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1 October 2019 The Guadalupian (Permian) Gufeng Formation on the North Margin of the South China Block: A Review of the Lithostratigraphy, Radiolarian Biostratigraphy, and Geochemical Characteristics
Tsuyoshi Ito, Koji U. Takahashi, Atsushi Matsuoka, Qinglai Feng
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Abstract

The Guadalupian (Permian) Gufeng Formation, distributed over the north margin of the South China block, is characterized by siliceous rock and muddy rock and yields several representative radiolarian fossils. The lithostratigraphy, radiolarian occurrences and biostratigraphy, and geochemical characteristics of the Gufeng Formation are reviewed and summarized in this paper. The distributional area of the Gufeng Formation is subdivided into the Lower, Middle, and Upper Yangtze regions. The Gufeng Formation in the Lower Yangtze region is lithostratigraphically characterized by muddy rock, chert, and nodule-bearing muddy rock in descending order. The Gufeng Formation in the Middle Yangtze region is lithostratigraphically characterized by chert, muddy rock with carbonate, and muddy rock in ascending order. The lithostratigraphic characteristics of the “Gufeng Formation” in the south margin of the South China block greatly differ from the typical Gufeng Formation in containing fewer siliceous rocks and a large amount of clastic rocks and in having a significantly greater total thickness; therefore, this article considers that the “Gufeng Formation” in the block's south margin should be isolated from the Gufeng Formation in the block's north margin. The radiolarian biostratigraphy of the Lower and Middle Yangtze regions is composed of the Pseudoalbaillella globosa, Ps. monacantha, and Follicucullus scholasticus-Ruzhencevispongus uralicus assemblage zones in ascending order. The lower Gufeng Formation has abundantly yielded the Albaillellaria; however, its occurrence ratio with respect to other radiolarian orders decreases stratigraphically upward. The geochemical characteristics indicate the following facts: (1) the siliceous rocks are generally biogenic; (2) even though a previous study concluded that the organic matter within the chert was originated from terrestrial or reworked organic matter, the origin remains debatable; and (3) the Gufeng Formation was formed on a continental shelf. The geochemical characteristics, in addition to the lithological characteristics, indicate that the redox conditions of the Gufeng Formation in the Lower Yangtze region changed from aerobic to suboxic to anoxic, while that in the Middle Yangtze region changed from oxic to anoxic to suboxic.

Introduction

The Permian period is one of the most diverse intervals during Earth's history (e.g. Hein, 2004) because a number of notable events occurred during this period, such as the most severe mass extinction in the Phanerozoic at the Guadalupian–Lopingian boundary and the end-Permian (Jin et al., 1994; Stanley and Yang, 1994), multiple glaciations (e.g. Isbell et al., 2011), a global cooling event termed the Kamura event (e.g. Isozaki et al., 2007a, b), and a large amount of chert accumulation in the middle Permian termed the mid-Permian chert event (Murchey and Jones, 1992) or the Permian Chert Event (Beauchamp and Baud, 2002).

Figure 1.

Guadalupian paleogeographic map, modified from Ziegler et al. (1997).

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The Gufeng (Kuhfeng) Formation in South China has yielded Guadalupian (middle Permian) fossils of several kinds (e.g. ammonoids, brachiopods, and conodonts). In particular, the Gufeng Formation is known to have abundant radiolarian-bearing strata. This fossiliferous formation has attracted attention in recent years (e.g. Zhang et al., 2019) because the formation may record paleobiological responses to environmental changes through the Permian. Yao et al. (2015) studied the fluctuation of chert bed thickness in the Gufeng Formation in relation to cyclic astronomical forcing of climate change, which in turn affected radiolarian productivity.

In addition, the Gufeng Formation is important from both paleogeographic and paleobiogeographic points of view. The Gufeng Formation consists of sediments on the South China block (Yangtze block). This block had been situated at the east end of the Paleotethys near the boundary between the superoceans Panthalassa and Paleotethys in the middle Permian (e.g. Ziegler et al., 1997; Golonka and Ford, 2000) (Figure 1). Because the South China block acted as a wall between the both superoceans, a paleobiogeographic boundary has been recognized around the South China block for several groups such as fusulinids (e.g. Kobayashi, 1997), brachiopods (e.g. Shen et al., 2009), and radiolarians (Ito et al., 2016b).

Furthermore, the Gufeng Formation is known to have oil-rich strata; therefore, petrochemical studies have been performed (e.g. Xia et al., 1995; Zeng et al., 2004; Yang and Yao, 2008). Previous studies have focused on the porosity of the rocks in the Gufeng Formation as a reservoir rock (Wu et al., 2012; Liang et al., 2014). In recent years, its potential as an origin and reservoir of shale gas has also been a focus of study (Du et al., 2015).

In short, the strata of the Gufeng Formation are extremely significant in terms of paleontology, sedimentology, paleogeography, paleobiogeography, and petroleum geology. Meanwhile, the formation has regional differences in several characteristics, such as lithostratigraphy and biostratigraphy. Due to these regional differences, even the definition and distributions of the formation have been debated (e.g. Hu, 2000; Kuwahara et al., 2004; Yao et al., 2007). On the basis of previous studies combined with ours, here we compile the lithostratigraphy, radiolarian occurrences with biostratigraphy, and geochemical characteristics of the Gufeng Formation in each region. This article aims to provide a general review of these aspects for future reference.

Lithostratigraphy

Definition and distribution

The Gufeng Formation was originally called the Gufeng Zhen Limestone at Hujia Village of Gufeng Town, Anhui Province by Ye and Li (1924) (Figure 2). The Bureau of Geology and Mineral Resources of Anhui Province (1997) re-defined the Gufeng Formation as follows (translated from the Chinese): It is characterized by black or gray-yellow thin-bedded siliceous rocks, siliceous shales, siltstones, carbonaceous shales, and manganese shales. The Gufeng Formation overlies the Qixia Formation and underlies the Longtan Formation. Basal shales include manganese and phosphate nodules. Several taxa of fossils (e.g. ammonoids, brachiopods, bivalves, and radiolarians) occur from it.

Figure 2.

Original and emended definitions of the Gufeng Formation. Note that the information by Ye and Li (1924) is re-quoted from Bureau of Geology and Mineral Resources of Anhui Province (1997). The English translations of the definitions have been made by the authors.

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The respective bureaus of geology and mineral resources in each province of China have compiled regional geologies for their provinces. The columnar sections of the stratotype and hypostratotype sections established by the bureaus with some notable sections are summarized in Figures 3 and 4. The Bureau of Geology and Mineral Resources of Anhui Province (1997) established the Hujia section (30°50′N, 118°24′E) in Gufeng as the stratotype section of the Gufeng Formation. In other provinces, the respective bureaus of geology and mineral resources established hypostratotype sections of the Gufeng Formation: the Lengwu section (29°55′N, 119°32′E) in Tonglu (Bureau of Geology and Mineral Resources of Zhejiang Province, 1996), the Hechong section (32°09′N, 119°06′E) in Jurong (Bureau of Geology and Mineral Resources of Jiangsu Province, 1997), the Bijiashan section (30°12′N, 114°47′E) in Daye (Bureau of Geology and Mineral Resources of Hubei Province, 1996), and the Lengshuixi section in Shizhu (Bureau of Geology and Mineral Resources of Sichuan Province, 1997).

The Gufeng Formation is distributed over the north margin of the South China block (Figure 3). Its distributional area is subdivided into three regions: the Lower Yangtze region (northern Zhejiang, southern Jiangsu, and south Anhui), the Middle Yangtze region (Hubei), and the Upper Yangtze region (Shaanxi and northern Sichuan). Previous studies have also considered siliceous rocks on the south margin of the South China block (southern Hunan, northwestern Guangdong, and eastern Guangxi) to be part of the Gufeng Formation. However, the so-called “Gufeng Formation” in the block's south margin differs from the typical Gufeng Formation in the north margin in its lithostratigraphy, as will be described in detail. We therefore regard the Gufeng Formation as being distributed only over the north margin.

Lithology and its correlations

North margin.—The Hujia section in Gufeng, the stratotype section of the Gufeng Formation, is divided into the following subsections in ascending order (Bureau of Geology and Mineral Resources of Anhui Province, 1997): subsection 1: brownish-black manganese mudstone; subsection 2: yellow mudstone, interbedding gray siliceous mudstone and thin-bedded chert; subsection 3: yellow mudstone including gray phosphate muddy nodules; subsection 4: gray siliceous mudstone; subsection 5: black thin-bedded chert interbedding black thin-bedded siliceous mudstone; and subsection 6: black thin-bedded siliceous mudstone interbedding carbonaceous mudstone. The Gufeng Formation of the section conformably contacts with the underlying Qixia and overlying Longtan formations.

Figure 3.

Distributions of the Gufeng Formation with the major localities of sections and the radiolarian localities from previous studies. The distributions are based on Wu et al. (2015). Detailed location of the Lengshuixi section in Shizhu was not shown by Bureau of Geology and Mineral Resources of Sichuan Province (1997); therefore, the location is not presented.

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The Gufeng Formation at Chaohu in Anhui has been studied in detail mainly by a research group of Nagoya University and Nanjing University (Nagai and Zhu, 1992; Nagai et al., 1998; Zhu et al., 1999; Kametaka et al., 2002, 2005, 2009; Takebe et al., 2007). Kametaka et al. (2002) and Kametaka et al. (2005) divided the Gufeng Formation of the Anmenkou section at Chaohu into two members: the Phosphate Nodule-bearing Mudstone Member (PNMM) and the Siliceous Rock Member (SRM) in ascending order. The former (ca. 4 m in total thickness) consists of mudstone including abundant phosphate nodules; the latter (ca. 25 m) is composed primarily of alternations of black chert, mudstone, and siliceous mudstone, with minor tuffaceous mudstone and porous chert beds. Ito et al. (2013a) investigated the Liuhuang section near the Anmenkou section and detected a lithologic similarity between the Liuhuang and Anmenkou sections. In the Liuhuang section, the siliceous rock is dark-colored (black to dark-gray) and well bedded (Figure 5A, B). The Gufeng Formation disconformably contacts with the limestone of the underlying Maokou Formation in the Liuhuang section (Figure 5C). Zhang et al. (2019) investigated the Hexian core drilled at Hexian 50 km northeast of Chaohu and subdivided the Gufeng Formation in the core into three members, the Lower Phosphate Nodule-bearing Mudstone Member (LPMM), the Lower Chert-Mudstone Member (LCMM), and the Upper Mudstone Member (UMM), with the Lower Shale Member (LSM) of the Yinping Formation. The LPMM and LCMM can be lithostratigraphically correlated to the PNMM and SRM, respectively.

Figure 4.

Lithostratigraphy of the stratotype section of the Gufeng Formation in Anhui Province and the hypostratotype sections in the Hubei, Jiangsu, Zhejiang, Hunan, and Guangdong provinces with major sections. White triangles with capital letters indicate occurrence horizons of each photograph of Figure 5.

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Porous chert (Kametaka et al., 2005; nectic chert in Zhu et al., 1999 and Kametaka et al., 2002) is a remarkable rock in the Gufeng Formation in the Lower Yangtze region. As its name suggests, the porous chert has abundant small cavities and shows a spongy structure compared to commonly known normal chert, which is characterized by being dense and nonporous. The bulk specific gravity of the porous chert is only 1.1–1.2 (Kametaka et al., 2005). The porous chert is interbedded in the normal chert beds and is generally thicker than the normal chert beds.

Ma et al. (2016) and Shi et al. (2016) studied the lithostratigraphy of the Luojiaba and Macaojie sections near Jianshi, western Hubei, respectively. The Gufeng Formation in both sections consists primarily of siliceous and muddy rocks. The lower parts of the Gufeng Formation in both sections are characterized by the dominance of dark-colored well bedded chert (Figure 5D), whereas the upper parts are characterized by muddy rock with carbonate (Figure 5E). The Gufeng Formation in both sections is conformably covered by the limestone of the Wuxue Formation (Figure 5F). In these sections, the Gufeng Formation conformably overlies the Maokou Formation. Meanwhile, Chen et al. (2000) observed clastic rocks in the basal part of the Gufeng Formation at Huangyan in Jianshi and concluded that the Gufeng Formation unconformably overlies the Maokou Formation there. The Bijiashan section contains thick carbonate rocks and is much thicker than the Luojiaba and Macaojie sections. This may indicate that the Bijiashan section represents a shallower facies.

In short, the Gufeng Formation in the north margin is characterized by siliceous and muddy rocks. Lithostratigraphy of the Gufeng Formation in the Lower Yangtze region comprises muddy rock, chert, and muddy rock with nodules in descending order whereas that in the Middle Yangtze region consists of chert, muddy rock with carbonate, and muddy rock in ascending order.

South margin.—The bureaus of geology and mineral resources in Hunan, Jiangxi, Guangxi, and Guangdong established hypostratotype section of the Gufeng Formation in each province: the Guanghuang section (27°17′N, 113°41′E) in You (Bureau of Geology and Mineral Resources of Hunan Province, 1997), the Majia'ao section (27°16′N, 113°53′E) in Lianhua (Bureau of Geology and Mineral Resources of Jiangxi Province, 1997), the Tongtianyan section in Liuzhou (Bureau of Geology and Mineral Resources of Guangxi Zhuang Autonomous Region, 1997), and the Youkeng section (24°32′N, 116°09′E) in Jianling (Bureau of Geology and Mineral Resources of Guangdong Province, 1996).

These sections are characterized by a great quantity of clastic rocks, such as carbonaceous mudstone, mudstone, and sandstone, with little chert (Figure 4). The typical Gufeng Formation in the north margin, however, is characterized by siliceous and muddy rocks as mentioned previously. We therefore believe that the “Gufeng Formation” in the south margin should be isolated from the Gufeng Formation and given another formation name.

Hu (2000) argued that the Gufeng Formation is also distributed over the south margin of the South China block based on discussions including fossil data. However, the Gufeng Formation is a lithostratigraphic unit. According to the International Stratigraphic Guide (Murphy and Salvador, 1999), “Lithostratigraphic units are defined and recognized by observable physical features and not by their inferred age, the time span they represent, inferred geologic history, or manner of formation.”

Radiolarian occurrences

The Gufeng Formation contains several kinds of macrofossils and microfossils, such as conodonts (e.g. Ching, 1960; Wang, 1995a; Kuwahara et al., 2008a; Ma et al., 2016), foraminifers (e.g. Wang, 1993c), brachiopods (e.g. Jing and Hu, 1978; Xu et al., 2004), sponge spicules (e.g. Kuwahara et al., 2007b; Ito et al., 2016e), mollusks (e.g. Xi, 1982; Kametaka et al., 2009), and fish microremains (e.g. Kuwahara et al., 2007b; Mao et al., 2013).

Figure 5.

Field occurrences of the Gufeng Formation. A, B, black bedded chert in the Liuhuang section in Chaohu, Anhui; C, overturned basal mudstone and stratigraphically overlying limestone of the Maokou Formation in the Liuhuang section; D, black bedded chert of the Maocaojie section in Jianshi, Hubei; E, mudstone including lenticular limestone in the Luojiaba section in Jianshi; F, carbonaceous mudstone and stratigraphically overlying limestone of the Wuxue Formation in the Maocaojie section. The occurrence horizons of each correspond to the white triangles in Figure 4.

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Figure 6.

Summarized radiolarian zones of the Gufeng Formation in each province in previous studies. Note that the Follicucullus monacanthus Zone is changed to the Pseudoalbaillella monacantha Zone according to the taxonomic reconsideration by Ito et al. (2015). F., Follicucullus; R., Ruzhencevispongus; Ps., Pseudoalbaillella; A., Albaillella.

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Since the 1980s, radiolarian occurrences have been reported in the Gufeng Formation in several areas. On that basis, radiolarian zones have been constructed. Meanwhile, an integrated radiolarian biostratigraphy has been compiled in Southwest Japan (Ishiga, 1986, 1990; Kuwahara et al., 1998) and South China (Wang and Yang, 2007, 2011). The radiolarian zones of Southwest Japan, South China, the Gufeng Formation in the north margin, and the “Gufeng Formation” in the south margin are summarized in Figure 6.

Radiolarian biostratigraphy of the north margin

Bi (1981) found spherical radiolarians in thin sections from the Tianbaoshan section in southeast Nanjing, Jiangsu, which was probably the first report of radiolarians from the Gufeng Formation. Sheng and Wang (1985) derived radiolarian fossils from siliceous rocks in the Longtan area in Nanjing using the hydrofluoric acid method and revealed radiolarian microphotographs via scanning electron microscopy (SEM) for the first time. Since these studies, several researchers have reported radiolarian occurrences in the Gufeng Formation in the Lower Yangtze region (Kong and Gong, 1986; Nagai and Zhu, 1992; Wang, 1993a, b, d, 1995b, c; Jiang et al., 1994; Wang and Qi, 1995; Wang et al., 1997; Nagai et al., 1998; He et al., 1999; Kuwahara et al., 2007b; Kametaka et al., 2009; Ito et al., 2013a; Zhang et al., 2019). Sheng and Wang (1985) constructed the Pseudoalbaillella scalprata-Ps. nanjingensis and Phanicosphaera mammilla assemblage zones, in ascending order. Wang (1995c) found the first occurrence of Follicucullus monacanthus Ishiga and Imoto in the Gufeng Formation. Wang (1995b) discussed the age assignment of F. monacanthus and concluded that the F. monacanthus assemblage from the Gufeng Formation corresponds to that of the F. monacanthus Zone of Japan and the USA. (Ishiga, 1986, 1990; Blome and Reed, 1992). Wang and Qi (1995) constructed the following assemblage zones: Ps. fusiformis-Ps. longtanensis, F. monacanthus, and Ruzhencevispongus uralicus-F. scholasticus in ascending order. Since the study by Wang and Qi (1995), the Gufeng Formation in the Lower Yangtze region has been divided into three radiolarian assemblage zones (e.g. He et al., 1999; Kametaka et al., 2009; Ito et al., 2013a).

Feng (1992) discovered radiolarians in the Wuchan area, which was the first radiolarian report from the Gufeng Formation in the Middle Yangtze region. Since this study, several researchers have reported radiolarian occurrences in this region (Feng and Zhong, 1994; Kuwahara et al., 2007a, 2008a; Ma and Feng, 2012; Ma et al., 2016; Shi et al., 2016). Ma and Feng (2012) constructed the Pseudoalbaillella globosa, Follicucullus monacanthus, and F. scholasticus assemblage zones in ascending order.

The radiolarian zonation of the Lower Yangtze and Middle Yangtze regions are well correlated based on the lineage from Pseudoalbaillella Holdsworth and Jones to Follicucullus Ormiston and Babcock in the Guadalupian (e.g. Ishiga et al., 1982; Wang and Yang, 2011; Zhang et al., 2014; Ito et al., 2015, 2016a).

In the Upper Yangtze region, fewer radiolarian studies have been performed compared to the Lower and Middle Yangtze regions. Kuwahara et al. (2007c) found Copicyntra? sp. and Copiellintra? sp. in the Gufeng Formation of the Mingyuexia 1 section in northern Sichuan. They also found Pseudoalbaillella cf. longtanensis Sheng and Wang and Ps. fusiformis (Holdsworth and Jones) from the uppermost part of the Maokou Formation just below the Gufeng Formation in that section. Kuwahara et al. (2008b) found Ps. fusiformis and Follicucullus cf. scholasticus Ormiston and Babcock in the Chejiaba section in Chaotian, northern Sichuan.

Radiolarian biostratigraphy of the south margin

The first occurrence of a radiolarian fossil from the “Gufeng Formation” in the south margin of the South China block was reported by Yao et al. (1993). They surveyed Late Paleozoic strata in Guizhou and Guangxi and obtained Follicucullus scholasticus, Latentifistula sp., and Pseudoalbaillella sp. from the “Gufeng Formation” in the Tongtianyan section in Guangxi. Wang and Li (1994) found F. charveti Caridroit and De Wever, F. bipartitus Caridroit and De Wever, and Albaillella triangularis Ishiga, Kito, and Imoto, corresponding to radiolarians of the F. bipartitus-F. charveti Assemblage Zone in Southwest Japan (Ishiga, 1986, 1990). Xian and Zhang (1998) researched the Bancheng area in Guangxi and constructed the following ascending radiolarian zones: Ps. scalprata, A. sinuata, Ps. banchengensis, Ps. globosa-Ps. fusiformis, F. monacanthus, and F. scholasticus. According to Xian and Zhang (1998), these zones correspond to radiolarian zones in Southwest Japan found by Ishiga (1986, 1990). However, judging from the text and figures of Xian and Zhang (1998), some of the radiolarian zones they constructed do not correspond directly to the radiolarian zones of Ishiga (1986, 1990). For example, F. scholasticus, which is a characteristic species of the F. scholasticus Assemblage Zone of Ishiga (1986, 1990), occurred in the Ps. globosa-Ps. fusiformis and F. monacanthus zones of Xian and Zhang (1998). The A. sinuata Zone of Ishiga (1986, 1990) is a range zone defined by the occurrence of A. sinuata. However, Xian and Zhang (1998) divided the A. sinuata-bearing strata of their section into the A. sinuata and Ps. banchengensis assemblage zones. Comparing the radiolarian zonation of Ishiga (1986, 1990) with that of Xian and Zhang (1998), the Ps. longtanensis Assemblage Zone, the Ps. globosa Assemblage Zone, and the F. monacanthus Range Zone of Ishiga (1986, 1990) are absent in the section of Xian and Zhang (1998). The Qinfang area, including the Bancheng area, is known as an orogenic belt in the late Paleozoic (e.g. He et al., 2014; Ke et al., 2018), and orogeny might cause the absence of some biozones.

Kuwahara et al. (2004) found Albaillella yamakitai from the Tongtianyan section, Guangxi, which is a characteristic species of the Follicucullus charveti-A. yamakitai Assemblage Zone. It has been proposed that the base of the Lopingian of the radiolarian biostratigraphy is defined by the first occurrence of A. yamakitai or just below it (e.g. Mitsumura and Kamata, 2009; Nishikane et al., 2011). This indicates that the top of the “Gufeng Formation” in Guangxi should reach the uppermost Guadalupian.

Wang and Yang (2003) found Pseudoalbaillella fusiformis and Ps. globosa in the Renhua area in Shaoguan, Guangdong. They constructed the Ps. fusiformis-Ps. globosa Zone corresponding to the Ps. fusiformis-Ps. longtanensis Zone in the Lower Yangtze region.

Stratigraphic change of radiolarian fauna

Stratigraphic change of radiolarian fauna has been clearly recognized in the Gufeng Formation in the north margin. Sheng and Wang (1985) divided radiolarians from the Longtan area into two faunas in ascending order: Pseudoalbaillella and Phanicosphaera. Kametaka et al. (2009) showed that Albaillellaria decrease but Latentifistularia increase upward in the Anmenkou section. Ito et al. (2013a) also recognized a similar pattern in the Liuhuang section. In the Middle Yangtze regions, Albaillellaria occur in the lower parts of the Gufeng Formation, but rarely occur in the upper part (Shi et al., 2016).

The radiolarian componential ratio at the order level (Albaillellaria, Latentifistularia, Entactinaria, and Spumellaria) has been used as an indicator of water depth (e.g. Kozur, 1993; Kuwahara, 1999). Kametaka et al. (2009) referred to these studies; however, they pointed out that the chief cause of the radiolarian faunal change in the Gufeng Formation in the Anmenkou section is not change in the water depth. This is because there are no remarkable lithological changes in the Anmenkou section. In other words, the depth of deposition of the Anmenkou section would have had to change by several hundreds of meters in order to be a critical factor for the faunal change.

Recently, Xiao et al. (2017) studied the latest Permian radiolarian vertical distribution based on a correspondence analysis. Their result suggests that radiolarians characterized different water depths at the species level even in the same order. Likewise, further studies on radiolarian vertical distributions in the middle Permian are necessary to understand the faunal change in the Gufeng Formation.

Figure 7.

SEM images of major remarkable radiolarians from the Gufeng Formation (reprinted from Ito et al., 2013a, reproduced with permission). A, B, Longtanella cf. zhengpanshanensis Sheng and Wang; C, Longtanella sp.; D, E, Ruzhencevispongus uralicus Kozur; F, Hegleria cf. mammilla (Sheng and Wang).

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Remarkable radiolarian occurrences

In this section, we focus on remarkable radiolarian taxa and forms from primarily taxonomic and paleobiogeographic points of view, combined with our previous studies in other areas.

Longtanella Sheng and Wang.—Longtanella is likely an endemic genus of the Gufeng Formation (Figure 7A–C). Longtanella generally occurs in the chert of the Gufeng Formation of the Lower Yangtze (Wang, 1993a; Kametaka et al., 2009; Ito et al., 2013a) and Middle Yangtze (Feng, 1992; Shi et al., 2016) regions. This genus also occurs in the chert of the “Gufeng Formation” in the south margin (Xian and Zhang, 1998). Probable Longtanella occurs in the Sa Kaeo Formation in the Sra Kaeo suture zone in eastern Thailand (Saesaengseerung et al., 2009) and the Kamiaso Unit in central Japan (Ito et al., 2016d).

The taxonomy of Longtanella, however, is currently debatable. Since Sheng and Wang (1985) described the genus, subsequent studies mainly in China have used this taxonomic name (e.g. Kozur and Mostler, 1989; Feng, 1992; Wang, 1993a; Kametaka et al., 2009; Ito et al., 2013a; Shi et al., 2016; Xiao et al., 2018). Meanwhile, several previous studies have synonymized this genus with Pseudoalbaillella (e.g. De Wever et al., 2001; Nestell and Nestell, 2010) or Parafollicucullus Holdsworth and Jones (Noble et al., 2017). Longtanella was diagnosed as “Shell smooth, straight, bilaterally symmetrical turriformis. The shell wall divided into the spire, the turribody and the turri-bottom composed of ring-like swollen segments. Last segment constrictive, with 4 flaps vertically extending downward” (Sheng and Wang, 1985, p. 179). According to the diagnosis, description, and holotype (Figure 8) of Longtanella, the genus seems to differ from Pseudoalbaillella and Parafollicucullus in lacking a winged pseudothorax and having four flaps. Further detailed observations are needed to solve this taxonomic problem.

Figure 8.

Sketch of a holotype specimen of Longtanella zhengpanshanensis Sheng and Wang, type species of the genus Longtanella Sheng and Wang (drawn from Sheng and Wang, 1985).

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Ruzhencevispongus uralicus Kozur.—Ruzhencevispongus uralicus is a characteristic species of the upper part of the Gufeng Formation (e.g. Wang, 1993a, b, 1995c; Wang and Qi, 1995; Kametaka et al., 2009; Ito et al., 2013a). This species possesses a triangular platy spongy shell (Kozur, 1980) (Figures 7D, 7E). Wang (1993d) examined the morphology of R. uralicus with samples from Chaohu and Hushan. He divided this species into three morphotypes, namely triadiatus, subtriadiatus, and uralicus. Even though Ruzhencevispongus commonly occurs in South China including in the Gufeng Formation, only a few such occurrences have been reported in Southwest Japan (e.g. Ishiga, 1990).

Hegleria Nazarov and Ormiston.—Occurrences of this genus have been reported worldwide, and this genus is seemingly a cosmopolitan taxon. However, there are similar outer-shaped radiolarians in the Permian. Ito et al. (2017c) stated these radiolarians as “Hegleria-shaped” radiolarians. The inner structure is important to identify “Hegleria-shaped” radiolarians. Hegleria has multiple internal rays that connect a central sphere to the outer shell (e.g. Noble and Jin, 2010) (Figure 7F). Several previous studies in the Gufeng Formation have shown radiolarians having this structure (e.g. Wang, 1993a, b, 1995c; Wang and Qi, 1995; Kametaka et al., 2009; Ito et al., 2013a), indicating that Hegleria surely occurred in the Gufeng Formation.

Meanwhile, “Hegleria-shaped” radiolarians having a concentric shell, probably Paracopicyntra spp., have also been discovered in the Gufeng Formation (e.g. Wang, 1993a, 1995b; Kametaka et al., 2009). Further, Kametaka et al. (2009) reported “Hegleria-shaped” radiolarians having a discoidal form as Hegleria sp. aff. H. mammilla, which might be Guiuva sashidai Ito and Feng.

Pseudotormentus De Wever and Caridroit.Pseudotormentus commonly occurs in deposits from the Panthalassa (e.g. De Wever and Caridroit, 1984; Blome and Reed, 1992, 1995; Mitsumura and Kamata, 2009; Nakae, 2011; Ito et al., 2013b; Ito and Matsuoka, 2015a, b, 2016, 2018) but rarely occurs in deposits from the Paleotethys. The Gufeng Formation, comprised of deposits from the Paleotethys, has rarely yielded Pseudotormentus. Ito et al. (2016b) examined this uneven distribution of Pseudotormentus and pointed out the possibility that it is a facies-dependent genus of a Panthalassan equatorial warm current.

Kametaka et al. (2009), however, reported the common occurrence of Pseudotormentus in the Gufeng Formation in the Anmenkou section. On the basis of the hypothesis of Ito et al. (2016b), the Gufeng Formation of the Anmenkou section might have been locally affected by the Panthalassan equatorial warm current. Alternatively, other factors such as lithology might control the uneven distribution of Pseudotormentus.

Corythoecidae Nazarov.—No radiolarian fossils of the family Corythoecidae, characterized by a bilaterally symmetrical shell with a lateral foramen, have been discovered in the Gufeng Formation. Even though the occurrence of this family is very rare worldwide (De Wever et al., 2001), Ito et al. (2017a) speculated that most species of the Corythoecidae occurred in phosphate-rich facies on the basis of a compilation of the previous occurrences and implied that this family preferred nutrient-rich conditions.

In the Lower Yangtze region, abundant phosphate nodules are contained in the lowermost part of the Gufeng Formation (e.g. Huang et al., 1994; Kametaka et al., 2009; Ito et al., 2013a). Although no radiolarians have been obtained in this part of the Gufeng Formation, it might have the potential to yield species of the Corythoecidae if the hypothesis of Ito et al. (2017a) is correct.

Swollen type.—Dimorphic pairs, comprised of normal and swollen types, are known in some taxa of the Order Albaillellaria (e.g. Ishiga, 1991; Ito and Matsuoka, 2015b, 2017; Ito, 2017; Ito et al., 2018). The swollen type is characterized by having a swollen apical portion. Ishiga (1991) suggested the possibility that the dimorphic pairs reflect alternating generations.

Previously, no occurrences of the swollen type have been reported from the Gufeng Formation; however, Xian and Zhang (1998) have reported the swollen type of Albaillella sinuata Ishiga and Watase and Pseudoalbaillella globosa Ishiga and Imoto in the “Gufeng Formation” in the Bancheng area.

Conjoined or malformed radiolarians.—Conjoined or malformed radiolarians are known in both living and fossil specimens (e.g. De Wever, 1985; Anderson and Gupta, 1998; Itaki and Bjørklund, 2007; Dumitrica, 2013; Afanasieva and Amon, 2016; Ito et al., 2017b). Afanasieva and Amon (2016) classified the conjoined or malformed radiolarians as two types: conjoined radiolarians in which two or more individuals are joined together were named as a multiplicative type; radiolarians having double or branching structure (e.g. spine, arm) were named as a supplemental type.

Certain radiolarian specimens of the multiplicative type have never discovered from the Gufeng Formation so far. Meanwhile, a specimen from the Gufeng Formation in the Anmenkou section shown by Kametaka et al. (2009, p. 117, fig. 7.18, identified as Ishigaum sp.) possesses a branching arm. The specimen can be classified as one of the supplemental type of Afanasieva and Amon (2016).

Age assignments

The age of the Gufeng Formation has been calibrated primarily based on fossil data. Ching (1960) discovered the conodont Jinogondolella nankingensis (Ching) in the basal mudstones of the Gufeng Formation in the Longtan area, Jiangsu. Subsequent studies have found this species in the basal mudstones of the Gufeng Formation in the Lower Yangtze region (e.g. Wang, 1995a; Kametaka et al., 2009). Jinogondolella nankingensis is an index species of the Roadian (Ogg et al., 2016). Meanwhile, Kametaka et al. (2009) also found ammonoids Shouchangoceras sp. and Erinoceras sp. from mudstones of the lower PNMM in the Anmenkou section, Anhui. The ranges of Shouchangoceras and Erinoceras are contained in the Wordian and the Roadian–Wordian, respectively (Zhao and Zheng, 1977); therefore, Kametaka et al. (2009) concluded that the age of the lower PNMM is Wordian and that of the SRM is Wordian or younger.

Ma et al. (2016) correlated conodont and radiolarian biozones in the Luojiaba section in western Hubei. They concluded that the Pseudoalbaillella globosa, Follicucullus monacanthus, and F. scholasticus radiolarian zones could be directly correlated with the Jinogondolella nankingensis gracilis, J. aserrata, and J. postserrata conodont zones.

In addition to the fossil data, Zhu et al. (2013) reported zircon U–Pb ages of 272.0 ± 5.5 Ma (MSWD = 2.6) and 271.5 ± 3.3 Ma (MSWD = 1.7) separated from volcanic ash beds within the basal shale strata of the Gufeng Formation in the Chaohu area, Anhui. The age of the boundary between the Kungurian (Cisuralian) and Roadian (Guadalupian) is 272.3 Ma according to the 2016 geologic time scale (Ogg et al., 2016), so that the zircon U–Pb ages can be correlated to the lowermost part of the Roadian. Zhang et al. (2010) correlated the conodont and radiolarian biozones across the Cisuralian-Guadalupian boundary and concluded that the base of the Roadian coincides with the first occurrence of Ps. globosa. Consequently, the zircon U–Pb ages are consistent with the fossil data, even though the taxonomy of Pseudoalbaillella globosa is debatable (Ito et al., 2016c).

In short, the Gufeng Formation is nearly consistent with the Guadalupian based on conodonts and the zircon U–Pb ages. In particular, the base of the Gufeng Formation should be near the boundary between the Cisuralian and Guadalupian. However, the top of the Gufeng Formation is uncertain because of fewer fossil occurrences and lack of numerical age dating.

Geochemical characteristics

Geochemical studies on the Gufeng Formation have increased since the 1990s (e.g. Lu and Qu, 1990; Xia et al., 1995; Yang and Feng, 1997). Siliceous rocks within the Maokou Formation, which is a heterotopic facies of the Gufeng Formation, have also been geochemically investigated (e.g. Zhou et al., 2009).

Origin of siliceous rock

Most previous studies have concluded that the siliceous rocks of the Gufeng Formation on the north margin are biogenic. The Al–Fe–Mn diagram defined by Adachi et al. (1986) and Yamamoto (1987) has generally been used in speculations about the origin of chert in the Paleozoic and Mesozoic (e.g. Du et al., 2007; Ito et al., 2016f). Most researchers have applied this diagram to the chert of the Gufeng Formation. Most previous studies date the analyzed samples in the biogenesis field, or near it, in the Al–Fe–Mn diagram but not near the hydrothermal field (e.g. Kametaka et al., 2005; Wang et al., 2008; Yang and Yao, 2008; Han et al., 2014). Meanwhile, a few studies have indicated the influence of hydrothermal activities in the Lower Yangtze region (Xia et al., 1995; Xie et al., 2013). Consequently, in general, a hydrothermal component barely contributed little to the composition of the rocks in the Gufeng Formation except in a few areas.

In contrast to the Yangtze region, a scattering of studies on the “Gufeng Formation” in the south margin indicate that the chert is likely hydrothermal. Fu et al. (2004) investigated the “Gufeng Formation” in Shaoyang in Hunan and showed that the chert plots in the hydrothermal field on the Al–Fe–Mn diagram. Shi et al. (2016) pointed out the differences in the chert formation processes between the north and south margins. Further research is necessary to interpret the origin of the siliceous rocks of the “Gufeng Formation” on the south margin because there are fewer studies pertaining to it compared to those on the Gufeng Formation in the north margin.

Origin of organic matter

In contrast to the studies on the origin of the siliceous rocks, a few studies have dealt with the origin of organic matter within the Gufeng Formation. Takebe et al. (2007) investigated organic matter in the black chert of the Anmenkou section using the van Krevelen diagram (atomic H/C ratio versus atomic O/C ratio). This diagram shows four types of kerogen according to the origin of the organic matter (van Krevelen, 1961). The analyzed data of Takebe et al. (2007) plotted in the field of type IV indicating reworked and highly oxidized organic material. Oxic weathering can cause an increase in the atomic O/C ratio of kerogen (e.g. Petsch et al., 2000). However, due to several geochemical results, such as the small variation of the atomic O/C ratio, S enrichment, and the inclusion of pyrites, Takebe et al. (2007) concluded that the black chert was not affected by oxic weathering and originated from terrestrial or reworked organic matter.

However, considering the high degree of maturity estimated in a subsequent study, the analyzed data by Takebe et al. (2007) were likely not primary. In general, kerogens subjected to increasing thermal stress move toward the lower left corner of the van Krevelen diagram (Hunt, 1995). This tendency has been reported by laboratory experiments (e.g. Kotarba and Lewan, 2004; Lewan and Kotarba, 2014; Takahashi and Suzuki, 2017). According to the geochemical works by Du et al. (2015), the vitrinite reflectance (VR %) and Rock-Eval Tmax of siliceous and muddy rocks in the Gufeng Formation have a range of 1.2–2.0% and 460–560°C, respectively. These values indicate a high degree of maturity. Under such a high degree of maturity, the van Krevelen diagram is not applicable to estimation of the origin of the organic matter.

The supply of terrestrial material to the Gufeng Formation is irrefutable due to several observed facts as mentioned in the previous section, such as the presence of intercalated clastics within the Gufeng Formation. The origin of the organic matter in the Gufeng Formation is debatable; therefore, further data such as the stable carbon isotopic composition of the organic matter are needed to discuss its origin.

Sedimentary environment

There had been speculations as to the sedimentary environment of the Gufeng Formation based on lithology and radiolarian faunal comparison. Kong and Gong (1987) postulated that the siliceous rocks of the Gufeng Formation were formed in a deep-sea environment resulting from rift faulting because the radiolarian fauna is similar to the Japanese assemblage. Zhu (1989) concluded that the Gufeng Formation was deposited in an intraplatformal environment. Since the 1990s, a geochemical approach to speculations about the sedimentary environment of the Gufeng Formation has been adopted. Such studies have generally concluded that the Gufeng Formation formed in a continental shelf environment (e.g. Kametaka et al., 2005).

Murray (1994) placed the pelagic and continental margin fields in the Fe2O3/TiO2 versus Al2O3/(Al2O3 + Fe2O3) diagram on the basis of chert from continental margin, pelagic, and ridge-proximal environments, ranging from the Early Paleozoic to the Neogene. To speculate about the sedimentary environment, the Murray diagram has been used (e.g. Hara et al., 2010; Ito et al., 2016f; Kemkin et al., 2017). Most of the analyzed samples from the Gufeng Formation plot in the continental margin field in the diagram (e.g. Kametaka et al., 2005; Wang et al., 2008; Yang and Yao, 2008; Han et al., 2014).

Redox conditions and changes

Redox conditions and changes during the deposition of the Gufeng Formation have been studied in detail, especially in the Lower Yangtze (Kametaka et al., 2005) and the Middle Yangtze (Shi et al., 2016) regions. In short, the redox condition of the Gufeng Formation in the Lower Yangtze region changed from aerobic to suboxic to anoxic, whereas that in the Middle Yangtze region changed from oxic to anoxic to suboxic. In this section, we focus on the Lower and Middle Yangtze regions based on the discussions and speculations of the previous studies.

The Anmenkou section in the Lower Yangtze region is divided into the PNMM and SRM in ascending order (Kametaka et al., 2005). The lowermost mudstone of the PNMM contains glauconite pellets. Glauconites are generally formed under aerobic shallow water (e.g. Tucker, 1991; Prothero and Schwab, 1996). Consequently, the lower PNMM was formed under such conditions.

The upper PNMM contains abundant phosphate nodules. Phosphate nodules are generally formed under oxygen-minimum zones during low clastic supply on the outer shelf and upper slope (e.g. Tucker, 1991; Prothero and Schwab, 1996; Trappe, 1998). Kametaka et al. (2005) therefore concluded that the upper PNMM is formed under suboxic conditions.

Kametaka et al. (2005) concluded that the SRM of the Anmenkou section was formed in a continental margin under anoxic conditions on the basis of several features of the chert, such as high Mo, Ni, Cu, and V and extremely low Mn contents. These elements are used as an indicator of the redox condition of the sediments. For example, Mo is scavenged by Mn-oxides under oxic conditions (Shimmield and Price, 1986); Mo is dissolved and remobilized under suboxic conditions (Shimmield and Price, 1986; Chaillou et al., 2002; McManus et al., 2002); and Mo forms strong associations with sulfide, concentrating in deposits (Vorlicek et al., 2004). Nickel and Cu also concentrate in sediments under reducing conditions (Calvert and Pedersen, 1993). Vanadium in deposits primarily originates from continental flux or inclusion in seawater. The V and U originating from continental flux decrease in proportion to the Al concentration. Conversely, the seawater-derived V in sediments depends on the redox condition of the deposits (Hori et al., 2000). Manganese generally deposits as Mn-oxide (MnO2) under oxidizing conditions, whereas it becomes Mn2 + and readily secedes from deposits under reducing conditions (Calvert and Pedersen, 1993).

In the Middle Yangtze region, Shi et al. (2016) subdivided the Maocaojie section into three units. The lower unit consists primarily of siliceous rocks; the middle unit is composed of limestone, carbonaceous mudstone, and muddy chert; and the upper part consists of muddy chert, siliceous mudstone, and calcareous mudstone. The geochemical results by Shi et al. (2016) indicated that the lower, middle, and upper units were formed under oxic, suboxic, and anoxic conditions, respectively. On the basis of comparison to the stratigraphic change of the radiolarian component, Shi et al. (2016) concluded that the widespread anoxia was promoted by the elevated primary productivity.

Concluding remarks

In this article, we reviewed the lithostratigraphy, radiolarian occurrences with biostratigraphy, and geochemical characteristics of the Gufeng Formation. Here we summarize the lithostratigraphy and redox conditions of the Gufeng Formation of the Anmenkou and Maocaojie sections as representative examples of the Lower and Middle Yangtze regions, respectively (Figure 9).

Figure 9.

Schematic model showing vertical changes of lithology, radiolarian fauna, and redox condition. Numerical ages with white arrows indicate zircon U–Pb ages of 272.0 ± 5.5 Ma (MSWD = 2.6) and 271.5 ± 3.3 Ma (MSWD = 1.7) separated from volcanic ash beds within the basal shale strata of the Gufeng Formation in Chaohu area, Anhui by Zhu et al. (2013). Lop., Lopingian; Cis., Cisuralian; F., Follicucullus; R., Ruzhencevispongus; Ps., Pseudoalbaillella; MK, Maokou Formation; WX, Wuxue Formation; YP, Yinpin Formation; UU, Upper Unit.

img-z14-1_261.jpg

In the Anmenkou section of the Lower Yangtze region, the dominant rock facies of the Gufeng Formation are nodule-bearing muddy rock, chert, and muddy rock in ascending order. The former is called the PNMM; the latter two are called the SRM by Kametaka et al. (2002, 2005). Based on the lithology, the lower PNMM formed under aerobic shallow water and the upper PNMM formed under suboxic conditions (Kametaka et al., 2005). The geochemical characteristics of the SRM indicate that it was formed under anoxic conditions (Kametaka et al., 2005).

In the Maocaojie section of the Middle Yangtze region, the dominant rock facies of the Gufeng Formation are chert, muddy rock with carbonate, and muddy rock (Shi et al., 2016). The geochemical results indicate that these parts were formed under oxic, anoxic, and suboxic conditions, respectively (Shi et al., 2016).

In contrast to the Lower and Middle Yangtze regions, fewer studies have focused on the Gufeng Formation in the Upper Yangtze region (e.g. Kuwahara et al., 2007c, 2008a; Zhou et al., 2009). In the recent decade, upper Capitanian carbonates of the Maokou Formation in the Chaotian section in northern Sichuan have been studied in detail (e.g. Lai et al., 2008; Saitoh et al., 2013, 2014; Chen et al., 2011). Further studies on stratigraphic change in the lithostratigraphy, radiolarian biostratigraphy, and geochemical characteristics of the Gufeng Formation and chert beds within the carbonates of the Maokou Formation in the Upper Yangtze region should reveal the paleoenvironmental developments on the north margin of the South China block.

Acknowledgements

We thank Weihong He (China University of Geosciences, Wuhan) and Masao Kametaka (Dia Consultant Co. Ltd.) for critical review on this manuscript and valuable suggestions. Comments given by Associate Editor, Toshiyuki Kurihara (Niigata University), improved greatly this manuscript. We are most grateful to the following students and PhD students of China University of Geosciences, Wuhan, for kind help for fieldwork of the Gufeng Formation in Chaohu (Anhui) and Jianshi (Hubei) and collecting and reading the Chinese articles: Lei Zhang, Yong Lei, Qing Hu, Lei Shi, Jun Shen, Wenchao Cao, Qiangfen Ma, Qi Wu, Hailong Gao, and others. This study has been financially supported by NSFC (40839903 and 40921062) and “111” Project (B08030) of China University of Geosciences, Wuhan and “Niigata University's Scholarship Program for Graduate School Students Conducting Research Abroad”.

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Appendices

Author contributions

T. I. initiated the study and wrote most part of the paper. K. U. T. re-wrote mainly the chapter of the Origin of organic matter. Q. F. and A. M. supervised this study and writing of the paper. All authors contributed to the writing of the paper.

© by the Palaeontological Society of Japan
Tsuyoshi Ito, Koji U. Takahashi, Atsushi Matsuoka, and Qinglai Feng "The Guadalupian (Permian) Gufeng Formation on the North Margin of the South China Block: A Review of the Lithostratigraphy, Radiolarian Biostratigraphy, and Geochemical Characteristics," Paleontological Research 23(4), 261-280, (1 October 2019). https://doi.org/10.2517/2018PR025
Received: 23 March 2018; Accepted: 17 December 2018; Published: 1 October 2019
KEYWORDS
Gufeng Formation
lithology
radiolarian biostratigraphy
Sedimentary environment
South China block
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