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rifting/stretching period ends, this shallow asthenosphere gradually cools back into mantle lithosphere over a period of many tens of millions of years. Because mantle lithosphere is denser than asthenospheric mantle, this cooling causes subsidence. This gradual subsidence due to cooling is known as "thermal subsidence".
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have short-lived subsidence that forms from transtensional strike-slip faults. Moderate strike-slip faults create extensional releasing bends and opposing walls pull apart from each other. Normal faults occur, inducing small scale subsidence in the area, which ceases once the fault stops propagating.
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occur at failed rifts, where continental crust does not completely split. Similar to the lithospheric heating that occurs during the formation of passive margins, subsidence occurs due to heated lithosphere sagging as spreading occurs. Once tensional forces cease, subsidence continues due to cooling.
214:, interaction of deformation around the edge of the basin and deep earth dynamics. The Illinois basin and Michigan basin are examples of intracontinental basins. Extensive swamps are sometimes formed along the shorelines of these basins, leading to the burial of plant matter that later forms coal.
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sheets that form toward the undeformed continental crust. They form as an isostatic response to an orogenic load. Basin growth is controlled by load migration and corresponding sedimentation rates. The broader a basin is, the greater the subsidence is in magnitude. Subsidence is increased in the
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is thinner than adjacent crust and subsides to create an accommodation space. Accumulation of non-marine sediment forms alluvial fans in the accommodation space. As rifting proceeds, listric fault systems form and further subsidence occurs, resulting in the creation of an ocean basin. After the
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adjacent basin as the load migrates further into the foreland, causing subsidence. Sediment eroded from the fold thrust is deposited in the basin, with thickening layers toward the thrust belt and thinning layers away from the thrust belt; this feature is called differential subsidence.
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Lithospheric stretching/thinning during rifting results in regional necking of the lithosphere (the elevation of the upper surface decreases while the lower boundary rises). The underlying asthenosphere passively rises to replace the thinned mantle lithosphere. Subsequently, after the
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or orogenic processes, or loading, causes crustal depression and subsidence. Sediments accumulate at the lowest elevation possible, in accommodation spaces. The rate and magnitude of sedimentation controls the rate at which subsidence occurs. By contrast, in
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is a zone of depression in the sea floor. Extensional faulting due to relative motion between the accretionary prism and the volcanic arc may occur. Abnormal cooling effects due to the cold, water-laden downgoing plate as well as crustal thinning due to
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Intracontinental basins are large areal depressions that are tectonically inactive and not near any plate boundaries. Multiple hypotheses have been introduced to explain this slow, long-lived subsidence: long-term cooling since the breakup of
427:
Ceramicola, S.; Stoker, M.; Praeg, D.; Shannon, P.M.; De Santis, L.; Hoult, R.; Hjelstuen, B.O.; Laberg, S.; Mathiesen, A. (2005). "Anomalous
Cenozoic subsidence along the 'passive' continental margin from Ireland to mid-Norway".
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Successful rifting forms a spreading center like a mid-ocean ridge, which moves progressively further from coastlines as oceanic lithosphere is produced. Due to this initial phase of rifting, the crust in a
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573:
Heine, Christian; Dietmar MĂĽller, R.; Steinberger, Bernhard; Torsvik, Trond H. (2008). "Subsidence in intracontinental basins due to dynamic topography".
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These fault systems allow the region to stretch, while also decreasing its thickness. A thinner crust subsides relative to thicker, undeformed crust.
665:
Mascle, Alain; PuigdefĂ bregas, Cai (1998). "Tectonics and sedimentation in foreland basins: Results from the
Integrated Basin Studies project".
610:"Polyphase tectonic subsidence evolution of the Vienna Basin inferred from quantitative subsidence analysis of the northern and central parts"
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Lee, E.Y., Novotny, J., Wagreich, M. (2019) Subsidence analysis and visualization: for sedimentary basin analysis and modelling, Springer.
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cessation of rifting, cooling causes the crust to further subside, and loading with sediment will cause further tectonic subsidence.
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These settings are not tectonically active, but still experience large-scale subsidence because of tectonic features of the crust.
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between the subducting oceanic lithosphere and the overriding continental plate. Between this wedge and the associated
62:. Three mechanisms are common in the tectonic environments in which subsidence occurs: extension, cooling and loading.
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processes, mountain building creates a large load on the Earth's crust, causing flexural depressions in adjacent
526:"Numerical Modelling to Evaluate Sedimentation Effects on Heat Flow and Subsidence during Continental Rifting"
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Cooling occurs after the fault fails to propagate further following the crustal thinning via normal faulting.
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Tectonic subsidence can occur in these settings as the plates collide against or under each other.
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Basin analysis and modeling of the burial, thermal and maturation histories in sedimentary basins
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Xie, Xiangyang; Heller, Paul (2006). "Plate tectonics and basin subsidence history".
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brought about subsidence on a large scale in a variety of environments, including
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as sedimentary material is scraped off the subducting oceanic plate, forming an
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McKenzie, D (1978). "Some remarks on the development of sedimentary basins".
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Tectonic subsidence can occur in these environments as the crust thinning.
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Where the lithosphere undergoes horizontal extension at a normal fault or
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608:Lee, Eun Young; Wagreich, Michael (2017-03-01).
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524:Kim, Yeseul; Huh, Min; Lee, Eun Young (2020).
197:Pull-apart basin created by strike-slip faults
16:Sinking of the Earth's crust on a large scale
575:Physics of the Earth and Planetary Interiors
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123:Weight causes crustal flexure and subsidence
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322:are flexural depressions created by large
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79:Normal faults extending crust through
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38:and accommodation spaces produced by
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481:Earth and Planetary Science Letters
344:Makhous, M.; Galushkin, Y. (2005).
205:Cross section of a pull-apart basin
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350:. Editions TECHNIP. p. 66.
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450:10.1016/j.marpetgeo.2005.04.005
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58:, intercontinental basins and
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687:10.1144/GSL.SP.1998.134.01.02
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511:10.1016/0012-821X(78)90071-7
430:Marine and Petroleum Geology
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551:10.3390/geosciences10110451
189:Formation of passive margin
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595:10.1016/j.pepi.2008.05.008
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635:10.1007/s00531-016-1329-9
468:10.1007/978-3-319-76424-5
136:The adding of weight by
493:1978E&PSL..40...25M
181:Intracontinental basins
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304:may also be at work.
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173:Tectonically inactive
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107:) or by a system of
679:1998GSLSP.134....1M
626:2017IJEaS.106..687L
587:2008PEPI..171..252H
542:2020Geosc..10..451K
442:2005MarPG..22.1045C
280:Volcanic arc system
20:Tectonic subsidence
293:accretionary prism
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163:Subduction erosion
157:Subduction erosion
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34:. The movement of
436:(9–10): 1045–67.
357:978-2-7108-0846-6
265:Pull-apart basins
260:Pull-apart basins
60:pull-apart basins
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109:listric faults.
99:(which creates
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56:foreland basins
52:fore-arc basins
44:passive margins
26:of the Earth's
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233:passive margin
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161:Main article:
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361:. Retrieved
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302:underplating
297:volcanic arc
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168:Environments
151:lithospheric
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673:(1): 1–28.
536:(11): 451.
530:Geosciences
363:18 November
324:fold thrust
252:Collisional
218:Extensional
331:References
245:Aulacogens
240:Aulacogens
66:Mechanisms
48:aulacogens
695:130915307
644:1437-3262
560:2076-3263
497:CiteSeerX
71:Extension
709:Category
652:54965303
287:form in
147:orogenic
40:faulting
675:Bibcode
622:Bibcode
583:Bibcode
538:Bibcode
489:Bibcode
438:Bibcode
153:crust.
142:erosion
132:Loading
115:Cooling
105:grabens
87:systems
24:sinking
22:is the
693:
650:
642:
558:
499:
354:
212:Pangea
101:horsts
85:graben
691:S2CID
648:S2CID
140:from
81:horst
32:geoid
28:crust
640:ISSN
556:ISSN
365:2011
352:ISBN
103:and
83:and
683:doi
671:134
630:doi
618:106
591:doi
579:171
546:doi
507:doi
464:doi
446:doi
405:doi
401:121
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