Ordovician: Difference between revisions
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{{Geological period |
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|from=488 |
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|to=443 |
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|image=MiddleOrdovicianGlobal.jpg |
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|o2=13.5 |
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|co2=4200 |
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|temp=16 |
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|timeline=off |
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|sea level = 180m; rising to 220m in Caradoc and falling sharply to 140m in end-Ordovician glaciations<ref>{{cite journal | author = Haq, B. U.| year = 2008| doi = 10.1126/science.1161648 | title = A Chronology of Paleozoic Sea-Level Changes | journal = Science | volume = 322 | pages = 64–68 }}</ref> |
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}} |
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The '''Ordovician''' is a [[geologic period|geologic period and system]], the second of six of the [[Paleozoic]] [[era (geology)|Era]], and covers the time between 488.3±1.7 to 443.7±1.5 million years ago {{ICS 2004}}. It follows the [[Cambrian]] Period and is followed by the [[Silurian]] Period. The Ordovician, named after the [[Wales|Welsh]] tribe of the [[Ordovices]], was defined by [[Charles Lapworth]] in 1879 to resolve a dispute between followers of FARTS [[Adam Sedgwick]] and [[Roderick Murchison]], who were placing the same [[Rock (geology)|rock]] beds in northern Wales into the [[Cambrian]] and [[Silurian]] periods respectively. Lapworth, recognizing that the [[fossil]] [[Fauna (animals)|fauna]] in the disputed [[Stratum|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. |
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While recognition of the distinct Ordovician Period was slow in the [[United Kingdom of Great Britain and Ireland|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]]. |
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==Dating== |
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The Ordovician Period started at a major extinction event called the [[Cambrian-Ordovician extinction events]] some time about 488.3 ± 1.7 [[annum|Ma]] (million years ago), and lasted for about 44.6 million years. It ended with the [[Ordovician–Silurian extinction event]], about 443.7 ± 1.5 Ma (ICS, 2004) that wiped out 60% of marine [[Genus|genera]]. |
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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 [[fossil]]s and in some regions, major [[petroleum]] and [[gas]] reservoirs. |
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<!--merged in from [[Tremadocian]]--> |
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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. |
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==Subdivisions{{anchor|Subdivisions}}== |
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{{include timeline}} |
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{{anchor|Tremadocian}} |
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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.<ref> Details on the Dapingian are available at {{cite doi|10.1111/j.1502-3931.2009.00169.x}}</ref> |
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The Ordovician Period in Britain was traditionally broken into Early ([[Tremadocian]] and [[Arenig]]), Middle ([[Llanvirn Series|Llanvirn]] [subdivided into Abereiddian and Llandeilian] and [[Llandeilo Series|Llandeilo]]) and Late ([[Caradoc Series|Caradoc]] and [[Ashgill Series|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 stage]]s (subdivisions of epochs) from youngest to oldest are: |
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* [[Hirnantian]]/Gamach (Late Ordovician: Ashgill) |
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* Rawtheyan/Richmond (Late Ordovician: Ashgill) |
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* Cautleyan/Richmond (Late Ordovician: Ashgill) |
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* Pusgillian/Maysville/Richmond (Late Ordovician: Ashgill) |
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* Trenton (Middle Ordovician: Caradoc) |
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* Onnian/Maysville/Eden (Middle Ordovician: Caradoc) |
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* Actonian/Eden (Middle Ordovician: Caradoc) |
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* Marshbrookian/Sherman (Middle Ordovician: Caradoc) |
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* Longvillian/Sherman (Middle Ordovician: Caradoc) |
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* Soundleyan/Kirkfield (Middle Ordovician: Caradoc) |
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* Harnagian/Rockland (Middle Ordovician: Caradoc) |
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* Costonian/Black River (Middle Ordovician: Caradoc) |
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* Chazy (Middle Ordovician: Llandeilo) |
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* Llandeilo (Middle Ordovician: Llandeilo) |
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* Whiterock (Middle Ordovician: Llanvirn) |
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* Llanvirn (Middle Ordovician: Llanvirn) |
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* Cassinian (Early Ordovician: Arenig) |
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* Arenig/Jefferson/Castleman (Early Ordovician: Arenig) |
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* Tremadoc/Deming/Gaconadian (Early Ordovician: Tremadoc) |
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==Paleogeography and atmosphere== |
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Sea levels were high during the Ordovician; in fact during the Tremadocian, [[Transgression (geology)|marine transgressions]] worldwide were the greatest for which evidence is preserved in the rocks. |
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During the Ordovician, the southern continents were collected into a single continent called [[Gondwana]]. Gondwana started the period in [[equator]]ial [[latitude]]s and, as the period progressed, drifted toward the [[South Pole]]. Early in the Ordovician, the continents [[Laurentia]] (present-day [[North America]]), [[Siberia (continent)|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. |
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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 arc|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 [[glacier|glaciated]]. |
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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.<ref name="Stanley and Hardie 1998">{{cite journal |last=Stanley |first=S. M. |authorlink= |coauthors=Hardie, L. A. |year=1998 |month= |title=Secular oscillations in the carbonate mineralogy of reef-building and sediment-producing organisms driven by tectonically forced shifts in seawater chemistry |journal=Palaeogeography, Palaeoclimatology, Palaeoecology |volume=144 |issue= |pages=3–19 |doi=10.1016/S0031-0182(98)00109-6 |url= |accessdate= |quote= }}</ref><ref name="Stanley and Hardie 1999">{{cite journal |last=Stanley |first=S. M. |authorlink= |coauthors=Hardie, L. A. |year=1999 |month= |title=Hypercalcification; paleontology links plate tectonics and geochemistry to sedimentology |journal=GSA Today |volume=9 |issue= |pages=1–7 |id= |url= |accessdate= |quote= }}</ref> |
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==Climate== |
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The Early Ordovician climate was thought to be quite warm, at least in the tropics. 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]]. |
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As the Ordovician progressed, we see evidence of [[glacier]]s 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]]. |
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==Life== |
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[[File:Orthoceras BW.jpg|thumb|Large [[Nautiloid]]s like [[Orthoceras]] were among the largest predatory animals in the Ordovician.]] |
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[[File:Nmnh fg09.jpg|thumb|A [[diorama]] depicting Ordovician flora and fauna.]] |
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For most of the Late Ordovician, life continued to flourish, but at and near the end of the period there were [[Ordovician-Silurian extinction events|mass-extinction events]] that seriously affected [[plankton]]ic forms like [[conodont]]s, [[graptolite]]s, and some groups of [[trilobite]]s ([[Agnostida]] and [[Ptychopariida]], which completely died out, and the [[Asaphida]] which were much reduced). [[Brachiopod]]s, [[bryozoa]]ns and [[echinoderm]]s were also heavily affected, and the [[endocerid]] [[cephalopod]]s 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. |
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===Fauna=== |
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Though less famous than the [[Cambrian explosion]], the Ordovician featured an [[adaptive radiation]], the [[Ordovician radiation]], that was no less remarkable; marine faunal [[genus|genera]] increased fourfold, resulting in 12% of all known [[Phanerozoic]] marine fauna.<ref name="Dixon2001">{{cite book |title=Atlas of Life on Earth |last=Dixon |first=Dougal |authorlink= |coauthors=''et al.'' |year=2001 |publisher=Barnes & Noble Books |location=New York |isbn=0760719578 |pages=87 }}</ref> The [[Trilobites|trilobite]], inarticulate [[Brachiopoda|brachiopod]], [[archaeocyathid]], and [[eocrinoid]] faunas of the Cambrian were succeeded by those which would dominate for the rest of the Paleozoic, such as articulate brachiopods, [[cephalopods]], and [[crinoid]]s; articulate brachiopods, in particular, largely replaced trilobites in [[continental shelf|shelf]] communities.<ref name="Cooper1986">{{cite book |title=A Trip Through Time: Principles of Historical Geology |last=Cooper |first=John D. |authorlink= |coauthors=Miller, Richard H.; Patterson, Jacqueline |year=1986 |publisher=Merrill Publishing Company |location=Columbus |isbn=0675201403 |pages=247, 255–259 }}</ref> Their success epitomizes the greatly increased diversity of [[calcium carbonate|carbonate]] shell-secreting organisms in the Ordovician compared to the Cambrian.<ref name="Cooper1986" /> |
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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. The first [[Bryozoa]] appeared in the early Ordovician as did the first [[coral reef]]s, although solitary [[coral]]s date back to at least the [[Cambrian]]. |
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[[Mollusc]]s, which had appeared during the Cambrian or even the [[Ediacaran]], became common and varied, especially [[bivalve]]s, [[gastropod]]s, and [[nautiloid]] cephalopods. |
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Now-extinct marine animals called [[graptolite]]s thrived in the oceans. Some new cystoids and [[crinoid]]s appeared. |
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It was long thought that the first true [[vertebrata|vertebrates]] (fish — [[Ostracoderm]]s) 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. |
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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.<ref name="WilsonPalmer2006">{{cite journal |last=Wilson |first=M. A. |authorlink= |coauthors=Palmer, T. J. |year=2006 |month= |title=Patterns and processes in the Ordovician Bioerosion Revolution |journal=Ichnos |volume=13 |issue= |pages=109–112 |doi=10.1080/10420940600850505 |url=http://www3.wooster.edu/geology/WilsonPalmer06.pdf |format=PDF|accessdate= |quote= }}</ref> It is marked by a sudden abundance of hard substrate trace fossils such as ''[[Trypanites]]'', ''Palaeosabella'' and ''[[Petroxestes]]''. |
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In the Early Ordovician, [[trilobite]]s were joined by many new types of organisms, including [[Tabulata|tabulate]] corals, [[Strophomenida|strophomenid]], [[Rhynchonellida|rhynchonellid]], and many new [[Orthida|orthid]] [[brachiopod]]s, [[bryozoa]]ns, [[plankton]]ic [[graptolite]]s and [[conodont]]s, and many types of [[mollusc]]s and [[echinoderm]]s, including the ophiuroids ("brittle stars") and the first [[sea star]]s. 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]]. |
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In the Middle Ordovician, the [[trilobite]]-dominated Early Ordovician communities were replaced by generally more mixed ecosystems, in which [[brachiopod]]s, [[bryozoa]]ns, [[mollusc]]s and [[echinoderm]]s all flourished, [[Tabulata|tabulate corals]] diversified and the first [[Rugosa|rugose corals]] appeared; trilobites were no longer predominant. The [[plankton]]ic [[graptolite]]s 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]] which appear in abundance at this time. One of the earliest known armoured [[agnatha]]n ("[[ostracoderm]]") vertebrate, ''[[Arandaspis]]'', dates from the Middle Ordovician. |
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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 [[shark]]s and [[nautiloid]]s 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.<ref name="Palaeos.com">{{cite web |url=http://www.palaeos.com/Paleozoic/Ordovician/Ordovician.htm#Life |title=Palaeos Paleozoic : Ordovician : The Ordovician Period |accessdate= |work= |date=April 11, 2002 }}</ref> Some trilobites such as ''Asaphus kowalewski'' evolved long eyestalks to assist in detecting predators whereas other trilobite eyes in contrast disappeared completely.<ref>[http://www.trilobites.info/ A Guide to the Orders of Trilobites<!-- Bot generated title -->]</ref> |
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<gallery> |
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Image:OrdovicianEdrio.jpg|The Upper Ordovician [[edrioasteroid]] ''Cystaster stellatus'' on a cobble from the Kope Formation in northern Kentucky. In the background is the cyclostome [[bryozoan]] ''Corynotrypa''. |
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Image:FossilMtnUT.jpg|Fossil Mountain, west-central Utah; Middle Ordovician fossiliferous shales and limestones in the lower half. |
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Image:OrdoutcropIN.jpg|Outcrop of Upper Ordovician rubbly limestone and shale, southern Indiana; [[College of Wooster]] students. |
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Image:OrdOutcropTN.JPG|Outcrop of Upper Ordovician limestone and minor shale, central Tennessee; [[College of Wooster]] students. |
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Image:LibertyBorings.jpg|''[[Trypanites]]'' borings in an Ordovician [[hardground]], southeastern Indiana.<ref name="WilsonPalmer2001">{{cite journal |last=Wilson |first=M. A. |authorlink= |coauthors=Palmer, T. J. |year=2001 |month= |title=Domiciles, not predatory borings: a simpler explanation of the holes in Ordovician shells analyzed by Kaplan and Baumiller, 2000 |journal=Palaios |volume=16 |issue= |pages=524–525 |doi=10.1669/0883-1351(2001)016<0524:DNPBAS>2.0.CO;2|url= |accessdate= }}</ref> |
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Image:Petroxestes_borings_Ordovician.jpg|''[[Petroxestes]]'' borings in an Ordovician [[hardground]], southern Ohio.<ref name="WilsonPalmer2006">{{cite journal |last=Wilson |first=M. A. |authorlink= |coauthors=Palmer, T. J. |year=2006 |month= |title=Patterns and processes in the Ordovician Bioerosion Revolution |journal=Ichnos |volume=13 |issue= |pages=109–112 |doi=10.1080/10420940600850505 |url=http://www3.wooster.edu/geology/WilsonPalmer06.pdf |accessdate= |quote= }}</ref> |
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File:OilShaleEstonia.jpg|Outcrop of Ordovician [[kukersite]] [[oil shale]], northern [[Estonia]]. |
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Image:OilShaleFossilsEstonia.jpg|Bryozoan fossils in Ordovician kukersite oil shale, northern [[Estonia]]. |
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Image:OrdFossilsMN.JPG|[[Brachiopods]] and [[bryozoans]] in an Ordovician limestone, southern Minnesota. |
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Image:PlatystrophiaOrdovician.jpg|''[[Platystrophia]] ponderosa'', Maysvillian (Upper Ordovician) near Madison, Indiana. Scale bar is 5.0 mm. |
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Image:Echinosphaerites.JPG|The Ordovician cystoid ''[[Echinosphaerites]]'' (an extinct [[echinoderm]]) from northeastern Estonia; approximately 5 cm in diameter. |
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Image:Prasopora.JPG|''Prasopora'', a trepostome [[bryozoan]] from the Ordovician of Iowa. |
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Image:EncrustedStroph.JPG|An Ordovician strophomenid brachiopod with encrusting inarticulate brachiopods and a bryozoan. |
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Image:Protaraea.jpg|The heliolitid coral ''Protaraea richmondensis'' encrusting a gastropod; Cincinnatian (Upper Ordovician) of southeastern Indiana. |
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Image:ZygospiraAttached.jpg|''Zygospira modesta'', spiriferid brachiopods, preserved in their original positions on a trepostome bryozoan; Cincinnatian (Upper Ordovician) of southeastern Indiana. |
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Image:DiplograptusCaneySprings.jpg|Graptolites (''Amplexograptus'') from the Ordovician near Caney Springs, Tennessee. |
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</gallery> |
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===Flora=== |
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Marine fungi were abundant in the Ordovician seas to [[decompose]] [[animal]] [[Carrion|carcasses]], and other wastes.{{Verify source|date=August 2007}} |
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[[Green algae]] were common in the Late [[Cambrian]] (perhaps earlier) and in the Ordovician. |
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Plants probably evolved from green algae. Terrestrial plants probably evolved from green algae, first appearing in the form of tiny non-vascular mosses resembling [[Marchantiophyta|liverwort]]s. Fossil spores from land plants have been identified in uppermost Ordovician sediments. |
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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 [[bryophyte]]s.<ref>{{cite journal |last=Redecker |first=D. |authorlink= |coauthors=Kodner, R. ; Graham, L. E. |year=2000 |month= |title=Glomalean fungi from the Ordovician |journal=[[Science (journal)|Science]] |volume=289 |issue=5486 |pages=1920–1921 |doi=10.1126/science.289.5486.1920 |url= |accessdate= |quote=| pmid=10988069 }}</ref> |
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==End of the period == |
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{{main|Ordovician-Silurian extinction events}} |
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The Ordovician came to a close in a series of [[extinction event]]s that, taken together, comprise the second largest of the five major extinction events in [[History of Earth|Earth's history]] in terms of percentage of [[genus|genera]] that went extinct. The only larger one was the [[Permian-Triassic extinction event]]. |
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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. |
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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. |
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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.<ref name="Stanley1999">{{cite book |title=Earth System History |last=Stanley |first=Steven M. |authorlink= |coauthors= |year=1999 |publisher=W.H. Freeman and Company |location=New York |isbn=0716728826 |pages=358, 360 }}</ref> Other researchers (Page et al.) estimate more temperate conditions did not return until the late Silurian. |
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The late Ordovician glaciation event was preceded by a fall in atmospheric carbon dioxide (from 7000 ppm to 4400 ppm) 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. |
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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.<ref>Emiliani (1992), 491</ref> Species limited to a single epicontinental sea on a given landmass were severely affected.<ref name="Stanley1999" /> Tropical lifeforms were hit particularly hard in the first wave of extinction, while cool-water species were hit worst in the second pulse.<ref name="Stanley1999" /> |
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Surviving species were those that coped with the changed conditions and filled the ecological niches left by the extinctions. |
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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. |
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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]],<ref name="Melott2006">{{cite journal |last=Melott |first=Adrian |authorlink= |coauthors=''et al.'' |year=2004 |month= |title=Did a gamma-ray burst initiate the late Ordovician mass extinction? |journal=International Journal of Astrobiology |volume=3 |issue= |pages=55–61 |doi=10.1017/S1473550404001910 |url= |accessdate= |quote= }}</ref> but most scientists agree that extinction events are complex with multiple causes. |
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==References== |
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{{Reflist|2}} |
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== External links == |
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{{Commonscat|Ordovician}} |
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*{{cite web |url=http://www.stratigraphy.org/gssp.htm |title=Overview of Global Boundary Stratotype Sections and Points (GSSP's) |accessdate=2006-04-30 |last=Ogg |first=Jim |coauthors= |month=June | year=2004 |work= |publisher=}} |
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*{{cite web |url=http://www.anr.state.vt.us/dec/geo/chazytxt.htm |title=Chazy Reef at Isle La Motte |accessdate= |last=Mehrtens |first=Charlotte |coauthors= |date= |work= |publisher=}} An Ordovician reef in Vermont. |
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*[http://www.geo-lieven.com/erdzeitalter/ordovizium/ordovizium.htm Examples of Ordovician Fossils] |
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*[http://members.wri.com/jeffb/Fossils Ordovician fossils of the famous Cincinnatian Group] |
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*[http://www.drydredgers.org The Dry Dredgers, an active group of amateur paleontologists in the Cincinnati area] |
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{{Phanerozoic eon}} |
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[[Category:Ordovician| ]] |
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[[ar:عصر أوردوفيسي]] |
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[[br:Ordovisian]] |
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[[ca:Ordovicià]] |
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[[cs:Ordovik]] |
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[[cy:Ordofigaidd]] |
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[[da:Ordovicium]] |
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[[de:Ordovizium]] |
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[[et:Ordoviitsium]] |
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[[es:Ordovícico]] |
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[[eo:Ordovicio]] |
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[[eu:Ordoviziar]] |
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[[fr:Ordovicien]] |
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[[ko:오르도비스기]] |
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[[hr:Ordovicij]] |
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[[id:Ordovisium]] |
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[[is:Ordóvisíumtímabilið]] |
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[[it:Ordoviciano]] |
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[[he:אורדוביק]] |
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[[ka:ორდოვიციული სისტემა]] |
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[[kk:Ордовик кезеңі]] |
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[[la:Aevum Ordovicicum]] |
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[[lb:Ordovizium]] |
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[[lt:Ordovikas]] |
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[[ja:オルドビス紀]] |
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[[pl:Ordowik]] |
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[[pt:Ordoviciano]] |
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[[ro:Ordovician]] |
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[[ru:Ордовикский период]] |
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[[simple:Ordovician]] |
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[[sk:Ordovik]] |
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[[sl:Ordovicij]] |
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[[sr:Ордовицијум]] |
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[[sh:Ordovicij]] |
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[[fi:Ordovikikausi]] |
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[[sv:Ordovicium]] |
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[[ta:ஓர்டோவிசியக் காலம்]] |
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[[tr:Ordovisyen]] |
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[[uk:Ордовицький період]] |
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[[vi:Kỷ Ordovic]] |
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[[vo:Lordovig]] |
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[[zh:奥陶纪]] |
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Revision as of 20:02, 12 March 2010
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