Efficient adaptive mesh refinement is based on tree-structured triangular meshes (see Appendix A2). However, what the initial conditions in the subduction-initialized earthquake in Section 4 reveal are shear traction and static friction depth profiles that vary with both depth and material, with the most obvious change from sediments to oceanic crust at approximately 28 km depth (Fig. The waves from the time-independent source arrive later at the coast along y < 0 and earlier at the coast along y > 0. Large megathrust events associated with this process likely pose a major earthquake and tsunami hazard to the surrounding community, but further effort … It implements a second-order Runge–Kutta discontinuous Galerkin method on triangular grids (Cockburn & Shu 1998; Giraldo & Warburton 2008), allowing wave propagation with high accuracy. Failure analysis according to the earthquake model failure criterion (eq. This results in an underestimate of the width of the inundation corridor everywhere except in the central region inland from the coast. Le défaut responsable était le Megathrust des Aléoutiennes, un défaut inversé causé par une force de compression. Similarly, we here restrict the off-fault constitutive behaviour of the earthquake physical models to purely elastic and use a linear slip weakening friction law on-fault. Instrumentation Services (IS), The large modelled slip results from the effect of reverberating seismic waves and the chosen Poisson’s ratio, similar to the 2-D case (van Zelst et al. Megathrust earthquakes rupture preferentially along flat (low-curvature) interfaces. To correctly assess its seismic and tsunami risk, it is of fundamental importance to understand why frontal sections can rupture and produce large tsunamis, and what controls the lateral extent of earthquakes. At y = 0, the time-independent source again over predicts the peak wave height (Fig. For example, realistic representations of complex topography and bathymetry are permissible in both the earthquake and tsunami computational models, which may be critical not only for inundation modelling, but also for modelling tsunami genesis and propagation in deep water (e.g. (2011). E.H.M., T.U. Fault dip gradually increases with depth, ranging from 2.3° to 34° and averaging 14.8°. Tsunamis are generated by seafloor deformation caused by up to tens of meters of slip on a megathrust fault; however, there are other phenomena that may cause seafloor upheaval sufficient to generate large tsunamis, such as … These benchmarks include tests for steady state solutions (Resting Lake) and the inundation of coasts (Oscillating Lake, Okushiri Tsunami). Figs 17(a) and (b) compare the wave profiles from the time-independent and time-dependent sources at t = 420 s. Along y = 0, the wave pattern is similar for both sources, but the time-independent source produces a 1.1 m higher peak and this peak is advanced ahead of that in the original source (Fig. Kame et al. We also would like to recognize the exceptional editorship by Editors Gabi Laske and Duncan Agnew, and to thank the reviewers, Joao Duarte, Brittany Erickson, Duncan Agnew and one anonymous reviewer, for their collegial and constructive reviews. 2-D dynamic rupture simulations are fully coupled to the time-dependent response of water layers hosting tsunamis by Lotto et al. However, recent 3-D earthquake-tsunami models of the 2004 Sumatra earthquake reveal the sensitive trade-off between shallow fault slip and off-fault elastoplastic deformation in controlling the tsunami height (Ulrich et al. This may correspond to natural megathrust behaviour. The two-dimensional isotropic case with external source terms, Earthquake damage patterns resolve complex rupture processes, Tsunami damage detection with remote sensing: a review, Rupture to the trench: dynamic rupture simulations of the 11 March 2011 Tohoku Earthquake, Constraining shallow slip and tsunami excitation in megathrust ruptures using seismic and ocean acoustic waves recorded on ocean-bottom sensor networks, Elastic-acoustic coupling for 3D tsunamigenic earthquake simulations with ADER-DG on unstructured tetrahedral meshes, Tsunami modelling with adaptively refined finite volume methods, Numerical resolution of well-balanced shallow water equations with complex source terms, Numerical Simulations of the 1960 Chilean Tsunami Propagation and Inundation at Hilo, Hawaii, The effect of compliant prisms on subduction zone earthquakes and tsunamis. Sea surface height (ssh) from the tsunami sourced by the subduction-initialized earthquake in Scenario C at (a) the end of the earthquake, (b) after evolving for 1000 s, (c) the approximate time of first inundation and (d) the approximate time of maximum inundation. We then identify the beginning of this event as the time step when two adjacent points are at failure due to local exceeding of the failure criterion. 2011; Sun et al. Dynamic implications of geodynamic simulations validated with laboratory models, The seismic cycle at subduction thrusts: insights from seismo-thermo-mechanical models, Modeling the seismic cycle in subduction zones: the role and spatiotemporal occurrence of off-megathrust events, Modeling megathrust earthquakes across scales: One-way coupling from geodynamics and seismic cycles to dynamic rupture, Well-balanced inundation modeling for shallow-water flows with Discontinuous Galerkin schemes, Finite Volumes for Complex Applications VII – Elliptic, Parabolic and Hyperbolic Problems, Vol. Such modelling may be specifically useful to constrain earthquake rupture and tsunami generation, propagation and inundation in complex megathrust systems, producing tsunami sources accounting for, for example, the effects of the slip to the trench, dynamic interaction between different fault segments (including splay faults) and off-fault coseismic deformation. Tsunamis. The mean values are similar in both scenarios, at 3.5 km s–1 for the blind rupture and 3.7 km s–1 for the surface-breaching rupture. A 'megathrust' earthquake caused by a rupture along New Zealand's largest fault line is a question of 'when', not 'if' according to experts (pictured: graphic illustrating projected tsunami) 2 / 4 For the surface-breaching rupture, the maximum is larger at 3.3 m, but the minimum is comparable at −1.1 m. The average vertical displacement at this time is 0.6 m for the blind rupture and twice as large, at 1.2 m, for the surface-breaching event. Its scalability enables large and long dynamic rupture models. 2002; Mai & Thingbaijam 2014; Bletery et al. (2018), assessing the worst local resolution achieved, we determine the following expected maximum errors for the results with this mesh: 0.09 per cent for the rupture arrival, 7.6 per cent for the peak slip rate, and 0.8 per cent for the final slip magnitude. Setting up the earthquake model in this way ensures physical consistency of the tsunami source with characteristics of both the subduction channel and the earthquake kinematics and dynamics. Values are ported to the earthquake model at the 500 m resolution of the subduction model. Fig. Near the material contrast at 27 km depth, |$\mu _{s}^{\prime }$| and |$\mu _{d}^{\prime }$| are anomalously large due to interpolation inaccuracies near stark material contrasts (Fig. The length of the fault rupture was about 1,000 kilometers (620 miles), with an average slip of 20 meters (66 ft). The structural model and mesh for the earthquake physical model used in scenarios A and B are generated with the open-source software Gmsh (www.gmsh.info) (Geuzaine & Remacle 2009). b(x,y) = \left\lbrace \begin{array}{@{}l@{\quad }l@{}}0.05\, (x-x_0) & \text{for } x \gt x_0 \\ Despite the obliquity of convergence, active volcanism and megathrust earthquakes are also present along this margin. (6). Scenario B (surface-breaching rupture): (d) accumulated slip, (e) vertical surface displacements at 56 s (time of maximum uplift) and (f) final vertical displacements. 2000; Day et al. 6, the (filtered) source displacements of the blind rupture in Scenario A produce a smooth wave while those in Scenario B produces more abrupt initial displacements of the water column, as discussed in Section 5.1. 2019), and large megathrust events (Galvez et al. 2011; Saito et al. We look forward to continuing discussions with the earthquake and tsunami modelling communities. Megathrust earthquakes happen at subduction zones, where one tectonic plate is being pushed under another. Hasil monitoring BMKG menunjukkan bahwa zona megathrust selatan Jawa memang sangat aktif yang tampak dalam peta aktivitas kegempaannya (seismisitas). Several approaches also incorporate seismic waves into tsunami models. This results in a Poisson solid with Lame’s parameter equal to the shear modulus (λ = G). ASAGI automatically replicates or migrates the corresponding data tiles across compute nodes, which greatly simplifies the computing access to material or geographic data at a specific location. 2015, 2019). s741). However, the difference in peak height diminishes during tsunami propagation towards the beach and the inundation patterns are similar in both scenarios; inundation occurs along the same stretch of the beach and has the same run-up. 2013a,b). Stochastic Tsunami Simulation. This effect in Scenario C may be related to overprediction of the central wave peak (at y = 0) and underprediction of the wave peaks away from here. These types of differences, shown here in generic models, may be challenging to distinguish from field data, for which regional and data-driven adjustment of the scenarios may be required. The first time the coast is inundated by the tsunami from (a) the time-dependent source, (b) the time-independent source and (c) the difference (time-dependent minus time-independent). Satellite data capturing wave heights in the ocean have resolutions on the order of cm (Hayashi 2008) and data used to determine inundation areas have resolutions on the order of m to tens of m (Koshimura et al. CLOSED CAPTIONING: A .srt file is included with the download. Along a 3-D fault, we must laterally restrict this location and do so by creating a 2-D nucleation patch centred on these points at failure. Now a team of geoscientists thinks the key to understanding some of these destructive events may lie in the deep, gradual slow-slip behaviors beneath the subduction zones. 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