Serpukhovian

Last updated
Serpukhovian
330.9 ± 0.2 – 323.2 ± 0.4 Ma
Geology of Asia 325Ma.jpg
Paleogeography of the mid Serpukhovian, 325 Ma
Chronology
Etymology
Name formalityFormal
Usage information
Celestial body Earth
Regional usageGlobal (ICS)
Time scale(s) usedICS Time Scale
Definition
Chronological unit Age
Stratigraphic unit Stage
Time span formalityFormal
Lower boundary definitionNot formally defined
Lower boundary definition candidates FAD of the conodont Lochriea ziegleri
Lower boundary GSSP candidate section(s)
Upper boundary definitionFAD of the conodont Declinognathodus nodiliferus
Upper boundary GSSP Arrow Canyon, Nevada, USA
36°44′00″N114°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]

Contents

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

Related Research Articles

<span class="mw-page-title-main">Carboniferous</span> Fifth period of the Paleozoic Era, 359–299 million years ago

The Carboniferous is a geologic period and system of the Paleozoic that spans 60 million years from the end of the Devonian Period 358.9 Ma to the beginning of the Permian Period, 298.9 Ma. In North America, the Carboniferous is often treated as two separate geological periods, the earlier Mississippian and the later Pennsylvanian.

<span class="mw-page-title-main">Permian</span> Sixth and last period of the Paleozoic Era 299–252 million years ago

The Permian is a geologic period and stratigraphic system which spans 47 million years from the end of the Carboniferous Period 298.9 million years ago (Mya), to the beginning of the Triassic Period 251.902 Mya. It is the last period of the Paleozoic Era; the following Triassic Period belongs to the Mesozoic Era. The concept of the Permian was introduced in 1841 by geologist Sir Roderick Murchison, who named it after the region of Perm in Russia.

The PaleozoicEra is the first of three geological eras of the Phanerozoic Eon. Beginning 538.8 million years ago (Ma), it succeeds the Neoproterozoic and ends 251.9 Ma at the start of the Mesozoic Era. The Paleozoic is subdivided into six geologic periods :

In the geological timescale, the Tithonian is the latest age of the Late Jurassic Epoch and the uppermost stage of the Upper Jurassic Series. It spans the time between 149.2 ±0.7 Ma and 145.0 ± 4 Ma. It is preceded by the Kimmeridgian and followed by the Berriasian.

The Bashkirian is in the International Commission on Stratigraphy geologic timescale the lowest stage or oldest age of the Pennsylvanian. The Bashkirian age lasted from 323.2 to 315.2 Ma, is preceded by the Serpukhovian and is followed by the Moscovian.

In the geologic timescale, the Capitanian is an age or stage of the Permian. It is also the uppermost or latest of three subdivisions of the Guadalupian Epoch or Series. The Capitanian lasted between 264.28 and 259.51 million years ago. It was preceded by the Wordian and followed by the Wuchiapingian.

In the geologic timescale, the Kungurian is an age or stage of the Permian. It is the latest or upper of four subdivisions of the Cisuralian Epoch or Series. The Kungurian lasted between 283.5 and 273.01 million years ago (Ma). It was preceded by the Artinskian and followed by the Roadian.

In the geologic timescale, the Wordian is an age or stage of the Permian. It is the middle of three subdivisions of the Guadalupian Epoch or Series. The Wordian lasted between 266.9 and 264.28 million years ago (Ma). It was preceded by the Roadian and followed by the Capitanian.

<span class="mw-page-title-main">Changhsingian</span> Ninth and last stage of the Permain

In the geologic time scale, the Changhsingian or Changxingian is the latest age or uppermost stage of the Permian. It is also the upper or latest of two subdivisions of the Lopingian Epoch or Series. The Changhsingian lasted from 254.14 to 251.9 Ma ago. It is preceded by the Wuchiapingian age/stage and is followed by the Induan age/stage.

<span class="mw-page-title-main">Ladinian</span> Age in the Middle Triassic

The Ladinian is a stage and age in the Middle Triassic series or epoch. It spans the time between 242 Ma and ~237 Ma. The Ladinian was preceded by the Anisian and succeeded by the Carnian.

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<span class="mw-page-title-main">Tournaisian</span> First stage of the Carboniferous

The Tournaisian is in the ICS geologic timescale the lowest stage or oldest age of the Mississippian, the oldest subsystem of the Carboniferous. The Tournaisian age lasted from 358.9 Ma to 346.7 Ma. It is preceded by the Famennian and is followed by the Viséan. In global stratigraphy, the Tournaisian contains two substages: the Hastarian and Ivorian. These two substages were originally designated as European regional stages.

<span class="mw-page-title-main">Viséan</span> Second stage of the Carboniferous

The Visean, Viséan or Visian is an age in the ICS geologic timescale or a stage in the stratigraphic column. It is the second stage of the Mississippian, the lower subsystem of the Carboniferous. The Visean lasted from 346.7 to 330.9 Ma. It follows the Tournaisian age/stage and is followed by the Serpukhovian age/stage.

<span class="mw-page-title-main">Late Paleozoic icehouse</span> Ice age

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The Hangenberg event, also known as the Hangenberg crisis or end-Devonian extinction, is a mass extinction that occurred at the end of the Famennian stage, the last stage in the Devonian Period. It is usually considered the second-largest extinction in the Devonian Period, having occurred approximately 13 million years after the Late Devonian mass extinction at the Frasnian-Famennian boundary. The event is named after the Hangenberg Shale, which is part of a sequence that straddles the Devonian-Carboniferous boundary in the Rhenish Massif of Germany.

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The Namurian is a stage in the regional stratigraphy of northwest Europe, with an age between roughly 331 and 319 Ma. It is a subdivision of the Carboniferous system or period, as well as the regional Silesian series. The Namurian is named for the Belgian city and province of Namur where strata of this age occur. The Millstone Grit Group in the lithostratigraphy of northern England and parts of Wales is also of Namurian age.

The Westphalian is a regional stage or age in the regional stratigraphy of northwest Europe, with an age between roughly 315 and 307 Ma. It is a subdivision of the Carboniferous System or Period and the regional Silesian Series. The Westphalian is named for the region of Westphalia in western Germany where strata of this age occur. The Coal Measures of England and Wales are also largely of Westphalian age, though they also extend into the succeeding Stephanian.

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References

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Further reading