research paper the capitanian (permian) kamura …...palaeoworld 16 (2007) 16–30 research paper...

Palaeoworld 16 (2007) 16–30

Research paper

The Capitanian (Permian) Kamura cooling event:The beginning of the Paleozoic–Mesozoic transition

Yukio Isozaki a,∗, Hodaka Kawahata b, Kayo Minoshima c

a Department of Earth Science and Astronomy, The University of Tokyo, Komaba, Meguro, Tokyo 153-8902, Japanb Graduate School of Frontier Sciences and Ocean Research Institute, The University of Tokyo, Minamidai, Nakano, Tokyo 164-8639, Japan

c Geological Survey of Japan, AIST, Tsukuba 305-8567, Japan

Received 4 January 2007; received in revised form 12 May 2007; accepted 15 May 2007Available online 25 May 2007

Abstract

The Capitanian (late Guadalupian) high positive plateau interval of carbonate carbon isotope ratio (�13Ccarb) was recognizedlately in a mid-Panthalassan paleo-atoll limestone in Japan as the Kamura event. This unique episode in the late-middle Permianindicates high productivity in the low-latitude superocean likely coupled with resultant global cooling. This event ended shortlybefore the Guadalupian–Lopingian (middle-late Permian) boundary (ca. 260 Ma); however, its onset time has not been ascertainedpreviously. Through a further analysis of the Wordian (middle Guadalupian) to lower Capitanian interval in the same limestone atKamura in Kyushu, we have found that the �13Ccarb values started to rise over +4.5‰ and reached the maximum of +7.0‰ within theYabeina (fusuline) Zone of the early-middle Capitanian. Thus the total duration of the Kamura event is estimated over 3–4 millionyears, given the whole Capitanian ranging for 5.4 million years. This 3–4 million years long unique cooling event occurred clearlyafter the Gondwana glaciation period (late Carboniferous to early Permian) in the middle of the long-term warming trend towardthe Mesozoic. This cooling may have been a direct cause of the end-Guadalupian extinction of low-latitude, warm-water adaptedfauna including the large fusulines (Verbeekinidae), gigantic bivalves (Alatoconchidae), and rugose corals (Waagenophyllidae). TheKamura event marks the first sharp excursion of �13Ccarb values in the volatile fluctuation interval that lasted for nearly 20 millionyears from the late-Middle Permian until the early-Middle Triassic. This interval with high volatility in �13C values represents
carb
the transition of major climate mode from the late Paleozoic icehouse to the Mesozoic–Cenozoic greenhouse regime. The end-Paleozoic double-phased extinction occurred within this interval and the Capitanian Kamura event is regarded as the prelude to thistransition.© 2007 Nanjing Institute of Geology and Palaeontology, CAS. Published by Elsevier Ltd. All rights reserved.

ndary; E
Keywords: Guadalupian; C isotope; Panthalassa; Permo-Triassic bou
1. Introduction

The terminal Paleozoic mass extinction represents thegreatest in magnitude throughout the Phanerozoic life

∗ Corresponding author. Tel.: +81 3 5454 6608;fax: +81 3 3465 3925.

E-mail address: [email protected] (Y. Isozaki).

1871-174X/$ – see front matter © 2007 Nanjing Institute of Geology and Paldoi:10.1016/j.palwor.2007.05.011

xtinction; Productivity

history (e.g., Erwin, 1993, 2006); however, it was notlong time ago when its double-phased nature becamewidely recognized. Jin et al. (1994) and Stanley andYang (1994) first pointed out that the Permian biodi-versity declined in two steps separated clearly from each
other; i.e., first at the Middle-Late Permian boundary(=Guadalupian–Lopingian boundary; G–LB) and sec-ond at the Permo-Triassic boundary (P–TB) sensu stricto(or Changhsingian–Induan boundary).
aeontology, CAS. Published by Elsevier Ltd. All rights reserved.

mailto:[email protected]

dx.doi.org/10.1016/j.palwor.2007.05.011

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Y. Isozaki et al. / Pal

In contrast to the P–TB issue, not much attentionas been paid to the G–LB event; however, the signif-cance of the G–LB event was re-emphasized from aifferent aspect relevant to the superocean Panthalassa.he timing of the end-Guadalupian extinction apparentlyoincides with the onset of the superanoxia in Pantha-assa, i.e., another global scale geologic phenomenoncross the P–TB (Isozaki, 1997a, 2007). In addition tohe faunal turnover in mid-oceanic plankton (radiolari-ns) detected in deep-sea chert, shallow marine sessileenthos (fusulines) also sharply declined in diversitycross the G–LB in mid-Panthalassan paleo-atoll com-lex (Isozaki and Ota, 2001; Ota and Isozaki, 2006).hese positively suggest the global nature of the G–LBxtinction and causal environmental change.

The mid-oceanic paleo-atoll carbonates also recordedecular change in stable carbon isotope composition.

usashi et al. (2001, 2007) and Isozaki et al. (2007)rst documented the secular change in carbonate carbon

sotopic ratio (�13Ccarb) of mid-Panthalassa across the–TB and the G–LB, respectively. Besides the bound-ry negative shifts both at P–TB and G–LB properlyredicted from previous studies (e.g., Baud et al., 1989;olser et al., 1989; Wang et al., 2004), a unique highroductivity interval in the Capitanian (late Guadalu-ian) was newly detected on the basis of the appreciableength of high positive �13Ccarb (between +5 and +6‰)nterval (Isozaki et al., 2007; Fig. 1). As such high posi-ive values over +5.0‰ are quite rare in the Phanerozoicecord except for several unique events in the Paleo-oic (e.g., Veizer et al., 1999; Saltzman, 2005), theyamed this Capitanian episode the “Kamura event”,mphasizing its significance of global cooling and rele-ant extinction of large fusulines and gigantic bivalvesn low-latitude Panthalassa (Isozaki et al., 2007). Inhe fusuline-tuned section, the waning history of theamura event was clearly documented in high reso-

ution, whereas the earlier history including the onsetiming was not yet revealed, owing to the absence of con-inuous exposure in the previously studied section. Thiseft a big chasm in our understanding of the major envi-onmental change in the late Guadalupian, in particularhe cause and processes of the Kamura cooling event.

This study aimed to clarify the earlier stage of theamura event, particularly focusing on the onset tim-

ng, and to bracket the total duration of the event. Inhe same Kamura area in Kyushu, Japan, we analyzed13C chemostratigraphy of two other sections that
carbxpose much lower parts of the Guadalupian (Wordiano lower Capitanian) mid-oceanic paleo-atoll carbon-tes. This article reports the �13Ccarb measurements andiscusses their implications to the Capitanian environ-
ld 16 (2007) 16–30 17

mental change and relevant extinction event. A particularemphasis is given to the Kamura event in the contextof a long-term change in environmental regime duringthe nearly 20 million years of the Paleozoic–Mesozoictransition.

2. Geologic setting

The Permian and Triassic limestone at Kamura(Takachiho town, Miyazaki prefecture; Fig. 2) in Kyushuforms a part of an ancient mid-oceanic atoll complexprimarily developed on a mid-oceanic paleo-seamount(Sano and Nakashima, 1997; Isozaki and Ota, 2001; Otaand Isozaki, 2006). This limestone, like many other Per-mian limestones in Japan, occurs as an allochthonousblock incorporated in the Middle-Upper Jurassic disor-ganized mudstone/sandstone of the Jurassic accretionarycomplex in the Chichibu belt (the tectonic outlier of theMino-Tanba belt; Isozaki, 1997b). The limestone blocksin the Kamura area retain parts of the primary mid-oceanic stratigraphy that ranges in age from the Wordian(middle Guadalupian) to Norian (Late Triassic) with sev-eral sedimentary breaks in the Triassic part (Kambe,1963; Kanmera and Nakazawa, 1973; Watanabe et al.,1979; Koike, 1996; Ota and Isozaki, 2006).

The Permian part consists of bioclastic limestone witha typical Tethyan shallow marine fauna that includesvarious fusulines, smaller foraminifera, large-shelledbivalves, gastropods, brachiopods, rugose corals, andcalcareous algae. The Permian rocks are stratigraphi-cally divided into the Guadalupian Iwato Formation (ca.70 m thick) and the overlying Lopingian Mitai Formation(ca. 30 m thick). Fusulines are the most abundant, andthey provide a basis for subdividing the Iwato Formationinto four biostratigraphic units; i.e., the NeoschwagerinaZone, Yabeina Zone, Lepidolina Zone, and a barren inter-val, in ascending order (Ota and Isozaki, 2006; Isozakiand Igo, in preparation). The overlying Lopingian MitaiFormation is subdivided into two fusuline zones, i.e.,the Codonofusiella-Reichelina Zone and PalaeofusulinaZone (Kanmera and Nakazawa, 1973; Ota and Isozaki,2006). All these fusuline assemblages and associatedfossils (rugose corals and large-shelled bivalves of Fam-ily Alatoconchidae; Isozaki, 2006) indicate that theseamount was located in a low-latitude warm-waterdomain in the superocean Panthalassa under a tropicalclimate.

The Neoschwagerina Zone is correlated with the
Wordian (middle Guadalupian) of Texas and with theMurgabian in Transcaucasia (Leven, 1996; Wilde et al.,1999), while the Yabeina Zone, Lepidolina Zone, andmost of the barren interval are correlated with the Capi-

18 Y. Isozaki et al. / Palaeoworld 16 (2007) 16–30

Fig. 1. Schematic diagram showing the late Guadalupian Kamura event documented by high positive �13Ccarb values at Kamura in Japan (modifiedfrom Isozaki et al., 2007) (A), and the composite Permian secular curve of �13Ccarb values modified from Korte et al. (2005) (B). Road: Roadian,Wor: Wordian. Note that the Guadalupian large fusuline and bivalve fauna became extinct in the middle of the Kamura cooling event, whereasthe post-extinction radiation of the Lopingian small fusulines started during the subsequent warming period. In contrast to the waning history ofthe Kamura event, its onset timing and processes were unknown previously. In (B), two possible paths (broken lines) for the Guadalupian secularchange of �13Ccarb values were shown by Korte et al. (2005); the lower for the Tethyan domain, the upper for the Delaware basin in Texas. TheCapitanian Kamura event recorded much higher positive �13Ccarb values between +5.0 and +7.0‰ in Kamura, suggesting the positive excursion ofglobal context in the late Guadalupian. See text and Figs. 4 and 5 for details.

Y. Isozaki et al. / Palaeoworld 16 (2007) 16–30 19

Fig. 2. Index map and stratigraphic columns of the three studied sections in the Kamura area, Kyushu. Not to scale. The present chemostratigraphicresearch focused on the Wordian and lower Capitanian parts of the Iwato Formation exposed in Sections 1 and 3. Refer to Ota and Isozaki (2006)and Isozaki et al. (2007) for more details of the area and Section 2. Loping.: Lopingian; Wuch.: Wuchiapingian; C-R: Codonofusiella-Reichelina.

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20 Y. Isozaki et al. / Pal
tanian (upper Guadalupian) of Texas and with Midianin Transcaucasia (Ota and Isozaki, 2006). The strati-graphic relationship between the Yabeina Zone andthe Lepidolina Zone has long been controversial (e.g.,Toriyama, 1967; Ishii, 1990), however, our recent studyclarified that the former stratigraphically underlies thelatter within the Iwato Formation (Isozaki and Igo, inpreparation). The Codonofusiella-Reichelina Zone cor-responds to the Wuchiapingian (Lower Lopingian) inSouth China. For details of fusuline biostratigraphy andage assignment, see Ota and Isozaki (2006) and Isozaki(2006).

The Iwato Formation is exposed in three sections inKamura; i.e., Sections 1–3 from the east to the west(Fig. 2). Section 2 (32◦44′58′′N, 131◦20′02′′E; Fig. 2)at south of Shioinouso displays a continuous outcropof the upper Iwato Formation and the lower Mitai For-mation that spans across the G–LB (Ota and Isozaki,2006). In this section, a unique high positive plateauin the Lepidolina Zone/barren interval and the follow-ing sharp negative shift in �13Ccarb were documented(Isozaki et al., 2007).

In the present study, we analyzed two additional sec-tions in the Kamura area that expose the lower part ofthe Iwato Formation; i.e., Sections 1 and 3 (Kambe,1963; Murata et al., 2003; Isozaki, 2006; Fig. 2). Sec-tion 1 (32◦45′12′′N, 131◦20′55′′E) to the southeast ofSaraito village is composed of 57 m-thick limestone thatbelongs to the Neoschwagerina Zone and Yabeina Zone,whereas Section 3 (32◦45′05′′N, 131◦19′52′′E) to thenortheast of Hijirikawa is 8 m thick and entirely belongsto the Yabeina Zone (Fig. 2). Detailed biostratigraphy ofthese two sections is under scrutiny and results will bepublished elsewhere (Isozaki and Igo, in preparation).

Among the three sections in Kamura, Section 1 rep-resents the stratigraphical lowest, whereas Section 2 thehighest (Fig. 2). A slight stratigraphic gap may existbetween Sections 2 and 3; however, the similarity inlithofacies suggests that the possible gaps are consid-erably small, if at all. The same fauna and lithofacies inSections 1 and 3 likewise indicate that a possible gap ismuch smaller or even absent.

3. Samples and analytical methods

We collected dark gray to black limestone specimensof the Guadalupian Iwato Formation for stable carbonand oxygen isotope measurements at 34 horizons; i.e.,
21 from Section 1 and 13 from Section 3. Rocks of thetwo sections are unmetamorphosed and mostly fresh,and those with strong weathering and with many calciteveins were screened out in the field and in the labora-
ld 16 (2007) 16–30

tory under the microscope. The black limestone of theIwato Formation has TOC around 0.1 wt% (Isozaki etal., 2007).

The micritic part of wackestone from each horizonwas milled by microdrill after examining under themicroscope. Approximately 100 �m of the aliquotsamples were reacted with 100% H3PO4 at 90 ◦Cin an automated carbonate device (Multiprep) cou-pled with a Micromass Optima mass spectrometerat the Geological Survey of Japan, AIST. Here,�13C = [((13C/12Csample)/(13C/12Cstandard)) − 1] × 1000,and �18O = [((18O/16Osample)/(18O/16Ostandard)) − 1] ×1000. All isotopic data are reported as per mil (‰)relative to Vienna Pee Dee belemnite (V-PDB) standard.The internal precision was 0.03‰ and 0.04‰ (1�)for �13C and �18O, respectively, based on replicatemeasurements of 23 consecutive samples of the NBS-19calcite standard (Suzuki et al., 2000).

4. Results

Table 1 lists all the measurements of �13Ccarb and�18Ocarb of 47 samples from 34 horizons from Sections1 and 3 in Kamura. Figs. 3 and 4 show secular changesin �13Ccarb values plotted on the stratigraphic columnsof Sections 1 and 3, respectively. All �13Ccarb valuesshowed a wide range from +3.55 to +6.97‰, whereas�18Ocarb values fluctuated between −7.58 to −12.36‰,which might be partly due to a slight diagenetic alter-ation, however, the correlation between �13Ccarb and�18Ocarb indicates that they behaved independently. Thuswe consider that the �13Ccarb values were not likelyaffected by secondary alteration but reflect the primaryisotopic composition of the inorganic carbon reser-voir in ancient seawater, in which the carbonates weredeposited.

At Section 1, the �13Ccarb values range between +3.5and +5.2‰. This section is divided into two parts in termsof �13Ccarb values; i.e., segment Sr-1 (NeoschwagerinaZone; 32 m) and the overlying segment Sr-2 (YabeinaZone; 3.5 m) (Fig. 3). In the segment Sr-1, the �13Ccarbvalues gradually and steadily increased from +3.5 to+4.3‰. On the other hand in the segment Sr-2, the�13Ccarb values fluctuated between +4.4 and +5.2‰.Although the boundary between the segments Sr-1 andSr-2 is covered, a general trend of increasing �13Ccarbvalues can be recognized in Section 1. The sample SrB35in the segment Sr-2 marked the lowest horizon of high
positive �13Ccarb values over +5.0‰ in the Iwato For-mation.
At Section 3, the �13Ccarb values range between+5.0 and +7.0‰. This section is chemostratigraphi-

Y. Isozaki et al. / Palaeowor

Table 1Analytical results of �13Ccarb and �18Ocarb normalized to the ViennaPee Dee belemnite of the Guadalupian Iwato Formation in the Kamuraarea, Kyushu

Sample Horizon (m) �13Ccarb (‰) �18Ocarb (‰)

Section 3 (Hijirikawa)Yabeina Zone (13 horizons)

Hj-0.5 7.50 5.332 −10.001Hj0 6.75 5.817 −8.480Hj1 6.15 5.425 −8.366Hj1.5 5.90 5.936 −11.370Hj2-1 5.45 6.872 −10.052Hj2-2 5.45 6.970 −8.559Hj3 5.15 5.791 −7.578Hj4 4.55 5.681 −9.013Hj5 4.15 5.191 −9.941Hj5.5 3.75 5.502 −8.697Hj6.1 3.35 5.005 −8.616Hj7.1-1 2.40 5.046 −10.414Hj7.1-2 2.40 5.008 −10.085Hj10 0.70 4.776 −11.163Hj11 0.20 4.857 −10.913

Section 1 (Saraito)Yabeina Zone (8 horizons)

B41 56.8 4.575 −10.049B40 56.4 4.478 −8.744B39-1 56.1 5.051 −10.426B39-2 56.1 5.235 −10.824B38 55.3 5.013 −10.893B38Y1 55.3 5.056 −10.789B38Y2 55.3 4.941 −11.677B37 55.0 4.932 −11.356B37Y2 55.0 4.774 −11.978B37Y3 55.0 4.917 −11.891B36 54.7 4.704 −8.933B35 54.1 5.050 −9.350B34 53.8 4.430 −8.081

Neoschwagerina Zone (13 horizons)B12-1 33.9 4.213 −10.435B12-2 33.9 4.384 −10.715B9 31.0 4.314 −11.773B6-1 28.0 4.042 −10.775B6-2 28.0 4.267 −9.899B5-1 27.7 4.128 −11.003B5-2 27.7 4.173 −11.245B4-1 27.0 4.123 −11.414B4-2 27.0 4.177 −12.362B3 26.0 4.201 −7.97051 25.5 3.935 −10.139B2 24.0 4.072 −8.329B1-1 21.0 3.550 −10.890B1-2 21.0 3.648 −10.570X-1 15.0 3.714 −10.602X-2 15.0 3.969 −7.75307-05 4.5 3.959 −9.19207-03 3.4 3.546 −8.841Z4 0.0 3.536 −9.747

ld 16 (2007) 16–30 21

cally divided into two parts; i.e., segment Hi-1 (3.5 m+)and the overlying segment Hi-2 (2.2 m+) (Fig. 4). Thesegment Hi-1 is characterized by a gradual increasein �13Ccarb values, whereas the Hi-2 by a reverseddecrease. The sample Hj-2 with +7.0‰ marked the high-est �13Ccarb value in the Iwato Formation.

In summary, the current C isotope analysis clarifiedthe following two facts: (1) the �13Ccarb values keepincreasing from the Neoschwagerina Zone (segment Sr-1; Wordian) to the Yabeina Zone (segments Sr-2 andHi-1; lower Capitanian) except for the upper part of theYabeina Zone (segment Hi-2); (2) all the �13Ccarb valuesof the Capitanian Iwato Formation range above +4.4‰up to the highest value of +7.0‰ in the upper YabeinaZone.

5. Discussion

This study confirms the development of the Kamuraevent in the late Guadalupian, and suggests that theinterval of this unique event has ranged stratigraphicallyfurther downward. We will discuss here the geologi-cal implications of the new dataset, focusing on theonset timing and total duration of the Kamura event withrespect to the end-Guadalupian environmental changesand mass extinction, and particularly to the transition ofclimatic regime from the late Paleozoic icehouse (Gond-wana glaciation) to Mesozoic greenhouse.

5.1. Onset of the Kamura event

The present study has clarified that the lower partof the Iwato Formation (Wordian Neoschwagerina Zoneand lower Capitanian Yabeina Zone) is thoroughly char-acterized by positive values of �13Ccarb over +3.5‰(Figs. 3 and 4). In particular, all the �13Ccarb val-ues of the Yabeina Zone both in Sections 1 and 3exceed +4.4‰, and they range mostly in a high posi-tive domain between +5.0 to +6.0‰. The Yabeina Zoneof the Iwato Formation in general has more or lessthe same isotopic signature as the overlying LepidolinaZone and barren interval in which the Kamura eventwas originally recognized (Isozaki et al., 2007). Thusthe interval of the Kamura event with �13Ccarb valuesover +5.0‰ ranges stratigraphically downward to theYabeina Zone.

On the other hand, the Wordian NeoschwagerinaZone recorded relatively lower �13C values between
carb+3.5 and +4.2‰, thus the Kamura event had notyet started in the Wordian. However, the �13Ccarbrecord of the Neoschwagerina Zone clearly demonstratesa steadily upward-increasing pattern, suggesting that


Fig. 3. Chemostratigraphy of stable carbon isotope of carbonates of Section 1 near Saraito in Kamura. Legends for columnar section are the sameas those for Fig. 2. This section is divided into two chemostratigraphic segments: Sr-1 and Sr-2.

Y. Isozaki et al. / Palaeoworld 16 (2007) 16–30 23

F Sections raphic s

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ig. 4. Chemostratigraphy of stable carbon isotope of carbonates ofame as those for Fig. 2. This section is divided into two chemostratig

he oceanographic condition started to shift graduallylready in the Wordian toward the extreme state of theapitanian with unusual enrichment of 13C in seawater.

The sample SrB35 in the Yabeina Zone in Sec-ion 1 marks the lowest horizon with �13Ccarb valuesver +5.0‰, suggesting the lower limit of the interval
f the Kamura event. Unfortunately much lower hori-on of the Yabeina Zone is covered and the boundaryetween the Neoschwagerina Zone and Yabeina Zoneas not been observed in Kamura. Nonetheless, the
3 near Hijirikawa in Kamura. Legends for columnar section are theegments: Hi-1 and Hi-2.

general secular trend of the �13Ccarb record positivelyindicates that the Kamura event has first emerged aroundthe Wordian/Capitanian boundary (265.8 Ma accordingto the latest geological timescale by Gradstein et al.,2004; Fig. 5). It is noteworthy that a strange conditionhas appeared in the middle of the superocean around
the Wordian/Capitanian boundary because the Kamuraevent may mark the first episode of large isotopic excur-sion in the Permian (Fig. 1B). Although the trigger forthis oceanographic change is unknown at present, the


Fig. 5. Schematic summary of the �13Ccarb chemostratigraphy of the Guadalupian Iwato Formation and Early Lopingian Mitai Formation in Kamura,ain ext
showing the total range of the Kamura event. Not to scale. Note the m
�13Ccarb values. C-R: Codonofusiella-Reichelina.

onset timing of the Kamura event should be checkedfurther carefully in continuous sections elsewhere inorder to examine whether or not this event started syn-chronously throughout the world.

inction occurred in the middle of the high positive plateau interval of

5.2. Duration of the Kamura event

As discussed above, the Kamura event apparentlyranged through three successive fusuline zones of the

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apitanian; i.e., the Yabeina Zone, Lepidolina Zone,nd barren interval in ascending order (Fig. 5). Theasal part of the Yabeina Zone in Kamura is miss-ng, whereas the uppermost part of the barren intervals free from high positive �13Ccarb values. Thus theamura event likely spanned throughout almost the

ntire Capitanian, except for the uppermost and pos-ibly the lowest parts. This is supported by the datarom the GSSP of the G–LB at Penglaitan and Tieqiao,outh China, as there is no high positive plateau recog-ized in the uppermost Capitanian immediately belowhe conodont-defined G–LB (Wang et al., 2004; Jin etl., 2006).

Although detailed chronology of the three fusulineones of the Capitanian has not yet been established,iven the whole Capitanian ranging for 5.4 million yearsrom 265.8 Ma to 260.4 Ma (according to the timescaley Gradstein et al., 2004), the total duration of theamura event is estimated to be more than a half of theapitanian, probably 3–4 million years. Such a remark-ble period characterized by an unusual positive �13Ccarbxcursion has never been recognized in the Permian.t is also noteworthy that the highest �13Ccarb value.0‰ was detected in the sample Hj-2 in the upperart of the Yabeina Zone, as no-such high positive valueas ever been reported from the Permian rocks (e.g.,rossman, 1994; Scholle, 1995; Korte et al., 2005). Thus

he maximum �13Ccarb value in the Yabeina Zone sug-ests that the Kamura event may have culminated in thearly-middle Capitanian, held the similar condition forwhile, and finally collapsed quickly in the late Capita-ian.

In general, extremely high positive �13Ccarb valuesndicate extraordinarily high productivity in the ocean.s oceanic productivity is strongly controlled by nutri-

nt availability, constant supply particularly of limitinglements such as P and N is necessary to maintain long-asting high productivity. Saltzman (2005) compiled allvailable �13Ccarb measurements from the Paleozoicmiddle Cambrian to Carboniferous) rocks in the Greatasin of western USA, and demonstrated a compos-

te Paleozoic secular curve that is punctuated by ninenique events of remarkable positive excursions by over3.0‰ lasted for more than a few million years. Heoncluded that these nine events, detected also in dif-erent continents, represent intermediate cool climatentervals between typical greenhouse and icehouse peri-ds. By lowering the sea surface temperature, oceanic
irculation can be accelerated to bring sufficient nutri-nts from the deep ocean to the surface and this willesult in high primary productivity by blooming ofhytoplankton/cyanobacteria. As to the nutrient condi-
ld 16 (2007) 16–30 25

tion, however, the high productivity will not hold for along time because of negative feedback mechanism, ifworld oceans are nitrogen-limited. In contrast, under aphosphorous-limited condition, high primary productiv-ity coupled with preferential organic carbon burial willcontinue to keep seawater �13C in high positive val-ues for certain duration until effective recycling of Pstops (Saltzman, 2005). Although the Silurian (Ireviken)event remains still controversial (Cramer and Saltzman,2007), other eight Paleozoic cases with prominent posi-tive �13Ccarb excursion all suggest the appearance of coolclimate.

Accordingly, the late Guadalupian Kamura event wasnominated as the 10th case in the Paleozoic character-ized by a remarkable positive �13Ccarb excursion, andthe Kamura event likewise represents a transient coolinterval that appeared in the late Guadalupian (Isozakiet al., 2007). The unique lithofacies of the Iwato For-mation dominated by black to dark gray, organic-rich(TOC ∼0.1 wt%) wackestone probably reflects the highproductivity in surface waters, as most of the Permianpaleo-atoll limestone in Japan has much lower TOCless than 0.01 wt%. It is worth noting that this eventmarks the first cooling episode, after the Gondwanaglaciation ended in the Artinskian (late Cisuralian; Jonesand Fielding, 2004), in the middle of the long-termwarming trend toward the generally warm Mesozoicera.

In good accordance with the above interpretation,the lately compiled Permian sea-level fluctuation curvedemonstrates that the Permian lowest-stand occurredaround the G–LB (Hallam and Wignall, 1999; Tong etal., 1999). A major hiatus on the top of the Guadalu-pian Maokou Formation has been recognized extensivelyin South China, and the top of the well-known Per-mian Reef complex in west Texas is unconformablycovered by the Lopingian evaporites (e.g., Mei andWardlaw, 1996). The “Permian chert event” in highlatitudes (Beauchamp and Baud, 2002) likely supportsthe appearance of a cool period in the Guadalupian,too.

5.3. Critical cooling

The end-Guadalupian is regarded as a timing of one ofthe two major extinction events of the terminal Paleozoicera (Jin et al., 1994; Stanley and Yang, 1994). Isozaki(1997a, 2007) emphasized the geological significance
of the G–LB event from a viewpoint of the timing coin-cidence between two global geological phenomena; i.e.,the biotic extinction and the onset of the P–TB supera-noxia in the superocean. As to the cause of the G–LB

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vent, a global environmental change triggered by thearge-scale volcanism of the Emeishan Trap in Southhina is currently favored by many workers (e.g., Chungt al., 1998; Ali et al., 2002; Wignall, 2001); however,etails including possible direct kill mechanisms are notet fully clarified.

In this regard, the extinction of the Guadalupianauna in the middle of the Capitanian Kamura eventppears critical. The clear extinction pattern of largeusulines (Verbeekinidae) and bivalves (Alatoconchi-ae) in the Capitanian part of the Iwato FormationIsozaki, 2006; Ota and Isozaki, 2006) suggests thathe claimed cooling of the Kamura event might havelayed the key role in the kill scenario, in particular forhe creatures well adapted to a warm tropical climaten low-latitude areas (Isozaki et al., 2007). The occur-ence/distribution of the middle Permian Verbeekinidae,latoconchidae, and Waagenophyllidae (rugose coral)

amilies was restricted in low-latitude shallow seas inethys and Panthalassa, and the gigantism in fusu-

ines and Alatoconchidae bivalves was probably dueo the symbiosis with photosynthetic algae/bacteria inuch oligotrophic environment in mid-ocean in generalIsozaki, 2006).

In the late Capitanian, large fusulines were screenedut by size (Wilde, 2002; Yang et al., 2004; Otand Isozaki, 2006), aberrant Alatoconchidae bivalvesecame totally extinct (Isozaki, 2006), and the diver-ity of rugose corals declined remarkably (Wang andugiyama, 2000). The possible drop in sea surface

emperature in low latitudes may have caused a totalalfunction of photosymbiosis factory shared by the

bove-mentioned “tropical trio” that were too muchdapted to warm-water environments to survive thehange. At Tieqiao, the last occurrence of large fusu-ine Metadoliolina (Verbeekinidae) was confirmed in theinogondolella xuanhanensis Zone with �13Ccarb val-es of +3 to +4‰ (Jin et al., 2006), suggesting that the
xtinction of large fusulines slightly delayed in Southhina probably owing to the local variability in water
emperature.

ig. 6. Secular change of �13Ccarb in the Paleozoic and early Mesozoic, comorte et al. (2005) and this study for the Permian, from Payne et al. (2004) annd Katz et al. (2005) for the Jurassic. Note the four distinct intervals of volardovician–Silurian, Late Devonian–Early Carboniferous, and the Middle PMT-interval). The PMT-interval from the Capitanian (Late Middle Permiaears, representing the transition from the late Paleozoic icehouse, centerehe Mesozoic/Cenozoic greenhouse. The PMT-interval recorded a period oetween icehouse and greenhouse modes, and the Kamura event marks theesozoic greenhouse. It is noteworthy that the two major mass extinctions (a

MT-interval chronologically overlaps the P–TB superanoxic period (Isozaki

ld 16 (2007) 16–30 27

In addition, some gastropods and brachiopodsbehaved similarly as the trio. For example, theoccurrence of extraordinarily large gastropods, suchas Bellerophon (13 cm in diameter), Pleurotomaria(18 cm × 16 cm), and Murchisonia (40 cm in height),were reported from the Capitanian limestone in Akasaka(Hayasaka and Hayasaka, 1953), whereas all the gas-tropods from the overlying Lopingian are no morethan 1 cm in diameter. It is also noteworthy that someearly-middle Permian brachiopods originated in middle-high paleolatitude domains (Attenuatella, Waagenites,Strophalosiina, Comuqia) migrated to low-latitudes andmade their first appearance in the paleoequatorial zone atthe end of the Capitanian (Shen and Shi, 2002). Althoughthe Permian gastropods and brachiopods as a whole didnot experienced a remarkable diversity loss at the G–LB(e.g., Pan and Erwin, 1994; Shen and Shi, 2002), theseobservations likewise support the appearance of a coolinterval in the Capitanian Tethys and Panthalassa.

The G–LB is placed not at the extinction level ofthe Guadalupian fauna but at the first appearance datum(FAD) of the Wuchiapingian index conodont Clarkinapostbitteri postbitteri as defined at the stratotype section(GSSP) at Penglaitan in South China (Jin et al., 1998;Henderson et al., 2002). Owing to the absence of con-odonts, the G–LB in Kamura is set at the horizon ca.11 m above the main extinction level in the upper part ofthe barren interval on the basis of the first appearance ofthe Lopingian fusulines and �13Ccarb chemostratigraph-ical correlation (Ota and Isozaki, 2006; Isozaki et al.,2007). The main extinction occurred not at the G–LBper se but in a much lower horizon in the midst of thepositive �13Ccarb excursion interval. Thus an appreciabletime has elapsed between the end-Guadalupian extinc-tion and the following radiation of the Lopingian faunain shallow mid-Panthalassa (Fig. 1A).

The present study demonstrated that the oceanic car-bon cycle started to change in mid-Panthalassa around
265 Ma, at least by 4–5 million years earlier than theG–LB (ca. 260 Ma). Should the claimed cooling havebeen responsible for the extinction of the Guadalupian
piled from Saltzman (2005) for the Cambrian to Carboniferous, fromd Gradstein et al. (2004) for the Triassic, and from Palfy et al. (2001)tility with high positive �13Ccarb excursion; i.e., Late Cambrian, Lateermian–Middle Triassic (=Paleozoic–Mesozoic transitional interval;n) to Anisian (Early Middle Triassic) ranged for ca. 20–25 milliond by the Pennsylvanian to Early Permian Gondwana glaciation, tof a transient cool climate with a P-limited oceanographic condition

beginning of the mode change from the Paleozoic icehouse to thet the G–LB and P–TB) occurred during the PMT-interval, and that the, 1997a).

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fauna, the ultimate cause of the environmental changemust have appeared by the early Capitanian time.

The Emeishan Trap volacanism in South China wasrecently dated 256–259 Ma (Zhou et al., 2002). Thisearly Lopingian age is obviously too young for the trapto be responsible for the environmental change in theearly Capitanian (ca. 265 Ma). In general, large-scalebasaltic volcanism likely drives the opposite conse-quence; i.e., global warming, rather than 3–4 millionyear-long cooling. Thus the superficial correlationbetween the end-Guadalupian extinction and the trapvolcanism needs re-consideration. Refer to Isozaki andOta (2007) for more details of relative timing betweenthe G–LB extinction and the Emeishan Trap volcanism.

5.4. δ13Ccarb volatility in the Paleozoic–Mesozoictransition interval

The Guadalupian major environmental change ofglobal context has appeared around 265 Ma (earlyCapitanian) several million years earlier than the end-Guadalupian mass extinction at the latest Capitanian.In a long-term viewpoint, the Capitanian Kamura eventis particularly significant because it marks not only theonset of wild �13Ccarb fluctuations across the P–TB intothe early Anisian, middle Triassic, but also the firstremarkable positive �13Ccarb excursion after a nearly 85million years of relative quiescence (Fig. 6). In addi-tion to the well-known sharp negative shift across theP–TB (Baud et al., 1989; Holser et al., 1989; Musashiet al., 2001), more positive and negative excursions ofgreater magnitude occurred particularly in the early Tri-assic (Payne et al., 2004). As to the Lopingian, similar�13Ccarb fluctuations are likely expected from the pre-liminary results (Baud et al., 1996; Shao et al., 2000;Korte et al., 2005); however, the dataset is too immatureto document detailed secular change particularly for theWuchiapingian (lower Lopingian).

In sharp contrast to the Paleozoic–Mesozoic transi-tion (PMT)-interval, such a wild fluctuation varying from+8 to −3‰ has not been recognized in the Cisuralian toearly Guadalupian nor in the middle Triassic and laterpart of the Mesozoic (Fig. 6). In fact, �13Ccarb valueover +5.0‰ has never been recorded throughout theMesozoic and Cenozoic (e.g., Veizer et al., 1999; Katzet al., 2005). Thus a volatile change in global carboncycle relevant to oceanography is restricted solely to the∼20 million year-long PMT-interval from the Capitanian
(ca. 265 Ma) to early Anisian (ca. 245 Ma).
As pointed out by Saltzman (2005), there are threeother intervals in the Paleozoic that are characterizedby volatile fluctuations of �13Ccarb values; i.e., the

ld 16 (2007) 16–30

Late Cambrian, Late Ordovician to Silurian, and LateDevonian to Early Carboniferous (Fig. 6). The firsttwo intervals was described as a transient cool intervalbetween two greenhouse periods when the globe wasalmost running into an icehouse but did not. Unlike these,the rest two correspond to bona fide transient cool periodsbetween an icehouse and a greenhouse period. The latePaleozoic (Carboniferous to Early Permian) was domi-nated by the icehouse climate centered by the Gondwanaglaciation, while the Mesozoic in total was governed bywarm greenhouse climate (e.g., Frakes et al., 1992).

It is noteworthy that this PMT-interval with high�13Ccarb volatility approximately overlaps the super-anoxic period in the superocean (Isozaki, 1997a).Regardless of climatic modes, the deep-sea cherts bothof the Pennsylvanian–Guadalupian (icehouse interval)and the Middle Triassic to Jurassic (greenhouse interval)were well oxygenated. This indicates that the growth andretreat of superanoxia have been controlled not solelyby the climate-dependent, global oceanic circulation butalso by other factors.

At any rate, a major re-organization of globaloceanography, including the global carbon cycle,occurred during the PMT-interval, and this clearly sep-arated the ancient regime of the Paleozoic and the newone of the Mesozoic. The causes and processes of thetwo major mass extinction events, at the G–LB and atP–TB, should better be explained in the scope of suchlong-term geological context.

After all, the late Guadalupian Kamura event pre-ludes all these drastic change in the PMT-interval fromthe Paleozoic to post-Paleozoic world, and the ultimatetrigger(s) of this major mode change in environmentcan be found neither in the strict G–LB nor P–TBintervals but likely in the upper Guadalupian rockrecords.

6. Summary

The present study on the mid-Panthalassan paleo-atollcomplex clarified the following new aspects of the lateGuadalupian environmental change relevant to the massextinction:

(1) The Kamura event with high positive �13Ccarb valuesranged for nearly 3–4 million years in the Capitanian(ca. 265–260 Ma), late Guadalupian.

(2) The end-Guadalupian extinction occurred in the
middle of the Kamura cooling event.
(3) The Kamura event marks the beginning of the majormode change of global climate and oceanographyfrom the Paleozoic to post-Paleozoic regime.

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cknowledgements

This article is dedicated to late Lao Jin (Prof. Jinugan) for honoring his great contributions to the Per-ian study. We thank Shen Shuzhong, Chen Siwei and

n anonymous reviewer for their constructive reviews,isayoshi Igo for identification of fusulines, Teruhisaasuya for drafting in part, plus Susumu Nohda andomomi Kani for their help in fieldwork. This researchas supported by the Grant-in-Aid of Japan Societyf Promoting Science (no. 16204040 to YI and no.7253006 to HK).

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