Luo et al. (1980) first proposed the Paragloborilus–Siphogonuchites Zone as the second Cambrian SSF Zone in the eastern Yunnan area. However, the significant problem of this zone is that all the index fossils can range into other biozones. In particular, S. triangularis has an extremely long range from Zone Ⅰ to Ⅲ. Thus, Steiner et al. (2007) established the Paragloborilus subglobosus–Purella squamulosa Assemblage Zone using the lowermost occurrence of P. subglobosus and Zhijinites longistriatus to define the lower boundary and the highest occurrence of P. squamulosa to define the upper boundary. Yang et al. (2014) excluded Z. longistriatus as the index fossil for its occurrence only in Zone Ⅲ and reassigned Oelandiella korobkovi (index fossil of Zone Ⅲ in Steiner et al., 2007) as the index fossil of Zone II for its most common occurrence in Zone II and only a few occurrences in Zone Ⅲ. It’s worth noting that all the index fossils except P. squamulosa (or Purella) can range into Zone Ⅲ. In addition, on the Yangtze Platform, P. squamulosa is not a wide-occurring species, and is only reported from a few sections in eastern Yunnan (Xiaotan, Xianfeng, and only P. elegans at Laolin) and northern Sichuan (Shatan) (Steiner et al., 2004, 2007; Yang et al., 2014). In western Hubei, only another species, P. antiqua, had been reported by Guo et al. (2014), but it was reinterpreted as maikhanellid sclerites by Steiner et al. (2020). All the above facts have made it difficult and problematical to recognize Zone II in the shallow facies on the Yangtze Platform, especially in southern Sichuan and western Hubei (Steiner et al., 2004, 2007, 2020; Yang et al., 2014; Yang and Steiner, 2021). Anyway, it’s still practicable to recognize Zone II based on the fossil combinations and their occurrences below the FAD of W. crosbyi in some sections with relatively successive strata (Meishucun, Lishuping, and Laolin section, Yang et al., 2014).

At the Fandian section, the SSF assemblage recovered from the 12.1–14 m interval of the basal Upper Member of the Maidiping Formation is temporarily assigned to the problematic Zone II (?) for the lack of Purella. Firstly, all the fossil elements in this interval are common in Zone II in eastern Yunnan, such as P. subglobosus, O. korobkovi, A. yangtzensis, O. rostriptuetus, cf. Maikhanella sp, B. simplex, C. subcurvata, I. maidipingensis, S. triangularis, P. sinensis, and Halkieria (Figure 2). Secondly, none of the three index fossils of Zone Ⅲ (FAD of W. crosbyi at 14.1 m; FAD of Z. longistriatus at 18 m; and no discovery of Aldanella attleborensis) occurs in this interval. Thirdly, the results of our continuous high-resolution carbon isotope and field observation show that there is no obvious hiatus or disconformity in the Upper Member of the Maidiping Formation (11.2–20.2 m) and this Zone (12.1–14 m) is below the onset of the ZHUCE excursion (Figure 2), which is consistent with the typical sections in eastern Yunnan (Li et al., 2009; 2013; Yang et al., 2014; Steiner et al., 2020; Figure 5). However, considering the much lower thickness of this zone compared with that in the sections in eastern Yunnan (Yang et al., 2014) and the lack of fossils below 12.1 m at the Fandian section, this problematic Zone II (?) at the Fandian section probably is not complete and lacks its lower interval of unknown thickness.

This fossil assemblage was first proposed by Qian et al. (1996) as the Heraultipegma yunnanensis Zone, but it was not defined in much detail. Later, Steiner et al. (2007) considered that H. yunnanensis was a junior synonym of W. crosbyi and therefore renamed this zone as the W. crosbyi Assemblage Zone, with the lower boundary defined by the first appearance of W. crosbyi and the upper boundary drawn by the highest occurrence of Aldanella yanjiahensis (a junior synonym of Aldanella attleborensis) and Oelandiella korobkovi. Yang et al. (2014) added Zhijinites longistriatus as a new index fossil of Zone Ⅲ for its FAD almost the same or slightly later than W. crosbyi and excluded O. korobkovi for its common occurrence in Zone II rather than Zone Ⅲ. In addition, Yang et al. (2014) also pointed out that the operculum-like fossil, Emarginoconus mirus, occurred only in Zone Ⅲ and may be another potential auxiliary index fossil, consistent with its stratigraphic distribution observed herein.

In the previous studies, W. crosbyi had not been reported from the Fandian section (Yin et al., 1980; He et al., 1984). Herein, W. crosbyi was recovered from the two horizons of the upper member of the Maidiping Formation (8 specimens in total from horizons 14.1 m and 18 m in Figure 2; Figures 4F–I). In addition, the lowest occurrences of Z. longistriatus (Figures 3AA–AE) and E. mirus (Figures 3Y,X) are respectively at 18 m and 16 m and are higher than that of W. crosbyi, being consistent with their stratigraphic sequences in eastern Yunnan. It’s noteworthy to mention that samples from horizon 13.5 m yield many newly occurring species compared with the underlying samples. But most of these species are still typical elements of Zone II in eastern Yunnan. The few specimens of W. crosbyi found in the Fandian section (only one at 14.1 m and seven at 18 m) may suggest that W. crosbyi could also exist below its lowest occurrence at 14.1 m, where it is hard to find for its rarity. Considering no hiatus was observed in the interval between 12.1 and 14.1 m, in the future more sample collection with much higher resolution for SSF extraction in this interval is a necessary and reliable way to check this assumption. At present, we temporarily prefer to place the lower boundary of the SSF Zone Ⅲ at the lowermost occurrence horizon of W. crosbyi (14.1 m) at the Fandian section.

Yang and Steiner, (2021) mentioned that many SSFs, such as Annelitellus, Obtusoconus, Ocruranus, and Paracarinachites, previously discovered only in Zone II in eastern Yunnan, can range upwards to Zone Ⅲ in the adjacent Maidiping section. This situation is similar to that in the Fandian section (Figure 2). Yang and Steiner (2021) gave two possible explanations for this fact: either all these fossils indeed have a higher stratigraphic range than previously discovered in eastern Yunnan; or these fossils were redeposited by the reworking of the sediment from the older strata. Herein, we prefer the former explanation because there is no distinct difference in fossil preservation between SSF specimens in Zone II (?) and Zone Ⅲ in the Fandian section. In addition, our own unpublished data from the Xiaotan section in eastern Yunnan also shows that the basal Zone Ⅲ contains such fossil elements that previously only occurred in Zone II. It's necessary to point out that the specimens preserved as steinkerns and generally named as Protohertzina sp. nearly occurred in all the samples regardless of their rare number in Zone II and Ⅲ (Figure 2; Figures 3S,T). This is quite different from other sections in the Yunnan and Sichuan regions. Herein, we prefer to assign them to some other younger species of Protohertzina rather than to the older species like Protohertzina unguliformis.

Although the basal part of the Maidiping section at the Fandian section is now absolutely covered by weathering residues and vegetations, but in the description of He et al. (1984, p. 73), the Maidiping Formation was fully exposed with the ca. 29.5m-thick Lower Member, and the basal ca. 6 m interval contains a few fossils, such as Anabarites trisulcatus, Conotheca, and Archaeooides, which are typical elements of the SSF Zone Ⅰ on the Yangtze Platform. Thus, we infer that the basal part of the Maidiping Formation at the Fandian section yields the Anabarites trisulcatus–Protohertzina anabarica Assemblage Zone.

As one of the most classical sections in southern Sichuan for the study of early Cambrian stratigraphy of the Yangtze Platform, the bio- and chemo-stratigraphy from the Maidiping section had got quite detailed studies by the pioneer researchers (Qian, 1977, 1989; Yin et al., 1980; He et al., 1984; Brasier et al., 1990; Qian et al., 1999). In the review of the SSF biostratigraphy of China, Qian et al. (1999, p.79-80, Figures 3, 4) subdivided the Maidiping Formation into 3 SSF biozones (Zones Ⅰ, II, Ⅲ) at the Maidiping section. However, recently, Yang and Steiner (2021) consider that the top 8 m (bed 36–39) of the Maidiping Formation, corresponding to the Zones II and Ⅲ in Qian et al. (1999), should only belong to the Zone Ⅲ, because below the lowest occurrence of Watsonella crosbyi, there is no Purella squamulosa in the less than 1m-thick interval of Zone II in Qian et al. (1999), and the fossil composition of this interval is similar to the above strata (Yang & Steiner, 2021). In addition, a disconformity has been observed below the base of the SSF Zone Ⅲ, and it can also be confirmed by the abrupt excursion of the δ¹³C carbon isotope (from –1.34‰ to +2.12‰ in Figure 2 of Yang & Steiner, 2021). This disconformity and the below 12m-thick dolostone with barren fossils (bed 35) might correlate to Zone II based on the restriction of the well-defined Zone Ⅰ and Ⅲ (Yang & Steiner, 2021). While in the Fandian section, no such hiatus or disconformity has been found in the Maidiping Formation. The δ¹³C value of the Fandian section (Figure 2, original data see Supplementary Material and Table 1 in Xiong et al., Forthcoming 2022) is relatively stable among –2‰ to –1‰ in the Lower Member (0–11 m) of the Maidiping Formation; gradually increases to about 0‰ (11–12.3 m) at the basal part of the Upper Member and keeps steady around 0‰ in a short interval (12.3–14 m, Zone II) below the lowest occurrence of Watsonella crosbyi; then from the base of the Zone Ⅲ the δ¹³C value increases fast but gradually from –0.141‰ to +3.432‰ (14.1–15.4 m) and oscillates between +0.941‰ and +3.432‰ in the rest part of the Upper Member (15.4–18.8 m). The δ¹³C value of the Fandian section records the relatively complete ZHUCE, while the ZHUCE in the Maidiping section, recognized by Yang & Steiner (2021, Figure 2), is probably equal to the top oscillating interval (14.1–15.4 m) of the Fandian section (Figures 2, 5). If the correlation of this positive excursion interval between the Fandian and Maidiping sections is the real case, the earliest/lowest occurrence of Watsonella crosbyi in the Maidiping section could be slightly later/higher than that in the Fandian section herein. It’s worthy to mention that both the maximum of this positive excursion at Fandian (+3.432‰) and Maidiping (+2.4‰) sections are much smaller than that of the Xiaotan section (+7.2‰ in Li et al., 2013), the referential section in eastern Yunnan, but close to that of the Lishuping (+2.69‰ in Steiner et al., 2020) and Laolin (+3.5‰ in Li et al., 2009) sections (Yang & Steiner, 2021). This may be due to the discrepancies in the local water environment as emphasized by Steiner et al. (2020). At least such positive excursion trends in these sections are comparable by the restriction of the SSF assemblage. The basal 11.2m-thick gray dolostone with no discovery of fossils at the Fandian section herein (same as He et al., 1984, p. 73) is comparable to the 12m-thick monotonous dolostone (bed 35) (containing rare indeterminate fossil fragments) at the Maidiping section described by Yang & Steiner (2021). For the lack of useful fossils, it is difficult to determine the age of this interval, which may correlate to either the lower part of Zone II or the upper part of Zone Ⅰ. In the description of the Fandian section by He et al. (1984, p. 73), the basal ca. 6m-thick interval of the fully exposed Maidiping Formation bears some typical fossils of the SSF Zone Ⅰ, such as Anabarites trisulcatus, Conotheca and Archaeooides. Thus, the basal Maidiping Formation at the Fandian section may also contain the SSF Zone Ⅰ and correlate to the beds 31 to 32 (or 34) of the Maidiping section (Figure 5). Rugatotheca and Ganloudina, together with both index fossils of the SSF Zone Ⅰ (P. anabarica and A. trisulcatus), have been reported from the basal Maidiping Formation at the Maidiping section (Yang and Steiner, 2021, Figures 2, 3). In eastern Yunnan, both P. anabarica and A. trisulcatus occurred not lower than the base of the Zhongyicun Member of the Zhujiaqing Formation and above the BACE (Basal Cambrian Carbon isotope Excursion) (Li et al., 2001; Steiner et al., 2007; Li et al., 2009, 2013; Yang et al., 2014). While the δ¹³C curve above the base of the Maidiping Formation from the Maidiping section is relatively steady and does not show the clear BACE (Yang & Steiner, 2021, Figure 2). Thus, we consider the base of the Maidiping Formation of the Maidiping section is probably above the base of the Zhongyicun Member at the Xiaotan section (reference Terreneuvian section in eastern Yunnan). However, in the adjacent Daqiao section, the basal Maidiping Formation (about 1 m) bears some common elements (Rugatotheca, Ganloudina, Olivooides) of the fossil assemblage at the base of the Daibu Member of the Zhujiaqing Formation at the Xiaotan section (Yang et al., 2016, Figure 1), together with Paracanthodus, Quadrosiphogonuchites, and Aetholicopalla and the possible P. anabarica and A. trisulcatus (Yang and Steiner, 2021, Figure 3). Furthermore, the δ¹³C results from the Daqiao section show a prominent negative excursion at the basal part of the Maidiping Formation, which may be correlated with the BACE at the Xiaotan section (Figure 5; Wusihe-Daqiao section in Xiong et al., Forthcoming 2022). Although the absolute value of the nadirs between Daqiao (−3.861‰) and Xiaotan (−12‰ in Li et al., 2013) sections shows quite a large discrepancy, this may be caused by the difference in regional aquafacies (see detailed discussion in Steiner et al., 2020). However, it’s also possible that this negative excursion of the Daqiao section could be compared one interval with the less negative δ¹³C curve of the upper Zone Ⅰ at the Xiaotan section, because Yang and Steiner (2021) mentioned there is an obvious hiatus (karst surface) at the boundary between the Maidiping and Dengying formations at the Daqiao section. Combining the above bio- and chemo-stratigraphic evidence, we tentatively infer that the base of the Maidiping Formation at the Daqiao section may roughly correlate to the upper Daibu Member of the Zhujiaqing Formation at the Xiaotan section (Figure 5).

Three SSF zones (Zone Ⅰ to Ⅲ), the BACE and ZHUCE carbon isotope excursions can be well recognized from the Zhujiaqing Formation in eastern Yunnan (Qian, 1989; Qian & Bengtson, 1989; Zhou et al., 1997; Li et al., 2001, 2011; Steiner et al., 2007; Li et al., 2009, 2013; Yang et al., 2014; 2016). In the Xiaotan and Laolin sections with the most continuous and well-studied Terreneuvian sequence, the lowermost occurrence of Watsonella crosbyi is around the onset of the ZHUCE (Li et al., 2001; 2004; Li et al., 2009; 2013; Yang et al., 2016). Herein, we consider the SSF Zone II “(?)”, Ⅲ and the ZHUCE in the Upper Member of the Maidiping Formation at the Fandian section can correlate to that from the upper Zhongyicun Member and the Dahai Member of the Zhujiaqing Formation in eastern Yunnan (Figure 5), while the basal Maidiping Formation bearing the typical SSF Zone Ⅰ elements (He et al., 1984) probably correlates to the basal Zhongyicun Member in eastern Yunnan (Figure 5). In western Hubei, the Yanjiahe Formation at the Gunziao (or Aijiahe) section records the most continuous and complete Terreneuvian succession. Guo et al. (2014, 2021) recognized 3 SSF zones (Ⅰ to Ⅲ) in the Yanjiahe Formation. However, Steiner et al. (2020) noted that the Purella antiqua recognized by Guo et al. (2014) should be maikhanellid sclerites and considered that SSF Zone II in Guo et al. (2014) belongs to the upper part of SSF Zone Ⅰ, which means that SSF Zone II is also lacking in the Yanjiahe Formation. To resolve this controversy, the more careful systematic study of the three-dimensional SSFs retrieved by the acid process from this interval is the only reliable and practicable way (Guo et al., 2020). There is no doubt that the SSF Zone Ⅲ, including its index fossils, Watsonella crosbyi and Aldanella attleborensis, is merely restricted in the top 2.2m-thick Bed 5 (Guo et al., 2014; 2020; 2021) or 1.1m-thick Unit 4 (Steiner et al., 2020) of the Yanjiahe Formation. However, Steiner et al. (2020) point out that there was a mixture of the reworked older sediments and fossils together with the younger ones and that there existed a long-time hiatus in this short unit 4. Thus, the SSF Zone Ⅲ in western Hubei may be incomplete and lack the basal and/or top parts (Steiner et al., 2020, fig. 11; Figure 5). In contrast, Guo et al. (2020) suggest an alternative explanation that this interval consists of a thin background deposit with abundant fossils and a slight thick storm-formed deposit containing the broken sediments and fossils from the underlying background deposit. And, some fossils previously known in the older strata occurring in this bed may be due to their longer stratigraphic ranges (Guo et al., 2020). Guo et al. (2020) also indicate that it’s suitable to temporarily set the lower boundary of SSF Zone Ⅲ at the base of Bed 5 of the Yanjiahe Formation, but it’s yet to be confirmed whether Watsonella crosbyi and Aldanella attleborensis can exist in the underlying Bed 4 with scarce fossils. More detailed work is needed in the future. When it comes to the carbon isotope stratigraphy of the Yanjiahe Formation, based on the SSF biostratigraphy, it’s possible that the prominent positive excursion interval (P2 in Ishikawa et al., 2008) below the lowest/first occurrence of W. crosbyi and A. attleborensis (Guo et al., 2014, 2021; Steiner et al., 2020) from the middle and upper Yanjiahe Formation may correlate to one interval of the δ¹³C curve in the Zhongyicun Member belonging to SSF Zone Ⅰ or II (Li et al., 2013; Steiner et al., 2020, Figure 11) rather than the ZHUCE in the Dahai Member of the Zhujiaqing Formation in eastern Yunnan. Steiner et al. (2020) reassigned the basal part of the Shuijingtuo Formation in Ishikawa et al. (2008, p. 197, 77.91–78.95m) as unit 4 of the Yanjiahe Formation. Both their results of the δ¹³C of conglomeratic carbonate in the lower part of unit 4 show a clear positive excursion (with few repeated oscillations in Ishikawa et al., 2008, Figure 3; Figure 5), which may be caused by the redeposition of the sediments with a high positive δ¹³C value from the underlying unit 3 (Steiner et al., 2020). While the δ¹³C of the limestone matrix in the upper unit 4 are relatively steady in negative (–4 to –2‰ in Ishikawa et al., 2008, Figure 3; about –1‰ in Steiner et al., 2020, Figure 10), which more likely represents the original sedimental signal and correlates to the lower part of ZHUCE (Steiner et al., 2020). However, the topmost ZHUCE in the Xiaotan section also shows such a short but relatively steady and negative curve (Li et al., 2013). Anyway, herein, we think it’s uncertain to correlate this extremely short and problematic δ¹³C in the top Yanjiahe Formation at the Gunziao (or Aijiahe) section to other sections on the Yangtze Platform.

In the northern Sichuan and southern Shaanxi, the SSFs from the Kuanchuanpu Formation have also been widely studied, with 3 SSF zones recognized (Xing et al., 1984; Qian et al., 1999; Steiner et al., 2004). Recently, Steiner et al. (2020, Figure 11) marked all the three zones (Zones Ⅰ to Ⅲ) with an incomplete carbon isotope curve in the Kuanchuanpu Formation. It's worth mentioning that the occurrences of the key index fossils of SSF Zone II and Ⅲ in this area are quite rare compared with those of Zone Ⅰ. W. crosbyi and A. attleborensis were merely reported in a 1m-thick bed in the upper Kuanchuanpu Formation at the Yuanjiaping section (Xing et al., 1984, p. 118, pls. 26, 27). In the nearby Xuanjiangping section, they may have relatively long stratigraphic ranges (ca. 7 m in Qian et al., 1999, Figure 3-11), but none of them had been discovered in the detailed description of this section by Qian (1989, p. 18). Purella squamulosa only occurred in the top 16-cm-thick bed of the Kuanchuanpu Formation (5.75-m-thick) at the Shatan section (Steiner et al., 2004). Thus, the distribution and time range of the SSF Zone II and Ⅲ in different sections of northern Sichuan and southern Shaanxi may also be quite variable or even missing. In addition, no such positive δ¹³C excursions like the ZHUCE in eastern Yunnan and the Fandian section herein have been reported in the associated strata in this area. Herein, based on the occurrences of W. crosbyi, A. attleborensis, and P. squamulosa reported from the Kuanchuanpu Formation (Xing et al., 1984; Qian et al., 1999, Figure 3-11; Steiner et al., 2004; and references therein), we tentatively correlate the SSF Zones II (?) and Ⅲ from the Maidiping Formation of the Fandian section to that from the upper/top Kuanchuanpu Formation.

In general, the key index fossils of SSF Zone Ⅰ to Ⅲ have wide distributions along the western margin of the Yangtze Platform and almost have a synchronous FAD in different areas, which makes them more reliable and useful for the regional stratigraphic subdivision and correlation compared to the variable δ¹³C curve. At present, W. crosbyi has been discovered in most of the classical Terreneuvian sections on the Yangtze Platform, while the nearly coeval A. attleborensis has relatively restricted distribution and yet to be extensively searched in southern Sichuan. Thus, the FAD of W. crosbyi is more suitable and useful for the definition of the base of Cambrian Stage 2 (Xiaotanian) in South China. And the onset of the ZHUCE carbon isotope excursion almost corresponds to the FAD of W. crosbyi in the Xiaotan and Laolin sections in eastern Yunnan and the Fandian section in southern Sichuan, indicating that ZHUCE can be an auxiliary maker to define the lower boundary of the Xiaotanian in South China under the control of SSF biostratigraphy.

Watsonella crosbyi was almost globally distributed in the upper Terreneuvian, such as, Siberia, Mongolia, South China, Australia, France, and Avalonia (see detailed list in Jacquet et al., 2017). It has been proposed to be a suitable candidate for the index fossil to define the base of the Cambrian Stage 2 (Li et al., 2011; Peng & Babcock, 2011; Zhu et al., 2019). However, W. crosbyi has been skeptical about the utility of global correlation due to its supposed long stratigraphic range (Parkhaev et al., 2012; Landing et al., 2013). The new bio, chemo, and chrono-stratigraphic progress of the Terreneuvian suggest that W. crosbyi had almost synchronous FAD in the areas mentioned above and its occurrence is in the lower to middle Cambrian Stage 2 (Brasier et al., 1996; Landing et al., 1989; Esakova & Zhegallo, 1996; Kouchinsky et al., 2007, 2017; Li et al., 2009, 2013; Maloof et al., 2010; Li et al., 2011; Devaere et al., 2013; Landing & Kouchinsky, 2016; Smith et al., 2016; see detailed discussion in Jacquet et al., 2017). However, as referred by Jacquet et al. (2017), the poorly preserved specimens on the bedding surfaces from the possible trilobite bearing zone in Avalonia (Bengtson & Fletcher, 1983; Landing et al., 2013) need to be reinvestigated. It’s noteworthy that the FAD of W. crosbyi all occurred below the prominent δ¹³C positive excursions in South China (ZHUCE in Zhu et al., 2006; Li et al., 2009, 2013), Siberia (I′ in Kouchinsky et al., 2007; Landing & Kouchinsky, 2016; Kouchinsky et al., 2017), Mongolia (peak “F” in Brasier et al., 1996; 5p in Smith et al., 2016) and Avalonia (Landing & Kouchinsky, 2016), which also proves that the ZHUCE δ¹³C positive excursion can be a useful auxiliary maker to define the base of Cambrian Stage 2 under well-constrained biostratigraphy.

Herein, based on the SSF biostratigraphic and carbon isotope stratigraphic correlations (ZHUCE), we consider that the Watsonella crosbyi Zone in the Yangtze Platform can be correlated to the Watsonella crosbyi Zone in Siberia (Kouchinsky et al., 2007; 2017), the Watsonella crosbyi Zone at the upper Bayangol Formation in the Western Mongolia (Esakova and Zhegallo, 1996; Smith et al., 2016), the Watsonella crosbyi–Oelandiella korobkovi Interval Zone in Montagne Noire of France (Devaere et al., 2013), the Watsonella crosbyi and Aldanella sp. cf. golubevi cooccurring strata in South Australia (Jacquet et al., 2017) and the Watsonella crosbyi Zone in the Avalon region (Landing et al., 1989).