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Insights into the long-to-intermediate-term pre-shock accelerating moment release (AMR) from the March 11, 2011, off the Pacific coast of Tohoku, Japan, M 9 earthquake

Abstract

Great earthquakes with extending rupture areas, such as the March 11, 2011, off the Pacific coast of Tohoku, Japan, M 9 earthquake, provide opportunities to inspect some details of the pre-shock moment release with the reference of the earthquake preparation and rupture processes. To this end, we investigated the cumulative seismic moment tensor for different segments of the earthquake fault. For the 3 decades time scale, pre-shock accelerating moment release (AMR) can be observed, with potential correlation with the segmentation of earthquake fault.

1. Introduction

In the assessment of long-to-intermediate-term time-dependent seismic hazards, one of the candidate models is the pre-shock accelerating moment release (AMR) model (Bufe et al., 1994; Brehm and Braile, 1998; Bowman and King, 2001) which was once related to the critical-point-like behavior of earthquake preparation (Sornette and Sammis, 1995; Bowman et al., 1998; Jaumé and Sykes, 1999; Rundle et al., 2000). Regarding this model, present results are somewhat controversial (Robinson, 2000; Chen, 2003; Wang et al., 2004; Robinson et al., 2005; Jiang and Wu, 2006a; Mignan et al., 2006; Papazachos et al., 2007; Hardebeck et al., 2008; Mignan and Giovambattista, 2008; Mignan, 2011). The main discrepancy is whether ‘precursory’ AMR exists before the ‘target’ earthquakes, and the discussion has been, to a large extent, influenced by two ambiguities in the AMR analysis. The first ambiguity is that it is the earthquake magnitude (rather than the seismic moment tensor) that is used in the calculation of the ‘moment’ release—theoretically this is not exact, since the simple use of magnitude is equivalent to summing up all the scalar seismic moments in the Kostrov (1974) method, which is intrinsically not physical. The second ambiguity is that previous studies tended to investigate the seismicity within a large area surrounding a ‘target earthquake’. In this case, the AMR behavior reflects a coarse or averaged property of the earthquake preparation process. Considering the complexity of earthquake preparation—for instance, the segmentation of earthquake faults—this average misses some important information of stress variation, if the assumption holds that AMR is related to the pre-shock stress evolution. To a large extent, these two ambiguities result from the limitation of earthquake data in use. For an earthquake less than magnitude 7, the sample of small earthquakes just within the fault zone of the ‘target’ earthquake, for checking the pre-shock AMR, is small; the seismic moment tensor dataset is even smaller, preventing a detailed and physical investigation of the pre-shock stress-related ‘moment’ release. Great earthquakes, characterized by their extending rupture areas, provide unique opportunities to overcome the above-mentioned two shortcomings (Jiang and Wu, 2005, 2006b, 2010; Mignan et al., 2006). In the present investigation related to the March 11, 2011, off the Pacific coast of Tohoku, Japan, M 9 earthquake (Lay and Kanamori, 2011; http://www.eqh.dpri.kyotou.ac.jp/src/etc/tohoku/), the seismic moment tensor data (http://www.globalcmt.org/) seems to provide some insights into the pre-shock AMR related to the earthquake preparation and rupture processes.

2. Data and Background Information

We used the Global Centroid Moment Tensor (http://www.globalcmt.org/) catalogue for the analysis, while, in principle, the analysis is also valid for other moment tensor datasets. The Gutenberg-Richter frequency-magnitude relation, together with other analyses, gives that the completeness of this catalogue for the Japan islands region is above Mw 5.2, satisfying the requirement of AMR analysis for the cutoff magnitude. As in the case of the RELM test (Field, 2007), we have considered both cases with and without de-clustering, and with and without eliminating the ‘interfering events’.

Because the earthquakes under consideration are all above Mw 5.2, we used the Gardner-Knopoff formula (Gardner and Knopoff, 1974) to identify the aftershocks, which is a simple de-clustering scheme, although less sophisticated than the ETAS model. In the AMR investigation, an ‘interfering event’ is one located near the ‘target event’, with a magnitude difference from the ‘target event’ less than 1.0 (e.g., Brehm and Braile, 1998), causing an abrupt change of the AMR curve, which is considered as an artifact in need of elimination. Focusing on the near source areas, we eliminated the ‘interfering events’ by considering only earthquakes with magnitudes ranging from 5.2 to 6.9, which is a more stringent elimination to make the cumulative moment release curve smoother. This also eliminates those foreshocks (such as the March 9, 2011, M 7.5, foreshock) which are above magnitude 6.9, so that the long-term AMR can be investigated without the influence of short-term, or immediate, foreshocks. Generally, these foreshocks would have a significant effect on the moment release curve if they were not eliminated in the analysis, but what is being focused on is the long-to-intermediate-term cumulative (and nearly gradual) moment release. For reasons of brevity, we present only the case with the elimination of the ‘interfering events’. The de-clustering of seismic events showed little effect on the qualitative behavior of the cumulative moment release with regard to accelerating or decelerating.

Traditionally, in the analysis of seismicity (e.g., Keilis-Borok and Rotwain, 1990), accounting for the quality of depth determination in the earthquake catalogue, the analysis simply considers all the ‘shallow’ earthquakes with depths ranging from 0 to 70 km. In this investigation, we followed the same convention. However, since the rupture of this great earthquake is large, with a low dip angle, the depth distribution can be ‘transformed’ into a horizontal distribution. Figure 1 shows the rupture of the March 11, 2011, M 9 mainshock (after Lay and Kanamori, 2011), together with the key areas subject to AMR analysis. It can be seen that the availability of enough moment tensor data is, to a large extent, due to the size of the earthquake rupture.

Fig. 1
figure1

The seismic rupture of the March 11, 2011, M 9 earthquake (Mw 9.0/NEIC, Mw 9.1/GCMT), and the distribution of earthquakes subject to analysis. Hexagons give the centroids of the mainshock and its immediate foreshock, respectively. Plate boundaries, as shown by dark gray lines, are from Bird (2003). In the figure, 5 areas for the AMR analysis, L-1, L-2, L-3, K-1 and K2, are marked (for the seismological significance of these areas, refer to Lay and Kanamori, 2011). Note that the boundaries of these areas consider both tectonics and seismic clustering. Top left subplot is the frequency-magnitude distribution of the earthquakes under consideration, giving the completeness magnitude.

After the March 11, 2011, Tohoku earthquake, several studies have been published relating to the seismicity before, and after, the mainshock. Ishikawa (see, http://www.ab.cyberhome.ne.jp/catfish/event/2011e-japan.html) provided a quick analysis of regional and global seismicity before, and after, the Tohoku earthquake. Seismicity was systematically outlined by Hirose et al. (2011). Katsumata (2011) discussed the long-term seismic quiescence which started some 20 years before the earthquake. The Tohoku earthquake also raises an unprecedented question regarding the along-dip segmentation versus the along-strike segmentation (Yomogida et al., 2011). According to the study of the rupture process (see, Lay and Kanamori, 2011, for a concise review), the earthquake rupture starts from the deeper part radiating high-frequency-predominant seismic waves, and continues by the shallower part radiating low-frequency-predominant seismic waves and generating tsunami-generic displacements. This along-dip segmentation characteristic is different from previous great earthquakes, such as the Sumatra-Andaman earthquake in 2004. In this study, therefore, we have investigated the cumulative moment release within several specific regions, as shown in Fig. 1. With regard to methodology, this idea is somehow similar to the Reverse Tracing of Precursors (RTP, see: Keilis-Borok et al., 2004), with the difference that the RTP considers long-term anomalies within the areas of short-term precursory anomalies, but the present approach investigates AMR within the specific areas related to the earthquake preparation and rupture processes.

3. Characterizing the Long-to-intermediate-term Moment Release

Whether the seismicity exhibits an accelerating behavior is described by fitting the cumulative moment release curve with a linear function and a power-law function, respectively. Eliminating the ‘interfering events’, this curve is relatively ‘smooth’ and reflects the long-to-intermediate-term deformation. Similar to previous works such as Bufe and Varnes (1993) and Bowman et al. (1998), which are especially for analyzing the cumulative Benioff strain, the power-law function for a moment tensor element M ij can be expressed by

(1)

In the equation, the left-hand side is the summation of the moment tensor element under consideration, which is similar to the formulation of Kostrov (1974) if divided by the area under consideration. In contrast, traditional AMR analysis corresponds to the summation of the absolute values (or their square root) of the moment tensor element, being less physical. On the right-hand side of the equation, A and B are constants, t0 is the ‘failure time’ of the ‘target’ earthquake, and m the power-law exponent. By definition, m less than 1 indicates the accelerating-like case; m larger than 1 indicates the decelerating-like case; and m near unity indicates the linear case. In this investigation, to focus on whether AMR exists by the exponent m, the failure time t0 was fixed to be the origin time of the March 11, 2011, M 9 earthquake, so that the fitting could be stabilized by reducing one free parameter, t0. In fitting Eq. (1), depending on the datasets, the uncertainty of the m value, Δm, can also be obtained. Another factor to be considered is to avoid the problem of over-fitting. To this end, we use the criteria that, comparing to a linear fit, the BIC gain of the power-law fit has to be positive—otherwise the moment release is not statistically-significant accelerating/decelerating. The BIC gain for AMR is a development of the ‘curvature parameter’ C (Bowman et al., 1998) defined by the quotient of the RMS residual for the power-law fit with that for the linear fit, being prescribed (somewhat arbitrarily) that the case with C smaller than 0.70 is ‘significantly’ accelerating/decelerating. Using the BIC gain to the AMR studies (Jiang and Wu, 2010) taking the simplified form of BIC (Seher and Main, 2004), represented by [−(N/2) 1n(RMS) − (p/2) 1n(N/2π)] in which N is the number of data samples and p the degrees-of-freedom of the model, a ‘reasonable’ AMR fitting is defined more ‘objectively’ by the criteria ΔBIC > 0 in comparison with a linear fit. That is, over-fitting due to the use of too many free parameters (or few data samples) will be penalized by the BIC function which includes both p and N.

4. Results and Discussion

In the present work, we used a two-level spatial scope, as shown in Fig. 1: the areas L-1, L-2, and L-3, with reference to the GPS-measured locking status (Loveless and Meade, 2010; Lay and Kanamori, 2011); and the areas K-1 and K-2, with reference to the earthquake rupture process (Koper et al., 2011; Lay and Kanamori, 2011). L-2 is the area accommodating the source of the great earthquake; and the great earthquake was started by K-1 and followed by K-2 (Lay and Kanamori, 2011). Similar to Yomogida et al. (2011) but with a different spatial scale, these areas can be naturally divided by the clustering of seismicity. Limitation of samples did not provide a statistically-reliable AMR result with respect to the along-strike segmentation of Yomogida et al. (2011) and is not presented here due to limitations of space. Figure 2 shows the cumulative seismic moment tensor elements (a–f), the cumulative scalar seismic moment (g), and the cumulative Benioff strain (h, as represented by the cumulative square root of the scalar seismic moment), respectively, for the 5 areas shown in Fig. 1. In Figs. 2(a)(f), for the 5 areas, respectively, the moment tensor elements are normalized by the maximum element, so that the accelerating/decelerating trend may be clearly visible and compared with each other. One of the main differences between the moment tensor summation (Kostrov, 1974) and the scalar moment summation is that the latter always provides a monotonically increasing curve, but the former does not. From the variation of different moment tensor elements it may be seen that the cumulative moment tensor is controlled by a few predominant elements, indicating the directivity of the focal mechanisms. Figure 3 further shows that these cumulative moment tensors are, to a differing extent, similar to that of the March 11, 2011, mainshock. Also note that the abrupt variations in the cumulative moment tensor element curves, such as that of L-2 in the period from 2005 to 2010, are not caused by a single event but a series of events accumulating.

Fig. 2
figure2

Cumulative seismic moment tensor elements (a)–(f), cumulative scalar seismic moment (g), and cumulative Benioff strain (h, as represented by the cumulative square root of the scalar seismic moment). Different line types correspond to the 5 areas shown in Fig. 1. In Figs. 2(a)(f), for the 5 areas, respectively, the moment tensor elements are normalized by the maximum cumulative element, so that the accelerating/decelerating trend may be clearly visible and compared with each other. The vertical dashed line shows the time of the Tohoku earthquake. Note that the abrupt variations in the cumulative moment tensor element curves, such as that of L-2 in the period from 2005 to 2010, are not caused by a single event but a series of events accumulating.

Fig. 3
figure3

Equal-area projection of the cumulative moment tensors before the March 11, 2011, M 9 mainshock, for the 5 areas shown in Fig. 1. (a) Since 1976/01/01; (b) Since 1990/01/01; (c) Focal mechanism of the March 11, 2011, M 9 mainshock (from GCMT).

Parameters of the fitting of the cumulative scalar seismic moment curve (g) and the curve of the cumulative square root of the scalar moment (h, corresponding to the cumulative Benioff strain traditionally used in AMR studies), respectively, are shown in Table 1, to check the statistical significance of the accelerating/decelerating behavior. In Table 1, two time scales are considered: the time period since 1976 (the starting time of the GCMT catalogue), and the time since 1990, which correspond to 3.5 decades and 2 decades time scale, respectively. From the table it may be seen that an apparent AMR exists for the L-2 and K-2 areas, as shown by the m exponent. From the Benioff strain curve, it is difficult to judge whether L-1, L-3, and K-1 are decelerating or linearly increasing, although the cumulative scalar moment curve indicates a decelerating-like trend. K-1 seems to exhibit an accelerating trend at the 2 decades time scale. But for the cumulative Benioff strain curve, (m + Δm) almost becomes 1, therefore the seemingly accelerating trend is suspicious. On the other hand, from either the Benioff strain or the scalar moment, L-2 and K-2 are significantly accelerating, within the 3.5 decades and 2 decades time scale. From Fig. 3 it may also be seen that the cumulative moment tensors for L-2, K-1, and K-2 are more similar to that of the March 11 mainshock. This also provides an opportunity to judge the ‘direction of the acceleration’, which is beyond the scope of this short letter.

Table 1 Parameters of the fitting*.

5. Concluding Remarks

The March 11, 2011, off the Pacific coast of Tohoku Japan, M 9 earthquake casts a new light on the study of the long-to-intermediate-term moment release problem. Due to its retrospective nature, this study has a very limited significance for ‘real forward’ time-dependent seismic hazard assessment. Remarkably, from the cumulative moment curves the ‘starting time’ of the accelerating stage would be difficult to judge if there were really an AMR process. Due to this reason, fitting of the ‘failure time’ is not within the scope of this work, which simply investigates whether or not AMR exists—a simpler but still tough problem. Seen from the moment release curve at the decades time scale, it is also difficult to differentiate an accelerating process and a quiescence-and-recovery process. However, results from the analysis may provide some heuristic clues to the understanding of the relation between the observed AMR and the process of earthquake preparation. Note that the L-2 area, showing AMR behavior, is that accommodating the great earthquake, which may not be surprising. But note that K-2 is the area that produces the latter initiated, tsunami generic slip, it seems that although the K-2 rupture is somehow a follow-up of the rupture in K-1, the preparation of the rupture of this area has been at least 3 decades, as indicated by the AMR behavior.

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Acknowledgements

We thank the anonymous referees as well as the editor for constructive suggestions in revising the manuscript. The study is supported by the international science and technology cooperation project (Grant No. 2012DFG20510), from the Ministry of Science and Technology of China.

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Correspondence to Zhongliang Wu.

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Jiang, C., Wu, Z. Insights into the long-to-intermediate-term pre-shock accelerating moment release (AMR) from the March 11, 2011, off the Pacific coast of Tohoku, Japan, M 9 earthquake. Earth Planet Sp 64, 765–769 (2012). https://doi.org/10.5047/eps.2012.03.002

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Key words

  • Accelerating moment release
  • Tohoku M 9 earthquake
  • fault segmentation