaves cited
above. Thus in the Daedong flora there is no leaf
safely referable to those of Lindleycladus lanceolatus of Yorkshire.
From the Upper Triassic-Lower Jurassic plantbeds in China, many Podozamites leaves wereidentified as Podozamites lanceolatus and its
varieties instituted by Heer, but their ratios(L/W) fall into 2.5-7.5 apart from one describedby Sze (1956, pI. 53, fig. 1) from the Upper
Triassic Yanchang Formation. Thus most of
Chinese leafy shoots and detached leaves regarded as Podozamites lanceolatus may rather
be included in our P. ex gr. distans than in P.
lanceolatus.
Kon'no (1961) described three types ofPodozamites leafy shoots as P. distans var.
osawae, P. distans var. nagatoensis and P. agardhianus var. acuminatus. The first was from theLower Carnic Nakatsuka Formation and therest from the Middle Carnic Momonoki Formation. His first and second varieties are distinguished from ours by their small-sized oblongleaves with small number of veins (6-7 and 7-13
in each leaf respectively). His third variety is773. Early Jurassic plants in Japan. Part 6279

also distinguished from ours by its small-sizedlanceolate leaves with small number of veins (8-9in each leaf).
Kon'no (1961) also illustrated four broken
leaves without description as Podozamites sp.
cfr. astartensis from the Ladino-Carnic Hiramatsu Formation. They are similar in form, sizeand venation to ours, and may be included in
our Podozamites ex gr. distans.
There are many Podozamites species having
been described with their cuticles from the older
Mesozoic plant-beds in Europe and Soviet
Union. Some of them are macroscopically similaror partly similar in leaf-form, size and venation
to ours, but we here do not compare them withours, because it is difficult to make a precise
comparison with geographically distant leaves
depending only on the macroscopical features,
especially with such Podozamites leaves.
Two detached leaves regarded by Kimura(1959b) as Podozamites sp. cfr. P. griesbachifrom the Kotaki Coal-Field may be proximal
ones on a shoot like that shown in Text-fig.
10d.

middle of leaf. The leaf-apex is not known.
Cuticle is not preserved.
Distribution and occurrence: Podozamites
sp. A is rare and known only from the Iwamuro
Formation.
Remarks: A broken shoot labelled A-700l
wa,c; once regarded by Kimura (1959a) as Problematicum B (Broad leave conifer ?). Since thensimilar shoots, though all broken, were obtained
from the Iwamuro Formation. Their macroscopical features lead us to place our shoots in
Podozamites. Their most characteristic featureis the hairy shoot. Hairy Podozamites shoots
have been described by Kon'no (1961) in his
P. dis tans (Presl) var. nagatoensis from theMiddle Carnic Momonoki Formation and by
Stanislavsky (1971) in his P. sp. 3 from theUpper Triassic of Donbass. In Kon'no's variety
the acicular appendages covering the main axis
are very crowded and minute, 2.7 mm long andits leaves are clearly distinguished from ours by
their small-size and small number of veins (7-13
in each leaf). Staniskavsky's Podozamites sp. 3
is also distinguished from ours in its long andslender leaves.

Podozamites sp. A

Podozamites sp. B

Text-figs. 12a-b

Text-fig. 13

Problematicum B (Broad leave conifer ?): Kimura, 1959a, p. 30, pI. 10, fig. 1 (Iwamuro).
Material: A-0401, 7001 and many otherdetached ·leaves.
Description: The rachis is rather thick, 2.54 mm wide, covered evenly by hairs on its
surface; the hairs are perpendicular to the surfaceof rachis, appearing to be rigid, up to 5 mm longand 1 mm wide at base, gradually narrowing to
the acuminate apex. The leaves are spirally
arranged at intervals of 0.75-1 cm and at wide
angle to the rachis, more than 5.2 cm long but
total length is unknown and 1.5 cm wide at thewidest portion near the base, not petiolate;the base is 1-1.b mm wide and the basal partpreserved is mostly bent and twist to bring eachleaf into the horizontal bedding plane. The
veins are numerous, simple or dichotomously
forking near the base, 23 in number at the

Podozamites sp.: Kimura, 1959a, p. 27, pI. 8,
fig. 1 (Iwamuro).
Material: A-7002 (Iwamuro) and many detached and broken leaves.
Description: The axis is 2 mm wide and longitudinally striated. The leaves are sessile, andappear to be attached oppositely to the axis at
an angle of 35 degrees. None of our leaves iscomplete, but the leaf is probably oblong or
short-Ianceolate, with abruptly narrowed base;the widest part is 1.15-1.40 cm. The veins are
numerous, dichotomously forked near the baseor in the lower half of leaf, 26 in number (23per cm) at the middle of leaf. Cuticle is notpreserved.
Distribution and occurrence: Rare, only
known from the Iwamuro Formation.
Remarks: The present leafy shoot is characterized by the oppositely disposed leaves.

280

Tatsuaki KIMURA and Masanori TSUJII

Unfortunately it is not clear whether they aredecussate or not, because in our Text-fig. 13,
the lower pair of leaves is broken at their joint.
The present leafy shoot is distinguished from
Podozamites ex gr. dis tans, P. sp. A and P.
(Cycadocarpidium 1) sp. C here described together by its oppositely disposed leaves. its glabrousaxis and its leaf with denser veins respectively.
Thus we at present regard it as Podozamites sp.

B.
Podozamites (Cycadocarpidium 1) sp. C

PI. 56, Fig. 11; Text-figs. 14a-e
Material: A-3080, 7540 (Iwamuro), NNW324, 393, 851 (Nishi-Neiridani).
Description: Obtained are all detached leaves.
The leaves are varied in form. A leaf shown in
Text-fig. 14e is elongate-oblong, narrowing
gradually towards the base to merge its long
petiole, its apex is missing; the veins are partly
visible, simple, 10 in number at the widest part(0.7 cm). A leaf shown in Text-fig. 14d, though
its basal part is missing, is similar in form to thatshown in Text-fig. 14e, but larger in size, probably 3.3 cm long (including the length of petiole)and at most 1.05 cm wide, its apex is rounded;
the veins on its apical half are visible, simple, 13
in number, not converging but ending at apicalmargin. The broken leaves shown in Text-figs.
14b and 14c are apical ones which are smallsized, with rounded apex; the veins are 11 and
9 in number respectively. A detached leaf shownin Text-fig. 14a is in association with that shownin Text-fig. 14d on the same slab and differs inform and venation from the others here described. Its form, though its petiole is missing,is crookedly oblong, 1.05 cm long and at most
0.75 cm wide, with 8 veins, one of which is once
forked at the middle. No interstitial between
veins is observed. Cuticle is not preserved.
Distribution and occurrence: Podozamites(Cycadocarpidium 1) sp. C is rare, and only
known from the Iwamuro and Negoya Formations.
Remarks: We think our leaves, though one
shown in Text-fig. 14a is fairly different inform and venation, belong to one and the same

Podozamites species. Our leaves are characterized
by their small-size and small number of veins(8-13 in each leaf), and differ in leaf-form
and vein-density from Podozamites ex gr. dis tans,P. sp. A and P. sp. B here described together.
It is undeniable that our leaves, such as
shown in Text-figs. 14d and 14e resemble closely
in form, size and venation the bracts of C!ycadocarpidium nagatoense described by Kon 'no(1961) from the Momonoki Formation. According to Kon'no (1961), Podozamites distans(Presl) var. nagatoensis and triovulate Cycadocarpidium nagatoense might most probably
belong to one and the same plant. Unfortunately
we could not recognize any traces of fertileorgans at the base of our leaves. Thus we regard
our leaves as Podozamites (Cycadocarpidium 1)
sp. C.
Podozamites (Cycadocarpidium 1) sp. C resembles in leaf-form and size P. distans (Presl)
var. osawae Kon'no from the lower part ofNakatsuka Formation (Lower Carnic), but isdistinguished by its number of veins (8-13 ineach leaf), instead of 5-8 in each leaf in Kon'no'svariety.
Podozamites (Cycadocarpidium 1) sp. C isindeed indistinguishable in leaf-form, size andnumber of veins from P. distans (Presl) var.
nagatoensis described by Kon'no. But at present
we refrain its identity, because this Kon'no'svariety is further characterized by that the surface of the leaf-bearing stem is densely coveredby minute stiff acicular appendages and such astem has not been recognized in our material.

Genus Sweden borgia Nathorst, 1876: 60
Sweden borgia sp. A

Text-fig. 11
Sweden borgia cryptomerioides Nathorst: Kimu-

ra, 1959a, p. 28, pI. 8, fig. 4-5 (Iwamuro).
Material: A-2040, 2040B (counterpart).
Description: The cone-scale is 1.5 cm in total

length, consisting of palm above and stalk below.
The scale-stalk is well defined, 1.0 cm long and1.5 mm wide at middle and 1.2 mm below.
The stalk-limb is mostly missing, leaving its

2S1

773. Early Jurassic plants in Japan. Part 6

17b

, 14a

14d

~4C

~II l
I(

14e
3cm

\

15a

Text-figs. 12-17 (all natural size except 17b) .
12a-b. Podozamites sp . A : 12a (A-7001) , drawn from Kimura, 1959a, pI. 10, fig . 1), 12b.
Details of hairs on the rachis (A-0401) .
13 . Podozamites sp. B : Drawn from Kimura, 1959a, pI. S, fig . 1 (A-7002) .
14a-e. Podozamites (Cycadocarpidium?) sp . C : 14a, d (A-'7540), 14b (NNW-S51), 14c (NNW393), 14e (A-30S0 , PI. 56, F ig . 11).
15a-b . Neocalamites sp. A : 15a (Kr-122), 15b (Kr-146).
16 . Marattia asiatica (Kawasaki) Harris: (NNW-S26) .
17a-b . Coniopteris sp. A: (SHI-662) .

282

Tatsuaki KIMURA and Masanori TSUJII

short piece on one side of the stalk-base. The
scale-stalk is expanded distally, 5 mm wide at
the widest portion and divided palmately into
five almost equal lobes. The lobe-proximal below
the widest part is broad and short; the lobedistal is elongated, narrowing gradually towards
the acutely pointed apex, 3.8-4.8 mm long; thewidth of broadest part is 1.6 mm. The seed-scaris at the upper surface of broadest part of eachlobe and nearly circular or short.oblong in outline, 1.25 mm (major) and 1 mm (minor) in
diameter. The seeds are not preserved. Further
details of cone-scale and seed-scar are not known.
Cuticle is not preserved.
Distribution and occurrence: Only a single
cone-scale and its minor fragments were obtained
from the Iwamuro Formation.
Remarks: The present cone-scale is characterized by its medium-size, very short lobe-proximal
and nearly circular or short-oblong seed-scar.
But at present we regard it as Swedenborgia sp.
A, because it is represented by an insufficiently
preserved single specimen.
In 1959, the senior author (Kimura) thoughtlessly identified it as Sweden borgia cryptomerioides Nathorst. But in our opinion it is atpresent distinguished from European Swedenborgia cryptomerioides by its longer and narrower lobe-distal.
Oishi and Yamasita (1935) described a laxcone, detached cone-scales and detached seeds
as Swedenborgia cryptomerioides from theUpper Triassic Nariwa Group. But their conescales are rather similar in having larger andnarrower lobes to ours than those of European
Swedenborgia cryptomerioides.
Based on his rich material from the Daedong

Supergroup in the Pyeongyang Coal-Field,
North Korea, Kon'no (1944) newly describedin detail Swedenborgia attenuata, S. coreanica,
S. lata, S. onoyamai, S. rigida and S. rigida var.
acuminata. Apart from the propriety of his
identification, our cone-scale resembles inform and size Kon'no's Sweden borgia coreanica
and S. rigida var. acuminata, but it is distinguished from S. coreanica by its nearly circularor short-oblong seed-scars instead of markedly
elongate-oblong ones, and from S. rigida var.
acuminata by its more thicker scale-stalk andgradually narrowing lobe-distal instead of narrower scale-stalk and more acuminate lobedistal.
Harris (1935) originally described Swedenborgia major and S. minor from the Liassic ofGreenland. Swedenborgia major is distinguishedfrom ours by its larger cone-scale and elongatedlobe-distal, and S. minor is also distinguishedfrom ours by its smaller cone-scale.
Swedenborgia longifolia originally describedby Stanislavsky (1971) from the Upper Triassicof Donbass is characterized by its markedly
elongated scale-lobes. Incidentally we may
mention that most characteristic are Swedenborgia megasperma and S. tuttosperma described
also by Stanislavsky (1976) from the Upper
Triassic of Donetz Basin, because they havetrilobed cone-scales with larger seeds.
In China Swedenborgia cones and detachedcone-scales similar in form to ours were described from the Upper Triassic Yanchang
Formation (Sze, 1956) and the Lower-Middle
Jurassic Xiangxi Formation (Sze, 1949; Wu etal., 1980) as S. cryptomerioides. An incomplete
cone was recorded by Sze (1959) from the

Explanation of Plate 54(all natural size)
Figs. 1-3. Ginkgo ex gr. sibirica Heer: 1 (Kr-060), 2 (A-0406), 3 (A-0425).
Figs. 4-5. Sphenobaiera efr. eurybasis Sze: 4 (NNW-053), 5 (NEE-207).
Fig. 6. Sphenobaiera nipponica Kimura and Tsujii sp. nov.: A divided (bilobed) leaf (NEG-Q95).
Figs. 8-9. Phoenicopsis ex gr. angustifolia Heer: 8 (SHI-060), 9 (SHI-120).
Fig. 10. Storgaardia spectabilis Harris: (NNW-237).

KIMURA and TSUJII: Early Jurassic plants

Plate 54

773. Early Jurassic plants in Japan. Part 6

Liassic Hongliugou Group as ?Swedenborgia
cryptomerioides.
Most authors think Sweden borgia is one of
the female reproductive organs of some Podozamites species of late Triassic--early Jurassic age.
In East Asia, too, Sweden borgia species are
known from the Upper Triassic to the Lower
Jurassic strata in association with several typesof Podozamites leafy shoots, but none of themhas been found in organic connection with
Podozamites shoots.
Supplementary description
Equisetales
Genus Neocalamites Halle, 1908: 6
Neocalamites sp. A

Text-figs. 15a-b
Neocalamites hoerensis (Schimper): Oishi, 1931,
p. 229, pi. 16, figs. 2-3 (Tsuchizawa): 1940,
p. 187 (pars) (remarks): Kimura, 1959a, p. 8,
pi. 1, figs. 7.,...10 (Iwamuro).
Neocalamites carrerei (Zeiller) Halle: Kimura,
1959b, p. 66, pi. 1, figs. 2, 6; pi. 2, fig. 3(Kotaki Coal·Field).
Neocalamites sp. cfr. N. hoerensis (Schimper)
Halle: Kimura, 1959b, p. 67, pi. 1, fig. 1(Kotaki Coal-Field).
Neocalamites? sp.: Kimura, 1959b, p. 68 (Kotaki
Coal-Field).
Material: A-3074 and other 17 specimens(Iwamuro), 4961801 and other 8 (Kotaki CoalField), Kr-106 and other 9 (Tsuchizawa).
Distribu Hon and occurrence: Locally very
abundant in the Iwamuro Formation and Kururna Group, but they are mostly represented bypith-casts of aerial stems.
Remarks: It is now difficult to identify
Neocalamites pith-casts specifically. Many Neocalamites pith-casts were described as N. carrerei, N. hoerensis and other names as cited
above by Oishi (1931, '40) and Kimura (1959a,b) from the Kuruma Group and Iwamuro Formation.
Halle (1908) mentioned that in Neocalamites
carrerei, the internode is generally shorter incomparison with the breadth of the stem than in
N. hoerensis, and the leaves are mostly shorter,

283

narrower and more in number than in N. hoerensis.
Kimura and Kim observed Neocalamites
carrerei-community in situ extensively preservedfor 3 kIn long in the lower horizons of Upper
Triassic Daedong Supergroup, Chungnam CoalField, Korea (Kimura et al., 1982) and collected
vast number of leafy stems, rhizomes and a few
cones. According to our observation of them,
the length of internodes is quite variable, usuallyshorter below and longer above (range notedfrom 204 cm to 8.5 cm even in the same leafystem) and the width is broader below and narrower above (range noted from 8 cm to 004 cm
in the same leafy stem). Thus it is difficult todistinguish between Neocalamites carrerei and
N. hoerensis depending only on the ratio (L/W)
of internode. In Korean Neocalamites carrerei,
leaves are not shorter but more than 20 cm long
and are not so generally narrower but many ofthem reaching 2 mm wide (range noted from
0.5 mm to 2 mm). Thus it is also difficult todistinguish between both species depending only
on the fragmentarily preserved leaves as shownby Oishi (1931, pI. 16, fig. 2 from Tsuchizawa).
Under the circumstances, we refrain fromthe specific identity of Neocalamites pith-casts
and detached leaves from the Kuruma Groupand Iwamuro Formation without the aid offurther material.
Filicales
Marattiaceae
Marattia asiatica (Kawasaki) Harris

Text-fig. 16
Marattia asiatica (Kawasaki) Harris: Kimura
and Tsujii, 1980b, p. 449, pi. 54, fig. 1; pi.
55, figs. 1-3; text-figs. 1a-j. For further references, see Kimura and Tsujii, 1980b, p. 449.
Additional material: NNW-826 (821, counterpart) (Nishi-Neiridani).
Additional description and remarks: Newly
obtained is a main rachis bearing sessile Marattia
pinnae which are, though broken, referable fully
to M. asiatica in all respects.
The main rachis is thick, 1 cm wide below
and 0.55 cm above, more than lOA cm long with

284

Tatsuaki KIMURA and Masanori TSUJIJ

longitudinal striations (a part was already shownin Kimura and Tsujji, 1980b, text-fig. 1b), giving
laterally off pinnae suboppositely at intervals of
3-3.5 cm and at a wide angle below and obliquely
above as shown in Text-fig. 16.
Judging from the dimension of partly preserved main rachis, the leaves of Marattia asiatica
are supposed to be fairly large in size, possibly
reaching 1 m in length.
Dicksoniaceae
Genus Coniopteris Brongniart, 1849: 26

Coniopteris sp. A
Text-figs. 17a-b

Material: SHI-062, 104 (Shinadani).
Description: The leaves obtained are mediumsized and partly fertile, but all are broken.
Text-fig. 17a shows a sterile part of leaf which
is at least tripinnate with main rachis, 1.8 mm
wide with a marked median furrow above, giving
alternately off penultimate pinnae at intervalsof 2 cm at an angle of 40-60 degrees. The ultimate pinnae are more than 1.3 cm long and 0.5
cm wide in the proximal ones, bearing 3-5
alternate pairs of closely set pinnules in katadromic order at an angle of 55 degrees. The pinnules are varied in size according to their position, generally larger in size on the proximal
and basal parts of a leaf, typically 0.5 cm long;its margins are regularly or often irregularly
lobed into 1-3 alternate pairs of lobes; eachlobe ending at rounded apex, but occasionally
not lobed but entire. The veins are weak; themidnerve is distinct but not persisting to thetip, sending off simple or once forked lateralveins; each lobe receives one lateral vein which
does not persist to its tip. The sori (or indusia)

are larger in size, nearly circular in form, 2.5
mm in diameter, produced at the tip of eachlobe on the large-sized pinnules as shown in
Text-fig. 17b which possibly shows a part ofbasal penultimate pinna. Unfortunately thedetails of sori are not known.
Distribution and occurrence: Coniopteris sp.
A is rare, and only known from the Shinadani
Formation.
Remarks: Our leaves clearly agree with the
Dicksoniaceae in the form of their pinnules
and a marginal soms, but as we have no detailsof the soms we make no precise generic identification. However, the name Coniopteris has
been widely used for leaves with such sori, nobetter known than ours.
A good many of these ill-known fossils havebeen given specific names, particularly hymenophylloides, but such names are scarcely useful.
We make no specific comparisons, but no suchleaf with large marginal sori is known fromthe older Mesozoic of Japan. Elsewhere thedicksoniaceous ferns become common in the
Middle Jurassic.
References
Doludenko, M. P. and Orlovskaja, E. R. (1976):
Jurassic flora of the Karatau. Acad. Sci.
USSR, Trans., vol. 284, p. 1-262, incl. pIs.
1-89 (in Russian).
Doludenko, M. P. and Rasskazova, E. S. (1972):
Ginkgoales and Czekanowskiales of the
Irkutsk Basin. In 'Mesozoic plants (Ginkgoales and Czekanowskiales) of East Siberia'.
Trans. Geol. Inst., Acad. Sci. USSR, vol.
230, p. 7-43, pIs. 1-49 (in Russian).
Geyler, T. (1877): Ueber fossile Pflanzen aus derJuraformation Japans. Palaeontographica,
Bd. 24, p. 221-232, pIs. 30-34.

Explanation of Plate 55(all natural size)
Figs. 1-4. Sphenobaiera nipponica Kimura and Tsujii sp. nov.: Undivided (entire) leaves.
1 (NNW-602, Paratype), 2 (NNW-345, Paratype), 3 (NEE-283, Paratype), 4 (NNW-217).
Figs. 5-6. Sphenobaiera cfr. ophioglossum Harris: 5 (NEG-021), 6 (NEE-123).
Figs. 7-8. Phoenicopsis ex gr. angustifolia Heer: 7 (SHI-D60), 8 (SHI-106).
Fig. 9. Podozamites ex gr. distans (Presl) Braun: (Kr-D73).

KIMURA and TSUJI!: Early Jurassic plants
Plate 55

773. Early Jurassic plants in Japan. Part 6
Gomolitzky, N. P. (1963): New Jurassic Coniferales from the Southwestern spurs of Hissar
Mts. Journ. Bot., Acad. Sci. USSR, t. 49,
no. 10, p. 1430-1437, pIs. 1-4 (in Russian).
Halle, T. G. (1908): Zur Kenntnis der mesozoischen Equisetales Schwedens. K. svensk.
Vet.-Akad. Handl., Bd. 43, p. 1-56, pIs.
1~.

Harris, T. M. (1935): The fossil flora of Scoresby
Sound East Greenland. Part 4: Ginkgoales,
Coniferales, Lycopodiales and isolated fructifications. Medd. om Grt5nland. Bd. 112,
nr.1, p. 1-176, pIs. 1-29.
--(1937): Ditto. Part 5: Stratigraphic relationsof the plant beds. Ibid., Bd. 112, nr. 2, p.
1-114, pI. 1.
- - (1945): Notes on the Jurassic flora of Yorkshire, 16-18. Ann. Mag. Nat. Hist., ser. 11,
vol. 12, p. 213-234.
--(1961): The Yorkshire Jurassic flora. I.
Thallophyta-Pteriodophyta. Brit. Mus. (Nat.
Hist.), ix + 212 pp.
--(1979): Ditto. V. Coniferales. Ibid., vi +166 pp., 7 pIs.
Harris, T. M., Millington, W. and Miller, J.
(1974): Ditto. IV-1. Ginkgoales. IV-2.
Czekanowskiales. Ibid. viii + 150 pp., 8 pIs.
Heer, O. (1876): Beitrage zur Jura-Flora Ostsibiriens und des Amurlandes. Acad. Imp.
Sci., St.-petersb., Mem., t. 22, p. 1-122,
pIs. 1-31.
HsU, J. (1954): Mesozoic plants. In 'Sze, H. C.
and HsU, J.: Index fossils of China (plants)'.
Geol. Publ. House, Peking. 83 pp., 68 pIs.
(in Chinese).
Kawasaki, S. (1925): Some older Mesozoic
plants in Korea. Bull. Geol. Surv. Chosen(Korea), vol. 4, pt. 1, p. 1-71, pIs. 1-47.
- - (1926): Addition to the older Mesozoic
plants in Korea. Ibid., pt. 2, p. 1-35, pIs.
1-11.
- - (1939): Second addition to the older Mesozoic plants in Korea. Ibid., pt. 3, p. 1-69,
pIs. 1-16.
Kimura, T. (1959a): Mesozoic plants from the
Iwamuro Formation (Liassic), Tone-gun,Gumma Prefecture, Japan. Bull. Sen. High
Sch., Tokyo Univ. Educ., no. 3, p. 1-59,
incl. pIs. 1-12.
--(1959b): Mesozoic plants from the Kotaki
Coal-Field, the Kuruma Group, Central

285

Honshu, Japan. Ibid., p. 61-83, incl. pIs.
1-2.
Kimura, T., Kim, B. K. and Ohana, T. (1982):
Neocalamites carrerei (Zeiller) Halle (Equisetales), found in situ from the Daedong
Supergroup, Korea. Proc. Japan Acad.,ser. B, vol. 58, no. 6, p. 156-159.
Kimura, T. and Sekido, S. (1965): Some interesting Ginkgoalean leaves from the ItoshiroSubgroup, the Tetori Group, Central Honshu, Japan. Mem. Mejiro Gakuen Woman's
Jr. Coli., vol. 2, p. 1-4, pIs. 1-2.
and - - (1976): Mesozoic plants from the
Akaiwa Formation (Upper Neocomian), theItoshiro Group, Central Honshu, Japan.
Trans. Proc. Palaeont. Soc. Japan, N. S.
no. 103, p. 343-378, pIs. 36-39.
Kimura, T. and Tsujii-, M. (1980a): Early Jurassic
plants in Japan. Part 1. Ibid., no. 119, p.
339-358, pIs. 38-40.
and - - (1980b): Ditto. Part 2. Ibid., no.
120, p. 449-465, pIs. 54-56.
-and - - (1981): Ditto. Part 3. Ibid., no.
124, p. 187-207, pIs. 30-32.
and - - (1982): Ditto. Part 4. Ibid., no.
125, p. 259-276, pIs. 41-43.
_
and - - (1983): Ditto. Part 5. Ibid., no.
129, p. 35-57, pIs. 12-14.
Kon'no, E. (1944): Contribution to our knowledge of Swedenborgia. Jap. Journ. Geol.
Geogr., vol. 19, nos. 1-4, p. 27---i>6, pIs.
1-5.
__ (1961): Some Cycadocarpidium and Podozamites from the Upper Triassic formations
in Yamaguchi Prefecture, Japan. Sci. Rep.,
Tohoku Univ., 2nd ser., vol. 32, no. 2, p.
195-211, pIs. 22-24.
Krasser, F. (1906): Fossile Pflanzen aus Transbaikalien der Mongolei und Mandschurei.
Akad. Wiss. Wien Denkschr., vol. 78, p.
589-634, pIs. 1-4.
Krassilov, V. A. (1972): Mesozoic flora from the
Bureja River (Ginkgoales and Czekanowskiales). Far East Geol. Inst., Far East Sci.
Centre, Acad. Sci. USSR, p. 1-103, pIs. 134 (in Russian).
Krassilov, V. A. and Schorochova, S. A. (1973):
Early Jurassic flora from the Petrovka River(Primorye). In 'Fossil floras and phytostratigraphy of the Far East'. Ibid., p. 13-27,
pIs. 3-12 (in Russian).
Lebedev, E. L. (1965): Late Jurassic flora from

286

Tatsuaki KIMURA and Masanori TSUJII

Zeia and boundary between Jurassic andCretaceous. Trans. Geol. Inst., Acad. Sci.
USSR, vol. 125, p. 1-142, pIs. 1-36 (inRussian).
Nathorst; A. G. (1906): Om n!igra Ginkgovlixter fran Kolgufvorna vid Stabbarp i
SUne. Lunds Uniu. Arrskrift. (n.{.) , Ald. 2,
Bd. 2, nr. 8, p. 1-14, pIs. 1-2.
Oishi, S. (1931): Mesozoic plants from KitaOtari, Prov. Shinano, Japan. Journ. Fac.
Sci., Hokkaido Imp. Uniu., ser. 4, vol. 1,
no. 2, p. 223-255, pIs. 16-18.
--(1932a): The Rhaetic plants from the
Nariwa District, Provo Bitchu (Okayama
Prefecture), Japan. Ibid., vol. 1, nos. 3-4, p.
257-380, pIs. 19-53.
--(1932b): The Jurassic plants from Shitaka(the Maizuru Coal-Field), Provo Tango(Kyoto Prefecture), Japan. Ibid., vol. 2, no.
I, p. 1-13, pIs. 1--3.
--(1932c): Rhaetic plants from Province
Nagato (Yamaguchi Prefecture), Japan.
Ibid., vol. 2, no. 1, p. 51-67, pIs. 9-10.
- - (1940): The Mesozoic floras of Japan.
Ibid., vol. 5, nos. 2-4, p. 123-480, pIs.
1-48.
Oishi, S. and Huzioka, K. (1938): Fossil plantsfrom Nariwa. A supplement. Ibid., vol. 4,
nos. 1-2, p. 69-101, pIs. 7-12.
Oishi, S. and Yamasita, K. (1935): On the genus
Sweden borgia Nathorst and its occurrencein the Nariwa bed, Okayama Pref., Japan.
hoc. Imp. Acad. Tokyo, vol. 11, no. 10, p.
438-440.
Samylina, V. A. (1963): Mesozoic flora of thelower course of the Aldan River. Komalov
Bot. Inst., Acad. Sci. USSR, ser.·8 (Palaeo-bot.), vol. 4, p. 59-138, pIs. 1-37 (inRussian).
Seward, A. C. (1911): Jurassic plants from
Chinese Dzungaria. Mem. Com. Geol., N. S.,
Livr. 75, p. 1-61, pIs. 1-7.
--(1926): The Cretaceous plant-bearing rocksof Western Greenland. Philos. Trans. Roy.
Soc. London, ser. B, vol. 215, p. 57-175,
pIs. 4-12.
Stanislavsky, F. A. (1971 ): Fossil {lora andstratigraphy of the Upper Triassic of Do n bass.
Inst. Geol. Sci., Acad. Sci. Ukraine, Kiev.
140 pp., 36 pIs. (in Russian).
--(1976): Middle Keuper {lora of the Donetz
Basin. Ibid. 168 pp., 87 pIs. (in Russian).
Sze, H. C. (1933): Jurassic plants from Shensi.
Mem. Natn. Res. Inst. Geol., Acad. Sinica,
no. 13, p. 77-86, pIs. 1'1-12.
--(1949): Die mesozoische Flora aus der
Hsiangchi Kohlen Serie in West Hupeh,
China. Palaeont. Sinica, N. S., ser. A, nr. 2,
p. 1-71, pIs. 1-15.
--(1956): Older Mesozoic plants from the
Yenchang Formation, Northern Shensi.
Ibid., nr. 5, p. 1-217, pIs. 1-56 (in Chineseand English).
--(1959): Jurassic plants from Tsaidam,
Chinghai Province. Acta Palaeont. Sinica,
vol. 7, no. 1, p. 1-31, pIs. 1-8 (in Chineseand English).
Sze, H. C., Li, X. X., Li, P. J., Zhou, Z. Y., Wu,
S. Q., Ye, M. N. and Shen, G. L. (1963):
Mesozoic plants from China. Fossil plantsof China. vol. 2, Sci. Press, Peking. 429 pp.,
118 pIs. (in Chinese).
Takahasi, E. and Okafuji, G. (1967): Ginkgoites
sibirica (Heer) from the Triassic of Omine

Explanation of Plate 56(all natural size)
Figs. 1-2. Ginkgo ex gr. sibirica Heer: (A-0354).
Figs. 3-4. Sphenobaiera nipponica Kimura and Tsujji sp. nov.: Divided (bilobed) leaves.
3. (NNW-627, Holotype), 4 (NNW-632, Paratype).
Fig. 5. A. Sphenobaiera cfr. ophioglossum Harris: B. Czekanowskia ex gr. rigida Heer: (NEE279).
Fig. 6. Phoenicopsis ex gr. angustifolia Heer: (SHI-144).
Fig. 7. Storgaardia spectabilis Harris: (NEE-Q70).
Fig. 8. Elatocladus sp. A: Shown partly from SHI-Q18.
Figs. 9-10. Podozamites ex gr. distans (Presl) Braun: 9 (TOB-048A), 10 (TOB-017B).
Fig.11. Podozamites (Cycadocarpidium?) sp. C: (A-3080).

KIMURA and TSUJII: Early Jurassic plants

Plate 56

773. Early Jurassic plants in Japan. Part 6
Coal-Field. Sci. Rep., Yamaguchi Univ.,
vol. 17, p. 15-17 (in Japanese).
and - - (1968): Ginkgoites and Baiera
from the Triassic of the Omine Coal-Field.
Ibid., vol. 18, p. 31-35, incl. pIs. 1-2 (inJapanese).
Vakhrameev, V. A. (1964): Jurassic and Early
Cretaceous floras of Eurasia and the palaeofloristic provinces of this period. Trans.
Geol. Inst., Acad. Sci. USSR, vol. 102, p.
1-263 (in Russian).
Vakhrameev, V. A., Dobruskina, 1. A., Doludenko, M. P., Samylina, V. A., Kiritchkova,
A. 1., Krassilov, V. A. and Burakova, A. T.
(1980): Mesozoic gymnospermous plants in
USSR. Nauka, Moscow. 232 pp. (in Russian ).
Wu, S. Q., Ye, M. N. and Li, B. X. (1980): Upper
Triassic and Lower and Middle Jurassic
plants from the Hsiangchi Group, Western

287

HubeL Mem. Nanjing Inst. Geol. Palaeont.,
Acad. Sinica, no. 14, p. 63-139, pIs. 1-39
(in Chinese).
Yabe, H. (1922): Notes on some Mesozoic plantsfrom Japan, Korea and China, in the collection of the Institute of Geology and Palaeontology of the Tohoku Imperial University.
Sci. Rep., Tohoku Imp. Univ., sec. ser., vol.
7, no. 1, p.1-28, pIs. 1-4.
Yokoyama, M. (1889): Jurassic plants from
Kaga, Hida and Echizen. Journ. ColI. Sci.,
Imp. Univ. Japan, vol. 3, pt. 1, p. 1-66,
pIs. 1-14.
- - (1891): On some fossil plants from the
Coal-bearing Series of Nagato. Ibid., vol. 4,
pt. 2, p. 239-247, pIs. 22-24.
- - (1905): Mesozoic plants from Nagato andBitchu. Journ. ColI. Sci., Imp. Univ. Tokyo,
vol. 20, art. 5, p. 1-13, pIs. 1-3.

Geographical names in Japan:
Akaiwa $!Et. Asahi·machi i¥JJ 131BJ. Dairagawa :.k:ifJII. Hokogase ~ ?'itJi. Higashi·Neiridani~lIlA1:t. Hiramatsu :iff'~. Itoshiro :oftaS. lwamuro :E~. Kiyosue (Kiyosue) j'j!f*. Kotaki'Nit. Kuruma *~. Kusaigawa 1Jr:Jj:JII. Kuwashima ~1it;. Michiichi )tim. Momonoki tl~/
Nakatsuka 9>~. Nariwa n\t:fl. Negoya w.J1E~. Nishi-Neiridani i1!i~A~. Shimodera r~. Shinadani fi?'~.
Tobiiwadani 1R:E~. Tsuchizawa (Tsunzawa) ±lR. Yamanoi L1~!Jf:tl:oGeographical names in China:
Chaidamu ~Jt*. Daanshan :.k'tCW. Hongliugou UWIJ(14:. Jiaohe !\'i:i'iiT. Jilin 5#. Mentougou
r~Mm.
Qinghai Wifii:. Xiangxi (Hsiangchi) ~~. Xinjiang ~m:. Yanchang l[f!:oGeographical names in Korea:
Chungnam !it'.l:¥f. Daedong :.kll'il. Pyeongyang :if~o*.

I3*O)fm!ll:;3.7*cllti~ft.:oo.:t0) 6: iliiml':'''?-?~. *.~JI~;}';.l:V::E~~IIi1·I?"?
~ 0) 1 "!- 3 ry. ,,!-::r. 71 / 7 A "f- 7 ;}.; .t V:~* I'H.:.H.lt-t 7.>ft.:o 1'; .l: lffil!JE.!: 1.... -C '" ~~~ 3 :fI-z.

BcttL.t.:o1 "!- 3 ry §: Ginkgo ex gr. sibirica Heer. Sphenobaiera cfr. eurybasis Sze, S.
nipponica Kimura and Tsujii sp. nov.. S. cfr. ophioglossum Harris and Millington.
Ginkgoidium ? sp.
"!-::r. 71 / 7 A 4'-7 §: Czekanowskia ex gr. rigida Heer. Phoenicopsis ex gr. angustifolia Heer.
f.1C* §: Elatocladus sp. A. E. sp. B. Storgaardia spectabilis Harris. Podozamites
ex gr. distans (Presl) Braun. P. sp. A. P. sp. B. P. (Cycadocarpidium?) sp. C.
Swedenborgia sp. A.
'" ~(ffif?J Oill@): Neocalamites sp. A. Marattia asiatica (Kawasaki) Harris. Coniopteris sp. A.
1:).1:0) ? i? Sphenobaiera .\!i\lt 13 *-c:MtWO)llctt-ea;oo Cuticle iI~f*ff~.h -C~ 't.n ,t.:10. 1:).J:I':'''?~'-Cj[;~t.diiJJEiI~-C~t.t:iI'...,t.:7'J~. ~'i'Jt t I3*O)WWl:; 3. 7*C.f1t(~~0)m:~t.t:
mn\t~.-c:~~. lli~O) • • ~~-z.~i'oJ:-c:m:~~~M.!:~~o*H~~·ft:Jj:~~Trans. Proc. Palaeont. Soc. Japan, N.S., No. 133, pp. 288-299, pIs. 57-60, April 30, 1984

774. CRETACEOUS NAUTILOIDS FROM HOKKAIDO - IV
PART 4. AN INTERESTING NAUTILOID SPECIES FROMTHE CENOMANIAN OF HOKKAIDO*TATSURO MATSUMOTO l ), TAKEMI TAKAHASHI 2),IKUWO OBATA 3) and MASAO FUTAKAMI4 )Abstract. This paper consists of sections A and B. In section A, Anglonautilus
japonicus Matsumoto et Takahashi, 1982, from the Lower Cenomanian Zone ofMantelliceras japonicum in the Ikushumbets area, central Hokkaido, is described in
more detail. It is distinguished from A. undulatus (Sowerby), the type species, by
its broader whorl which has a shallow median ventral groove on the adoral part,
weaker and less distant ribs which tend to be approximated on the last part, andsomewhat more sinuous sutures. Its characters suggest the relationships of Anglonautilus with certain subgroups of Cymatoceras on one hand and Paracymatocerason the other.
In section B, the ontogeny, especially an individual allometry, of the same
species is examined in detail on the early whorl. An observation of the spiralgrowth in early stage on Anglonautilus japonicus has confirmed the existence of
two critical points, i.e. 1.27T and 27T in total rotation angle from the axis. The
nepionic constriction is recognized at a point between the two critical points. As
to the septal interspace three growth stages are noticed in the early whorl: thefirst and the second chambers are small, the third to the seventh large, and theeigh~h and the successive chambers again small in total rotation angle from axis.
Thus the pattern of septal growth on the early whorl in the present species has
some similarity with that in Nautilus pompilius. Anglonautilus japonicus, which
has an adult shell of about 90 mm in diameter, shows a great changes of the growth
pattern near the nepionic constriction (D = 15 mm). Thus the end of the embryonicstage of the species can be defined at about 15 mm in diameter. Accordingly, theegg diameter of Anglonautilus japonicus is presumed to be smaller than that of theliving Nautilus.

Introduction

to deal with in this paper, has been nomenclatorially established by the first two authors(Matsumoto and Takahashi, 1982). That reportwas, however, so brief that the description in
more details is given in this paper.
The present study is based on a number ofwell preserved specimens obtained mostly by
the second author (T. T.), sometimes with thefirst (T. M.), during the field works for years_
The specimens of Takahashi's collection aremarked as TTC, in this paper. Most of themoccurred in the Lower Cenomanian Zone of

An interesting nautiloid species from the
Cenomanian of Hokkaido, which we are going*Read October 17, 1982, Mie University; received Jan. 13, 1983.
1) c/o Department of Geology, Kyushu University 33, Fukuoka 812.
2) 28-109 Hanazono-cho, Yayoi, Mikasa 06822.
3) Department of Paleontology, National Science
Museum, Tokyo 160.
4) Tadawo Senior High School, Tokyo 194.
288

774. Cretaceous Nautiloids
Mantelliceras japonicum at one and the same
locality (loc. Ik 1100) and a few at other localities in the same zone. They include the specimens of various growth-stages. Therefore, wehave attempted to examine the ontogeny aswell as the variation in addition to the routine
taxonomy.

The results are described below in the following two sections:
A. Taxonomic Description by T. Matsumoto
and T. Takahashi
B. Ontogeny by I. Obata and M. Futakami
A. TAXONOMIC DESCRIPTION(T. Matsumoto and T. Takahashi)
Family Cymatoceratidae
Genus A nglonautilus Spath, 1927
Type species:-Nautilus undulatus J. de
Sowerby (original designation).
Remarks:-See Kummel (1956, p. 431),
Matsumoto and Takahashi (1982, p. 297) andMatsumoto and Miyauchi (1983, p. 226) for
the generic diagnosis and the relationships
with Cymatoceras and Paracymatoceras.
Anglonautilus japonicus Matsumoto et Takahashi
PI. 57, Fig. 1; PI. 58, Fig. 1; PI. 59,
Figs. 1, 2; PI. 60, Figs. 1-6; Text-fig. 1

1982. Anglonautilus japonicus Matsumoto et
Takahashi, Proc. Japan Acad., vol. 58,
ser. B, p. 295, figs. 1-3.

Material:-Holotype TTC. 390715 (PI. 1, Fig.
1; Text-fig. 1A), adult specimen, internal mould
for the most part but for the last ventral part
where a portion of the test is preserved. Paratype 1, TTC. 500413 (PI. 58, Fig. 1; Text-fig.
1B), another adult example in which the test is
better preserved but the sutures are not so wellshown as in the holotype.
Other 18 paratypes are smaller than the above
two, representing immature stages. The majorityof them is TTC. (400606, 390419, 380414,
390726-3, 410710, 390717-1, 400530, 390726-

289

1,390726-2,400516,391102,370524,3909172, 370717, 410723, 500900) and 2 others are in
Kyushu University Geological Collection (GK.
H 5568 and GK. H. 5930 obtained by M. Suda
and T. Takahashi respectively, both presented
through T. Matsumoto).
Description:-The adult shell is of moderatesize, about 90 mm in diameter in the holotype
and 95 mm in the paratype 1. The body-chamber
occupies about 150° - 170°, slightly less than ahalf whorl.
The adult body-chamber is subrounded-subquadrate in section. It is somewhat broader thanhigh, with the proportion of B/H about 1.18 to
1.20, being broadest somewhat below the middleof the whorl·height. In its last part (for about
110° - 130°) where its coiling deviates fromnormal spire, its venter is broadened, somewhat
flattened and provided with a shallow mediangroove. It has a rounded venter in the preceding
part. Its ventrolateral parts are well rounded,flanks are gently convex and inflated, umbilicalshoulders are abruptly rounded, passing to asteeply inclined umbilical wall. The umbilicus
is very narrow, about 6 per cent of the diameteron the internal mould. The adult shell is somewhat scaphitoid (clioscaphitoid) in aspect by adeviation from the normal spiral coiling forthe last 110° in the holotype and 130° in theparatype 1.
In the phragmocone, the whorl is morerounded in section, with a well rounded ventral
part and convex flanks. It is somewhat broader
than high, with the maximum breadth near theumbilical shoulder.
The shell formed in the mature stage, i.e. thebody-chamber and the last 75° (±l00) of thephragmocone, is ornamented with low andbroad ribs or undulations, which are distinct on
the outer part of the whorl but weakened andfading away as they approach the umbilicus.
They are fairly distant for each 90° or so before
and after the last suture, about 5 or 6 being
counted per quarter whorl. In the paratype 1,
they become more approximated on the lastpart of the body-chamber, numbering about
15 in the last 120°. In the holotype the distantMATSUMOTO etal.

290

A

t

Text-fig.1. Diagrammatic sketch of Anglonautilus japonicus. A: TTC. 390715(Holotype); B: TTC. 500413 (Paratype 1). Frontal and lateral views, with sutures
in A and the last suture (LS) only in B. Scale bar is 10 mm. (T. Matsumoto delin.)ribbing persists for a longer period and the ribs
tend to be gradually approximated on the lastpart, but they are not so dense and so numerous
as in the corresponding part of the paratype 1(about 9 in the last 120°). The ribs or undulations in the mature stage are so coarse thatthey are not only distinct on the surface of theshell but also well marked on the internal mould,
except near the umbilical area. They show aconvex curvature on the flanks and a considerably backward sinus on crossing the venter.
In the late part of the immature shell, withdiameters of 45 - 55 mm, the ribs on the external surface of the shell are fairly dense but

774. Cretaceous Nautiloids
Table 1.

291

Measurements (in mm) of Anglonautilus japonicus.

Specimen

DiameterUmbilicus

HeightBreadthB/H

Holotype(end)

88.0 (1)5.4 (.06)

51.0 (.58)

64.0 (.73)

1.19

"

(-110° )75.1 (1)5.1 (.07)

45.0 (.60)

53.0 (.71)

1.18(-145°)*

64.0 (1)39.0 (.61)

46.0 (.72)

1.18(-180°)

57.0 (1)34.0 (.60)

40.0 (.70)

1.18

Paratype 1 (end)"93.0 (1)3.2 (.03)

57.0 (.61)

68.5 (.73)

1.20(-120°)

75.0 (1)4.4 (.06)

46.0 (.61)

55.0 (.73)

1.20(-170°)*

64.0 (1)39.0 (.61)

47.0 (.73)

1.20

43.0 (.61)

53.0 (.76)

1.23

Paratype 2

70.0 (1)3.0 (.04)*end of phragmocone
weak. In still earlier stages they are almost imperceptible. There are fine lirae in parallel to theribs. Their curvature is similar to that of the ribson the adult shell. On the well preserved smaller
shell (less than 17 mm in diameter) spiral lirae
are also discernible, showing a finely reticulated
pattern by combination with the radial ones. The
surface of the internal mould is smooth in theimmature stages.
The suture is moderately sinuous, with ashallow ventral lobe, a low asymmetric saddle
at the ventrolateral shoulder, a shallow but
distinct lateral lobe on the flank and a smaller
saddle at about the umbilical shoulder. The
sinuosity of the suture varies to some (but not
to a great) extent with growth and also between
individuals. The well exposed sutures on theholotype represent the moderate state. The last
suture of the paratype 1 is a comparatively lesssinuous example. The sutures of the paratype 2,(TTC.400606)(PI. 59, Fig. 2), which is of middle
growth-stage, are fairly sinuous, showing a prominent saddle at about the umbilical shoulder.
The siphuncle crosses septa at a point somewhat ventrad from the center, about two fifthsof the ventro-dorsal distance from the venter.
Remarks:-The details of the ontogenetic
change in early immature stages will be describedin section B of this paper by Obata and Futakami.
Among numerous specimens from loco Ik

1100, there are two specimens which deviate
from the above descriptions. One is small andprobably immature, but distinct from others inhaving a compressed whorl (H > B); the otheris a distorted specimen of moderate size, but
unlike others of the corresponding size it has
the ribbing of Cymatoceras type. These two
specimens are excluded from the material of thepresent species, although we hesitate to givethem a definite specific name.
Comparison and discussion:-As there arefold-like major ribs which are distinct on theouter part of the adult whorl but weakened anddisappearing toward the umbilicus, this species
is undoubtedly referred to A nglonautilus. The
holotype of the present species is indeed similar
to the topotype of A. undulatus (Sowerby),from the Lower Greensand of England (Kummel,
1956, p. 430, pI. 20, figs. 1, 2; text-fig. 26),
with respect to the major ribs and the subquadrate section of the adult whorl, but theformer has lower and somewhat more numerous
ribs, a more inflated and broader whorl andmore sinuous suture with a small but distinct
saddle at about the umbilical shoulder. The
shallow ventral groove, approximation of theribs on the adoral part and somewhat scaphitoid
coiling of the body-chamber are characteristicof the present species.
Any of the specimens of A. japonicus representing various growth-stages is different

292

MATSUMOTO etal.

from the illustrated specimens of A. undulatus
from the Cenomanian of England (Sharpe, 1953,
p. 15, pI. 5, figs. 4a-c) and the northern Caucasus(Shimansky, 1960, pI. 7, fig. 1) by its more
inflated broader whorl and weaker, less distantfold·like ribs. It is, however, noted that an
exceptional specimen (TTC. 400516) in our
population somewhat approaches to the British
Cenomanian form, as will be explained in moredetail in section B.
As one of us (T. M.) has mentioned in Part 2of this serial publication (Matsumoto in Matsu·
moto and Muramoto, 1983), the pattern ofsuture varies between species of Cymatoceras,
but the majority of the species has somewhat
sinuous sutures which range between those of
Cenoceras and Kummeloceras. A few species
show more sinuous sutures in which a small
but distinct saddle is developed at about theumbilical shoulder. This pattern is similar to thatof A. japonicus. In A. japonicus, however, there
is some extent of variation in the sinuosity ofsutures and the most sinuous example approach·es to, if not so strongly folded as, the suture of
Paracymatoceras asper (Oppel) or P. texanum(Shumard) (see Miller and Harris, 1945, pIs. 3·5,
text·figs. 3A, 8).
The paratype 1 of A. japonicus somewhat
resembles the holotype of Paracymatoceras
tunghaicum Matsumoto et Amano (1964, p. 175,
pI. 26, fig. 1; text·figs. 2, 3), from the Lower
Cenomanian of western Kyushu, in having thesubquadrate whorl·section, the ventral groove
and the Cymatoceras type ribs which are shownin the last stage not only on the surface of shell
but also on the internal mould. The angle of theventral sinus in the former is not so sharp andso small as in the latter.
Although the latter is imperfectly preserved,

it has no fold·like ribs in the preceding mainpart of the mature shell. The whorl of the former
has more inflated flanks. The strongly folded
suture in P. tunghaicum is the prime distinction.
A. japonicus is similar to A. mamiyai Matsu·
moto et Miyauchi (1983, p. 226, pI. 50, fig. 1),
from the Campanian of northern Hokkaido, inthe subrounded-subquadrate section of the body·chamber and the shallow ventral groove on theadoral part, but is distinguished by much weakerribs, narrower almost closed umbilicus andless sinuous sutures of the latter species.
Occurrence:-The holotype and 16 otherspecimens occurred in the sandstone of loco
Ik 1100, Katsurazawa pit (now abandoned),on the right side of the main stream of the
Ikushumbets, central Hokkaido. The silty fine·grained sandstone of the pit belongs to the Zoneof Mantelliceras japonicum, upper Lower Ceno·
manian. A few other specimens were obtained
from the same zone in the Torii·zawa (=Shimo.
ichi.no·sawa), a tributary to the Ikushumbets
and in the Onko·no-sawa, a branch of the Pom·bets. See Matsumoto, 1965 and Matsumoto
et al., 1969 for the location of Ik 1100.
B.ONTOGENY(I. Obata and M. Futakami)Material and Method
Twenty specimens, which were collected
mainly by T. Takahashi, of Anglonautilus japon·
icus are used for this study. As to the details ofmaterial see section A of this paper by Matsu·
moto and Takahashi. All the localities belong to
the Mantelliceras japonicum Zone, upper Lower
Cenomanian.
As the first step to examine the biometry,
we have measured the shell·diameter, the whorl·

Explanation of Plate 57
Fig.l. Anglonautilus japonicus Matsumoto et Takahashi . . . . . . . . . . . . . . . . . . . . Page 289
Holotype, TTC. 390715, from loco Ik 1100, Katsurazawa Pit, Ikushumbets area.
Left (a) and right (b) lateral, back (c) and frontal (d) views, xl.
Photos in Pis. 57-(>9 all by courtesy of Dr. M. Noda.

MATSUMOTO et at. ,' Cretaceous Nautiloids - IV

Plate 57

774. Cretaceous Nautiloids
height and the whorl·breadth of each individual
by means of calipers and discussed on the averagerelative growth of the species. We also have
prepared polished cross-section (TTC. 3909171) and longitudinal ones (i.e. TTC. 380414 andTTC. 400530), which have been examined bymeans of the profIle projector (V-16D, Nippon
Kogaku Co.) and the WILD microscope.
Observation of Variation
Adult stage:-The specific diagnosis of thepresent species has been described in detail in
section A by Matsumoto and Takahashi. Accord·
ing to them, the fold·like ribbing is character·istic of the adult stage (e.g. TTC. 390715 andTTC. 500413) and a shallow median groove isformed in the adoral part.
The ribs are thick and widely interspaced in
the main part of the adult stage but gradually
approximated in the last part.
Middle stage:-The middle stage is here
defined as being from the appearance of nepionicconstriction to that of distinct ribs. Eighteen
Table 2.

293

specimens have been examined. A variation isrecognized in the shell form: the ratio of whorl·breadth (B) to whorl·height (H) varies from
1.10 to 1.40, that of whorl·height (H) to shell
diameter (D) from 0.53 to 0.71, and that ofwhorl·breadth (B) to shell diameter (D) 0.67 to
0.81.
The whorl·section is generally semi-circularin outline, being rounded on the venter andthe ventro·lateral margin, except for TTC.
400516 which has a rather subquadrate to sub·rounded cross·section. In TTC. 400516, theventer is more gently arched, and the flanks areflattened and slightly convergent to the sub·rounded or subquadrate ventro·lateral margin.
TTC. 400516 shows, however, a pattern ofsuture·line similar to that of the other speci·
mens, a similar value of B/H and was obtained
from the same locality with most of them.
Thus TTC. 400516 can be included within thescope of variation of this species.
So far as the examined specimens (TTC.
390419, TTC. 390726-3, TTC. 400530) areconcerned, the position of siphuncle clearly

Measurements of the middle-aged and the earlier individuals in diameter, whorl·height
and whorl·breadth.
Specimen

D

H

HID

B

B/D

B/H

TTC.390419 (-180°)
TTC.380414 (-180°)
TTC.390726-3 (-180°)
TTC.410710
TTC.390917-1 (-180°)
TTC.400530 (-180°)

62.2
43.6
45.5
47.8
42.6
42.1
27.8
39.0
30.4
29.9
23.4
22.5
27.2
22.0
19.3
52.0
30.0

43.9
(27.5)
26.7
32.6
26.4
27.8
15.4
23.9
(18.4)
17.5
13.7
11.9
15.6
13.5
11.0
33.5
18.5

0.71
(0.63)
0.59
0.68
0.62
0.66
0.55
0.61
(0.61 )
0.59
0.59
0.53
0.57
0.61
0.57
0.64
0.62

48.1
32.4

0.77
0.74

1.10
(1.18)

38.2
34.0
32.1
19.7
(30.1 )
21.6
22.7
18.9
(16.1 )
21.9
16.0
13.0
40.0
23.2

0.80
0.80
0.76
0.71
0.77
0.71
0.76
0.81
(0.72)
0.81
0.73
0.67
0.77
0.77

1.17
1.29
1.15
1.28
1.26
(1.17)
1.30
1.38(1.35 )
1.40
1.19
1.18
1.19
1.25

TTC.390726-1
TTC. 390726-2
TTC.400516
TTC.391102
TTC.370524 (-180°)
TTC.390917-2 (-180°)
TTC.370717
TTC.410723
TTC.500900
GK. H 5568
GK. H 5930

MATSUMOTO etal.

294

the standard line. The radius (R) against the
total rotation angle (S) is shown on the Textfigs. 3,4.
The result of measurements by means of
the profile projector (Nikon) illustrated in Textfigs. 5, 6 is based on Table 3. Two critical points
are recognized at 1.21T and 21T, in the totalrotation angle, respectively (Text-fig. 6). Thus
the distinguished spiral stages are represented
as an equation, r .. ae kO (Obata, 1960). Some
previous authors (e.g. Hirano, 1977; Hirano
and Obata, 1979; Hirano et al., 1980) havestudied the biometric characteristics of therecent Nautilus. The spiral growth of theexamined specimens of Cretaceous Anglonautilus
japonicus can be expressed thus:

deviates from the median, longitudinal plane tothe left side. Among them TTC. 390726-3 is anextreme example.
Ontogenetic Development
Average relative growth:-The allometricequation of coiled cephalopods is represented
as follows (e.g. Obata, 1959): y = {3XCl!, where(3 is initial growth index, and Cl! is growth ratio.
We calculated the constant values of allometricequation of Anglonautilus japonicus Matsumoto
et Takahashi on the average relative growth(Table 2). The result is that the whorl-height (H)shows a positive allometry against the shelldiameter (D), being H = 2.055Dl.061 and thewhorl-breadth (B) shows a negative allometry
against the shell-diameter (D) and the whorlheight (H) respectively, being B = 1.222Do. 86s
and B = 2.136Ho. s:zS (Text-fig. 2).
Individual spiral growth:-For measurementsof spiral growth on the venter in the longitudinal
section we regard a straight line which connects
the cross-point of first septum to ventral walland that to dorsal inner wall as a standard axis.
The other axis is defined as the perpendicularline, which passes through the latter point, to
A
E
E

~

R=2.535eo. 2678
w=74.72°

2nd stage

R=4.808eo. llS9
w=83.46°

R=4.592eo. 1049
w=84.10o

3rd stage

R=3.304eo. 16s9
w=80.40o

R=3.914eo. 1S99
w=80.93°

c

B

~

.s:

50

E
.' E
.s: 50

50

"'0

"'0

...

...

a

Cl

a

QI

QI

~

I

I

...
0

10

~
20

n=20

...

H=2.05501.061.s:

r ~0.9942~

50

Shell -

Text-fig. 2.
breadth.

QI

m 20

20

.s:

1st stage

TTC.380414
R=2.477eo.:z 728
w=89.94°

E
E

..s:
I

TTC.400530

n=19

0

10

20

20.:"

...o

n=19

B=1.22200. 865.s: 10

B=2.136HO. 825

r=0.9915~

r=0.9943

50

Diameter (mm)2050Whorl-Height (mm)Average relative growth on the shell-diameter, the whorl-height and the whorl-

Explanation of Plate 58
Fig. 1. A nglonautilu8 japonicu8 Matsumoto et Takahashi . . . . . . . . . . . . . . . . . . . . Page 289
Paratype 1, TTC. 500413, from loco Ik 1100. Lateral (a), adorally ventral (b),back (c) and frontal (d) views, xl.

MATSUMOTO et at.: Cretaceous Nautiloids - IV

Plate 58lc

774. Cretaceous Nautiloids

295

T
T

~R4

R21
R6

------iText-fig. 3. Illustration of the longitudinal section showing theradius (R1-R7) from the axis. N.C.: Nepionic constriction.
represents a slow transitional one between the
rapid first and the moderate third ones (Text-fig.
6) in the early whorl.
As to the pattern of the septal formation(Table 3) the following three stages are distinguished:
514

510

Text-fig. 4. Illustration of the longitudinal
section showing the total rotation angle (81817) from the axis. N.C.: Nepionic constriction.
The growth ratio of the second stage isminimum amongst the ratios. In TTC. 400530
the nepionic constriction is detectable at 1.71r
in the second stage. To know the growth patternin detail we examine the value of radius (R) between R4 and R5 by each 10° in the total rotation angle (Text-fig. 7).
If we ignore the dropping of radius caused by
the shape of nepionic constriction, the relation
between Rand () may be almost linear (Text-figs.
7, 8). Thus the second stage :>f spiral growth

1st stage
1st and 2nd chamber

8 (degree) is small

2nd stage
3rd to 7th chamber

8 (degree) is large

3rd stage
8th to 21st chamber

8 (degree) is small

The nepionic constriction is just situated at
the anterior side of the seventh chamber (Textfigs. 3, 4). In other words, the formation of
nepionic constriction seems to be related to theformative velocity of periodic septum.
Naef (1921-1923) has already pointed out
the similar tendency of ontogenetic change inthe septal interspace on a living Nautilus: theinterspace of the first to third chamber is narrow,that of the fourth to seventh is wide, and thatof the eighth and the successive chambers isagain narrow. Shimanskiy (1948) also observed
an ontogenetic difference of the septal interspace on some Paleozoic orthocerids.

296

MATSUMOTO etal.

A

20

B

20

o

N

III
~

15

III

c

0.
CII

III

10

10

.

.x_I.e.
~

CII

.c

E

::J

Z

Total

rotation

angle

from

the

axis

Text-fig. 5. Relation of the septum number (81-820) and the total rotation angle from theaxis. A: TTC. 400530; B: TTC. 380414. N.C.: Nepionic constriction.

B

A

E

E
......

50

..

III

c

..

CII

.s::.

E
o

1=2.5IUO. 1II1-=11.12· I

1
1
III

I
I

11

I

114 .. ,x~" t

~

•. '

RI

III
::J

HI

I

I

I

I
I
I

I

II
H=2.I111 0.2111

HI

11.1=11.'"III
10

1=1.1111 1.1111

I

.

I

HI

HI

1=1.I1I1 I . UII

I.~~•• ' · I

t&.I=IO.U·

hI= 11.13'

I
I

HI

1=1.1011 0.1111

"C

a:

I

I
I

1=1.5,,,0.1011
k.I=".100

W=IU.·

11

HI

Total

rotation

angle

from

the

axis

Text-fig. 6. Relation of the radius and the total rotation angle from the axis. Equation of the
spiral growth is shown. A: TTC. 400530; B: TTC. 380414.

Explanation of Plate 59
Figs. 1, 2. Anglonautilus japonicus Matsumoto et Takahashi . . . . . . . . . . . . . . . . . Page 289
1. GK. H 5568, from loco Ik 1100. Two lateral (a, b), frontal (c) and back (d)views of an immature example, xl.
2. TTC. 400606, from loco Ik 1100. Two lateral (a, b) and back (c) views of a
middle-aged example, showing fairly sinuous sutures, xL

MATSUMOTO et al. : Cretaceous Nautiloids - IV

Plate 59

3

2a

6a

6b

6e

6d

774. Cretaceous Nautiloids

297

10

E
E

E
E

H5

20

Ul
>C

Cl

Ul

..
-

>C

83

GI
£

a
QJ

£

ER!
0

HI
15
____
_______

HI

10. - - - - - - ••iI'
N&pionic constriction

I

~

E
0

Ul

~

;:,

Ul

;:,

"0
Cl

HI

"0

a

0:

3/2

0:
3/2

Tota 1 rotation angle

2 ""

Total

rotationangle

Text-fig. 7. Relation of the radius (R4 to
R5) and total rotation angle from the axis on
TTC. 400530. N.C.: Nepionic constriction.
Table 3.

5/21[,

Text-fig. 8. Relation of the radius (R2R6) and the total rotation angle from the axis on
TTC. 400530.

Measurements on the spiral growth in radius from the axis (R), total rotation angle from the axis (8) and the septum number.
TTC.380414

TTC.400530

SeptumR (in mm)S (degrees)

R (in mm)S (degrees)

1
2
3
4
5
6
7
8
9
10
11
12
13
14
15
16
17
18
19
20

1.999
4.252
5.813
7.571
8.953
12.16015.866
20.11434° 43'63°35'
52°08'
62° 45'45°51'
40°30'
27°34'
27°35'
23°20'
27°12'
25°15'
22°30'
21°13'
19° 40'20°56'
21 0 56 '21 °15'23°00'
24°20'
23°35'

2.383
3.851
5.878
8.275
9.910
12.36715.92420.97425.48026°20'
49°35'
55°04'
53° 40'45°24'
37°31'
22°50'
16°00'
19°18'
22°26'
29° 40'20°30'
21 °22'
21 °32'
21 °54'23°36'
22°18'
14°19'
23°00'
19° 47'

MATSUMOTO etal.

298
Concluding Remarks

1. An observation of the spiral growth in earlystage on Anglonautilus japonicus from the
Cenomanian of Hokkaido has confirmed theexistence of two critical points, i.e. 1.21T and
21T in total rotation angle from the axis. The
nepionic constriction is recognized at a point
between the two critical points.
2. As to the septal interspace three growthstages are noticed in the early whorl. In otherwords, the first and the second chambers are
small, the third to the seventh large, and theeighth and the successive chambers again small
in total rotation angle from the axis.
3. Thus the pattern of septal growth on theearly whorl in Anglonautilus japonicus has
some similarity with that in Nautilus pompilius.
However, the latter differs from the former inthat the first three septa are close together,
the third to the seventh septa are the mostwidely spaced, from the seventh septum on
they are fairly close together again (Stenzel,1964).
4. Anglonautilus japonicus, which has an adultshell of about 90 mm in diameter,. shows agreat changes of the growth pattern near thenepionic constriction (D=15 mm). Thus theend of the embryonic stage of the species canbe defined at about 15 mm in diameter. On theother hand, the nepionic constriction of Nautilus
pompilius, a living nautilus which has an adultshell of about 200 mm in diameter, is at about

25 to 27 mm in diameter (Naef, 1921-1923)
and is regarded as the end of the embryonicstage (Stenzel, 1964; Cochran et al., 1981;
non Eichler and Ristedt, 1966). On Nautilus
macromphalus the egg is estimated as 45 mm indiameter (Stenzel, 1964). Accordingly, theegg diameter of Anglonautilus japonicus ispresumed to be smaller than that of the living
Nautilus.
References Cited(For brevity the references listed in Parts 1-3
are not repeated here.)
Cochran, J. K., Rye, D. M. and Landman, N. H.
(1981): Growth rate and habitat of Nautilus
pompilius inferred from radioactive andstable isotope studies. Paleobiology, vol. 7,
p.469-480.
Eichler, R. and Ristedt, H. (1966): Untersuchungen zur Fruhontogenie von Nautilus
pompilius (Linnaeus). Paliiont. Z., va!' 40,
p. 173--191, pis. 16-17.
Hirano, H. (1977): Biometrical characteristics
of Nautilus pompilius, Gakujutsu Kenkyu(the Sci. Resear.), Ser. Bioi. Geol., Schoolof Educ., Waseda Univ., vol. 26, p. 13-23.
- and Obata, I. (1979): Shell morphology
of Nautilus pompilius and N. macromphalus.
Bull. Natn. Sci. Mus., Ser. C. (Geo!.), vol.
5,no.3,p.113-130.
- , - - and Tanabe, K. (1980): Biometriccharacteristics. In Hamada et al. (eds.)
Nautilus macromphalus in captivity, p. 34-

Explanation of Plate 60
Anglonautilus japonicus Matsumoto et Takahashi

Fig.1. Frontal (a), lateral (b) and ventral (c) views of TTC. 370717 from loco Ik 7758 p, theOnko-no-sawa, a branch of the Pombets.
Fig. 2. Frontal (a), lateral (b, d) and ventral (c) views of TTC. 391102 from loco Ik 1100, Katsurazawa Pit, Ikushumbets.
Fig. 3. A longitudinal section of TTC. 400530 from loco Ik 1100.
Fig. 4. A cross-section of TTC. 390917-1 from loco Ik 1100.
Fig. 5. Frontal (a), lateral (b, d) and ventral (c) views of TTC. 390726-3 from loco Ik 1100.
Fig. 6. Frontal (a), lateral (b, d) and ventral (c) views of TTC. 410710 from loco Ik 1100.
All specimens were collected by Takemi Takahashi and photographed by Masao Futakami.

MATSUMOTO et al. : Cretaceous Nautiloids - IV

Plate 60lb

774. Cretaceous Nautiloids
43, Tokai Univ. Press, Tokyo.
Matsumoto, T. (1965): A monograph of the
Collignoniceratidae from Hokkaido. Part 1.
Mem. Fac. Sci., Kyushu Uniu., Ser. D,
vol. 16, no. 1, p. 1-80, pIs. 1-18.
and Miyauchi, T. (1983): Cretaceous
nautiloids from Hokkaido - III. Trans.
Proc. Palaeont. Soc. Japan, n.s., no. 132,
p. 220-229, pIs. 47-50.
and Muramoto, K. (1983): Cretaceous
nautiloids from Hokkaido - II. Ibid.,n.s., no. 130, p. 85--95, pIs. 16-20.
Muramoto, T. and Takahashi, T. (1969):
Selected acanthoceratids from Hokkaido.
Mem. Fac. Sci., Kyushu Uniu., Ser. D,
vol. 19, no. 2, p. 251-296, pIs. 25-38.
and Takahashi, T. (1982): A new nautiloid
species from the Cretaceous of Hokkaido.
Proc. Japan Acad., vol. 58, Ser. B, no. 10,
p.295-298.
Naef, A. (1921-1923): Die Cephalopoden,

299

Fauna e Flora di Golfo di Napoli, Stazione
Zool. Napoli Mon., vol. 35, pt. 1. 1. p. 5578.
Obata, I. (1959): Croissance relative sur quelques
especes des Desmoceratidae. Mem. Fac. Sci.,
Kyushu Uniu., Ser. D, vol. 9, no. 1, p. 3345, pIs. 4, 5.
-(1960): Spirale de quelques ammonites.
Ibid., vol. 9, no. 3, p. 151-163, pI. 15.
Shimanskiy [Shimansky], V. N. (1948): Sovremenniy nautilus i ego znachenie dlya
izucheniya
iskopaemykh golovonogikh,Moskouskoie gosudarst. Pedagog. Inst. V. N.
Lenin, vol. 52, no. 3, p. 78-151, pis. 10-14.
--(1960): In Drushchic, V. V. and Kudryavcer,
M. P., Atlas of the Lower Cretaceous faunaof the northern Caucasus and Crimea.
VNIIGAS Trudy, p. 239-248, pIs. 1-8 (inRussian).
Stenzel, H. B. (1964): Living Nautilus. In Moore,
R. C. (ed.): Treatise on Inuertebrate Paleontology (K) Mollusca 3, p. 59--93.

Ikushumbets [IkushunbetsuJ ~1!fZIj, Katsurazawa tlUR, Onko-no-sawa *:/::z Q)~,
[PonbetsuJ ~ZU, Shimo-ichi-no-sawa ~-Q)~, Torii-zawa .~Ii5~~trlaj!tg[8!.1Uc* ry J.. jl1 Jf{-IV.

7CQ) 4.

~trla~ Q) -!z /"7

Pombets=- 7:/ ,ii:Q)Jl,*il; 7.> 1 fI:

A. 7tMa ~~7JIJ:it!tljQ)TIl'Il-!z / "7 =- 7:/ Mantelliceras japonicum *,ii:Q)k1-~*,H.:.£-:i ~Anglonautilus japonicus ~~c~L.. t-:o *f!I!'t~~fi A. undulatus (Sowerby) I.:.~t L.., Jt1Jn~~~ <r,,'J!Fhn~~ <, {3:mm:~ml-cwl':' t.r..., "( ~, <.: c. ~JlQ).Mn'$ <. :Iil~ifll71-ITiis:p:!R:I':'~
H!:!F~n'il;7.>': c. n1MJJtQ)illUitJn' J: 9 ~ U'': c t.r. c"'(IK7JIJ~.h7.>o 1ITJ1I\l1.:.:t:-Q)tt~I':'lt.

Cymatoceras It ~c J: I). Paracymatoceras c ~~;;m~7f--rgn'il; I) Jl'*f,!E1.

'0(f'~*}ti!~ • i*if.ljil;;~)OO~.~. ~~f!I!Q)OO~W~~~. ~~.A~J:~OO.A~c~~NL..ko :t:-Q)M*.
<1.:.!I\l«J.i.~if<~-Clt. ~~~Q).~@]~~n' 1. 21: ~ J: ~ 21: #jl[I.:.:t:-.n.:f.n.3gn:~69-'tQ)r,,'t.:. nepionic constriction tMf:f£-r 7.> 0 t-:Iffflm;Q)Jf%tW~I':' ~3~Q).~Wln'~
jlj~.n. m~* ry J.. 711 M c Q)~Jmg Ultilt~i1'~69t?.n 7.>0(/h!il.fi~~ • =H&;Ic)

a

t?.n.

c

'*

Trans. Proc. Palaeont. Soc. Japan, N.S., No. 133, pp. 300-312, pI. 61, April 30, 1984

775. EARL Y CARBONIFEROUS (VISEAN) BRACHIOPODS FROM
THE HIKOROICHI FORMATION OF THE KITAKAMI MOUNTAINS,NORTHEAST JAP AN*
JUN-ICHI TAZAWA
Institute of Geology and Paleontology, Tohoku University, Sendai 980

Abstract.
A brachiopod fauna from the upper 105 m of the Hikoroichi
Formation of the southern Kitakami Mountains suggests a Late Visean age forthat part of the formation. It matches well with the fact that the Hikoroichi Formation is overlain conformably by the Upper Visean Onimaru Formation. The
fauna includes the following species: Schizophoria resupinata, Rhipidomella sp.,
Orthotetes sp., Pustula cf. pustulosa, Karavankina sp., Cleiothyridina sp., Spirifersp., Choristites bisulcatus and Tomiopsis sp.

Okubo, 1951a; Endo and Matsumoto, 1962;
Araki and Koizumi, 1968; Kobayashi and Hamada, 1980) and 2 crinoids (Minato, 1951). Theseauthors assigned the Hikoroichi Formation or its

Introduction
The Lower Carboniferous sequence, excluding the uppermost limestone unit, of the Hikoroichi district (Fig. 1), southern Kitakami Mountains, northeast Japan has long been famous
because it contains fossiliferous marine strata
of earliest Carboniferous age. This sequence was
first introduced in 1948 by Minato and Okubo
as the Hikoroichi Series, and subsequently
defined lithostratigraphically as the Hikoroichi
Formation (Onuki, 1956).
Stratigraphy of the Hikoroichi Formation
became more firmly established by Minato(1950), Okubo (1951b), Minato et al. (1953),
Onuki (1956, 1969), Saito (1968) and Haga
(in Minato et ai., 1979). The following species
have hitherto been described from this formation: 1 rugose coral (Kato, 1959), 1 conularid(Sugiyama, 1938, 1942), 21 bryozoans (Sakagami, 1962), 16 brachiopods (Minato, 1951,
1952; Minato and Kato, 1977), 1 pelecypod(Minato, 1951), 10 trilobites (Sugiyama, 1944;

Fig. 1. Map showing the fossil localities
and the Hikoroichi district.

*Received March 3, 1983; read January 23,
1983 in Tokyo.
300

775. Early Carboniferous Brachiopods

fossil fauna to a Toumaisian age. Also, it wasconsidered that there was a log hiatus between
the Hikoroichi Formation and the overlying
Upper Visean Onimaru Formation (e.g. Minato,
1955a, 1966; Minato et al., 1953,1979).
In recent years, Mori and Tazawa (1980)
found some Visean rugose corals and brachiopods in the upper part of the Hikoroichi Formation of the type locality, and regarded thestratigraphic relationship between these twoformations as highly probably conformable.
Further occurrences of rugose corals indicating
a Visean age were reported by Kawamura,Niikawa and Kato (1981), Kawamura andKato (1982) and Niikawa (1982), from theupper Hikoroichi Formation. But these fossils
have remained undescribed.
In this paper brachiopods from the upper
part (upper 105 m) of the Hikoroichi Formation of the Hikoroichi district, previously only
listed as species (see ~1ori and Tazawa, 1980,
p. 143), plus newly identified forms, are described, and the age of the fauna is discussed.
The specimens are stored in the Institure of
Geology and Paleontology, Faculty of Science,
Tohoku University.
Stratigraphy
A thick sequence of marine Toumaisian andVisean carbonates, clastics and pyroclastics ispresent in the Hikoroichi district. The Lower
Carboniferous rocks are exposed in the Sakamotozawa, Yonosawa, Higuchizawa and Onimarusawa Valleys, forming a syncline plunging
gently to the north (Fig. 2). They have been
divided lithologically into two units: the Hikoroichi Formation and the Onimaru Formation.
The Hikoroichi Formation overlies, withangular unconformity, the Middle Devonian
Nakazato Formation (e.g. Okubo, 1951b; Minato
et al., 1979), and is in tum overlain conformably
by the Onimaru Formation. It consists mostlyof sandstone, with a basal conglomerate andintercalations of shale, acidic to intermediate
tuffs and limestone, 560 m in total thickness(Fig. 3). A rather thick (40-90 m), greyish

301

green, dacitic to andesitic tuff is developed at
the middle horizon, about 250 to 300 m above
the base of the formation. Fossils are generally
sparse, but in the lower part it contains highly
fossiliferous
sandstone and shale beds.
Brachiopods are predominant among various
invertebrates represented.
The brachiopods treated in this paper werecollected from localities KF151, 152, 153,
163 and 167. The geographic and stratigraphic
location and the host rock types are as follows(Figs. 1, 3):
KF151: Grey, fine-grained, calcareous sandstone, the top of the Hikoroichi Formation, at 590 m N of the peak of Mt.
Senokita, eastern slope facing theupper
Higuchizawa
Valley(Lat.
39°6'58"N, Long. 141°39'31"E).
KF152: Grey, fine-grained sandstone, 2 m
below the top of the Hikoroichi Formation, at 15 m SW of KF151.
KF153: Grey, fine-grained, calcareous sandstone, the top of the Hikoroichi Formation, at 20 m SW of KF151.
KF163: Grey, oolitic limestone, 80 m below
the top of the Hikoroichi Formation,
at 50 m SE of KF151.
KF167: Grey, fine-grained sandstone, 105 m
below the top of the Hikoroichi Formation, at 280 m SW of the junctionof the Sakamotozawa and Onimarusawa Valleys, eastern slope facing thelower
Onimarusawa
Valley(Lat.
39°7'34"N, Long. 141°39'32"E).

Age of the Fauna
The brachiopod fauna described here includes
the following species:
Schizophoria resupinata (Martin)
Rhipidomella sp.
Orthotetes sp.
Pustula cf. P. pustulosa (Phillips)
Karavankina sp.
Cleiothyridina sp.
Spirifer sp.
Choristites bisulca tus (Sower by)
Tomi6psis sp.

Jun-ichi TAZA WA

302

t

~1

8E\2l

2

~10

~3

mImI

~,

Rz\~;a 12

mIiiii!

S

11

13

§6
~ 7

EE] IS.8 [ZJ 16
.

-100

-aoo

-.

-100

L

Pro'il. L: H. I : 1_400

Fig. 2. Geologic map of the Hikoroichi district. I, 2: Sakamotozawa Formation (Lower
Permian; 1: Limestone; 2: Sandstone); 3,4: Nagaiwa Formation (Lower to Middle Carboniferous;
3: Limestone; 4: Sandstone); 5: Limestone of the Onimaru Formation (Lower Carboniferous);
6-8: Hikoroichi Formation (Lower Carboniferous; 6: Sandstone and shale; 7: Tuff of the upper
part; 8: Limestone); 9: Nakazato Formation (Middle Devonian); 10: Ono Formation (Lower
Devonian); 11: Kawauchi Formation (Middle to Upper Silurian); 12: Conglomerate of the Hikoroichi, Nagaiwa and Sakamotozawa Formations; 13: Shale of the Onimaru, Nagaiwa and Sakamotozawa Formations; 14: Tuff of the lower part of the Hikoroichi Formation and the Nagaiwa Formation; 15: Granitic rocks (Hikami Granite); 16: Dyke rocks.

775. Early Carboniferous Brachiopods

303

( 1)

I

~

I

J

Saka motozawa F.
(150 m+)°:0 ogooQg(PERMIAN)'0" '~~'o a '0 '00·.·· . :-:., _ _ _ _ _ _ _ _ _ _ _ __

( 2)

u.:
11I~

~

E

...

._ 0

111

N

Ol~

111

Z
DO

D

E5j
~ 2
~ 3

.. c
~ 0

•

::l

111

E

4

~ 5

EZJ 6
g:ooo*o 7m']00°00°.:';',':.-':::.'.::::.,',;',~::'.::,..':.:'..

;ffitf*t 8:J:~: tr:-'I>!.;~.:.!r/

o
..J

ITID
B
N a ka z a to

9
10
11

F.

(DEVON I AN)

Fig. 3. Columnar sections of the Carboniferous and Permian in the northern area (1) andthe southern area (2) of the Hikoroichi district, showing the stratigraphic positions of the fossil
localities shown on the index map, see Fig.!. 1-4: Limestone; 5: Shale; 6: Sandstone; 7: Conglomerate; 8, 9: Tuff; 10: Nakazato Formation; 11 : Stratigraphic discontinuity.

Jun-ichi TAZA WA

304

Each of the species listed above is represented
by a single specimen, except for four Rhipidomella sp. specimens and two Tomiopsis
sp. specimens.
Among these species, S. resupinata is a longranging species, which occurs in the Tournaisianto Visean. C. bisulcatus has been known fromthe Visean and Namurian of Europe, Asia andAustralia. Orthotetes sp. closely resembles O.
australis Campbell, 1957 from the Upper Viseanof New South Wales. Pustula cf. pustulosa iscompared with shells of P. pustulosa (Phillips,
1836), described or figured from the Visean ofwestern Europe and the Soviet Union. Karavankina sp. most resembles K. jizodoensis Tazawa ,1980 from the Upper Visean of the Nagasaka
district, southern Kitakami Mountains. Spirifer(s.s.) sp. is close to S. liangchowensis Chao,
1929 from the Visean of Gansu, South China.
The genus Karavankina Ramovs, 1969 has
not been found below the Upper Visean (Winkler
Prins, 1982). On the other hand, the upper age
limit of this fauna is assigned to Late Viseanfrom its stratigraphic level directly below theUpper Visean (e.g. Minato, 1955b; Okimura,1966) Onimaru Formation. Therefore, Karavankina sp., collected from the lowest fossil horizon(KF167), appears to have value in correlation.
The brachiopod fauna is considered to beof Early Carboniferous, Late Visean age. Thisconclusion agrees with the opinion (Kawamura
and Kato, 1982) based on rugose corals, andmatches well with the stratigraphic data suggesting that the Hikoroichi Formation is overlain
conformably by the Upper Visean Onimaru
Formation.
Description of Species
Order Orthida Schuchert and Cooper, 1932
Suborder Orthidina Schuchert and Cooper, 1932
Superfamily Enteletacea Waagen, 1884
Family Enteletidae Waagen, 1884
Subfamily Schizophoriinae Schuchert andLe Vene, 1929
Genus Schizophoria King, 1850

Schizophoria resupinata (Martin, 1809)

PI. 61, Figs. 9a, 9b
1809
1952
1968

1979
1979
1980

1981
1981

Conchyliolithus (Anomites) resupinatus
Martin, pI. 49, figs. 13, 14.
Schizophoria resupinata (Martin): Minato,
p. 150, pI. 5, fig. 3; pI. 6, fig. 4.
Schizophoria resupinata (Martin): Pocock,p. 80, pI. 18, figs. 7a, 7b;text-figs.13-15.
Schizophoria resupinata (Martin): Tazawa
and Katayama, p. 169, pI. 11, figs. 8 -14.
Schizophoria resupinata (Martin): Minato(in Minato et al. ), pI. 22, figs. 1, 2.
Schizophoria resupinata (Martin): Mori
and Tazawa, text-fig. 3.3.
Schizophoria resupinata (Martin): Tazawa,
Itabashi and Mori, pI. 1, figs. 4-6.
Schizophoria resupinata (Martin): Tazawa,p. 67, pI. 5, figs. 3-5. .

Material:-One specimen, internal mould of apedicle valve with the posterior portion of thebrachial valve attached, from locality KF167,
IGPS coIl. cat. no. 97898.
Descriptive remarks:-The single speCimen
from Hikoroichi is referred to Schizophoria
resupinata (Martin, 1809) on account of its large,
elliptical, flat pedicle valve and the ventral
internal structure, viz. a large, flabellate muscle
field, long, subparallel dental plates, high, strong
median septum and a pair of long vascularmarkings. The dimensions of the pedicle valve
are as follows: length about 45 mm, width about
70 mm, width of the hinge line about 32 mm.
The ventral muscle field is faintly sculptured
with several radial ribs on the anterior portion,and is bounded anteriorly by an accessory ridgeand postero-Iaterally by dental plates. The
median septum is low and thin on the posterior
portion, becomes high and strong anteriorly,
extends to but not projects beyond the anterior
margin of the muscle field. The vascula media
occurs just anterior to the muscle field, firstslightly diverging, then converging anteriorly.
In the Lower Carboniferous of the southern
Kitakami Mountains S. resupinata has been
described or figured from the Arisu Formation(Minato, 1952, 1979 in Minato et al.), Odaira
Formation (Tazawa and Katayama, 1979),

775. Early Carboniferous Brachiopods
Karoyama Formation (Tazawa, Itabashi andMori, 1981; Tazawa, 1981) and Hikoroichi
Formation (Mori and Tazawa, 1980).
Family Rhipidomellidae Schuchert, 1913
Genus Rhipidomella Oehlert, 1890
Rhipidomella sp.
PI. 61, Figs. 5-7

1979
1980

Rhipidomella sp. Tazawa and Katayama,
p. 170, pI. 11, figs. 1-7.
Rhipidomella sp. Mori and Tazawa,text-figs. 3.4-3.6.

Material:-Four specimens, from locality
KF163: (1) two pedicle valves showing theinternal structures, lOPS colI. cat. nos. 97899,
97900; (2) internal moulds of two brachialvalves, lOPS colI. cat. nos. 97901, 97902.
Remarks:-These specimens are assigned to
the genus Rhipidomella Oehlert, 1890 on thebasis of their small (length 25 mm, width 19
mm in the largest specimen, IGPS colI. cat. no.
97902), suboval shells, with the internal structure consisting of a large, flabellate ventral
muscle field, a large cardinal process, a pair ofstrong brachiophores and a quadripartite dorsal
muscle field.
The Hikoroichi species appears to be conspecific with Rhipidomella sp., described andfigured by Tazawa and Katayama (1979, p.
170, pI. 11, figs. 1-7) from the Odaira Formation of the Yokota district, southern Kitakami
Mountains because of similarities in size andshell outline.
Order Strophomenida Opik, 1934
Suborder Strophomenidina Opik, 1934

Material:-One specimen, external and internal moulds of a brachial valve, from locality
KF167, lOPS colI. cat. no. 97903.
Description:-Brachial valve gently and evenly
convex in lateral profile; length about 59 mm,
width uncertain but probably over 80 mm.
External ornament of the brachial valve
consisting of numerous costellae, fine radiallirae, irregular, strong concentric or oblique
rugae and very fine growth lines. Costellae
with many intercalations, slightly sinuous anteriorly; 7-8 costellae in 5 mm width near theanterior margin of the valve; 1 or 2 lirae occurring in the intercostal troughs. Rugae strongly
developed on the anterior half of the valve,mostly concentric, a few of them oblique; 3-5
rugae within 20 mm of the anterior valve margin.
Brachial valve interior with a pair of long,straight vascula media extending to the midvalve.
Other internal structure not observed.
Remarks:-This specimen agrees with Orthotetes australis (Campbell, 1957, p. 45, pI. 11,
figs. 1-7) from the upper part of the lower
Burindi Group (=Upper Visean Merlewood
Formation, after Roberts, 1975, p. 13) of Watts,
Babbinboon, New South Wales in shape andexternal ornament of the brachial valve, especially the density of lirae in the intercostal
troughs.
In size and external ornament, the Hikoroichi
specimen somewhat resembles Orthotetes sp.
from the Lower Namurian of Akiyoshi, southwest Japan (Yanagida, 1965, p. 120, pI. 27,
figs. 9-14), and also Orthotetes cf. australis
from the Upper Visean Karoyama Formationof the Nisawa district, southern Kitakami Mountains (Tazawa, 1981, p. 69, pI. 5, figs. Sa, 8b).
But the poor preservation of the present material
makes accurate comparison difficult.

Superfamily Davidsoniacea King, 1850

Suborder Productidina Waagen, 1883

Family Orthotetidae Waagen, 1884

Superfamily Productacea Gray, 1840

Subfamily Orthotetinae Waagen, 1884

Family Echinoconchidae Stehli, 1954

Genus Orthotetes Fischer, 1829

Subfamily Echinoconchinae Stehli, 1954

Orthotetes sp.

GenusPustula Thomas, 1914

PI. 61, Figs. 11a, 11b

305

Jun-ichi T AZA WA

306

Pustula cf. P. pustulosa (Phillips, 1836)

PI. 61, Fig. 81980 Pustula cf. P. pustulosa (Phillips): Mori
and Tazawa, text-fig. 3.2.

Material:-One specimen, external mould of abrachial valve, from locality KF152, IGPS coIl.
cat. no. 97904.
Descriptive remarks:-The brachial valve from
Hikoroichi may have originally been about 80
mm wide, although the right half of the valve
has been broken off. The valve has a low andbroad fold, and is ornamented by numerous,
quincuncially arranged, elongate spine bases
and regular, concentric rugae on the externalsurface; 6-9 spine bases in 10 mm width, 6 rugaein 10 mm length at about the midvalve.
In size and external ornament, the Hikoroichi
specimen resembles shells of Pustula pustulosa(Phillips, 1836), described or figured from the
Visean of Britain (Phillips, 1836, p. 216, pI. 7,
fig. 15; Thomas, 1914, p. 261, pI. 17, figs. 2428; pI. 18, fig. 1; Muir-Wood and Cooper, 1960,
pI. 84, figs. 1--7; pI. 85, figs. 6-10), Belgium(Muir-Wood and Cooper, 1960, pI. 59, fig. 4),
Germany (Paeckelmann, 1931, p. 138, pI. 13,
figs_ 2, 3) and the Soviet Union (Sarytcheva
and Sokolskaja, 1952, p. 106, pI. 19, fig. 127;
Gubareva, 1964, p. 161, pI. 3, figs. 6-9; Kalashnikov, 1974, p. 51, pI. 10, figs. 6-9; pI. 11, figs.
1-2; pI. 13, figs. 4-5; pI. 30, fig. 6; Volginand Kushnar, 1975, p. 45, pI. 3, figs. 10-12).
Pustula sp., described by Minato (1952, p.
155) from the Odaira Formation of the Yokota
district, southern Kitakami Mountains, is close to
P. pustulosa in shape of th(' pedicle valve. It isa possible that Minato's Pustula sp. is a synonymof the present form.
Pustula cf. P. tenuipustulata (Thomas, 1914)
from the Arisu Formation of the Yokota district(Minato, 1952, p. 154, pI. 11, fig. 7) is clearly
distinguished from thp. present form by its
irregular and more closely arranged spine baseson the pedicle valve.

Family Buxtoniidae Muir-Woodand Cooper, 1960
Subfamily Karavankininae Ramovs, 1969
Genus Karavankina Ramovs, 1969
Karavankina sp.

PI. 61, Figs. 2a, .2bMaterial:-Gne specimen, external and internal moulds of a brachial valve, from locality
KF167, IGPS coIl. cat. no. 97905.
DescrzPtion:-Brachial valve elongate subrectangular in outline, flat on visceral disc,slightly concave near the anterior and lateral
margins of the valve. Hinge line straight, a little
less than the greatest width of the valve; thelatter occurring at about three-quarters of thelength of the valve. Umbo narrow, strongly
concave, not projecting behind hinge line. Ears
rather large, flat, trigonal, not clearly delimited
from visceral disc. Dimensions of the brachialvalve: length about 19 mm, width about 17 mm,
width of hinge line 13 mm.
External surface of the brachial valve ornamented by regular, concentric, lamellose bands
bearing numerous, quincuncially arranged, elongate spine bases; 7-9 bands in 10 mm length at
the anterior half of the valve.
Internally, brachial valve with a median
septum and a pair of buttress plates; median
septum being 6.3 mm long, not fusing withcardinal process, low and thin on the posterior
portion, becoming high and strong anteriorly;
buttress plates elongate, trigonal, 4.2 mm long,situated on both sides of median septum.
Remarks:-The fragmentary external mouldof brachial valve described here is slightly indented at the mid portion, but this concavity
may not be original. The dorsal external ornament is badly preserved, except for the concentric, lamellose bands. The internal structureis also poorly preserved; both the cardinal
process and lateral ridges cannot be observedin the present material.

775. Early Carboniferous Brachiopods

In spite of the ill state of preservation, thisspecimen is assigned to the genus Karavankina
Ramovs, 1969 on the basis of its small, sub·rectangular brachial valve, the external ornamentof concentric, lamellose bands and quincunciallyarranged spine bases and the presence of buttressplates in the brachial valve.
Karavankina jizodoensis Tazawa (1980, p.
362, pI. 41, figs. 8-16; pI. 42, fig. 14; text.fig.
2) from the top of the Karaumedate Formationof the Nagasaka district, southern Kitakami
Mountains, resembles the present form in thedensity of concentric bands on the brachialvalve (8-9 bands in 10 mm length in K. jizodo·
ensis; 7-9 bands in 10 mm length in Karavankinasp). Unfortunately the preservation of the
Hikoroichi specimen does not permit compari·son with K. jizodoensis.
Karavankina praepermica Ramovs (1969, p.
258, 265, pI. 3, figs. 1-6) from the Upper
Carboniferous (Orenburgian) of the Karavanken,
Yugoslavia, is small in size like Karavankina sp.,
but the former is distinguished from the latter by
its thin, more widely divaricated buttress plates
in the brachial valve.
Order Spiriferida Waagen, 1883
Suborder Athyrididina Boucot,
Johnson and Staton, 1964
Superfamily Athyridacea Davidson, 1881
Family Athyrididae Davidson, 1881
Subfamily Athyridinae Davidson, 1881
Genus Cleiothyridina Buchman, 1906
Cleiothyridina sp.
Pl. 61, Fig. 3

Material:-One specimen, external mould of avalve fragment, from locality KF167, IGPS coIl.
cat. no. 97907.
Remarks:-One fragmentarily preserved speci.
men from Hi koroichi , having the characteristic
external ornament of concentric lamellae, theedges of which are fringed with numerous
flattened spines. It can be assigned to the genus

307

Cleiothyridina Buckman, 1906.
Externally, this specimen somewhat resembles
the lectotype (BM(NH)BB58678) of Cleio·
thyridina fimbriata (Phillips, 1836) from theUpper Visean of Ireland; the latter was selected
and figured by Brunton (1980, p. 228, figs.
19a, 19b). But the Hikoroichi specimen is too
poorly preserved for specific determination.

Suborder Spiriferidina Waagen, 1883
Superfamily Spiriferacea King, 1846
Family Spiriferidae King, 1846
Subfamily Spiriferinae King, 1846
Genus Spirifer Sowerby, 1816
Spirifer sp.
Pl. 61, Figs. la -Ie

Material.·-One specimen with valves con·joined, from locality KF151, IGPS coIl. cat.
no. 97908.
Descriptive remarks:-An imperfect specimen
from Hikoroichi, lacking the anterior portion of
the pedicle valve and most of the brachial valve,
is wider than long, sub quadrate in outline, withrounded cardinal extremities; length presumably
about 35 mm, width about 55 mm. Numerous
bifurcating costae are developed on the sulcus
and each ventral lateral slope. Intercalationsof costae often occur on the lateral slopes.
This specimen is assigned to the genus Spirifers.s. on the basis of its size, shape and external
ornament of the pedicle valve, particularly inhaving rounded cardinal extremities, a sulcus
with numerous bifurcating costae and lateralslopes ornamented by numerous, freely bifurcat·
ing and intercalating costae.
The Hikoroichi specimen superficially reo
sembles Spirifer liangchowensis Chao (1929,
p. 6, pI. 1, figs. 1-7; text·fig. 1) from the Viseanof Gansu, South China.

Family Choristitidae Waterhouse, 1968
Genus Choristites Fischer, 1825

Jun-ichi TAZA WA

308

Choristites bisulcatus (Sowerby, 1825)

PI. 61, Figs. 4a, 4b1836 Spirifer bisulcatus Sowerby: Phillips,
p. 218, pI. 9, fig. 14.
1858 Spirifera bisulcata (Sowerby): Davidson,
p. 31, pI. 5, fig. 1; pI. 6, figs. 6-16 only.
1908 Spirifer bisulcatus Sowerby: Grober, p.
222, 239, pI. 26, figs. 3a-3c, 8-10; textfigs. 3,4.
1916 Spirifer bisulcatus Sowerby: Frech, p.
252, pI. 8, fig. 7.
1918 Spirifer bisulcatus Sowerby: Yanishevsky,p. 82, pI. 6, figs. 1, 15 only.
1920 Spirifera bisulcata (Sowerby): Benson
and Dun, p. 347, pI. 21, fig. l.
1922 Spirifer bisulcatus Sowerby: Hayasaka, p.
63, pI. 3, figs. 8-9.
1924 Spirifer bisulcatus Sowerby: Grabau, fig.
152.
1931 Choristites bisulcatus (Sowerby): Grabau,
fig. 6.
1932 Choristites bisulcatus (Sowerby): Grabau,
pI. 2, fig. 13.
1938 Spirifer bisulcatus Sowerby: Demanet, p.
88, pI. 8, figs. 17-19.
1970 Spirifer ex gr. bisulcatus Sowerby:
Abrampv, p. 142, pI. 22, fig. 8.
1980 Choristites bisulcatus Sowerby): Mori
and Tazawa, text-figs. 3.1a, 3.1b.

Remarks:-Bipartite development of sinal
costae, which characterized the Carboniferous
spiriferids, can be observed in the pedicle valve
specimen of Hikoroichi.
This specimen is referred to Choristites
bisulcatus (Sowerby, 1825) on account of its
size, shape and external ornament of the pedicle
valve. The Hikoroichi specimen superficiallymost resembles the pedicle valve figured by
Demanet (1938, pI. 8, fig. 18) as Spirifer
bisulcatus Sowerby from the Upper Visean ofBelgium.
Concerning the generic assignment ofSowerby's Spirifer bisulcatus, I follow Grabau's
opinion (Grabau, 1931, p. 26), in which thespecies is regarded as a simplest form of
Choristites. This species has been known fromthe Visean and Namurian of Britain, Belgium,
Siberia, Asia Minor, Central Asia, South China,
Japan and eastern Australia.
C. bisulcatus differs from Choristites mosquensis (Fischer, 1825) in having a smaller, moretransverse shell, with less complicated sinal
costae and less bifurcated lateral costae.

Suborder Delthyrididina Ivanova, 1972
Superfamily Martiniacea Waagen, 1883
Family Martiniidae Waagen, 1883

Material:-one specimen, external mould andcast of a pedicle valve, from locality KF153,
IGPS colI. cat. no. 97909.
Description:-Shell small size for the genus,
wider subtrigonal in outline, the maximum width
at hinge line, length 28 mm, width 34 mm.
Pedicle valve strongly and unevenly convex inlateral profile, with the greatest convexity at theumbonal region. Cardinal extremities blunt,
produced. Sulcus moderately deep, angular,
having a pair of simple primary costae, 1 or 2
simple costae on outside the primary costae.
External surface of ventral lateral slopes ornamented by numerous rounded costae; costae
mostly simple, a few of them bifurcated near
the anterior margin of the valve, with narrowintercostal grooves; 9 costae on one side ofthe lateral slope. Shell substance thick at umbonal region.

Subfamily Ingelarellinae Campbell, 1959
Genus Tomiopsis Benediktova, 1956
Tomiopsis sp.

PI. 61, Figs. lOa, lOb
Material:-Two specimens, internal moulds oftwo pedicle valves, with the external moulds ofthe posterior portion attached, from locality
KF163, IGPS colI. cat. nos. 97910, 97911.
Remarks:-These two specimens appear tobelong to the genus Tomiopsis Benediktova,
1956, because of their straight hinge line,
rounded cardinal extremities, clearly developed
ventral interarea and shallow sulcus, and thepresence of long, subparallel dental plates in
the pedicle valve.
The Hikoroichi specimens cannot be iden-

775. Early Carboniferous Brachiopods

tified with any previously known species of
Tomiopsis, because of the lack of infonnation

about the ventral external ornament and thedorsal external and internal features.
Acknowledgements
I wish to thank Professor K. fllIori of theInstitute of Geology and Paleontology, Tohoku
University for his field assistance, and for readingof the manuscript. My thanks are due to Professor S. Kanisawa of the Department of Earth
Sciences, Tohoku University for advice on
petrography, Professor P. Copper of the Department of Geology, Laurentian University, Canada
for critical reading of the manuscript, Mr. S.
Otomo of our institute for help with photography, and Mr. and Mrs. Sato of Setamai,
Sumita-cho for hospitality in the field.
References
Abramov, B. S. (1979): A6paMoB, b. C.: bHOCTpaTHrpacjlHll
KaMeHHoyroJlbHblX OTJlOlKeHHH
CeTTe-LI.a6aHa (lOlKHoe BepxollHbe). 178 p., 38
pis., HaYKa, MocKBa.

Araki, H. and Koizumi, H. (1968): Carboniferous and Permian trilobites of the Kitakami Mountains (2). Chigaku Kenkyu, vol.
19, no. 8, p. 211-214 (in Japanese).
Benson, W. N. and Dun, W. S. (1920): Thegeology and petrology of the Great Serpentine Belt of New South Wales, Pt. 9. The
geology, palaeontology and petrography of
the Currabubula district, with notes on
adjacent regions, Sec. B. Palaeontology.
Proc. Lin. Soc. N.S. W., vol. 45, p. 337374, pis. 18-24.
Brunton, C. H. C. (1980): Type specimens ofsome Upper Palaeozoic Athyridide brachiopods. Bull. Brit. Mus. (Nat. Hist.), Geol.,
vol. 34, no. 4, p. 219-234.
Campbell, K. S. W. (1957): A Lower Carboniferous brachiopod-coral fauna from New
South Wales. J. Paleont., vol. 31, no. 1, p.
34-98, pis. 11-17.
Chao, Y. T. (1929): Carboniferous and Permianspiriferids of China. Palaeont. Sinica, Ser. B,
vol. 11, fasc. 1, p. 1-101, pis. 1-11.

309

Davidson, T. (1858): British Fossil Brachiopoda.
Vol. 2, Pt. 5, No. 1. Monograph of British
Carboniferous Brachiopoda. Palaeontogr.
Soc. (1858), p. 11-48, pis. 1-8.
Demanet, F. (1938): La faune des couches depassage du Dinantien au Namurien dans Ie
synclinorium de Dinant. Mem. Mus. roy.
Hist. nat. Belg., no. 84, p. 1--201, pis. 1-14.
Endo, R. and Matsumoto, E. (1962): PermoCarboniferous trilobites from Japan. Sci.
Rep., Saitama Univ., Ser. B, vol. 4, no. 2,
p. 149-172, pis. 8-10.
Frech, F. (1916): Geologie Kleinasiens im
Bereich der Bagdadbahn: Ergebnisse eigener
Reisenundpaliiontologische
Untersuchungen. Zeitschr. Deut. geol. Gesell.,Bd. 68, p. 1-325, pis. 1-24.
Grabau, A. W. (1924): The Dinantian or Mississippian System. in Grabau, A. W.: Stratigraphy of China, p. 208-263, Geol. Surv.
China, Peking.
--(1931): Studies for students, Ser. 1. Palaeontology; The Brachiopoda, Part 2. Sci.
Quart., Nat. Univ. Peking, vol. 2, p. 397422.
--(1932): The significance of the sinal formulain Devonian and post-Devonian Spirifers.
Bull. Geol. Soc. China, vol. 11, p. 93-95,
pis. 1, 2.
Grober, P. (1908): Ueber die Faunen des untercarbonischen
Transgressionsmeeresdeszentralen Tian-schan, die in der Umgebung
des Sartdschol-Passes gefunden worden sind.
N. Jb. f. Min. Geol. Paliiont., Bd. 26, Ht.
2, p. 213--248, pis. 25-30.
Gubareva, V.S. (1964): fy6apeBa, B. C.: HOBbie)I.aHHble 0 6paXHOllO)l.aX HHlKHero Kap60Ha
BOJlro-Ypa.%'::Kofl 06J1aCTH. Tp. BHHTPH, T.
43, p. 146-179. pis. 1-4.

Hayasaka, 1. (1922): Paleozoic Brachiopoda
from Japan, Korea and China, Part 1.
Middle and Southern China. Sci. Rep.,
Tohoku Imp. Univ., 2nd Ser., vol. 6, no. 1,
p. 1-116, pis. 1-5.
Kalashnikov, N. V. (1974): KaJlaWHHKOB, H. B. :PaHHe KaMeHHoyroJlbHble 6paXHOllO)l.bI ne'lopCKoro YpaJla. 166 p., 52 pis., HaYKa, JIeHIIH-.
rpa)l..

Kato, M. (1959): On some Carboniferous corals
from the Kitakami Mountains. Trans. Proc.
Palaeont. Soc. Japan, N.S., no. 33, p. 33-43.

310

Jun-ichi TAZA WA

Kawamura, T. and Kato, M. (1982): Lower
Carboniferous biostratigraphy of the southern Kitakami Mountains, based on rugose
corals. Abst. 89th Ann. Mtg. Geol. Soc.
Japan, p. 247 (in Japanese).
- - , Niikawa, I. and Kato, M. (1981): On thestratigraphy of the Hikoroichi Formation.
Abst. 88th Ann. Mtg. Geol. Soc. Japan, p.
175 (in Japanese).
Kobayashi, T. and Hamada, T. (1980): Carboniferous trilobites of Japan, in comparison
with Asian, Pacific and other faunas. Palaeonto Soc. Japan, Spec. Pap., no. 23, p. 1132, pIs. 1-22.
Martin, W. (1809): Petri{icata Derbiensia; orfigures and descriptions of petrifactions
collected in Derbyshire. 28 p., 52 pIs.,
Wigan.
Minato, M. (1950): Stratigraphische Stellung derHikoroichi-Serie. J. Geol. Soc. Japan, vol.
56, no. 65'5, p. 143-148 (in Japanese).
--(1951): On the Lower Carboniferous fossilsof the Kitakami Massif, northeast Honsyu,
Japan. J. Fac. Sci., Hokkaido Uniu., Ser. 4,
vol. 7, no. 4, p. 355-382, pIs. 1-5.
--(1952): A further note on the Lower Carboniferous fossils of the Kitakami Mountainland, northeast Japan. Ibid., vol. 8, no. 2,
p. 146-174, pIs. 2-11.
- - (1955a): Zur stratigraphischen Lucke der
Pdi-Onimaru-8erie (Ober Vise) in Japan.
Ibid., vol. 9, no. 1, p. 31-41.
- - (1955b):
Japanese Carboniferous andPermian corals. Ibid., vol. 9, no. 2, p. 1202, pIs. 1-43.
--(1966): Stratigraphie des Palaeozoikums desKitakami·Gebirges und Abe-Orogenese inJapan. Prof S. Matsushita Mem. Vol., p.
143-159 (in Japanese).
- - , Hashimoto, S., Suyama, K., Takeda, H.,
Suzuki, Y., Kimura, S., Yamada, K., Kakimi,T., Ichikawa, T. and Suetomi, H. (1953):
Biostratigraphie des Karbons im KitakamiGebirge, nordostliches Honshu, Japan. J.
Geol. Soc. Japan, vol. 59, no. 695, p. 385399 (in Japanese).
- - , Hunahashi, M., Watanabe, J. and Kato, M.
(ed., 1979): Variscan geohistory of northern
Japan: The Abean Orogeny. 427 p., 144
pIs., Tokai Univ. Press, Tokyo.
--and Kato, M. (1977): Two spiriferids fromthe Hikoroichi Formation (Tournaisian) in

the Kitakami Mountains, Japan. J. Fac. Sci.,
Hokkaido Uniu., Ser. 4, vol. 17, no. 4, p.
613-617, pI. 1.
and Okubo, M. (1948): Correlation of theLower Carboniferous System of Japan.
J. Geol. Soc. Japan, vol. 54, no. 638, p.
167-168 (in Japanese).
Mori, K. and Tazawa, J. (1980): Discovery andsignificance of Visean rugose corals andbrachiopods from the type locality of theLower Carboniferous Hikoroichi Formation.
Ibid., vol. 86, no. 2, p. 143--146 (in Japanese ).
Muir-Wood, H. M. and Cooper, G. A. (1960):
Morphology, classification and life habitsof the Productoidea (Brachiopoda). Geol.
Suru. Amer. Mem. 81, p. 1-447, pIs. 1-135.
Niikawa, I. (1982): Early Carboniferous rugose
corals from the upper Hikoroichi and thelower Onimaru Formations in the southern
Kitakami Mountains. Abst. 89th Ann. Mtg.
Geol. Soc. Japan, p. 245 (in Japanese).
Okubo, M. (1951a): Trilobites from Japan.
Earth Science (Chikyu Kagaku), no. 4, p.
25-31, pI. 1 (in Japanese and English) ..
--(1951b): Zur Hikoroichi-8erie und derbedeutenden Diskordanz vor der Hikoroichi-Epoche. J. Geol. Soc. Japan, vol. 57,
no. 669, p. 195-209 (in Japanese).
Onuki, Y. (1956): Geology of the Kitakami
Massif. in Iwate Prefecture (ed.): Explana--

tory text of geologic map (scale 1 :100,000)
of Iwate Prefecture, 2, 189 p., Sasaki Printing Co., Ltd., Sendai (in Japanese).
--(1969): Geology of the Kitakami Massif,
northeast Japan. Tohoku Uniu., lnst. Geol.
Pal., Contr., no. 69, p. 1-239, pIs. 1-4(in Japanese).
Paeckelmann, W. (1931): Die Brachiopoden desdeutschen Unterkarbons, 2 Teil: Die Productinae und Productus-iihnlichen Chonetinae.
Abh. Preul1. Geol. Landesanst., N. F., Ht.
136, p. 1-440, pIs. 1-41.
Phillips, J. (1836): Illustrations of the geology
of Yorkshire, Pt. 2. The Mountain Limestone district. 253 p., 25 pIs., John Murray,
London.
Pocock, Y. P. (1968): Carboniferous Schizophoriid brachiopods from western Europe.
Palaeontology, vol. 11, pt. 1, p. 64-93,
pI. 18.
Ramovs, A. (1969): Karavankininae, nova

775. Early Carboniferous Brachiopods
poddruzina Produktid (Brachiopoda) iz
Alpskih Zgornjekarbonskih in Permijskih
skladov. Jeseniski Zbornik Jeklo in Ljudje,
2 Del, p. 251-268, pIs. 1--3.
Roberts, J. (1975): Early Carboniferous brachiopod zones of eastern Australia. J. Geol.
Soc. Aust., vol. 22, pt. 1, p. 1-31.
Saito, Y. (1968): Geology of the younger Paleo·zoic System of the southern Kitakami
Massif, Iwate Prefecture, Japan. Sci. Rep.,
Tohoku Uniu., 2nd Ser., vol. 40, no. 2, p.
79-139, pIs. 18, 19.
Sakagami, S. (1962): Lower Carboniferous
Bryozoa from the Hikoroichi Series, Japan.

Trans. Proc. Palaeont. Soc. Japan, N.S.,
no. 46, p. 227-242, pIs. 35-37.
Sarytcheva, T.G. and Sokolskaja, A.N. (1952):
CapbI'IeBa, T. r. H COKOJlbCKaH, A. H.: Onpe){eJlliTeJlb naJle030HCKHX opaXHOnO){ nO){MOCKOBHOH KOTJlOBHHbI. Tp. nl1H, T. 38, p. 1-303,
pIs. 1-71.
Sugiyama, T. (1938): A new Lower Carboniferous Conularia from the Kitakami Mountainland. J. Geol. Soc. Japan, vol. 45, no.
541, p. 771-773.
--(1942): Studies on the Japanese Conularida.
Ibid., vol. 49, no. 589, p. 390-399, pI. 15.
--(1944): On Japanese trilobites. Study Rep.,

Geol. Min. Inst., Tokyo Bunrika Daigaku,
no. 1, p. 21-30, pI. 1 (in Japanese).
Tazawa, J. (1980): Visean brachiopods fromthe Karaumedate Formation, southern Kitakami Mountains. Trans. Proc. Palaeont.
Soc. Japan, N.S., no. 119, p. 359-370,
pIs. 41, 42.
--(1981): An Early Carboniferous brachiopod
fauna from the Karoyama Formation in the311

Kitakami Mountains, northeast Japan. Saito
Ho-on-Kai Mus. Res. Bull., no. 49, p. 6378, pI. 5.
- - , Itabashi, F. and Mori, K. (1981): Lower
Carboniferous System in the Nisawa district,southern Kitakami Mountains, Japan. Tohoku Uniu., Inst. Geol. Pal., Contr., no. 83,
p. 21-37, pIs. 1, 2 (in Japanese).
--and Katayama, T. (1979): Lower Carboniferous brachiopods from the Odaira Formation in the southern Kitakami Mountains.
Sci. Rep., Tohoku Uniu., 2nd Ser., vol. 49,
no. 2, p. 165-173, pI. 11.
Thomas, I. (1914): The British Carboniferous
Producti, 1. Genera Pustula and Ouertonia.

Mem. Geol. Suru.

Gt.

Brit.

(Palaeont.),

vol. 1, pt. 4, p. 197-366, pIs. 17-20.
Volgin, V.1. and Kushnar, L. V. (1975): BOJlrHH,
B.Y!. H KYIlIHapb, JI. B.: n03){HeBH3eHcKHe
opaXHOnO){bI H ){BycTBOp'laTbIe MOJlJlIOCKH
IO>KHOH <l>epraHbI. 112 p., 10 pIs., Y!3){-BO.
JIeHHHrpa){. YH-Ta., JIeHHHrpa){.
Winkler Prins, C. F. (1982):· Brachiopods andthe Lower/Middle Carboniferous (Mississippian/Pennsylvanian) boundary. in Ramsbottom, W. H. C., Sanders, W. B. and Owens,B. (eds.): Biostratigraphic data for a MidCarboniferous boundary, p. 61-68, lUGS
Publication, Leeds.
Yanagida, J. (1965): Carboniferous brachiopods
from Akiyoshi, southwest Japan, Part 2.
Mem. Fac. Sci.. Kyushu Uniu., Ser. D,
vol. 16, no. 2, p. 11:'1-142, pIs. 25-28.
Yanishevsky, M. (1918): 5!HHweBcKiH, M.: MaTepiaJlbI K"b H 3Y'IeHiIO HH>KHeKaMeHHoyroJlbHoH
ljlaYHbI cI>epraHbI. Tp. reo.tl. HOM., H. C., BbIJI
162, p. 1-145, pIs. 1-8.

Akiyoshi ~1\tf, Arisu 1if±, Higuchizawa M IJ iR, Hikami 7Jc..l::, Hikoroichi a1jfi{r(J, Karaumedate Jl!f~«f!, Karoyama :hn~lll, Kawauchi Jlifj, Kitakami Mountains ~t..l::Ill!t!l, Mt. Senokita-l! / ;~ 11I, Nagaiwa :lit!Ef, Nagasaka :lit:!Jii, Nakazato JfI!I!., Nisawa 7iliiR, Odaira *3JZ, Onimaru }tn, Onimarusawa }tniR, Ono *!f, Sakamotozawa :!Jii*iR, Setamai tltm*, Sumitacho tHBIDY, Yokota lI'lIm, Yonosawa '" - / iR
~1:..I::Ill!t!lO)E~r(J!I.t t)Hl!:l:lLt.:iitrWl:fi~~ (~-It-Wl) .Il1ilJE~: ifH!B~I:..I::Ill:!t!!, BI!I{r(J:!t!!1g1( (~'¥~**Wtr(JBI!I{r(JiBT) 1:::.7.}1ff-tr., Bljfi{iTI/lO)..I::$1I (..1::$ 105m) n'Q, ~Wl~-It- WlO).Il1il@~fl::fin~.i£:!:I:l Lt.:o ;: 0);: cit, B~r(JJln~..I::&O)..I::$ ~ -It -1IM'}tn!lI:::.~fiB91:::'linn r., !fjj.$~ c r.F1I-t r., 0 ; : O).Il1ilJE~fl::fi!IJ¥l.Jil'f't, (j(O):f!ll~1!;tr: Schizophoria re-supinata (Martin), Rhipidomella sp., Orthotetes sp., Pustula cf. P. Pllstlllosa (Phillips),
Karavankina sp .• Cleiothyridina sp., Spirijer sp., Choristites bisulcatus (Sowerby) ~.t rP Tomiopsis sp.
miRMi-

Jun-ichi TAZA WA

312

Explanation of Plate 61(Natural size unless otherwise indicated)
Figs. 1a-1c. Spirifer sp.
la, 1b, 1c. Ventral, dorsal and internal views of a specimen, with an almost decorticatedbrachial valve, IGPS colI. cat. no. 97908.
Figs. 2a, 2b. Karauankina sp.
Rubber casts of a brachial valve exterior and interior, IGPS colI. cat. no. 97905. Fig. 2b is

X 2.
Fig. 3. Cleiothyridina sp.
Rubber cast of a valve exterior, IGPS colI. cat. no. 97907.
Figs. 4a, 4b. Choristites bisulcatus (Sowerby)
4a. Ventral view of a partly decorticated pedicle valve, 4b. Rubber cast of a pedicle valve
exterior, IGPS colI. cat. no. 97909.
Figs. 5-7. Rhipidomella sp.
5. Rubber cast of a pedicle valve interior, IGPS colI. cat. no. 97900, 6, 7. Internal mouldsof two brachial valves: 6. IGPS colI. cat. no. 97902, 7. IGPS colI. cat. no. 97901.
Fig. 8. Pustula cf. P. pustulosa (Phillips)
External mould of a brachial valve, IGPS colI. cat. no. 97904.
Figs. 9a, 9b. Schizophoria resupinata (Martin)
Internal mould of a pedicle valve and the rubber cast, IGPS colI. cat. no. 97898.
Figs. lOa, lOb. Tomiopsis sp.
Internal mould of a pedicle valve and the rubber cast, IGPS colI. cat. no. 97910.
Figs. 11a, 11b. 'Orthotetes sp.
11a. Rubber cast of a brachial valve exterior, 11b. Internal mould of a brachial valve, IGPS
colI. cat. no. 97903.

TAZA WA: Early Carboniferous Brachiopods

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Plate 61Trans. Proc. Palaeont. Soc. Japan, N.S., No. 133, pp. 313-331, April 30, 1984

776. PALYNOLOGICAL INVESTIGATION OF THE POSTGLACIAL DEPOSITSIN LAGOON KAHOKU-GATA, KANAZAWA, CENTRAL JAPAN*
NORIO FUJI
Department of Earth Science, Faculty of Education, Kanazawa University, Kanazawa 920

Abstract.
The palaeovegetational and palaeoclimatic changes during thelast 20,000 years in and around Lagoon Kahoku-gata, Kanazawa, Central Japanare analysed from the viewpoint of pollen analysis. The palaeoclimatic change isinferred as follows:
The last 1,500 years (Pollen Subzone A-d): mild and wet (the last 500 years. . . . . mild as climate of the present-day, 500-1,500 years . . . . . moreor less warm);
1,500-5,000 years ago (Pollen Subzone A-c): cool and slightly dry (15003,500 years ..... cool or slightly cool);
5,000-8,000 years ago (Pollen Subzone A-b): warm and wet;
8,000-11,000 years ago (Pollen Subzone A-a): more or less cold and slightly
wet;
11,000-12,000 years ago (Pollen Subzone B-d): cool and slightly wet;
12,000-14,000 years ago (Pollen Subzone B-c): more or less cold and slightly
dry;
14,000-16,500 years ago (Pollen Subzone B-b): cold and slightly dry;
16,500-21,000 years ago (Pollen Subzone B-a): cold or slightly cold and dry.
The pollen zones from Lagoon Kahoku-gata may be correlated with the divisions in Northwestern Europe as follows:
Subzone A-d may be correlated with the Subatlantic, Subzone A-c with the
Sub boreal, Subzone A-b with the Atlantic, Subzone A-a with the Preboreal andthe late Younger Dryas, Subzone B-d with the early Younger Dryas - Alleri:id Older Dryas, Subzone B-c with Bolling - the late Oldest Dryas, Subzone B-b
with the early Oldest Dryas, and Subzone B-a with age before the Oldest Dryas
respectively.

selian Glacial Age in the Northwestern Europe,a large transgression confinned over the world
had begun_ This transgression has been internationally called the Flandrian Transgression,and it has been called Yurakucho Transgression
in the Japanese Islands, and also the later partof the transgression has been named theJomonian Transgression. Though an ancient
inlet called the Ko-kahoku-irie had existed during
the transgressional age, the inlet had beenchanged a lagoon by the fonnation of large

Introduction
After the last glaciation called the Wlinnian
Glacial Age in the Middle Europe, the Weich*Received March 31,1983; read Oct. 11, 1980,
at the 126th Meeting of the PalaeontologicalSociety of Japan at Toyama; and Aug. 7, 1982,
at the 11th International Union for Quaternary
Research at Moscow, USSR.
Contribution of the Department of Earth Science,
Kanazawa University; New Series No. 89.
313

NorioFUJI

314

coastal sand dunes in the small regression during
the stage of the middle Jomonian to the late
Yayoian Age, and the environment as a lagoon
has been kept since the Yayoian Age (Fuji,
1975; Fuji et al., 1981). Therefore, the present
writer infers that all of the deposits throughout
the latest Quaternary deposits called the Postglacial deposits have been distributed beneath
this lagoon. If this inference is correct and aboring will be drilled at the lagoon, all of thedeposits after the last glacial age may be collected. If the deposits are obtained, palaeovegetational and palaeoclimatic changes in andaround the lagoon during about 20,000 years
since the last glacial age may be ascertained.
The present writer has obtained many coresamples from the two drilled wells, about 15-m
and about 85-m borings, and these core samples
have been studied from the viewpoint of palynological investigation.
This article consists of three parts of descriptions of the stratigraphy of the Postglacial
period around and in Lagoon Kahoku-gata, thepalynological study on the last Quaternary
deposits, and the palaeovegetational and palaeoclimatic signif!cance during the last 20,000 years.
The present writer takes this opportunity to
express his deepest gratitude to the late Dr.
Naoto Kawai, former Professor of Osaka University, for his continuous encouragement andsupervision. Thanks are due to Assistant Professor Tadashi Nakajima of Fukui University,and Professor Kimio Hiro'oka of Toyama University for their advice on the palaeomagnetismof the present core samples. Finally, the writer
expresses his deep appreciation to the Ministryof Education of the Japanese Government for
grants from the Science Expenditure Funds
during the period 1977 to 1979, and also to theJapan Society for the Promotion of Science for
grants during the period 1978 to 1979.

which were formed during the middle andlate Holocene Epoch have been distributed in
front of the simple coastal region of the Japan
Sea. The alluvial lowland areas around thislagoon were formed during the period since
the Flandrian Transgression. This lagoon is
the second largest lagoon on the Japan Sea
side, and had been an old inlet called Ko-kahokuirie during the Flandrian Transgression age.
In the middle Holocene Epoch, the lagoon
was changed from a marine condition to abrackish condition. The change of palaeoenvironment as -mentioned above agrees chronologically with the relative small regression age.
The ancient inlet was isolated from the Japan
Sea by the formation of the coastal sand dunes
and by a lowering of sea-level during this regression age, and changed to a lagoon (Fuji, 1975;
Fuji et al., 1981; Fuji, 1982a; Fuji, 1982b).
The deposits beneath the Kanazawa Plain
including Lagoon Kahoku-gata are stratigraphically divided into two parts: the lower andthe upper parts. The lower part is composed
mainly of hard Neogene strata and loose Pleistocene deposits, and the upper one is composedof the postglacial deposits which are divided
into three subparts; the alternation of coarse
sand and mud layers in the lower horizon, aloose medium sand layer in the middle horizon,
and a mud layer in the upper horizon. A
gravel layer, about 5 m to 8 m thick and 50
mm to 100 mm in diameter of gravel, is intercalated between the lower and upper parts,and belongs to the last stage of the last glacialage.
The gravel layer is generally distributed justbelow the Postglacial deposits of the Holocene
alluvial plain developing along the coastal areaof the Japan Sea, and called the First Gravel
Layer in Japan, and a key bed indicating theboundary between the Postglacial and thelast glacial deposits.

1. Topography and Geology
Lagoon Kahoku-gata is located in the central
part of Ishikawa Prefecture, facing the Japan
Sea of Central Japan. The coastal sand dunes

2. Palynological Study2-1) Preparation for Pollen Analyses
Pollen grains in the sediments were con-

776. Palynology in Postglacial, Lagoon Kahoku-gatacentrated in the laboratory by slight modifications of the process described by Faegri andIversen (1964).
2-2) Microscopic Examination
Pollen grains and spores mounted on slides
were identified and counted by means of amechanical stage of a microscope. The counting was continued up to more than 300 identifiable arboreal pollen grains. Determination
was made with the aid of the key by Faegri
and Iversen (1964) and McAndrews (1973),
and also in reference to the pollen grains obtainable from the Japanese Islands. Hard-toidentify pollen grains were identified with theaid of a reference collection of about 500 slides
for important trees, shrubs, and acquatic herbsof the Japanese Islands in possession of theInstitute of Earth Science, Kanazawa University,a reference collection of about 9,000 slides
owned by the Limnological Research Center,
University of Minnesota, Minneapolis, U.S.A.,
and also a reference collection of about 5,000
slides owned by the Department of Quaternary
Geology, Faculty of Science, University of
Uppsala, Uppsala, Sweden.
2-3) Method for Interpretation of Palaeovegetation and Climatic History
The writer depends upon the pollen analyses
for the reconstruction of vegetation during a
glacial age. For the interpretation of the pollen
spectra obtained from the 200-m core samples,
he has employed two methods, namely, (1)pollen spectra of the modern samples collectedfrom Lagoon Kahoku-gata and its vicinity, andalso from various localities of some climatic
zones throughout the Japanese Islands and (2)the warmth index (month-degrees). The methods
are described in detail in the present writer's
previous paper (1978).
2-4) Pollen Analyses of the 15-m Core Samples(1) Location of the Boring and Samples
The boring site is situated in a reclaimed
land, about -50 cm in the present altitude,near Kurotsubune of Uchinada-machi.
The 15-m core samples are composed mainlyof homogeneous dark bluish grey clay. As
measured by Kigoshi of Gakushuin University,315

the 14C dating age of dark bluish grey clay inthe 13.60 - 13.70 m horizon of this 15-mcore is 3,220 ± 160 years B.P. (Gak-7146).
All of the core samples belong to the late
Holocene deposits according to the stratigraphyof this core and 14C dating.
(2) Zoning of Pollen Assemblage and Palaeoclimate based on Palaeovegetation
In order to facilitate their description anddiscussion, the pollen diagrams are divided intosome zones. These zones are based upon conspicuous changes in pollen percentages. Changes
in the ratio, Total AP/Total NAP, can be described, while alternation of values of one or
two pollen types may also lead to the establishment of pollen zones. Where pollen zones display the same nature characterized by assemblageof pollen grains and spores, the writer has attempted to indicate them under the same lettercode in order to facilitate comparison. These
pollen zones are restricted to the series of diagrams under discussion. The minor differencesof the pollen assemblage in the zones are shownby subzones.
The 15-m core samples are divided into threepollen zones as Zone ex, Zone ~, Zone 'Y in an
ascending order. They are described as follows:
Zone ex, spectra: 1-470 to 1-1500; depth:
4.7 to 15 m; age: -about 1,500 to 3,500
years ago.
This zone is characterized by a large amplitude
and a long duration of every maximum (up to
about 60%) or minimum (down to ca. 17%)
period in a fluctuation of pollen value of Cryptomeria. The percentage of arboreal pollen grains
shows the highest value throughout the 15-mboring core. Such plants as Abies, Picea, andTsuga growing in the Subpolar area reach only
1 to 6% in this zone. Plants adapted to the Cool
Temperate climatic zone appear 7 to 24% in thefluctuation of pollen percentage. Among them,
Fagus large-type which is inferred to be Fagus
crenata appears about 13% on the average (1%at a minimum and 23% at a maximum). Plants
growing in both climatic zones of the Cool
Temperate and the Temperate (Warmth-index:
55° to 140°) reach 45 to 72% in pollen value,

NorioFUJI

316

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NorioFUJI

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776. Palynology in Postglacial, Lagoon Kahoku-gatawhich is the highest percentage throughout
the 15-m core samples. Most of the highest value
is taken by Cryptomeria. Plants growing in the
middle part of the Cool Temperate zone andthe Warm Temperate zone (70° to 140°) havea pollen value of 12 to 37%, which is lower
than those of Pollen Zones {3 and 'Y. Plants ofboth climatic areas of the South Warm Temperate and Subtropical zones (Warmth-index:
100° to 180°) reach 8% at a maximum value,
which is lower than those of Pollen Zones{3 and 'Y. The pollen percentage of Fagus crenatatype shows a negative interrelation to that of
Cryptomeria.
On the basis of the above-mentioned description, the palaeoclimate during the sedimentation of the deposits of this zone may have been
the same as the climate in the present Cool
Temperate area.
Zone {3, spectra: 1-320 to 1-460; depth: 2.5
to 4.7 m; age: about 500 to 1,500 years
ago.
This zone is characterized by a large percentage of non-arboreal pollen grains, pollen value of
which is about 50%. Boreal conifers growing in
the Subpolar and/or Subalpine zones appear as
follows; Abies: 0 to 4%, Picea: 0 to 3%, Tsuga:
1 to 7%. Cool Temperate plants of this zone
show a value higher than that of Zone 'Y. Somechanges are recognized in the percentage ofpollen assemblages. Namely, plants adapted to
the Cool Temperate and Temperate zones record
a drastic decrease from 64% to 22% because ofa drastic decrease (from 49% to 12%) of Cryptomeria, especially remarkable at 4.6 m to 4.7 m
in depth. In contrast to the above-mentioned
phenomenon, plants of the middle area of theCool Temperate zone and the Warm Temperatezone increase gradually from 32% to 50% due toan increase (6% to 23%) of Pinus diploxylontype. Warm Temperate and Subtropical plants
show a pollen percentage (2% to 8%) which isthe same as that of Zone 'Y.
According to palaeovegetation mentioned
above, the palaeoclimate during the age ofZone {3 may have been more or less warm incomparison with the present climate.
Zone 'Y, spectra: 1-20 to 1-250; depth: 0 to319

2.5 m; age: the present-day to about 500
years ago.
In this zone, arboreal pollen grains occupy
about 43% to 63%, being higher than the value of
nonarboreal pollen grains. As Abies and Picea
pollen grains are respectively 2% to 12% and 3%
to 18%. Subpolar plants show the highest value(21% to 35%) over this zone. Plants growing in
the Cool Temperate zone have a low value, which
is 4% to 8% in the total percentage. On the other
hand plants growing in the Cool Temperate andWarm Temperate zones show the lowest value
throughout all of the zones. However, plants
growing in the middle area of the Cool Temperatezone and the Warm Temperate zone reach thehighest percentage over the boring core samples
due to an increase (25% to 49%) of Pinus diploxylon-type. Among them, Ilex pollen percentage shows a large amplitude, e.g., from 0% to35%. Warm Temperate and Subtropical plants
show a 3 to 7% value in this zone. The percentage of Oryza pollen grains records a drastic
increase.
Judging from the above-mentioned description, the palaeoclimate during this zone may
have been warm as the present climate.
Nakai, Mori and Ohta (1982) studied thestable carbon isotopic composition ratio (13C/
12C) of sedimentary organic materials in the 15-m
core. Judging from the isotopic and pollen analyses, the change of climate on the basis of thepollen analysis is a close agreement to the changeof the isotopic composition in a pattern ofchange.
The frequency of pollen grains of Oryza(rice plant) found in Zone 'Y shows a value larger
than those of Zones a and (3. This phenomenon
reveals the remarkable development of ricecultivation around Lagoon Kahoku-gata during
the time of Zone 'Y, and this inference is supported by many old documents and pieces ofarchaeological evidence.
2-5) Pollen Analyses of the 85-m Core Samples(1) Locality of the Boring and Samples
The 85-m boring site is situated in the bottomof Lagoon Kahoku-gata near Bridge Konanohashi, Tsubata, northwest Kanazawa, andabout -100 cm in the present altitude. Thes. ..,;
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776. Palynology in Postglacial, Lagoon Kahoku-gata

writer can divide the 85-m core samples into
seven parts. Fuji, the present writer, calls themLayers A to G in a descending order. They aredescribed as follows (Fuji, 1982b):
Layer A: This layer is distributed locally ina deltaic area near the mouths of the Tsubata,Morimoto and Asano Rivers flowing into Lagoon
Kahoku-gata. The layer is composed of loose
brown coarse-grained sand. It is about 2 - 5 m
thick.
Layer B: This is composed mainly of homogeneous loose dark bluish grey silt intercalatedwith thin (2 m thick) loose dark bluish greymud (about 18 to 20 m deep). This layer isabout 26 m thick (-2 to -28 m below thepresent sea-level).
Layer C: This is composed mainly of loose
dark yellowish brown silty sand and mediumgrained sand, and about 10 m thick (-28 to -37
m below the present sea-level).
Layer D: This is composed of alternation ofloose brown-colored sand and dark bluish grey
mud or silt, and about 25 m thick (-37 to -62
m below the present sea-level).
Layer E: This is composed of brown-coloredgravels, kinds of which are sandstone, homogeneous hard mudstone, hornblende andesite,and pyroxyne andesite, etc. The gravel is 5 to 10
cm in diameter. It is about 4 m thick, and -62
to -66 m in the present altitude.
Layer F: This layer is composed of alternation of dark bluish grey clayey silt and dark
bluish grey silty mud. This is about 16 m thick,and -66 to -82 m below the present sea-level.
Layer G: This layer is composed of brown
medium- and coarse-grained sand, and -82 to-85 m below the present sea-level.
Layer E to G belong to the latest Pleistocene
deposits according to stratigraphy and 14C datingon this core sample (Fuji, 1982a, 1982b).
(2) Zoning of Pollen Assemblage and Palaeoclimate based on Palaeovegetation
The 85-m core samples are divided into twopollen zones as Zones A and B, and eight pollen
subzones as Subzones A-d, A-c, ..... A-a, B-d,
B-c, ..... B-a in a descending order as described
below. The present palynological study of the321

85-m core samples has been made in order todiscover, in detail, changes of palaeovegetationand palaeoclimate during the sedimentation of
the 85-m core samples.
Zone A, spectra: 0.82 to 39.70; depth: 0 m
to 40 m; age: about 10,000 years ago to
the present-day.
Zone A is characterized by a dominant percentage of plants growing in the middle area of
the Cool Temperate and Warm Temperate zones,
and A-a, A-b, A-c, and A-d in an ascending order.
Subzone A-d, spectra: 0.82 to 4.95; depth:o m to 5 m; age: 1,500 years ago to thepresent.
Arboreal grains show up with a total pollen
value of 61% to 72%, which is higher than thepercentage of non-arboreal pollen grains. Boreal
conifers reach about 15% on the average (3%at a minimum and 24% at a maximum), whichis influenced by an increase of Abies, Picea,
and Larix. Plants growing in the Cool Temperate zone are 11% to 75%, which is influenced
by an increase of Cryptomeria. Plants growing
in the middle part of the Cool Temperate andthe Warm Temperate zones show a high percent,
11% to 62%. Among them, Pinus's and Cory Ius's
percentages are respectively 3 to 48% and 2 to
8%. Oryza pollen grains are found to be 8.1 to23%.
Judging from the above-mentioned pollen
assemblage, it is inferred that the palaeoclimate
since about 1,500 years ago may have been
mild and wet.
Subzone A-c, spectra: 5.75 to 17.70; depth:
5 m to 19 m; age: 1,500 to 5,000 years
ago.
Arboreal pollen grains have a large percentage,
65% to 88%, which is the highest one throughout
the 85-m core samples under the influence ofan increase of Abies (about 3%) and Picea (1.5
to 8%). Plants adapted to the Cool Temperate
and Temperate zones show 14% to 45% due toan increase of Cryptomeria pollen grains, though
Zelkova pollen grains decrease from about 16%
to 1%. Plants of the middle Cool Temperate
and the Warm Temperate zones reach 30% to70%. Plants growing in the Warm Temperate

Norio FUJI

322_::J:jl!*!:!:!:;%JibMA_·"ufl:!!:!!s~ ·.·.··...t.a:!:!:!:i*:~~:!_;i:i:!:!*!:m*m:!:!:!:!~1I

8iii I i;aj ~iIIi i:II::S

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g

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.. II .;I:!I::IIiI!ll)t :ftllDClt_ ~15~tII:ttsl:S:!i!I.

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Stratigraphy
Depth in meter

Iill II

Spectrum nas

80/IIII;) !las"\:: doting aestimoted datesiiPollen Zaring-I-If---~~~~

I-----~--.---::;>""""~~-__.:_r_~]-It---T--<:::~~~-.---+-..
-1 t----~-__.__------.-r--.--r___+....
Jr----==v---====-~-=~~~

l:l~~~.J_Jr---------~------~~~~--~------~-k.31--_____,..---__~_...:...-__----k
83_ll----------=~~~---n.....

._~r----:~~::::----r~r----~1:l~

L-____________________________________

Text-fig. 5.

~L_~

__

~L-

____________~

Diagram of conifer and arboreal pollen grains found from the 85-m core samples.

776. Palynology in Postglacial, Lagoon Kahoku-gata

323

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Text-fig. 6.

Diagram of arboreal pollen grains found from the 85-m core samples.

and the Subtropical zones are 1% to 9%, which
is a decrease as compared to Subzone A-b.
Oryza pollen grains are found in an upper horizon from this subzone, and the percentage ofthese grains is 0.5% to 10.2%.
On the basis of the result mentioned above,
the palaeoclimate is inferred to have been cooler
than those of the present-day, Subzones A-dand A-b.

Subzone A-b, spectra: 19.25 to 33.45; depth:
19 m to 34 m; age: 5,000 to 8,000 years
ago.
Arboreal pollen grains have a value of 39%
to 73%, lower than those of the other subzones. Therefore, non-arboreal pollen grains
increase. Such boreal conifers as Abies Picea
Tsuga, and Larix decrease to 0% or 2.5%, andNorioFUJI

324

I

!o

I

8

Cj

I Depth in meter

I

o

IS

Pollen Zoring~l-3r---~--..:::::>~::::::::::::==:::-:;"----v----'-~_J~________~____________~____________~~~____________________________________~~_J~:l~====~:=;:;;::;;~~~~,______ ______-3~~~-=~~~~~~-Jr-------------~~~----~~~~--~~~~~~~~-3 t----------....1.o::::=-----..---:----k-~:~r------~~-.::--~-31--------->-'-----...l..L------.....--"..--..-....,...._.+....

-3F~~~~~~~~~-3~--~--~--~~~~==~~----~_J.J_J~~====~~~~~~~.~r----~~~--::::::=""'\~~~~~~_J~=======~==~~~=~~~::::::::~_J_J ~~:;:::::;;;;;::;====:::::;;:~;;;;:::::::::;:::::::;;:~~~~~

Jt--~___~~=_~=_~~~~~~,~~~=-----.,.,,~---I-..

-3t---~==___<'~___"..,.........,~-..........~=--_ _~_k.~

1
.J~~~~~~.~_J.~ )----~~=----~=-~~~-=-::::>...............

·31---::::;;::;::::::=::==-==:r~~~===~==---t--3-31-----"""=""'""------.::-",...---....,,-~-~~~~-3r----=-;:::::::;:;:'=::::::::::=--7'\""""::--::::=::::::;:;:;;:;::::;::::;:::;::::::~*•31------...-.".-_......-----.::~_~-=--::::>~.~ L-______ ______________~

Text-fig. 7.

~

L-_____________L_____L~~__________~

Diagram of non-arboreal pollen grains and spores found from the 85-m core samples.

776. Palynology in Postglacial, Lagoon Kahoku-gata

the percentages of their conifers show thelowest value throughout all of the eight subzones. Cool Temperate plants decrease. Plants
growing in the Cool Temperate and the Warm
Temperate zones show such a high percentage
as 28% to 55% because of an increase of Zelkova(9% to 20%), Lepidobalanus (8% to 28%), andCryptomeria (4% to 20%). Middle Cool Temperate and Warm Temperate plants reach a highvalue (36% to 58%) of pollen grains due to anincrease of Cory Ius (12%). Plants adapting to theWarm Temperate and Subtropical zones havethe highest percentage throughout all of theeight subzones.
Judging from the above-mentioned palynological results, the palaeoclimate during theage of this subzone may have been the warmest
over the 85-m core samples.
Subzone A-a, spectra: 34.75 to 39.70; depth:
34 m to 41 m; age: 8,000 to 11,000 years
ago.
Arboreal pollen grains show a high percentage
of 71% to 87%, and non-arboreal pollen grains
have a low percentage. Plants growing in the
Subpolar zone reach to a value of about 4.6%
at a maximUl:n, which is low. Cool Temperate
plants decrease from 11% to 3%. This phenomenon is influenced by a decrease (from 10% to0%) of Fagus. In contrast to this decrease, plantsof the Cool Temperate and the Warm Temperatezones increase from 32% of the Subzone B-d to
72% of this Subzone A-a. This increase is influenced by an increase of Zelkova (1% to 24%) and
Lepidobalanus (25% on the average). Warm
Temperate and Subtropical plants reach 1%
to 7%.
Judging from the above-mentioned pollen
assemblage, it is inferred that the palaeoclimate
during the Subzone A-a may have been more orless cold.
Subzone B-d, spectra: 42.77 to 44.30; depth:
41 m to 46 m; age: 11,000 to 12,000 years
ago.
Arboreal pollen grains are 51% to 62%, andoccupy a value more than that of non-arboreal
pollen grains. Plants growing in the Subpolarzone are few. Am~ng them, Abies, Tsuga, and325

Larix pollen grains are lacking, and only 6% of
Picea grains are included. Cool Temperate

plants show a high percentage (15% to 38%);
that is, Betula grains reach 1.8% to 2.7%, Ulmus
1.2% to 2.7%, and Fagus 10% to 35%. Plantsof the Cool Temperate and Warm Temperatezones increase gradually in contrast to thelower horizon as Subzone B-c. Plants growing
in the middle part of the Cool Temperate andWarm Temperate zones are 33% to 40%. The
Warm Temperate and Subtropical plants increase
from a lower subzone to this subzone; that is,
Myrica pollen grains are 0.6% on the average,
and Cyclobalanopsis grains 0.6% to 1.5%.
As mentioned above, this subzone is characterized by the abundance of plants growing
in the Cool Temperate zone, and the middle
area of the Cool Temperate and the Warm
Temperate zones. Also, Warm Temperate andSubtropical plants increase gradually from thelower horizon of this subzone.
The palaeoclimate during the age of thesedimentation of deposits of Subzone B-d
had been a cool condition.
Subzone Is-c, spectra: 46.74 to 53.70; depth:
46 m to 54 m; age: 12,000 to 14,000 years
ago.
Arboreal pollen grains show a high percentage(74% to 90%) throughout the 85-m core samples,and in contrast, non-arboreal pollen grains arevery rare. Subpolar plants increase to about
10% on the average. Plants growing in the Cool
Temperate and Warm Temperate zones increase
to about 25% on the average (12% at a minimum
and 39% at a maximum) owing to an increase(31% to 44%) of Lepidobalanus. Middle Cool
Temperate and Warm Temperate plants decrease
from about 62% on the average (77% at a maximum) of Subzone B-b to about 40% of thissubzone. This decrease results from a decreaseof Alnus pollen grains from 67% in lower Subzone B-b to 22% in this subzone. Warm Temperate and Subtropical plants increase, though
the increase is a small percentage.
The palaeoclimate at the time of this Subzone
B-c may have been a more or less cold condition.
"ubzone B-b, spectra: 55.38 to 67.80; depth:

NorioFUJI

326

This subzone is characterized by the abundance of conifers, and by the absence of Subtropical and Warm Temperate plants. Cool
Temperate plants appear about 5% on the
average (11% at a maximum). Plants growing
in the Cool Temperate and Warm Temperatezones show the lowest percentage throughout
all of the eight subzones by the influence ofthe low values of Cryptomeria and Zelkova.
Plants of the middle part of the Cool Temperateand Warm Temperate zones reach 46% (at aminimum) to 85% (at a maximum), which arehigher than those of the other subzone in the
85·m core samples.
Judging from the above-mentioned descrip·
tion, the palaeoclimate of Subzone B-a is inferredas having been cold or slightly cold.

54 m to 68.2 m; age: 14,000 to 16,500
years age.
This subzone is characterized by the abundance of conifers, and by the absence of Subtropical and Warm Temperate plants. Accord·
ingly, Subpolar plants are about 70% on the
average, which is influenced by a high value ofAbies (12% to 18%) and Picea (5% to 20%).
Cool Temperate plants appear about 4% on the
average (1% at a minimum and 7% at a maxi·mum) except Alnus. Cool Temperate and Warm
Temperate plants change from 10% to 30% in
Subzone B·b. The percentage of plants growing
in the middle area of the Cool Temperate andWarm Temperate zones shows a high value(46% to 77%), which is influenced by Alnus
pollen grains (20% to 47%).
The palaeoclimate in the stage of Subzone
B-b may have been a cold condition.
Subzone B·a, spectra: 69.20 to 79.25; depth:
68.2 m to 79.25 m; age: 16,500 to 21,000
years ago.
j!
,'!

I~

&
e

!

e

=
~

~

iii

~

jj

G

c

0-

3. The Comparison between the Climatic
Changes by the Isotopic andPalynological Studies

~

~
.u

-----

J i , i i.:o' , I lOA' J,

Text-fig. 8.

ji+Alnll.

i ~ I I i ~.b i i i

e!o i , i !J'.b i i i ~ I i j ~ I~ I i i ~ i i i :0: .:, i i i 4t I I i '.J':' I , i ~ i i i i~.t.

Summary diagram of the palynological analysis of the 85-m core samples.

776. Palynology in Postglacial, Lagoon Kahoku-gata

The comparison between the profiles forenvironmental changes by the isotopic andgeochemical studies and the fossil pollen anddiatom analyses gave a close agreement toeach other (Nakai et al., 1982). According to
the studies, it is concluded that the isotopic
and chemical records of embayment sediments
can be used as useful indicators for the pastenvironment.
To study the environmental changes such as
the climatic and sea-level fluctuation in thepast geologic time, the 15-m and 85-m coresamples were analyzed by N. Nakai for the stablecarbon isotopic composition ratio (13C/ 12C) of
sedimentary organic materials. Total organic materials in the cores have a {j 13C-range from -29 to-23 0100 relative to PDB-standard. Large rangesof (j 13C values are due to the past depositional
history affected primarily by. the relative contribution of terrestrial- and marine-derived
Verticalmatters
-

23

-

24

-

25

variation of
from Logoon

327

organic materials to the bottom sediments.
Besides a difference in the source of organic
materials, {j 13C value is affected by the sedimentary environment and temperature conditions. From the fluctuation pattern of {j 13C,
the present writer can find the following feature
indicating the sea-level and the climatic (temperature) changes during the end of the lastglacial age, Wiirmian or Wisconsinian glacial age,and the Holocene. A cold climate can apparently
be seen at the lower horizon of the core in the
14C_age of 9,000 to 14,000 years B.P. According
to the investigation based on diatom analysis(Fuji et al., 1981), a sea-level at that time wasabout -50 to -5 m in the studied area. Afterthat period, the sea-level rose gradually, andthe high sea-level and climatic optimum appearedin the 14C_age of 8,000 to 4,000 years B.P. corresponding to "the Jomonian Transgression".
This warm and high sea-level period is followed
f,13 C values of organic
Kahoku - gata Core BP- 22(N. NAKAI)

.

~

u
0

c

~

0

- 26

';;
u
r<)

""

Deplh 1m)

-

27

-

28

-29 0

10

20

30

40

50

60

70

80

2.630

5,260

7,890

10.52013,15015,78018,41021,00014 C - oge( years B.P.)

Pal yno log I co I
climateIFuJI)

Present

I

mild

I

cool

worm

I morelessor
Imore
less or I cool
cold

cold

I

cold

I

more or lesscold

I

Text-fig. 9. Vertical variation of {j 13C values of organic matters found from the 85-m coresamples (after Nakai, Mori and Ohta, 1982).

NorioFUJI

328

above-mentioned gives a close agreement to theclimatic change based on the palynologicalstudy as shown in Text-fig. 9.

by a low sea-level and a cool climate corresponding to a small scale regression called "the Yayoian
Regression" in Japan and correlated internationally with "a little ice age". After the small
scale regression, about 1,500 years B.P., thesea-level rose again gradually toward the present
sea-level.
The climatic change by the isotopic analysis
pollenzo ning

4. The Comparison between Changes of
the Palaeoclimate and Palaeomagnetism
The palaeomagnetic study of the 85-m coreBA

cl i male mild

a

c

b

cool

warm

d

d

c

more ormore or
less
cool
less
cold
cold

b

a

cold

more or
less
cold

.-

:;

...

80

m

10·'

-.
:>.
I II

c:::

c:::

10-5

E

-..
III

c:::

a>

c

..

E

..;

0

oS!

;;

c

a.

Ii
!l
0

soo
c:::

-

30"

u

o·

0

"

c

c:::

c:::

liS
-30·

-SOO

10
2I3D

5HO

8.P,

7'"

8.P.

I052G

SO

50

40

30
B.P.

B. p.

131SO

B. P.

15710

70
B.P.

11410

80 m
B.P.

21OCO

B.P.

Year

Text-fig. 10. Diagram showing the changes of the palaeomagnetism and the palaeoclimatebased on the palynological anlysis of the 85-m core samples (after Kawai & Nakajima, unpubl.
data).

776. Palynology in Postglacial, Lagoon Kahoku-gatasamples has been made by the late Dr. Naoto
Kawai, former Professor of Osaka University
and Assistant Professor Tadashi Nakajima of
Fukui University. The result of the palaeomagnetism on the 85-m core is shown in Text-fig.
10. Judging from the results of the palaeomagnetic and palynological studies, it seems to
be concluded that when the intensity of themagnetism was weak, the climate was a cold
condition, and in contrast, when the intensity
was strong, the climate was a warm or mild condition. The relationship between the palaeomagnetism and plaeoclimate as above-mentioned
has been found in the long core samples obtained from the bottom of Lake Biwa, Central
Japan (Kawai etal., 1975).
5. Correlation
In Northwestern Europe, the Late Glacial
Period is divided into five stages on the basisof changes of palaeoclimate, namely, the Oldest
Dryas (12,400 to 15,000 years ago), Bolling(12,100 to 12,400 years ago), Older Dryas(11,800 to 12,100 years ago), Allerod (11,000
to 11,800 years ago), and Younger Dryas(10,350 to 11,000 years ago).
As a detailed dating on the deposits from
Lagoon Kahoku-gata has not been measured,
the writers cannot correctly state the age ofthe boundary between some pollen subzones
and pollen zones. However, judging from thechanges of palaeoclimate based on the palynology and 14C dating and palaeomagnetic
stratigraphy of a few horizons, the ages ofsome pollen subzones are estimated roughly
as mentioned already in the description ofindividual pollen zones.
According to the writer's investigation on
the deposits obtained from Lagoon Kahokugata, Pollen Subzone A-a (about 8,000 to 11,000
years ago, more or less cold) may be correlatedwith the Preboreal and the Late Younger Dryas
stage; Pollen Subzone B-d (about 11,000 to
12,000 years ago, cool) with the early Younger
Dryas - Allerod - Older Dryas stages; Pollen
Subzone B-c (about 12,000 to 14,000 years

329

ago, more or less cold) with Bolling - the lateOldest Dryas; and Pollen Subzone B-b (about
14,000 to 16,500 years ago, cold) with theearly Oldest Dryas and the previous age, respectively.
In addition, Pollen Subzone A-b (about
5,000 to 8,000 years ago, warm) may be correlated with the Atlantic stage; Pollen Subzone
A-c (about 5,000 to 1,500 years ago, cooler thanthat of the present-day) with the Subboreal;and Pollen Subzone A-d (the present-day toabout 1,500 years ago, mild and wet) with theSubatlantic stage, respectively.
6. Conclusion(1) The palaeovegetation and palaeoclimate
during the last about 20,000 years in and around
Lagoon Kahoku-gata are analysed by a palynological investigation.
(2) Judging from the pollen analyses, the palaeoclimate may be inferred as follows:
Subzone B-a: 16,500 - 21,000 years ago;
cold or slightly cold, dry;
Subzone B-b: 14,000 - 16,500 years ago;
cold and slightly dry;
Subzone B-c: 12,000 - 14,000 years ago;
more or less cold, slightly dry;
Subzone B-d: 11,000 - 12,000 year ago;cool, slightly wet;
Subzone A-a: 8,000 - 11,000 years ago;
more or less cold, slightly wet;
8,000 years ago;
Subzone A-b: 5,000
warm and wet;
Subzone A-c: 1,500
5,000 years ago;cool and slightly dry;
Subzone A-d: the present-day - 1,500 years
ago; mild and wet.
(3) Judging from the palynological investigation of the samples obtained from the 15-mboring core of Lagoon Kahoku-gata, the deposits
below this lagoon are divided into three pollen
zones as Zones a, (3 and 1 in an ascending order.
Zone a: 1,500 - 3,500 years ago; cool orslightly cool.
Zone (3: 500 - 1,500 years ago; more or lesswarm.
Zone 1: the present-day - 500 years ago;

NorioFUJI

330

mild as the present-day.
(4) A change of the Carbon-13 (13C) and
Carbon-12 ct 2 C) ratio is shown in Text-fig. 9.
The pattern of the change of 813C corresponds topattern of the change of 8 13 C corresponds tothe pattern of the change of palaeoclimate.
Especially, the boundary between Zones 0: and~ is sharper than the boundary between Zones~ and 'Y.
(5) The frequency of pollen grains of Oryza(rice plant) found in Zones ~ and 'Y is larger thanthe value in the Zone 0:. This phenomenon shows
the remarkable development of rice-cultivation
around Lagoon Kahoku-gata during the age ofZones ~ and 'Y, and this inference is supported
by many old documents and pieces of archaeological evidence.
(6) The pollen zones of the core samples below
Lagoon Kahoku-gata are correlated with thedivisions in Northwestern Europe as follows:
Subzone A-d may be correlated with the Subatlantic stage, Subzone A-c with Subboreal,
Subzone A-b with Atlantic, Subzone A-a with
Preboreal and the late Younger Dryas, Subzone
B-d with the early Younger Dryas - AllerOd Older Dryas, Subzone B-c with Bolling - the lateOldest Dryas, Subzone B-b with the early Oldest
Dryas and its previous age, and Subzone B-a withtimes before the Oldest Dryas, respectively.

References
Faegri, K. and Iversen, T. (1964): Textbook ofPollen Analysis. Copenhagen, Munksgaarb.,
237pp.
Fuji, N. (1975): The coastal sand dunes of
Hokuriku district, Central Japan. QUlJternaryRes., vol. 14, p. 195-220.

--(1982a): Chronostratigraphic subdivision of
the Postglacial deposits in the JapaneseIslands. Striae, vol. 16, p. 24-35.
--(1982b): Paleolimnological study of Lagoon
Kahoku-gata, Central Japan. Abstract of thell-INQUA Congress (Moscow), vol. 1, p. 97.
--and Kobayashi, R. (1978): Palynologicalinvestigation of the Holocene deposits from
Lagoon Kahoku-gata, Central Japan. Bull.
Japan Sea Res. Inst. Kanazawa Univ., vol.
10, p. 29-51.
--and Miyamatsu, M. (1981): Fossil diatom
assemblage of the latest Quaternary deposits from Lagoon Kahoku-gata, Kanazawa,
Central Japan. Bull. Fac. Educ., Kanazawa
Univ., Natural Sci., vol. 30, p. 83-96.
Kawai, N., Yaskawa, K., Nakajima, T., Torii, M.
and Hatsuhara, N. (1975): Voice of geomagnetism from Lake Biwa. In Paleolimnology of Lake Biwa and the Japanese
Pleistocene, vol. 3, p. 143-160.
McAndrews, K. (1973): Pollen analysis of thesediments of the Great Lakes of North
America. In the 3rd. Internat. Palynological
Conferences, "Palynology Holocene andMarine Palynology (ed. N. A. Khotinsky)",
Moscow, Nauka, p. 76-80.
Nakai, N., Ohta, T., Fujisawa, H. and Yoshida,M.
(1982): Paleoclimatic and sea-level changes
deduced from organic carbon isotope
ratios, CIN ratios and Pyrite contents ofcored sediments from Nagoya Harbor,
Japan. Quaternary Res., vol. 21, p. 169177.
Nakai, N., Mori, S. and Ohta, T. (1982): Climaticand sea-level changes deduced from 6 13C
and CIN of sedimentary organic mattersand Pyrite contents of sediment columns
from brackish basins for the past 20000
years. Fifth Intemat. Conf. Geochronol.
Cosmochronol., Isotope Geol. (Abst.), 2612.62.

Kohoku-gata fPJ~t¥~. Kanazawa ~lR. Jomonian Age tlXllifft. Yayoian Age 5IJ;1:.lIifft, Kokahoku-irie iifuJ~tAiI. Konan-ohashi iMm*1i!il, Tsubata J'iIl:_, Asano River mmrJl/, Lake
Biwa fIl:r;!rNI, Yurakucho Transgression 1i~lBJij;1i776. Palynology in Postglacial, Lagoon Kahoku-gata
fjg!1:~I~H~iJm'9j'nJ~t~~riU;!:, ;&1$: 2 7J#<:¥r"j'9, ~ 'nl1> Q 1f~ll!Jiia~ic.J: ') -e%nJI; ~ht.:ftF1l~iJ:JmkdtL.-e:lt1lL.-e\"Qo ;f-- D:/ .;fic.J:')-e~i?ht.:;:''9.l1l!~'k1E~7.t;frj-L., ~~R'9~.~'k.~L.~M*, ~K~~Q.J:5~M~'k~~o(1) ;&1*p.:J 2 7J:¥r"j'9~3(tff§.'f'9~{t,!: ~t~Jtg~'9fE~7.t*'!: '9:%j.lt:@:.llI 1,500 :¥r"j m~lJli:* A·d)··· ·tlit'fO-e~iIl\l, Subatlantic JtIlic:%jlt
1,500-5.000 :¥lltr (.ft~lJli:* A·c)··· .~iJj(-e-'f'~iliZ::IlIk, Subboreal JtJHc:%jJt
5,000-8,000 :¥lltr UE~lJli:* A·b)··· ·tlitl!l~iIl\l, Atlantic JtIl~c:%j.lt

8;000-11,000 if:lltrUE~lJli:* A·a)··· '~-'f'*~ -C*'~ ~i!lll, Preboreal- Younger
Dryas 1&Wllc:%j J:t
11,000-12,000 if:1ltr UE~lJli:* B·d)··· ·1tW-*,*,~iIl\l; Younger Dryas 1ltrWl-Older
Dryas Wlic)<'Ht
12,000-14,000 :¥lltr (re-~lJli:* B·c)··· '-'f'*'*t-t; -'f'*' iliZ::IlIk; Bolling-Oldest Dryas
f&WlIC:%j .It
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332

PROCEEDINGS OF THE P ALAEONTOLOG !CAL
SOCIETY OF J AP AN

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. . . . . . . . . . . . . . .. ~ ~. 1JQ~ ~. ~ JII ~m10@]1E~:tiER*it;~ (9)j 1 S -9 )j 26 S, '"7
F Y ." F) ...... ~~R~· HliRfJll-· :t<J¥~T

Revision of two Vascoceratid Ammonites fromthe Upper Cretaceous of Nigeria _.H. Hirano

Symposium on Cretaceous Stage Boundaries~,!il;~MYilIi~:It!lO)B!II!*,cY/~T-1 ~(lO)j18S-10)j21S, ::z,,/,,-,//) ....
........................ t~*J¥fl~· 11!f5l-iti
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1Jj~ ·1t1JQT!1 ~ .::. ." !1 7. c~W)lUI; .. J:Hl~m.YYYO)"iS~.~c5ms*0)«.~~k"iS~.~~O){JlUiIDl;, 0-............ m:~~jl{$

YYYO)JRI!fJ;![!fi~c"iS~m .......... ~Hl~±
7 ; ( Y T~0)"iS1=.~~J:!IlI;'0~t::..Y Y yO)-;Iv - ~ T!1 ~ .::. ." !lim{t ........... .INR~~=~IUc': Vf£a~J:!IlIK .................. ltZJ:li~-It/ ::z-{t:tiO)7t1ii 1;'07;.t::. .!II!<P. "iS1=.~1=.¥J~J:!Il .............................. 1JQ~ ~.YYYo)"'t.-J..*lWHJElI1¥J1K ........ <PttfJt:=
Y / ~ T -( ~ 1;, 0 J! t::."iS1=.¥J~J:!Il ........... .
. " ........... ltZ.~i'fj· ftili ~. t~*J¥fl~
S*N.VlfflLi.!10)=1'!I:$C=tlcJl. .......... Hltt ~Y 7*,cO)=tlcfl.-t!fI:' Wallace Mlc Pacificar,,~~I:'~.il L -C _. _ .............. " .)!)~: j;I}
JlJr"'lt:lt!lmI1=.lI1¥J~ .... -....... 'J':i*A - (~Wi:)=>.

An early Cretaceous Chondrophorine (Medusoid Hydrozoa) .. Y. Kanie and G. D. Stanley~t$itiJ:$B!II!*~JJr~~~9-1 1:':};;Vf 7.> Y / ~ T-1 ~O)f!f:ffcj£~(I) ................ 1lfjHl~.Il!
....... .
. ............. Hl~~Z· JII~7i'l!- • t~Hl~i'fj

Some Ammonites from the Campanian (Upper
Cretaceous) of Northern Hokkaido, Part I,
Upper Campanian Ammonites from theTeshio Mountains ............ T. Matsumoto
Ditto, Part II, Some Campanian Ammonites
from the Soya area ..................... .
............ T. Matsumoto and T. Miyauchi
Ditto, Part ill, Summary of results ....... .
............................ T. Matsumoto
Taphonomy of the half and compressed ammonites from the Lower Jurassic Nishinakayama Formation in West Japan .. K. Tanabe,
A. Inazumi, K. Tamahara and T. Katsuta
Early shell morphology and development insome Mesozoic Ammonoidea ............. .
................ K. Tanabe and Y_ Ohtsuka
Cretaceous Corbulidae from Japan, Part 1,
Pulsides ......................... .T. Kozai~t$iti*;I?-/T-1J11!1j£ Apiolrigonia (Apiolrigonia) hetonaiana Tashiro f:'0~\-C .. t~!:8~T~,!il;Yf<MJilIi~~O) B!II!*=tlcfl.

............. .
. ............. Hl~~Z· JAitIi~Z· JIIn1¥'l!-;f1J.w~~~.*m*O)u*~JI1!I"~~j£lliLk
ilik{:UI;¥J.1{t:ti~c-t:-O)~:~ .. <p1R~=. };j}fl!I ilMi
~Wl=:I:*,c=tlcR Manolis 0)j£~1:'0~\-C ....

. . . . . . . . . . . . . . . . . . . . -. . . . . . . . -. . .. 'tCiii ji(f JI3~t$itiii'ilJj:lt!l~ 1:':};;Vf 7.> <P~~"ffl!l,*"fll1¥!.iM

333Q)~~fH;llnlt:to.J: Lf~~m~.......... ~!I!f;fll!¥:

Ontogenies of three peculiar Glossaulax
species (Gastropoda, Naticidae) from theLate Cenozoic strata in Southwest japan ..
................................ R. Majima
Morphological comparison of Vicarya verneuili d' Archiac, V. callosa Jenkins, and V.
callosa japonica Yabe and Hatai .. S. Kanno
mi!lillm.lllrH"[9*i!€Q) Paphia (Neotapes) undulata ft1:iOOf*~ffi ..................... .

.............. ""fJlJIE-· JJj( ~~. tl~'*9'J
9='tfii!tJlIHiJfi~i!€=1:l!:ffil9=' .J: I) iiIIr9 /~ l' - ,/Q)
~J!-}3 Q)f?tEIDEtm................ *ffP.~)(

Pleistocene Ostracoda from Atsumi, Central
japan (71fD ...... M. Yajima and H. Honda? p 7'; ';/;f.M "=]![~" Q)~rl3'm1f,fi t:~5J'ft ..

· . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .. ilIlJ 1.fz
~BitJlll,9='tfik1Eii~fE~i!€ ~ r 7'Mft1:i........
· ..................... ~i1!!7¥)(. =Mr1ih_fa-~!l!fJlll,m~~mmffi*tt~~JlJ#Jl[Q)~~*.J:I) S]![*B1&Iti$.ftEQ)~Je. ............... .
........... '" :fl;1fEJI1j:'j3 • W~Iirt:!ll!: • ~~~~
~JRJlJ:ItB[97]-r*/J'ifiJ~~~.J: I) i!€-t7.> ~JtlJs]![*'B1&Iit$. ft1:i (7¥ID ................... .
............ fjI--9-B3*-C~. :f~B3J11j~ • ~Ml/I~lN
WJ*w<*lii(mifgrl3'JII:ItB~Q) ~M=~UB ~ / r '/r t;::,,,?\,,'L ........................ 7k!l!fk1t:ti
JIOjrlll\""f:5#-m~Q)=~ • =~*Q)JfiJI: t: ft1:i~ ..................... . /NR!W1: • IJ'**)(~!fi#-m~Q)J:llB=~*i!€;ff.fL$.ft1:i~ ....... .
........................ IJ'**)(~. 'NR~1:
ilJX:Jjl.t'P<1:iJlJ1:iER!fiQ)J:fffI=~*Q) $t:i~$. t;::,,,?\,,'L ........................ ~Ml/I~~ • *""ftIiIJ~ 7" 1l' 7- ~ T ..f -/ "- ~ p ' / i:::'" 7 ~+Ii!€Q) v ~o r ~7"~$t:i~$.t;::,,,?\,,'L ..................... .
.............. ~/i~~. )j,!liIlffi;f: • E#-jij!fJ\tfE)j](!fi~ Millerella *oJt'/ :iftEt;::,,,?\,,'L.................................. ~)II:litifg

Sanbongicola (Annelida) and its burrow fromthe Pliocene Shimizu Formation, Kanagawa
Prefecture .............. !l!ffE~1'f) • fjI-/i ,~Archaeozostera I;::,"?\,''L ................... .
· ................. mJII~-Il~. A. Seilacher

Notes on a new genus of Heterocorallia fromthe Akisoshi Limestone, Southwest japan.............................. T. Sugiyama
mllB~tJ:JlJj1l! I3ljf{m~Q) Gigantoproductus ~*~~~~;f.-~'/~~7Q)~7T~?Am~

Silurian cephalopods from Yokokurayama,
Kochi Prefecture, japan ...... T. Kobayashi
E ~*B 7 '/ ~ /.-[ r-' Faqirngoceras I;::'''?\'' 'L ..

t;::,.J: 7.> 1:JIHt1:i ...... ll§Mb= - • 9='i!tii~,*Il~........ fjl-Jlf/!ifg
Toberculodinium vancampoae (Rossignol) Q)1:
m~t: 13*Jl[~I;::,:to~7.>5J';{jj ....... ·t~!liIl~3C<j:IllB:;t:i(Ztft;::,~~7.> '7'/7/'/ / Y "- -/I.-Q) MnX:
t:1:!Io/.JQ)~1l!U ...................... lJl{fE!'M.7L~ii-/{ :7*~l$tQ)i!fiiffri!t'7'/7l'/ffi!:l1! ......
~t~tfi~=*Q):tm~ t:IE~~JI:· ...... " ., ............. 1RVC~*· ll§fE~M~ts1:il!R*,BIlffl,!Em7 ~ -7"........... B3iJUJ/i-........................ MI3,m'T· ll§B3~M£
Porites Ji.JiQ) nlt:fit)£g[ t: nX::fitM ....
.................................. 9='~ lj:~~oJt '/~.

The Evolution of Laqueus (Brachiopoda) andthe theory of games .............. Y. Gunji*Ji.J: IJ i!€Lt.::""ffffl1:il!Rt:cllHf!OftEI'::'''?\'''L ..

mtia r :7 7 Q)1&Iit$. ........ ll§tttm'T • JlJ~«rtm........................ mrl3'-~· ~iimll~~ll§:;t:i(Ztf7~*~~*~mQ)1&Iit$.*:i(Z5J';(PDipteridaceae from the Upper Triassic Mine
Group in Yamaguchi Prefecture, japan (2).................................. G. Naito
Xenoxylon Q):ltB3ll!a%\.;{jj t: .:tQ)r.mm,~ ....... .

· ................................. JlJ~«rtm*~iJ!<flf~±Q) ~ft1:i5J',fJT t: ±~~~*6:!f!: t: Q)

ffimlf1:t;::, "?\" 'L ................ 9='i!tii~,*~~
Follicucullus (.....:.,1.- A*,c1&1it$.) t;::,,,?\,,'L ...................... 1:i1(r§tm~1l1IHI1\J:i\If~t:JjQ) l!R~ '7 '/ ~- '/ ~*ii, I? Q)
1&/lt$.~~-!/'Ift;::, Nassellaria t;::, "?\" 'L ....
· ................................. ¥r~tJ!i1'f)~Il· ftiBi:1lfi!€Q)~1l*J:I#1::ItB~~*~17) ~ '7'/7:l'/'7.-[ ?

P.............. JlJ~*J!!~. 6If4]B3¥1'f) • *1- iP<1*f!Ilpmi~ii' I? Q)m*ftE (Polyporaceae) t;::, ,,?~,'L ................................ W1#-Iirt~.~*:to.J:Lf~ffflM~K.J:~~='/ffi7Ji.Ji(AH4) Q)tR~Q)5J'M ...... *~{!Mlc • *ttittm
ffl.1::to .l: Lfft1:i ~ T';/ § Q) Cuticle Q)m~~~/ Y,,- -/1.-7' -\' - r ii, I? iltrWlY "- :7 *-C1&/lt$.

(~llIUii' I? I7)m~) ....... ·mF':l)I/Ji:~ • *ttittm· ....................... ~~rrM£· t~fEtr;k• • JllI,ll§llBa~.*m*Q)iltr·*MY,,-:7*-C1&
lt5c9='ft1:i .......................... t~!liIl ~~ft1:i1F~ • Ii'lJliif;fdf-~:to.J: Lfmnltf'Fffl - **11
9='1:~Q):51:i~17iJ t: L'L .......... *~f$~~~"Carcharodon" megalodon Q) *k1E5J'M .. ~*~ZFirst record of carnivorous dinosaur from theUpper Cretaceous of Kyushu, japan ..... .
.............. Y. Hasegawa and M. Murata
Second Cetotherid (Cetacea, Mammalia) skull

334
from the Ashiya Group, northern Kyushu................................ Y. Okazaki
mipp;ji'liQ)$ilgg~J1I!.f.4ft:Eff~ C -"tQ) ~~/jl;::":)I,'L ..•.... ·*~mz.

. 4-M7'l-l'& • ll.J*~-

Stegodon Q)*kilHtM ...... .:::.:tt~~ • **Wlc
I,':b~'=' "" - f,l ry :/~nl1;:11!! .l: I) g[lillA.:: "Stegolophodon" ft:E ....................... .

. ......... lEJf.fm~w· :lHtJII~fIl· ~* it~. A r :/ • ::r 7

mJII:11!!~tT$il':::'* Q) l¥i&fM:1f:rL~~)jFf:~i\!!iIii
I;::":)I,'L .......................... T.it*fltr
m.~JiiE~1f:rL~MQ)j1j/Ja!lJr~tmcQ) m'lf* I;::":)
I,'L .............................. ~t!l!. ~Calcidiscus leptoporus (Murry and Blackman)
Loeblich and Tappan (:EW(J( 1- :/ / 77 :/!/ r:/) Q)"~1;;t.,! r 1) - c"i!lJ.l!t ........,........................ 'NhI~ ·llijmrhlJit

KH79-3, C-3 (~tt:ll) Q)~S

1jJf~, -"tQ) 1, :lfUltJ!:ll:· ............. *MIJJ.I$
Fiijl:, -"tQ) 2, 1f:rL~ ................. . 1J~.~$
Fiijl:, -"tQ) 3, :EW(J(1-:/ / 77:/ !/ r :/ ..... .

.................................. il1lill.J~1IB
1iiJl:, -"tQ) 4, :litlti:~ ................ i§*!a':::'fl~Fiijl:, -"tQ) 5, I!~ ..................... 'N~ ~Fiijl:, -"tQ) 6, l!iU~Fiij(ftf*.It ............ *:II.;}i!;',~
Fiijl:, -"tQ) 7, ~¥.5 ........ *:II.;.'i!;',~. *MIJJ.I$• 1J~.~$ • 'N~ ~ • i§*!1:':::'fl~ • il1lill.J~1IB
OXygen and Carbon isotopic composition of
shelf and upper bathyal benthic foraminifera of Late Pleistocene age ........... .
T. Saito, S. Hasegawa and Y. Takayanagi
A Danian planktonic forminiferal fauna from
Tokotan, Hokkaido ..................... .
............ Y. Takayanagi and H. Yasuda
Upper Cretaceous to Middle Eocene foraminifera from eastern Hokkaido, Japan .. K. Kaiho
On the crystalline structure of Patellina corrugata Williamson ................ ffMfiI!leNew membership approved by the Council
Meeting held on June 20, 1984
Ordinary Members
ASAI, Akito; IYODA, Norio; NISHI, Hiroshi;
OHTA, Hiroyuki; SATO, Jun-ichi; SEKINE,
Hideto; SUZUKI, Tadashi ; TAKAYAMA, Kuniaki; TANAKA, Yoshihiro

Foreign Members
CHUNG, Kuang-gyi; HONG, Soo Park

Honorary Members
HUZIOKA, Kazuo; HASHIMOTO, Wataru; IKEBE, Nobuo

Fellows
HAYAMI, Tomoko; INOUE, Masao; KAWABE,
Tetsuya; KOMURA, Seiichi; MIKI, Takashi;
MURAMOTO, Kikuo; NOMURA, Ritsuo; SHIMOY AMA, Shoichi; SUGANO, Kozo; TOM IT A,
Yukimitsu; Y AJIMA, Michiko ; YAMADA, Jun

~ 133 @19854-{7IJ~

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19851j:: 2 J3 2,3 B

1984~1OJ3 3113

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Errata for No, 130
Plates 26 and 27 [Furutani: Middle Paleozoic Radiolaria]
Read Plate 27 for Plate 26, and read Plate 26 for Plate .27.

Errata for No. 131
Back cover, line 8
Read Ostracoda from the Pliocene Ananai ,I<·ormation, Shikoku, Japan-Description- for Ostracoda
from the Ananai Formation.

1984~4J32513

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Transactions and Proceedings of the PalaeontologicalSociety of Japan
April 30, 1984

New Series No. 133

CONTENTS
TRANSACTIONS
773. KIMURA, Tatsuaki and TSUJu, Masanori: Early Jurassic plants in Japan, Part 6 ..•.• 265
774. MATSUMOTO, Tatsuro, 1'AKAHASHI, Takemi, OBATA, Ikuwo and FUTAKAMI, Masao:
Cretaceous nautiloids from Hokkaido - IV • . . . . . . . . . . . . • . . • . . . . . . . 288
775. TAZAWA, Jun-ichi: Early Carboniferous (Visean) brachiopods from the Hikoroichi
Formation of the Kitakami Mountains, Northeast Japan ..•..........•. 300
776. FUJI, Norio: Palynological investigation of the postglacial deposits in Lagoon Kahokugata, Kanazawa, central Japan . . . . . . . . • . . . . . . . . . . . . . . . . . . • . . . . . 313
PROCEEDINGS . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . • . . . • . . . 332