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Early/Lower Triassic
251.9 – 247.2 Ma PreꞒ Ꞓ O S D C P T J K Pg N ↓
A map of Earth as it appeared 250 million years ago during the Early Triassic Epoch, Olenekian Age
Sandstone from the Lower Triassic Series
Chronology
−255 —–−250 —–−245 —–−240 —–−235 —–−230 —–−225 —–−220 —–−215 —–−210 —–−205 —–−200 — PzMesozoicPTriassicJLopingianEarlyMiddleLateEarly JOlenekianInduanAnisianLadinianCarnianNorianRhaetian     ← Permian-Triassic extinction event ← Smithian–Spathian boundary event ← Carnian pluvial episode ← Full recovery of woody trees ← Coals return ← Scleractinian corals & calcified sponges ← Triassic–Jurassic extinction event ← Manicouagan impact Subdivision of the Triassic according to the ICS, as of 2023. Vertical axis scale: Millions of years ago
Etymology
Chronostratigraphic name	Lower Triassic
Geochronological name	Early Triassic
Name formality	Formal
Usage information
Celestial body	Earth
Regional usage	Global (ICS)
Time scale(s) used	ICS Time Scale
Definition
Chronological unit	Epoch
Stratigraphic unit	Series
Time span formality	Formal
Lower boundary definition	FAD of the Conodont Hindeodus parvus
Lower boundary GSSP	Meishan, Zhejiang, China 31°04′47″N 119°42′21″E / 31.0798°N 119.7058°E / 31.0798; 119.7058
Lower GSSP ratified	2001
Upper boundary definition	Not formally defined
Upper boundary definition candidates	FAD of the Conodont Chiosella timorensis Base of magnetic zone MT1n
Upper boundary GSSP candidate section(s)	Desli Caira, Northern Dobruja, Romania Guandao, Guizhou, China

The Early Triassic is the first of three epochs of the Triassic Period of the geologic timescale. It spans the time between 251.9 Ma and 247.2 Ma (million years ago). Rocks from this epoch are collectively known as the Lower Triassic Series, which is a unit in chronostratigraphy. The Early Triassic is the oldest epoch of the Mesozoic Era. It is preceded by the Lopingian Epoch (late Permian, Paleozoic Era) and followed by the Middle Triassic Epoch. The Early Triassic is divided into the Induan and Olenekian ages. The Induan is subdivided into the Griesbachian and Dienerian subages and the Olenekian is subdivided into the Smithian and Spathian subages.

The Lower Triassic series is coeval with the Scythian Stage, which is today not included in the official timescales but can be found in older literature. In Europe, most of the Lower Triassic is composed of Buntsandstein, a lithostratigraphic unit of continental red beds.

The Early Triassic and partly also the Middle Triassic span the interval of biotic recovery from the Permian-Triassic extinction event, the most severe mass extinction event in Earth's history. A second extinction event, the Smithian-Spathian boundary event, occurred during the Olenekian. A third extinction event occurred at the Olenekian-Anisian boundary, marking the end of the Early Triassic epoch.

Early Triassic climate

The climate during the Early Triassic Epoch (especially in the interior of the supercontinent Pangaea) was generally arid, rainless and dry and deserts were widespread; however the poles possessed a temperate climate. The pole-to-equator temperature gradient was temporally flat during the Early Triassic and may have allowed tropical species to extend their distribution poleward. This is evidenced by the global distribution of ammonoids. The extremely hot ocean temperatures facilitated extremely powerful hurricanes that frequently hit the coast of North China.

The mostly hot climate of the Early Triassic may have been caused by late volcanic eruptions of the Siberian Traps, which had probably triggered the Permian-Triassic extinction event and accelerated the rate of global warming into the Triassic. Studies suggest that Early Triassic climate was very volatile, punctuated by a number of relatively rapid global temperature changes, marine anoxic events, and carbon cycle disturbances, which led to subsequent extinction events in the aftermath of the Permian-Triassic extinction event. On the other hand, an alternative hypothesis proposes these Early Triassic climatic perturbations and biotic upheavals that inhibited the recovery of life following the P-T mass extinction to have been linked to forcing driven by changes in the Earth's obliquity defined by a roughly 32.8 thousand year periodicity with strong 1.2 million year modulations. According to proponents of this hypothesis, radiometric dating indicates that major activity from the Siberian Traps ended very shortly after the end-Permian extinction and did not span the entire Early Triassic epoch, thus not being the primary culprit for the climatic changes throughout this epoch.

Early Triassic life

Fauna and flora

The Triassic Period opened in the aftermath of the Permian–Triassic extinction event. The massive extinctions that ended the Permian Period (and with that the Paleozoic Era) caused extreme hardships for the surviving species.

The Early Triassic Epoch saw the biotic recovery of life after the biggest mass extinction event of the past, which took millions of years due to the severity of the event and the harsh Early Triassic climate. Many types of corals, brachiopods, molluscs, echinoderms, and other invertebrates had disappeared. The Permian vegetation, which was dominated by Glossopteris in the Southern Hemisphere, ceased to exist. Other groups, such as Actinopterygii, appear to have been less affected by this extinction event and body size was not a selective factor during the extinction event. Animals that were most successful in the Early Triassic were those with high metabolisms. Different patterns of recovery are evident on land and in the sea. Early Triassic faunas lacked biodiversity and were relatively homogeneous due to the effects of the extinction. The ecological recovery on land took 30 million years, well into the Late Triassic. Two Early Triassic lagerstätten stand out due to their exceptionally high biodiversity, the Dienerian aged Guiyang biota and the earliest Spathian aged Paris biota.

Terrestrial biota

The most common land vertebrate was the small herbivorous synapsid Lystrosaurus. Often interpreted as a disaster taxon (although this view was questioned), Lystrosaurus had a wide range across Pangea. In the southern part of the supercontinent, it co-occurred with the non-mammalian cynodonts Galesaurus and Thrinaxodon, early relatives of mammals. The first archosauriforms appeared, such as Erythrosuchus (Olenekian-Ladinian). This group includes the ancestors of crocodiles and dinosaurs (including birds). Fossilized foot prints of dinosauromorphs are known from the Olenekian. The Early Triassic entomofauna is very poorly understood because of the paucity of insect fossils from this epoch.

The flora was gymnosperm-dominated at the onset of the Triassic, but changed rapidly and became lycopod-dominated (e.g. Pleuromeia) during the Griesbachian-Dienerian ecological crisis. This change coincided with the extinction of the Permian Glossopteris flora. In the Spathian subage, the flora changed back to gymnosperm and pteridophyte dominated. These shifts reflect global changes in precipitation and temperature. Floral diversity was overall very low during the Early Triassic, as plant life had yet to fully recover from the Permian-Triassic extinction.

Microbially induced sedimentary structures (MISS) are common in the fossil record of North China in the immediate aftermath of the Permian-Triassic extinction, indicating that microbial mats dominated local terrestrial ecosystems following the Permian-Triassic boundary. The regional prevalence of MISS is attributable to a decrease in bioturbation and grazing pressure as a result of aridification and temperature increase. MISS have also been reported from Early Triassic fossil deposits in Arctic Canada. The disappearance of MISS later in the Early Triassic has been interpreted as a signal of increased bioturbation and recovery of terrestrial ecosystems.

Aquatic biota

In the oceans, the most common Early Triassic hard-shelled marine invertebrates were bivalves, gastropods, ammonoids, echinoids, and a few articulate brachiopods. Conodonts experienced a revival in diversity following a nadir during the Permian. The first oysters (Liostrea) appeared in the Early Triassic. They grew on the shells of living ammonoids as epizoans. Microbial reefs were common, possibly due to lack of competition with metazoan reef builders as a result of the extinction. However, transient metazoan reefs reoccurred during the Olenekian wherever permitted by environmental conditions. Ammonoids show blooms followed by extinctions during the Early Triassic.

Aquatic vertebrates diversified after the extinction:

• Fishes: Many species of fish had a worldwide distribution during the Early Triassic. Typical Triassic ray-finned fishes, such as Australosomus, Birgeria, Bobasatrania, Boreosomus, Pteronisculus, Parasemionotidae and Saurichthys appeared close to the Permian-Triassic boundary, whereas neopterygians (including stem teleosts) diversified later during the Triassic, though the pattern of the Triassic diversification of bony fishes is not well understood due to a taphonomic megabias (Spathian-Bithynian Gap, SBG) in the late Early Triassic and early Middle Triassic. The earliest large durophagous neopterygian is known from this gap, suggesting an early onset in feeding specializations of this group. Most bony fish reached large body sizes during the Early Triassic. Coelacanths show a peak in their diversity during this epoch, including new modes of life, such as the fork-tailed Rebellatrix. Chondrichthyes are represented by Hybodontiformes like Palaeobates, Omanoselache, Lissodus, some Neoselachii, as well as a few last survivors of the Eugeneodontida (Caseodus, Fadenia).

• Amphibians: Relatively large, marine temnospondyl amphibians, such as Aphaneramma or Wantzosaurus, were geographically widespread during the Induan and Olenekian ages. The fossils of these crocodile-shaped amphibians were found in Greenland, Spitsbergen, Pakistan and Madagascar.

• Reptiles: In the oceans, the first marine reptiles appeared during the Early Triassic. Their descendants ruled the oceans during the Mesozoic. Hupehsuchia, Ichthyopterygia and sauropterygians are among the first marine reptiles to enter the scene in the Olenekian (e.g. Cartorhynchus, Chaohusaurus, Utatsusaurus, Hupehsuchus, Grippia, Omphalosaurus, Corosaurus). Other marine reptiles such as Tanystropheus, Helveticosaurus, Atopodentatus, placodonts or the thalattosaurs followed later in the Middle Triassic. The Anisian aged ichthyosaur Thalattoarchon was one of the first marine macropredators capable of eating prey that was similar in size to itself, an ecological role that can be compared to that of modern orcas.

Fossil gallery

• Early Triassic brittle stars (echinoderms)
• Fossils of the bivalve Claraia clarai
• Early Triassic ammonoid Hedenstroemia
• Fossil of the Early Triassic neopterygian Candelarialepis argentus
• Early Triassic Hupehsuchus fossil in the Paleozoological Museum of China
• Skull of the Early Triassic archosauriform Erythrosuchus
• Lystrosaurus hedini skeleton at the Museum of Paleontology in Tübingen

See also

• Geologic time scale
• Triassic
• Mass extinction

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Further reading

• Martinetto, Edoardo; Tschopp, Emanuel; Gastaldo, Robert, eds. (2020). Nature through Time: Virtual field trips through the Nature of the past. Springer International Publishing. ISBN 978-3-030-35057-4.

External links

• GeoWhen Database – Early Triassic
• Palaeos (archived 2 January 2006)
• scotese

v t e Geological history of Earth
Cenozoic Era (present–66.0 Ma)	Quaternary (present–2.58 Ma) Holocene (present–11.7 ka) Pleistocene (11.7 ka–2.58 Ma) Neogene (2.58–23.0 Ma) Pliocene (2.59–5.33 Ma) Miocene (5.33–23.0 Ma) Paleogene (23.0–66.0 Ma) Oligocene (23.0–33.9 Ma) Eocene (33.9–56.0 Ma) Paleocene (56.0–66.0 Ma)
Mesozoic Era (66.0–252 Ma)	Cretaceous (66.0–145 Ma) Late (66.0–100 Ma) Early (100–145 Ma) Jurassic (145–201 Ma) Late (145–164 Ma) Middle (164–174 Ma) Early (174–201 Ma) Triassic (201–252 Ma) Late (201–237 Ma) Middle (237–247 Ma) Early (247–252 Ma)
Paleozoic Era (252–539 Ma)	Permian (252–299 Ma) Lopingian (252–260 Ma) Guadalupian (260–272 Ma) Cisuralian (272–299 Ma) Carboniferous (299–359 Ma) Pennsylvanian (299–323 Ma) Mississippian (323–359 Ma) Devonian (359–419 Ma) Late (359–383 Ma) Middle (383–393 Ma) Early (393–419 Ma) Silurian (419–444 Ma) Pridoli (419–423 Ma) Ludlow (423–427 Ma) Wenlock (427–433 Ma) Llandovery (433–444 Ma) Ordovician (444–485 Ma) Late (444–458 Ma) Middle (458–470 Ma) Early (470–485 Ma) Cambrian (485–539 Ma) Furongian (485–497 Ma) Miaolingian (497–509 Ma) Series 2 (509–521 Ma) Terreneuvian (521–539 Ma)
Proterozoic Eon (539 Ma–2.5 Ga)	Neoproterozoic (539 Ma–1 Ga) Ediacaran (539–635 Ma) Cryogenian (635–720 Ma) Tonian (720 Ma–1 Ga) Mesoproterozoic (1–1.6 Ga) Stenian (1–1.2 Ga) Ectasian (1.2–1.4 Ga) Calymmian (1.4–1.6 Ga) Paleoproterozoic (1.6–2.5 Ga) Statherian (1.6–1.8 Ga) Orosirian (1.8–2.05 Ga) Rhyacian (2.05–2.3 Ga) Siderian (2.3–2.5 Ga)
Archean Eon (2.5–4 Ga)	Neoarchean (2.5–2.8 Ga) Mesoarchean (2.8–3.2 Ga) Paleoarchean (3.2–3.6 Ga) Eoarchean (3.6–4 Ga)
Hadean Eon (4–4.6 Ga)
ka = kiloannum (thousand years ago); Ma = megaannum (million years ago); Ga = gigaannum (billion years ago). See also: Geologic time scale  • Geology portal  • World portal

• Early Triassic
• Triassic geochronology
• Geological epochs
• Triassic