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He found that small-scale convection is able to initiate subduction in weak plates with σ y,const=0.0003 (4.4 MPa) but not in "strong" plates with σ y,const=0.0004 (5.8 MPa).
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Necessitating a strong plate, single-sided subduction is therefore harder to initiate.
This is due to strong plate coupling, as shown in Figure 4a.
In contrast, every segment appears to be with strong plate coupling for other megathrust earthquakes.
In contrast, Goto (2013) suggested strong plate coupling caused the 1911 Kikai-jima Earthquake in the northern Ryukyu Trench.
This idea agrees with strong plate coupling in that region estimated from GPS data (Nishimura et al., 2007).
The locations of these mainshocks may be related to the strong plate coupling resulting from the high resistance of the fracture zones.
Interestingly, subduction of a "strong" plate with σ y,const=0.0004 (5.8 MPa) can be initiated using the same model setup plus a free surface (Fig. 3 e).
The strong plate-internal deformation occurring in the model with a vertically fixed surface is reduced when applying a free surface and accommodated by vertical deflection of the whole plate: The plate is bending.
Significant along-strike variability is also important for the 2011 Tohoku earthquake, with segments of both weak (e.g., slow or tsunami earthquakes) and strong plate couplings located adjacent to each other.
Figures 3a and 4c also suggest a quiescence of the VLFEs around the center of strong plate coupling, which may correspond to the fact that VLF after-events were not observed off Miyagi (Matsuzawa et al. 2012).
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CEO of Professional Science Editing for Scientists @ prosciediting.com