Serpukhovian
330.9 ± 0.2 – 323.2 ± 0.4 Ma
Paleogeography of the mid Serpukhovian, 325 Ma
Chronology
Etymology
Name formalityFormal
Usage information
Celestial bodyEarth
Regional usageGlobal (ICS)
Time scale(s) usedICS Time Scale
Definition
Chronological unitAge
Stratigraphic unitStage
Time span formalityFormal
Lower boundary definitionNot formally defined
Lower boundary definition candidatesFAD of the conodont Lochriea ziegleri
Lower boundary GSSP candidate section(s)
Upper boundary definitionFAD of the conodont Declinognathodus nodiliferus
Upper boundary GSSPArrow Canyon, Nevada, USA
36°44′00″N 114°46′40″W / 36.7333°N 114.7778°W / 36.7333; -114.7778
Upper GSSP ratified1996[2]

The Serpukhovian is in the ICS geologic timescale the uppermost stage or youngest age of the Mississippian, the lower subsystem of the Carboniferous. The Serpukhovian age lasted from 330.9 Ma to 323.2 Ma.[3] It is preceded by the Visean and is followed by the Bashkirian. The Serpukhovian correlates with the lower part of the Namurian Stage of European stratigraphy and the middle and upper parts of the Chesterian Stage of North American stratigraphy.[4]

Name and definition

The Serpukhovian Stage was proposed in 1890 by Russian stratigrapher Sergei Nikitin and was introduced in the official stratigraphy of European Russia in 1974.[5] It was named after the city of Serpukhov, near Moscow. The ICS later used the upper Russian subdivisions of the Carboniferous in its international geologic time scale.

The base of the Serpukhovian is informally defined by the first appearance of the conodont Lochriea ziegleri, though the utility and systematic stability of this species is not yet certain. No lower GSSP has been assigned to the Serpukhovian Stage yet. Two candidate GSSPs have been proposed: the Verkhnyaya Kardailovka section in the South Urals of Russia, and the Naqing (Nashui) section in Guizhou, China.[4]

The top of the stage (the base of the Pennsylvanian subsystem and Bashkirian stage) is at the first appearance of the conodont Declinognathodus nodiliferus in the lower Bird Spring Formation, which overlies the Battleship Formation in Nevada.[6] It is also slightly above the first appearance of the foram Globivalvulina bulloides, genozone of the ammonoid genus Homoceras and the ammonoid biozone of Isohomoceras subglobosum.[7]

Subdivision

Biostratigraphy

In Europe, the Serpukhovian Stage includes three conodont biozones: the Gnathodus postbilineatus Zone (youngest), Gnathodus bollandensis Zone, and Lochriea ziegleri Zone (in part, oldest). There are three foraminifera biozones: the Monotaxinoides transitorius Zone (youngest), Eostaffellina protvae Zone, and Neoarchaediscus postrugosus Zone (oldest).

In North America, the stage encompassed four conodont biozones: the Rhachistognathus muricatus Zone (youngest), Adetognathus unicornis Zone, Cavusgnathus naviculus Zone, and Gnathodus bilineatus Zone (in part, oldest).

Regional subdivisions

In the regional stratigraphy of Russia (and Eastern Europe as a whole), the Serpukhovian is subdivided into four substages, from oldest to youngest: the Tarusian, Steshevian, Protvian, and Zapaltyubian. The former three are found in the Moscow Basin and are named after places near Serpukhov (Tarusa and Protva). Strata belonging to the Zapaltyubian are not exposed in the Moscow Basin, though they are found in the Donets Basin and the Urals.[4]

In the regional stratigraphy of the United Kingdom (and Western Europe as a whole), the Serpukhovian corresponds to the lower half of the Namurian regional stage. This portion of the Namurian includes three substages, from oldest to youngest: the Pendleian, Arnsbergian and Chokierian. Only the lowermost Chokierian falls in the Serpukhovian, the upper part of the substage corresponds to the earliest Bashkirian.[8][4]

In North America, the Serpukhovian corresponds to the upper part of the Chesterian regional stage, while in China the Serpukhovian is roughly equivalent to the Dewuan regional stage.[4]

Serpukhovian extinction

The largest extinction event of the Carboniferous Period occurred in the early Serpukhovian. This extinction came in the form of ecological turnovers, with the demise of diverse Mississippian assemblages of crinoids and rugose corals. After the extinction, they were replaced by species-poor cosmopolitan ecosystems. The extinction selectively targeted species with a narrow range of temperature preferences, as cooling seawater led to habitat loss for tropical specialists.[9] Ammonoids appear to have not been impacted by this event, as they reached a zenith in diversity at this time.[10] The long-term ecological impact of the Serpukhovian extinction may have exceeded that of the Ordovician-Silurian extinction, where taxonomic diversity was abruptly devastated but quickly recovered to pre-extinction levels.[11][12][13]

Sepkoski (1996) plotted an extinction rate of around 23-24% for the Serpukhovian as a whole, based on marine genera which persist through multiple stages.[14] Bambach (2006) found an early Serpukhovian extinction rate of 31% among all marine genera.[15] Using an extinction probability procedure generated from the Paleobiology Database, McGhee et al. (2013) estimated an extinction rate as high as 39% for marine genera.[12] On the other hand, Stanley (2016) estimated that the extinction was much smaller, at a loss of only 13-14 % of marine genera.[16]

Relative to other biological crises, the Serpukhovian extinction was much more selective in its effects on different evolutionary faunas. Stanley (2007) estimated that the early Serpukhovian saw the loss of 37.5% of marine genera in the Paleozoic evolutionary fauna. Only 15.4% of marine genera in the modern evolutionary fauna would have been lost along the same time interval.[17] This disconnect, and the severity of the extinction as a whole, is reminiscent of the Late Devonian extinction events. Another similarity is how the Serpukhovian extinction was seemingly driven by low rates of speciation, rather than particularly high rates of extinction.[18][11]

It is disputed whether the aftermath of the extinction saw a relative stagnation of biodiversity or a major increase. Some studies have found that in the following Late Paleozoic Ice Age (LPIA) of the Late Carboniferous and Early Permian, both speciation and extinction rates were low,[18][19] with this stagnation in biological diversity driven by a reduction of carbonate platforms, which otherwise would have helped to maintain high biodiversity.[20] More recent studies have instead shown that biodiversity surged during the LPIA in what is known as the Carboniferous-Earliest Permian Biodiversification Event (CPBE).[21][22] Foraminifera especially saw extremely rapid diversification.[23] The CPBE's cause may have been the dramatically increased marine provincialism caused by sea level fall during the LPIA combined with the assembly of Pangaea, which limited the spread of taxa from one region of the world ocean to another.[21]

See also

References

  1. ^ "Chart/Time Scale". www.stratigraphy.org. International Commission on Stratigraphy.
  2. ^ Lane, H.; Brenckle, Paul; Baesemann, J.; Richards, Barry (December 1999). "The IUGS boundary in the middle of the Carboniferous: Arrow Canyon, Nevada, USA". Episodes. 22 (4): 272–283. doi:10.18814/epiiugs/1999/v22i4/003.
  3. ^ Gradstein, F.M.; Ogg, J.G. & Smith, A.G.; 2004: A Geologic Time Scale 2004, Cambridge University Press.
  4. ^ a b c d e Aretz, M.; Herbig, H. G.; Wang, X. D.; Gradstein, F. M.; Agterberg, F. P.; Ogg, J. G. (2020-01-01), Gradstein, Felix M.; Ogg, James G.; Schmitz, Mark D.; Ogg, Gabi M. (eds.), "Chapter 23 - The Carboniferous Period", Geologic Time Scale 2020, Elsevier, pp. 811–874, ISBN 978-0-12-824360-2, retrieved 2021-11-03
  5. ^ Fedorowsky, J.; 2009: Early Bashkirian Rugosa (Anthozoa) from the Donets Basin, Ukraine. Part 1. Introductory considerations and the genus Rotiphyllum Hudson, 1942, Acta Geologica Polonica 59 (1), pp. 1–37.
  6. ^ Lane, H.R.; Brenckle, P.L.; Baesemann, J.F. & Richards, B.; 1999: The IUGS boundary in the middle of the Carboniferous: Arrow Canyon, Nevada, USA, Episodes 22 (4), pp 272–283
  7. ^ Menning, M.; Alekseev, A.S.; Chuvashov, B.I.; Davydov, V.I.; Devuyst, F.-X.; Forke, H.C.; Grunt, T.A.; Hance, L.; Heckel, P.H.; Izokh, N.G.; Jin, Y.-G.; Jones, P.J.; Kotlyar, G.V.; Kozur, H.W.; Nemyrovska, T.I.; Schneider, J.W.; Wang, X.-D.; Weddige, K.; Weyer, D. & Work, D.M.; 2006: Global time scale and regional stratigraphic reference scales of Central and West Europe, East Europe, Tethys, South China, and North America as used in the Devonian–Carboniferous–Permian Correlation Chart 2003 (DCP 2003), Palaeogeography, Palaeoclimatology, Palaeoecology 240 (1-2): pp 318–372
  8. ^ Heckel, P.H. & Clayton, G.; 2006: The Carboniferous system, use of the new official names for the subsystems, series and stages, Geologica Acta 4 (3), pp 403–407
  9. ^ Powell, Matthew G. (2008-08-01). "Timing and selectivity of the Late Mississippian mass extinction of brachiopod genera from the Central Appalachian Basin". PALAIOS. 23 (8): 525–534. Bibcode:2008Palai..23..525P. doi:10.2110/palo.2007.p07-038r. ISSN 0883-1351. S2CID 129588228.
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  11. ^ a b McGhee, George R. Jr; Sheehan, Peter M.; Bottjer, David J.; Droser, Mary L. (2012-02-01). [[[Geology (journal)|Geology]] "Ecological ranking of Phanerozoic biodiversity crises: The Serpukhovian (early Carboniferous) crisis had a greater ecological impact than the end-Ordovician"]. Geology. 40 (2): 147–150. Bibcode:2012Geo....40..147M. doi:10.1130/G32679.1. ISSN 0091-7613. ((cite journal)): Check |url= value (help)
  12. ^ a b McGhee, George R.; Clapham, Matthew E.; Sheehan, Peter M.; Bottjer, David J.; Droser, Mary L. (2013-01-15). "A new ecological-severity ranking of major Phanerozoic biodiversity crises" (PDF). Palaeogeography, Palaeoclimatology, Palaeoecology. 370: 260–270. Bibcode:2013PPP...370..260M. doi:10.1016/j.palaeo.2012.12.019. ISSN 0031-0182.
  13. ^ Cózar, Pedro; Vachard, Daniel; Somerville, Ian D.; Medina-Varea, Paula; Rodríguez, Sergio; Said, Ismail (2014-01-15). "The Tindouf Basin, a marine refuge during the Serpukhovian (Carboniferous) mass extinction in the northwestern Gondwana platform". Palaeogeography, Palaeoclimatology, Palaeoecology. 394: 12–28. Bibcode:2014PPP...394...12C. doi:10.1016/j.palaeo.2013.11.023. ISSN 0031-0182.
  14. ^ Sepkoski, J. John (1996), Walliser, Otto H. (ed.), "Patterns of Phanerozoic Extinction: a Perspective from Global Data Bases", Global Events and Event Stratigraphy in the Phanerozoic: Results of the International Interdisciplinary Cooperation in the IGCP-Project 216 "Global Biological Events in Earth History", Berlin, Heidelberg: Springer, pp. 35–51, doi:10.1007/978-3-642-79634-0_4, ISBN 978-3-642-79634-0
  15. ^ Bambach, Richard K. (2006). "Phanerozoic Biodiversity Mass Extinctions" (PDF). Annual Review of Earth and Planetary Sciences. 34 (1): 127–155. Bibcode:2006AREPS..34..127B. doi:10.1146/annurev.earth.33.092203.122654. ISSN 0084-6597.
  16. ^ Stanley, Steven M. (2016-10-18). "Estimates of the magnitudes of major marine mass extinctions in earth history". Proceedings of the National Academy of Sciences of the United States of America. 113 (42): E6325–E6334. Bibcode:2016PNAS..113E6325S. doi:10.1073/pnas.1613094113. ISSN 0027-8424. PMC 5081622. PMID 27698119.
  17. ^ Stanley, Steven M. (2007). "Memoir 4: An Analysis of the History of Marine Animal Diversity". Paleobiology. 33 (S4): 1–55. Bibcode:2007Pbio...33Q...1S. doi:10.1017/S0094837300019217. ISSN 0094-8373. S2CID 90130435.
  18. ^ a b Stanley, Steven M.; Powell, Matthew G. (2003-10-01). "Depressed rates of origination and extinction during the late Paleozoic ice age: A new state for the global marine ecosystem". Geology. 31 (10): 877–880. Bibcode:2003Geo....31..877S. doi:10.1130/G19654R.1. ISSN 0091-7613.
  19. ^ Powell, Matthew G. (2005-05-01). "Climatic basis for sluggish macroevolution during the late Paleozoic ice age". Geology. 33 (5): 381–384. Bibcode:2005Geo....33..381P. doi:10.1130/G21155.1. ISSN 0091-7613.
  20. ^ Balseiro, Diego; Powell, Matthew G. (2019-11-22). "Carbonate collapse and the late Paleozoic ice age marine biodiversity crisis". Geology. 48 (2): 118–122. doi:10.1130/G46858.1. hdl:11336/145657. ISSN 0091-7613. S2CID 213580499.
  21. ^ a b Shi, Yukun; Wang, Xiangdong; Fan, Junxuan; Huang, Hao; Xu, Huiqing; Zhao, Yingying; Shen, Shuzhong (September 2021). "Carboniferous-earliest Permian marine biodiversification event (CPBE) during the Late Paleozoic Ice Age". Earth-Science Reviews. 220: 103699. Bibcode:2021ESRv..22003699S. doi:10.1016/j.earscirev.2021.103699. Retrieved 4 September 2022.
  22. ^ Fan, Jun-Xuan; Shen, Shu-Zhong; Erwin, Douglas H.; Sadler, Peter M.; MacLeod, Norman; Cheng, Qiu-Ming; Hou, Xu-Dong; Yang, Jiao; Wang, Xiang-Dong; Wang, Yue; Zhang, Hua; Chen, Xu; Li, Guo-Xiang; Zhang, Yi-Chun; Shi, Yu-Kun; Yuan, Dong-Xun; Chen, Qing; Zhang, Lin-Na; Li, Chao; Zhao, Ying-Ying (17 January 2020). "A high-resolution summary of Cambrian to Early Triassic marine invertebrate biodiversity". Science. 367 (6475): 272–277. Bibcode:2020Sci...367..272F. doi:10.1126/science.aax4953. PMID 31949075. S2CID 210698603. Retrieved 23 April 2023.
  23. ^ Groves, John R.; Yue, Wang (1 September 2009). "Foraminiferal diversification during the late Paleozoic ice age". Paleobiology. 35 (3): 367–392. Bibcode:2009Pbio...35..367G. doi:10.1666/0094-8373-35.3.367. S2CID 130097035. Retrieved 4 September 2022.

Further reading

External links

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