Stratigraphy of the Permian Iwato and Mitai Formations in the Kamura area, Southwest Japan: Maokouan, Wuchiapingian, and Changhsingian carbonates formed on paleo-seamount.

彩乃, 太田; 亀齢, 勘米良; 行雄, 磯崎

doi:10.5575/geosoc.106.853

Cited by 13 publications

(33 citation statements)

References 15 publications

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“…globosa (Yabe), and Lepidolina cf. shiraiwensis (Ozawa) (Saito et al, 1958;Ota et al, 2000;Murata et al, 2003). The Mitai Formation consists of white to light gray dolomitic limestone, yielding a Lopingian fusuline assemblage including Codonofusiella kwangsiana Sheng, Reichelina media Miklukho-Maklay, R. changhsingensis Sheng, Palaeofusulina sp., Nankinella sp.…”

Section: Kamura Areamentioning

confidence: 97%

“…Later, Kanmera and Nakazawa (1973) distinguished the Mitai Formation between these two formations on the basis of Changhsingian (Upper Lopingian) fusulines including Palaeofusulina. In addition, Ota et al (2000) recognized a Wuchiapingian (Lower Lopingian) interval within the Mitai Formation. Also Watanabe et al (1979) and Koike (1996) added conodont data to confirm the Triassic stratigraphy of the Kamura Formation.…”

Section: Kamura Areamentioning

confidence: 98%

“…1). Following reconnaissance reports (Ota et al, 2000;Isozaki and Ota, 2001), this article describes details of the litho-and bio-stratigraphy of the sections at Kamura and Akasaka on the basis of field research and microscopic study of over 600 thin sections. In addition, we demonstrate the biostratigraphic correlation of these sections mainly with continental shelf sequences in South China, and discuss the significance of the G-L boundary fusuline turnover in the mid-superocean that may provide new constraints on the cause of the G-L boundary mass extinction.…”

Section: Introductionmentioning

confidence: 99%

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Fusuline biotic turnover across the Guadalupian–Lopingian (Middle–Upper Permian) boundary in mid-oceanic carbonate buildups: Biostratigraphy of accreted limestone in Japan

Ota

Isozaki

2006

Journal of Asian Earth Sciences

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122

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Section: Kamura Areamentioning

confidence: 97%

Section: Kamura Areamentioning

confidence: 98%

Section: Introductionmentioning

confidence: 99%

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Fusuline biotic turnover across the Guadalupian–Lopingian (Middle–Upper Permian) boundary in mid-oceanic carbonate buildups: Biostratigraphy of accreted limestone in Japan

Ota

Isozaki

2006

Journal of Asian Earth Sciences

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122

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“…Although its foraminiferal biostratigraphy is currently under more detailed investigation, previous fusuline studies have succeeded to establish the Codonofusiella-Reichelina Zone (or the C. kwangsiana-R. changhsingensis assemblage) in the Wuchiapingian part and the Palaeofusulina Zone (or the Reichelina changhsingensis-Nanlingella cf. meridionalis assemblage) and the Staffella-Nankinella Zone in the Changhsingian part of the Mitai Formation (Figure 9) (Kanmera and Nakazawa, 1973;Sano and Nakashima, 1997;Ota et al, 2000; and see also Ueno and Tsutsumi, 2009 for the Lopingian biostratigraphical subdivisions of the Kamura Limestone). For the Wuchiapingian, a recent examination revealed that primitive Nanlingella, which is similar to what Chediya in Kotlyar et al (1983) called Pseudodunbarula, is rather dominant (Hoshiki and Ueno, 2010).…”

Section: Correlation Of Lopingian Foraminiferal Zones/ Faunas Among Tmentioning

confidence: 99%

“…The Kamura Limestone in Japan is a typical Panthalassan mid-oceanic buildup x consisting of late Middle Permian-Triassic strata (Isozaki, 1997;Sano and Nakashima, 1997) and is distributed now as a kilometre-sized exotic limestone block in a Jurassic accretionary complex of the Chichibu Belt of Southwest Japan (Sano and Nakashima, 1997;Ota et al, 2000;Ota and Isozaki, 2006). The Mitai Formation (Kanmera and Nakazawa, 1973) of the Kamura Limestone provides the only known example that possesses a continuous shallow-marine succession of the entire Lopingian in the Panthalassan domain.…”

Section: Correlation Of Lopingian Foraminiferal Zones/ Faunas Among Tmentioning

confidence: 99%

The Lopingian (Late Permian) of mid‐oceanic carbonates in the Eastern Palaeotethys: stratigraphical outline and foraminiferal faunal succession

2010

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The Changning-Menglian Belt of West Yunnan, SW China and the Inthanon Zone of Northern Thailand are the two best-studied Palaeotethyan collisional belts in Asia. These belts comprise thick pure carbonate successions with basalt at the base, ranging from the Early Carboniferous to the end of the Permian. They are interpreted to have a mid-oceanic buildup x origin and have been formed on the top of seamounts and/or oceanic plateaus. The mid-oceanic carbonates in the Inthanon Zone are called the Doi Chiang Dao Limestone and we newly propose in this paper the term Banka Limestone for those in the Changning-Menglian Belt. Foraminiferal faunas from these limestones revealed that they have good Lopingian records of a mid-oceanic shallow-marine domain in the Palaeotethys, and three consecutive foraminiferal zones can be established. The Wuchiapingian is represented by the Codonofusiella kwangsiana Zone comprising four fusuline and 21 non-fusuline foraminiferal genera. The early Changhsingian is distinguished by the Palaeofusulina simplicata/minima Zone, and contains seven fusuline and 27 non-fusuline genera. The succeeding Palaeofusulina sinensis/prisca Zone in the late Changhsingian is characterized by the occurrence of large and advanced Palaeofusulina, and still maintained a high generic diversity with eight fusuline and 36 non-fusuline genera. The Lopingian foraminiferal faunal succession of the mid-oceanic Palaeotethys is essentially similar to those observed in cratonic South China. This is suggestive of a major oceanic part of the Palaeotethys to be included palaeobiogeographically in the Cathaysian Province. The coeval Neotethyan domain also had a high-diversified fauna with the occurrence of six fusuline and nearly 30 non-fusuline genera but lacked Palaeofusulina in Changhsingian time. Panthalassan mid-oceanic build-ups during Lopingian time carried likely lower foraminiferal diversity than those of the Palaeo-and Neotethys. Essentially, Tethyan mid-oceanic carbonate buildups x presumably provided a peculiar habitat suitable for shallow-marine foraminifers in a pelagic equatoro-tropical setting throughout almost the entire Lopingian time.

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Lopingian (Late Permian) foraminiferal faunal succession of a Paleo‐Tethyan mid‐oceanic carbonate buildup: Shifodong Formation in the Changning–Menglian Belt, West Yunnan, Southwest China

Ueno

Tsutsumi

2009

Island Arc

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This paper deals with a Lopingian (Late Permian) foraminiferal faunal succession of the Shifodong Formation in the Changning-Menglian Belt, West Yunnan, Southwest China, which has been geologically interpreted as one of the closed remnants in East Asia of the Paleo-Tethys Ocean. The Shifodong Formation is the uppermost stratigraphic unit in thick Carboniferous-Permian carbonates of the belt. These carbonates rest upon bases consisting of oceanic island basalt and are widely accepted as having a Paleo-Tethyan mid-oceanic (seamount-or oceanic plateau-top) origin. Sixteen taxa of fusuline foraminifers and 37 taxa of smaller (non-fusuline) foraminifers are recognized from the type section of the Shifodong Formation located in the Gengma area of the northern part of the Changning-Menglian Belt. Based on their stratigraphic distribution, three fusuline zones can be established in this section: they are, in ascending order, the Codonofusiella cf. C. kwangsiana Zone, Palaeofusulina minima Zone, and Palaeofusulina sinensis Zone. These three biozones are respectively referable to the Wuchiapingian, early Changhsingian, and late Changhsingian, of which the Wuchiapingian is first recognized in this study in the Changning-Menglian mid-oceanic carbonates. The present study clearly demonstrates that the foraminiferal fauna in a Paleo-Tethyan pelagic shallow-marine environment still maintained high faunal diversity throughout the almost entire Lopingian, although the very latest Permian fauna in the upper part of the Palaeofusulina sinensis Zone of the Shifodong section records a sudden decrease in both faunal diversity and abundance. Moreover, the Shifodong faunas are comparable in diversity with those observed in circum-Tethyan shelves such as South China. The present Paleo-Tethyan mid-oceanic foraminiferal faunas are definitely more diversified than coeval mid-oceanic Panthalassan faunas, which are typically represented by those from the Kamura Limestone in a Jurassic accretionary complex of Southwest Japan. It is suggestive that the Paleo-Tethyan mid-oceanic buildups presumably supplied a peculiarly hospitable habitat for foraminiferal faunal development in a pelagic paleo-equatorial condition.

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Stratigraphy of the Permian Iwato and Mitai Formations in the Kamura area, Southwest Japan: Maokouan, Wuchiapingian, and Changhsingian carbonates formed on paleo-seamount.

Cited by 13 publications

References 15 publications

Fusuline biotic turnover across the Guadalupian–Lopingian (Middle–Upper Permian) boundary in mid-oceanic carbonate buildups: Biostratigraphy of accreted limestone in Japan

Fusuline biotic turnover across the Guadalupian–Lopingian (Middle–Upper Permian) boundary in mid-oceanic carbonate buildups: Biostratigraphy of accreted limestone in Japan

The Lopingian (Late Permian) of mid‐oceanic carbonates in the Eastern Palaeotethys: stratigraphical outline and foraminiferal faunal succession

Lopingian (Late Permian) foraminiferal faunal succession of a Paleo‐Tethyan mid‐oceanic carbonate buildup: Shifodong Formation in the Changning–Menglian Belt, West Yunnan, Southwest China

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