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Palaeogeography, Palaeoclimatology, Palaeoecology 499 (2018) 13–21

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Palaeogeography, Palaeoclimatology, Palaeoecology

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Middle () seawater 87Sr/86Sr minimum coincided with T disappearance of tropical biota and collapse in NE Japan and Primorye (Far East ) ⁎ Tomomi Kania, , Yukio Isozakib, Ryutaro Hayashib, Yuri Zakharovc, Alexander Popovc a Faculty of Advanced Science and Technology, Division of Natural Science and Environmental Science, Kumamoto University, 2-39-1, Kurokami, Kumamoto, Japan 850-8555 b Department of Earth Science and Astronomy, The University of Tokyo, Komaba, Tokyo 153-8902, Japan c Far-Eastern Geological Institute, Russian Academy of Sciences (Far Eastern Branch), Stoletija Prospect 159, Vladivostok RU-690022, Russia

ARTICLE INFO ABSTRACT

Keywords: To investigate the secular changes in Permian seawater chemistry and to constrain the global environmental Seawater changes during the end- (Middle Permian) , we analyzed 87Sr/86Sr ratios in Capitanian Extinction (Upper Guadalupian) shallow-marine in NE Japan and in southern Primorye, Far East Russia. These Guadalupian limestones were deposited on the continental shelf/platform of the northern part of Greater South , which faced the northern connecting seaway between the Tethys and . The measured limestone samples Sr isotope were collected from the Capitanian fusuline (Lepidolina)-bearing intervals and overlying beds at Iwaizaki in the South Kitakami belt, NE Japan, and at Senkina Shapka in the Sergeevka belt, southern Primorye. The present analysis of bulk 87Sr/86Sr ratios clarified extremely low 87Sr/86Sr ratios of 0.7068–0.7070 from all measured samples. These Sr isotopic values support a Capitanian age for these strata. The topmost 30 m-thick interval of the Iwaizaki Limestone, in particular, witnessed a stepwise biodiversity decline in the shallow marine warm- water biota and the collapse of the carbonate factory after the reef development during the Capitanian in the northern part of Greater South China. The disappearance of the tropical biota and the collapse of the reef during the late Capitanian suggest that the biotic responses to a significant environmental change appeared relatively earlier at mid-latitudes than in the tropical regions.

1. Introduction throughout the entire the , whereas it tended to increase throughout the -Cenozoic (Fig. 1). The most significant The seawater 87Sr/86Sr ratio is mainly driven by the radiogenic flux change, in particular, an extremely low 87Sr/86Sr ratio interval, oc- from the continental crust and a less radiogenic flux from the mantle. curred in the Middle Permian, which marks the most unusual condition The balance of the fluxes has changed through geological time, and it is in the Sr cycle in the oceans (Veizer et al., 1999; Korte linked to global-scale changes in tectonics, sea level, continental et al., 2003, 2006; Kani et al., 2008; McArthur et al., 2012). This unique rates, mid-ocean ridge activity, and diagenetic processes “Permian minimum” has occurred in general coevally with the major (e.g., Veizer, 1989; McArthur et al., 2012). The residence time of Sr in mass extinction in the Middle Permian (Guadalupian), which represents seawater is estimated as ca. 3 million in modern oceans, which is the first major decline in the Permian marine biodiversity, but clearly much longer than the ocean circulation interval; therefore, seawater predates the terminal crisis at the Permo- boundary (P–TB) 87Sr/86Sr ratios are expected to be uniform worldwide. As the seawater (Stanley and Yang, 1994; Jin et al., 1994; Isozaki and Ota, 2001). The 87Sr/86Sr ratio is potentially recorded in marine carbonates, numerous Guadalupian biocrisis occurred not within a short time but over a studies to date have built a large archive of ancient seawater 87Sr/86Sr prolonged period of a few million years (Clapham et al., 2009). Its cause records, particularly for the Phanerozoic, which indeed demonstrate is still controversial (e.g., Erwin, 2006; Isozaki, 2009; Bond et al., remarkable secular changes through time (e.g., Burke et al., 1982; 2010a, 2010b); nonetheless, the relevant global environmental changes Denison et al., 1994; Martin and MacDougall, 1995; Veizer et al., 1999; no doubt involved significant changes in seawater chemistry including McArthur et al., 2012). The 87Sr/86Sr value generally tended to decline the Sr isotope composition.

⁎ Corresponding author. E-mail address: [email protected] (T. Kani). https://doi.org/10.1016/j.palaeo.2018.03.033 Received 12 September 2017; Received in revised form 26 March 2018; Accepted 26 March 2018 Available online 30 March 2018 0031-0182/ © 2018 Elsevier B.V. All rights reserved. T. Kani et al. Palaeogeography, Palaeoclimatology, Palaeoecology 499 (2018) 13–21

Fig. 1. Overview of secular changes in sea level (modified from Haq and Schutter, 2008) and the seawater Sr isotopic profile during the Phanerozoic (modified from McArthur et al., 2012) with major extinction timings.

Previous Sr isotope studies on the Guadalupian- boundary et al., 2010), NE Japan and Primorye naturally have pre- (G-LB) interval were carried out mostly in fossiliferous and thus well- with striking similarity. For example, the Sikhote-Alin fold belt dated shallow marine limestone sections deposited in low-latitude areas in southern Primorye comprises some geotectonic units that are (e.g., Denison and Koepnick, 1995; Martin and MacDougall, 1995; equivalent to those found in Japan; the Triassic- accretionary Jones et al., 1995; Korte et al., 2006; Kani et al., 2008, 2013). These complexes of the Samarka belt are no doubt correlated with those of the studies confirmed that unusually the low 87Sr/86Sr ratio in seawater (as Ultra-Tanba and Mino-Tanba-Ashio-North Kitakami belt in Japan (e.g., low as 0.7068) persisted throughout the Capitanian of the Gua- Kojima et al., 2000; Kemkin, 2012; Khanchuk et al., 2016). In addition, dalupian (the last one-third of the Guadalupian). This extremely Paleozoic granitoids and ophiolite units are common between the two low Sr isotope value naturally reflected a minimum flux from con- regions (e.g., Ishiwatari, 1991; Nevolin et al., 2010; Tsutsumi et al., tinental crust with respect to that from mid-oceanic ridges. For the 2014, 2016; Isozaki et al., 2015, 2017). cause of this unique phenomenon, a conventional explanation might The latest studies on detrital zircons in Paleozoic sandstones in the prefer a high sea level under global warming, which can suppress the South Kitakami belt in NE Japan (Okawa et al., 2013; Isozaki et al., global total weathering/erosion as a result of concealing vast con- 2014) and the Sergeevka belt in Primorye (Isozaki et al., 2017) have tinental coastal zones. Nonetheless, the sea level during the Capitanian confirmed the occurrence of Neoproterozoic grains that suggest the contradictorily recorded the lowest stand of the Phanerozoic (Haq and origin of NE Japan and southern Primorye together in an intimate link Schutter, 2008), suggesting a global cooling instead. Ice coverage and/ with the South China block (Isozaki et al., 2017). The common occur- or the predominance of arid climates under cooling during the Permian rence of Early Paleozoic arc granitoids in the two regions (Nevolin likely accelerated the decrease in the seawater Sr ratio. et al., 2010; Isozaki et al., 2015; Tsutsumi et al., 2016) also supports the For checking the spatiotemporal extent of the Capitanian Sr- interpretation that NE Japan and southern Primorye have been located minimum and its possible relations to the mass extinction, more data along the Pacific margin of Greater South China, i.e., a reconstructed are needed elsewhere with relevant records of biotic responses, parti- continental block composed of the South China block per se in the cularly from non-tropical higher-latitude areas. This study analyzed the mainland China together with SW-NE Japan and southern Primorye Sr isotope ratios of -Capitanian (Middle-Upper Guadalupian) (Isozaki et al., 2017). During the Permian, the main part of Greater limestones in the South Kitakami belt of northeast Japan, and the South China remained in a low-latitude area under a tropical climate Sergeevka belt in southern Primorye, Far East Russia. The latest ana- with typical warm-water Tethyan fauna, whereas its northern-eastern lyses on detrital zircon geochronology confirmed that both the South extension may have been positioned near the northern connecting Kitakami belt and the Sergeevka belt once formed northeastern exten- seaway between the Tethys and Panthalassa at relatively higher latitude sions of the Paleozoic South China block and have been overlooked for under subtropical conditions (Fig. 2A), probably to the north of the years (Isozaki et al., 2014, 2017; Fig. 2A); thus, the shallow marine North China block (Isozaki et al., 2017). shelf limestones in these two belts were deposited on the shelf/platform As to the Permian shallow marine sequence of continental shelf of Greater South China during the Permian, but likely at slightly higher facies, the South Kitakami belt (Fig. 2C) and the Sergeevka belt latitudes of the subtropical zone in the northern part of South China (Fig. 2D) share almost the same sedimentary packages with similar li- than in the mainland China with equatorial signatures. There is no thofacies and faunal assemblage, as preliminarily noted by Zakharov significant information to date for the biotic response in relatively et al. (1992); for example, the Middle Permian shallow marine lime- higher latitude region of Greater South China. This article reports the stone of the Iwaizaki-Kanokura formations in the South Kitakami belt results of the Sr isotopic analysis of the Iwaizaki Limestone in the South yield the same fauna as the Chandalaz Formation in the Sergeevka belt, Kitakami belt and a coeval limestone of the Chandalaz Formation and the overlying thick Upper Permian black shale of the Toyoma Fm in (Horizon) in the Sergeevka belt and discusses their geological im- the South Kitakami belt appears almost identical to the Lyudyanza Fm plications. in the Sergeevka belt. These Permian limestones indeed yield Tethyan fusulines (Lepidolina), rugose (Waagenophyllum, Wentzelella), 2. Geologic setting (Leptodus) and ammonoids (Stacheoceras) (e.g., Morikawa, 1960; Zakharov et al., 1992; Belyaeva et al., 1997; Ehiro, 1997, 2001; Ueno As currently located on the opposite sides of the Japan Sea, which et al., 2005; Kotlyar et al., 2006, 2007; Kossovaya and Kropatcheva, opened as a Miocene back-arc basin (Fig. 2A; Tamaki, 1988; Isozaki

14 T. Kani et al. Palaeogeography, Palaeoclimatology, Palaeoecology 499 (2018) 13–21

Fig. 2. Index maps for the study sections. A. Middle Permian paleogeographic map of the world, showing the locations of the study sections in NE Japan and in southern Primorye, Far East Russia, with respect to Pangea, Tethys, and Panthalassa (modified from Scotese, 2008; Kofukuda et al., 2014; Kirschvink et al., 2015; Isozaki et al., 2017). The locations of the reference sections are also shown, i.e., the GSSP of the G-LB at Penglaitan in South China and the sections on mid-oceanic seamounts in Panthalassa (Kamura and Akasaka). Note that the study sections were deposited in the northern part of Greater South China. B. Locality index for the Iwaizaki section in NE Japan, and the Senkina Shapka section in southern Primorye, Far East Russia. C. Geotectonic subdivision of NE Japan showing the South Kitakami belt with the Iwaizaki section (modified from Isozaki et al., 2015). D. Geotectonic subdivision of southern Primorye, showing the Sergeevka belt with the Senkina Shapka section (modified from Khanchuk et al., 2016). E. Age ranges of the Iwaizaki Limestone and the limestone of the Chandalaz Formation.

2013; Isozaki and Kase, 2014), and ammonoids (Ehiro, 1997, 2001); intercalated bioclastic limestones of continental shelf facies (e.g., Choi, nonetheless, they are slightly different in faunal content from the ty- 1976; Tazawa, 1991; Kawamura et al., 1990). Within the shallow pical Tethyan assemblage found in South China on mainland China by marine limestones, patch reefs occasionally develop, and the best-ex- including some boreal brachiopods (e.g., Yakovlevia, Cancrinella, and posed example is represented by the Iwaizaki Limestone in the southern Waagenoconcha; Tazawa, 1991; Shen and Shi, 2002) probably owing part of Kesen-numa City along the Pacific coast (Fig. 2B; Kawamura and the northerly position. Machiyama, 1995; Shen and Kawamura, 2001). Fig. 2C sketches a schematic profile of the Middle-Upper Permian strata in the Kesen-numa area, showing the mode of occurrence of the 2.1. Iwaizaki section Iwaizaki Limestone. The thickness of the limestone attains ca. 200 m in total. The stratigraphically lower part of the limestone is hidden under Within the thick Middle-Upper Paleozoic sedimentary package in the coastal waters; nonetheless, the basal part is composed of sandy the South Kitakami belt, the Permian strata consist mostly of shallow limestone that likely formed a pedestal of patch reef (Kawamura and marine terrigenous clastics (mudstone-dominated) and sporadically

15 T. Kani et al. Palaeogeography, Palaeoclimatology, Palaeoecology 499 (2018) 13–21

Machiyama, 1995). In contrast, the top of the limestone is covered by According to Kotlyar et al. (2006, 2007), this section comprises three thick black mudstone with slump structures. fusuline zones, i.e., 1) the Monodiexodina sutchanica-Metadoliolina On the basis of a detailed analysis of the depositional facies, dutkevitchi Zone, 2) the Parafusulina stricta Zone, and 3) the Metado- Kawamura and Machiyama (1995) subdivided the Iwaizaki Limestone liolina lepida-Lepidolina kumaensis Zone, in ascending order. The M. into 8 units, i.e., Units 1 to 8, in ascending order. The lowermost in- sutchanica-M. dutkevitchi Zone and M. lepida-L. kumaensis Zone are terval (Unit 1) consists of bioclastic limestone interbedded with sand- correlated with the Wordian and Capitanian, respectively. The P. stricta stone, whereas the main part (Units 2–7) is composed of massive Zone is also correlated also with the Wordian except for its topmost limestone with reef structures. In turn, the uppermost part (Unit 8) is horizon that contains an early Capitanian composed of interbedded bioclastic limestone and black mudstone. As postserrata (Behnken). As the topmost part of this limestone still yields to the age, the occurrence of large-tested fusuline Monodiexiodina large-tested fusulines (Lepidolina), the G-LB horizon likely occurs in a matsubaishi indicates a probable Wordian age for the Unit 1, whereas much higher horizon, probably in the overlying mudstone, which is not that of Lepidolina multiseptata (Morikawa et al., 1958; Morikawa, 1960) exposed at Senkina Shapka. A preliminary analysis of stable carbon indicates a Capitanian (late Guadalupian) age for the middle-upper isotopes was done for the Senkina Shapka section by Zakharov et al. parts of the limestone (Units 6 and 7 and the lower part of Unit 8). The (1997), and a positive excursion of up to 4‰ was recognized. topmost 30 m-thick interval, i.e., the upper part of Unit 8, has not yet been dated biostratigraphically, owing to the absence of index . 3. Methods Unit 8 is composed of well-bedded dark gray bioclastic limestone and black mudstone without any coarse-grained terrigenous clastics 3.1. Material and likely represents a terminal interval for the patch reef in the shelf setting (Kawamura and Machiyama, 1995). In addition to the mollusks, Fine-grained micritic limestone (or lime mudstone) is suitable for these mudstone beds contain abundant bioclasts of various shallow- measuring primary 87Sr/86Sr signatures, rather than sparitic bioclastic marine organisms, such as rugose/tabulate corals, bryozoans, brachio- limestones, as the former is demonstrated to have a good agreement pods, , calcisponges, ammonoids, and calcareous algae with signatures from coeval , brachiopods, and limestones (Morikawa et al., 1958; Kawamura and Machiyama, 1995; Isozaki and (Popp et al., 1986; Denison et al., 1994; Denison and Koepnick, 1995; Kase, 2014; Niko, 2015). The tropical biota, large-tested fusulines in Martin and Macdougall, 1995). We collected limestone samples for Sr particular, rugose corals, and large bivalves (Isozaki and Aljinovic, isotope analysis from the Iwaizaki section in NE Japan and the Senkina 2009), disappeared in a stepwise manner in the lower half of Unit 8 Shapka section in southern Primorye, specifically from fine-grained (Tobita and Isozaki, 2017). limestones (micritic parts composed of pure calcite with scarce terri- The overlying black mudstone (Unit 9 by Kawamura and genous components and without dolomitization and other diagenetic Machiyama, 1995) belongs to the basal Toyoma Formation (e.g., features). From the Iwaizaki section, 12 samples were measured, i.e., 6 Murata and Shimoyama, 1979), most of which is confirmed as Lo- from the Lepidolina Zone (upper Unit 7 and lower Unit 8) and the other pingian by ammonoids (e.g., Ehiro and Bando, 1985; Ehiro, 2006). The 6 from the overlying barren interval (upper Unit 8) (Fig. 3). From the occurrence of L. kumaensis in a thin limestone lens in the lowest Senkina Shapka section, > 20 samples were collected; however, the Toyoma Fm needs reevaluation, as the surrounding black mudstone limestones of the lower section at Senkina Shapka were too sandy, contains debris flow structures. Lopingian fossils are found not within whereas those of the upper part were too siliceous for analysis. Con- the Iwaizaki Limestone but in the overlying black mudstone at some sequently, we could measure 7 samples, i.e., 6 from the middle horizon hundreds of meters above the limestone. Thus, the exact horizon of the near the boundary between the P. stricta Zone and M. lepida-L. ku- G-LB has not been clearly assigned in this section; however, the maensis Zone, and 1 from the upper part in the L. kumaensis Zone boundary horizon probably exists somewhere in the black mudstone (Fig. 3). All analyzed samples lacked coarse-grained terrigenous clastic above Unit 8. A preliminary analysis of stable carbon isotopes in car- grains and were totally free of apparent diagenetic features such as bonates was conducted by Zakharov et al. (1997), and a positive ex- dolomitization. cursion of up to 4‰ was recognized. 3.2. Sr isotope analysis 2.2. Senkina Shapka section For Sr isotope measurements, 40–50 mg of handpicked specimens The Sergeevka belt occurs in the southwestern corner of the Sikhote- from each sample was dissolved in 5 ml of 1 M suprapure acetic acid. Sr Alin folded belt (Khanchuk et al., 1996; Khanchuk et al., 2016; Fig. 2C) was extracted in 1 ml microcolumns filled with 100 μl Sr Spec resin in direct contact with the tectonically underlying Jurassic accretionary (ElChrom Industries). The column was rinsed with 3 ml of 3 M HNO3, complex of the Samarka belt to the northeast, which is correlated with a and Sr was eluted with 1 ml of H2O. The separated Sr was loaded on coeval unit in the Mino-Tanba belt in SW Japan (Kojima et al., 2000). single W filaments with a Ta activator. The samples were analyzed with The Sergeevka belt is composed of arc granitoids, a thermal ionization mass spectrometer (TIMS; Finnigan MAT 262) at ophiolite, and Middle-Upper Paleozoic to Mesozoic sedimentary covers. the Faculty of Science, Kumamoto University, with a reproducibility of − The Permian strata of the Sergeevka belt comprise terrigenous clastics 1×10 5. All data were corrected for internal mass bias using associated with shallow marine limestones of continental shelf facies 87Sr/86Sr = 0.1194. The recent average value of the standard NIST SRM (Belyaeva et al., 1997; Izosov, 2002). The fossiliferous (with fusulines, 987 was 87Sr/86Sr = 0.710270 ± 20 (2SD; n = 18). Our laboratory rugose corals, and brachiopods) shallow marine limestones occur blanks were < 500 pg. within the Chandalaz Formation (Horizon), for which biostratigraphic In the and Permian accreted paleo-atoll carbonates in zonation and correlation have been documented by Ueno et al. (2005), Japan, strontium concentrations vary from 300 to 3400 ppm, and Rb/Sr Kotlyar et al. (2006, 2007), and Kossovaya and Kropatcheva (2013). ratios are always very low (< 0.01) (e.g., Fujinuki, 1968). The very low The best-exposed limestone of the Chandalaz Formation is observed Rb/Sr ratios make the measured 87Sr/86Sr ratios of the carbonates close at the Senkina Shapka section in the Partizanskaya River Basin, ca. to the initial ratios during the Permian with a negligible age effect. 40 km to the north of Nakhodka (Fig. 2C). This section exceeds ca. 200 m in thickness and is composed of well-bedded limestone with 4. Results abundant and diverse fusulinids, small foraminifers, bryozoans, corals and brachiopods and rare ammonoids. The basal part of the limestone is Table 1 shows the measurements of the 87Sr/86Sr ratios for 12 sandy, whereas some upper horizons are siliceous and thus hard. carbonate samples from the Iwaizaki and Senki na Shapka sections, and

16 T. Kani et al. Palaeogeography, Palaeoclimatology, Palaeoecology 499 (2018) 13–21

Table 1 Analytical results of 87Sr/86Sr ratio of the Guadalupian (Middle Permian) limestones in Iwaizaki section, Japan and Senkina Shapka section, Russia.

Sample Stage Fusulinids 87Sr/86Sr 2 Sigma

Iwaizaki section s23 Unknown Barren 0.706861 0.000188 s25 Unknown Barren 0.706766 0.000020 s22 Unknown Barren 0.706826 0.000017 s13 Unknown Barren 0.706866 0.000018 s30 Unknown Barren 0.706922 0.000023 s15 Unknown Barren 0.706845 0.000017 IW-115 Unknown Barren 0.706807 0.000017 IW-g Capitanian Lepidolina multiseptata 0.706822 0.000022 IW-67 Capitanian Lepidolina multiseptata 0.706897 0.000017 s35 Capitanian Lepidolina multiseptata 0.706825 0.000022 s55 Capitanian Lepidolina multiseptata 0.706754 0.000007 s60 Capitanian Lepidolina multiseptata 0.706833 0.000012 Senkina Shapka section ssu8 Capitanian Lepidolina kumaensis 0.706871 0.000006 ssm13 Capitanian Lepidolina kumaensis 0.706919 0.000005 ssm11 Capitanian Lepidolina kumaensis 0.707007 0.000005 ssm10 Capitanian Lepidolina kumaensis 0.706923 0.000005 ssm6 Capitanian Lepidolina kumaensis 0.706972 0.000005 ssm3 Capitanian Lepidolina kumaensis 0.706946 0.000005 ssm1 Capitanian Lepidolina kumaensis 0.706944 0.000004

The measurement ratios were normalized to the average value of 0.710248 for standard NIST SRM987 (McArthur et al., 2001).

Fig. 3. Overall and correlation of the Middle-Upper Permian Iwaizaki Limestone and the Chandalaz Formation at the Senkina Shapka. Left: The Iwaizaki Limestone (modified from Kawamura and Machiyama, 1995). Right: The limestone of the Chandalaz Formation at Senkina Shapka section (modified from Ueno et al., 2005). The analyzed parts in this study are shown in rectangles.

Fig. 4 displays their stratigraphic profiles. In the Iwaizaki section, the measured values are restricted to an extremely narrow range from 87 86 0.70675 to 0.70692. Those from the Senkina Shapka section likewise Fig. 4. The secular change in the Sr/ Sr ratios of bulk carbonates from the show a similar range of 0.70687 to 0.70701. These values are regarded Iwaizaki Limestone and the limestone of the Chandalaz Formation. as primary signals because a diagenetic overprint by meteoric water usually drives Sr ratios toward much higher values in general, although upward to the top of Unit 8, as discussed later. At the Senkina Shapka these values are of bulk Sr isotopic ratios. According not only to their section, similar low values were confirmed in the middle and upper extremely low values with respect to the previously reported Phaner- parts of the section, which correspond to the Capitanian Lepidolina- ozoic values but also to their consistency, these values likely record the bearing interval that is ca. 80 m thick (Fig. 3). These results confirmed unique Sr signature of the Permian seawater under which the Iwaizaki that the two sections are fairly correlated with each other not only by and Chandalaz limestones were deposited. but also by Sr isotopic stratigraphy. At the Iwaizaki section, these extremely low Sr ratios were detected from a ca. 50 m-thick interval, i.e., the fusuline-bearing Capitanian Unit 7 and the lower half of Unit 8, and from the overlying barren interval of Unit 8 (Fig. 3). It is noteworthy that the extremely low values continued

17 T. Kani et al. Palaeogeography, Palaeoclimatology, Palaeoecology 499 (2018) 13–21

5. Discussion non‑carbonate setting toward the end of the Permian. As to the Iwaizaki Limestone, the disappearance of the Guadalupian tropical biota did not 5.1. Confirmation of the 87Sr/86Sr minimum from the northeastern margin correspond to a fluctuation in water depth. The tropical large-shelled of Greater South China bivalves, large-tested fusulines (Lepidolina), and rugose corals dis- appeared in a stepwise manner in the topmost Unit 7 and Unit 8–1; The present results confirm that extremely low 87Sr/86Sr values of however, they did not recover when thick-bedded carbonates returned ~0.7069 characterize not only the topmost part of the Iwaizaki in Unit 8–2(Tobita and Isozaki, 2017). These observations indicate that Limestone in NE Japan but also the middle/upper parts of the limestone a significant change in the background environment occurred in the of the Chandalaz Formation in southern Primorye (Fig. 4). Most of these late Capitanian to destroy the pre-existing habitable niches for tropical low Sr isotopic values are from the Lepidolina-bearing intervals of Ca- biota and the depositional settings for carbonate production on the pitanian age, and these values are in general agreement with previous continental shelf. results (87Sr/86Sr values of < 0.7070) reported from the Capitanian In the Senkina Shapka section, the top of the thick Capitanian intervals elsewhere in the world (Denison and Koepnick, 1995; Martin limestone is not exposed; thus, any significant facies change was not and MacDougall, 1995; Jones et al., 1995; Korte et al., 2006; Kani et al., directly observed except for the siliceous nature (e.g., Kotlyar et al., 2008, 2013). The occurrence of a nearly 5 Myr-long interval with such 2006). In the neighboring area near Nakhodka, the overlying Wuchia- extremely low 87Sr/86Sr values is unique in the Phanerozoic (Fig. 1). pingian unit (Lyudyanza Formation) is composed of thick black shales As to the Iwaizaki Limestone in particular, it is noteworthy that the that appear almost identical lithologically to the Toyoma Formation in topmost 20 m-thick unfossiliferous interval records the same low value the South Kitakami belt (Zakharov et al., 1992). The carbonate pro- of approximately 0.7068 as the underlying Lepidolina-bearing interval. duction was aborted once at the end of the Capitanian in southern As the inflection point for the increase in Sr ratios is assigned to the Primorye, as well as in NE Japan. The development of a minor reef (Korte et al., 2006), the present result indicates that the complex during the Lopingian in the Nakhodka area (Zakharov et al., topmost barren interval is no doubt correlated with the Capitanian, 1992) probably suggests the short-term return of a warmer climate after confirming that the G-LB exists not within the Unit 8 of the Iwaizaki the G-LB. Limestone but in a much higher horizon somewhere in Unit 9, i.e., in Such an overall common trend in sedimentary regime shared be- the overlying black shale of the Toyoma Formation. Wuchiapingian tween the South Kitakami and Sergeevka belts suggests a common ammonoids are found in the lower part of the Suenosaki Fm (ca. 800 m episode of losing the Capitanian shallow marine carbonate factory, thick), which is correlated with the lower Toyoma Fm. The G-LB hor- including reef development, at the end of the Capitanian in the izon is probably preserved in the lowest part of the overlying black northern part of the Greater South China block (Fig. 2A). shale of Unit 9, ca. 100–150 m above the top of the Iwaizaki Limestone. Although the base of the Capitanian is estimated somewhere within 5.3. Effect of Capitanian cooling in the northern Greater South China Unit 7 or lower units, nevertheless, this study confirms that the Capi- tanian interval ranges at least 80 m in thickness in the Iwaizaki Lime- This study confirmed that the carbonate production rapidly declined stone, i.e., 35 m in the upper Unit 7 and 45 m in the entire Unit 8. in NE Japan and Primorye immediately before the G-LB timing and As to the Senkina Shapka section, on the other hand, the extremely scarcely recovered during the rest of the Permian, particularly in NE low values of ~0.70690 were detected from a ca. 80 m-thick interval in Japan. In contrast, the carbonate deposition continued throughout the the middle-upper part of the limestone, not only from the Lepidolina- Capitanian and across the G-LB in the main part of South China, which bearing interval but also from the underlying 3 m-thick interval (5 was located in an equatorial domain (Fig. 2A). This difference may samples) of the topmost Parafusulina stricta Zone. Owing to the highly possibly reflect the varying latitude-dependent different reactions of the siliceous nature, we could not acquire any Sr isotope measurements carbonate factory even within a conterminous continental block. In from the uppermost part of the section despite of intense efforts. On the general, the termination of shallow marine carbonates may occur with a basis of the occurrence of the Capitanian fusuline (Lepidolina), none- decrease in the seawater temperature. Two possible causes can be in- theless, we predict that the extremely low Sr isotopic ratios continue all ferred for the late Capitanian temperature decrease, i.e., 1) the ap- the way to the top of the limestone. The present study has documented pearance of global cooling, and 2) the migration of depositional sites to that the Capitanian intervals of the continental shelf facies at the two higher latitudes with cooler climates. sections in NE Japan and southern Primorye have indeed recorded a The Capitanian global cooling was proposed first on the basis of the unique episode of extremely low Sr isotopic values in seawater. unique carbon isotope record in low-latitude paleo-atoll carbonates (12°S) (Isozaki et al., 2007), a signature that was reproduced later in 5.2. The end of tropical biota and carbonate production in the Capitanian other parts of the world, e.g., in Croatia and in South China (Isozaki et al., 2011; Chen and Benton, 2012). In addition, in a global summary The present Sr-isotopic analysis at the Iwaizaki section confirms for of sequence stratigraphy (Haq and Schutter, 2008), the findings of the first time that the disappearance of tropical biota and the collapse of coeval glacial deposits in eastern and in Mongolia (Fielding the carbonate factory indeed occurred during the Capitanian prior to et al., 2008; Fujimoto et al., 2012), the selective extinction of tropical the G-LB. The deposition of reef limestone continued during the earlier fauna (Isozaki and Aljinovic, 2009), the migration of mid-latitude fauna Capitanian to accumulate > 35 m-thick massive limestones (Unit 7), to low latitudes (Shen and Shi, 2002), and the Milankovitch tuning which was followed by the deposition of the ca. 40 m-thick interbedded (Fang et al., 2017), all support the onset of cooling in the Capitanian. limestone/mudstone unit (Unit 8) and the overlying mudstone with The most convincing line of evidence is revealed in the low-latitude extremely rare and thin calcareous lenses. This clear facies change re- paleo-atoll carbonates at Akasaka in Japan, where the top of the Ca- cords the decline of carbonate production, in particular, the dis- pitanian rocks is truncated by a remarkable (Kofukuda appearance of a patch reef on the Capitanian shelf in NE Japan et al., 2014). (Kawamura and Machiyama, 1995; Shen and Kawamura, 2001). Al- Furthermore, the Sitsa flora from the Partizanskaya River Basin near though the G-LB horizon has not been precisely constrained, it is no- Senkina Shapka, considered to be of latest Wordian to Capitanian age teworthy that Upper Permian rocks in the South Kitakami belt are (Burago, 1986; Kotlyar et al., 2006; Zakharov et al., 2009), suggests composed mostly of thick black mudstone with Lopingian ammonoids that the Capitanian climate in southern Primorye was cool-temperate (Toyoma Formation; up to 1500 m thick). The late Capitanian termi- and humid, because this flora yields less frequent Cathasian elements nation not only of tropical biota but also of carbonate production is (only 14–22% instead of 23–34% during -Wordian time) and obvious, suggesting that the shelf domain in NE Japan changed to a instead features more emerging Angarian ones. Despite the claim for a

18 T. Kani et al. Palaeogeography, Palaeoclimatology, Palaeoecology 499 (2018) 13–21

interpretation is not the case for the Capitanian under a cooling trend, however, as evidenced by the observed lowest sea level of the Phanerozoic and by the preferential elimination of tropical fauna. To reconcile this apparent disagreement, Kani et al. (2013) proposed that the appearance of extensive ice coverage over continental blocks might have occurred, and the weathering/erosion of continental crust could have been suppressed to drive a lower riverine flux with high 87Sr/86Sr ratios. Alternatively, an arid weathering regime might have developed extensively under the cool climate, particularly on the vast super- continent Pangea, which also contributed to suppressing the riverine fluxes (Korte et al., 2006). A change in seawater chemical conditions

(pH, pCO2,pO2, etc.) needs to be inspected for an alternative ex- planation for the termination of carbonate deposition. To test whether the biotic crisis occurred earlier in higher latitude domains than in the tropical region during the Capitanian, we need more data from areas at various latitudes.

6. Conclusions

The newly observed 87Sr/86Sr profiles of the Capitanian limestones, i.e., the topmost Iwaizaki Limestone in NE Japan and the middle-upper part of the limestone in the Chandalaz Formation in southern Primorye, show extremely low values of ~0.7069 equivalent to that of the Capitanian minimum. These results clarify the following new aspects of these limestones, i.e., 1) the two sections are correlated chemostrati- graphically as well as litho- and biostratigraphically, confirming that these rockes were deposited in the same setting, probably side-by-side within the northern part of Greater South China, and 2) the dis- appearance of tropical biota and the collapse of the carbonate factory has occurred in NE Japan undoubtedly during the Capitanian im- mediately before the G-LB. Fig. 5. A schematic correlation diagram showing an updated secular change in It is noteworthy that both sections were deposited in a relatively seawater Sr isotope ratios, together with coeval global environmental changes, high latitude domain close to the northern connecting seaway between sea-level changes, and the end-Guadalupian extinction. The measurements of the Tethys and Panthalassa at mid-latitudes. The biotic responses to a 87 86 Sr/ Sr ratios in the Iwaizaki and the Senkina Shapka sections are given with global environmental change in the Capitanian likely appeared much 87 86 respect to the compiled curve for the Permian seawater Sr/ Sr ratio from the earlier in the northern part of Greater South China at higher latitudes Tethyan domain (Korte et al., 2006; Liu et al., 2013; Wang et al., 2004). than in the tropical regions, such as the main part of the South China block. much older age for the Sitsa flora (Zimina, 1997), oxygen-isotopic ra- 18 tios (δ O) of some latest Wordian-Capitanian fossils from the Gizhiga- Acknowledgments Omolon area in northern Far East Russia rose from −2‰ (in late Wordian fossils) to −1‰ (in Capitanian fossils), indicating a gradual We appreciate Prof. Masayuki Ehiro for his valuable suggestions on cooling trend from the late Wordian to the Capitanian (from 20.4 to the Permian rocks in the South Kitakami belt and Hiroki Nakahata and 16.5 °C; Zakharov and Biakov, 2008; Zakharov et al., 2009) and sup- Tomoyo Tobita for their help with fieldwork at Senkina Shapka in porting the abovementioned floristic data. Indeed, the signs of the Primorye and Iwaizaki in NE Japan. The Ministry of Environment, the cooling appeared slightly earlier at high latitudes; the disappearance of Cultural Committee of Miyagi Prefecture, and the Education Panel of carbonates occurred during the middle Capitanian in Greenland and Kesen-numa City kindly provided permission for the present research Spitsbergen (e.g., Beauchamp and Grasby, 2012; Blomeier et al., 2013) on the Iwaizaki Limestone. This study was funded by JSPS KAKENHI (Fig. 5). (Grant-in-Aid, no. 26257212 to and no. 25400490 to TK) and by the On the other hand, in the Senkina Shapka section, at least, the oc- Russian FEB grant 18-2-004 and grant RFBR 18-05-00023. currence of Early Permian Angara (boreal) flora from an underlying unit suggests negating the second option. It seems difficult to blame a References northward latitudinal shift for South China over the northern limit of reef development (ca. 30°N) in the Middle Permian. The end-Middle Beauchamp, B., Grasby, S.E., 2012. Permian lysocline shoaling and ocean acidification Permian extinction was in fact a prolonged but gradual decrease in along NW Pangea led to carbonate eradication and chert expansion. Palaeogeogr. – – diversity from the Wordian to the end of the Capitanian (Clapham et al., Palaeoclimatol. Palaeoecol. 350 352, 73 90. Belyaeva, G.V., Kiseleva, A.V., Nikitina, A.P., 1997. Stage of Late Permian biogenic 2009). The main phase of the extinction appears to have occurred al- buildups in Southern Primorye. In: Baud, A., Popova, I., Dickins, J.M., Zakharov, Y.D. most simultaneously during the Capitanian minimum of Sr isotope re- (Eds.), Late Paleozoic and Early Mesozoic Circum-Pacific Events: Biostratigraphy, Tectonics and Ore Deposites of Primorye (Far East Russia). Memoires de Geologie cords. – fi (Lausanne) Universite de Lausanne 30, pp. 151 154. The present study on Sr isotopes eventually con rms that the car- Blomeier, D.P.G., Dustira, A.M., Forke, H., Scheibner, C., 2013. Facies analysis and de- bonate deposition declined and consequently ceased during the interval positional environments of a storm-dominated, temperate to cold, mixed siliceous- called the “Capitanian minimum” with extremely low 87Sr/86Sr ratios carbonate ramp: the Permian Kapp Starostin formation in NE Svalbard. Nor. J. Geol. 93, 75–98. below 0.7070, at least in the northern part of Greater South China. In Bond, D.P.G., Hilton, J., Wignall, P.B., Ali, J.R., Stevens, L.G., Sun, Y.-D., Lai, X.L., 2010a. 87 86 general, intervals with low seawater Sr/ Sr ratios are interpreted as The Middle Permian (Capitanian) mass extinction on land and in the oceans. Earth indicating high sea levels, with lesser contributions from drowned Sci. Rev. 102, 100–116. Bond, D.P.G., Wignall, P.B., Wang, W., Izon, G., Jiang, H.-S., Lai, X.-L., Sun, Y.-D., continental crust with respect to those from mid-oceanic ridges. This

19 T. Kani et al. Palaeogeography, Palaeoclimatology, Palaeoecology 499 (2018) 13–21

Newton, R.J., Shao, L.-Y., Védrine, S., Cope, H., 2010b. The mid-Capitanian (Middle Izosov, L.A., 2002. Srednepaleozoiskiye formatsii i tektonika Yaponomorskogo regiona Permian) mass extinction and carbon isotope record of South China. Palaeogeogr. (Middle Paleozoic Formations and Tectonics of Japan Sea Region). Dalnauka, Palaeoclimatol. Palaeoecol. 292, 282–294. Vladivostok, pp. 278 (in Russian). Burago, V.I., 1986. On the problem of the boundary between Angarian and Cathaysian Jin, Y.G., Zhang, J., Shang, Q.H., 1994. Two phases of the end-Permian mass extinction. vegetable kingdoms. In: Zakharov, Y.D., Onoprienko, Y.I. (Eds.), Permo-triasovye In: Embry, A.F., Beauchamp, B., Glass, D.J. (Eds.), Pangea: Global Environments and sobytiya v razvitii organicheskogo mira Cevero-Vostochnoj Azii (Permian-Triassic Resources. Memoir, Canadian Soc. Petrol. Geologists 17pp. 813–822. Events During the Evolution of North-East Asia Biota). Dalnevostochnoye Otdeleniye Jones, C.E., Halliday, A.N., Lohman, K.C., 1995. The impact of diagenesis on high-pre- Akademii nauk SSSR, Vladivostok, pp. 6–23 (in Russian). cision U-Pb dating of ancient carbonates: an example from the Late Permian of New Burke, W.H., Denison, R.E., Hetherington, E.A., Koepnick, R.B., Nelson, H.F., Otto, J.B., Mexico. Earth Planet. Sci. Lett. 134, 409–423. 1982. Variation of seawater 87Sr/86Sr throughout Phanerozoic time. Geology 10, Kani, T., Fukui, M., Isozaki, Y., Nohda, S., 2008. The Paleozoic minimum of 87Sr/86Sr 516–519. initial ratio in the upper Guadalupian (Permian) mid-oceanic carbonates: a critical Chen, Z.Q., Benton, M.J., 2012. The timing and pattern of biotic recovery following the turning point in the Late Paleozoic. J. Asian Earth Sci. 32, 22–33. end-Permian mass extinction. Nat. Geosci. 5, 375–383. Kani, T., Hisanabe, C., Isozaki, Y., 2013. The Capitanian (Permian) minimum of 87Sr/86Sr Choi, D.R., 1976. Distribution of the Upper Permian fusulinids with relation to limestone ratio in the mid-Panthalassan paleo-atoll carbonates and its demise by the degla- lithofacies in the southern Kitakami Mountains, N. E. Japan. Jour. Geol. Soc. Japan ciation and continental doming. Res. 24, 212–221. 82, 113–125. Kawamura, T., Machiyama, H., 1995. A Late Permian reef complex, South Kitakami Clapham, M.E., Shen, S., Bottjer, D.J., 2009. The double mass extinction revisited: re- terrane, Japan. Sediment. Geol. 99, 135–150. assessing the severity, selectivity, and causes of the end-Guadalupian biotic crisis Kawamura, M., Kato, M., Kitakami Paleozoic Research , 1990. Southern Kitakami (Late Permian). Paleobiology 35, 32–50. Terrane. In: Ichikawa, K., Mizutani, S., Hara, I., Hada, S., Yao, A. (Eds.), Pre- Denison, R.E., Koepnick, R.B., 1995. Variation in 87Sr/86Sr of Permian seawater: an Terranes of Japan 249–266. Nihon-insatsu, Osaka. overview. In: Scholle, P.A., Peryt, T.M., Ulmer-Scholle, D.S. (Eds.), The Permian of Kemkin, I.V., 2012. Microfaunal biostratigraphy and structural framework of the Northern Pangea Vol. I: Paleogeography, Paleoclimates, Stratigraphy. Springer- Nadanhada-Bikin terrane within a Jurassic accretionary prism of the Sikhote-Alin Verlag, New York, pp. 124–132. Fold Belt, eastern Russia. J. Asian Earth Sci. 61, 88–101. Denison, R.E., Koepnick, R.B., Burke, W.H., Hetherington, E.A., Fletcher, A., 1994. Khanchuk, A.I., Ratkin, V.V., Ryazantseva, M.D., Golozubov, V.V., Gonokhova, N.G., Construction of the and Permian seawater 87Sr/86Sr curve. Chem. Geol. 1996. Geology and Mineral Resources of Primoye Krai (Territory): An Outline. Far 112, 145–167. Eastern Geological Institute, Russian Academy of Science, Vladivostok, pp. 61 (in Ehiro, M., 1997. Ammonoid palaeobiogeography of the South Kitakami Palaeoland and Russian). palaeogeographu of wastern Asia during Permian to Triassic time. In: Jin, Y.G., Khanchuk, A.I., Kemkin, I.V., Kruk, N.N., 2016. The Sikhote-Alin orogenic belt, Russian Dineley, D. (Eds.), Palaeontology and (Proceedings of the 30th south east: terranes and the formation of continental lithosphere based on geological International Geological Congress, Vol. 12). VSP, Utrecht, pp. 18–28. and isotopic data. J. Asian Earth Sci. 120, 117–138. Ehiro, M., 2001. Origins and drift histories of some microcontinents distributed in the Kirschvink, J.L., Isozaki, Y., Shibuya, H., Otofuji, Y.T., Raub, D., Hilburn, I.A., Kasuya, T., eastern margin of Asian continent. Earth Sci. (Chikyu-Kagaku) 55, 71–81. Yokoyama, M., Bonifacie, M., 2015. Challenging the sensitivity limits of paleo- Ehiro, M., 2006. A new of Stacheoceras (Permian ammonoid) from the upper magnetism: Magnetostratigraphy of weakly magnetized Guadalupian-Lopingian Permian in the South Kitakami Belt, Northeast Japan. Paleontological Res. 10, (Permian) limestone from Kyushu, Japan. Palaeogeogr. Palaeoclimatol. Palaeoecol. 261–264. 418, 75–89. Ehiro, M., Bando, Y., 1985. Late Permian ammonoids from the southern Kitakami Massif, Kofukuda, D., Isozaki, Y., Igo, H., 2014. A remarkable sea-level drop across the Northeast Japan. Trans. Proc. Paloent. Soc. Japan, NS 137, 25–49. Guadalupian–Lopingian (Permian) boundary in low-latitude mid-Panthalassa: irre- Erwin, D.H., 2006. Extinction. Princeton University Press, New York, pp. 296. versible changes recorded in accreted paleo-atoll limestones in Akasaka and Fang, Q., Wu, H.C., Hinnov, L.A., Jing, X.C., Wang, X.L., Yang, T.S., Li, H.Y., Zhang, S.H., Ishiyama, Japan. J. Asian Earth Sci. 82, 47–65. 2017. Astronomical cycles of Middle Permian Maokou Formation in South China and Kojima, S., Kemkin, I.G., Kametaka, M., Ando, A., 2000. A correlation of accretionary their implications for sequence stratigraphy and paleoclimate. Palaeogeogr. complexes of southern Sikhote-Alin of Russia and the inner zone of Southwest Japan. Palaeoclimatol. Palaeoecol. 474, 130–139. Geosci. J. 4, 175–185. Resolving the Late Paleozoic in time and space. In: Fielding, C.R., Frank, T.D., Korte, C., Kozur, H.W., Bruckschen, P., Vizer, J., 2003. Strontium isotope evolution of Isbell, J.L. (Eds.), Geol. Soc. America Special Pub. 441. pp. 354. Late Permian and Triassic seawater. Geochim. Cosmochim. Acta 67, 47–62. Fujimoto, T., Otoh, S., Orihashi, Y., Hirata, T., Yokoyama, T., Shimojo, S., Kouchi, Y., Korte, C., Jasper, T., Kozur, H.W., Veizer, J., 2006. 87Sr/86Sr record of Permian seawater. Obara, H., Ishizaki, Y., Tsukada, K., Kurihara, T., Nuramkhan, M., Gonchigdorj, S., Palaeogeogr. Palaeoclimatol. Palaeoecol. 240, 89–107. 2012. Permian Peri-glacial deposits from Central Mongolia in central Asian Orogenic Kossovaya, O.L., Kropatcheva, G.S., 2013. Extinction of Guadalupian rugose corals: an Belt: a possible indicator of the Capitanian cooling event. Resour. Geol. 62, 408–422. example of biotic response to the Kamura event (southern Primorye, Russia). In: Fujinuki, T., 1968. Geochemical study of limestone (1) - on the minor elements in the Gasiewicz, A., Słowakiewicz, M. (Eds.), Palaeozoic Climate Cycles: Their Akasaka limestone. Report Geol. Surv. Japan 19, 603–624 (in Japanese with English Evolutionary and Sedimentological Impact. Geological Society, London, Special Pub abstract). 376. pp. 407–429. Haq, B.U., Schutter, S.R., 2008. A chronology of Paleozoic sea-level changes. Science 322, Kotlyar, G.V., Belyansky, G.C., Burago, V.I., Nikitina, A.P., Zakharov, Y.D., Zhuravlev, 64–68. A.V., 2006. South Primorye, Far East Russia – a key region for global Permian cor- Ishiwatari, A., 1991. Ophiolites in the Japanese Islands: typical segment of the circum- relation. J. Asian Earth Sci. 26, 280–293. Pacific multiple ophiolite belts. Episodes 14, 274–279. Kotlyar, G.V., Shen, S.Z., Kossovaya, O.L., Zhuravlev, A.V., 2007. Middle Permian Isozaki, Y., 2009. Integrated plume winter scenario for the double-phased extinction (Guadalupian) biostratigraphy in South Primorye, Russian Far East and correlation during the Paleozoic-Mesozoic transition: the G-LB and P-TB events from a with Northern China. Palaeoworld 16, 173–189. Panthalassan perspective. J. Asian Earth Sci. 36, 459–480. Liu, X.-C., Wang, W., Shen, S.-Z., Gorgij, M.N., Ye, F.-C., Zhang, Y.-C., Furuyama, S., Kano, Isozaki, Y., Aljinovic, D., 2009. Extinction of the Permian large bivalve Alatoconchidae: A., Chen, X.-Z., 2013. Late Guadalupian to Lopingian (Permian) carbon and strontium end of gigantism in tropical seas at the end-Guadalupian. Palaeogeogr. isotopic chemostratigraphy in the Abadeh section, central Iran. Gondwana Res. 24, Palaeoclimatol. Palaeoecol. 284, 11–21. 222–232. Isozaki, Y., Kase, T., 2014. The occurrence of a large gastropod “” yokoyami Martin, E.E., Macdougall, J.D., 1995. Sr and Nd isotopes at the Permian/Triassic Hayasaka from the Capitanian (Permian) Iwaizaki Limestone in Northeast Japan. boundary: a record of climate change. Chem. Geol. 125, 73–99. Paleontological Res. 18, 1–8. McArthur, J.M., Howarth, R.J., Bailey, T.R., 2001. Strontium isotope stratigraphy: Isozaki, Y., Ota, A., 2001. Middle/Upper Permian (Maokouan/Wuchapingian) boundary LOWESS version 3: best fit to the marine Sr-isotope curve for 0–509 Ma and ac- in mid-oceanic paleo-atoll limestone in Kamura and Akasaka. Japan. Proc. Japan companying look-up table for deriving numerical age. J. Geol. 109, 155–170. Acad. 77B, 104–109. McArthur, J.M., Howarth, R.J., Shields, G.A., 2012. Strontium isotope stratigraphy. In: Isozaki, Y., Kawahata, H., Ota, A., 2007. A unique carbon isotope record across the Gradstein, F.M., Ogg, J.G., Schmitz, M.D., Ogg, G.M. (Eds.), The . Guadalupian-Lopingian (Middle-Upper Permian) boundary in mid-oceanic paleoatoll Elsevier, pp. 127–144. carbonates: the high-productivity “Kamura event” and its collapse in Panthalassa. Morikawa, R., 1960. Fusulinids From the Iwaizaki Limestone. Science Report of Saitama Glob. Planet. Chang. 55, 21–38. University Series B 3. pp. 273–299. Isozaki, Y., Aoki, K., Nakama, T., Yanai, S., 2010. New insight into a subduction-related Morikawa, R., Sato, T., Shibazaki, T., Shinada, Y., Okubo, M., Nakazawa, K., Horiguchi, orogen: reappraisal on geotectonic framework and evolution of the Japanese Islands. M., Murata, M., Kikuchi, Y., Taguchi, Y., Takahashi, K., 1958. Stratigraphy and Gondwana Res. 18, 82–105. biostratigraphy of the “Iwaizaki Limestone” in the Southern Kitakami mountainland. Isozaki, Y., Aljinović, D., Kawahata, H., 2011. The Guadalupian (Permian) Kamura event In: Jubilee Publication in the Commemoration of Professor H. Fujimoto 60th in European Tethys. Palaeogeogr. Palaeoclimatol. Palaeoecol. 308, 12–21. Birthday. Kokusai-bunken-insatsu Co., Tokyo, pp. 81–90. Isozaki, Y., Aoki, K., Sakata, S., Hirata, T., 2014. The eastern extension of Paleozoic South Murata, M., Shimoyama, S., 1979. Stratigraphy near the Perminan-Triassic boundary and China in NE Japan evidenced by detrital zircon. GFF 136, 123–126. the pre-Trassic unconformity in the Kitakami massif, Northeast Japan. Kumamoto Isozaki, Y., Ehiro, M., Nakahata, H., Aoki, K., Sakata, S., Hirata, T., 2015. Cambrian arc Jour. Sci., Earth Sci. 11, 11–31. plutonism in Northeast Japan and its significance in East Asia: new U-Pb zircon ages Nevolin, P.L., Utkin, V.P., Mitrokhin, A.N., 2010. The Tafuinsky Granite Massif, southern of the oldest granitoids in the Kitakami and Ou Mountains. J. Asian Earth Sci. 108, Primorye region: the structures and geodynamics of longitudinal compression. 136–149. Russian Jour. Pac. Geol. 4, 331–346. Isozaki, Y., Nakahata, H., Zakharov, Y.D., Popov, A.M., Sakata, S., Hirata, T., 2017. Niko, S., 2015. Yokoyamapora mabuti, a new species of tabulate coral from the Permian Greater South China extended to the Khanka block: detrital zircon geochronology of Iwaizaki Limestonem Miyagi prefecture, Japan. Bulletin National Mus. Nature middle-upper Paleozoic sandstones in Primorye, Far East Russia. J. Asian Earth Sci. Science ser. C 41, 25–28. 145, 565–575. Okawa, H., Shimojo, M., Orihashi, Y., Yamamoto, K., Hirata, T., Sano, S., Ishizaki, Y.,

20 T. Kani et al. Palaeogeography, Palaeoclimatology, Palaeoecology 499 (2018) 13–21

Kouchi, Y., Yanai, S., Otoh, S., 2013. Detrital zircon geochronology of the - Permian) Metadoliolina dutkevitchi-Monodiexiodina sutchanica Zone of the Senkina Lower Carboniferous continuous succession of the South Kitakami Belt, Northeast Shapka section, South Primorye, Far East Russia. Alcheringa 29, 257–273. Japan. Memoir Fukui Mus. 12, 35–78. Veizer, J., 1989. Strontium isotopes in seawater through time. Annu. Rev. Earth Planet. Popp, B.N., Anderson, T.F., Sandberg, P.A., 1986. Brachiopods as indicators of original Sci. 17, 141–167. isotopic compositions in some Paleozoic limestones. Geol. Soc. Am. Bull. 97, Veizer, J., Ala, D., Azmy, K., Bruckschen, P., Buhl, D., Bruhn, F., Carden, G.A.F., Diener, 1262–1269. A., Ebneth, S., Godderis, Y., Jasper, T., Korte, C., Pawellek, F., Podlaha, O.G., Strauss, Scotese, C.R., 2008. PALEOMAP project. http://www.scotese.com. H., 1999. 87Sr/86Sr, d13C and d18O evolution of Phaenrozoic seawater. Chem. Geol. Shen, J.W., Kawamura, T., 2001. Guadalupian algal- reefs in siliciclastic en- 161, 59–88. vironments – the reefs at Lengwu (South China) compared with the reef at Iwaizaki Wang, W., Cao, C.Q., Wang, Y., 2004. The carbon isotope excursion on GSSP candidate (Japan). Facies 45, 137–156. section of Lopingian-Guadalupian boundary. Earth Planet. Sci. Lett. 220, 57–67. Shen, S.Z., Shi, G.R., 2002. Paleobiogeographical extinction patterns of Permian bra- Zakharov, Y.D., Biakov, A.S., 2008. Carbon-isotope of organic carbonates of the Late chiopods in the Asian-western Pacific region. Paleobiology 28, 449–463. Paleozoic and Early Mesozoic. In: Markevich, P.V., Zakharov, Y.D. (Eds.), Trias I yura Stanley, S.M., Yang, X., 1994. A double mass extinction at the end of the Paleozoic era. Sikhote-Alinya. 2. Vulkanogenno-osadochnyj complex, paleobiogejgraphiya (Triassic Science 266, 1340–1344. and Jurassic of the Sikhote-Alin. 2. Volcano-Sedimtary Assemblage, Tamaki, K., 1988. Geological structure of the Japan Sea and its tectonic implications. Bull. Paleobiogeography). Dalnauka, Vladivostok, pp. 226–232 (in Russian). Geol. Surv. Jpn 39, 269–365. Zakharov, Y.D., Panchenko, I.V., Khanchuku, A.I., 1992. A Field Guide to the Late Tazawa, J., 1991. Middle Permian biogeography of Japan and adjacent re- Paleozoic and Early Mesozoic Circum-Pacific Bio- and Geological Events. Far-Eastern gions in East Asia. In: Ishii, K., Liu, X., Ichikawa, K., Huang, B.H. (Eds.), Pre-Jurassic Geological Institute, Russ. Acad. Sci., Far Eastern Branch, Vladivostok (88p.). Geology of Inner Mongolia, China. Report of China-Japan Cooperative Research Zakharov, Y.D., Ukhaneva, N.G., Kiseleva, A.V., Kotlyar, G.V., Nikitina, A.P., Tazawa, J., Group 1987–1989. Matsuya Insatsu, Osaka, pp. 213–230. Gvozdzev, V.I., Ignatyev, A.V., Cherbadzhi, A.K., 1997. Geochemical signals as gui- Tobita, T., Isozaki, Y., 2017. Reef Collapse in the mid-Capitanian Near the Northern dance for definition of the Middle–Upper Permian boundary in the South Kitakami Connection Channel Between the Tethys and Panthalassa: Lithostratigraphy of the (Japan) and Primorye Region (Russia). In: Dheerradilok, P., Hinthong, C., Topmost Iwaizaki Limestone (Capitanian) in NE Japan Geological Society of America Chaodumrong, P. (Eds.), Proceedings of the International Conference on Stratigraphy Abstr. with Programs. 49. pp. 6. and Tectonic Evolution of Southeast Asia and the South Pacific. vol. 1. Dep. of Tsutsumi, Y., Yokoyama, K., Kasatkin, S.A., Golozoubov, V.V., 2014. Zircon U-Pb age of Mineral Res., Bangkok, Thailand, pp. 88–100. granitoids in the Maizuru belt, southwest Japan and the southernmost Khanka massif, Zakharov, Y.D., Sha, J., Popov, A.M., et al., 2009. Permian to earliest cretaceous climatic Far East Russia. J. Mineral. Petrol. Sci. 109, 97–102. oscillations in the eastern Asian continental margin (Sikhote-Alin area), as indicated Tsutsumi, Y., Yokoyama, K., Kasatkin, S.A., Golozoubov, V.V., 2016. Ages of igneous by fossils and isotope data. GFF 131, 25–47. rocks in southern Primorye, Far East Russia. Memoir National Museum Natural Sci. Zimina, V.G., 1997. Sitsa Flora from the Permian of South Primorye. In: Dickins, J.M. 51, 71–78. (Ed.), Late Palaeozoic and Early Mesozoic Circum-Pacific Events and their Global Ueno, K., Shi, G.R., Shen, S.Z., 2005. Fusulinoideans from the early Midian (late Middle Correlation. Cambridge University Press, Cambridge, pp. 66–86.

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