Abstract
Subduction initiation induced by a hot and buoyant mantle plume head is unique among proposed subduction initiation mechanisms because it does not require pre-existing weak zones or other forces for lithospheric collapse. Since recognition of the first evidence of subduction nucleation induced by a mantle plume in the Late Cretaceous Caribbean realm, the number of studies focusing on other natural examples has grown. Here, we review numerical and physical modeling and geological-geochemical studies which have been carried out thus far to investigate onset of a new subduction zone caused by impingement of a mantle plume head. As geological-geochemical data suggests that plume-lithosphere interactions have long been important - spanning from the Archean to the present - modeling studies provide valuable information on the spatial and temporal variations in lithospheric deformation induced by these interactions. Numerical and physical modeling studies, ranging from regional to global scales, illustrate the key role of plume buoyancy, lithospheric strength and magmatic weakening above the plume head on plume-lithosphere interactions. Lithospheric/crustal heterogeneities, pre-existing lithospheric weak zones and external compressional/extensional forces may also change the deformation regime caused by plume-lithosphere interaction.
Highlights
In the mid-20th century, new technologies like sonar and magnetometers provided the ability to map the seafloor and its magnetic anomalies, the basis of observations which led to the theory of plate tectonics
An important recent hypothesis is that the impingement of a new mantle plume head on the Revisiting Plume-Induced Subduction Initiation base of the lithosphere can sometimes cause a new subduction zone to form
Different mechanisms of subduction initiation have been proposed including onset of a new subduction zone along lithospheric weaknesses like transform faults zones (e.g., McKenzie, 1977; Mueller and Phillips, 1991; Hall et al, 2003; Lebrun et al, 2003; Gurnis et al, 2004; Stern 2004; Stern and Gerya, 2018), conversion of passive margins into active plate boundaries (e.g., Wilson 1966; Regenauer-Lieb et al, 2001; Nikolaeva et al, 2010; Duarte et al, 2013; Zhou et al, 2020), subduction initiation induced by pre-existing plate forces (e.g., Kemp and Stevenson, 1996; Baes et al, 2011; Levy and Jaupart, 2012; Zhong and Li, 2019) and subduction initiation induced by mantle suction flow (e.g., Lu et al, 2015; Baes and Sobolev, 2017; Baes et al, 2018)
Summary
In the mid-20th century, new technologies like sonar and magnetometers provided the ability to map the seafloor and its magnetic anomalies, the basis of observations which led to the theory of plate tectonics. Different mechanisms of subduction initiation have been proposed including onset of a new subduction zone along lithospheric weaknesses like transform faults zones (e.g., McKenzie, 1977; Mueller and Phillips, 1991; Hall et al, 2003; Lebrun et al, 2003; Gurnis et al, 2004; Stern 2004; Stern and Gerya, 2018), conversion of passive margins into active plate boundaries (e.g., Wilson 1966; Regenauer-Lieb et al, 2001; Nikolaeva et al, 2010; Duarte et al, 2013; Zhou et al, 2020), subduction initiation induced by pre-existing plate forces (e.g., Kemp and Stevenson, 1996; Baes et al, 2011; Levy and Jaupart, 2012; Zhong and Li, 2019) and subduction initiation induced by mantle suction flow (e.g., Lu et al, 2015; Baes and Sobolev, 2017; Baes et al, 2018). A short video overview of PISI can be watched at https://www.youtube. com/watch?v Hb47L8S7fMU&t 5s
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