|Proposed redefinition(s)||850–541 Ma|
Gradstein et al., 2012
|Proposed subdivisions||Cryogenian Period, 850–630 Ma|
Gradstein et al., 2012
|Regional usage||Global (ICS)|
|Time scale(s) used||ICS Time Scale|
|Time span formality||Formal|
|Lower boundary definition||Defined Chronometrically|
|Lower boundary GSSP||N/A|
|Upper boundary definition||Appearance of the Ichnofossil Treptichnus pedum|
|Upper boundary GSSP||Fortune Head section, Newfoundland, Canada|
It is the last era of the Precambrian Supereon and the Proterozoic Eon; it is subdivided into the Tonian, Cryogenian, and Ediacaran periods. It is preceded by the Mesoproterozoic Era and succeeded by the Paleozoic Era of the Phanerozoic Eon.
According to Rino and co-workers, the sum of the continental crust formed in the Pan-African orogeny and the Grenville orogeny makes the Neoproterozoic the period of Earth's history that has produced most continental crust.
At the onset of the Neoproterozoic the supercontinent Rodinia, which had assembled during the late Mesoproterozoic, straddled the equator. During the Tonian, rifting commenced which broke Rodinia into a number of individual land masses.
Possibly as a consequence of the low-latitude position of most continents, several large-scale glacial events occurred during the Neoproterozoic Era including the Sturtian and Marinoan glaciations of the Cryogenian Period.
These glaciations are believed to have been so severe that there were ice sheets at the equator—a state known as the "Snowball Earth".
Russian regional timescale
In the regional timescale of Russia, the Tonian and Cryogenian correspond to the Late Riphean; the Ediacaran corresponds to the Early to middle Vendian. Russian geologists divide the Neoproterozoic of Siberia into the Mayanian (from 1000 to 850 Ma) followed by the Baikalian (from 850 to 650 Ma).
The idea of the Neoproterozoic Era was introduced in the 1960s. Nineteenth-century paleontologists set the start of multicellular life at the first appearance of hard-shelled arthropods called trilobites and archeocyathid sponges at the beginning of the Cambrian Period. In the early 20th century, paleontologists started finding fossils of multicellular animals that predated the Cambrian. A complex fauna was found in South West Africa in the 1920s but was inaccurately dated. Another fauna was found in South Australia in the 1940s, but it was not thoroughly examined until the late 1950s. Other possible early animal fossils were found in Russia, England, Canada, and elsewhere (see Ediacaran biota). Some were determined to be pseudofossils, but others were revealed to be members of rather complex biotas that remain poorly understood. At least 25 regions worldwide have yielded metazoan fossils older than the classical Precambrian–Cambrian boundary (which is currently dated at ).
A few of the early animals appear possibly to be ancestors of modern animals. Most fall into ambiguous groups of frond-like organisms; discoids that might be holdfasts for stalked organisms ("medusoids"); mattress-like forms; small calcareous tubes; and armored animals of unknown provenance.
These were most commonly known as Vendian biota until the formal naming of the Period, and are currently known as Ediacaran Period biota. Most were soft bodied. The relationships, if any, to modern forms are obscure. Some paleontologists relate many or most of these forms to modern animals. Others acknowledge a few possible or even likely relationships but feel that most of the Ediacaran forms are representatives of unknown animal types.
In addition to Ediacaran biota, two other types of biota were discovered in China. The Doushantuo Formation preserves fossils of microscopic marine organisms in great detail. The Hainan biota consists of small worm-shaped organisms.
Molecular phylogeny suggests that animals may have emerged even earlier in the Proterozoic, but physical evidence for such animal life is lacking. Possible keratose sponge fossils have been reported in reefs dating back to 890 million years before the present, but remain unconfirmed.
The nomenclature for the terminal period of the Neoproterozoic Era has been unstable. Russian and Nordic geologists referred to the last period of the Neoproterozoic as the Vendian, while Chinese geologists referred to it as the Sinian, and most Australians and North Americans used the name Ediacaran.
However, in 2004, the International Union of Geological Sciences ratified the Ediacaran Period to be a geological age of the Neoproterozoic, ranging from 635 to 538.8 (at the time to 542) million years ago. The Ediacaran Period boundaries are the only Precambrian boundaries defined by biologic Global Boundary Stratotype Section and Points, rather than the absolute Global Standard Stratigraphic Ages.
- Boring Billion – Earth history between 1.8 and 0.8 billion years ago
- "Stratigraphic Chart 2022" (PDF). International Stratigraphic Commission. February 2022. Retrieved 22 April 2022.
- Rino, S.; Kon, Y.; Sato, W.; Maruyama, S.; Santosh, M.; Zhao, D. (2008). "The Grenvillian and Pan-African orogens: World's largest orogenies through geologic time, and their implications on the origin of superplume". Gondwana Research. 14 (1–2): 51–72. Bibcode:2008GondR..14...51R. doi:10.1016/j.gr.2008.01.001.
- Craig, J. (26 November 2015). "Global Climate, the Dawn of Life and the Earth's Oldest Petroleum Systems". Retrieved 15 March 2019.
- Khomentovsky, V; Nagovitsin, K; Postnikov, A (2008). "Mayanian (1100–850 Ma) – Prebaikalian Upper Riphean of Siberia". Russian Geology and Geophysics. 49 (1): 1. Bibcode:2008RuGG...49....1K. doi:10.1016/j.rgg.2007.12.001.
- Knoll, A. H.; Walter, M.; Narbonne, G.; Christie-Blick, N. (2006). "The Ediacaran Period: a new addition to the geologic time scale". Lethaia. 39 (1): 13–30. doi:10.1080/00241160500409223.
- Muscente, A.D.; Hawkins, Andrew D.; Xiao, Shuhai (September 2015). "Fossil preservation through phosphatization and silicification in the Ediacaran Doushantuo Formation (South China): a comparative synthesis". Palaeogeography, Palaeoclimatology, Palaeoecology. 434: 46–62. doi:10.1016/j.palaeo.2014.10.013.
- Malenkov, A. G. (May 2018). "13C, Ontogeny, and the Paradox of Evolution". Biophysics. 63 (3): 477–484. doi:10.1134/S0006350918030156.
- Turner, Elizabeth C. (28 July 2021). "Possible poriferan body fossils in early Neoproterozoic microbial reefs". Nature. 596 (7870): 87–91. Bibcode:2021Natur.596...87T. doi:10.1038/s41586-021-03773-z. PMC 8338550. PMID 34321662.
- Ogg, James G.; Ogg, Gabi; Gradstein, Felix M. (2008). The Concise Geologic Time Scale. Cambridge University Press. p. 184. ISBN 978-0-521-89849-2.
- U.S. Geological Survey Geologic Names Committee (March 2007). "Divisions of Geologic Time— Major Chronostratigraphic and Geochronologic Units" (PDF). USGS Fact Sheet 2007–3015. USGS. Retrieved 22 April 2022.
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