The present-day stress field along the Northwest Pacific Wadati-Benioff zone constrained by focal mechanisms of moderate earthquakes

Abstract

The present-day stress field in the northwest Pacific Wadati-Benioff Zone (WBZ) has been investigated on the basis of earthquake focal mechanism catalog covering the period from 2012 to 2021. Our catalog contains 201 focal mechanism solutions (Mw 4.0–5.9) compiled from the F-net network along three profiles (southern Kurile trench, central Japan trench and northern Izu-Bonin trench). According to the spatial variations in the stress regimes, we outlined 12 subvolumes for three profiles. Our results present that the maximum compressive stress is, slab-normal in trench-outer rise regions and nearly strike-normal and sub-horizontal in the depth range 0–70 km. At intermediate depths, a two-planar stress pattern is observed (70–200 km) in southern Kurile and central Japan trench WBZ, with the maximum compressive stress closely parallel to the slab in upper plane and slab-normal in lower plane, respectively. However, the southern Kurile trench WBZ exposes an extension stress regime in 200–300 km depth range. At depths below 300 km, northern Izu-Bonin trench WBZ shows a stress regime of pure compression. We infer the dominant forces may be the slab blending in the shallow trench-outer rise regions, slab pull and ridge push at shallow depths, and the slab resistance provided by the mantle to the penetration of the slab at deep depths. Whereas the two-planar stress pattern may be caused by the unbending of the slab, and the unusual stress state along the junction of the trench WBZ at intermediate depths may be influenced by lateral deformation due to increasing slab’s dip.

Introduction

Subduction zones are home to the most seismically active faults on Earth (Hayes et al., 2018). The Northwest Pacific subduction zone, located at the eastern edge of the Eurasian continent, is one of the most typical subduction zones in the world (Figure 1A) Schellart et al., 2007; Sandiford et al., 2020). At the Northwest Pacific margin, the Pacific plate is subducting west-northwestward the North American plate from the Kuril and Japan trenches at a rate of ∼8.2–9.2 cm/yr, and meanwhile subducting beneath the Philippine Sea plate at ∼5.5 cm/yr (Figure 1A) (Seno et al., 1993; DeMets et al., 1994; Schellart et al., 2007; Wei et al., 2015; Gong et al., 2021). As a product of the mutual subduction collision between different plates, numerous earthquakes (Figure 1B) occurred on the subducting Pacific slab and formed a clear Wadati-Benioff Zone (WBZ) that extends down to the mantle transition zone. Besides, the Northwest Pacific subduction zone has a typical “trench-arc-basin” system with magmatic activities and regional metamorphism (Forsyth and Uyedaf, 1975; Schellart et al., 2007; Liu et al., 2017; Yang et al., 2018; Liu et al., 2022). Such complex and intense tectonics has characterized this region with a complicated stress state.

FIGURE 1

Knowledge of the crustal stress field is a prerequisite for understanding the kinematics and distribution of continental deformation (Konstantinou et al., 2017; Liu et al., 2021). Focal mechanism solutions (FMS) of earthquakes and their spatial distributions play a key role in evaluating tectonic/local stress fields (Townend and Zoback, 2006; Terakawa and Matsu’ura, 2010; Saito et al., 2018; Song et al., 2022). Many scholars have carried out a series of stress field analyses in the Pacific WBZ based on the spatial variation of the stress regimes. The stress models have been proposed in previous studies such as 1) the stress state within the subducting plate varies with the geotectonic position and thrust depth (e.g., Yoshida et al., 2015; Maeda et al., 2020; Gong et al., 2021); 2) the stress pattern in Kurile trench WBZ and Japan trench WBZ with the down-dip compression in the upper plane and down-dip tension in the lower plane at intermediate-depth (e.g., Hasegawa et al., 1979; Kita et al., 2010; Reynard et al., 2010; Florez and Prieto, 2019) and 3) the non-parallel directional stress states to slab subduction in some shallow and deep depth (e.g., Christova, 2015; Li and Chen, et al., 2019). These efforts enriched our recognition of the shape and dynamics processes of subducting plate. The present-day stress field, however, remains highly controversial along the Northwest Pacific WBZ (especially double seismic zone), which may be attributable to the different time periods of data collection, the various FMS datasets, and different evaluation methods used. In addition, it remains enigmatic whether the stress field characteristics are consistent between different trenches (e.g., Kuril, Japan, and Izu-Bonin) within the Northwest Pacific subduction system.

To address the above questions, we accurately inverted the Centroid Moment Tensor of moderate earthquakes (Mw 4.0–5.9) and established a new high-quality dataset of FMS to investigate the stress field along the Northwest Pacific WBZ. Combined with previous geological and geophysical analysis, we aim to provide a more robust comparative analysis of the stress field at the different depths of trench WBZ and tectonic position. Our findings provide new insight into stress states and intrinsic dynamical mechanisms along the WBZ in southern Kuril, central Japan, and northern Izu-Bonin trenches.

Data and method

Dataset

For this study, we used seismic waveform data that have been recorded by the regional broadband stations of F-net (Okada et al., 2004; Kimura et al., 2015; NIED, 2019) in the time span between 2012 and 2021 (Figure 1A). A total of 201 earthquakes with 4.0 ≤ Mw < 6.0 were collected along the southern Kurile arc, the central Japan arc, and the northern Izu-Bonin arc (Figure 3A; Table 1). Accordingly, we eliminated all the earthquakes above Mw 6.0, since large earthquakes can have important effects on the short-term stress field and cause stress field deviation (Huang et al., 2011; Yoshida et al., 2012; Yoshida et al., 2016a, 2016b; Hardebeck and Okada, 2018; Sheng and Meng, 2020). Meanwhile, indicated by the distribution of the epicenters from ISC earthquake catalogue (http://ds.iris.edu), seismic profiles with widths of 60–100 km were firstly selected with Mw greater than 4.0 for a period between 1 January2017 and 31 December 2021. Due to the lack of seismic events at depth range 70–180 km in profile A-A’ and profile B-B’, we then expanded the geographic width of the profile and extended the time interval (Table 1). In addition, the principles of seismic profile selection are to cover as many intermediate to deep source earthquakes as possible, and we excluded seismic events that were clearly far from the subduction zone based on their epicenter distribution. Afterwards, we inverted the FMS via these data and the following method.

Focal mechanism calculation

We utilize the Mttime software to determine FMS of selected earthquakes (Chiang, 2019). Mttime is a procedure developed for time domain inversion of full seismic waveform data to obtain the Centroid Moment Tensor. This technique employs a time-domain, generalized least squares inversion method (Minson and Dreger, 2008), and the details of the procedure are described in previous work (e.g., Dreger,2003; Chiang et al., 2016). The waveforms were firstly instrument corrected to ground displacement, rotated to the great-circle path, decimated to one sample per second and filtered between 0.05 and 0.2 Hz. Then, after constructing the velocity model, synthetic seismograms were generated using the frequency-wavenumber integration method through the “Computer Programs in Seismology” software package proposed by Herrmann (2013). The same filtering and down-sampling parameters are applied to the synthetic seismograms. Finally, the FMS were estimated according to the maximum variance reduction (VR) percentage between the observed waveforms and synthetic data. In the step of generating synthetic seismograms, we adopted a one-dimensional (1-D) velocity structure model (Table 2) derived from NIED (https://www.fnet.bosai.go.jp/faq/) and Kubo et al. (2002). We set searching step to 5–10 km firstly when conduct moment tensor inversion, and then we perform the inversion again around optimal solution of the initial inversion and set searching step to 1 km. The inversion method also allows for small time shifts between the data and synthetic seismograms to compensate for uncertainties in origin time, location, and velocity structure (Pasyanos and Chiang, 2020). The depth with the optimum fit is taken as an estimate for focal depth, and the corresponding source mechanism provides an estimate for the moment tensor. The results are demonstrated in the form of the double couple component with the scalar moment (Mo), FMS depth, strike, dip, and rake.

Stress field inversion

One of the challenges in stress field determination from FMS is the ambiguous choice of a fault plane from the two nodal planes. Compared with previous stress field inversion (Gephart and Forsyth, 1984; Michael, 1984, 1987; Zoback, 1992; Delvaux and Barth, 2010), we used an updated iterative stress inversion method based on the Mohr-Coulomb failure criterion, for identifying the fault plane based on evaluating the fault instability (Michael, 1984, 1987; Vavryčuk, 2011, 2014). The iterative joint stress inversion can be run using the open STRESSINVERSE code written in Python available at http://www.ig.cas.cz/stress-inverse. Random bootstrap uncertainty assessments using 2,000 re-samplings of the original input are performed to calculate uncertainties with 95% confidence level. The stress inversion allows us to estimate the orientation of the principal stress axes and the shape ratio , where are the principal stresses. The value of R estimates the magnitude of the intermediate principal stress (σ₂) relative to the maximum (σ₁) and the minimum (σ₃) principal stresses. When R = 0, σ₃ remains relatively stable, σ₁ and σ₂ rotate freely in the plane perpendicular to σ₃, and both are in compression; when R = 0.5, the σ₁, σ₂ and σ₃ are relatively stable; When R = 1, σ₁ is relatively stable, σ₃ and σ₂ are free to rotate in the plane perpendicular to σ₁, and both are in tension (Guiraud et al., 1989; Wan et al., 2011; Cui et al., 2019). Furthermore, we evaluate the relative homogeneity of the regional stress field by the average misfit angle β between the observed and predicted slip directions of the focal mechanisms (Michael et al., 1990; Michael, 1991; Sheng and Meng, 2020). Michael, (1991) found that this requirement can be satisfied when β is <∼35–45°, assuming that the focal mechanism error is on the order of ∼10–20°. In this paper, considering the accuracy of FMS, we strictly set the lower limit of β as 35°. When β ≤ 35°, we suggest the stress field to be homogenous.

Results

We obtained a total of 201 FMS in our study area, among them, the number of solutions in profiles A-A’, B-B’, and C-C’ are 42, 96, and 63 respectively (Figure 4; Table 3). The depths of all events range from 5 to 450 km (Table 3; Supplementary Table S1). In the waveform inversion, we conducted the inversion quality by the number of stations used, the percentage of double-couple (DC) and VR between the observed waveforms and synthetic data. We excluded the data that the number of stations used for inversion less than 3 and the VR< 0.5. Figure 2 shows an example of earthquake waveform fitting using the Mttime technology. This earthquake event occurred on 20 June 2021 in profile A-A’ (Figure 1B). The upper panel shows the waveforms fitting between vertical, radial and tangential components of waves. The robust and reliable results show high VR and DC% value, with the number of stations used for inversion more than 3. The lower panel shows that the FMS depth is constrained at 160 km, while the magnitude is Mw 5.45. The same procedure is used to obtain FMS for the remaining earthquakes in the three profiles. All FMS we conducted are available in Supplementary Material (Supplementary Table S1). The distribution of the FMS in this study area is projected into Figure 3.

FIGURE 2

FIGURE 3

According to the spatial variations in the stress regimes, we divided them into 12 WBZ subvolumes for three profiles (Figure 4; Supplementary Table S1). The principles of classification are as follows.

FIGURE 4

Firstly, Rb0 and Rc0 were outlined separately since they are located in the region of trench-outer rise, where a subducting oceanic plate begins to flex and descends into the trench (Lefeldt and revemeyer, 2008; Moscoso and Grevemeyer, 2015; Hatakeyama et al., 2017). Secondly, according to Gutenberg & Richter (1954), shallow, intermediate and deep earthquakes have traditionally been defined as those in the approximately 0–70 km, 70–300 km, and above 300 km. Meanwhile, indicated by the distribution of the epicenters (Figure 5), the dips of the WBZ are not the same in different depth intervals. We can clearly see that along profile A-A’ (Figure 5A), the dip of the WBZ is about 15°at shallow depths and then turns to steeper approximately 30° at intermediate depths. Figure 5B shows that the dip of the WBZ along profile B-B’ is about 30° at shallow depth, while turn to about 60°at intermediate depths. Along profile C-C’ (Figure 5C), corresponding to the shallow, intermediate and deep depths, the dips of the WBZ are characterized by a complex change from 30° to 60°–45°. Therefore, Ra1 and Rb1 and Rc1 were defined as the shallow portion of the WBZ with depths between 0 and 70 km. However, the outline of subvolumes at intermediate depths is complex, since the possible existence of a double seismic zone at intermediate depths (e.g., Brudzinski et al., 2007; Hasegawa and Nakajima, 2017; Florez and Prieto, 2019). The outlining of WBZ subvolumes here is carried out manually, based on a detailed analysis of the orientation spatial distribution of the P and T axes of the individual earthquake FMS. Then we outlined 6 subvolumes at intermediate depths namely Ra2, Ra3, Ra4, Rb2, Rb3, Rc2. Finally, Rc3 was outlined as the deep portion (300–500 km) of the WBZ. In order to further analyze the faulting types and distribution of FMS in the study area, we categorized the data using a ternary visualization (Kaverina diagram) of the relative proportion of variations in normal, thrust, and strike-slip faulting components for the respective profiles (Figure 6).

FIGURE 5

FIGURE 6

In the trench-outer rise regions (Rb0 and Rc0), the P axes for a depth range of 5–35 km cluster around the slab normal, but the T axes, while lying in the slab plane, show a greater range of directions (Figure 4). The results are consistent with the stress inversions, showing slab normal σ₁ and slab horizontal σ₃ within its 95% confidence ranges (Figure 7; Table 3). Such stress inversions indicate that the slab plane is under a pure extensional stress regime dominated by the normal earthquakes type (Figures 6E,I).

FIGURE 7

In a shallow portion of the WBZ (Ra1 and Rb1 and Rc1), we can clearly see that the dominant faulting style is characterized by a considerable number of reverse faulting earthquakes (Figures 6A,F,J) which have steeply plunging T and gently plunging P axes.

In addition, the distribution of P and T axes at intermediate depths (70–300 km) are more complex, as well as faulting types. Notably, Double Seismic Zones existed in the shallow portion of intermediate-depth (70–180 km) of profiles A-A’ and B-B’ (Figures 4A,B). There are distinct interfaces, in which the distribution of P and T axes varies significantly. Subvolumes in the upper WBZ plane (UP), i.e., above the interfaces, were named Ra2 and Rb2, while lower WBZ plane (LP), i.e., below the interfaces, were named Ra3 and Rb3, respectively. A notable feature of Double Seismic Zones in profile A-A’ is that the Ra2 (UP) favors oblique strike-slip with a reverse component faulting, while the dominant faulting style in Ra3 (LP) is normal with a strike-slip component (Figures 6B,C). In profile B-B’, the Double Seismic Zone is characterized by reverse faulting with steeply plunging T axes in Rb2 (UP) and normal faulting with steeply plunging P axes in Rb3 (LP) (Figures 6G,H). Ra4 belongs to the deep portion of intermediate depths (200–300 km). This subvolume is dominated by the normal fault with a strike-slip component, in which the T axes cluster within the NE quadrant, and P axes scatter within the SW quadrant (Figures 4A, 6D). At deep depths (300–500 km), Rc3 is dominated by the reverse fault with the P axes clustered in NW quadrant and the T axes scattered in SE quadrant (Figures 4C, 6L).

Discussion

Table 3 lists the number of the input data, and the best-fit stress models obtained for the considered WBZ subvolumes: the directions of σ₁, σ₂, σ₃, the R-value estimate, the average misfit angle β, and depth. Obviously, most WBZ subvolumes can reflect the homogeneous stress field characteristics. However, in Rc2, the value of β exceeds the threshold reflecting the inhomogeneous stress field. Therefore, it is not meaningful to study its stress state. In the following, we analyze and discuss the stress field in four parts.

The stress field in trench-outer rise regions

As described in the above section, the Rb0 and Rc0 represent trench-outer rise regions in the Northwest Pacific plate subduction system (Figure 4). We clearly observe that most of FMS are normal-faulting type in these regions (Figures 6E,I). The stress tensors in both subvolumes are almost similar (Figure 7; Table 3), showing the slab-normal σ₁ and sub-horizontal σ₃. The shape ratios (R values) in Rb0 and Rc0 are 0.77 and 0.82, respectively, indicating a stable σ₁.

The above analysis shows that the region of shallow trench-outer rise is most likely under a pure tension regime, which is consistent with the previous studies (Emry and Wiens, 2015; Uchida et al., 2016; Gong et al., 2021). The force driving the normal-faulting in these regions is attributed to slab pull prior to subduction, which causes the elastic lithosphere bending (Hatakeyama et al., 2017; Obana et al., 2019; Contreras-Reyes et al., 2021). The shallow extensional stress regime also explains bending-related normal faults that are widely observed in such regions (e.g., Obana et al., 2019), which may play an important role in promoting water circulation in subduction zones. According to Ranero et al. (2003), a large normal fault event that ruptures the surface may provide a pathway for sea water to penetrate the mantle. The amount of water brought into the mantle is related to the maximum depth of tension fault cut into the lithosphere which is directly linked to the maximum FMS depths (Lefeldt and Grevemeyer, 2008). As a consequence, the hydrated oceanic lithosphere produces a reduction of crustal and upper mantle velocities, supporting serpentinization of the upper mantle (Lefeldt and Grevemeyer, 2008; Moscoso and Grevemeyer, 2015; Hatakeyama et al., 2017).

The stress field in double seismic zones

Double Seismic Zones are ubiquitous features of subduction zones (Brudzinski et al., 2007; Reynard et al., 2010; Florez and Prieto, 2019). Earthquakes within the subducted lithosphere cluster into two distinct layers, that eventually merge at depth (Green II et al., 2010; Hasegawa and Nakajima, 2017; Wei et al., 2017).

In Ra2 (UP), σ₁ is closely parallel to the slab, while σ₃ is NE trending with a gentle plunging (37.2°), i.e., close to in-slab all along the arc. The R value is 0.6, implying a relatively stable σ₁. In Ra3 (LP), the best-fit stress models obtained show close to slab-normal σ₁ with a steeply plunging (59.1°) and close to slab-parallel σ₃ (N2.7°E) with a gentle plunging (29.9°). The R value is 0.16, implying a very stable σ₃. Compared with the stress state in Ra2 and Ra3, the azimuth of σ₁ is rotated counter-clockwise by 90° from NWW (288.7°) in Ra2 to the SSW (198.1°) in Ra3. Our model indicates that the dominant stress regime in Ra2 and Ra3 shifts from general compression to general extension (Guiraud et al., 1989).

In Rb2 (UP), the best-fit stress models show close to slab-parallel σ₁ (286.9°), the σ₃ is close to slab-normal. The intermediate compression σ₂ is almost horizontal trending NE close to in-slab all along the arc. In Rb3 (LP), the best-fit stress models show close to slab normal σ₁ and close to slab-parallel σ₃. The intermediate compressive stress σ₂ is close to in-slab. The R value in Rb2 is 0.71 while in Rb3 is 0.69, both implying relatively stable σ₁. Our model indicates that the dominant stress regime in Ra2 is pure compression while in Ra3 is pure extension (Guiraud et al., 1989).

Overall, we find that the UP and LP have almost opposite stress states. The stress regime in UP is dominantly down-dip compression type while in LP is dominantly down-dip tension type. The findings are consistent with the typical stress model of Double Seismic Zones, which is described in the previous studies (Hasegawa et al., 1979, 1994; Christova, 2015; Li & Chen, 2019).

In the last century, several mechanisms have been proposed to explain the coexistence of parallel compression and tension of the slabs observed at Double Seismic Zones, including sagging of the plate (Sleep, 1979; Yoshii, 1979), thermoelastic stress (Fujita and Kanamori, 1981; Goto et al., 1985), and unbending of the slab (Engdahl and Scholz, 1977; Kawakatsu, 1986). However, the recent dehydration-related embrittlement of different hydrate minerals in subducted slabs is widely considered as a promising hypothesis for events of Double Seismic Zones (Reynard et al., 2010; Chernak and Hirth, 2011; Proctor and Hirth, 2015; Okazaki and Hirth, 2016). According to Faccenda et al. (2012), the Double Seismic Zones observed in many subduction zones can be explained by the formation of the Double Hydrated Zone during plate dehydration. The redistribution of fluids caused by the unbending of the plate at intermediate depths is responsible for the formation of the Double Hydrated Zone. Reynard et al. (2010) argued that the driving force that keeps slab unbending comes from the mantle flow which sustaining the slab pushes the tip of the slab forward. Our results also support the conclusion of numerical models (Reynard et al., 2010; Faccenda et al., 2012) that down-dip compression is enhanced by mantle flow opposing the dip of the slab, whereas overall downdip extension is favored by mantle flow in the same direction of the slab dip. Thus, we believe that the unbending of the slab is more likely to be the kinetic explanation for the stress state of Double Seismic Zones.

The stress field in shallow and deep portions of the Wadati-Benioff zone

The Ra1, Rb1, and Rc1 represent the shallow regions of the WBZ in Northwest Pacific plate subduction system. Overall, the reverse faults account for the majority of earthquake types (Figures 6A,F,J). The best-fit stress models show that σ₁ is sub-horizontal and strike-normal, while σ₃ is close to slab-normal, and σ₂ is close to in-slab all along the arc (Figure 7; Table 3). All the R values are higher than 0.5 (Ra1: 0.55; Ra2: 0.72; Ra3: 0.71) implying a relatively stable σ₁. A combination of the best-fit stress model and the R values indicates a stress regime of pure compression. Since the parallelism of the stress axes with the plunge of the subducted slab is the primary evidence that the earthquakes occur in the subducted slab in response to stresses within the plate (Isacks and Molnar, 1971), our results reveal that the present-day stress state of the shallow WBZ is nearly uniform across the three selected profiles. The orientation of the maximum compressive σ₁ have geomorphological expression and points to the axes of the trench, which is interpreted as the relative motion of two converging plates of lithosphere. The dominant forces acting within the shallow WBZ are related to negative buoyancy of the plate and convergence between the plates, consistent with plate pull or ridge push mechanics (Isacks and Molnar, 1971; Christova et al., 2004, 2015; Doglioni et al., 2007).

The Rc3 represents the deep portion of the slab in our study area with the depth of 320–420 km. The reverse faults also account for the majority of earthquake types (Figure 6L) which is similar to the shallow regions of the WBZ. The best-fit stress model and the R value (0.52) indicates a stress regime of pure compression with close to slab-parallel σ₁, nearly horizontal σ₂ close to in-slab and close to slab-normal σ₃ with a steeply plunge of 64.1° (Guiraud et al., 1989). Our results are consistent with the hypothesis that predominance of compression below about 300 km in several arcs, i.e., the most striking regularity in the mechanisms of deep earthquakes is the tendency of the compressional axis to parallel the local dip of the seismic zone (Isacks et al., 1968; Stauder and Mualchin, 1976; Christova, 2015). A reasonable interpretation is that there are forces on the lower portions of the slab that resist its motion. The compressive stress inside the slab will be the result of a downward-directed force applied to the upper portions of the slab and the upward-directed resisting force applied to the lower part of the slab. The cause of this resistance might be either an increase in strength in the surrounding mantle or a buoyant effect if the density of the slab were lower than that in the surrounding mantle. Our speculation agrees with the numerical models conducted by Carminati and Petricca (2010). They suggested the mantle flow drives the plate downward suffering resistance offered by the mantle to the penetration of the slab.

The stress field along the junction of the trench Wadati-Benioff zone

The junction of the Kurile and Japan arcs is expressed as a cuspate feature at the trench with a complex lithospheric structure, is known as the Hokkaido corner (Miller et al., 2006). Since the profile A-A’ (southern Kurile trench WBZ) is located here, it can be served as a window to understanding the stress characteristics of intermediate-depth earthquakes and investigating deformation of the oceanic lithosphere beneath the arc junction in this paper.

A closer look through the FMS data of Double Seismic Zones in profile A-A’, we find that more than half of them have considerate strike-slip component (Figures 6B,C) in contrast to the central Japan trench WBZ (Figures 6G,H), although the best-fit stress models are characterized with down-dip compression or down-dip tension in both the UP and LP (Figure 7A; Table 3). Going forward to the deeper at intermediate-depth, in Ra4, the best-fit stress model shows close to in-slab σ₃ and slab-normal σ₁. The R value is 0.15, indicating a general extension stress regime (Guiraud et al., 1989). However, this extensional feature revealed by best-fit stress model is inconsistent with the present-day overall stress field in northeast Japan, which is characterized by a reverse-faulting regime (Zoback, 1992; Kubo et al., 2002; Townend and Zoback, 2006).

The above two unusual stress states imply the additional forces acting at intermediate depths. The lateral deformation at intermediate depths is considered to be the more likely hypothesis (Isacks and Molnar, 1971; DeMets, 1992). Tomography imaging revealed by Miller et al. (2006) shows that a region of low-velocity depth and a distorted, buckled lower slab boundary exists at approximately 50–150 km depth beneath the Hokkaido corner, which are likely to be related to lateral deformation of the subducted Pacific plate at the arc-arc junction. The possible causes of lateral stretching are local hinge folding of the slab plate, which resulting from the increase of the slab’s dip, as well as the different subduction rate between the two trench WBZs (Katsumata, 2003). Unfortunately, the lack of enough FMS from that particular segment hurdles us to look for more finer variations in spatial stress.

Conclusion

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