The Precambrian (or Pre-Cambrian, sometimes abbreviated pꞒ, or Cryptozoic) is the earliest part of Earth's history, set before the current Phanerozoic Eon. The Precambrian is so named because it preceded the Cambrian, the first period of the Phanerozoic Eon, which is named after Cambria, the Latinised name for Wales, where rocks from this age were first studied. The Precambrian accounts for 88% of the Earth's geologic time.
The Precambrian (colored red in the timeline figure) is an informal unit of geologic time, subdivided into three eons (Hadean, Archean, Proterozoic) of the geologic time scale. It spans from the formation of Earth about 4.6 billion years ago (Ga) to the beginning of the Cambrian Period, about 541 million years ago (Ma), when hard-shelled creatures first appeared in abundance.
Relatively little is known about the Precambrian, despite it making up roughly seven-eighths of the Earth's history, and what is known has largely been discovered from the 1960s onwards. The Precambrian fossil record is poorer than that of the succeeding Phanerozoic, and fossils from the Precambrian (e.g. stromatolites) are of limited biostratigraphic use. This is because many Precambrian rocks have been heavily metamorphosed, obscuring their origins, while others have been destroyed by erosion, or remain deeply buried beneath Phanerozoic strata.
Eozoic (from eo- “earliest”) was a synonym for pre-Cambrian, or more specifically Archean.
Landmass positions near the end of the Precambrian
A specific date for the origin of life has not been determined. Carbon found in 3.8 billion-year-old rocks (Archean eon) from islands off western Greenland may be of organic origin. Well-preserved microscopic fossils of bacteria older than 3.46 billion years have been found in Western Australia. Probable fossils 100 million years older have been found in the same area. However, there is evidence that life could have evolved over 4.280 billion years ago. There is a fairly solid record of bacterial life throughout the remainder (Proterozoic eon) of the Precambrian.
Complex multicellular organisms may have appeared as early as 2100 Ma. However, the interpretation of ancient fossils is problematic, and "... some definitions of multicellularity encompass everything from simple bacterial colonies to badgers." Other possible early complex multicellular organisms include a possible 2450 Ma red alga from the Kola Peninsula, 1650 Ma carbonaceous biosignatures in north China, the 1600 Ma Rafatazmia, and a possible 1047 Ma Bangiomorpha red alga from the Canadian Arctic. The earliest fossils widely accepted as complex multicellular organisms date from the Ediacaran period. A very diverse collection of soft-bodied forms is found in a variety of locations worldwide and date to between 635 and 542 Ma. These are referred to as Ediacaran or Vendian biota. Hard-shelled creatures appeared toward the end of that time span, marking the beginning of the Phanerozoic eon. By the middle of the following Cambrian period, a very diverse fauna is recorded in the Burgess Shale, including some which may represent stem groups of modern taxa. The increase in diversity of lifeforms during the early Cambrian is called the Cambrian explosion of life.
While land seems to have been devoid of plants and animals, cyanobacteria and other microbes formed prokaryotic mats that covered terrestrial areas.
Tracks from an animal with leg-like appendages have been found in what was mud 551 million years ago.
Evidence of the details of plate motions and other tectonic activity in the Precambrian has been poorly preserved. It is generally believed that small proto-continents existed prior to 4280 Ma, and that most of the Earth's landmasses collected into a single supercontinent around 1130 Ma. The supercontinent, known as Rodinia, broke up around 750 Ma. A number of glacial periods have been identified going as far back as the Huronian epoch, roughly 2400–2100 Ma. One of the best studied is the Sturtian-Varangian glaciation, around 850–635 Ma, which may have brought glacial conditions all the way to the equator, resulting in a "Snowball Earth".
The atmosphere of the early Earth is not well understood. Most geologists believe it was composed primarily of nitrogen, carbon dioxide, and other relatively inert gases, and was lacking in free oxygen. There is, however, evidence that an oxygen-rich atmosphere existed since the early Archean.
At present, it is still believed that molecularoxygen was not a significant fraction of Earth's atmosphere until after photosynthetic life forms evolved and began to produce it in large quantities as a byproduct of their metabolism. This radical shift from a chemically inert to an oxidizing atmosphere caused an ecological crisis, sometimes called the oxygen catastrophe. At first, oxygen would have quickly combined with other elements in Earth's crust, primarily iron, removing it from the atmosphere. After the supply of oxidizable surfaces ran out, oxygen would have begun to accumulate in the atmosphere, and the modern high-oxygen atmosphere would have developed. Evidence for this lies in older rocks that contain massive banded iron formations that were laid down as iron oxides.
Proterozoic: this eon refers to the time from the lower Cambrian boundary, 541 Ma, back through 2500 Ma. As originally used, it was a synonym for "Precambrian" and hence included everything prior to the Cambrian boundary. The Proterozoic eon is divided into three eras: the Neoproterozoic, Mesoproterozoic and Paleoproterozoic.
Neoproterozoic: The youngest geologic era of the Proterozoic Eon, from the Cambrian Period lower boundary (541 Ma) back to 1000 Ma. The Neoproterozoic corresponds to Precambrian Z rocks of older North American stratigraphy.
Hadean Eon: 4000–4600 Ma. This term was intended originally to cover the time before any preserved rocks were deposited, although some zircon crystals from about 4400 Ma demonstrate the existence of crust in the Hadean Eon. Other records from Hadean time come from the moon and meteorites.
It has been proposed that the Precambrian should be divided into eons and eras that reflect stages of planetary evolution, rather than the current scheme based upon numerical ages. Such a system could rely on events in the stratigraphic record and be demarcated by GSSPs. The Precambrian could be divided into five "natural" eons, characterized as follows:
The movement of Earth's plates has caused the formation and break-up of continents over time, including occasional formation of a supercontinent containing most or all of the landmass. The earliest known supercontinent was Vaalbara. It formed from proto-continents and was a supercontinent 3.636 billion years ago. Vaalbara broke up c. 2.845–2.803 Ga ago. The supercontinent Kenorland was formed c. 2.72 Ga ago and then broke sometime after 2.45–2.1 Ga into the proto-continent cratons called Laurentia, Baltica, Yilgarn craton and Kalahari. The supercontinent Columbia, or Nuna, formed 2.1–1.8 billion years ago and broke up about 1.3–1.2 billion years ago. The supercontinent Rodinia is thought to have formed about 1300-900 Ma, to have embodied most or all of Earth's continents and to have broken up into eight continents around 750–600 million years ago.
Phanerozoic – Fourth and current eon of the geological timescale
Paleozoic – First era of the Phanerozoic Eon 541-252 million years ago
Mesozoic – Second era of the Phanerozoic Eon: ~252–66 million years ago
Cenozoic – Third era of the Phanerozoic Eon 66 million years ago to present
^Gradstein, F.M.; Ogg, J.G.; Schmitz, M.D.; Ogg, G.M., eds. (2012). The Geologic Timescale 2012. 1. Elsevier. p. 301. ISBN 978-0-44-459390-0.
^ abMonroe, James S.; Wicander, Reed (1997). The Changing Earth: Exploring Geology and Evolution (2nd ed.). Belmont: Wadsworth Publishing Company. p. 492. ISBN 9781285981383.
^Levin, Harold L. (2010). The earth through time (9th ed.). Hoboken, N.J.: J. Wiley. pp. 230–233. ISBN 978-0470387740. Outlined in Gore, Pamela J.W. (25 October 2005). "The Earliest Earth: 2,100,000,000 years of the Archean Eon".
^"Zircons are Forever". Department of Geoscience. 2005. Retrieved 28 April 2007.
^Cavosie, Aaron J.; Valley, John W.; Wilde, Simon A. (2007). "Chapter 2.5 The Oldest Terrestrial Mineral Record: A Review of 4400 to 4000 Ma Detrital Zircons from Jack Hills, Western Australia". Developments in Precambrian Geology. 15: 91–111. doi:10.1016/S0166-2635(07)15025-8. ISBN 9780444528100.
^U.S. Geological Survey Geologic Names Committee (2010), "Divisions of geologic time – major chronostratigraphic and geochronologic units", U.S. Geological Survey Fact Sheet 2010–3059, United States Geological Survey, p. 2, retrieved 20 June 2018
^Senter, Phil (1 April 2013). "The Age of the Earth & Its Importance to Biology". The American Biology Teacher. 75 (4): 251–256. doi:10.1525/abt.2013.75.4.5. S2CID 85652369.
^Kamp, Ulrich (6 March 2017). "Glaciations". International Encyclopedia of Geography: People, the Earth, Environment and Technology: 1–8. doi:10.1002/9781118786352.wbieg0612. ISBN 9780470659632.
^"Stratigraphic Guide". International Commission on Stratigraphy. Table 3. Retrieved 9 December 2020.CS1 maint: location (link)
^Hitchcock, C. H. (1874). The Geology of New Hampshire. p. 511. The name Eozoic seems to have been proposed by Dr. J.W. Dawson, of Montreal, in 1865. He did not fully define the limits of its application at that time; but it seems to have been generally understood by geologists to embrace all the obscurely fossiliferous rocks older than the Cambrian.
^Bulletin. 767. U.S. Government Printing Office. 1925. p. 3.  Sir J. W. Dawson prefers the term “Eozoic” [to Archean], and would have it include all the Pre-Cambrian strata.
^Salop, L.J. (2012). Geological Evolution of the Earth During the Precambrian. Springer. p. 9. ISBN 978-3-642-68684-9. a possibility of dividing the Precambrian history into two eons: the Eozoic, embracing the Archean Era only, and the Protozoic, comprising all the remaining Precambrian Eras.
^Dodd, Matthew S.; Papineau, Dominic; Grenne, Tor; slack, John F.; Rittner, Martin; Pirajno, Franco; O'Neil, Jonathan; Little, Crispin T. S. (2 March 2017). "Evidence for early life in Earth's oldest hydrothermal vent precipitates". Nature. 543 (7643): 60–64. Bibcode:2017Natur.543...60D. doi:10.1038/nature21377. PMID28252057.
^Donoghue, Philip C. J.; Antcliffe, Jonathan B. (July 2010). "Origins of multicellularity". Nature. 466 (7302): 41–42. doi:10.1038/466041a. PMID20596008. S2CID 4396466.
^Rozanov, A. Yu.; Astafieva, M. M. (1 March 2013). "A unique find of the earliest multicellular algae in the Lower Proterozoic (2.45 Ga) of the Kola Peninsula". Doklady Biological Sciences. 449 (1): 96–98. doi:10.1134/S0012496613020051. PMID23652437. S2CID 15774804.
^Qu, Yuangao; Zhu, Shixing; Whitehouse, Martin; Engdahl, Anders; McLoughlin, Nicola (1 January 2018). "Carbonaceous biosignatures of the earliest putative macroscopic multicellular eukaryotes from 1630 Ma Tuanshanzi Formation, north China". Precambrian Research. 304: 99–109. doi:10.1016/j.precamres.2017.11.004.
^Bengtson, Stefan; Sallstedt, Therese; Belivanova, Veneta; Whitehouse, Martin (14 March 2017). "Three-dimensional preservation of cellular and subcellular structures suggests 1.6 billion-year-old crown-group red algae". PLOS Biology. 15 (3): e2000735. doi:10.1371/journal.pbio.2000735. PMC5349422. PMID28291791.
^Gibson, Timothy M; Shih, Patrick M; Cumming, Vivien M; Fischer, Woodward W; Crockford, Peter W; Hodgskiss, Malcolm S.W; Wörndle, Sarah; Creaser, Robert A; Rainbird, Robert H; Skulski, Thomas M; Halverson, Galen P (2017). "Precise age of Bangiomorpha pubescens dates the origin of eukaryotic photosynthesis" (PDF). Geology. 46 (2): 135–138. doi:10.1130/G39829.1.
^Laflamme, M. (9 September 2014). "Modeling morphological diversity in the oldest large multicellular organisms". Proceedings of the National Academy of Sciences. 111 (36): 12962–12963. Bibcode:2014PNAS..11112962L. doi:10.1073/pnas.1412523111. PMC4246935. PMID25114212.
^Kolesnikov, Anton V.; Rogov, Vladimir I.; Bykova, Natalia V.; Danelian, Taniel; Clausen, Sébastien; Maslov, Andrey V.; Grazhdankin, Dmitriy V. (October 2018). "The oldest skeletal macroscopic organism Palaeopascichnus linearis". Precambrian Research. 316: 24–37. Bibcode:2018PreR..316...24K. doi:10.1016/j.precamres.2018.07.017.
^Clemmey, Harry; Badham, Nick (1982). "Oxygen in the Precambrian Atmosphere". Geology. 10 (3): 141–146. Bibcode:1982Geo....10..141C. doi:10.1130/0091-7613(1982)10<141:OITPAA>2.0.CO;2.
^Geological Society of America's "2009 GSA Geologic Time Scale."
^Harrison, T. Mark (27 April 2009). "The Hadean Crust: Evidence from >4 Ga Zircons". Annual Review of Earth and Planetary Sciences. 37 (1): 479–505. Bibcode:2009AREPS..37..479H. doi:10.1146/annurev.earth.031208.100151.
^Abramov, Oleg; Kring, David A.; Mojzsis, Stephen J. (October 2013). "The impact environment of the Hadean Earth". Geochemistry. 73 (3): 227–248. Bibcode:2013ChEG...73..227A. doi:10.1016/j.chemer.2013.08.004.
^Bleeker, W. (2004) . "Toward a "natural" Precambrian time scale". In Felix M. Gradstein; James G. Ogg; Alan G. Smith (eds.). A Geologic Time Scale 2004. Cambridge University Press. ISBN 978-0-521-78673-7. also available at Stratigraphy.org: Precambrian subcommission
^Zhao, Guochun; Cawood, Peter A.; Wilde, Simon A.; Sun, M. (2002). "Review of global 2.1–1.8 Ga orogens: implications for a pre-Rodinia super-continent". Earth-Science Reviews. 59 (1): 125–162. Bibcode:2002ESRv...59..125Z. doi:10.1016/S0012-8252(02)00073-9.
^Zhao, Guochun; Sun, M.; Wilde, Simon A.; Li, S.Z. (2004). "A Paleo-Mesoproterozoic super-continent: assembly, growth and breakup". Earth-Science Reviews (Submitted manuscript). 67 (1): 91–123. Bibcode:2004ESRv...67...91Z. doi:10.1016/j.earscirev.2004.02.003.
^Li, Z. X.; Bogdanova, S. V.; Collins, A. S.; Davidson, A.; De Waele, B.; Ernst, R. E.; Fitzsimons, I. C. W.; Fuck, R. A.; Gladkochub, D. P.; Jacobs, J.; Karlstrom, K. E.; Lul, S.; Natapov, L. M.; Pease, V.; Pisarevsky, S. A.; Thrane, K.; Vernikovsky, V. (2008). "Assembly, configuration, and break-up history of Rodinia: A synthesis" (PDF). Precambrian Research. 160 (1–2): 179–210. Bibcode:2008PreR..160..179L. doi:10.1016/j.precamres.2007.04.021. Retrieved 6 February 2016.
Valley, John W., William H. Peck, Elizabeth M. King (1999) Zircons Are Forever, The Outcrop for 1999, University of Wisconsin-Madison Wgeology.wisc.edu – Evidence from detrital zircons for the existence of continental crust and oceans on the Earth 4.4 Gyr ago Accessed Jan. 10, 2006
Wilde, S. A.; Valley, J. W.; Peck, W. H.; Graham, C. M. (2001). "Evidence from detrital zircons for the existence of continental crust and oceans on the Earth 4.4 Gyr ago". Nature. 409 (6817): 175–178. Bibcode:2001Natur.409..175W. doi:10.1038/35051550. PMID11196637. S2CID 4319774.
Wyche, S.; Nelson, D. R.; Riganti, A. (2004). "4350–3130 Ma detrital zircons in the Southern Cross Granite–Greenstone Terrane, Western Australia: implications for the early evolution of the Yilgarn Craton". Australian Journal of Earth Sciences. 51 (1): 31–45. Bibcode:2004AuJES..51...31W. doi:10.1046/j.1400-0952.2003.01042.x.
Wikimedia Commons has media related to Precambrian.
Late Precambrian Supercontinent and Ice House World from the Paleomap Project