Continuity, segmentation and faulting type of active fault zones of the 2016 Kumamoto earthquake inferred from analyses of a gravity gradient tensor

Abstract

We analyze Bouguer anomalies in/around the focal region of the 2016 Kumamoto earthquake to examine features, such as continuity, segmentation and faulting type, of the active fault zones related to the earthquake. Several derivatives and structural parameters calculated from a gravity gradient tensor are applied to highlight the features. First horizontal and vertical derivatives, as well as a normalized total horizontal derivative, characterize well the continuous subsurface fault structure along the Futagawa fault zone. On the other hand, the Hinagu fault zone is not clearly detected by these derivatives, especially in the case of the Takano-Shirahata segment, suggesting a difference of cumulative vertical displacement between the two fault zones. The normalized total horizontal derivative and the dimensionality index indicate a discontinuity of the subsurface structure of the Hinagu fault zone, that is, a segment boundary between the Takano-Shirahata and the Hinagu segments. The aftershock distribution does not extend beyond this segment boundary. In other words, this segment boundary controls the southern end of the rupture area of the foreshock. We also recognize normal fault structures dipping to the northwest in some areas of the fault zones from estimations of dip angles.

Introduction

The 2016 Kumamoto earthquake consisted of the foreshock (M _JMA 6.5, 21:26 JST on April 14, 2016) and the mainshock (M _JMA 7.3, 01:25 JST on April 16, 2016). The focal mechanism of the foreshock was a right lateral slip, and the mainshock was a right lateral slip with a normal fault component (JMA 2016a, b). The sources of the foreshock and mainshock were located in the Takano-Shirahata segment of the Hinagu active fault zone and the Futagawa segment of the Futagawa active fault zone, respectively (GSI 2016a). The Headquarters for Earthquake Research Promotion of Japan (HERP 2013a) extended the Futagawa active fault zone to the west because steep horizontal gradients of Bouguer anomalies are distributed continuously to the end of the Uto Peninsula and a normal fault, the displacement of which reaches the sea floor, was revealed off the coast of Ota (AIST et al. 2010; Sugiyama et al. 2010). They divided the fault zone into the Futagawa segment, the Uto segment and the north coast of the Uto Peninsula segment.

The north–south extensional tectonics is dominant in central Kyushu (Tada 1984; Takayama and Yoshida 2007). The Beppu-Shimabara rift zone (Matsumoto 1979), of which the south end is bounded by the Oita-Kumamoto tectonic line, is a subsidence zone due to the extension and may lead to the Okinawa trough (Tada 1984, 1985) (Fig. 1). Major active fault zones in the study area, composed of normal faults extending in the EW direction, are the Minou and the Beppu-Haneyama fault zones, and right lateral faults with normal fault components extending in the NE–SW direction are the Futagawa, the Hinagu and the Midorikawa fault zones (HERP 2013b).

Fig. 1

Topography and distribution of the gravity measuring points used in this study. Red lines show the active faults (Nakata and Imaizumi 2002) and the broken red lines show the extended fault lines of the Futagawa fault zone (HERP 2013a). The black dots indicate the gravity measuring points. The magenta and cyan circles represent subsequent seismicity [April 14, 2016, at 21:16 and April 16, 2016, at 14:00 (JST)] after the mainshock and the foreshock, respectively. The yellow star indicates the epicenter of the mainshock and the orange star that of the foreshock. The black triangles indicate the active volcanoes

As shown in Fig. 2, in the middle part of Kyushu, Quaternary volcanic rocks and pyroclastic rocks are extensively deposited around the Beppu-Shimabara rift zone. From the south of the Oita-Kumamoto tectonic line to the Usuki-Yatsushiro tectonic line, the basement rocks are mainly Mesozoic metamorphic rocks and Cretaceous sedimentary rocks which are mostly covered with Quaternary pyroclastic rocks. To the south of the Usuki-Yatsushiro tectonic line, Paleozoic and Mesozoic accretionary complexes mainly accumulated.

Fig. 2

Geological map of the analyzed area modified from the seamless digital geological map (1:200,000) published by the Geological Survey of Japan, AIST (2009). The continuous black lines show the active faults (Nakata and Imaizumi 2002) and the dotted black lines show the extended fault line of the Futagawa fault zone (HERP 2013a). The heavy broken black lines show the tectonic lines. The thin broken line shows the north end of the Beppu-Shimabara rift zone

Gravity anomaly analysis is useful for examining the subsurface structures of active fault zones. Fedi et al. (2005) show the fine image of the structural setting in the southern Apennines which is obtained from analyzing several single components of a gravity gradient tensor. Also, there exist several studies of gravity anomalies around source faults of large earthquakes. From a comparison of gravity anomalies and aftershock distributions, Honda et al. (2002) have shown that the source area of the 2000 Tottori-ken Seibu earthquake was controlled by a geological boundary. Gravity analysis around the aftershock region of the 2007 Noto Hanto earthquake showed that the rupture size of the earthquake was constrained by block structures in the Noto Peninsula (Honda et al. 2008). In Kyushu, Nishijima and Fujimitsu (2015) reveal the fault structure of the Minou fault zone by a three-dimensional (3D) modeling with microgravity survey data.

In this study, we examine the subsurface structures in/around the focal region through gravity anomalies. We calculate the first horizontal derivative (HD), the first vertical derivative (VD), the normalized total HD, the dip angle of a two-dimensional structure and the dimensionality index, from the gravity gradient tensor. We discuss the continuity, segmentation and the faulting type of active fault zones, which caused the 2016 Kumamoto earthquake, through these derivatives and the structural parameters, together with the aftershock distribution.

Data and methods

Gravity data and corrections

We apply the gravity data published by the Gravity Research Group in Southwest Japan (2001), the Geographical Survey Institute (2006), Yamamoto et al. (2011), Honda et al. (2012) and the Geological Survey of Japan, AIST (2013), in this study. The distribution of the gravity measuring points is shown in Fig. 1, and the total number of data points is 16,861 in the area shown. We apply terrain corrections with 10 m DEM (Sawada et al. 2015). The assumed density of the terrain corrections is 2670 kg/m³ according to HERP (2013b). This density is suitable for the basement rocks around the Futagawa and the Hinagu fault zones, which are the Mesozoic and Paleozoic rocks. If we apply the assumed density of 2300 kg/m³ for the terrain correction, then Bouguer anomalies tend to correlate with topography, indicating that the assumed density of 2300 kg/m³ is not suitable. We also apply a low-pass filter with a cutoff wavelength of 10 km to emphasize a structure that corresponds to a scale of the segment of active fault zones, which is mainly 15–20 km, and to reduce local singularities of derivative values mentioned in the next subsection. Finally, a linear trend is removed to obtain the Bouguer anomalies.

Derivatives and structural parameters calculated from a gravity gradient tensor

We use the first HD, the first VD and the normalized total horizontal derivative (TDX) (Cooper and Cowan 2006), to detect structural boundaries, and also the dip angle (β) (Beiki 2013) and the dimensionality index (D _i) (Beiki and Pedersen 2010), as structural parameters to evaluate the subsurface fault structure (Kusumoto 2015). These derivatives and structural parameters are calculated from a gravity gradient tensor.

We follow a technique using a Fourier transform to calculate a gravity gradient tensor (Γ) from a Bouguer anomaly proposed by Mickus and Hinojosa (2001), as indicated below. The gravity gradient tensor is defined with the gravity vector ${\mathbf{g}} = (g_{x} , g_{y} , g_{z} )$ as

$$ \varGamma = \left[ {\begin{array}{*{20}c} {\frac{{\partial g_{x} }}{\partial x}} & \quad{\frac{{\partial g_{x} }}{\partial y}} & \quad{\frac{{\partial g_{x} }}{\partial z}} \\ {\frac{{\partial g_{y} }}{\partial x}} & \quad{\frac{{\partial g_{y} }}{\partial y}} & \quad{\frac{{\partial g_{y} }}{\partial z}} \\ {\frac{{\partial g_{z} }}{\partial x}} & \quad{\frac{{\partial g_{z} }}{\partial y}} & \quad{\frac{{\partial g_{z} }}{\partial z}} \\ \end{array} } \right] = \left[ {\begin{array}{*{20}c} {g_{xx} } & \quad{g_{xy} } & \quad{g_{xz} } \\ {g_{yx} } & \quad{g_{yy} } & \quad{g_{yz} } \\ {g_{zx} } & \quad{g_{zy} } & \quad{g_{zz} } \\ \end{array} } \right]. $$

(1)

where g _z is measured on a horizontal surface in the (x, y)-plane.

The gravity potential $\phi$ satisfies Laplace’s equation, $\nabla^{2} \phi = 0.$ The Fourier transform of $\phi$ $(\varPhi ({\mathbf{k}}))$ thus satisfies $(k_{x}^{2} + k_{y}^{2} + k_{z}^{2} )\varPhi ({\mathbf{k}}) = 0,$ where ${\mathbf{k}} = (k_{x} , k_{y} , k_{z} )$ is the wavenumber vector and k _x , k _y and k _z are the wavenumbers in the x-, y- and z-directions, respectively. Then, the wave number k _z can be expressed in terms of k _x and k _y as $- ik_{z} = \left| {\mathbf{k}} \right|,$ where $\left| {\mathbf{k}} \right| = (k_{x}^{2} + k_{y}^{2} )^{1/2}$ (e.g., Blakely 1996). Finally, together with $\nabla \times {\mathbf{g}} = 0,$ the gravity gradient tensor is expressed as

$$ \varGamma = {\mathcal{F}}^{ - 1} \left\{ {[K({\mathbf{k}})]G_{z} ({\mathbf{k}})} \right\}, $$

(2)

where ${\mathcal{F}}^{ - 1}$ is the inverse Fourier transform operation, G _z is the two-dimensional Fourier transform of g _z and

$$ \left[ {K({\mathbf{k}})} \right] = \left[ {\begin{array}{*{20}c} {\frac{{ - k_{x}^{2} }}{{\left| {\mathbf{k}} \right|}}} & \quad{\frac{{ - k_{x} k_{y} }}{{\left| {\mathbf{k}} \right|}}} & \quad{ - ik_{x} } \\ {\frac{{ - k_{x} k_{y} }}{\left| k \right|}} & \quad{\frac{{ - k_{y}^{2} }}{{\left| {\mathbf{k}} \right|}}} & \quad{ - ik_{y} } \\ { - ik_{x} } & \quad{ - ik_{y} } & {\left| {\mathbf{k}} \right|} \\ \end{array} } \right]. $$

(3)

From the gravity gradient tensor, HD, VD and TDX (Cooper and Cowan 2006) are defined as

$$ {\text{HD}} = \sqrt {g_{zx}^{2} + g_{zy}^{2} } , $$

(4)

$$ {\text{VD}} = g_{zz} , $$

(5)

$$ \begin{aligned} {\text{TDX}} & = \tan^{ - 1} \left( {\frac{\text{HD}}{{\left| {\text{VD}} \right|}}} \right) \\ & = \tan^{ - 1} \left( {\frac{{\sqrt {g_{zx}^{2} + g_{zy}^{2} } }}{{\left| {g_{zz} } \right|}}} \right). \\ \end{aligned} $$

(6)

These derivatives work as a high-pass filter, which detect relatively shallow and detailed structures. HD evaluates horizontally steep gravity gradients. Therefore, HD is often used to detect faults and structural boundaries (Kudo and Kono 1999; Yamamoto 2003; Honda et al. 2005; Kusumoto 2015, 2016). The maximal value of HD is more sensitive to shallower structure boundaries, so deep structures are occasionally underestimated (SEGJ 1998). VD does not emphasize the short-wavelength structures too much. Thus, VD is used to detect density boundaries such as geological boundaries the size and distribution depth of which are in a middle range (Sawada et al. 2012; Kusumoto 2016). Structural boundaries are recognized as zero isolines of VD, which indicate the inflection points of gravity anomalies (SEGJ 1998). TDX can detect both short- and long-wavelength components and is useful for detecting geological boundaries, as well as VD (Kusumoto 2016).

For two-dimensional (2D) structures, the minimum and maximum eigenvectors of the gravity tensor represent the strike and dip angles, respectively (Beiki 2013). β is defined by the components of the maximum eigenvector, $v_{1x} ,v_{1y} ,v_{1z} ,$ as

$$ \beta = \tan^{ - 1} \left( {\frac{{v_{1z} }}{{\sqrt {v_{1x}^{2} + v_{1y}^{2} } }}} \right) . $$

(7)

The distribution of β along a fault zone can be useful for evaluating a faulting type if the subsurface structure is assumed to be 2D-like (Kusumoto 2015). Kusumoto (2015) showed that a decrease in dip angle with depth was observed for a normal fault and an increase with depth was observed for a reverse fault, from a numerical simulation.

D _i evaluates the dimension of the subsurface structure, 2D or 3D (Beiki and Pedersen 2010). D _i is close to 0 or 1, respectively, depending on whether the dimension of the structure is 2D or 3D. D _i is defined by using the eigenvalues of a gravity gradient tensor (Pedersen and Rasmussen 1990), $\lambda_{1} ,\lambda_{2} ,\lambda_{3} ,$ as

$$ D_{\text{i}} = \frac{{ - 27I_{2}^{2} }}{{4I_{1}^{3} }}, $$

(8)

where $I_{1} = \lambda_{1} \lambda_{2} + \lambda_{2} \lambda_{3} + \lambda_{1} \lambda_{3} ,$ and $I_{2} = \lambda_{1} \lambda_{2} \lambda_{3} .$

Results

Subsurface fault structures related to the Futagawa fault zone

Figure 3 shows a low-pass filtered Bouguer anomaly with a cutoff wavelength of 10 km. Around the Aso volcano zone shows low Bouguer anomalies, lower than −20 mGal, while the south of the Oita-Kumamoto tectonic line shows high Bouguer anomalies, higher than 0 mGal. These distributions are related closely to the geology in this area. The Aso volcano is filled with relatively light Quaternary volcanic and pyroclastic rocks (Fig. 2). On the other hand, heavier Mesozoic metamorphic rocks and Cretaceous sedimentary rocks are accumulated from the Oita-Kumamoto tectonic line to the Usuki-Yatsushiro tectonic line (Fig. 2).

Fig. 3

Bouguer anomaly distribution of the analyzed area. A low-pass filter with a cutoff wavelength of 10 km is applied. The assumed density of the terrain corrections is 2670 kg/m³. The continuous red lines show active faults (Nakata and Imaizumi 2002) and the broken red lines show the extended fault line of the Futagawa fault zone (HERP 2013a)

A structural boundary, where the density boundary is clear, is generally detected as a higher value of HD, a zero isoline of VD and/or a large, around 90°, TDX. The obtained HD (Fig. 4), VD (Fig. 5) and TDX (Fig. 6) clearly illustrate the continuous subsurface structural boundary from the Uto Peninsula to the west end of the Aso volcano along the Futagawa fault zone. In Fig. 1, we show the distribution of earthquakes between April 14, 2016, at 21:16 and April 16, 2016, at 14:00 JST, which includes the aftershocks of the foreshock and the mainshock. The aftershocks are distributed along this structural boundary from the confluence of the Futagawa and the Hinagu fault zones to the east end of the Aso volcano, indicating the existence of a fault structure.

Fig. 4

First horizontal derivative (HD) distribution of the Bouguer anomaly shown in Fig. 3. A structural boundary is recognized as higher values. The continuous black lines show active faults (Nakata and Imaizumi 2002) and the broken black lines show the extended fault line of the Futagawa fault zone (HERP 2013a)

Fig. 5

First vertical derivative (VD) distribution of the Bouguer anomaly shown in Fig. 3. A structural boundary is recognized as a zero isoline. The continuous black lines show active faults (Nakata and Imaizumi 2002) and the broken black lines show the extended fault line of the Futagawa fault zone (HERP 2013a)

Fig. 6

Normalized total horizontal derivative (TDX) distribution of the Bouguer anomaly shown in Fig. 3. A structural boundary is recognized as large degree isoline. The continuous black lines show active faults (Nakata and Imaizumi 2002) and the broken black lines show the extended fault line of the Futagawa fault zone (HERP 2013a)

Figure 7 shows the distribution of the dip angle $\beta .$ Kusumoto (2015) demonstrated that the dip angle increases with depth along a reverse fault, while it decreases with depth along a normal fault based on a numerical simulation with a 3D fault model. β indicates the dip angle only when the assumed structure is 2D-like, that is, D _i ≤ 0.5 (Beiki 2013) (Fig. 8). Focusing on β around the fault zone, the distribution of β across the Futagawa segment decreases from the south to the north. The Futagawa fault is dipping to the northwest (GSI 2016a). The dip angle distribution across the Futagawa segment, therefore, implies a normal fault, corresponding to the faulting of the focal mechanism of the 2016 Kumamoto earthquake (HERP 2016).

Fig. 7

Dip angle (β) distribution. For a two-dimensional structure, a decrease and an increase with depth indicate a normal fault structure and a reverse fault structure, respectively. The continuous red lines show active faults (Nakata and Imaizumi 2002) and the broken red lines show the extended fault line of the Futagawa fault zone (HERP 2013a)

Fig. 8

Dimensionality index (D _i) distribution. D _i is close to 0 or 1 depending on whether the dimension of a structure is 2D or 3D. The continuous red lines show active faults (Nakata and Imaizumi 2002) and the broken red lines show the extended fault line of the Futagawa fault zone (HERP 2013a)

Subsurface fault structures related to the Hinagu fault zone

Bouguer anomalies are high around the Hinagu fault zone. It is interesting that the contour lines around the southern part of the Hinagu segment and the Midorikawa fault zone show an S-shaped distribution across the fault (Fig. 3). According to Hagiwara (1987), a lateral displacement of a geological structure can be recognized from Bouguer anomalies as changes in contour direction and interval, discontinuous contour and S- or U-shaped features across a fault. For example, S-shaped contours of Bouguer anomalies are observed over a left lateral displacement of the Naguri fault (Hagiwara et al. 1997). Thus, we consider that the S-shaped distributions observed for the Hinagu segment and the Midorikawa fault zone indicate a right lateral faulting (Fig. 3). This is consistent with the geological and geomorphological estimation of the faulting (HERP 2013a, c).

The VD and TDX show the existence of a subsurface structural boundary, which is a fault structure, along the southern part of the Hinagu segment, but it is not so clear (Figs. 5, 6). Focusing on β around the fault zone, the distribution of β across the Hinagu segment, which decreases from the southwest to the northeast, implies a normal faulting (Fig. 7). No clear structural boundaries are observed along the Takano-Shirahata segment (Figs. 4, 5, 6), although most of the aftershocks occurred around this segment (Fig. 1). Around the segment boundary between the Takano-Shirahata and the Hinagu segments, the large value of TDX is not continuous along the fault zone (Fig. 6) and D _i shows the existence of a 3D-like structure with a NW–SE trend (Fig. 8).

Discussion

In the previous section, we have characterized the features of the subsurface fault structures of the Futagawa and the Hinagu fault zones. We focus here on the difference in features between these two fault zones and discuss the segmentation of the Hinagu fault zone based on the aftershock distribution and the size of the source fault estimated from a geodetic investigation.

We recognize the subsurface fault structures through HD, VD and TDX more clearly along the Futagawa fault zone than the Hinagu fault zone (Figs. 4, 5, 6), indicating that the cumulative vertical displacement of the Futagawa fault zone is larger than that of the Hinagu fault zone. This result is supported by GNSS data, which indicate that the subsidence velocity is remarkably large around the middle part of the Oita-Kumamoto tectonic line (HERP 2013b). Also, the vertical crustal deformation of the 2016 Kumamoto earthquake is larger in the western part of this tectonic line (GSI 2016c). However, from the derivatives, it is difficult to find a continuous subsurface structure along the Takano-Shirahata segment.

The average vertical slip rate of the Takano-Shirahata segment is 0.04–0.2 mm/year (NUPEC 1996), which is relatively small, while that of the Futagawa segment is 0.1–0.3 mm/year (Kumamoto Prefecture 1996a, b) and that of the Hinagu segment is 0.2–0.5 mm/year (HERP 2013a). In addition, surface traces of the fault around the Takano-Shirahata segment are intermittent and the direction of the displacement is irregular (HERP 2013a). This supports the smaller average vertical slip rate of the segment. Therefore, the undetected subsurface structure infers that the cumulative vertical displacement of the Takano-Shirahata segment is not large enough to be detected by Bouguer anomalies.

Around the boundary between the Takano-Shirahata and the Hinagu segments, the discontinuity of a large value of TDX, and a zone of D _i larger than 0.5 are distributed across the fault zone with a NW–SE trend (Figs. 6, 8). This suggests that a 2D-like subsurface structure, such as a fault, is discontinuous at this boundary. Also, the active area of the aftershocks does not extend to the south beyond this structural boundary. Furthermore, the result of multiple aperture interferometry (GSI 2016b) suggests that the displacement is diminished around the segment boundary. The fault model of the foreshock estimated from the coseismic crustal deformation is restricted in the Takano-Shirahata segment (GSI 2016a). These observations imply that the source fault of the 2016 Kumamoto earthquake does not extend to the south beyond this boundary. Therefore, we conclude that this boundary detected by the TDX and D _i controls the spatial extent of the source fault.

The geological map indicates that this boundary corresponds to a boundary between metamorphic rocks and sedimentary rocks on the ground surface (Fig. 2). According to Honda et al. (2002), the source area at the 2002 Tottori-ken Seibu earthquake was also limited by the geological boundary between granite and Sangun metamorphic rocks. It is, therefore, important for a more accurate characterization of the subsurface continuity and segmentation of an active fault to interpret gravity anomalies, together with geological and geomorphological information.

In this study, we show that gravity analysis enables the determination of the features, continuity, segmentation, faulting type and dipping direction of an active fault zone which occur as a result of large earthquakes. The gravity data used in this study were obtained prior to the Kumamoto earthquake. We emphasize that an effective use of gravity anomalies can enhance the understanding of active faults.

Conclusions

We have used derivatives and structural parameters derived from a gravity gradient tensor calculated from Bouguer anomalies to investigate the subsurface structure of the active fault zones related to the 2016 Kumamoto earthquake. The continuous subsurface fault structure along the Futagawa fault zone is clearly detected with HD, VD and TDX. The distribution of β around the Futagawa segment implies a normal faulting. In the Hinagu fault zone, structural boundaries are not detected along the Takano-Shirahata segment, reflecting a smaller average vertical slip rate and unclear surface traces. In the Hinagu segment, Bouguer anomalies show an S-shaped distribution, which indicates a right lateral faulting, and subsurface fault structures are detected with VD and TDX. Furthermore, the distribution of β implies a normal faulting. Around the segment boundary between the Hinagu segment and the Takano-Shirahata segment, we detect the structural boundary with TDX and D _i, which corresponds to a geological boundary. The aftershock distribution and geodetic observations suggest that a spatial extent of the source fault is controlled by this boundary. Gravity analysis is a useful method to evaluate the continuity, segmentation and faulting type of active fault zones.