For other uses, see Cambrian (disambiguation).
Cambrian Period
541–485.4 million years ago
PreЄ
Є
O
S
D
C
P
T
J
K
Pg
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| Mean atmospheric O2 content over period duration |
ca. 12.5 Vol %[1]
(63 % of modern level) |
| Mean atmospheric CO2 content over period duration |
ca. 4500 ppm[2]
(16 times pre-industrial level) |
| Mean surface temperature over period duration |
ca. 21 °C[3]
(7 °C above modern level) |
| Sea level (above present day) |
Rising steadily from 30m to 90m[4] |
Key events in the Cambrian
view • discuss • edit
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-540 —
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-530 —
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-520 —
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-510 —
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-500 —
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-490 —
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←
Archaeocyatha extinction
←
SSF diversification, first brachiopods & archaeocyatha
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First halkieriids, mollusсs, hyoliths SSF
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Treptichnus pedum trace
Large negative peak δ 13Ccarb excursion
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First Cloudina & Namacalathus mineral tubular fossils
Stratigraphic scale of the ICS subdivisions and Precambrian/Cambrian boundary.
The Cambrian is the first geological period of the Paleozoic Era, lasting from 541.0 ± 1.0 to 485.4 ± 1.9 million years ago (mya) and is succeeded by the Ordovician.[5] Its subdivisions, and indeed its base, are somewhat in flux. The period was established by Adam Sedgwick, who named it after Cambria, the Latin name for Wales, where Britain's Cambrian rocks are best exposed.[6] The Cambrian is unique in its unusually high proportion of lagerstätten. These are sites of exceptional preservation, where 'soft' parts of organisms are preserved as well as their more resistant shells. This means that our understanding of the Cambrian biology surpasses that of some later periods.[7]
The Cambrian Period marked a profound change in life on Earth; prior to the Cambrian, living organisms on the whole were small, unicellular and simple. Complex, multicellular organisms gradually became more common in the millions of years immediately preceding the Cambrian, but it was not until this period that mineralized – hence readily fossilized – organisms became common.[8] The rapid diversification of lifeforms in the Cambrian, known as the Cambrian explosion, produced the first representatives of many modern phyla, representing the evolutionary stems of modern groups of species, such as the molluscs and arthropods.[citation needed] While diverse life forms prospered in the oceans, the land was comparatively barren – with nothing more complex than a microbial soil crust[9] and a few molluscs that emerged to browse on the microbial biofilm[10] Most of the continents were probably dry and rocky due to a lack of vegetation. Shallow seas flanked the margins of several continents created during the breakup of the supercontinent Pannotia. The seas were relatively warm, and polar ice was absent for much of the period.
The United States Federal Geographic Data Committee uses a "barred capital C" character similar to the capital letter Ukrainian Ye ‹Є› to represent the Cambrian Period.[11] The proper[12] Unicode character is U+A792 Ꞓ latin capital letter c with bar.[13]
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Contents
- 1 Stratigraphy
- 1.1 Subdivisions
- 1.2 Cambrian dating
- 2 Paleogeography
- 3 Climate
- 4 Flora
- 5 Fauna
- 6 See also
- 7 References
- 8 Further reading
- 9 External links
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Stratigraphy [edit]
Further information: Stratigraphy of the Cambrian
For an up-to-date stratigraphy of the Cambrian, see "The Cambrian Period". 2012.
Despite the long recognition of its distinction from younger Ordovician rocks and older Precambrian rocks, it was not until 1994 that this time period was internationally ratified. The base of the Cambrian is defined on a complex assemblage of trace fossils known as the Treptichnus pedum assemblage.[14] Nevertheless, the usage of Treptichnus pedum, a reference ichnofossil for the lower boundary of the Cambrian, for the stratigraphic detection of this boundary is always risky because of occurrence of very similar trace fossils belonging to the Treptichnids group well below the T. pedum in Namibia, Spain and Newfoundland, and possibly, in the western USA. The stratigraphic range of T. pedum overlaps the range of the Ediacaran fossils in Namibia, and probably in Spain.[15][16]
Subdivisions [edit]
The Cambrian period follows the Ediacaran and is followed by the Ordovician period. The Cambrian is divided into four epochs or series and ten ages or stages. Currently only two series and five stages are named and have a GSSP.
Because the international stratigraphic subdivision is not yet complete, many local subdivisions are still widely used. In some of these subdivisions the Cambrian is divided into three epochs with locally differing names – the Early Cambrian (Caerfai or Waucoban, 541 ± 0.3 to 509 ± 1.7 mya), Middle Cambrian (St Davids or Albertan, 509 ± 0.3 to 497 ± 1.7 mya) and Furongian (497 ± 0.3 to 485.4 ± 1.7 mya; also known as Late Cambrian, Merioneth or Croixan). Rocks of these epochs are referred to as belonging to the Lower, Middle, or Upper Cambrian.
Trilobite zones allow biostratigraphic correlation in the Cambrian.
Each of the local epochs is divided into several stages. The Cambrian is divided into several regional faunal stages of which the Russian-Kazakhian system is most used in international parlance:
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Chinese |
North American |
Russian-Kazakhian |
Australian |
Regional |
C
A
M
B
R
I
A
N |
Furongian |
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Ibexian (part) |
Ayusokkanian |
Datsonian |
Dolgellian (Trempealeauan, Fengshanian) |
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Payntonian |
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Sunwaptan |
Sakian |
Iverian |
Ffestiniogian (Franconian, Changshanian) |
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Steptoan |
Aksayan |
Idamean |
Maentwrogian |
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Marjuman |
Batyrbayan |
Mindyallan |
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| Cambrian Series 3 |
Maozhangian |
Mayan |
Boomerangian |
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| Zuzhuangian |
Delamaran |
Amgan |
Undillian |
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| Zhungxian |
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Florian |
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Templetonian |
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Dyeran |
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Ordian |
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| Cambrian Series 2 |
Longwangmioan |
Toyonian |
Lenian |
| Changlangpuan |
Montezuman |
Botomian |
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| Qungzusian |
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Atdabanian |
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| Terreneuvian |
Meishuchuan
Jinningian |
Placentian |
Tommotian
Nemakit-Daldynian* |
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Cordubian |
| PRECAMBRIAN |
Sinian |
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Nemakit-Daldynian*
Sakharan |
Adeladean |
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*In Russian tradition the lower boundary of the Cambrian is suggested to be defined at the base of the Tommotian Stage which is characterized by diversification and global distribution of organisms with mineral skeletons and the appearance of the first Archaeocyath bioherms.[17][18][19]
Cambrian dating [edit]
Archeocyathids from the Poleta formation in the Death Valley area
The time range for the Cambrian has classically been thought to have been from about 542 mya to about 488 mya. The lower boundary of the Cambrian was traditionally set at the earliest appearance of trilobites and also unusual forms known as archeocyathids (literally "ancient cup") that are thought to be the earliest sponges and also the first non-microbial reef builders.
The end of the period was eventually set at a fairly definite faunal change now identified as an extinction event. Fossil discoveries and radiometric dating in the last quarter of the 20th century have called these dates into question. Date inconsistencies as large as 20 million years are common between authors. Framing dates of ca. 545 to 490 mya were proposed by the International Subcommission on Global Stratigraphy as recently as 2002.
A radiometric date from New Brunswick puts the end of the Lower Cambrian around 511 mya. This leaves 21 mya for the other two series/epochs of the Cambrian.
A more precise date of 542 ± 0.3 mya for the extinction event at the beginning of the Cambrian has recently been submitted.[20] The rationale for this precise dating is interesting in itself as an example of paleological deductive reasoning. Exactly at the Cambrian boundary there is a marked fall in the abundance of carbon-13, a "reverse spike" that paleontologists call an excursion. It is so widespread that it is the best indicator of the position of the Precambrian-Cambrian boundary in stratigraphic sequences of roughly this age. One of the places that this well-established carbon-13 excursion occurs is in Oman. Amthor (2003) describes evidence from Oman that indicates the carbon-isotope excursion relates to a mass extinction: the disappearance of distinctive fossils from the Precambrian coincides exactly with the carbon-13 anomaly. Fortunately, in the Oman sequence, so too does a volcanic ash horizon from which zircons provide a very precise age of 542 ± 0.3 mya (calculated on the decay rate of uranium to lead). This new and precise date tallies with the less precise dates for the carbon-13 anomaly, derived from sequences in Siberia and Namibia.
Paleogeography [edit]
Plate reconstructions suggest a global supercontinent, Pannotia, was in the process of breaking up early in the period,[21][22] with Laurentia (North America), Baltica, and Siberia having separated from the main supercontinent of Gondwana to form isolated land masses.[23] Most continental land was clustered in the Southern Hemisphere at this time, but was gradually drifting north.[23] Large, high-velocity rotational movement of Gondwana appears to have occurred in the Early Cambrian.[24]
With a lack of sea ice – the great glaciers of the Marinoan Snowball Earth were long melted[25] – the sea level was high, which led to large areas of the continents being flooded in warm, shallow seas ideal for thriving life. The sea levels fluctuated somewhat, suggesting there were 'ice ages', associated with pulses of expansion and contraction of a south polar ice cap.[26]
Climate [edit]
The Earth was generally cold during the early Cambrian, probably due to the ancient continent of Gondwana covering the South Pole and cutting off polar ocean currents. There were likely polar ice caps and a series of glaciations, as the planet was still recovering from an earlier Snowball Earth. It became warmer towards the end of the period; the glaciers receded and eventually disappeared, and sea levels rose dramatically. This trend would continue into the Ordovician period.
Flora [edit]
A reconstruction of
Margaretia dorus from the Burgess Shale, which are believed to be green algae
Although there were a variety of macroscopic marine plants (e.g. Margaretia and Dalyia), no true land plant (embryophyte) fossils are known from the Cambrian. However, biofilms and microbial mats were well developed on Cambrian tidal flats and beaches.,[27] and further inland were a variety of lichens[citation needed], fungi and microbes forming microbial earth ecosystems, comparable with modern soil crust of desert regions, contributing to soil formation.[28]
Fauna [edit]
Main article: Cambrian explosion
Most animal life during the Cambrian was aquatic, with trilobites as the dominant life form.[29] The period marked a steep change in the diversity and composition of Earth's biosphere. The incumbent Ediacaran biota suffered a mass extinction at the base of the period, which corresponds to an increase in the abundance and complexity of burrowing behaviour. This behaviour had a profound and irreversible effect on the substrate which transformed the seabed ecosystems. Before the Cambrian, the sea floor was covered by microbial mats. By the end of the period, burrowing animals had destroyed the mats through bioturbation, and gradually turned the seabeds into what they are today. As a consequence, many of those organisms who were dependent on the mats went extinct, while the other species adapted to the changed environment who now offered new ecological niches.[30] Around the same time there was a seemingly rapid appearance of representatives of all the mineralized phyla.[31] However, many of these phyla were represented only by stem-group forms; and since mineralized phyla generally have a benthic origin, they may not be a good proxy for (more abundant) non-mineralized phyla.[32]
While the early Cambrian showed such diversification that it has been named the Cambrian Explosion, this changed later in the period, when it was exposed to a sharp drop in biodiversity. About 515 million years ago, the number of species going extinct exceeded the amount of new species appearing. Five million years later, the number of genera had dropped from an earlier peak of about 600 to just 450. Also the speciation rate in many groups was reduced to between a fifth and a third of previous levels. The later half of Cambrian was surprisingly barren; the stromatolites which had been replaced by reef building sponges known as Archaeocyatha, returned once more as the archaeocyathids went extinct. This declining trend did not change before Ordovician.[33]
Some Cambrian organisms ventured onto land, producing the trace fossils Protichnites and Climactichnites. Fossil evidence suggests that euthycarcinoids, an extinct group of arthropods, produced at least some of the Protichnites.[34][35] Fossils of the maker of Climactichnites have not been found; however, fossil trackways and resting traces suggest a large, slug-like mollusk.[36][37]
In contrast to later periods, the Cambrian fauna was somewhat restricted; free-floating organisms were rare, with the majority living on or close to the sea floor;[38] and mineralizing animals were rarer than in future periods, in part due to the unfavourable ocean chemistry.[38]
Many modes of preservation are unique to the Cambrian, resulting in an abundance of Lagerstätten.
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Trilobites were very common during this time
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Anomalocaris was an early marine predator, among the various arthropods of the time.
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Pikaia was an early chordate from the Middle Cambrian
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Opabinia was a creature with an unusual body plan; it was probably related to arthropods
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Protichnites were the trackways of arthropods that walked Cambrian beaches.
See also [edit]
| Part of a series on |
| The Cambrian explosion |
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Fossil localities
- Burgess Shale
- Chengjiang
- Sirius Passet
- Doushantuo
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Key organisms
- Ediacara biota
- Kimberella
- Vernanimalcula
- Burgess-type
- Marrella
- Anomalocaridids
- Halwaxiids
- Opabinia
- Odontogriphus
- Small shelly fauna
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Evolutionary concepts
- Trends
- Cambrian substrate revolution
- Themes
- Cladistics
- Convergent evolution
- Stem and crown groups
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- Cambro-Ordovician extinction event – circa 488 mya
- Dresbachian extinction event—circa 502 mya
- End Botomian extinction event—circa 517 mya
- List of fossil sites (with link directory)
- Type locality (geology), the locality where a particular rock type, stratigraphic unit, fossil or mineral species is first identified
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Modes of preservation in the Cambrian
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| Exceptional |
- Orsten
- Doushantuo type
- Bitter Springs type
- Burgess Shale type
- Beecher's Trilobite Bed type
- Ediacaran type
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| Conventional |
- Small shelly fossils
- Acritarchs
- Trace fossils
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References [edit]
- ^ 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): 64–8. Bibcode:2008Sci...322...64H. doi:10.1126/science.1161648. PMID 18832639.
- ^ "Stratigraphic Chart 2012". International Stratigraphic Commission. Retrieved 9 November 2012.
- ^ Sedgwick, A. (1852). "On the classification and nomenclature of the Lower Paleozoic rocks of England and Wales". Q. J. Geol. Soc. Land. 8: 136–138. doi:10.1144/GSL.JGS.1852.008.01-02.20.
- ^ Orr, P. J.; Benton, M. J.; Briggs, D. E. G. (2003). "Post-Cambrian closure of the deep-water slope-basin taphonomic window". Geology 31 (9): 769–772. Bibcode:2003Geo....31..769O. doi:10.1130/G19193.1. Retrieved 2008-06-28.
- ^ Butterfield, N. J. (2007). "Macroevolution and macroecology through deep time". Palaeontology 50 (1): 41–55. doi:10.1111/j.1475-4983.2006.00613.x. }
- ^ Schieber, 2007, pp. 53–71.
- ^ Seilacher, A. and Hagadorn, J.W. (2010) Early Molluscan evolution: evidence from the trace fossil record. Palaios, 25, 565-575
- ^ Federal Geographic Data Committee, ed. (August 2006). FGDC Digital Cartographic Standard for Geologic Map Symbolization FGDC-STD-013-2006 (PDF). U.S. Geological Survey for the Federal Geographic Data Committee. p. A–32–1. Retrieved 23 August 2010.
- ^ Priest, Lorna A.; Iancu, Laurentiu; Everson, Michael (October 2010). "Proposal to Encode C WITH BAR" (PDF). Retrieved 6 April 2011.
- ^ "Proposed New Characters: Pipeline Table". Unicode Consortium Web Site. Unicode, Inc. Retrieved 6 April 2011.
- ^ A. Knoll, M. Walter, G. Narbonne, and N. Christie-Blick (2004) "The Ediacaran Period: A New Addition to the Geologic Time Scale." Submitted on Behalf of the Terminal Proterozoic Subcommission of the International Commission on Stratigraphy.
- ^ M.A. Fedonkin, B.S. Sokolov, M.A. Semikhatov, N.M.Chumakov (2007). "Vendian versus Ediacaran: priorities, contents, prospectives." In: edited by M. A. Semikhatov "The Rise and Fall of the Vendian (Ediacaran) Biota. Origin of the Modern Biosphere. Transactions of the International Conference on the IGCP Project 493, August 20–31, 2007, Moscow." Moscow: GEOS.
- ^ A. Ragozina, D. Dorjnamjaa, A. Krayushkin, E. Serezhnikova (2008). "Treptichnus pedum and the Vendian-Cambrian boundary". 33 Intern. Geol. Congr. 6–14 August 2008, Oslo, Norway. Abstracts. Section HPF 07 Rise and fall of the Ediacaran (Vendian) biota. P. 183.
- ^ A.Yu. Rozanov, V.V. Khomentovsky, Yu.Ya. Shabanov, G.A. Karlova, A.I. Varlamov, V.A. Luchinina, T.V. Pegel’, Yu.E. Demidenko, P.Yu. Parkhaev, I.V. Korovnikov, N.A. Skorlotova (2008). "To the problem of stage subdivision of the Lower Cambrian". Stratigraphy and Geological Correlation 16 (1): 1–19. Bibcode:2008SGC....16....1R. doi:10.1007/s11506-008-1001-3.
- ^ B. S. Sokolov, M. A. Fedonkin (1984). "The Vendian as the Terminal System of the Precambrian". Episodes 7 (1): 12–19.
- ^ V. V. Khomentovskii and G. A. Karlova (2005). "The Tommotian Stage Base as the Cambrian Lower Boundary in Siberia". Stratigraphy and Geological Correlation 13 (1): 21–34.
- ^ Gradstein, F.M.; Ogg, J.G., Smith, A.G., others (2004). A Geologic Time Scale 2004. Cambridge University Press.
- ^ Powell, C.M.; Dalziel, I.W.D.; Li, Z.X.; McElhinny, M.W. (1995). "Did Pannotia, the latest Neoproterozoic southern supercontinent, really exist". EOS (Transactions, American Geophysical Union) 76: 46–72.
- ^ Scotese, C.R. (1998). "... supercontinents: The assembly of Rodinia, its break-up, and the formation of Pannotia during the Pan...". Journal of African Earth Sciences 27 (1): 171.
- ^ a b Mckerrow, W. S.; Scotese, C. R.; Brasier, M. D. (1992). "Early Cambrian continental reconstructions". Journal of the Geological Society 149 (4): 599–593. doi:10.1144/gsjgs.149.4.0599.
- ^ Mitchell, R. N.; Evans, D. A. D.; Kilian, T. M. (2010). "Rapid Early Cambrian rotation of Gondwana". Geology 38 (8): 755. doi:10.1130/G30910.1.
- ^ Smith, A.G. (in press (2008)). "Neoproterozoic time scales and stratigraphy". Geol. Soc. (Special publication).
- ^ Brett, C. E.; Allison, P. A.; Desantis, M. K.; Liddell, W. D.; Kramer, A. (2009). "Sequence stratigraphy, cyclic facies, and lagerstätten in the Middle Cambrian Wheeler and Marjum Formations, Great Basin, Utah". Palaeogeography Palaeoclimatology Palaeoecology 277: 9–33. doi:10.1016/j.palaeo.2009.02.010.
- ^ Schieber et al., 2007, pp. 53–71.
- ^ Retallack, G.J., 2008, Cambrian palaeosols and landscapes of South Australia. Alcheringa, v.55, p.1083–1106
- ^ Cambrian HSU NHM
- ^ As the worms churn
- ^ Landing, E.; English, A.; Keppie, J. D. (2010). "Cambrian origin of all skeletalized metazoan phyla--Discovery of Earth's oldest bryozoans (Upper Cambrian, southern Mexico)". Geology 38 (6): 547. doi:10.1130/G30870.1.
- ^ Budd, G. E.; Jensen, S. (2000). "A critical reappraisal of the fossil record of the bilaterian phyla". Biological Reviews of the Cambridge Philosophical Society 75 (2): 253–95. doi:10.1111/j.1469-185X.1999.tb00046.x. PMID 10881389.
- ^ The Ordovician: Life's second big bang
- ^ Collette & Hagadorn, 2010.
- ^ Collette, Gass & Hagadorn, 2012
- ^ Yochelson & Fedonkin, 1993.
- ^ Getty & Hagadorn, 2008.
- ^ a b 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 (3–4): 389–413. doi:10.1016/j.palaeo.2010.08.001.
Further reading [edit]
- Amthor, J. E.; Grotzinger, John P.; Schröder, Stefan; Bowring, Samuel A.; Ramezani, Jahandar; Martin, Mark W.; Matter, Albert (2003). "Extinction of Cloudina and Namacalathus at the Precambrian-Cambrian boundary in Oman". Geology 31 (5): 431–434. Bibcode:2003Geo....31..431A. doi:10.1130/0091-7613(2003)031<0431:EOCANA>2.0.CO;2.
- Collette, J. H., Gass, K. C. & Hagadorn, J. W. (2012). "Protichnites eremita unshelled? Experimental model-based neoichnology and new evidence for a euthycarcinoid affinity for this ichnospecies". Journal of Paleontology 86 (3): 442–454. doi:10.1666/11-056.1.
- Collette, J. H. & Hagadorn, J. W. (2010). "Three-dimensionally preserved arthropods from Cambrian Lagerstatten of Quebec and Wisconsin". Journal of Paleontology 84 (4): 646–667. doi:10.1666/09-075.1.
- Getty, P. R. & Hagadorn, J. W. (2008). "Reinterpretation of Climactichnites Logan 1860 to include subsurface burrows, and erection of Musculopodus for resting traces of the trailmaker". Journal of Paleontology 82 (6): 1161–1172. doi:10.1666/08-004.1.
- Gould, S. J.; Wonderful Life: the Burgess Shale and the Nature of Life (New York: Norton, 1989)
- Ogg, J.; June 2004, Overview of Global Boundary Stratotype Sections and Points (GSSPs) http://www.stratigraphy.org/gssp.htm Accessed 30 April 2006.
- Owen, R. (1852). "Description of the impressions and footprints of the Protichnites from the Potsdam sandstone of Canada". Geological Society of London Quarterly Journal 8: 214–225. doi:10.1144/GSL.JGS.1852.008.01-02.26.
- Schieber, J.; Bose, P. K.; Eriksson, P. G.; Banerjee, S.; Sarkar, S.; Altermann, W.; Catuneau, O. (2007). Atlas of Microbial Mat Features Preserved within the Clastic Rock Record. Elsevier. pp. 53–71.
- Yochelson, E. L. and M. A. Fedonkin (1993). "Paleobiology of Climactichnites, and Enigmatic Late Cambrian Fossil" (Free full text). Smithsonian Contributions to Paleobiology 74: 1–74.
External links [edit]
- Cambrian period on In Our Time at the BBC. (listen now)
- Biostratigraphy – includes information on Cambrian trilobite biostratigraphy
- Dr. Sam Gon's trilobite pages (contains numerous Cambrian trilobites)
- Examples of Cambrian Fossils
- Paleomap Project
- Report on the web on Amthor and others from Geology vol. 31
- Weird Life on the Mats
| 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 |
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Geologic history of Earth
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Precambrian supereon (4.57 Gya – 541 Mya)
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In left column are eons; right column: bold are eras; not bold are periods:
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Hadean
(4.57 – 4 Gya) |
Paleohadean (4.5 - 4.3 Gya)
Mesohadean (4.3 - 4.1 Gya)
Neohadean (4.1 - 4 Gya)
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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)
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Proterozoic
(2.5 Gya – 541 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 – 541 Mya): Tonian (1 Gya – 850 Mya) · Cryogenian (850 – 635 Mya) · Ediacaran (635 – 541 Mya)
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Mya = millions years ago. Gya = billions years ago.
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Phanerozoic eon (541.0 – 0 Mya)
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In horizontal bars are eras; in left column are periods; right column: bold are epochs; not bold not italic are ages; italic are chrons:
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Paleozoic (541.0 – 252.2 Mya)
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Cambrian
(541.0 – 485.4 Mya)
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Terreneuvian (541.0 – 521 Mya): Fortunian (541.0 – 529 Mya) · Age 2* (529 – 521 Mya)
Epoch 2* (521 – 509 Mya): Age 3* (521 – 514 Mya) · Age 4* (514 – 509 Mya)
Epoch 3* (509 – 497 Mya): Age 5* (509 – 504.5 Mya) · Drumian (504.5 – 500.5 Mya) · Guzhangian (500.5 – 497 Mya)
Furongian (497 – 485.4 Mya): Paibian (497 – 494 Mya) · Jiangshanian (494 – 489.5 Mya) · Age 10* (489.5 – 485.4 Mya)
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Ordovician
(485.4 – 443.4 Mya)
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Lower Ordovician (485.4 – 470.0 Mya): Tremadocian (485.4 – 477.7 Mya) · Floian (477.7 – 470.0 Mya)
Middle Ordovician (470.0 – 458.4 Mya): Dapingian (470.0 – 467.3 Mya) · Darriwilian (467.3 – 458.4 Mya)
Upper Ordovician (458.4 – 443.4 Mya): Sandbian (458.4 – 453.0 Mya) · Katian (453.0 – 445.2 Mya) · Hirnantian (445.2 – 443.4 Mya)
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Silurian
(443.4 – 419.2 Mya)
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Llandovery (443.4 – 433.4 Mya): Rhuddanian (443.4 – 440.8 Mya) · Aeronian (440.8 – 438.5 Mya) · Telychian (438.5 – 433.4 Mya)
Wenlock (433.4 – 427.4 Mya): Sheinwoodian (433.4 – 430.5 Mya) · Homerian (430.5 – 427.4 Mya)
Ludlow (427.4 – 423.0 Mya): Gorstian (427.4 – 425.6 Mya) · Ludfordian (425.6 – 423.0 Mya)
Pridoli (423.0 – 419.2 Mya)
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Devonian
(419.2 – 358.9 Mya)
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Lower Devonian (419.2 – 393.3 Mya): Lochkovian (419.2 – 410.8 Mya) · Pragian (410.8 – 407.6 Mya) · Emsian (407.6 – 393.3 Mya)
Middle Devonian (393.3 – 382.7 Mya): Eifelian (393.3 – 387.7 Mya) · Givetian (387.7 – 382.7 Mya)
Upper Devonian (382.7 – 358.9 Mya): Frasnian (382.7 – 372.2 Mya) · Famennian (372.2 – 358.9 Mya)
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Carboniferous
(358.9 – 298.9 Mya)
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Mississippian (358.9 – 323.2 Mya): Tournaisian / Early Mississippian (358.9 – 346.7 Mya) · Viséan / Middle Mississippian (346.7 – 330.9 Mya) · Serpukhovian / Late Mississippian (330.9 – 323.2 Mya)
Pennsylvanian (323.2 – 298.9 Mya): Bashkirian / Early Pennsylvanian (323.2 – 315.2 Mya) · Moscovian / Middle Pennsylvanian (315.2 – 307.0 Mya) · Late Pennsylvanian (307.0 – 298.9 Mya): Kasimovian (307.0 – 303.7 Mya) · Gzhelian (303.7 – 298.9 Mya)
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Permian
(298.9 – 252.2 Mya)
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Cisuralian (298.9 – 272.3 Mya): Asselian (298.9 – 295.5 Mya) · Sakmarian (295.5 – 290.1 Mya) · Artinskian (290.1 – 279.3 Mya) · Kungurian (279.3 – 272.3 Mya)
Guadalupian (272.3 – 259.9 Mya): Roadian (272.3 – 268.8 Mya) · Wordian (268.8 – 265.1 Mya) · Capitanian (265.1 – 259.9 Mya)
Lopingian (259.9 – 252.2 Mya): Wuchiapingian (259.9 – 254.2 Mya) · Changhsingian (254.2 – 252.2 Mya)
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Mesozoic (252.2 – 66.0 Mya)
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Triassic
(252.2 – 201.3 Mya)
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Lower Triassic (252.2 – 247.2 Mya): Induan (252.2 – 251.2 Mya) · Olenekian (251.2 – 247.2 Mya)
Middle Triassic (247.2 – 235 Mya): Anisian (247.2 – 242 Mya) · Ladinian (242 – 235 Mya)
Upper Triassic (235 – 201.3 Mya): Carnian (235 – 228 Mya) · Norian (228 – 208.5 Mya) · Rhaetian (208.5 – 201.3 Mya)
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Jurassic
(201.3 – 145.0 Mya)
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Lower Jurassic (201.3 – 174.1 Mya): Hettangian (201.3 – 199.3 Mya) · Sinemurian (199.3 – 190.8 Mya) · Pliensbachian (190.8 – 182.7 Mya) · Toarcian (182.7 – 174.1 Mya)
Middle Jurassic (174.1 – 163.5 Mya): Aalenian (174.1 – 170.3 Mya) · Bajocian (170.3 – 168.3 Mya) · Bathonian (168.3 – 166.1 Mya) · Callovian (166.1 – 163.5 Mya)
Upper Jurassic (163.5 – 145.0 Mya): Oxfordian (163.5 – 157.3 Mya) · Kimmeridgian (157.3 – 152.1 Mya) · Tithonian (152.1 – 145.0 Mya)
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Cretaceous
(145.0 – 66.0 Mya)
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Lower Cretaceous (145.0 – 100.5 Mya): Berriasian (145.0 – 139.8 Mya) · Valanginian (139.8 – 132.9 Mya) · Hauterivian (132.9 – 129.4 Mya) · Barremian (129.4 – 125.0 Mya) · Aptian (125.0 – 113.0 Mya) · Albian (113.0 – 100.5 Mya)
Upper Cretaceous (100.5 – 66.0 Mya): Cenomanian (100.5 – 93.9 Mya) · Turonian (93.9 – 89.8 Mya) · Coniacian (89.8 – 86.3 Mya) · Santonian (86.3 – 83.6 Mya) · Campanian (83.6 – 72.1 Mya) · Maastrichtian (72.1 – 66.0 Mya)
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Cenozoic (66.0 – 0 Mya)
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Paleogene, Neogene and early Pleistocene comprise former Tertiary* (66.0 – 1.8 Mya) period. Gelasian and Calabrian comprise Early Pleistocene (2.588 Mya – 781 kya) subepoch.
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Paleogene
(66.0 – 23.03 Mya)
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Paleocene (66.0 – 56.0 Mya): Danian (66.0 – 61.6 Mya) · Selandian (61.6 – 59.2 Mya) · Thanetian (59.2 – 56.0 Mya)
Eocene (56.0 – 33.9 Mya): Ypresian (56.0 – 47.8 Mya) · Lutetian (47.8 – 41.3 Mya) · Bartonian (41.3 – 38.0 Mya) · Priabonian (38.0 – 33.9 Mya)
Oligocene (33.9 – 23.03 Mya): Rupelian (33.9 – 28.1 Mya) · Chattian (28.1 – 23.03 Mya)
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Neogene
(23.03 – 2.588 Mya)
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Miocene (23.03 – 5.333 Mya): Aquitanian (23.03 – 20.44 Mya) · Burdigalian (20.44 – 15.97 Mya) · Langhian (15.97 – 13.82 Mya) · Serravallian (13.82 – 11.62 Mya) · Tortonian (11.62 – 7.246 Mya) · Messinian (7.246 – 5.333 Mya)
Pliocene (5.333 – 2.588 Mya): Piacenzian (5.333 – 3.600 Mya) · Zanclean (3.600 – 2.588 Mya)
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Quaternary
(2.588 – 0 Mya)
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Pleistocene (2.588 Mya – 11.7 kya): Gelasian (2.588 – 1.806 Mya) · Calabrian (1.806 Mya – 781 kya) · Middle Pleistocene / Ionian (781 – 126 kya) · Late Pleistocene / Tarantian (126 – 11.7 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 – 11.7 kya)
Holocene (11.7 – 0 kya): Preboreal* (11.7 – 9 kya) · Boreal* (9 – 8 kya) · Atlantic* (8 – 5 kya) · Subboreal* (5 – 2.5 kya) · Subatlantic* (2.5 – 0 kya)
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kya = thousands years ago. Mya = millions years ago. * Not officially recognized by the I.C.S.
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Source: International Chronostratigraphic Chart (January 2013). International Commission on Stratigraphy. Retrieved 27 March 2013. Divisions of Geologic Time—Major Chronostratigraphic and Geochronologic Units USGS Retrieved 10 March 2013.
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