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Deposition of continental shelf sediments (the Yaeyama Group) took place in Southern Ryukyu, which at the time was stable and had no crustal movement, during early Miocene.<ref name=":1" /><ref name=":6" /><ref name=":21">{{cite journal |last1=Ujiié |first1=H. |title=Early Pleistocene birth of the Okinawa Trough and Ryukyu Island Arc at the northwestern margin of the Pacific: evidence from Late Cenozoic planktonic foraminiferal zonation |journal=Palaeogeography, Palaeoclimatology, Palaeoecology |date=1994 |volume=108 |issue=3–4 |pages=457–474 |doi=10.1016/0031-0182(94)90246-1|bibcode=1994PPP...108..457U }}</ref> After a cessation of subduction around 10–6 Ma, the Philippine Sea Plate resumed subducting since the late Miocene (about 6 Ma), leading to back-arc spreading of the Okinawa Trough.<ref name=":22">{{cite journal |last1=Kamata |first1=H. |last2=Kodama |first2=K. |title=Tectonics of an arc-arc junction: an example from Kyushu Island at the junction of the Southwest Japan Arc and the Ryukyu Arc |journal=Tectonophysics |date=1994 |volume=233 |issue=1–2 |pages=69–81 |doi=10.1016/0040-1951(94)90220-8|bibcode=1994Tectp.233...69K }}</ref> Initial rifting of the northern Okinawa Trough may have caused a counterclockwise rotation in Northern Ryukyu and southern Kyushu after 6 Ma.<ref name=":22" /> Meanwhile, paleomagnetic data record a clockwise rotation of Southern Ryukyu after 10 Ma.<ref name=":17" /> [[Reflection seismology|Seismic reflection]] surveys indicate initial rifting of the southern part of the Okinawa Trough in the early Pleistocene, which gave rise to distinct tectonic processes, i.e., [[sedimentation]], crustal doming, [[erosion]], and [[Tectonic subsidence|subsidence]].<ref name=":3" /> The emergence of the Ryukyu Arc, together with the subsidence of the Okinawa Trough, may have occurred in the late Pleistocene (1.7–0.5 Ma) after the development of the Shimajiri Group and before that of the Ryukyu Group.<ref name=":21" /> The back-arc rifting and associated sedimentation in the southern Okinawa Trough have continued since 2 Ma.<ref name=":3" />
A study following the 2018 Hualien earthquake sequence show that the Ryukyu Arc may be kinematically connected to the northern Central Range in Taiwan. Shallow earthquake data shows that the offset in the northern Central Range follows the strike of the Ryukyu Arc, not the Longitudinal Fault Valley which is the suture between the Philippine Sea Plate and the Eurasian Plate, east out into the sea. Additionally, GPS data shows that the northern Central Range follows the motion of the Ryukyu arc to the south-east as opposed to the west like the rest of the mountain range.<ref>{{Cite journal |last=Jian |first=Pei‐Ru |last2=Liang |first2=Wen‐Tzong |last3=Kuo |first3=Ban‐Yuan |date=September 2022 |title=Three‐Dimensional Stress Model of the Collision‐Subduction Junction East of Taiwan: Implications for the Decoupling of the Luzon Arc During Subduction |url=https://agupubs.onlinelibrary.wiley.com/doi/10.1029/2022JB024054 |journal=Journal of Geophysical Research: Solid Earth |language=en |volume=127 |issue=9 |doi=10.1029/2022JB024054 |issn=2169-9313|url-access=subscription }}</ref>
==See also==
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