Subduction polarity reversal: Difference between revisions

Revision as of 17:37, 16 April 2020

Revision as of 16:41, 3 October 2020

Line 63:

In reality, the magmatic arc is a relatively weak zone at the overriding plate because it has a thin lithosphere and is further weakened by high heat flow<ref>{{Cite journal|last=Currie|first=Claire A.|last2=Hyndman|first2=Roy D.|date=2006-08-01|title=The thermal structure of subduction zone back arcs|journal=Journal of Geophysical Research: Solid Earth|language=en|volume=111|issue=B8|pages=B08404|doi=10.1029/2005JB004024|issn=2156-2202|bibcode=2006JGRB..111.8404C}}</ref><ref>{{Cite journal|last=Currie|first=C. A|last2=Wang|first2=K|last3=Hyndman|first3=Roy D|last4=He|first4=Jiangheng|date=2004-06-30|title=The thermal effects of steady-state slab-driven mantle flow above a subducting plate: the Cascadia subduction zone and backarc|journal=Earth and Planetary Science Letters|volume=223|issue=1–2|pages=35–48|doi=10.1016/j.epsl.2004.04.020|bibcode=2004E&PSL.223...35C}}</ref> and hot fluid.<ref>{{Cite journal|last=Arcay|first=D.|last2=Doin|first2=M.-P.|last3=Tric|first3=E.|last4=Bousquet|first4=R.|last5=de Capitani|first5=C.|date=2006-02-01|title=Overriding plate thinning in subduction zones: Localized convection induced by slab dehydration|journal=Geochemistry, Geophysics, Geosystems|language=en|volume=7|issue=2|pages=Q02007|doi=10.1029/2005GC001061|issn=1525-2027|bibcode=2006GGG.....7.2007A}}</ref><ref>{{Cite journal|last=Honda|first=Satoru|last2=Yoshida|first2=Takeyoshi|date=2005-01-01|title=Application of the model of small-scale convection under the island arc to the NE Honshu subduction zone|journal=Geochemistry, Geophysics, Geosystems|language=en|volume=6|issue=1|pages=Q01002|doi=10.1029/2004GC000785|issn=1525-2027|bibcode=2005GGG.....6.1002H}}</ref> Pre-existing faults in this simulation are also common in the magmatic arc.<ref>{{Cite journal|last=Toth|first=John|last2=Gurnis|first2=Michael|date=1998-08-10|title=Dynamics of subduction initiation at preexisting fault zones|journal=Journal of Geophysical Research: Solid Earth|language=en|volume=103|issue=B8|pages=18053–18067|doi=10.1029/98JB01076|issn=2156-2202|bibcode=1998JGR...10318053T|url=https://authors.library.caltech.edu/38328/1/1998_TothGurnis_JGR.pdf}}</ref> This experiment is a successful analogy to subduction polarity reversal happening at Kamchatka in early Eocene<ref name=":54" /><ref>{{Cite journal|last=Konstantinovskaia|first=Elena A|date=2000-10-15|title=Geodynamics of an Early Eocene arc–continent collision reconstructed from the Kamchatka Orogenic Belt, NE Russia|journal=Tectonophysics|volume=325|issue=1–2|pages=87–105|doi=10.1016/S0040-1951(00)00132-3|bibcode=2000Tectp.325...87K}}</ref> and the active example at Taiwan region<ref name=":113" /><ref name=":03" /> as well as at Timor.<ref>{{cite journal|last1=Silver|first1=Eli A.|last2=Reed|first2=Donald|last3=McCaffrey|first3=Robert|last4=Joyodiwiryo|first4=Yoko|title=Back arc thrusting in the Eastern Sunda Arc, Indonesia: A consequence of arc-continent collision|journal=Journal of Geophysical Research: Solid Earth|date=1983-09-10|volume=88|issue=B9|pages=7429–7448|doi=10.1029/JB088iB09p07429|bibcode=1983JGR....88.7429S}}</ref><ref>{{Cite journal|last=Snyder|first=D. B.|last2=Prasetyo|first2=H.|last3=Blundell|first3=D. J.|last4=Pigram|first4=C. J.|last5=Barber|first5=A. J.|last6=Richardson|first6=A.|last7=Tjokosaproetro|first7=S.|date=1996-02-01|title=A dual doubly vergent orogen in the Banda Arc continent-arc collision zone as observed on deep seismic reflection profiles|journal=Tectonics|language=en|volume=15|issue=1|pages=34–53|doi=10.1029/95TC02352|issn=1944-9194|bibcode=1996Tecto..15...34S}}</ref>

[[File:Lithospheric_break-up_model_setup.svg|thumb|444x444px|A. Chemenda's Experiment setup of lithosphere break-up model: White colour indicates the oceanic plate ( Higher density) ; Brown colour indicates the continental plate ( Lower density) ;Green colour shows the pre-existing fault ; The plates represented by hydrocarbons floats at the asthenosphere represented by water.|center]][[File:Lithoshperic_break-up.gif|thumb|444x444px|The evolution diagram showing how the subduction reversal initiated by a pre-existing fault at the overriding plate. 1: Compression pushing ; 2: New slab develops with the failure of the fault ; 3: New slab penetrates ; 4: New slab breaks the old slab|center]]

== Taiwan as an active example of flipping of subduction reversal ==

[[File:Taiwan_222222.jpg|thumb|382x382px|Map of Taiwan shows the ___location of geological cross-section and the major subuductions]]

A sharp contrast of landforms in Taiwan lures many people to investigate. The northern part of Taiwan has lots ofmany flat plains such as Ilan Plain and Pingtung Plain,<ref name=":52222">{{Cite journal|last=Angelier|first=Jacques|last2=Chang|first2=Tsui-Yü|last3=Hu|first3=Jyr-Ching|last4=Chang|first4=Chung-Pai|last5=Siame|first5=Lionel|last6=Lee|first6=Jian-Cheng|last7=Deffontaines|first7=Benoît|last8=Chu|first8=Hao-Tsu|last9=Lu|first9=Chia-Yü|date=2009-03-10|title=Does extrusion occur at both tips of the Taiwan collision belt? Insights from active deformation studies in the Ilan Plain and Pingtung Plain regions|journal=Tectonophysics|series=Geodynamics and active tectonics in East Asia|volume=466|issue=3–4|pages=356–376|doi=10.1016/j.tecto.2007.11.015|bibcode=2009Tectp.466..356A}}</ref> while the southern part of Taiwan is concentrated with many high mountains like [[Yushan (mountain)|Yushan]] reaching about 3950m. This huge difference in topography is the consequence of '''the flipping of subduction polarity'''.<ref name=":132222"/> Most of models studying this phenomenon will focus on an active collision in Taiwan which appears to reveal the incipient stages of subduction reversal.<ref name=":132222"/><ref name=":03" /><ref name=":322"/><ref name=":23" /><ref name=":73" /><ref name=":93" />

The collision of N- trending Luzon arc in [[Philippine Sea Plate|Philippine Sea plate]] (PP) with E-trending [[Eurasian Plate|Eurasian plate]] (EP) started at mid-Miocene<ref name=":132222"/> forming an intra-oceanic subduction system.<ref name=":322" /><ref>{{Cite journal|last=Leat|first=P. T.|last2=Larter|first2=R. D.|date=2003-01-01|title=Intra-oceanic subduction systems: introduction|url=http://sp.lyellcollection.org/content/219/1/1|journal=Geological Society, London, Special Publications|language=en|volume=219|issue=1|pages=1–17|doi=10.1144/GSL.SP.2003.219.01.01|issn=0305-8719|bibcode=2003GSLSP.219....1L}}</ref> Taiwan was formed by this process. The south-north topographic difference in Taiwan is like a story book telling the evolution in subduction zone. The [[Philippine Sea Plate|Philippine Sea plate]] subducts below the [[Eurasian Plate|Eurasian plate]] at south-west part of WEP (Western edge of north-dipping Philippine Sea Plate),<ref name=":132222"/> and the latter overrides the former at north east part of WEP.<ref name=":132222"/> The collision between two plates started at the Northern Taiwan and propagated south with the younger region at the southern part. Each incipient stage of subduction reversal process could be studied by correlating cross-sections in various parts of Taiwan.<ref>{{Cite journal|last=Van Avendonk|first=Harm J. A.|last2=McIntosh|first2=Kirk D.|last3=Kuo-Chen|first3=Hao|last4=Lavier|first4=Luc L.|last5=Okaya|first5=David A.|last6=Wu|first6=Francis T.|last7=Wang|first7=Chien-Ying|last8=Lee|first8=Chao-Shing|last9=Liu|first9=Char-Shine|date=2016-01-01|title=A lithospheric profile across northern Taiwan: from arc-continent collision to extension|url=http://gji.oxfordjournals.org/content/204/1/331|journal=Geophysical Journal International|language=en|volume=204|issue=1|pages=331–346|doi=10.1093/gji/ggv468|issn=0956-540X|bibcode=2016GeoJI.204..331V}}</ref>