Ordovician

Ordovician Period 488.3 – 443.7 million years ago PreЄ Є O S D C P T J K Pg N Mean atmospheric O2 content over period duration ca. 13.5 Vol %1 (68 % of modern level) Mean atmospheric CO2 content over period duration ca. 4200 ppm2 (15 times pre-industrial level) Mean surface temperature over period duration ca. 16 °C3 (2 °C above modern level) Sea level (above present day) 180m; rising to 220m in Caradoc and falling sharply to 140m in end-Ordovician glaciations4 The Ordovician /ɔrdəˈvɪʃən/ is a geologic period and system, the second of six of the Paleozoic Era, and covers the time between 488.3±1.7 to 443.7±1.5 million years ago (ICS, 2004,5 chart). It follows the Cambrian Period and is followed by the Silurian Period. The Ordovician, named after the Celtic tribe of the Ordovices, was defined by Charles Lapworth in 1879 to resolve a dispute between followers of Adam Sedgwick and Roderick Murchison, who were placing the same rock beds in northern Wales into the Cambrian and Silurian periods respectively. Lapworth, recognizing that the fossil fauna in the disputed strata were different from those of either the Cambrian or the Silurian periods, realized that they should be placed in a period of their own. While recognition of the distinct Ordovician Period was slow in the United Kingdom, other areas of the world accepted it quickly. It received international sanction in 1906, when it was adopted as an official period of the Paleozoic Era by the International Geological Congress. Contents 1 Dating 2 Subdivisions 3 Paleogeography 4 Geochemistry 5 Climate and sea level 6 Life 6.1 Fauna 6.2 Flora 7 End of the period 8 References 9 External links // Dating The Ordovician Period started at a major extinction event called the Cambrian-Ordovician extinction events some time about 488.3 ± 1.7 Mya (million years ago), and lasted for about 44.6 million years. It ended with the Ordovician–Silurian extinction event, about 443.7 ± 1.5 Mya (ICS, 2004) that wiped out 60% of marine genera. The dates given are recent radiometric dates and vary slightly from those used in other sources. This second period of the Paleozoic era created abundant fossils and in some regions, major petroleum and gas reservoirs. The boundary chosen for the beginning both of the Ordovician Period and the Tremadocian stage is highly useful. Since it correlates well with the occurrence of widespread graptolite, conodont, and trilobite species, the base of the Tremadocian allows scientists not only to relate these species to each other, but to species that occur with them in other areas as well. This makes it easier to place many more species in time relative to the beginning of the Ordovician Period. Subdivisions Key events in the Ordovician view • discuss •  -490 — – -485 — – -480 — – -475 — – -470 — – -465 — – -460 — – -455 — – -450 — – -445 — –     Cambrian   Tremadocian Floian Dapingian Darriwilian Sandbian Katian Hirnantian Hirnantian Early Ordovician Llanvirn Llandeilo Caradoc Ashgill Silurian       ← First land plant spores6 O r d o v i c i a n  Palæozoic Key events of the Ordovician Period. Left: ICS approved stages. Right: "General" stages. Axis scale: millions of years ago. A number of regional terms have been used to refer to subdivisions of the Ordovician Period. In 2008, the ICS erected a formal international system of subdivisions, illustrated to the right.7 The Ordovician Period in Britain was traditionally broken into Early (Tremadocian and Arenig), Middle (Llanvirn [subdivided into Abereiddian and Llandeilian] and Llandeilo) and Late (Caradoc and Ashgill) epochs. The corresponding rocks of the Ordovician System are referred to as coming from the Lower, Middle, or Upper part of the column. The faunal stages (subdivisions of epochs) from youngest to oldest are: Hirnantian/Gamach (Late Ordovician: Ashgill) Rawtheyan/Richmond (Late Ordovician: Ashgill) Cautleyan/Richmond (Late Ordovician: Ashgill) Pusgillian/Maysville/Richmond (Late Ordovician: Ashgill) Trenton (Middle Ordovician: Caradoc) Onnian/Maysville/Eden (Middle Ordovician: Caradoc) Actonian/Eden (Middle Ordovician: Caradoc) Marshbrookian/Sherman (Middle Ordovician: Caradoc) Longvillian/Sherman (Middle Ordovician: Caradoc) Soundleyan/Kirkfield (Middle Ordovician: Caradoc) Harnagian/Rockland (Middle Ordovician: Caradoc) Costonian/Black River (Middle Ordovician: Caradoc) Chazy (Middle Ordovician: Llandeilo) Llandeilo (Middle Ordovician: Llandeilo) Whiterock (Middle Ordovician: Llanvirn) Llanvirn (Middle Ordovician: Llanvirn) Cassinian (Early Ordovician: Arenig) Arenig/Jefferson/Castleman (Early Ordovician: Arenig) Tremadoc/Deming/Gaconadian (Early Ordovician: Tremadoc) Paleogeography Sea levels were high during the Ordovician; in fact during the Tremadocian, marine transgressions worldwide were the greatest for which evidence is preserved in the rocks. During the Ordovician, the southern continents were collected into a single continent called Gondwana. Gondwana started the period in equatorial latitudes and, as the period progressed, drifted toward the South Pole. Early in the Ordovician, the continents Laurentia (present-day North America), Siberia, and Baltica (present-day northern Europe) were still independent continents (since the break-up of the supercontinent Pannotia earlier), but Baltica began to move towards Laurentia later in the period, causing the Iapetus Ocean to shrink between them. The small continent Avalonia separated from Gondwana and began to head north towards Baltica and Laurentia. The Rheic Ocean between Gondwana and Avalonia was formed as a result. A major mountain-building episode was the Taconic orogeny that was well under way in Cambrian times. In the beginning of the Late Ordovician, from 460 to 450 Ma, volcanoes along the margin of the Iapetus Ocean spewed massive amounts of carbon dioxide into the atmosphere, turning the planet into a hothouse. These volcanic island arcs eventually collided with proto North America to form the Appalachian mountains. By the end of the Late Ordovician these volcanic emissions had stopped. Gondwana had by that time neared or approached the pole and was largely glaciated. Geochemistry The Ordovician was a time of calcite sea geochemistry in which low-magnesium calcite was the primary inorganic marine precipitate of calcium carbonate. Carbonate hardgrounds were thus very common, along with calcitic ooids, calcitic cements, and invertebrate faunas with dominantly calcitic skeletons.89 Unlike Cambrian times, when calcite production was dominated by microbial and non-biological processes, animals (and macroalgae) became a dominant source of calcareous material in Ordovician deposits.10 Climate and sea level The Ordovician saw the highest sea levels of the Palaeozoic, and the low relief of the continents led to many shelf deposits being formed under hundreds of metres of water.10 Sea level rose more or less continuously throughout the Early Ordovician, levelling off somewhat during the middle of the period.10 Locally, some regressions occurred, but sea level rise continued in the beginning of the Late Ordovician. A change was soon on the cards, however, and sea levels fell steadily in accord with the cooling temperatures for the ~30 million years leading up to the Hirnantian glaciation. Within this icy stage, sea level seems to have risen and dropped somewhat, but despite much study the details remain unresolved.10 At the beginning of the period, around 480 million years ago, the climate was very hot due to high levels of CO2, which gave a strong greenhouse effect. The marine waters are assumed to have been around 45°C, which restricted the diversification of complex multi-cellular organisms. But over time, the climate become cooler, and around 460 million years ago, the ocean temperatures became comparable to those of present day equatorial waters.11 As with North America and Europe, Gondwana was largely covered with shallow seas during the Ordovician. Shallow clear waters over continental shelves encouraged the growth of organisms that deposit calcium carbonates in their shells and hard parts. The Panthalassic Ocean covered much of the northern hemisphere, and other minor oceans included Proto-Tethys, Paleo-Tethys, Khanty Ocean, which was closed off by the Late Ordovician, Iapetus Ocean, and the new Rheic Ocean. As the Ordovician progressed, we see evidence of glaciers on the land we now know as Africa and South America. At the time these land masses were sitting at the South Pole, and covered by ice caps. Life Nautiloids like Orthoceras were among the largest predators in the Ordovician. A diorama depicting Ordovician flora and fauna. For most of the Late Ordovician, life continued to flourish, but at and near the end of the period there were mass-extinction events that seriously affected planktonic forms like conodonts, graptolites, and some groups of trilobites (Agnostida and Ptychopariida, which completely died out, and the Asaphida, which were much reduced). Brachiopods, bryozoans and echinoderms were also heavily affected, and the endocerid cephalopods died out completely, except for possible rare Silurian forms. The Ordovician-Silurian Extinction Events may have been caused by an ice age that occurred at the end of the Ordovician period as the end of the Late Ordovician was one of the coldest times in the last 600 million years of earth history. Fauna On the whole, the fauna that emerged in the Ordovician set the template for the remainder of the Palaeozoic.10 The fauna was dominated by tiered communities of suspension feeders, mainly with short food chains; this said, the ecological system reached a new grade of complexity far beyond that of the Cambrian fauna,10 which has persisted until the present day.10 Though less famous than the Cambrian explosion, the Ordovician featured an adaptive radiation, the Ordovician radiation, that was no less remarkable; marine faunal genera increased fourfold, resulting in 12% of all known Phanerozoic marine fauna.12 Another change in the fauna was the strong increase in filter feeding organisms.13 The trilobite, inarticulate brachiopod, archaeocyathid, and eocrinoid faunas of the Cambrian were succeeded by those that dominated the rest of the Paleozoic, such as articulate brachiopods, cephalopods, and crinoids. Articulate brachiopods, in particular, largely replaced trilobites in shelf communities.14 Their success epitomizes the greatly increased diversity of carbonate shell-secreting organisms in the Ordovician compared to the Cambrian.14 In North America and Europe, the Ordovician was a time of shallow continental seas rich in life. Trilobites and brachiopods in particular were rich and diverse. Although solitary corals date back to at least the Cambrian, reef-forming corals appeared in the early Ordovician, corresponding to an increase in the stability of carbonate and thus a new abundance of calcifying animals.10 Molluscs, which appeared during the Cambrian or even the Ediacaran, became common and varied, especially bivalves, gastropods, and nautiloid cephalopods. Now-extinct marine animals called graptolites thrived in the oceans. Some new cystoids and crinoids appeared. It was long thought that the first true vertebrates (fish — Ostracoderms) appeared in the Ordovician, but recent discoveries in China reveal that they probably originated in the Early Cambrian. The very first gnathostome (jawed fish) appeared in the Late Ordovician epoch. During the Middle Ordovician there was a large increase in the intensity and diversity of bioeroding organisms. This is known as the Ordovician Bioerosion Revolution.15 It is marked by a sudden abundance of hard substrate trace fossils such as Trypanites, Palaeosabella and Petroxestes. In the Early Ordovician, trilobites were joined by many new types of organisms, including tabulate corals, strophomenid, rhynchonellid, and many new orthid brachiopods, bryozoans, planktonic graptolites and conodonts, and many types of molluscs and echinoderms, including the ophiuroids ("brittle stars") and the first sea stars. Nevertheless the trilobites remained abundant, with all the Late Cambrian orders continuing, and being joined by the new group Phacopida. The first evidence of land plants also appeared; see Evolutionary history of life. In the Middle Ordovician, the trilobite-dominated Early Ordovician communities were replaced by generally more mixed ecosystems, in which brachiopods, bryozoans, molluscs, cornulitids, tentaculitids and echinoderms all flourished, tabulate corals diversified and the first rugose corals appeared; trilobites were no longer predominant. The planktonic graptolites remained diverse, with the Diplograptina making their appearance. Bioerosion became an important process, particularly in the thick calcitic skeletons of corals, bryozoans and brachiopods, and on the extensive carbonate hardgrounds that appear in abundance at this time. One of the earliest known armoured agnathan ("ostracoderm") vertebrate, Arandaspis, dates from the Middle Ordovician. Trilobites in the Ordovician were very different than their predecessors in the Cambrian. Many trilobites developed bizarre spines and nodules to defend against predators such as primitive sharks and nautiloids while other trilobites such as Aeglina prisca evolved to become swimming forms. Some trilobites even developed shovel-like snouts for ploughing through muddy sea bottoms. Another unusual clade of trilobites known as the trinucleids developed a broad pitted margin around their head shields.16 Some trilobites such as Asaphus kowalewski evolved long eyestalks to assist in detecting predators whereas other trilobite eyes in contrast disappeared completely.17 The Upper Ordovician edrioasteroid Cystaster stellatus on a cobble from the Kope Formation in northern Kentucky. In the background is the cyclostome bryozoan Corynotrypa. Fossil Mountain, west-central Utah; Middle Ordovician fossiliferous shales and limestones in the lower half. Outcrop of Upper Ordovician rubbly limestone and shale, southern Indiana; College of Wooster students. Outcrop of Upper Ordovician limestone and minor shale, central Tennessee; College of Wooster students. Trypanites borings in an Ordovician hardground, southeastern Indiana.18 Petroxestes borings in an Ordovician hardground, southern Ohio.15 Outcrop of Ordovician kukersite oil shale, northern Estonia. Bryozoan fossils in Ordovician kukersite oil shale, northern Estonia. Brachiopods and bryozoans in an Ordovician limestone, southern Minnesota. Platystrophia ponderosa, Maysvillian (Upper Ordovician) near Madison, Indiana. Scale bar is 5.0 mm. The Ordovician cystoid Echinosphaerites (an extinct echinoderm) from northeastern Estonia; approximately 5 cm in diameter. Prasopora, a trepostome bryozoan from the Ordovician of Iowa. An Ordovician strophomenid brachiopod with encrusting inarticulate brachiopods and a bryozoan. The heliolitid coral Protaraea richmondensis encrusting a gastropod; Cincinnatian (Upper Ordovician) of southeastern Indiana. Zygospira modesta, spiriferid brachiopods, preserved in their original positions on a trepostome bryozoan; Cincinnatian (Upper Ordovician) of southeastern Indiana. Graptolites (Amplexograptus) from the Ordovician near Caney Springs, Tennessee. Flora Green algae were common in the Late Cambrian (perhaps earlier) and in the Ordovician. Terrestrial plants probably evolved from green algae, first appearing in the form of tiny non-vascular mosses resembling liverworts. Fossil spores from land plants have been identified in uppermost Ordovician sediments. Among the first land fungi may have been arbuscular mycorrhiza fungi (Glomerales), playing a crucial role in facilitating the colonization of land by plants through mycorrhizal symbiosis, which makes mineral nutrients available to plant cells; such fossilized fungal hyphae and spores from the Ordovician of Wisconsin have been found with an age of about 460 million years ago, a time when the land flora most likely only consisted of plants similar to non-vascular bryophytes.19 End of the period Main article: Ordovician-Silurian extinction events The Ordovician came to a close in a series of extinction events that, taken together, comprise the second largest of the five major extinction events in Earth's history in terms of percentage of genera that went extinct. The only larger one was the Permian-Triassic extinction event. The extinctions occurred approximately 447–444 million years ago and mark the boundary between the Ordovician and the following Silurian Period. At that time all complex multicellular organisms lived in the sea, and about 49% of genera of fauna disappeared forever; brachiopods and bryozoans were greatly reduced, along with many trilobite, conodont and graptolite families. The most commonly accepted theory is that these events were triggered by the onset of most cold conditions in the late Katian, followed by an ice age, in the Hirnantian faunal stage, that ended the long, stable greenhouse conditions typical of the Ordovician. The ice age was possibly not long-lasting, study of oxygen isotopes in fossil brachiopods showing that its duration could have been only 0.5 to 1.5 million years.9 Other researchers (Page et al.) estimate more temperate conditions did not return until the late Silurian. The late Ordovician glaciation event was preceded by a fall in atmospheric carbon dioxide (from 7000 ppm to 4400 ppmcitation needed), which selectively affected the shallow seas where most organisms lived. As the southern supercontinent Gondwana drifted over the South Pole, ice caps formed on it, which have been detected in Upper Ordovician rock strata of North Africa and then-adjacent northeastern South America, which were south-polar locations at the time. Glaciation locks up water from the world-ocean, and the interglacials free it, causing sea levels repeatedly to drop and rise; the vast shallow intra-continental Ordovician seas withdrew, which eliminated many ecological niches, then returned carrying diminished founder populations lacking many whole families of organisms, then withdrew again with the next pulse of glaciation, eliminating biological diversity at each change.20 Species limited to a single epicontinental sea on a given landmass were severely affected.9 Tropical lifeforms were hit particularly hard in the first wave of extinction, while cool-water species were hit worst in the second pulse.9 Surviving species were those that coped with the changed conditions and filled the ecological niches left by the extinctions. At the end of the second event, melting glaciers caused the sea level to rise and stabilise once more. The rebound of life's diversity with the permanent re-flooding of continental shelves at the onset of the Silurian saw increased biodiversity within the surviving Orders. Melott et al. (2006) suggested a ten-second gamma ray burst could have destroyed the ozone layer and exposed terrestrial and marine surface-dwelling life to deadly radiation and initiated global cooling.21 References ^ Image:Sauerstoffgehalt-1000mj.svg ^ Image:Phanerozoic Carbon Dioxide.png ^ Image:All palaeotemps.png ^ Haq, B. U.; Schutter, SR (2008). "A Chronology of Paleozoic Sea-Level Changes". Science 322 (5898): 64–68. doi:10.1126/science.1161648. PMID 18832639.  ^ Gradstein, Felix M.; Ogg, J. G.; Smith, A. G. (2004). A Geologic Time Scale 2004. Cambridge: Cambridge University Press. ISBN 0521786738.  ^ Wellman, C.H., Gray, J. (2000). "The microfossil record of early land plants". Phil. Trans. R. Soc. B 355 (1398): 717–732. doi:10.1098/rstb.2000.0612.  ^ Details on the Dapingian are available at Wang, X.; Stouge, S.; Chen, X.; Li, Z.; Wang, C. (2009). "Dapingian Stage: standard name for the lowermost global stage of the Middle Ordovician Series". Lethaia 42: 377–380. doi:10.1111/j.1502-3931.2009.00169.x.  ^ Template:Cite doi 10.1016/S0031-0182(98)00109-6 ^ a b c d Stanley, S. M.; Hardie, L. A. (1999). "Hypercalcification; paleontology links plate tectonics and geochemistry to sedimentology". GSA Today 9: 1–7.  ^ a b c d e f g h Munnecke, A.; Calner, M.; Harper, D. A. T.; Servais, T. (2010). "Ordovician and Silurian sea-water chemistry, sea level, and climate: A synopsis". Palaeogeography, Palaeoclimatology, Palaeoecology 296: 389. doi:10.1016/j.palaeo.2010.08.001.  ^ Explosion in marine biodiversity explained by climate change ^ Dixon, Dougal; et al. (2001). Atlas of Life on Earth. New York: Barnes & Noble Books. pp. 87. ISBN 0760719578.  ^ Palaeos Paleozoic : Ordovician : The Ordovician Period ^ a b Cooper, John D.; Miller, Richard H.; Patterson, Jacqueline (1986). A Trip Through Time: Principles of Historical Geology. Columbus: Merrill Publishing Company. pp. 247, 255–259. ISBN 0675201403.  ^ a b Wilson, M. A.; Palmer, T. J. (2006). "Patterns and processes in the Ordovician Bioerosion Revolution" (PDF). Ichnos 13: 109–112. doi:10.1080/10420940600850505. http://www3.wooster.edu/geology/WilsonPalmer06.pdf.  ^ "Palaeos Paleozoic : Ordovician : The Ordovician Period". April 11, 2002. http://www.palaeos.com/Paleozoic/Ordovician/Ordovician.htm#Life.  ^ A Guide to the Orders of Trilobites ^ Wilson, M. A.; Palmer, T. J. (2001). "Domiciles, not predatory borings: a simpler explanation of the holes in Ordovician shells analyzed by Kaplan and Baumiller, 2000". PALAIOS 16: 524–525. doi:10.1669/0883-1351(2001)016<0524:DNPBAS>2.0.CO;2.  ^ Redecker, D.; Kodner, R. ; Graham, L. E. (2000). "Glomalean fungi from the Ordovician". Science 289 (5486): 1920–1921. doi:10.1126/science.289.5486.1920. PMID 10988069.  ^ Emiliani (1992), 491 ^ Melott, Adrian; et al. (2004). "Did a gamma-ray burst initiate the late Ordovician mass extinction?". International Journal of Astrobiology 3: 55–61. doi:10.1017/S1473550404001910.  External links Wikimedia Commons has media related to: Ordovician Ogg, Jim (June 2004). "Overview of Global Boundary Stratotype Sections and Points (GSSP's)". Archived from the original on 2006-04-23. http://web.archive.org/web/20060423084018/http://www.stratigraphy.org/gssp.htm. Retrieved 2006-04-30.  Mehrtens, Charlotte. "Chazy Reef at Isle La Motte". http://www.anr.state.vt.us/dec/geo/chazytxt.htm.  An Ordovician reef in Vermont. Examples of Ordovician Fossils Ordovician fossils of the famous Cincinnatian Group The Dry Dredgers, an active group of amateur paleontologists in the Cincinnati area Preceded by Proterozoic Eon 542 Ma - Phanerozoic Eon - Present 542 Ma - Paleozoic Era - 251 Ma 251 Ma - Mesozoic Era - 65 Ma 65 Ma - Cenozoic Era - Present Cambrian Ordovician Silurian Devonian Carboniferous Permian Triassic Jurassic Cretaceous Paleogene Neogene Quaternary v · d · eGeologic history of Earth  Precambrian (4.57 Gya – 542 Mya) In left column are eons; right column: bold are eras; not bold are periods: Hadean (4.57 – 4 Gya) (informal) Archean (4 – 2.5 Gya) Eoarchean (4 – 3.6 Gya) Paleoarchean (3.6 – 3.2 Gya) Mesoarchean (3.2 – 2.8 Gya) Neoarchean (2.8 – 2.5 Gya) Proterozoic (2.5 Gya – 542 Mya) Paleoproterozoic (2.5 – 1.6 Gya): Siderian (2.5 – 2.3 Gya) · Rhyacian (2.3 – 2.05 Gya) · Orosirian (2.05 – 1.8 Gya) · Statherian (1.8 – 1.6 Gya) Mesoproterozoic (1.6 – 1 Gya): Calymmian (1.6 – 1.4 Gya) · Ectasian (1.4 – 1.2 Gya) · Stenian (1.2 – 1 Gya) Neoproterozoic (1 Gya – 542 Mya): Tonian (1 Gya – 850 Mya) · Cryogenian (850 – 635 Mya) · Ediacaran (635 – 542 Mya) Mya = millions years ago. Gya = billions years ago.  Phanerozoic (542 – 0 Mya) In horizontal bars are eras; in left column are periods; right column: bold are epochs; not bold not italic are ages; italic are chrons:  Paleozoic (542 – 251 Mya) Cambrian (542 – 488.3 Mya) Terreneuvian (542 – 521 Mya): Fortunian (542 – 528 Mya) · Age 2* (528 – 521 Mya) Epoch 2* (521 – 510 Mya): Age 3* (521 – 515 Mya) · Age 4* (515 – 510 Mya) Epoch 3* (510 – 499 Mya): Age 5* (510 – 506.5 Mya) · Drumian (506.5 – 503 Mya) · Guzhangian (503 – 499 Mya) Furongian (499 – 488.3 Mya): Paibian (499 – 496 Mya) · Age 9* (496 – 492 Mya) · Age 10* (492 – 488.3 Mya) Ordovician (488.3 – 443.7 Mya) Early Ordovician (488.3 – 471.8 Mya): Tremadocian (488.3 – 478.6 Mya) · Floian (478.6 – 471.8 Mya) Middle Ordovician (471.8 – 460.9 Mya): Dapingian (471.8 – 468.1 Mya) · Darriwilian (468.1 – 460.9 Mya) Late Ordovician (460.9 – 443.7 Mya): Sandbian (460.9 – 455.8 Mya) · Katian (455.8 – 445.6 Mya) · Hirnantian (445.6 – 443.7 Mya) Silurian (443.7 – 416 Mya) Llandovery (443.7 – 428.2 Mya): Rhuddanian (443.7 – 439 Mya) · Aeronian (439 – 436 Mya) · Telychian (436 – 428.2 Mya) Wenlock (428.2 – 422.9 Mya): Sheinwoodian (428.2 – 426.2 Mya) · Homerian (426.2 – 422.9 Mya) Ludlow (422.9 – 418.7 Mya): Gorstian (422.9 – 421.3 Mya) · Ludfordian (421.3 – 418.7 Mya) Pridoli (418.7 – 416 Mya) Devonian (416 – 359.2 Mya) Early Devonian (416 – 397.5 Mya): Lochkovian (416 – 411.2 Mya) · Pragian (411.2 – 407 Mya) · Emsian (407 – 397.5 Mya) Middle Devonian (397.5 – 385.3 Mya): Eifelian (397.5 – 391.8 Mya) · Givetian (391.8 – 385.3 Mya) Late Devonian (385.3 – 359.2 Mya): Frasnian (385.3 – 374.5 Mya) · Famennian (374.5 – 359.2 Mya) Carboniferous (359.2 – 299 Mya) Mississippian (359.2 – 318.1 Mya): Tournaisian / Early Mississippian (359.2 – 345.3 Mya) · Viséan / Middle Mississippian (345.3 – 328.3 Mya) · Serpukhovian / Late Mississippian (328.3 – 318.1 Mya) Pennsylvanian (318.1 – 299 Mya): Bashkirian / Early Pennsylvanian (318.1 – 311.7 Mya) · Moscovian / Middle Pennsylvanian (311.7 – 307.2 Mya) · Late Pennsylvanian (307.2 – 299 Mya): Kasimovian (307.2 – 303.4 Mya) · Gzhelian (303.4 – 299 Mya) Permian (299 – 251 Mya) Cisuralian (299 – 270.6 Mya): Asselian (299 – 294.6 Mya) · Sakmarian (294.6 – 284.4 Mya) · Artinskian (284.4 – 275.6 Mya) · Kungurian (275.6 – 270.6 Mya) Guadalupian (270.6 – 260.4 Mya): Roadian (270.6 – 268 Mya) · Wordian (268 – 265.8 Mya) · Capitanian (265.8 – 260.4 Mya) Lopingian (260.4 – 251 Mya): Wuchiapingian (260.4 – 253.8 Mya) · Changhsingian (253.8 – 251 Mya)  Mesozoic (251 – 65.5 Mya) Triassic (251 – 199.6 Mya) Early Triassic (251 – 245.9 Mya): Induan (251 – 249.5 Mya) · Olenekian (249.5 – 245.9 Mya) Middle Triassic (245.9 – 228.7 Mya): Anisian (245.9 – 237 Mya) · Ladinian (237 – 228.7 Mya) Late Triassic (228.7 – 199.6 Mya): Carnian (228.7 – 216.5 Mya) · Norian (216.5 – 203.6 Mya) · Rhaetian (203.6 – 199.6 Mya) Jurassic (199.6 – 145.5 Mya) Early Jurassic (199.6 – 175.6 Mya): Hettangian (199.6 – 196.5 Mya) · Sinemurian (196.5 – 189.6 Mya) · Pliensbachian (189.6 – 183 Mya) · Toarcian (183 – 175.6 Mya) Middle Jurassic (175.6 – 161.2 Mya): Aalenian (175.6 – 171.6 Mya) · Bajocian (171.6 – 167.7 Mya) · Bathonian (167.7 – 164.7 Mya) · Callovian (164.7 – 161.2 Mya) Late Jurassic (161.2 – 145.5 Mya): Oxfordian (161.2 – 155.6 Mya) · Kimmeridgian (155.6 – 150.8 Mya) · Tithonian (150.8 – 145.5 Mya) Cretaceous (145.5 – 65.5 Mya) Early Cretaceous (145.5 – 99.6 Mya): Berriasian (145.5 – 140.2 Mya) · Valanginian (140.2 – 133.9 Mya) · Hauterivian (133.9 – 130 Mya) · Barremian (130 – 125 Mya) · Aptian (125 – 112 Mya) · Albian (112 – 99.6 Mya) Late Cretaceous (99.6 – 65.5 Mya): Cenomanian (99.6 – 93.6 Mya) · Turonian (93.6 – 88.6 Mya) · Coniacian (88.6 – 85.8 Mya) · Santonian (85.8 – 83.5 Mya) · Campanian (83.5 – 70.6 Mya) · Maastrichtian (70.6 – 65.5 Mya)  Cenozoic (65.5 – 0 Mya) Paleogene, Neogene and early Pleistocene comprise former Tertiary* (65.5 – 1.8 Mya) period. Gelasian and Calabrian comprise Early Pleistocene (2.588 Mya – 781 kya) subepoch. Paleogene (65.5 – 23.03 Mya) Paleocene (65.5 – 55.8 Mya): Danian (65.5 – 61.1 Mya) · Selandian (61.1 – 58.7 Mya) · Thanetian (58.7 – 55.8 Mya) Eocene (55.8 – 33.9 Mya): Ypresian (55.8 – 48.6 Mya) · Lutetian (48.6 – 40.4 Mya) · Bartonian (40.4 – 37.2 Mya) · Priabonian (37.2 – 33.9 Mya) Oligocene (33.9 – 23.03 Mya): Rupelian (33.9 – 28.4 Mya) · Chattian (28.4 – 23.03 Mya) Neogene (23.03 – 2.588 Mya) Miocene (23.03 – 5.332 Mya): Aquitanian (23.03 – 20.43 Mya) · Burdigalian (20.43 – 15.97 Mya) · Langhian (15.97 – 13.82 Mya) · Serravallian (13.82 – 11.608 Mya)  · Tortonian (11.608 – 7.246 Mya)  · Messinian (7.246 – 5.332 Mya) Pliocene (5.332 – 2.588 Mya): Piacenzian (5.332 – 3.6 Mya) · Zanclean (3.6 – 2.588 Mya) Quaternary (2.588 – 0 Mya) Pleistocene (2.588 Mya – 11.4 kya): Gelasian (2.588 – 1.806 Mya) · Calabrian (1.806 Mya – 781 kya) · Middle Pleistocene / Ionian (781 – 126 kya) · Late Pleistocene / Tarantian (126 – 11.4 kya): Oldest Dryas* (18 – 14.67 kya) · Bølling* (14.67 – 14 kya) · Older Dryas* (14 – 13.7 kya) · Allerød* (13.7 – 12.8 kya) · Younger Dryas* (12.8 – 11.4 kya) Holocene (11.4 – 0 kya): Preboreal* (11.4 – 9 kya) · Boreal* (9 – 8 kya) · Atlantic* (8 – 5 kya) · Subboreal* (5 – 2.5 kya) · Subatlantic* (2.5 – 0 kya) kya = thousands years ago. Mya = millions years ago. * Not officially recognized by the I.C.S. Source: International Stratigraphic Chart. International Commission on Stratigraphy. Retrieved 8 February 2008.