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Journal article(2025)
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C. P. Marsman, F. C. Vossepoel, M. D’Acquisto, Y. van Dinther, L. van de Wiel, R. Govers
Geodetic data spanning different phases of the earthquake cycle offer insights into the spatiotemporal interplay between processes driving surface deformation, such as viscoelastic relaxation, afterslip, and (re)locking. However, quantifying their contributions and explaining pre- and post-earthquake displacements with a single set of rheological parameters is challenging. We set up a 2-D earthquake cycle finite element model that simulates the mantle and a thin low-viscosity shear zone with a temperature-dependent linear Maxwell or nonlinear power-law rheology. We use the ensemble smoother with multiple data assimilation to estimate ensembles of parameters describing the rheological makeup of the subduction zone. We assimilate onshore and offshore displacement time series acquired before and after the 2011 Tohoku-Oki earthquake. Our models provide a unique, robust solution using a temperature-dependent power-law rheology. The estimated creep parameters for the mantle wedge deeper than ∼50 km and sub-slab mantle align with laboratory experiments. However, different creep parameters are required for the shallow part of the mantle wedge than the deeper part to explain the observed postseismic response—highlighting the need for shallow viscoelastic relaxation. The trade-off between water fugacity and activation energy hinders their individual estimation but yields a well-constrained viscosity structure. The spatial distribution of vertical displacements as well as the temporal signature of early postseismic horizontal displacements are required to estimate individual parameters for afterslip and viscoelastic relaxation. Afterslip occurs downdip of the coseismic rupture. Near-trench landward motion during the early postseismic period is driven by elastic stress release beneath the oceanic plate and sub-slab asthenospheric flow.
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Geodetic data spanning different phases of the earthquake cycle offer insights into the spatiotemporal interplay between processes driving surface deformation, such as viscoelastic relaxation, afterslip, and (re)locking. However, quantifying their contributions and explaining pre- and post-earthquake displacements with a single set of rheological parameters is challenging. We set up a 2-D earthquake cycle finite element model that simulates the mantle and a thin low-viscosity shear zone with a temperature-dependent linear Maxwell or nonlinear power-law rheology. We use the ensemble smoother with multiple data assimilation to estimate ensembles of parameters describing the rheological makeup of the subduction zone. We assimilate onshore and offshore displacement time series acquired before and after the 2011 Tohoku-Oki earthquake. Our models provide a unique, robust solution using a temperature-dependent power-law rheology. The estimated creep parameters for the mantle wedge deeper than ∼50 km and sub-slab mantle align with laboratory experiments. However, different creep parameters are required for the shallow part of the mantle wedge than the deeper part to explain the observed postseismic response—highlighting the need for shallow viscoelastic relaxation. The trade-off between water fugacity and activation energy hinders their individual estimation but yields a well-constrained viscosity structure. The spatial distribution of vertical displacements as well as the temporal signature of early postseismic horizontal displacements are required to estimate individual parameters for afterslip and viscoelastic relaxation. Afterslip occurs downdip of the coseismic rupture. Near-trench landward motion during the early postseismic period is driven by elastic stress release beneath the oceanic plate and sub-slab asthenospheric flow.
Journal article(2023)
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M. D’Acquisto, M. W. Herman, R.E.M. Riva, R. Govers
Greater landward velocities were recorded after six megathrust earthquakes in subduction zone regions adjacent to the ruptured portion. Previous explanations invoked either increased slip deficit accumulation or plate bending during postseismic relaxation, with different implications for seismic hazard. We investigate whether bending can be expected to reproduce this observed enhanced landward motion (ELM). We use 3D quasi-dynamic finite element models with periodic earthquakes. We find that afterslip downdip of the brittle megathrust exclusively produces enhanced trenchward surface motion in the overriding plate. Viscous relaxation produces ELM when a depth limit is imposed on afterslip. This landward motion results primarily from in-plane elastic bending of the overriding plate due to trenchward viscous flow in the mantle wedge near the rupture. Modeled ELM is, however, incompatible with the observations, which are an order of magnitude greater and last longer after the earthquake. This conclusion does not significantly change when varying mantle viscosity, plate elasticity, maximum afterslip depth, earthquake size, megathrust locking outside of the rupture, or nature and location of relevant model boundaries. The observed ELM consequently appears to reflect faster slip deficit accumulation, implying a greater seismic hazard in lateral segments of the subduction zone.
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Greater landward velocities were recorded after six megathrust earthquakes in subduction zone regions adjacent to the ruptured portion. Previous explanations invoked either increased slip deficit accumulation or plate bending during postseismic relaxation, with different implications for seismic hazard. We investigate whether bending can be expected to reproduce this observed enhanced landward motion (ELM). We use 3D quasi-dynamic finite element models with periodic earthquakes. We find that afterslip downdip of the brittle megathrust exclusively produces enhanced trenchward surface motion in the overriding plate. Viscous relaxation produces ELM when a depth limit is imposed on afterslip. This landward motion results primarily from in-plane elastic bending of the overriding plate due to trenchward viscous flow in the mantle wedge near the rupture. Modeled ELM is, however, incompatible with the observations, which are an order of magnitude greater and last longer after the earthquake. This conclusion does not significantly change when varying mantle viscosity, plate elasticity, maximum afterslip depth, earthquake size, megathrust locking outside of the rupture, or nature and location of relevant model boundaries. The observed ELM consequently appears to reflect faster slip deficit accumulation, implying a greater seismic hazard in lateral segments of the subduction zone.
