Editing Subduction (section)

===End of subduction===
Subduction can continue as long as the oceanic lithosphere moves into the subduction zone. However, the arrival of buoyant [[continental lithosphere]] at a subduction zone can result in increased coupling at the trench and cause plate boundary reorganization. The arrival of continental crust results in ''[[continental collision]]'' or ''[[terrane]] [[Accretion (geology)|accretion]]'' that may disrupt subduction.{{sfn|Stern|2002|pp=6-7}} Continental crust can subduct to depths of {{cvt|250|km}} where it can reach a point of no return.<ref>{{cite journal |last1=Ernst |first1=W. G. |title=Metamorphism, partial preservation, and exhumation of ultrahigh-pressure belts |journal=Island Arc |date=June 1999 |volume=8 |issue=2 |pages=125–153 |doi=10.1046/j.1440-1738.1999.00227.x|bibcode=1999IsArc...8..125E |s2cid=128908164 }}</ref>{{sfn|Stern|2002|p=1}} Sections of crustal or intraoceanic arc crust greater than {{cvt|15|km}} in thickness or oceanic plateau greater than {{cvt|30|km}} in thickness can disrupt subduction. However, island arcs subducted end-on may cause only local disruption, while an arc arriving parallel to the zone can shut it down.{{sfn|Stern|2002|pp=6-7}} This has happened with the [[Ontong Java Plateau]] and the [[Vitiaz Trench]].<ref>{{cite journal|last1=Cooper |first1=P. A. |last2=Taylor |first2=B. |title=Polarity reversal in the Solomon Islands arc |journal=Nature |volume=314 |pages=428–430 |year=1985 |issue=6010 |doi=10.1038/314428a0 |bibcode=1985Natur.314..428C |s2cid=4341305 |url=https://www.nature.com/articles/314428a0.pdf?origin=ppub |access-date=4 December 2020}}</ref>