The end-Ediacaran extinction is a mass extinction believed to have occurred near the end of the Ediacaran period, the final period of the Proterozoic eon. Evidence suggesting that such a mass extinction occurred includes a massive reduction in diversity of acritarchs, the sudden disappearance of the Ediacara biota and calcifying organisms, and the time gap before Cambrian organisms "replaced" them. Some lines of evidence suggests that there may have been two distinct pulses of the extinction event, one occurring 550 million years ago and the other 539 million years ago.[1]

Evidence

Biotic evidence

Ediacaran organisms

Most of the Ediacaran organisms featured in this image went extinct because of the extinction event.

During the Ediacaran period, two main groups of organisms are found in the fossil record: the "Ediacaran biota" of soft-bodied organisms, preserved by microbial mats; and calcifying organisms such as Cloudina and Namacalathus, which had a carbonate skeleton.[2] Because both these groups disappear abruptly at the end of the Ediacaran period, 538.8 ± 0.2 million years ago,[3] their disappearance cannot simply represent the closure of a preservational window,[4] as had previously been suspected.[2]

Additionally, the late Ediacaran saw a faunal turnover between the White Sea biota, which lived between 560 and 550 million years ago, and the Nama biota, which lived between 550 and 539 million years ago.[5] The transition from the White Sea to the Nama biota saw a major reduction in diversity that was not recovered during the interval of the depauperate Nama biota, which has been attributed to either increased biological competition[1] or an anoxic event[5] and in either case suggests that large-scale extinction began well before the boundary between the Ediacaran and Cambrian.

Post-Ediacaran survivors

The fossil record of the earliest Cambrian, just after the Ediacaran period, shows a sudden increase in burrowing activity and diversity. However, the Cambrian explosion of animals that gave rise to body fossils did not happen instantaneously. This implies that the "explosion" did not represent animals "replacing" the incumbent organisms, and pushing them gradually to extinction; rather, the data are more consistent with a radiation of animals to fill in vacant niches, left empty as an extinction cleared out the pre-existing fauna.[6]

The theory that all Ediacarans became extinct at the start of the Cambrian is disproven if any post-Ediacaran survivors are found. Organisms from the lower Cambrian, such as Thaumaptilon, were once thought to be Ediacarans, but this hypothesis no longer has many adherents.[7] One possible Ediacaran survivor whose status is still open to scrutiny is Ediacaria booleyi, a purported holdfast structure known from the upper Cambrian. If this does turn out to be a true Ediacaran, the biota cannot have disappeared completely. Disbelievers have claimed that the fossils don't actually have a biological origin, which doesn't seem to be the case—evidence is mounting to suggest that it is an organism (or at least of biological origin, perhaps a microbial colony),[8] just not one that is related to the Ediacara biota.[9]

Some organisms clearly survived the extinction since life on Earth has continued. However, very few organisms are known from both sides of the Ediacaran-Cambrian boundary. One such organism is the agglutinated foraminifera Platysolenites.[10] Swartpuntia is one well known late Ediacaran vendobiont, which survived into the earliest Cambrian.[11] Cambrian Erytholus is a similar sandstone cast to Ediacaran Ventogyrus.[12] Ordovician and Silurian Rutgersella[13] and Devonian Protonympha[14] have been interpreted as surviving vendobionts, comparable with Ediacaran Dickinsonia and Spriggina, respectively.

Geochemical evidence

Negative δ13C excursions—geochemical signals often associated with mass extinctions—are observed during the Late Ediacaran. The Shuram excursion occurred around the same time as the boundary between the White Sea and Nama assemblages.[15] Another major negative carbon isotope excursion is known to have occurred at the end of the Ediacaran period and the beginning of the Cambrian.[16]

Sedimentary evidence

The transition between the White Sea and Nama biotas near the end of the Ediacaran is reflected in the geological record by an increase in black shale deposition,[17] representing global anoxia.[18] This may be related to global changes in oceanic circulation and may have been the worst marine anoxic event of the last 550 million years,[6][17][19] although its causal relationship with the White Sea-Nama biotic turnover is controversial and has been challenged by studies concluding that this expansion of anoxia postdated the turnover.[20]

References

  1. 1 2 Darroch, Simon A. F.; Sperling, Erik A.; Boag, Thomas H.; Racicot, Rachel A.; Mason, Sara J.; Morgan, Alex S.; Tweedt, Sarah; Myrow, Paul; Johnston, David T.; Erwin, Douglas H.; Laflamme, Marc (7 September 2015). "Biotic replacement and mass extinction of the Ediacara biota". Proceedings of the Royal Society B. 282 (1814): 1–10. doi:10.1098/rspb.2015.1003. PMC 4571692. PMID 26336166.
  2. 1 2 Amthor, Joachim 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. ISSN 0091-7613.
  3. ↑ "Stratigraphic Chart 2022" (PDF). International Stratigraphic Commission. February 2022. Retrieved 25 April 2022.
  4. ↑ Marshall, Charles R. (2006). "Explaining The Cambrian "Explosion" Of Animals". Annual Review of Earth and Planetary Sciences. 34: 355–384. Bibcode:2006AREPS..34..355M. doi:10.1146/annurev.earth.33.031504.103001. S2CID 85623607.
  5. 1 2 Evans, Scott D.; Tu, Chenyi; Rizzo, Adriana; Surprenant, Rachel L.; Boan, Phillip C.; McCandless, Heather; Marshall, Nathan; Xiao, Shuhai; Droser, Mary L. (7 November 2022). "Environmental drivers of the first major animal extinction across the Ediacaran White Sea-Nama transition". Proceedings of the National Academy of Sciences. 119 (46): e2207475119. Bibcode:2022PNAS..11907475E. doi:10.1073/pnas.2207475119. hdl:10919/112639. PMC 9674242. PMID 36343248.
  6. 1 2 Wille, M; Nägler, T.F.; Lehmann, B; Schröder, S; Kramers, J.D (June 2008). "Hydrogen sulphide release to surface waters at the Precambrian/Cambrian boundary". Nature. 453 (7196): 767–9. Bibcode:2008Natur.453..767W. doi:10.1038/nature07072. PMID 18509331. S2CID 4425120.
  7. ↑ Antcliffe, Jonathan B.; Brasier, Martin D. (2007). "Charnia and sea pens are poles apart". Journal of the Geological Society. 164 (1): 49–51. Bibcode:2007JGSoc.164...49A. doi:10.1144/0016-76492006-080. S2CID 130602154.
  8. ↑ See Ediacaria
  9. ↑ MacGabhann, B. A.; Murray, J.; Nicholas, C. (2007), "Ediacaria booleyi: weeded from the Garden of Ediacara?", in Vickers-Rich, Patricia; Komarower, Patricia (eds.), The Rise and Fall of the Ediacaran Biota, Special publications, vol. 286, London: Geological Society, pp. 277=295, doi:10.1144/SP286.20, ISBN 978-1-86239-233-5, OCLC 156823511
  10. ↑ Kontorovich, A; Varlamov, A; Grazhdankin, D; Karlova, G; Klets, A; Kontorovich, V; Saraev, S; Terleev, A; Belyaev, S; et al. (2008). "A section of Vendian in the east of West Siberian Plate (based on data from the Borehole Vostok 3)". Russian Geology and Geophysics. 49 (12): 932. Bibcode:2008RuGG...49..932K. doi:10.1016/j.rgg.2008.06.012.
  11. ↑ Jensen, Sören; James G. Gehling; Mary L. Droser (1998). "Ediacara-type fossils in Cambrian sediments". Nature. 393 (6685): 567–569. Bibcode:1998Natur.393..567J. doi:10.1038/31215. S2CID 205001064.
  12. ↑ Retallack, G.J. (2011). "Problematic megafossils in Cambrian palaeosols of South Australia". Palaeontology. 54 (6): 1223–1242. Bibcode:2011Palgy..54.1223R. doi:10.1111/j.1475-4983.2011.01099.x. S2CID 130692406.
  13. ↑ Retallack, G.J. (2015). "Reassessment of the Silurian problematicum Rutgersella as another post-Ediacaran vendobiont". Alcheringa. 39 (4): 573–588. doi:10.1080/03115518.2015.1069483. S2CID 54780312.
  14. ↑ Retallack, G.J. (2018). "Reassessment of the Devonian Problematicum Protonympha as another post-Ediacaran vendobiont". Lethaia. 50. doi:10.1111/let12253 (inactive 1 August 2023).{{cite journal}}: CS1 maint: DOI inactive as of August 2023 (link)
  15. ↑ Erwan Le Guerroué; et al. (Apr 2006). "Chemostratigraphic and sedimentological framework of the largest negative carbon isotopic excursion in Earth history: The Neoproterozoic Shuram Formation (Nafun Group, Oman)". Precambrian Research. 146 (1–2): 68–92. Bibcode:2006PreR..146...68L. doi:10.1016/j.precamres.2006.01.007.
  16. ↑ Zhu; Babcock, L; Peng, S (2006). "Advances in Cambrian stratigraphy and paleontology: Integrating correlation techniques, paleobiology, taphonomy and paleoenvironmental reconstruction". Palaeoworld. 15 (3–4): 217. doi:10.1016/j.palwor.2006.10.016.
  17. 1 2 Schroder, S.; Grotzinger, J.P. (2007). "Evidence for anoxia at the Ediacaran-Cambrian boundary: the record of redox-sensitive trace elements and rare earth elements in Oman". Journal of the Geological Society. 164 (1): 175–187. Bibcode:2007JGSoc.164..175S. doi:10.1144/0016-76492005-022. S2CID 18376742.
  18. ↑ Fike, D.A.; Grotzinger, J.P.; Pratt, L.M.; Summons, R.E. (2006). "Multi-Stage Ediacaran Ocean Oxidation and Its Impact on Evolutionary Radiation". Geochimica et Cosmochimica Acta. 70 (18S): 173. Bibcode:2006GeCAS..70Q.173F. doi:10.1016/j.gca.2006.06.347.
  19. ↑ "What caused the mass extinction of Earth's first animals? Unravelling mystery of the Ediacaran-Cambrian transition". ScienceDaily. Retrieved 20 February 2020.
  20. ↑ Tostevin, Rosalie; Clarkson, Matthew O.; Gangl, Sophie; Shields, Graham A.; Wood, Rachel A.; Bowyer, Fred; Penny, Amelia M.; Stirling, Claudine H. (15 January 2019). "Uranium isotope evidence for an expansion of anoxia in terminal Ediacaran oceans". Earth and Planetary Science Letters. 506: 104–112. Bibcode:2019E&PSL.506..104T. doi:10.1016/j.epsl.2018.10.045. S2CID 134663328. Retrieved 17 December 2022.
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