Variations in trace elements, isotopes, and organic geochemistry during the Hangenberg Crisis, Devonian–Carboniferous transition, northeastern Vietnam

Shizuya, Atena; Oba, Makoto; Ando, Takuto; Ogata, Yukari; Takashima, Reishi; Nishi, Hiroshi; Komatsu, Toshimitsu; Nguyen, Phong Duc

doi:10.1111/iar.12337

Cited by 8 publications

(5 citation statements)

References 79 publications

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“…Geochemical studies (trace element proxies, total organic carbon, framboidal pyrite distributions, etc.) and a significant mercury enrichment suggest dysoxic/ anoxic conditions from the latest Famennian through the early Tournaisian with severe anoxia (approaching euxinia) throughout the Hangenberg Event interval (Paschall et al 2019;Shizuya et al 2020). The authors interpret the mercury anomaly as the result of large-scale volcanic activity.…”

Section: Vietnammentioning

confidence: 93%

“…The Cat Co section, located in the Cat Ba Island (northwestern Vietnam) and exposing rocks of the Pho Han Formation, has been studied in detail in the recent period with multidisciplinary studies including conodont biostratigraphy, facies analysis, trace elements, isotopes and organic geochemistry (Komatsu et al 2012(Komatsu et al , 2014Paschall et al 2019;Shizuya et al 2020). The section (Fig.…”

Section: Vietnammentioning

confidence: 99%

“…5) is very condensed around the D/C boundary and consists of micritic light grey to grey limestones, marls and interbedded thin dark grey limestones and organic carbon-rich, black, friable limestones (Komatsu et al 2014). The Hangenberg Event is expressed by a c. 1 m (beds 116-118) of laminated black shales alternated with dark grey limestone (Komatsu et al 2014;Shizuya et al 2020).…”

Section: Vietnammentioning

confidence: 99%

“…HBS = Hangenberg Black Shale. (modified fromShizuya et al 2020) position of the DCB within the Yellow Drum Formation remains unknown.…”

mentioning

confidence: 99%

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The Devonian-Carboniferous Boundary around the globe: a complement

Aretz

Corradini

Denayer

2021

Palaeobio Palaeoenv

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This article compiles data on the Devonian-Carboniferous Boundary successions from countries and regions, which have not been dealt with separately in this special issue. Data derive from different palaeocontinents on a large palaeoclimatic gradient from the southern high latitudes of western Gondwana through the palaeotropics into the temperate/boreal northern latitudes of Siberia. The quality of the data is variable, but often surprisingly good, although major uncertainties can persist and traditional positions of the boundary do not withhold modern stratigraphic results and concepts. Not all these regions have been on the forefront of the DCB discussions in recent years, but they provide invaluable insights into the regional and global dimensions of uppermost Devonian and lowermost Carboniferous changes in the biosphere and geosphere. Almost globally documented are faunal turnovers and collapse of ecosystems in the Hangenberg extinctions. Those allow the placement of the DCB even if index fossils are absent or scarce. However, it also shows the regional differences, which advocate for a holistic approach to the boundary by ensuring global correlation without relying on the conceptual dominance a single taxon, which might be less powerful outside its usual facies.

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Section: Vietnammentioning

confidence: 93%

Section: Vietnammentioning

confidence: 99%

Section: Vietnammentioning

confidence: 99%

“…HBS = Hangenberg Black Shale. (modified fromShizuya et al 2020) position of the DCB within the Yellow Drum Formation remains unknown.…”

mentioning

confidence: 99%

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The Devonian-Carboniferous Boundary around the globe: a complement

Aretz

Corradini

Denayer

2021

Palaeobio Palaeoenv

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“…2). However, there is still debate about the cause/effect relationship between anoxia and extinction in the Devonian (Bratton et al 1999;Copper 2002;Joachimski and Buggisch 2002;George et al 2014;Shizuya et al 2019;Aretz 2021), as the epeiric seas and tectonic basins of eastern North America and Europe generally show a close association between the two (Bond and Wignall 2009 and references therein) but sites elsewhere (particularly in Australia) do not (Becker et al 1991;Bratton et al 1999;George et al 2014;. Others have suggested that climate cooling rather than anoxia was the cause of the mass extinction (Copper 1986;Joachimski and Buggisch 2002;Huang et al 2018).…”

Section: State Of the Artmentioning

confidence: 99%

Stratigraphy and facies of mid-Palaeozoic successions in southern Mongolia

Munkhjargal¹

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Mongolia covers a huge area in Asia and provides excellent Palaeozoic successions although large regions still lack detailed information on fauna and flora in Palaeozoic rocks. Of special interest is the Central Asian Orogenic Belt (CAOB), one of the largest collisional complexes on Earth. The CAOB is composed of a large number of terranes, continental margins, island arcs, backarc/forearc basins and accretionary wedges (Badarch et al. 2002; Safonova et al. 2017). Many terranes and regions underwent strong metamorphism, such as areas north of the Main Mongolian Lineament. To the south, Palaeozoic rocks exhibit low-grade metamorphism, thrusting and folding. Two promising long successions of Palaeozoic rocks were studied, namely the Hushoot Shiveetiin gol section and the Bayankhoshuu Ruins section. The intention of the PhD was to study marine facies settings in Palaeozoic rocks of southern and southwestern Mongolia, in an area little is known in terms of biostratigraphy and events. In order to get a better understanding on events and what might have been the driving forces I studied sections in Mongolia which have not been in the focus of research in the last decades. In order to complement studies on Late Devonian events elsewhere, I decided to study sections in open ocean environments (CAOB), far away from mainly studied epicontinental areas.As stated in many publications, events are the driving force for evolution. They exhibit dramatical changes in the palaeontological record of organisms and they are often associated with dramatic extinctions (Walliser 1996) and anoxic sediments (but not always). Mass extinctions are episodes in which a large number of plant and animal species became extinct within a few thousand to a hundred thousand years. Most events (first and second order events) are traceable worldwide. For instance, in the Late Devonian, mass extinction events recognized at the Frasnian–Famennian (F/F) stage boundary and at the Devonian–Carboniferous (D/C) boundary (McLaren and Goodfellow 1990; Sepkoski 1996; Walliser 1996). Overall, 19% of all families, 50% of all genera and at least 70% of all species became extinct (Raup and Sepkoski 1982; Sepkoski 1996; McGhee et al. 2013), but extinctions also concerned palaeoecosystems and due to Late Devonian events whole coral/stromatoporoid reef ecosystems became extinct. What might be the reason(s) for these dramatical changes? Why did the carbonate factory brake down? There are several reasons which have been discussed. For instance, extraterrestrial bolide impacts (McLaren 1970), anoxia within the water column due to climate changes (House 1985; Becker and House 1994; Caplan and Bustin 1999; Bond and Wignall 2005), transgressions and regressions (Newell 1967; Hallam and Wignall 1999; Purdy 2008; Ruban 2010, 2013; Smith and Benson 2013), eutrophication and increased sediment transport (Joachimski et al. 1993; Schobben et al. 2016), explosive volcanism (Paschall et al. 2019) and/ or large igneous provinces (LIP’s, Ernst et al. 2019; Racki et al. 2020, among others) and much more has been considered. The main problem is that previous studies preferably have been done along former epicontinental margins between Laurassia and Gondwana. Less information is available in deep open oceanic successions and shallow-water areas around island arcs. Generally, events are characterized by bituminous rocks, such as black limestones and shales within marine realms, but they do not necessarily occur everywhere (see Carmichael et al. 2016). So, the question was: “Can we recognize Palaeozoic event layers or equivalents in the CAOB?” If so, is this comparable to already published data? What might be the main trigger, as there are many reasons still in discussion? And finally, what has happened in the aftermath of those events as it seems that the CAOB may have acted as a refugium for at least some groups, such as for crinoids (Waters and Webster 2009; Tolokonnikova and Ernst 2010). In this thesis, I will provide data from isolated ecosystems from a rather unstudied region, which will complement studies from other parts of the World.

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Organic carbon isotope stratigraphy of Devonian-Carboniferous boundary sections in the Rhenish Mountains

Korn,

Schmid,

Struck

2023

Palaeobio Palaeoenv

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The boundary between the Devonian and the Carboniferous has been drawn using ammonoids, conodonts and miospores, while geochemical data have only rarely been used. The sampling of eight sections (Aprath, Apricke, Effenberg, Wocklum, Stockum, Drewer WJ, Drewer WA, Marsberg) at the northern margin of the Rhenish Mountains demonstrates the potential of the isotope ratio of organic carbon to regionally correlate sections in different facies areas. With the help of the carbon isotopes, a distinct stratigraphic succession is documented, which is characterised by several positive and negative excursions; this succession was recorded in all examined sections. The carbon isotopes can therefore make a significant contribution to the stratigraphic subdivision of sections and complement the biostratigraphic methods.

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Variations in trace elements, isotopes, and organic geochemistry during the Hangenberg Crisis, Devonian–Carboniferous transition, northeastern Vietnam

Cited by 8 publications

References 79 publications

The Devonian-Carboniferous Boundary around the globe: a complement

The Devonian-Carboniferous Boundary around the globe: a complement

Stratigraphy and facies of mid-Palaeozoic successions in southern Mongolia

Organic carbon isotope stratigraphy of Devonian-Carboniferous boundary sections in the Rhenish Mountains

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