Orogenic collapse is the thinning and spreading of thickened crust

In geology, orogenic collapse is the thinning and lateral spread of thickened crust. It is a broad term referring to processes which distribute material from regions of high gravitational potential energy to regions of low gravitational potential energy.[1][2] Orogenic collapse can begin at any point during an orogeny due to overthickening of the crust. Post-orogenic collapse and post-orogenic extension refer to processes which take place once tectonic forces have been released, and represent a key phase of the Wilson Cycle, between continental collision and rifting.[3]

Orogens (also known as orogenic belts, or more simply mountain ranges) are sections of thickened crust which are built up as tectonic plates collide. The thickening of the crust marks the start of an orogeny, or "mountain building event." As the orogeny progresses, the orogen may start spreading apart and thinning. Collapse processes can begin either once the orogeny ends as the tectonic forces cease, or during the orogeny if the crust becomes unstable.[1]

There are two primary mechanisms at work in an orogenic collapse: excess gravitational potential energy and heat flow into the thickened crust. Overthickened crust can become brittle and begin collapsing and spreading under its own weight. The added weight from the thickened crust also causes it to sink deeper into the mantle, where additional heat can flow into the crust. The added heat softens the rock and makes it flow more easily, which can allow material in deeper sections to move up into thinner areas via buoyancy forces, reducing the total thickness.[1] Orogens can also be destroyed by eduction and erosion, but these processes are not necessarily associated with orogenic collapse.[2] It has been argued that extension during orogenic collapse is a more effective mechanism of lowering mountains than erosion.[4]

Models

Orogenic collapse can occur under different circumstances

Fixed-boundary collapse

A fixed-boundary collapse is the breakdown of the brittle upper crust, and occurs when crust has overthickened while tectonic forces are still active. Flow in the lower crust may or may not occur when this happens. This can lead to exhumation of buried features.[2][1]

Free-boundary collapse

Free-boundary collapse occurs when tectonic forces have been released and the thickened crust is free to move. This results in both the extension of the surface crust and flow of the lower crust to thinner regions. The surface expression of the extension can include extensive normal faulting.[1][2] This type of deformation has been compared to leaving a piece of Camembert cheese out overnight - as the cheese starts to sag and spread, the rind will eventually crack and split.[5]

Examples

Caledonian Orogeny

The Scandinavian Caledonides is an example of an orogeny and mountain chain that reached heights of 8–9 km and then collapsed in the Devonian, forming major extensional structures such as the Nordfjord-Sogn Detachment.[6] The collapse was such that the modern Scandinavian Mountains do not owe their height to the former orogeny but to other processes that occurred in the Cenozoic.[7][8]

Basin and Range Province

The Basin and Range region of the Western United States was previously a high plateau within the American Cordillera, which has since been extended and thinned. The characteristic topography is caused by the crust breaking up into fault blocks as a result of the extension. The exact cause of the extension is debated, though it is likely related to the transition from a subduction zone to a transform boundary between the North American and Pacific plates, as well as possible mantle upwelling.[9][10]

Aegean Sea Plate

The Aegean Sea Plate is a section of continental crust which has been thinned, and is considered a high plateau between the Mediterranean and the Black Sea. The northern part of the plate underwent the Aegean Orogeny (c. 70 - 14 Ma), followed by crustal extension and thinning due to slab rollback of the African Plate.[11]

Variscan Orogeny

The Variscan (or Hercynian) orogeny was a result of the collision between the Laurussia and Gondwana plates during the formation of Pangaea. This resulted in a high plateau of thickened crust. c. 345 - 310 Ma, the northward subducting slab began retreating southward, resulting in the thickened crust beginning to thin due to a combination of gravitational collapse, fault detachment, and softening of the crust due to added heat.[12][13]

Tibetan Plateau

Although the Tibetan Plateau is in a primarily compressional environment due to the collision of the Indian and Eurasian plates, it is also experiencing east-west extension which began c. 14 Ma.[14][15][16] The primary cause of this extension is likely gravitational collapse of the plateau due to excess gravitational potential energy, as well as possible basal shearing as the Indian plate subducts under Tibet.[17][18]

See also

References

  1. 1 2 3 4 5 Selverstone, Jane (May 2005). "Are the Alps collapsing?". Annual Review of Earth and Planetary Sciences. 33: 113–132. Bibcode:2005AREPS..33..113S. doi:10.1146/annurev.earth.33.092203.122535 – via ResearchGate.
  2. 1 2 3 4 Adamuszek, Marta (2013-07-28). "Lecture - Orogenic Collapse". YouTube.
  3. ↑ Dai, Liming; Li, Sanzhong; Li, Zhong-Hai; Somerville, Ian; Liu, Xiaochun (2018-02-09). "Post-orogenic unrooting and collapse". www.mantleplumes.org. Archived from the original on 2021-12-11. Retrieved 2021-12-10.
  4. ↑ Dewey, J.F.; Ryan, P.D.; Andersen, T.B. (1993). "Orogenic uplift and collapse, crustal thickness, fabrics and metamorphic phase changes: the role of eclogites". Geological Society, London, Special Publications. 76 (1): 325–343. Bibcode:1993GSLSP..76..325D. doi:10.1144/gsl.sp.1993.076.01.16. S2CID 55985869.
  5. ↑ Nance, Damian (2014-03-24). "What is Orogenic Collapse?". Oxford University Press.
  6. ↑ Johnston S., Hacker B.R. & Ducea M.N. (2007). "Exhumation of ultrahigh-pressure rocks beneath the Hornelen segment of the Nordfjord-Sogn Detachment Zone, western Norway" (PDF). Bulletin of the Geological Society of America. 119 (9–10): 1232–1248. Bibcode:2007GSAB..119.1232J. doi:10.1130/B26172.1.
  7. ↑ Gabrielsen, Roy H.; Faleide, Jan Inge; Pascal, Christophe; Braathen, Alvar; Nystuen, Johan Petter; Etzelmuller, Bernd; O'Donnel, Sejal (2010). "Latest Caledonian to Present tectonomorphological development of southern Norway". Marine and Petroleum Geology. 27 (3): 709–723. Bibcode:2010MarPG..27..709G. doi:10.1016/j.marpetgeo.2009.06.004.
  8. ↑ Green, Paul F.; Lidmar-Bergström, Karna; Japsen, Peter; Bonow, Johan M.; Chalmers, James A. (2013). "Stratigraphic landscape analysis, thermochronology and the episodic development of elevated, passive continental margins". Geological Survey of Denmark and Greenland Bulletin. 30: 18. doi:10.34194/geusb.v30.4673. Archived from the original on 24 September 2015. Retrieved 30 April 2015.
  9. ↑ Cassel, Elizabeth J.; Breecker, Daniel O.; Henry, Christopher D.; Larson, Toti E.; Stockli, Daniel F. (Nov 2014). "Profile of a paleo-orogen: High topography across the present-day Basin and Range from 40 to 23 Ma". Geology. 42 (11): 1007–1010. Bibcode:2014Geo....42.1007C. doi:10.1130/G35924.1. ISSN 1943-2682.
  10. ↑ Liu, Mian; Shen, Yunqing (April 1998). "Crustal collapse, mantle upwelling, and Cenozoic extension in the North American Cordillera". Tectonics. 17 (2): 311–321. Bibcode:1998Tecto..17..311L. doi:10.1029/98tc00313. ISSN 0278-7407.
  11. ↑ Searle, Michael P.; Lamont, Thomas N. (2020-03-03). "Compressional origin of the Aegean Orogeny, Greece". Geoscience Frontiers (published 2020-08-07). 13 (2): 101049. doi:10.1016/j.gsf.2020.07.008.
  12. ↑ Vanderhaeghe, Olivier; Laurent, Oscar; Gardien, Véronique; Moyen, Jean-François; Gébelin, Aude; Chelle-Michou, Cyril; Couzinié, Simon; Villaros, Arnaud; Bellanger, Mathieu (2020-09-23). "Flow of partially molten crust controlling construction, growth and collapse of the Variscan orogenic belt: the geologic record of the French Massif Central". Bulletin de la Société Géologique de France. 191 (1): 25. doi:10.1051/bsgf/2020013. ISSN 0037-9409.
  13. ↑ Vacek, František; Žák, Jiří (March 2019). "A lifetime of the Variscan orogenic plateau from uplift to collapse as recorded by the Prague Basin, Bohemian Massif". Geological Magazine. 156 (3): 485–509. Bibcode:2019GeoM..156..485V. doi:10.1017/S0016756817000875. ISSN 0016-7568. S2CID 133712817.
  14. ↑ Ni, James; York, James E. (1978). "Late Cenozoic tectonics of the Tibetan Plateau". Journal of Geophysical Research. 83 (B11): 5377. Bibcode:1978JGR....83.5377N. doi:10.1029/jb083ib11p05377. ISSN 0148-0227.
  15. ↑ Yin, An; Kapp, Paul A.; Murphy, Michael A.; Manning, Craig E.; Mark Harrison, T.; Grove, Marty; Lin, Ding; Xi-Guang, Deng; Cun-Ming, Wu (1999-09-01). "Significant late Neogene east-west extension in northern Tibet". Geology. 27 (9): 787–790. Bibcode:1999Geo....27..787Y. doi:10.1130/0091-7613(1999)027<0787:SLNEWE>2.3.CO;2. ISSN 0091-7613.
  16. ↑ Blisniuk, Peter M.; Hacker, Bradley R.; Glodny, Johannes; Ratschbacher, Lothar; Bi, Siwen; Wu, Zhenhan; McWilliams, Michael O.; Calvert, Andy (2001-08-01). "Normal faulting in central Tibet since at least 13.5 Myr ago". Nature. 412 (6847): 628–632. doi:10.1038/35088045. ISSN 1476-4687. PMID 11493918. S2CID 4349309.
  17. ↑ Liu, Mian; Yang, Youqing (2003-08-01). "Extensional collapse of the Tibetan Plateau: Results of three-dimensional finite element modeling". Journal of Geophysical Research: Solid Earth. 108 (B8): 2361. Bibcode:2003JGRB..108.2361L. doi:10.1029/2002JB002248. ISSN 2156-2202.
  18. ↑ Guo, Xiaoyu; Gao, Rui; Zhao, Junmeng; Xu, Xiao; Lu, Zhanwu; Klemperer, Simon L.; Liu, Hongbing (2018-10-01). "Deep-seated lithospheric geometry in revealing collapse of the Tibetan Plateau". Earth-Science Reviews. 185: 751–762. Bibcode:2018ESRv..185..751G. doi:10.1016/j.earscirev.2018.07.013. ISSN 0012-8252.
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