Source: Wikipedia, the free encyclopedia.
298.9 ± 0.15 – 251.902 ± 0.024 Ma
morphotype Streptognathodus wabaunsensis chronocline.
Lower boundary GSSPAidaralash, Ural Mountains, Kazakhstan
50°14′45″N 57°53′29″E / 50.2458°N 57.8914°E / 50.2458; 57.8914
Lower GSSP ratified1996[2]
Upper boundary definitionFAD of the Conodont Hindeodus parvus.
Upper boundary GSSPMeishan, Zhejiang, China
31°04′47″N 119°42′21″E / 31.0798°N 119.7058°E / 31.0798; 119.7058
Upper GSSP ratified2001[3]

The Permian (

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.[5][6][7][8][9]

The Permian witnessed the diversification of the two groups of

Euramerica and Gondwana during the Carboniferous. Pangaea was surrounded by the superocean Panthalassa. The Carboniferous rainforest collapse left behind vast regions of desert within the continental interior.[10]
Amniotes, which could better cope with these drier conditions, rose to dominance in place of their amphibian ancestors.

Various authors recognise at least three,

therapsids. The end of the Capitanian Stage of the Permian was marked by the major Capitanian mass extinction event,[13] associated with the eruption of the Emeishan Traps. The Permian (along with the Paleozoic) ended with the Permian–Triassic extinction event, the largest mass extinction in Earth's history (which is the last of the three or four crises that occurred in the Permian), in which nearly 81% of marine species and 70% of terrestrial species died out, associated with the eruption of the Siberian Traps. It took well into the Triassic for life to recover from this catastrophe;[14][15][16] on land, ecosystems took 30 million years to recover.[17]

Etymology and history

Prior to the introduction of the term "Permian", rocks of equivalent age in Germany had been named the Rotliegend and Zechstein, and in Great Britain as the New Red Sandstone.[18]

The term "Permian" was introduced into geology in 1841 by Sir Roderick Impey Murchison, president of the Geological Society of London, after extensive Russian explorations undertaken with Édouard de Verneuil in the vicinity of the Ural Mountains in the years 1840 and 1841. Murchison identified "vast series of beds of marl, schist, limestone, sandstone and conglomerate" that succeeded Carboniferous strata in the region.[19][20] Murchison, in collaboration with Russian geologists,[21] named the period after the surrounding Russian region of Perm, which takes its name from the medieval kingdom of Permia that occupied the same area hundreds of years prior, and which is now located in the Perm Krai administrative region.[22] Between 1853 and 1867, Jules Marcou recognised Permian strata in a large area of North America from the Mississippi River to the Colorado River and proposed the name "Dyassic", from "Dyas" and "Trias", though Murchison rejected this in 1871.[23] The Permian system was controversial for over a century after its original naming, with the United States Geological Survey until 1941 considering the Permian a subsystem of the Carboniferous equivalent to the Mississippian and Pennsylvanian.[18]


The Permian Period is divided into three

formation (a stratotype) identifying the lower boundary of the stage. The ages of the Permian, from youngest to oldest, are:[24]

Epoch Stage Lower boundary
Early Triassic Induan 251.902 ±0.024
Lopingian Changhsingian 254.14 ±0.07
Wuchiapingian 259.51 ±0.21
Guadalupian Capitanian 264.28 ±0.16
Wordian 266.9 ±0.4
Roadian 273.01 ±0.14
Cisuralian Kungurian 283.5 ±0.6
Artinskian 290.1 ±0.26
Sakmarian 293.52 ±0.17
Asselian 298.9 ±0.15

For most of the 20th century, the Permian was divided into the Early and Late Permian, with the Kungurian being the last stage of the Early Permian.[25] Glenister and colleagues in 1992 proposed a tripartite scheme, advocating that the Roadian-Capitanian was distinct from the rest of the Late Permian, and should be regarded as a separate epoch.[26] The tripartite split was adopted after a formal proposal by Glenister et al. (1999).[27]

Historically, most marine biostratigraphy of the Permian was based on ammonoids; however, ammonoid localities are rare in Permian stratigraphic sections, and species characterise relatively long periods of time. All GSSPs for the Permian are based around the first appearance datum of specific species of conodont, an enigmatic group of jawless chordates with hard tooth-like oral elements. Conodonts are used as index fossils for most of the Palaeozoic and the Triassic.[28]


The Cisuralian Series is named after the strata exposed on the western slopes of the Ural Mountains in Russia and Kazakhstan. The name was proposed by J. B. Waterhouse in 1982 to comprise the Asselian, Sakmarian, and Artinskian stages. The Kungurian was later added to conform to the Russian "Lower Permian".

Albert Auguste Cochon de Lapparent in 1900 had proposed the "Uralian Series", but the subsequent inconsistent usage of this term meant that it was later abandoned.[29]

The Asselian was named by the Russian stratigrapher V.E. Ruzhenchev in 1954, after the

Aqtöbe, Kazakhstan, which was ratified in 1996. The beginning of the stage is defined by the first appearance of Streptognathodus postfusus.[30]

The Sakmarian is named in reference to the

Sakmara River in the southern Urals, and was coined by Alexander Karpinsky in 1874. The GSSP for the base of the Sakmarian is located at the Usolka section in the southern Urals, which was ratified in 2018. The GSSP is defined by the first appearance of Sweetognathus binodosus.[31]

The Artinskian was named after the city of Arti in Sverdlovsk Oblast, Russia. It was named by Karpinsky in 1874. The Artinskian currently lacks a defined GSSP.[24] The proposed definition for the base of the Artinskian is the first appearance of Sweetognathus aff. S. whitei.[28]

The Kungurian takes its name after Kungur, a city in Perm Krai. The stage was introduced by Alexandr Antonovich Stukenberg in 1890. The Kungurian currently lacks a defined GSSP.[24] Recent proposals have suggested the appearance of Neostreptognathodus pnevi as the lower boundary.[28]


The Guadalupian Series is named after the Guadalupe Mountains in Texas and New Mexico, where extensive marine sequences of this age are exposed. It was named by George Herbert Girty in 1902.[32]

The Roadian was named in 1968 in reference to the Road Canyon Member of the Word Formation in Texas.[32] The GSSP for the base of the Roadian is located 42.7m above the base of the Cutoff Formation in Stratotype Canyon, Guadalupe Mountains, Texas, and was ratified in 2001. The beginning of the stage is defined by the first appearance of Jinogondolella nankingensis.[28]

The Wordian was named in reference to the Word Formation by Johan August Udden in 1916, Glenister and Furnish in 1961 was the first publication to use it as a chronostratigraphic term as a substage of the Guadalupian Stage.[32] The GSSP for the base of the Wordian is located in Guadalupe Pass, Texas, within the sediments of the Getaway Limestone Member of the Cherry Canyon Formation, which was ratified in 2001. The base of the Wordian is defined by the first appearance of the conodont Jinogondolella aserrata.[28]

The Capitanian is named after the Capitan Reef in the Guadalupe Mountains of Texas, named by George Burr Richardson in 1904, and first used in a chronostratigraphic sense by Glenister and Furnish in 1961 as a substage of the Guadalupian Stage.[32] The Capitanian was ratified as an international stage by the ICS in 2001. The GSSP for the base of the Capitanian is located at Nipple Hill in the southeast Guadalupe Mountains of Texas, and was ratified in 2001, the beginning of the stage is defined by the first appearance of Jinogondolella postserrata.[28]


The Lopingian was first introduced by Amadeus William Grabau in 1923 as the "Loping Series" after Leping, Jiangxi, China. Originally used as a lithostraphic unit, T.K. Huang in 1932 raised the Lopingian to a series, including all Permian deposits in South China that overlie the Maokou Limestone. In 1995, a vote by the Subcommission on Permian Stratigraphy of the ICS adopted the Lopingian as an international standard chronostratigraphic unit.[33]

The Wuchiapinginan and Changhsingian were first introduced in 1962, by J. Z. Sheng as the "Wuchiaping Formation" and "Changhsing Formation" within the Lopingian series. The GSSP for the base of the Wuchiapingian is located at Penglaitan, Guangxi, China and was ratified in 2004. The boundary is defined by the first appearance of Clarkina postbitteri postbitteri[33] The Changhsingian was originally derived from the Changxing Limestone, a geological unit first named by the Grabau in 1923, ultimately deriving from Changxing County, Zhejiang .The GSSP for the base of the Changhsingian is located 88 cm above the base of the Changxing Limestone in the Meishan D section, Zhejiang, China and was ratified in 2005, the boundary is defined by the first appearance of Clarkina wangi.[34]

The GSSP for the base of the Triassic is located at the base of Bed 27c at the Meishan D section, and was ratified in 2001. The GSSP is defined by the first appearance of the conodont Hindeodus parvus.[35]

Regional stages

The Russian Tatarian Stage includes the Lopingian, Capitanian and part of the Wordian, while the underlying Kazanian includes the rest of the Wordian as well as the Roadian.[25] In North America, the Permian is divided into the Wolfcampian (which includes the Nealian and the Lenoxian stages); the Leonardian (Hessian and Cathedralian stages); the Guadalupian; and the Ochoan, corresponding to the Lopingian.[36][37]


Geography of the Permian world

During the Permian, all the

epicontinental sea, existed in what is now northwestern Europe.[42]

Large continental landmass interiors experience climates with extreme variations of heat and cold ("

) appeared in the Permian.

Three general areas are especially noted for their extensive Permian deposits—the Ural Mountains (where Perm itself is located), China, and the southwest of North America, including the Texas red beds. The Permian Basin in the U.S. states of Texas and New Mexico is so named because it has one of the thickest deposits of Permian rocks in the world.[44]


Sea levels dropped slightly during the earliest Permian (Asselian). The sea level was stable at several tens of metres above present during the Early Permian, but there was a sharp drop beginning during the Roadian, culminating in the lowest sea level of the entire Palaeozoic at around present sea level during the Wuchiapingian, followed by a slight rise during the Changhsingian.[45]


Selwyn Rock, South Australia, an exhumed glacial pavement of Permian age

The Permian was cool in comparison to most other geologic time periods, with modest pole to Equator temperature gradients. At the start of the Permian, the Earth was still in the Late Paleozoic icehouse (LPIA), which began in the latest Devonian and spanned the entire Carboniferous period, with its most intense phase occurring during the latter part of the Pennsylvanian epoch.[46][47] A significant trend of increasing aridification can be observed over the course of the Cisuralian.[48] Early Permian aridification was most notable in Pangaean localities at near-equatorial latitudes.[49] Sea levels also rose notably in the Early Permian as the LPIA slowly waned.[50][51] At the Carboniferous-Permian boundary, a warming event occurred.[52] In addition to becoming warmer, the climate became notably more arid at the end of the Carboniferous and beginning of the Permian.[53][54] Nonetheless, temperatures continued to cool during most of the Asselian and Sakmarian, during which the LPIA peaked.[47][46] By 287 million years ago, temperatures warmed and the South Pole ice cap retreated in what was known as the Artinskian Warming Event (AWE),[55] though glaciers remained present in the uplands of eastern Australia,[46][56] and perhaps also the mountainous regions of far northern Siberia.[57] Southern Africa also retained glaciers during the late Cisuralian in upland environments.[58] The AWE also witnessed aridification of a particularly great magnitude.[55]

In the late Kungurian, cooling resumed,[59] resulting in a cool glacial interval that lasted into the early Capitanian,[60] though average temperatures were still much higher than during the beginning of the Cisuralian.[56] Another cool period began around the middle Capitanian.[60] This cool period, lasting for 3-4 Myr, was known as the Kamura Event.[61] It was interrupted by the Emeishan Thermal Excursion in the late part of the Capitanian, around 260 million years ago, corresponding to the eruption of the Emeishan Traps.[62] This interval of rapid climate change was responsible for the Capitanian mass extinction event.[13]

During the early Wuchiapingian, following the emplacement of the Emeishan Traps, global temperatures declined as carbon dioxide was weathered out of the atmosphere by the large igneous province's emplaced basalts.[63] The late Wuchiapingian saw the finale of the Late Palaeozoic Ice Age, when the last Australian glaciers melted.[46] The end of the Permian is marked by a temperature excursion, much larger than the Emeishan Thermal Excursion, at the Permian-Triassic boundary, corresponding to the eruption of the Siberian Traps, which released more than 5 teratonnes of CO2, more than doubling the atmospheric carbon dioxide concentration.[47] A -2% δ18O excursion signifies the extreme magnitude of this climatic shift.[64] This extremely rapid interval of greenhouse gas release caused the Permian-Triassic mass extinction,[65] as well as ushering in an extreme hothouse that persisted for several million years into the next geologic epoch, the Triassic.[66]

The Permian climate was also extremely seasonal and characterised by

megamonsoons,[67] which produced high aridity and extreme seasonality in Pangaea's interiors.[68] Precipitation along the western margins of the Palaeo-Tethys Ocean was very high.[69] Evidence for the megamonsoon includes the presence of megamonsoonal rainforests in the Qiangtang Basin of Tibet,[70] enormous seasonal variation in sedimentation, bioturbation, and ichnofossil deposition recorded in sedimentary facies in the Sydney Basin,[71] and palaeoclimatic models of the Earth's climate based on the behaviour of modern weather patterns showing that such a megamonsoon would occur given the continental arrangement of the Permian.[72] The aforementioned increasing equatorial aridity was likely driven by the development and intensification of this Pangaean megamonsoon.[73]


Hercosestria cribrosa, a reef-forming productid brachiopod (Middle Permian, Glass Mountains, Texas)

Marine biota

Permian marine deposits are rich in

Goniatitida were a major group during the Early-Mid Permian, but declined during the Late Permian. Members of the order Prolecanitida were less diverse. The Ceratitida originated from the family Daraelitidae within Prolecanitida during the mid-Permian, and extensively diversified during the Late Permian.[82] Only three families of trilobite are known from the Permian, Proetidae, Brachymetopidae and Phillipsiidae. Diversity, origination and extinction rates during the Early Permian were low. Trilobites underwent a diversification during the Kungurian-Wordian, the last in their evolutionary history, before declining during the Late Permian. By the Changhsingian, only a handful (4-6) genera remained.[83] Corals exhibited a decline in diversity over the course of the Middle and Late Permian.[84]

Terrestrial biota

Terrestrial life in the Permian included diverse plants, fungi, arthropods, and various types of tetrapods. The period saw a massive desert covering the interior of Pangaea. The warm zone spread in the northern hemisphere, where extensive dry desert appeared.[85] The rocks formed at that time were stained red by iron oxides, the result of intense heating by the sun of a surface devoid of vegetation cover. A number of older types of plants and animals died out or became marginal elements.

The Permian began with the Carboniferous flora still flourishing. About the middle of the Permian a major transition in vegetation began. The

South China.[86]

The Permian saw the radiation of many important conifer groups, including the ancestors of many present-day families. Rich forests were present in many areas, with a diverse mix of plant groups. The southern continent saw extensive seed fern forests of the Glossopteris flora. Oxygen levels were probably high there. The ginkgos and cycads also appeared during this period.


Fossil and life restoration of Permocupes sojanensis, a permocupedid beetle from the Middle Permian of Russia

Insects, which had first appeared and become abundant during the preceding Carboniferous, experienced a dramatic increase in diversification during the Early Permian. Towards the end of the Permian, there was a substantial drop in both origination and extinction rates.

xylophagous, feeding on decaying wood. Several lineages such as Schizophoridae expanded into aquatic habitats by the Late Permian.[89] Members of the modern orders Archostemata and Adephaga are known from the Late Permian.[90][91] Complex wood boring traces found in the Late Permian of China suggest that members of Polyphaga, the most diverse group of modern beetles, were also present in the Permian.[92] Based on molecular evidence, Phasmatodea likely originated sometime in the Permian, in conjunction with the spread of insectivory among tetrapods.[93]


from the Late Permian of Europe. Weigeltisaurids represent the oldest known gliding vertebrates.

The terrestrial fossil record of the Permian is patchy and temporally discontinuous. Early Permian records are dominated by equatorial Europe and North America, while those of the Middle and Late Permian are dominated by temperate

synapsids including the herbivorous edaphosaurids, and carnivorous sphenacodontids, diadectids and amphibians.[95][96] Early Permian reptiles, such as acleistorhinids, were mostly small insectivores.[97]


Cynodonts, the group of therapsids ancestral to modern mammals, first appeared and gained a worldwide distribution during the Late Permian.[106] Another group of therapsids, the therocephalians (such as Lycosuchus), arose in the Middle Permian.[107][108] There were no flying vertebrates, though the extinct lizard-like reptile family Weigeltisauridae from the Late Permian had extendable wings like modern gliding lizards, and are the oldest known gliding vertebrates.[109][110]


Permian stem-amniotes consisted of lepospondyli and batrachosaurs, according to some phylogenies;[111] according to others, stem-amniotes are represented only by diadectomorphs.[112]

Temnospondyls reached a peak of diversity in the Cisuralian, with a substantial decline during the Guadalupian-Lopingian following Olson's extinction, with the family diversity dropping below Carboniferous levels.[113]

Embolomeres, a group of aquatic crocodile-like limbed vertebrates that are reptilliomorphs under some phylogenies. They previously had their last records in the Cisuralian, are now known to have persisted into the Lopingian in China.[114]

Modern amphibians (lissamphibians) are suggested to have originated during Permian, descending from a lineage of dissorophoid temnospondyls[115] or lepospondyls.[112]


The diversity of fish during the Permian is relatively low compared to the following Triassic. The dominant group of

Xenacanthiformes, another extinct group of shark-like chondrichthyans, were common in freshwater habitats, and represented the apex predators of freshwater ecosystems.[123]


Map of the world at the Carboniferous-Permian boundary, showing the four floristic provinces


angiosperm trees.[126]

Life reconstruction of Permian wetland environment, showing an Eryops

The oldest likely record of

lycopsid tree Sigillaria, with a lower canopy consisting of Marattialean tree ferns, and Noeggerathiales.[124] Early conifers appeared in the Late Carboniferous, represented by primitive walchian conifers, but were replaced with more derived voltzialeans during the Permian. Permian conifers were very similar morphologically to their modern counterparts, and were adapted to stressed dry or seasonally dry climatic conditions.[126] The increasing aridity, especially at low latitudes, facilitated the spread of conifers and their increasing prevalence throughout terrestrial ecosystems.[131] Bennettitales, which would go on to become in widespread the Mesozoic, first appeared during the Cisuralian in China.[132] Lyginopterids, which had declined in the late Pennsylvanian and subsequently have a patchy fossil record, survived into the Late Permian in Cathaysia and equatorial east Gondwana.[133]

Permian–Triassic extinction event

The Permian–Triassic extinction event, labeled "End P" here, is the most significant extinction event in this plot for marine genera which produce large numbers of fossils

The Permian ended with the most extensive

, a subclass of cephalopods, surprisingly survived this occurrence.

There is evidence that magma, in the form of flood basalt, poured onto the Earth's surface in what is now called the Siberian Traps, for thousands of years, contributing to the environmental stress that led to mass extinction. The reduced coastal habitat and highly increased aridity probably also contributed. Based on the amount of lava estimated to have been produced during this period, the worst-case scenario is the release of enough carbon dioxide from the eruptions to raise world temperatures five degrees Celsius.[135]

Another hypothesis involves ocean venting of hydrogen sulfide gas. Portions of the deep ocean will periodically lose all of its dissolved oxygen allowing bacteria that live without oxygen to flourish and produce hydrogen sulfide gas. If enough hydrogen sulfide accumulates in an anoxic zone, the gas can rise into the atmosphere. Oxidizing gases in the atmosphere would destroy the toxic gas, but the hydrogen sulfide would soon consume all of the atmospheric gas available. Hydrogen sulfide levels might have increased dramatically over a few hundred years. Models of such an event indicate that the gas would destroy ozone in the upper atmosphere allowing ultraviolet radiation to kill off species that had survived the toxic gas.[136] There are species that can metabolize hydrogen sulfide.

Another hypothesis builds on the flood basalt eruption theory. An increase in temperature of five degrees Celsius would not be enough to explain the death of 95% of life. But such warming could slowly raise ocean temperatures until frozen methane reservoirs below the ocean floor near coastlines melted, expelling enough methane (among the most potent greenhouse gases) into the atmosphere to raise world temperatures an additional five degrees Celsius. The frozen methane hypothesis helps explain the increase in carbon-12 levels found midway in the Permian–Triassic boundary layer. It also helps explain why the first phase of the layer's extinctions was land-based, the second was marine-based (and starting right after the increase in C-12 levels), and the third land-based again.[137]

See also


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Further reading

External links