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Triassic - Wikipedia

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The Triassic ( try-ASS-ik)[8] is a geologic period and system which spans 50.6 million years from the end of the Permian Period 251.902 million years ago (Mya), to the beginning of the Jurassic Period 201.36 Mya.[9] The Triassic is the first and shortest period of the Mesozoic Era. Both the start and end of the period are marked by major extinction events.[10] The Triassic period is subdivided into three epochs: Early Triassic, Middle Triassic and Late Triassic.

The Triassic began in the wake of the Permian-Triassic extinction event, which left the Earth's biosphere impoverished; it was well into the middle of the Triassic before life recovered its former diversity. Therapsids and archosaurs were the chief terrestrial vertebrates during this time. A specialized subgroup of archosaurs, called dinosaurs, first appeared in the Late Triassic but did not become dominant until the succeeding Jurassic Period.[11]

The first true mammals, themselves a specialized subgroup of therapsids, also evolved during this period, as well as the first flying vertebrates, the pterosaurs, who, like the dinosaurs, were a specialized subgroup of archosaurs. The vast supercontinent of Pangaea existed until the mid-Triassic, after which it began to gradually rift into two separate landmasses, Laurasia to the north and Gondwana to the south.

The global climate during the Triassic was mostly hot and dry,[12] with deserts spanning much of Pangaea's interior. However, the climate shifted and became more humid as Pangaea began to drift apart. The end of the period was marked by yet another major mass extinction, the Triassic-Jurassic extinction event, that wiped out many groups and allowed dinosaurs to assume dominance in the Jurassic.

Etymology[edit]

The Triassic was named in 1834 by Friedrich von Alberti, after the three distinct rock layers (Greek triás meaning 'triad') that were widespread in southern Germany: the lower Buntsandstein, the middle Muschelkalk and the upper Keuper.[13]

Dating and subdivisions[edit]

On the geologic time scale, the Triassic is usually divided into Early, Middle, and Late Triassic Epochs, and the corresponding rocks are referred to as Lower, Middle, or Upper Triassic. The faunal stages from the youngest to oldest are:

Paleogeography[edit]

230 Ma plate tectonic reconstruction

During the Triassic, almost all the Earth's land mass was concentrated into a single supercontinent centered more or less on the equator and spanning from pole to pole, called Pangaea (lit. 'entire land'). From the east, along the equator, the Tethys sea penetrated Pangaea, causing the Paleo-Tethys Ocean to be closed.

Later in the mid-Triassic a similar sea penetrated along the equator from the west. The remaining shores were surrounded by the world-ocean known as Panthalassa (lit. 'entire sea'). All the deep-ocean sediments laid down during the Triassic have disappeared through subduction of oceanic plates; thus, very little is known of the Triassic open ocean.

The supercontinent Pangaea was rifting during the Triassic—especially late in that period—but had not yet separated. The first nonmarine sediments in the rift that marks the initial break-up of Pangaea, which separated New Jersey from Morocco, are of Late Triassic age; in the U.S., these thick sediments comprise the Newark Group.[15]

Because a super-continental mass has less shoreline compared to one broken up, Triassic marine deposits are globally relatively rare, despite their prominence in Western Europe, where the Triassic was first studied. In North America, for example, marine deposits are limited to a few exposures in the west. Thus Triassic stratigraphy is mostly based on organisms that lived in lagoons and hypersaline environments, such as Estheria crustaceans.

Africa[edit]

At the beginning of the Mesozoic Era, Africa was joined with Earth's other continents in Pangaea.[16] Africa shared the supercontinent's relatively uniform fauna which was dominated by theropods, prosauropods and primitive ornithischians by the close of the Triassic period.[16] Late Triassic fossils are found throughout Africa, but are more common in the south than north.[16] The time boundary separating the Permian and Triassic marks the advent of an extinction event with global impact, although African strata from this time period have not been thoroughly studied.[16]

Scandinavia[edit]

During the Triassic peneplains are thought to have formed in what is now Norway and southern Sweden.[17][18][19] Remnants of this peneplain can be traced as a tilted summit accordance in the Swedish West Coast.[17] In northern Norway Triassic peneplains may have been buried in sediments to be then re-exposed as coastal plains called strandflats.[18] Dating of illite clay from a strandflat of Bømlo, southern Norway, have shown that landscape there became weathered in Late Triassic times (c. 210 million years ago) with the landscape likely also being shaped during that time.[20]

Paleooceanography[edit]

Eustatic sea level was consistently low compared to the other geological periods for the entire Triassic. The beginning of the Triassic was around present sea level, rising to about 10-20 m above sea level during the Early and Middle Triassic. Beginning in the Ladinan, the sea level began to rise, culminating with the sea level being up to 50 metres above present during the Carnian. The sea level declined beginning in the Norian, reaching a low of 50 metres below present sea level during the mid-Rhaetian, which continued into the earliest Jurassic. The long term sea level trend is superimposed with 22 sea level drop events widespread in the geologic record, mostly of minor (<25 metres) and medium (25-75 metres) magnitudes. Lack of evidence for Triassic continental ice sheets suggest that glacial eustasy is unlikely to be the cause of these changes.[21]

Climate[edit]

The Triassic continental interior climate was generally hot and dry, so that typical deposits are red bed sandstones and evaporites. There is no evidence of glaciation at or near either pole; in fact, the polar regions were apparently moist and temperate, providing a climate suitable for forests and vertebrates, including reptiles. Pangaea's large size limited the moderating effect of the global ocean; its continental climate was highly seasonal, with very hot summers and cold winters.[22] The strong contrast between the Pangea supercontinent and the global ocean triggered intense cross-equatorial monsoons.[22]

The Triassic may have mostly been a dry period, but evidence exists that it was punctuated by several episodes of increased rainfall in tropical and subtropical latitudes of the Tethys Sea and its surrounding land.[23] Sediments and fossils suggestive of a more humid climate are known from the Anisian to Ladinian of the Tethysian domain, and from the Carnian and Rhaetian of a larger area that includes also the Boreal domain (e.g., Svalbard Islands), the North American continent, the South China block and Argentina.

The best studied of such episodes of humid climate, and probably the most intense and widespread, was the Carnian Pluvial Event. A 2020 study found bubbles of carbon dioxide in basaltic rocks dating back to the end of the Triassic, and concluded that volcanic activity helped trigger climate change in that period.[24]

Life[edit]

Three categories of organisms can be distinguished in the Triassic record: survivors from the Permian-Triassic extinction event, new groups which flourished briefly, and other new groups which went on to dominate the Mesozoic Era.

Flora[edit]

On land, the surviving vascular plants included the lycophytes, the dominant cycadophytes, ginkgophyta (represented in modern times by Ginkgo biloba), ferns, horsetails and glossopterids. The spermatophytes, or seed plants, came to dominate the terrestrial flora: in the northern hemisphere, conifers, ferns and bennettitales flourished. The seed fern genus Dicroidium would dominate Gondwana throughout the period.

Plankton[edit]

Before the Permian extinction, Archaeplastida (red and green algae) had been the major marine phytoplanktons since about 659-645 million years ago,[25] when they replaced marine planktonic cyanobacteria, which first appeared about 800 million years ago, as the dominant phytoplankton in the oceans.[26] In the Triassic, secondary endosymbiotic algae became the most important plankton.[27]

Marine fauna[edit]

Middle Triassic marginal marine sequence, southwestern Utah

In marine environments, new modern types of corals appeared in the Early Triassic, forming small patches of reefs of modest extent compared to the great reef systems of Devonian or modern times. Serpulids appeared in the Middle Triassic.[29] Microconchids were abundant. The shelled cephalopods called ammonites recovered, diversifying from a single line that survived the Permian extinction.

The fish fauna was remarkably uniform, with many families and genera exhibiting a global distribution in the wake of the mass extinction event.[30] Ray-finned fishes went through a remarkable diversification during the Triassic, leading to peak diversity during the Middle Triassic; however, the pattern of this diversification is still not well understood due to a taphonomic megabias.[31] There were also many types of marine reptiles. These included the Sauropterygia, which featured pachypleurosaurus and nothosaurs (both common during the Middle Triassic, especially in the Tethys region), placodonts, and the first plesiosaurs. The first of the lizardlike Thalattosauria (askeptosaurs) and the highly successful ichthyosaurs, which appeared in Early Triassic seas soon diversified, and some eventually developed to huge size during the Late Triassic. Subequatorial saurichthyids and birgeriids have also been described in Early Triassic strata.[32]

Terrestrial and freshwater fauna[edit]

Groups of terrestrial fauna, which appeared in the Triassic period or achieved a new level of evolutionary success during it include:[33][34]

The Permian-Triassic extinction devastated terrestrial life. Biodiversity rebounded as the surviving species repopulated empty terrain, but these were short-lived. Diverse communities with complex food-web structures took 30 million years to reestablish.[10]

Temnospondyl amphibians were among those groups that survived the Permian-Triassic extinction; some lineages (e.g. trematosaurs) flourished briefly in the Early Triassic, while others (e.g. capitosaurs) remained successful throughout the whole period, or only came to prominence in the Late Triassic (e.g. Plagiosaurus, metoposaurs). As for other amphibians, the first Lissamphibia, progenitors of first frogs, are known from the Early Triassic, but the group as a whole did not become common until the Jurassic, when the temnospondyls had become very rare.

Most of the Reptiliomorpha, stem-amniotes that gave rise to the amniotes, disappeared in the Triassic, but two water-dwelling groups survived: Embolomeri that only survived into the early part of the period, and the Chroniosuchia, which survived until the end of the Triassic.

Archosauromorph reptiles, especially archosaurs, progressively replaced the synapsids that had dominated the previous Permian period. The Cynognathus was the characteristic top predator in earlier Triassic (Olenekian and Anisian) on Gondwana. Both kannemeyeriid dicynodonts and gomphodont cynodonts remained important herbivores during much of the period, and ecteniniids played a role as large-sized, cursorial predators in the Late Triassic. During the Carnian (early part of the Late Triassic), some advanced cynodonts gave rise to the first mammals. At the same time the Ornithodira, which until then had been small and insignificant, evolved into pterosaurs and a variety of dinosaurs. The Crurotarsi were the other important archosaur clade, and during the Late Triassic these also reached the height of their diversity, with various groups including the phytosaurs, aetosaurs, several distinct lineages of Rauisuchia, and the first crocodylians (the Sphenosuchia). Meanwhile, the stocky herbivorous rhynchosaurs and the small to medium-sized insectivorous or piscivorous Prolacertiformes were important basal archosauromorph groups throughout most of the Triassic.

Among other reptiles, the earliest turtles, like Proganochelys and Proterochersis, appeared during the Norian Age (Stage) of the Late Triassic Period. The Lepidosauromorpha, specifically the Sphenodontia, are first found in the fossil record of the earlier Carnian Age. The Procolophonidae were an important group of small lizard-like herbivores.

During the Triassic, archosaurs displaced therapsids as the dominant amniotes. This "Triassic Takeover" may have contributed to the evolution of mammals by forcing the surviving therapsids and their mammaliaform successors to live as small, mainly nocturnal insectivores. Nocturnal life may have forced the mammaliaforms to develop fur and a higher metabolic rate.[38]

Coal[edit]

Immediately above the Permian-Triassic boundary the glossopteris flora was suddenly[39] largely displaced by an Australia-wide coniferous flora.

No known coal deposits date from the start of the Triassic period. This is known as the "coal gap" and can be seen as part of the Permian-Triassic extinction event.[40] Possible explanations for the coal gap include sharp drops in sea level at the time of the Permo-Triassic boundary;[41] acid rain from the Siberian Traps eruptions or from an impact event that overwhelmed acidic swamps; climate shift to a greenhouse climate that was too hot and dry for peat accumulation; evolution of fungi or herbivores that were more destructive of wetlands; the extinction of all plants adapted to peat swamps, with a hiatus of several million years before new plant species evolved that were adapted to peat swamps;[40] or soil anoxia as oxygen levels plummeted.[42]

Lagerstätten[edit]

The Monte San Giorgio lagerstätte, now in the Lake Lugano region of northern Italy and Switzerland, was in Triassic times a lagoon behind reefs with an anoxic bottom layer, so there were no scavengers and little turbulence to disturb fossilization, a situation that can be compared to the better-known Jurassic Solnhofen Limestone lagerstätte.

The remains of fish and various marine reptiles (including the common pachypleurosaur Neusticosaurus, and the bizarre long-necked archosauromorph Tanystropheus), along with some terrestrial forms like Ticinosuchus and Macrocnemus, have been recovered from this locality. All these fossils date from the Anisian/Ladinian transition (about 237 million years ago).

Triassic-Jurassic extinction event[edit]

The mass extinction event is marked by 'End Tr'

The Triassic period ended with a mass extinction, which was particularly severe in the oceans; the conodonts disappeared, as did all the marine reptiles except ichthyosaurs and plesiosaurs. Invertebrates like brachiopods, gastropods, and molluscs were severely affected. In the oceans, 22% of marine families and possibly about half of marine genera went missing.

Though the end-Triassic extinction event was not equally devastating in all terrestrial ecosystems, several important clades of crurotarsans (large archosaurian reptiles previously grouped together as the thecodonts) disappeared, as did most of the large labyrinthodont amphibians, groups of small reptiles, and some synapsids (except for the proto-mammals). Some of the early, primitive dinosaurs also became extinct, but more adaptive ones survived to evolve into the Jurassic. Surviving plants that went on to dominate the Mesozoic world included modern conifers and cycadeoids.

The cause of the Late Triassic extinction is uncertain. It was accompanied by huge volcanic eruptions that occurred as the supercontinent Pangaea began to break apart about 202 to 191 million years ago (40Ar/39Ar dates),[43] forming the Central Atlantic Magmatic Province (CAMP),[44] one of the largest known inland volcanic events since the planet had first cooled and stabilized. Other possible but less likely causes for the extinction events include global cooling or even a bolide impact, for which an impact crater containing Manicouagan Reservoir in Quebec, Canada, has been singled out. However, the Manicouagan impact melt has been dated to 214±1 Mya. The date of the Triassic-Jurassic boundary has also been more accurately fixed recently, at 201.3 Mya. Both dates are gaining accuracy by using more accurate forms of radiometric dating, in particular the decay of uranium to lead in zircons formed at time of the impact. So, the evidence suggests the Manicouagan impact preceded the end of the Triassic by approximately 10±2 Ma. It could not therefore be the immediate cause of the observed mass extinction.[45]

Skull of a Triassic Period Phytosaur found in the Petrified Forest National Park

The number of Late Triassic extinctions is disputed. Some studies suggest that there are at least two periods of extinction towards the end of the Triassic, separated by 12 to 17 million years. But arguing against this is a recent study of North American faunas. In the Petrified Forest of northeast Arizona there is a unique sequence of late Carnian-early Norian terrestrial sediments. An analysis in 2002 found no significant change in the paleoenvironment.[46] Phytosaurs, the most common fossils there, experienced a change-over only at the genus level, and the number of species remained the same. Some aetosaurs, the next most common tetrapods, and early dinosaurs, passed through unchanged. However, both phytosaurs and aetosaurs were among the groups of archosaur reptiles completely wiped out by the end-Triassic extinction event.

It seems likely then that there was some sort of end-Carnian extinction, when several herbivorous archosauromorph groups died out, while the large herbivorous therapsids—the kannemeyeriid dicynodonts and the traversodont cynodonts—were much reduced in the northern half of Pangaea (Laurasia).

These extinctions within the Triassic and at its end allowed the dinosaurs to expand into many niches that had become unoccupied. Dinosaurs became increasingly dominant, abundant and diverse, and remained that way for the next 150 million years. The true "Age of Dinosaurs" is during the following Jurassic and Cretaceous periods, rather than the Triassic.

See also[edit]

Notes[edit]

  1. ^ Widmann, Philipp; Bucher, Hugo; Leu, Marc; et al. (2020). "Dynamics of the Largest Carbon Isotope Excursion During the Early Triassic Biotic Recovery". Frontiers in Earth Science. 8 (196): 1-16. doi:10.3389/feart.2020.00196.
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  3. ^ Retallack, G. J.; Veevers, J.; Morante, R. (1996). "Global coal gap between Permian-Triassic extinctions and middle Triassic recovery of peat forming plants". GSA Bulletin. 108 (2): 195-207. doi:10.1130/0016-7606(1996)108<0195:GCGBPT>2.3.CO;2. Retrieved 2007-09-29.
  4. ^ Payne, J. L.; Lehrmann, D. J.; Wei, J.; Orchard, M. J.; Schrag, D. P.; Knoll, A. H. (2004). "Large Perturbations of the Carbon Cycle During Recovery from the End-Permian Extinction". Science. 305 (5683): 506-9. doi:10.1126/science.1097023. PMID 15273391.
  5. ^ Ogg, James G.; Ogg, Gabi M.; Gradstein, Felix M. (2016). "Triassic". A Concise Geologic Time Scale: 2016. Elsevier. pp. 133-149. ISBN 978-0-444-63771-0.
  6. ^ Hongfu, Yin; Kexin, Zhang; Jinnan, Tong; Zunyi, Yang; Shunbao, Wu (June 2001). "The Global Stratotype Section and Point (GSSP) of the Permian-Triassic Boundary" (PDF). Episodes. 24 (2): 102-14. doi:10.18814/epiiugs/2001/v24i2/004. Retrieved 8 December 2020.
  7. ^ Hillebrandt, A.v.; Krystyn, L.; Kürschner, W.M.; et al. (September 2013). "The Global Stratotype Sections and Point (GSSP) for the base of the Jurassic System at Kuhjoch (Karwendel Mountains, Northern Calcareous Alps, Tyrol, Austria)". Episodes. 36 (3): 162-98. CiteSeerX 10.1.1.736.9905. doi:10.18814/epiiugs/2013/v36i3/001. Retrieved 12 December 2020.
  8. ^ "Triassic". Dictionary.com Unabridged. Random House.
  9. ^ Ogg, James G.; Ogg, Gabi M.; Gradstein, Felix M. (2016). "Triassic". A Concise Geologic Time Scale: 2016. Elsevier. pp. 133-49. ISBN 978-0-444-63771-0.
  10. ^ a b Sahney, S. & Benton, M.J. (2008). "Recovery from the most profound mass extinction of all time". Proceedings of the Royal Society B: Biological Sciences. 275 (1636): 759-65. doi:10.1098/rspb.2007.1370. PMC 2596898. PMID 18198148.
  11. ^ Brusatte, S. L.; Benton, M. J.; Ruta, M.; Lloyd, G. T. (2008-09-12). "Superiority, Competition, and Opportunism in the Evolutionary Radiation of Dinosaurs" (PDF). Science. 321 (5895): 1485-88. Bibcode:2008Sci...321.1485B. doi:10.1126/science.1161833. PMID 18787166. S2CID 13393888. Archived from the original (PDF) on 2014-06-24. Retrieved 2012-01-14.
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  13. ^ Friedrich von Alberti, Beitrag zu einer Monographie des bunten Sandsteins, Muschelkalks und Keupers, und die Verbindung dieser Gebilde zu einer Formation [Contribution to a monograph on the colored sandstone, shell limestone and mudstone, and the joining of these structures into one formation] (Stuttgart and Tübingen, (Germany): J. G. Cotta, 1834). Alberti coined the term "Trias" on page 324 :

    "… bunter Sandstein, Muschelkalk und Keuper das Resultat einer Periode, ihre Versteinerungen, um mich der Worte E. de Beaumont's zu bedeinen, die Thermometer einer geologischen Epoche seyen, … also die bis jezt beobachtete Trennung dieser Gebilde in 3 Formationen nicht angemessen, und es mehr dem Begriffe Formation entsprechend sey, sie zu einer Formation, welche ich vorläufig Trias nennen will, zu verbinden."

    ( … colored sandstone, shell limestone, and mudstone are the result of a period; their fossils are, to avail myself of the words of E. de Beaumont, the thermometer of a geologic epoch; … thus the separation of these structures into 3 formations, which has been maintained until now, isn't appropriate, and it is more consistent with the concept of "formation" to join them into one formation, which for now I will name "trias".)
  14. ^ Herbert, Chris; Helby, Robin (1980). A Guide to the Sydney basin. Maitland, NSW: Geological Survey of NSW. p. 582. ISBN 978-0-7240-1250-3.
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  22. ^ a b Stanley, 452-53.
  23. ^ Preto, N.; Kustatscher, E.; Wignall, P. B. (2010). "Triassic climates - State of the art and perspectives". Palaeogeography, Palaeoclimatology, Palaeoecology. 290 (1-4): 1-10. Bibcode:2010PPP...290....1P. doi:10.1016/j.palaeo.2010.03.015.
  24. ^ Manfredo Capriolo; et al. (2020). "Deep CO2 in the end-Triassic Central Atlantic Magmatic Province". 11 (1670). Nature Communications. doi:10.1038/s41467-020-15325-6.
  25. ^ How snowball Earth gave rise to complex life - Cosmos Magazine
  26. ^ December: Phytoplankton | News | University of Bristol
  27. ^ The rise of algae in Cryogenian oceans and the emergence of animals - ResearchGate
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  30. ^ Romano, Carlo; Koot, Martha B.; Kogan, Ilja; Brayard, Arnaud; Minikh, Alla V.; Brinkmann, Winand; Bucher, Hugo; Kriwet, Jürgen (February 2016). "Permian-Triassic Osteichthyes (bony fishes): diversity dynamics and body size evolution". Biological Reviews. 91 (1): 106-47. doi:10.1111/brv.12161. PMID 25431138. S2CID 5332637.
  31. ^ Romano, Carlo (January 2021). "A Hiatus Obscures the Early Evolution of Modern Lineages of Bony Fishes". Frontiers in Earth Science. 8: 618853. doi:10.3389/feart.2020.618853.
  32. ^ Romano, Carlo; Jenks, James F.; Jattiot, Romain; Scheyer, Torsten M. (2017). "Marine Early Triassic Actinopterygii from Elko County (Nevada, USA): implications for the Smithian equatorial vertebrate eclipse". Journal of Paleontology. 91 (5): 1-22. doi:10.1017/jpa.2017.36.
  33. ^ Prehistoric Life: The Definitive Visual History of Life On Earth. London: Dorling Kindersley. 2009. pp. 206-07. ISBN 978-0756655730.
  34. ^ Douglas Palmer & Peter Barrett (2009). Evolution: The Story of Life. London: The Natural History Museum. ISBN 978-1845333393.CS1 maint: uses authors parameter (link)
  35. ^ Agnolin, F. L., Mateus O., Milàn J., Marzola M., Wings O., Adolfssen J. S., & Clemmensen L. B. (2018). Ceratodus tunuensis, sp. nov., a new lungfish (Sarcopterygii, Dipnoi) from the Upper Triassic of central East Greenland. Journal of Vertebrate PaleontologyJournal of Vertebrate Paleontology. e1439834
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  42. ^ Retallack, G.J.; Krull, E.S. (2006). "Carbon isotopic evidence for terminal-Permian methane outbursts and their role in extinctions of animals, plants, coral reefs, and peat swamps" (PDF). Geological Society of American Special Paper. 399: 249. doi:10.1130/2006.2399(12). ISBN 9780813723990. Retrieved 14 December 2020.
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  44. ^ Marzoli et al., 1999, Science 284. Extensive 200-million-year-old continental flood basalts of the Central Atlantic Magmatic Province, pp. 618-620.
  45. ^ Hodych & Dunning, 1992.
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References[edit]

External links[edit]

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