Ediacaran cap dolomite of Shennongjia, northern Yangtze Craton, South China

Sedimentary model of the Ediacaran Doushantuo cap carbonates from the southeastern margin of the Yangtze Block: Evidence from carbon and oxygen isotopes and elemental geochemistry

“…Previous researches about δ 13 C and δ 18 O isotopes of the Ediacaran cap carbonates were concentrated in the southeastern margin of the Yangtze Block and the Three Gorges of the Yangtze River (Chen et al, 2013, 2015; Furuyama et al, 2017; Jiang, Sohl, & Christie‐Blick, 2003; Jiang, Kennedy, & Christie‐Blick, 2003; Jiang, Shi, & Zhang, 2006; Jiang, Kennedy, & Christie‐Blick, 2003; Jiang et al, 2007, 2011; Lang et al, 2016; Li et al, 2017; Tahata et al, 2013; Wang, Guan, et al, 2017; Xiao et al, 2012; Zhou & Xiao, 2007; Zhou et al, 2007; Zhu et al, 2013), but less attention has been paid to the Ediacaran cap carbonates in northern margin of the Yangtze Block. δ 13 C and δ 18 O isotopes of the Ediacaran cap carbonates from multiple sections in the Shennongjia and Chengkou areas on the northern margin of the Yangtze Block have been increasingly reported in recent years (Kuang et al, 2019, 2022; Wang, Wang, et al, 2017). The Ediacaran cap carbonates are only around 1 m thick in the Shengnongjia area, commonly thinner than those in other places of the Yangtze Block.…”

“…Cailteux et al, 2015; Hoffman et al, 2011; Mickala et al, 2014), Kalahari (Hoffman et al, 2011, 2017), India (Jiang, Sohl, & Christie‐Blick, 2003; Kaufman et al, 2006), Laurentia (e.g., Creveling et al, 2016; Kunzmann et al, 2017; Macdonald et al, 2010; Macdonald, McClelland, et al, 2009; Prave et al, 2009), South China (Huang et al, 2009, 2011, 2013; Jiang et al, 2007, 2008, 2011; Jiang, Kennedy, et al, 2006; Jiang, Kennedy, & Christie‐Blick, 2003; Jiang, Shi, & Zhang, 2006; Tahata et al, 2013; Wang et al, 2008, 2014; Wang, Wang, et al, 2012; Xiong et al, 2013, 2014; Zhao et al, 2018; Zhou et al, 2007, 2010; Zhou, Luo, et al, 2017; Zhou & Xiao, 2007), Siberia (Sovetov & Komlev, 2005; Sovetov & Le Heron, 2016), Tarim (Shen et al, 2008; Xiao et al, 2004), Tuva‐Mongolia (Macdonald & Jones, 2011; Macdonald, Jones, & Schrag, 2009), and West Africa (Hoffman, 2011; Nédélec et al, 2007; Porter et al, 2004; Shields et al, 2007). As these Ediacaran cap carbonates were formed in transgressive system tracts (TST) in the process of rapid sea‐level rise after the Marinoan glacier ablation (Kennedy, 1996; Kuang et al, 2019, 2022; Mei et al, 2006; Wang, Wang, et al, 2017; Zhou et al, 2010), they generally share the following distinctive features: (1) direct overlying the Marinoan glacial diamictites, which are usually interpreted as a precursor of the Marinoan terminal deglaciation; (2) remarkably thin (usually only meter‐ to decameter‐thick) but laterally continuous strata (Hoffman et al, 2017); (3) unusual sedimentary structures, such as tepee‐like structures, tube‐like structures, sheet‐cracks and isopachous cemented brecciations (Hoffman &amp...…”

“…Ediacaran Doushantuo cap carbonates in South China are widespread from a platform (or tidal flat) to a basin environment and well‐preserved in most parts of South China, mainly in the southeastern margin of the Yangtze Craton (Ader et al, 2009; Furuyama et al, 2017; Huang et al, 2013; Jiang et al, 2007, 2008, 2010, 2011; Jiang, Kennedy, et al, 2006; Jiang, Kennedy, & Christie‐Blick, 2003; Jiang, Shi, & Zhang, 2006; Jiang, Sohl, & Christie‐Blick, 2003; Lang et al, 2016, 2018; Li et al, 2017; McFadden et al, 2008; Sato et al, 2016; Shen et al, 2005; Tahata et al, 2013; Wang et al, 2005, 2008; Wang, Guan, et al, 2017; Wang, Wang, et al, 2012; Xiao et al, 2012; Zhou et al, 2004, 2007, 2010; Zhou & Xiao, 2007; Zhu et al, 2007) and minor in the northern margin of the Yangtze Craton (Kuang et al, 2019, 2022; Wang, Wang, et al, 2017; Zhu et al, 2013). However, whether they were deposited in different environments from slope to deepwater basin facies or not remains controversial (Hoffman et al, 2007, 2011; Hoffman & Macdonald, 2010; Jiang et al, 2007; Jiang, Sohl, & Christie‐Blick, 2003; Kuang et al, 2019, 2022). Some studies over the past two decades have demonstrated the obvious C‐isotope gradient of the Doushantuo cap carbonates precipitating in different sedimentary facies commonly occur in the surface‐ to deep‐water ocean in South China (Furuyama et al, 2017; Jiang et al, 2004, 2007, 2011; Lang et al, 2016; Li et al, 2017; Shen et al, 2005; Wang, Guan, et al, 2017; Wang, Wang, et al, 2017; Xiong, 2007) and in other regions of China (Calver & Walter, 2000; Volkov,…”

The Marinoan cap carbonate of Svalbard: Syngenetic marine dolomite with 17O‐anomalous carbonate‐associated sulphate

“…Hence the carbonate is diachronous and deposition accompanied sea-level rise (Hoffman et al, 2007(Hoffman et al, , 2017. Whilst some caps have similar lack of facies variation to D1-D2, most demonstrate greater variability in facies which Kuang et al (2022) attribute to a further down-ramp setting, although there are also likely to be basin-specific factors. Some caps contain columnar stromatolites and can be overlain by limestone, locally with sea-floor aragonite fans and barite precipitates; some are cherty.…”

Sedimentology of the Ediacaran barite‐bearing cap dolostone from Gaolan, northern Three Gorges, South China

“…However, Jiang et al (2003) and Kennedy et al (2001) are in favour of the mechanism of gas hydrate destabilization. Actually, the water-escape and liquification induced by the release of pore fluid pressure (Corkeron, 2007) or gas expansion (Kennedy et al, 2008) in the supratidal zone and upper intertidal zone led to the formation of the tepee structures and sheet cracks, as well as the siliceous cements (Kuang et al, 2022).…”