Earth:Eifelian
| Eifelian | |
|---|---|
| 393.3 ± 1.2 – 387.7 ± 0.8 Ma | |
| Chronology | |
| Etymology | |
| Name formality | Formal |
| Usage information | |
| Celestial body | Earth |
| Regional usage | Global (ICS) |
| Time scale(s) used | ICS Time Scale |
| Definition | |
| Chronological unit | Age |
| Stratigraphic unit | Stage |
| Time span formality | Formal |
| Lower boundary definition | FAD of the conodont Polygnathus costatus partitus |
| Lower boundary GSSP | Wetteldorf Richtschnitt section, Wetteldorf, Eifel, Germany [ ⚑ ] 50°08′59″N 6°28′18″E / 50.1496°N 6.4716°E |
| GSSP ratified | 1985[5] |
| Upper boundary definition | FAD of the conodont Polygnathus hemiansatus |
| Upper boundary GSSP | Jebel Mech Irdane, Tafilalt, Morocco [ ⚑ ] 31°14′15″N 4°21′15″W / 31.2374°N 4.3541°W |
| GSSP ratified | 1994[6] |
The Eifelian is the first of two faunal stages in the Middle Devonian Epoch. It lasted from 393.3 ± 1.2 million years ago to 387.7 ± 0.8 million years ago. It was preceded by the Emsian Stage and followed by the Givetian Stage.
North American subdivisions of the Eifelian Stage include Southwood, and part of Cazenovia (or Cazenovian).
Name and definition
The Eifelian is named after the Eifel Mountains of Western Germany , which exposed the GSSP section at the Wetteldorf Richtschnitt outcrop. The base of the Eifelian is defined by the start of the Polygnathus partitus conodont zone. This layer lies within the Upper Heisdorf Formation, 1.9 metres (6.2 ft) below the base of the Lauch Formation.[7]
Extinctions
The end of the Eifelian was marked by a biological crisis known as the Kačák Event, a two-part interval of extinction which led to ecological turnover among ammonoids, conodonts, and other free-swimming animals.[8][9] In deep marine waters, the event is indicated by anoxic black shales. There is evidence for a major pulse of transgression (sea level rise) and warming during the event.[10][11][12]
Warming and sea level rise through the Eifelian and beyond would have had major effects on diversity, likely leading to the downfall of several marine biogeographic realms. The cool-water Malvinokaffric Realm (MKR), on the northwest edge of Gondwana, was decimated as rising temperatures eliminated suitably temperate habitat. Fauna of the Eastern Americas Realm (EAR), which was restricted to a shallow basin in southwest Laurussia, were gradually replaced by aggressive cosmopolitan species of the Old World Realm (OWR), which invaded through a seaway cutting along a flooded continental arch on the western edge of Laurussia.[9]
References
- ↑ Parry, S. F.; Noble, S. R.; Crowley, Q. G.; Wellman, C. H. (2011). "A high-precision U–Pb age constraint on the Rhynie Chert Konservat-Lagerstätte: time scale and other implications". Journal of the Geological Society (London: Geological Society) 168 (4): 863–872. doi:10.1144/0016-76492010-043. http://jgs.lyellcollection.org/content/168/4/863.abstract.
- ↑ Kaufmann, B.; Trapp, E.; Mezger, K. (2004). "The numerical age of the Upper Frasnian (Upper Devonian) Kellwasser horizons: A new U-Pb zircon date from Steinbruch Schmidt(Kellerwald, Germany)". The Journal of Geology 112 (4): 495–501. doi:10.1086/421077. Bibcode: 2004JG....112..495K.
- ↑ Algeo, T. J. (1998). "Terrestrial-marine teleconnections in the Devonian: links between the evolution of land plants, weathering processes, and marine anoxic events". Philosophical Transactions of the Royal Society B: Biological Sciences 353 (1365): 113–130. doi:10.1098/rstb.1998.0195.
- ↑ "Chart/Time Scale". International Commission on Stratigraphy. http://www.stratigraphy.org/index.php/ics-chart-timescale.
- ↑ Ziegler, W.; Klapper, G. (June 1985). "Stages of the Devonian System". Episodes 8 (2): 104–109. doi:10.18814/epiiugs/1985/v8i2/006. https://stratigraphy.org/gssps/files/eifelian.pdf. Retrieved 18 December 2020.
- ↑ Walliser, O.; Bultynck, P.; Weddige, K.; Becker, R.; House, M. (September 1995). "Definition of the Eifelian-Givetian Stage boundary". Episodes 18 (3): 107–115. doi:10.18814/epiiugs/1995/v18i3/002. https://www.researchgate.net/publication/262723723. Retrieved 19 December 2020.
- ↑ "GSSP for the Emsian - Eifelian Stage Boundary". stratigraphy. http://www.stratigraphy.org/eifel.htm.
- ↑ House, Michael R. (1985). "Correlation of mid-Palaeozoic ammonoid evolutionary events with global sedimentary perturbations" (in en). Nature 313 (5997): 17–22. doi:10.1038/313017a0. ISSN 1476-4687. https://www.nature.com/articles/313017a0.
- ↑ 9.0 9.1 Jamart, V.; Denayer, J. (2020). "The Kačák event (late Eifelian, Middle Devonian) on the Belgian shelf and its effects on rugose coral palaeobiodiversity". Bulletin of Geosciences 95 (3): 279–311. doi:10.3140/bull.geosci.1788. http://www.geology.cz/bulletin/fulltext/1788_Jamart_20200808.pdf.
- ↑ Königshof, P.; Silva, A. C. Da; Suttner, T. J.; Kido, E.; Waters, J.; Carmichael, S. K.; Jansen, U.; Pas, D. et al. (2016-01-01). "Shallow-water facies setting around the Kačák Event: a multidisciplinary approach" (in en). Geological Society, London, Special Publications 423 (1): 171–199. doi:10.1144/SP423.4. ISSN 0305-8719. https://sp.lyellcollection.org/content/423/1/171.
- ↑ DeSantis, M. K.; Brett, C. E.; Straeten, C. A. Ver (2007-01-01). "Persistent depositional sequences and bioevents in the Eifelian (early Middle Devonian) of eastern Laurentia: North American evidence of the Kačák Events?" (in en). Geological Society, London, Special Publications 278 (1): 83–104. doi:10.1144/SP278.4. ISSN 0305-8719. https://sp.lyellcollection.org/content/278/1/83.
- ↑ Marshall, J. E. A.; Astin, T. R.; Brown, J. F.; Mark-Kurik, E.; Lazauskiene, J. (2007-01-01). "Recognizing the Kačák Event in the Devonian terrestrial environment and its implications for understanding land–sea interactions" (in en). Geological Society, London, Special Publications 278 (1): 133–155. doi:10.1144/SP278.6. ISSN 0305-8719. https://sp.lyellcollection.org/content/278/1/133.
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