- Email: [email protected]
Stratigraphic range of the genus Monodiexodina (Permian Fusulinoidea): additional data from the Southern Kitakami Massif, Northeast Japan
Journal of Asian Earth Sciences 23 (2004) 483–490 www.elsevier.com/locate/jseaes
Stratigraphic range of the genus Monodiexodina (Permian Fusulinoidea): additional data from the Southern Kitakami Massif, Northeast Japan Masayuki Ehiroa,*, Akihiro Misakib b
a The Tohoku University Museum, Sendai 980-8578, Japan Institute of Geology and Paleontology, Tohoku University, Sendai 980-8578, Japan
Received 14 June 2002; revised 17 June 2003; accepted 3 July 2003
Abstract The fusulinoidean species Monodiexodina matsubaishi (Fujimoto), thought formerly to be an index fossil of the lower Middle Permian M. matsubaishi Zone, was recovered from the Lepidolina multiseptata Zone in the Kamiyasse-Imo district, Southern Kitakami Massif, Northeast Japan. This indicates that the stratigraphic range of the genus Monodiexodina in the Southern Kitakami Massif should be extended upward into the Capitanian Stage of the upper Middle Permian, as in the southern Primorye. q 2003 Elsevier Ltd. All rights reserved. Keywords: Middle Permian Fusulinoidea; Monodiexodina; Kitakami Massif
1. Introduction The fusulinoidean species Monodiexodina matsubaishi (Fujimoto) possesses a unique morphology characterized by a highly elongate cylindrical test. This test morphology is reflected in the species name which was coined from two Japanese words matsuba (Needle-like leaves of pine tree) and ishi (stone), alluding to this extraordinary morphology reminiscent of a pine needle. In the Southern Kitakami Massif, Northeast Japan, this species occurs abundantly and exclusively in a calcareous facies of sandy limestone, calcareous sandstone, or calcareous mudstone. In Japan, a stratigraphic interval characterized by this species is named the M. matsubaishi Zone, which has long been regarded as designating an early Middle Permian time interval. However, there had been some disagreement among Japanese workers with regard to the chronostratigraphic range of M. matsubaishi. Fujimoto (1956) who originally proposed the species under the genus Parafusulina considered it ranges up into the upper Middle Permian ‘Yabeina’ Zone, although he did not present actual stratigraphic data to support his contention. However, Morikawa (1960) and Choi (1973) disagreed and showed * Corresponding author. Tel./fax: þ 81-22-217-7759. E-mail address: [email protected] (M. Ehiro). 1367-9120/$ - see front matter q 2003 Elsevier Ltd. All rights reserved. doi:10.1016/S1367-9120(03)00177-9
the species to be restricted to the lower part of the Middle Permian, which, in Japan, is biostratigraphically equated with the M. matsubaishi Zone. Recently, we found specimens of M. matsubaishi from the Lepidolina multiseptata Zone in the Kamiyasse-Imo district in the Southern Kitakami Massif, Northeast Japan. This new discovery is quite important in assessment of biostratigraphic values of fusulinoidean genera in recognizing the Middle Permian interval not only in the Southern Kitakami but also in the eastern Tethyan region. In spite of the wide geographic distribution of Monodiexodina in the eastern Tethys, opinions have diverged with regard to the stratigraphic range of this genus, as discussed later. The purpose of this paper is to describe the occurrence of M. matsubaishi above the horizon of the first occurrence of the genus Lepidolina in the Kamiyasse-Imo district and to discuss the stratigraphic range of the genus Monodiexodina based on this new discovery.
2. Regional geology and stratigraphy The Kamiyasse-Imo district (Fig. 1), north of Kesennuma City, Southern Kitakami Massif, represents one of the well-known, extensive outcrop areas of Permian strata in Japan. Many geological and paleontological investigations
484
M. Ehiro, A. Misaki / Journal of Asian Earth Sciences 23 (2004) 483–490
Fig. 1. Location map of the study area.
have been carried out there (see Onuki, 1969; Tazawa, 1976). The Permian sedimentary rocks exposed in areas north of Kesennuma City are divided into three formations, in upward sequence, the Nakadaira, Ochiai and Nabekoshiyama Formations (Ehiro, 1977). Of these, the first two formations characterize the Kamiyasse-Imo district. The Nakadaira Formation is essentially a shallow-water limestone unit and is intercalated with conglomerate, sandstone and mudstone. The limestone yields such fusulinoideans as Robustoschwagerina schellwieni and Pseudofusulina fusiformis (Tazawa, 1973, 1976), and is correlated with the Sakmarian to Kungurian Stages of the Lower Permian.
The Ochiai Formation is primarily a mudstone unit, intercalated in its middle part by a calcareous facies, named the Toyazawa Member (Ehiro, 1977). The lower part of the Ochiai Formation, which is more than 300 m thick, consists predominantly of mudstone and contains lesser amounts of sandstone. This lower part has few fossils, but is thought to be correlatable with the upper Kungurian to Roadian interval based on the stratigraphic relationships with the underlying Nakadaira Formation and the overlying Toyazawa Member. The Toyazawa Member is from 200 to 300 m thick and comprises beds of calcareous sandstone, calcareous
M. Ehiro, A. Misaki / Journal of Asian Earth Sciences 23 (2004) 483–490
mudstone and limestone, which altogether yield many fusulinoideans, corals, brachiopods, molluscs and other fossils. The occurrence in the Toyazawa Member of two fusulinoidean species, M. matsubaishi and L. multiseptata, and ammonoid genera such as Paraceltites, Cibolites, Waagenoceras and Timorites, enables a correlation of this member with a stratigraphic interval spanning from the Roadian to Capitanian Stages of the Middle Permian (Ehiro, 1998). Tazawa (1976) proposed two fusulinoidean zones to represent the Middle Permian sequence of the KamiyasseImo district, namely the lower M. matsubaishi Zone and the upper L. multiseptata Zone. The upper part of the Ochiai Formation is composed mainly of mudstone and its total thickness exceeds more than 1000 m. Specimens of Lepidolina and some ammonoid species indicative of a Capitanian age have been discovered from the lower part. Ehiro and Araki (1997) assigned a late Capitanian age to this part of the Ochiai Formation based on these fossils. The genus Lepidolina occurs from the upper part of the Toyazawa Member through the lower part of the upper part of the Ochiai Formation.
3. Stratigraphy of the uppermost part of the Toyazawa Member and its fusulinoidean fauna Rocks of the Ochiai Formation are distributed in the Kamiyasse-Imo district, forming basin-like synclinal
485
structures and anticlines having E – W trending fold axes. A syncline is developed around Mt Yatsumoridairayama, which rises on the border between the Kamiyasse and Imo districts. The Toyazawa Member and the basal part of the upper part of the Ochiai Formation are distributed around this mountain (Fig. 2). Both the Lepidolina-bearing limestone and the overlying Monodiexodina-bearing sandy limestone crop out on some small ridges forming the southern as well as southwestern slopes of the mountain. They constitute the southern wing of the syncline and dip northward at an angle of 20– 408. The fusulinoid-bearing succession of the upper part of the Toyazawa Member was observed at the following three ridges: first located between the Orendaizawa Valley and an east tributary of the Minamisawa River (section a of Fig. 2), second between the Takanosuzawa and Orendaizawa Valleys (section b of Fig. 2), and third between the Ohorazawa and Takanosuzawa Valleys (section c of Fig. 2). At the second ridge, the upper part of the Toyazawa Member is well exposed at elevations between 350 and 450 m. Below the 350 m altitude, sporadic outcrops of impure limestone with subordinate amounts of calcareous sandstone are developed. Many moulds of elongate shells, presumably tests of M. matsubaishi can be observed in these outcrops. Above 350 m, sporadic exposures of about 30 m-thick, dark gray muddy limestone with calcareous mudstone are observable (Fig. 3b). The upper part of this limestone bed yields Parafusulina
Fig. 2. Geologic map of the study area around Mt Yatsumoridairayama in the Kamiyasse-Imo district, Southern Kitakami Massif, Northeast Japan. Thick solid lines a, b and c indicate the study sections shown in Fig. 3.
486
M. Ehiro, A. Misaki / Journal of Asian Earth Sciences 23 (2004) 483–490
Fig. 3. Generalized columnar section of the Ochiai Formation (part) in the Kamiyasse-Imo district (left column) and the stratigraphic sections of the upper part of the Toyazawa Member to the lowermost part of the upper part of the Ochiai Formation on the southern slope of Mt Yatsumoridairayama with fusulinoidean data (columns a –c). Localities of the sections are shown in Fig. 2.
cf. guatemaraensis and Pseudofusulina sp. Above this muddy limestone, in upward sequence, lies a measured stratigraphic column including a 12 m light gray limestone, about 9 m massive conglomerate-sandstone, more than 2 m sandy limestone and about 20 m calcareous mudstone. This whole sequence grades upward into a massive black mudstone of the basal part of the upper part of the Ochiai Formation. The 12 m light gray limestone contains Lepidolina cf. multiseptata, L. sp. and Neoschwagerinidae gen. et sp. indet. This bed is therefore called the Lepidolina Limestone. Tazawa (1973) described the 9 m conglomerate-bearing sandstone as a ‘key conglomerate bed.’ A bedded sandy limestone, lying at about 17 m above the top of the Lepidolina Limestone, yields M. matsubaishi?, Parafusulina motoyoshiensis and Pseudofusulina sp. A dense concentration of shells of M. matsubaishi? can be seen in some thin interbeds of this bedded limestone (Monodiexodina Limestone).
The same successions of the Lepidolina Limestone and Monodiexodina Limestone can also be observed at the first and third ridges. At the first ridge, the Lepidolina Limestone yields Neoschwagerinidae gen. et sp. indet. and the Monodiexodina Limestone occurring at a higher stratigraphic horizon (Fig. 3a) contains abundant specimens of M. matsubaishi and Pseudofusulina sp. The Lepidolina Limestone at the third ridge is more than 8 m thick and contains in its upper part Lepidolina? sp., Colania? sp., Verbeekina verbeeki, V. sp. and Neoschwagerinidae gen. et sp. indet. The Monodiexodina Limestone, about 2.5 m thick, is exposed some 22 m stratigraphically above the Lepidolina Limestone (Fig. 3c) and contains abundant specimens of M. matsubaishi with addition of P. motoyoshiensis. Shells of Monodiexodina in the Monodiexodina Limestone are densely concentrated in some thin beds, but they are well preserved (Fig. 4 (4 and 5)). On the other hands, those of Parafusulina and Pseudofusulina crowded
M. Ehiro, A. Misaki / Journal of Asian Earth Sciences 23 (2004) 483–490
487
Fig. 4. Photomicrographs of Middle Permian fusulinoideans from the upper part of the Toyazawa Member of the Kamiyasse-Imo district, Southern Kitakami Massif, Northeast Japan. (1–2), Pseudofusulina sp., £ 11.0, from the Monodiexodina Limestone at Section b of Fig. 2. (3), Paratusulina motoyoshiensis (Morikawa), £ 11.0, from the Monodiexodina Limestone at Section c of Fig. 2. (4–5), Monodiexodina matsubaishi (Fujimoto), £ 5.5, from the Monodiexodina Limestone at section c of Fig. 2. (6), Verbeekina verbeeki(Geinitz), £ 8.0, from the Lepidolina Limestone at section c of Fig. 2. (7),Colania? sp., £ 8.0, from the Lepidolina Limestone at section c of Fig. 2. (8), Lepidolina cf. multiseptata (Deprat), £ 8.0, from the Lepidolina Limestone at section b of Fig. 2.
in alternated interbeds are sometimes fragmental (Fig. 4 (1, 2 and 3)) and considered to be more or less reworked. The Lepidolina Limestone and the underlying muddy limestone are considered to correspond to, respectively, ‘the gray massive limestone’ and the upper part of ‘the dark gray sandy limestone’ described by Tazawa (1973). Tazawa (1973, 1976) reported L. multiseptata, V. verbeeki and Codonofusiella explicata from his gray massive limestone
and abundant occurrences of M. matsubaishi, Chusenella chosiensis and P. motoyoshiensis from the sandy limestone. On the southern slope of Mt. Yatsumoridairayama, specimens of M. matsubaishi reappear in a sandy limestone facies above a Lepidolina-bearing limestone. Similar M. matsubaishi-bearing sandy limestone facies can be traced southeastward over a distance of 1 km to the western slope of Mt Kurosawayama. This process of identifying the same sandy limestone beds across the mountain slope was greatly
488
M. Ehiro, A. Misaki / Journal of Asian Earth Sciences 23 (2004) 483–490
facilitated by recognizing the ‘key conglomerate bed’ that underlies the M. matsubaishi-bearing sandy limestone.
4. Range of Monodiexodina matsubaishi in the Southern Kitakami Massif M. matsubaishi has long been thought to have a limited stratigraphic range in the lower part of the Middle Permian. Morikawa (1960) studied the fusulinoidean biostratigraphy of the Middle Permian Iwaizaki Limestone distributed in a district south of Kesennuma (Cape Iwaizaki) and established three zones, in ascending order, the Parafusulina matsubaishi Zone ( ¼ M. matsubaishi Zone), Pseudofusulina paramotohashii Zone and Yabeina shiraiwensis Zone ( ¼ L. multiseptata Zone). The short stratigraphic range of M. matsubaishi is used to define the M. matsubaishi Zone. Choi (1973) studied the Middle Permian Kanokura Formation developed in the Setamai-Yahagi district, northeast of the Kamiyasse-Imo district, and recognized three fusulinoidean zones, the M. matsubaishi Zone, Colania kotsuboensis Zone and L. multiseptata Zone. The occurrence of M. matsubaishi in this district is also confined to the zone of the same name and neither the C. kotsuboensis nor L. multiseptata Zone yields this species. Choi (1970) who examined the Permian stratigraphy of the Imo district concluded that the range of M. matsubaishi is nearly the same between Setamai-Yahagi and Imo districts. Choi (1973) correlated the P. paramotohashii Zone established in Iwaizaki with a combined interval encompassing the upper part of the M. matsubaishi Zone and the C. kotsuboensis Zone of the Setamai-Yahagi district. This correlation would place the uppermost range of M. matsubaishi somewhat higher in the Setamai-Yahagi district than Iwaizaki. Such a discrepancy of the uppermost range of M. matsubaishi between the two districts can possibly be explained by facies differences in the two areas. M. matsubaishi has been found exclusively in calcareous coarse clastic rocks (Igo, 1989; Ishii, 1990), including sandy limestone, calcareous sandstone and calcareous sandy mudstone, whereas the species is absent in a pure limestone or in a non-calcareous mudstone. Tazawa (1973) who studied the stratigraphy of Permian rocks in the Kamiyasse district recognized only two fusulinoidean zones for the Middle Permian, the lower M. matsubaishi and the upper L. multiseptata Zone. Although Tazawa’s range chart of fusulinoidean species (Fig. 4 of Tazawa, 1973) clearly shows a short overlapping range of M. matsubaishi and L. multiseptata within the L. multiseptata Zone, this fact was not described in the text of his paper. In his later study of the Permian stratigraphy of the Kesennuma district, Tazawa (1976; table 1) reconfirmed that M. matsubaishi is confined to the M. matsubaishi Zone and does not range up into the L. multiseptata Zone. Our observations reveal two facts regarding the species M. matsubaishi. Firstly, it serves as an important index
species of the M. matsubaishi Zone, but in the KamiyasseImo district the upper range of this species does extend to the lower part of the L. multiseptata Zone equatable with the Capitanian Stage. Secondly, the longer stratigraphic range of M. matsubaishi in the Kamiyasse-Imo district than those in the Setamai and Iwaizaki districts largely resulted from the presence of calcareous coarse clastic sediments subsequent to the first appearance of Lepidolina. As suggested by Igo (1989) and Ishii (1990), such a favorable lithology is needed for the occurrence of M. matsubaishi. In the Setamai and Iwaizaki districts, on the contrary, more calcareous and less siliciclastic sediments, which were not suitable for M. matsubaishi, prevail in the strata of the L. matsubaishi Zone.
5. Stratigraphic range of the genus Monodiexodina in the Tethyan region Species belonging to the genus Monodiexodina are widely recorded from the eastern Tethys, including such districts as Inner Mongolia, Heilonjiang and Jiling of North China, southern Primorye, Southern Kitakami, Kurosegawa and Hida Gaien Belts of Japan, Salt Range, Karakorum, Thailand, Malaysia, and Timor (e.g. Han, 1980; Ozawa, 1987; Tazawa et al., 1993; Shi et al., 1995). This genus comprises two morphologically different groups, M. sutschanica and M. kattaensis groups (Choi, 1973; Han, 1980). M. matsubaishi belongs to the former group. Han (1980) also compared the stratigraphic ranges of these two groups and showed the former group to range from the Cancellina Zone to the lower part of the Neoschwagerina Zone and the latter being restricted to the Cancellina Zone. Kanmera et al. (1976) suggested that the genus Monodiexodina ranges from the Misellina Zone to the lower part of the Neoschwagerina Zone. Ross (1995) considered that the genus ranges from the Misellina Zone to the lower part of the Cancellina Zone. Therefore, it has generally been believed that the range of the genus Monodiexodina does not extend into the Lepidolina Zone or Yabeina Zone equatable with the Capitanian Stage of the upper Middle Permian. In the southern Primorye, the Middle Permian Chandalaz Formation has been classified into three fusulinoidean zones in ascending order, the Monodiexodina sutschanica – Metadoliolina dutkevitchi Zone, Parafusulina stricta Zone, and Metadoliolina lepida – Lepidolina kumaensis Zone (Sosnina, 1960; Sosnina and Nikitina, 1977). Contrary to the general understanding of the pre-Capitanian range of the genus Monodiexodina, Kotlyar et al. (1989) assigned the M. sutschanica –M. dutkevitchi Zone to the lower part of the Midian ( ¼ Capitanian) Stage on account of the presence in this zone of two species of the genus Lepidolina, L. kumaensis and L. ussurica. The genus Lepidolina is an index fossil of the Capitanian Stage of the upper Middle Permian. Leven (1993) also contended that the genus Monodiexodina
M. Ehiro, A. Misaki / Journal of Asian Earth Sciences 23 (2004) 483–490
ranged upward into the Capitanian Stage based on his argument on the morphological similarity between M. sutschanica, reported from the southern Primorye and M. matsubaishi from the Southern Kitakami. Additionally, Leven (1993) cited the occurrence of Codonofusiella and Rauserella in the M. matsubaishi Zone of the Southern Kitakami as another evidence of correlating it with the Capitanian Stage. However, the joint occurrence of Monodiexodina and two Lepidolina species, L. kumaensis –L. ussurica in the southern Primorye needs to be questioned because Leven (1996) made the following statement: “ Kotlyar et al. (1989) believed that this form [L. kumaensis ] is also present in the underlying M. sutschanica –M. dutkevitchi Zone, however, this assumption was turned out to be invalid (G.V. Kotlyar, personal communication)”. In fact Taschi et al. (1992) showed only the occurrence of Lepidolina sp. within the M. sutschanica – M. dutkevitchi Zone in the southern Primorye, and besides these specimens of Lepidolina from the M. sutschanica – M. dutkevitchi Zone have not been described, nor figured. Also, the Southern Kitakami evidence cited by Leven (1993) does not support the Capitanian age of Monodiexodina. These two fusulinoidean genera Codonofusiella and Rauserella, regarded by Leven (1993) as index fossils of the Capitanian Stage, have been shown to range downward into the lower Middle Permian (for example, Sheng et al., 1988; Ross, 1995). Contrary to such an interpretation by Leven (1993), Choi (1973) did find Cancellina sp., an index fossil of the Cancellina Zone, in the lower part of the M. matsubaishi Zone and correlated the latter zone with the Neoschwagerina simplex to N. craticulifera Zones (Roadian to Wordian Stages). Although several lines of evidence presented by Leven (1993) need to be reevaluated, the present discovery of M. matsubaishi from the lower part of the Lepidolina Zone in the Kamiyasse-Imo district, Southern Kitakami, does strongly support the extended range of Monodiexodina into the Capitanian Stage in the eastern Tethys.
6. Conclusions In the Kamiyasse-Imo district of the Southern Kitakami Massif, Northeast Japan, fusulinoidean species of M. matsubaishi, whose range has so far been thought to be confined to the M. matsubaishi Zone, occurs in the lower part of the overlying L. multiseptata Zone. Such an extended range is interpreted to have resulted from the presence of coarse clastic calcareous sediments in the strata of the L. multiseptata Zone in the sedimentary basin. The present discovery of Monodiexodina from the L. multiseptata Zone in the Southern Kitakami strongly supports data in southern Primorye presented by Kotlyar et al. (1989) and indicates that the stratigraphic range of the genus Monodiexodina in the eastern Tethys does extend upward into the Capitanian Stage.
489
Acknowledgements Dr K. Ishizaki is cordially thanked for identification of fusulinoidean fossils and critical reading of the early draft of the manuscript. We also thank Drs T. Saito and B.F. Glenister for their critical reading of the manuscript. Dr N. Suzuki kindly translated some Russian papers. The paper has been greatly improved by comments and suggestions from Drs K. Ueno and F. Kobayashi.
References Choi, D.R., 1970. Permian fusulinids from Imo, Southern Kitakami Mountains, NE Japan. Journal of the Faculty of Science, Hokkaido University, Series 4 (14), 327–354. Choi, D.R., 1973. Permian fusulinids from the Setamai-Yahagi district, Southern Kitakami Mountains, NE Japan. Journal of the Faculty of Science, Hokkaido University, Series 4 (16), 1–132. Ehiro, M., 1977. The Hizume–Kesennuma Fault—with special reference to its character and significance on the geologic development. Contributions from the Institute of Geology and Paleontology, Tohoku University 77, 1–37.(in Japanese with English abstract). Ehiro, M., 1998. Ammonoid biostratigraphy of the Middle Permian in the South Kitakami Belt, Japan and correlation with the reference sections in the Tethyan region and North America. Proceedings of the Royal Society of Victoria 110, 147 –156. Ehiro, M., Araki, H., 1997. Permian cephalopods of Kurosawa, Kesennuma City in the Southern Kitakami Massif, Northeast Japan. Paleontological Research 1, 55–66. Fujimoto, H., 1956. A new species of Parafusulina from the Kitakami Massif Japan. Transactions and Proceedings of the Palaeontological Society of Japan, New Series 21, 157–160. Han, J., 1980. The morphology, evolution and distribution of the genus Monodiexodina and its allied genera. Bulletin of the Chinese Academy of Geological Sciences, Series 5 (1), 90–102.(in Chinese with English abstract). Igo, H., 1989. Fusulinaceans as an indicator of paleobiogeography. In: Takayanagi, Y., Ishizaki, K. (Eds.), Collected Papers on Foraminifera from the Japanese Islands, Toko Printing Co. Ltd, Sendai, pp. 1–9, (in Japanese). Ishii, K., 1990. Provinciality of some fusulinacean faunas of Japan. In: Ichikawa, K., Mizutani, S., Hara, I., Hada, S., Yao, A. (Eds.), PreCretaceous Terranes of Japan, Nippon Insatsu Shuppan Co. Ltd, Osaka, pp. 297–305. Kanmera, K., Ishii, K., Toriyama, R., 1976. The evolution and extinction patterns of Permian fusulinaceans. In: Kobayashi, T., Hashimoto, W. (Eds.), Geology and Palaeontology of Southeast Asia 17, The University of Tokyo Press, Tokyo, pp. 129– 154. Kotlyar, G.V., Zakharov, Yu.D., Kropatcheva, G.S., Pronina, G.P., Chedija, I.O., Burago, V.I., 1989. Evolution of the Latest Permian Biota: Midian Regional Stage in the USSR, Nauka, Leningrad, 184 pp. (in Russian). Leven, E.Ya., 1993. Main events in Permian history of the Tethys and fusulinids. Stratigraphy and Geological Correlation 1, 59–75. Leven, E.Ya., 1996. The Midian Stage of the Permian and its boundaries. Stratigraphy and Geological Correlation 4, 450–551. Morikawa, R., 1960. Fusulinids from the Iwaizaki Limestone. Science Report of the Saitama University, Series B 3, 273–299. Onuki, Y., 1969. Geology of the Kitakami Massif, Northeast Japan. Contributions from the Institute of Geology and Paleontology, Tohoku University 69, 1–239.(in Japanese with English abstract). Ozawa, T., 1987. Permian fusulinacean biostratigraphic provinces in Asia and their tectonic implications. In: Taira, A., Tashiro, M. (Eds.),
490
M. Ehiro, A. Misaki / Journal of Asian Earth Sciences 23 (2004) 483–490
Historical Biogeography and Plate Tectonic Evolution of Japan and Eastern Asia, Terra Scientific Publishing Company, Tokyo, pp. 45–63. Ross, C.A., 1995. Permian fusulinaceans. In: Scholle, P.A., Peryt, T.M., Ulmer-Scholle, D.S. (Eds.), The Permian of Northern Pangea 1. Paleogeography, Paleoclimate, Stratigraphy, Springer, Berlin, pp. 167– 185. Sheng, J., Zhang, L., Wang, J., 1988. Fusulinids, Science Press, Beijing, 240 pp. (in Chinese). Shi, G.R., Archbold, N.W., Zhan, L.P., 1995. Distribution and characteristics of mixed (transitional) mid-Permian (Late Artinskian –Ufimian) marine faunas in Asia and their palaeogeographical implications. Palaeogeography, Palaeoclimatology, Palaeoecology 114, 241–271. Sosnina, M.I., 1960. Microfaunistic zones in the Carboniferous and Permian deposits of the Sikhote-Alin. International Geological Congress, 21 session, Report of Soviet Geologist, Problem 6, 65–68.(in Russian with English abstract).
Sosnina, M.I., Nikitina, A.P., 1977. In: Iskopaemaya Flora i Fauna Dal’nego Vostoka Voprosy Stratigrafii Fanerozoya, Akademiya Nauk SSSR, Dal’nevostochnyy Geologicheskiy Institut, pp. 27 –52, (in Russian). Taschi, S.M, Kotlyar, G.V., Nikitina, A.P., Kiseleva, A.V., 1992. Stop 11Senkina Shapka Mountain. In: Zakharov, Yu.D, Panchenko, I.V., Khanchuk, A.I. (Eds.), A Field Guide to the Late Paleozoic and Early Mesozoic Circum-Pacific Bio- and Geological Events, Far Eastern Geological Institute, Far Eastern Branch of Russian Academy of Sciences, Vladivostok, pp. 51–59. Tazawa, J., 1973. Geology of the Kamiyasse area, Southern Kitakami Mountains. Journal of the Geological Society of Japan 79, 677–686.(in Japanese with English abstract). Tazawa, J., 1976. The Permian of Kesennuma, Kitakami Mountain: a preliminary report. Earth Science (Chikyu Kagaku) 30, 175 –185. Tazawa, J., Tsusima, K., Hasegawa, Y., 1993. Discovery of Monodiexodina from the Permian Moribu Formation in the Hida Gaien Belt, Central Japan. Earth Science (Chikyu Kagaku) 47, 345–348.(in Japanese).
Stratigraphic range of the genus Monodiexodina (Permian Fusulinoidea): additional data from the Southern Kitakami Massif, Northeast Japan Masayuki Ehiroa,*, Akihiro Misakib b
a The Tohoku University Museum, Sendai 980-8578, Japan Institute of Geology and Paleontology, Tohoku University, Sendai 980-8578, Japan
Received 14 June 2002; revised 17 June 2003; accepted 3 July 2003
Abstract The fusulinoidean species Monodiexodina matsubaishi (Fujimoto), thought formerly to be an index fossil of the lower Middle Permian M. matsubaishi Zone, was recovered from the Lepidolina multiseptata Zone in the Kamiyasse-Imo district, Southern Kitakami Massif, Northeast Japan. This indicates that the stratigraphic range of the genus Monodiexodina in the Southern Kitakami Massif should be extended upward into the Capitanian Stage of the upper Middle Permian, as in the southern Primorye. q 2003 Elsevier Ltd. All rights reserved. Keywords: Middle Permian Fusulinoidea; Monodiexodina; Kitakami Massif
1. Introduction The fusulinoidean species Monodiexodina matsubaishi (Fujimoto) possesses a unique morphology characterized by a highly elongate cylindrical test. This test morphology is reflected in the species name which was coined from two Japanese words matsuba (Needle-like leaves of pine tree) and ishi (stone), alluding to this extraordinary morphology reminiscent of a pine needle. In the Southern Kitakami Massif, Northeast Japan, this species occurs abundantly and exclusively in a calcareous facies of sandy limestone, calcareous sandstone, or calcareous mudstone. In Japan, a stratigraphic interval characterized by this species is named the M. matsubaishi Zone, which has long been regarded as designating an early Middle Permian time interval. However, there had been some disagreement among Japanese workers with regard to the chronostratigraphic range of M. matsubaishi. Fujimoto (1956) who originally proposed the species under the genus Parafusulina considered it ranges up into the upper Middle Permian ‘Yabeina’ Zone, although he did not present actual stratigraphic data to support his contention. However, Morikawa (1960) and Choi (1973) disagreed and showed * Corresponding author. Tel./fax: þ 81-22-217-7759. E-mail address: [email protected] (M. Ehiro). 1367-9120/$ - see front matter q 2003 Elsevier Ltd. All rights reserved. doi:10.1016/S1367-9120(03)00177-9
the species to be restricted to the lower part of the Middle Permian, which, in Japan, is biostratigraphically equated with the M. matsubaishi Zone. Recently, we found specimens of M. matsubaishi from the Lepidolina multiseptata Zone in the Kamiyasse-Imo district in the Southern Kitakami Massif, Northeast Japan. This new discovery is quite important in assessment of biostratigraphic values of fusulinoidean genera in recognizing the Middle Permian interval not only in the Southern Kitakami but also in the eastern Tethyan region. In spite of the wide geographic distribution of Monodiexodina in the eastern Tethys, opinions have diverged with regard to the stratigraphic range of this genus, as discussed later. The purpose of this paper is to describe the occurrence of M. matsubaishi above the horizon of the first occurrence of the genus Lepidolina in the Kamiyasse-Imo district and to discuss the stratigraphic range of the genus Monodiexodina based on this new discovery.
2. Regional geology and stratigraphy The Kamiyasse-Imo district (Fig. 1), north of Kesennuma City, Southern Kitakami Massif, represents one of the well-known, extensive outcrop areas of Permian strata in Japan. Many geological and paleontological investigations
484
M. Ehiro, A. Misaki / Journal of Asian Earth Sciences 23 (2004) 483–490
Fig. 1. Location map of the study area.
have been carried out there (see Onuki, 1969; Tazawa, 1976). The Permian sedimentary rocks exposed in areas north of Kesennuma City are divided into three formations, in upward sequence, the Nakadaira, Ochiai and Nabekoshiyama Formations (Ehiro, 1977). Of these, the first two formations characterize the Kamiyasse-Imo district. The Nakadaira Formation is essentially a shallow-water limestone unit and is intercalated with conglomerate, sandstone and mudstone. The limestone yields such fusulinoideans as Robustoschwagerina schellwieni and Pseudofusulina fusiformis (Tazawa, 1973, 1976), and is correlated with the Sakmarian to Kungurian Stages of the Lower Permian.
The Ochiai Formation is primarily a mudstone unit, intercalated in its middle part by a calcareous facies, named the Toyazawa Member (Ehiro, 1977). The lower part of the Ochiai Formation, which is more than 300 m thick, consists predominantly of mudstone and contains lesser amounts of sandstone. This lower part has few fossils, but is thought to be correlatable with the upper Kungurian to Roadian interval based on the stratigraphic relationships with the underlying Nakadaira Formation and the overlying Toyazawa Member. The Toyazawa Member is from 200 to 300 m thick and comprises beds of calcareous sandstone, calcareous
M. Ehiro, A. Misaki / Journal of Asian Earth Sciences 23 (2004) 483–490
mudstone and limestone, which altogether yield many fusulinoideans, corals, brachiopods, molluscs and other fossils. The occurrence in the Toyazawa Member of two fusulinoidean species, M. matsubaishi and L. multiseptata, and ammonoid genera such as Paraceltites, Cibolites, Waagenoceras and Timorites, enables a correlation of this member with a stratigraphic interval spanning from the Roadian to Capitanian Stages of the Middle Permian (Ehiro, 1998). Tazawa (1976) proposed two fusulinoidean zones to represent the Middle Permian sequence of the KamiyasseImo district, namely the lower M. matsubaishi Zone and the upper L. multiseptata Zone. The upper part of the Ochiai Formation is composed mainly of mudstone and its total thickness exceeds more than 1000 m. Specimens of Lepidolina and some ammonoid species indicative of a Capitanian age have been discovered from the lower part. Ehiro and Araki (1997) assigned a late Capitanian age to this part of the Ochiai Formation based on these fossils. The genus Lepidolina occurs from the upper part of the Toyazawa Member through the lower part of the upper part of the Ochiai Formation.
3. Stratigraphy of the uppermost part of the Toyazawa Member and its fusulinoidean fauna Rocks of the Ochiai Formation are distributed in the Kamiyasse-Imo district, forming basin-like synclinal
485
structures and anticlines having E – W trending fold axes. A syncline is developed around Mt Yatsumoridairayama, which rises on the border between the Kamiyasse and Imo districts. The Toyazawa Member and the basal part of the upper part of the Ochiai Formation are distributed around this mountain (Fig. 2). Both the Lepidolina-bearing limestone and the overlying Monodiexodina-bearing sandy limestone crop out on some small ridges forming the southern as well as southwestern slopes of the mountain. They constitute the southern wing of the syncline and dip northward at an angle of 20– 408. The fusulinoid-bearing succession of the upper part of the Toyazawa Member was observed at the following three ridges: first located between the Orendaizawa Valley and an east tributary of the Minamisawa River (section a of Fig. 2), second between the Takanosuzawa and Orendaizawa Valleys (section b of Fig. 2), and third between the Ohorazawa and Takanosuzawa Valleys (section c of Fig. 2). At the second ridge, the upper part of the Toyazawa Member is well exposed at elevations between 350 and 450 m. Below the 350 m altitude, sporadic outcrops of impure limestone with subordinate amounts of calcareous sandstone are developed. Many moulds of elongate shells, presumably tests of M. matsubaishi can be observed in these outcrops. Above 350 m, sporadic exposures of about 30 m-thick, dark gray muddy limestone with calcareous mudstone are observable (Fig. 3b). The upper part of this limestone bed yields Parafusulina
Fig. 2. Geologic map of the study area around Mt Yatsumoridairayama in the Kamiyasse-Imo district, Southern Kitakami Massif, Northeast Japan. Thick solid lines a, b and c indicate the study sections shown in Fig. 3.
486
M. Ehiro, A. Misaki / Journal of Asian Earth Sciences 23 (2004) 483–490
Fig. 3. Generalized columnar section of the Ochiai Formation (part) in the Kamiyasse-Imo district (left column) and the stratigraphic sections of the upper part of the Toyazawa Member to the lowermost part of the upper part of the Ochiai Formation on the southern slope of Mt Yatsumoridairayama with fusulinoidean data (columns a –c). Localities of the sections are shown in Fig. 2.
cf. guatemaraensis and Pseudofusulina sp. Above this muddy limestone, in upward sequence, lies a measured stratigraphic column including a 12 m light gray limestone, about 9 m massive conglomerate-sandstone, more than 2 m sandy limestone and about 20 m calcareous mudstone. This whole sequence grades upward into a massive black mudstone of the basal part of the upper part of the Ochiai Formation. The 12 m light gray limestone contains Lepidolina cf. multiseptata, L. sp. and Neoschwagerinidae gen. et sp. indet. This bed is therefore called the Lepidolina Limestone. Tazawa (1973) described the 9 m conglomerate-bearing sandstone as a ‘key conglomerate bed.’ A bedded sandy limestone, lying at about 17 m above the top of the Lepidolina Limestone, yields M. matsubaishi?, Parafusulina motoyoshiensis and Pseudofusulina sp. A dense concentration of shells of M. matsubaishi? can be seen in some thin interbeds of this bedded limestone (Monodiexodina Limestone).
The same successions of the Lepidolina Limestone and Monodiexodina Limestone can also be observed at the first and third ridges. At the first ridge, the Lepidolina Limestone yields Neoschwagerinidae gen. et sp. indet. and the Monodiexodina Limestone occurring at a higher stratigraphic horizon (Fig. 3a) contains abundant specimens of M. matsubaishi and Pseudofusulina sp. The Lepidolina Limestone at the third ridge is more than 8 m thick and contains in its upper part Lepidolina? sp., Colania? sp., Verbeekina verbeeki, V. sp. and Neoschwagerinidae gen. et sp. indet. The Monodiexodina Limestone, about 2.5 m thick, is exposed some 22 m stratigraphically above the Lepidolina Limestone (Fig. 3c) and contains abundant specimens of M. matsubaishi with addition of P. motoyoshiensis. Shells of Monodiexodina in the Monodiexodina Limestone are densely concentrated in some thin beds, but they are well preserved (Fig. 4 (4 and 5)). On the other hands, those of Parafusulina and Pseudofusulina crowded
M. Ehiro, A. Misaki / Journal of Asian Earth Sciences 23 (2004) 483–490
487
Fig. 4. Photomicrographs of Middle Permian fusulinoideans from the upper part of the Toyazawa Member of the Kamiyasse-Imo district, Southern Kitakami Massif, Northeast Japan. (1–2), Pseudofusulina sp., £ 11.0, from the Monodiexodina Limestone at Section b of Fig. 2. (3), Paratusulina motoyoshiensis (Morikawa), £ 11.0, from the Monodiexodina Limestone at Section c of Fig. 2. (4–5), Monodiexodina matsubaishi (Fujimoto), £ 5.5, from the Monodiexodina Limestone at section c of Fig. 2. (6), Verbeekina verbeeki(Geinitz), £ 8.0, from the Lepidolina Limestone at section c of Fig. 2. (7),Colania? sp., £ 8.0, from the Lepidolina Limestone at section c of Fig. 2. (8), Lepidolina cf. multiseptata (Deprat), £ 8.0, from the Lepidolina Limestone at section b of Fig. 2.
in alternated interbeds are sometimes fragmental (Fig. 4 (1, 2 and 3)) and considered to be more or less reworked. The Lepidolina Limestone and the underlying muddy limestone are considered to correspond to, respectively, ‘the gray massive limestone’ and the upper part of ‘the dark gray sandy limestone’ described by Tazawa (1973). Tazawa (1973, 1976) reported L. multiseptata, V. verbeeki and Codonofusiella explicata from his gray massive limestone
and abundant occurrences of M. matsubaishi, Chusenella chosiensis and P. motoyoshiensis from the sandy limestone. On the southern slope of Mt. Yatsumoridairayama, specimens of M. matsubaishi reappear in a sandy limestone facies above a Lepidolina-bearing limestone. Similar M. matsubaishi-bearing sandy limestone facies can be traced southeastward over a distance of 1 km to the western slope of Mt Kurosawayama. This process of identifying the same sandy limestone beds across the mountain slope was greatly
488
M. Ehiro, A. Misaki / Journal of Asian Earth Sciences 23 (2004) 483–490
facilitated by recognizing the ‘key conglomerate bed’ that underlies the M. matsubaishi-bearing sandy limestone.
4. Range of Monodiexodina matsubaishi in the Southern Kitakami Massif M. matsubaishi has long been thought to have a limited stratigraphic range in the lower part of the Middle Permian. Morikawa (1960) studied the fusulinoidean biostratigraphy of the Middle Permian Iwaizaki Limestone distributed in a district south of Kesennuma (Cape Iwaizaki) and established three zones, in ascending order, the Parafusulina matsubaishi Zone ( ¼ M. matsubaishi Zone), Pseudofusulina paramotohashii Zone and Yabeina shiraiwensis Zone ( ¼ L. multiseptata Zone). The short stratigraphic range of M. matsubaishi is used to define the M. matsubaishi Zone. Choi (1973) studied the Middle Permian Kanokura Formation developed in the Setamai-Yahagi district, northeast of the Kamiyasse-Imo district, and recognized three fusulinoidean zones, the M. matsubaishi Zone, Colania kotsuboensis Zone and L. multiseptata Zone. The occurrence of M. matsubaishi in this district is also confined to the zone of the same name and neither the C. kotsuboensis nor L. multiseptata Zone yields this species. Choi (1970) who examined the Permian stratigraphy of the Imo district concluded that the range of M. matsubaishi is nearly the same between Setamai-Yahagi and Imo districts. Choi (1973) correlated the P. paramotohashii Zone established in Iwaizaki with a combined interval encompassing the upper part of the M. matsubaishi Zone and the C. kotsuboensis Zone of the Setamai-Yahagi district. This correlation would place the uppermost range of M. matsubaishi somewhat higher in the Setamai-Yahagi district than Iwaizaki. Such a discrepancy of the uppermost range of M. matsubaishi between the two districts can possibly be explained by facies differences in the two areas. M. matsubaishi has been found exclusively in calcareous coarse clastic rocks (Igo, 1989; Ishii, 1990), including sandy limestone, calcareous sandstone and calcareous sandy mudstone, whereas the species is absent in a pure limestone or in a non-calcareous mudstone. Tazawa (1973) who studied the stratigraphy of Permian rocks in the Kamiyasse district recognized only two fusulinoidean zones for the Middle Permian, the lower M. matsubaishi and the upper L. multiseptata Zone. Although Tazawa’s range chart of fusulinoidean species (Fig. 4 of Tazawa, 1973) clearly shows a short overlapping range of M. matsubaishi and L. multiseptata within the L. multiseptata Zone, this fact was not described in the text of his paper. In his later study of the Permian stratigraphy of the Kesennuma district, Tazawa (1976; table 1) reconfirmed that M. matsubaishi is confined to the M. matsubaishi Zone and does not range up into the L. multiseptata Zone. Our observations reveal two facts regarding the species M. matsubaishi. Firstly, it serves as an important index
species of the M. matsubaishi Zone, but in the KamiyasseImo district the upper range of this species does extend to the lower part of the L. multiseptata Zone equatable with the Capitanian Stage. Secondly, the longer stratigraphic range of M. matsubaishi in the Kamiyasse-Imo district than those in the Setamai and Iwaizaki districts largely resulted from the presence of calcareous coarse clastic sediments subsequent to the first appearance of Lepidolina. As suggested by Igo (1989) and Ishii (1990), such a favorable lithology is needed for the occurrence of M. matsubaishi. In the Setamai and Iwaizaki districts, on the contrary, more calcareous and less siliciclastic sediments, which were not suitable for M. matsubaishi, prevail in the strata of the L. matsubaishi Zone.
5. Stratigraphic range of the genus Monodiexodina in the Tethyan region Species belonging to the genus Monodiexodina are widely recorded from the eastern Tethys, including such districts as Inner Mongolia, Heilonjiang and Jiling of North China, southern Primorye, Southern Kitakami, Kurosegawa and Hida Gaien Belts of Japan, Salt Range, Karakorum, Thailand, Malaysia, and Timor (e.g. Han, 1980; Ozawa, 1987; Tazawa et al., 1993; Shi et al., 1995). This genus comprises two morphologically different groups, M. sutschanica and M. kattaensis groups (Choi, 1973; Han, 1980). M. matsubaishi belongs to the former group. Han (1980) also compared the stratigraphic ranges of these two groups and showed the former group to range from the Cancellina Zone to the lower part of the Neoschwagerina Zone and the latter being restricted to the Cancellina Zone. Kanmera et al. (1976) suggested that the genus Monodiexodina ranges from the Misellina Zone to the lower part of the Neoschwagerina Zone. Ross (1995) considered that the genus ranges from the Misellina Zone to the lower part of the Cancellina Zone. Therefore, it has generally been believed that the range of the genus Monodiexodina does not extend into the Lepidolina Zone or Yabeina Zone equatable with the Capitanian Stage of the upper Middle Permian. In the southern Primorye, the Middle Permian Chandalaz Formation has been classified into three fusulinoidean zones in ascending order, the Monodiexodina sutschanica – Metadoliolina dutkevitchi Zone, Parafusulina stricta Zone, and Metadoliolina lepida – Lepidolina kumaensis Zone (Sosnina, 1960; Sosnina and Nikitina, 1977). Contrary to the general understanding of the pre-Capitanian range of the genus Monodiexodina, Kotlyar et al. (1989) assigned the M. sutschanica –M. dutkevitchi Zone to the lower part of the Midian ( ¼ Capitanian) Stage on account of the presence in this zone of two species of the genus Lepidolina, L. kumaensis and L. ussurica. The genus Lepidolina is an index fossil of the Capitanian Stage of the upper Middle Permian. Leven (1993) also contended that the genus Monodiexodina
M. Ehiro, A. Misaki / Journal of Asian Earth Sciences 23 (2004) 483–490
ranged upward into the Capitanian Stage based on his argument on the morphological similarity between M. sutschanica, reported from the southern Primorye and M. matsubaishi from the Southern Kitakami. Additionally, Leven (1993) cited the occurrence of Codonofusiella and Rauserella in the M. matsubaishi Zone of the Southern Kitakami as another evidence of correlating it with the Capitanian Stage. However, the joint occurrence of Monodiexodina and two Lepidolina species, L. kumaensis –L. ussurica in the southern Primorye needs to be questioned because Leven (1996) made the following statement: “ Kotlyar et al. (1989) believed that this form [L. kumaensis ] is also present in the underlying M. sutschanica –M. dutkevitchi Zone, however, this assumption was turned out to be invalid (G.V. Kotlyar, personal communication)”. In fact Taschi et al. (1992) showed only the occurrence of Lepidolina sp. within the M. sutschanica – M. dutkevitchi Zone in the southern Primorye, and besides these specimens of Lepidolina from the M. sutschanica – M. dutkevitchi Zone have not been described, nor figured. Also, the Southern Kitakami evidence cited by Leven (1993) does not support the Capitanian age of Monodiexodina. These two fusulinoidean genera Codonofusiella and Rauserella, regarded by Leven (1993) as index fossils of the Capitanian Stage, have been shown to range downward into the lower Middle Permian (for example, Sheng et al., 1988; Ross, 1995). Contrary to such an interpretation by Leven (1993), Choi (1973) did find Cancellina sp., an index fossil of the Cancellina Zone, in the lower part of the M. matsubaishi Zone and correlated the latter zone with the Neoschwagerina simplex to N. craticulifera Zones (Roadian to Wordian Stages). Although several lines of evidence presented by Leven (1993) need to be reevaluated, the present discovery of M. matsubaishi from the lower part of the Lepidolina Zone in the Kamiyasse-Imo district, Southern Kitakami, does strongly support the extended range of Monodiexodina into the Capitanian Stage in the eastern Tethys.
6. Conclusions In the Kamiyasse-Imo district of the Southern Kitakami Massif, Northeast Japan, fusulinoidean species of M. matsubaishi, whose range has so far been thought to be confined to the M. matsubaishi Zone, occurs in the lower part of the overlying L. multiseptata Zone. Such an extended range is interpreted to have resulted from the presence of coarse clastic calcareous sediments in the strata of the L. multiseptata Zone in the sedimentary basin. The present discovery of Monodiexodina from the L. multiseptata Zone in the Southern Kitakami strongly supports data in southern Primorye presented by Kotlyar et al. (1989) and indicates that the stratigraphic range of the genus Monodiexodina in the eastern Tethys does extend upward into the Capitanian Stage.
489
Acknowledgements Dr K. Ishizaki is cordially thanked for identification of fusulinoidean fossils and critical reading of the early draft of the manuscript. We also thank Drs T. Saito and B.F. Glenister for their critical reading of the manuscript. Dr N. Suzuki kindly translated some Russian papers. The paper has been greatly improved by comments and suggestions from Drs K. Ueno and F. Kobayashi.
References Choi, D.R., 1970. Permian fusulinids from Imo, Southern Kitakami Mountains, NE Japan. Journal of the Faculty of Science, Hokkaido University, Series 4 (14), 327–354. Choi, D.R., 1973. Permian fusulinids from the Setamai-Yahagi district, Southern Kitakami Mountains, NE Japan. Journal of the Faculty of Science, Hokkaido University, Series 4 (16), 1–132. Ehiro, M., 1977. The Hizume–Kesennuma Fault—with special reference to its character and significance on the geologic development. Contributions from the Institute of Geology and Paleontology, Tohoku University 77, 1–37.(in Japanese with English abstract). Ehiro, M., 1998. Ammonoid biostratigraphy of the Middle Permian in the South Kitakami Belt, Japan and correlation with the reference sections in the Tethyan region and North America. Proceedings of the Royal Society of Victoria 110, 147 –156. Ehiro, M., Araki, H., 1997. Permian cephalopods of Kurosawa, Kesennuma City in the Southern Kitakami Massif, Northeast Japan. Paleontological Research 1, 55–66. Fujimoto, H., 1956. A new species of Parafusulina from the Kitakami Massif Japan. Transactions and Proceedings of the Palaeontological Society of Japan, New Series 21, 157–160. Han, J., 1980. The morphology, evolution and distribution of the genus Monodiexodina and its allied genera. Bulletin of the Chinese Academy of Geological Sciences, Series 5 (1), 90–102.(in Chinese with English abstract). Igo, H., 1989. Fusulinaceans as an indicator of paleobiogeography. In: Takayanagi, Y., Ishizaki, K. (Eds.), Collected Papers on Foraminifera from the Japanese Islands, Toko Printing Co. Ltd, Sendai, pp. 1–9, (in Japanese). Ishii, K., 1990. Provinciality of some fusulinacean faunas of Japan. In: Ichikawa, K., Mizutani, S., Hara, I., Hada, S., Yao, A. (Eds.), PreCretaceous Terranes of Japan, Nippon Insatsu Shuppan Co. Ltd, Osaka, pp. 297–305. Kanmera, K., Ishii, K., Toriyama, R., 1976. The evolution and extinction patterns of Permian fusulinaceans. In: Kobayashi, T., Hashimoto, W. (Eds.), Geology and Palaeontology of Southeast Asia 17, The University of Tokyo Press, Tokyo, pp. 129– 154. Kotlyar, G.V., Zakharov, Yu.D., Kropatcheva, G.S., Pronina, G.P., Chedija, I.O., Burago, V.I., 1989. Evolution of the Latest Permian Biota: Midian Regional Stage in the USSR, Nauka, Leningrad, 184 pp. (in Russian). Leven, E.Ya., 1993. Main events in Permian history of the Tethys and fusulinids. Stratigraphy and Geological Correlation 1, 59–75. Leven, E.Ya., 1996. The Midian Stage of the Permian and its boundaries. Stratigraphy and Geological Correlation 4, 450–551. Morikawa, R., 1960. Fusulinids from the Iwaizaki Limestone. Science Report of the Saitama University, Series B 3, 273–299. Onuki, Y., 1969. Geology of the Kitakami Massif, Northeast Japan. Contributions from the Institute of Geology and Paleontology, Tohoku University 69, 1–239.(in Japanese with English abstract). Ozawa, T., 1987. Permian fusulinacean biostratigraphic provinces in Asia and their tectonic implications. In: Taira, A., Tashiro, M. (Eds.),
490
M. Ehiro, A. Misaki / Journal of Asian Earth Sciences 23 (2004) 483–490
Historical Biogeography and Plate Tectonic Evolution of Japan and Eastern Asia, Terra Scientific Publishing Company, Tokyo, pp. 45–63. Ross, C.A., 1995. Permian fusulinaceans. In: Scholle, P.A., Peryt, T.M., Ulmer-Scholle, D.S. (Eds.), The Permian of Northern Pangea 1. Paleogeography, Paleoclimate, Stratigraphy, Springer, Berlin, pp. 167– 185. Sheng, J., Zhang, L., Wang, J., 1988. Fusulinids, Science Press, Beijing, 240 pp. (in Chinese). Shi, G.R., Archbold, N.W., Zhan, L.P., 1995. Distribution and characteristics of mixed (transitional) mid-Permian (Late Artinskian –Ufimian) marine faunas in Asia and their palaeogeographical implications. Palaeogeography, Palaeoclimatology, Palaeoecology 114, 241–271. Sosnina, M.I., 1960. Microfaunistic zones in the Carboniferous and Permian deposits of the Sikhote-Alin. International Geological Congress, 21 session, Report of Soviet Geologist, Problem 6, 65–68.(in Russian with English abstract).
Sosnina, M.I., Nikitina, A.P., 1977. In: Iskopaemaya Flora i Fauna Dal’nego Vostoka Voprosy Stratigrafii Fanerozoya, Akademiya Nauk SSSR, Dal’nevostochnyy Geologicheskiy Institut, pp. 27 –52, (in Russian). Taschi, S.M, Kotlyar, G.V., Nikitina, A.P., Kiseleva, A.V., 1992. Stop 11Senkina Shapka Mountain. In: Zakharov, Yu.D, Panchenko, I.V., Khanchuk, A.I. (Eds.), A Field Guide to the Late Paleozoic and Early Mesozoic Circum-Pacific Bio- and Geological Events, Far Eastern Geological Institute, Far Eastern Branch of Russian Academy of Sciences, Vladivostok, pp. 51–59. Tazawa, J., 1973. Geology of the Kamiyasse area, Southern Kitakami Mountains. Journal of the Geological Society of Japan 79, 677–686.(in Japanese with English abstract). Tazawa, J., 1976. The Permian of Kesennuma, Kitakami Mountain: a preliminary report. Earth Science (Chikyu Kagaku) 30, 175 –185. Tazawa, J., Tsusima, K., Hasegawa, Y., 1993. Discovery of Monodiexodina from the Permian Moribu Formation in the Hida Gaien Belt, Central Japan. Earth Science (Chikyu Kagaku) 47, 345–348.(in Japanese).