大阪平野における地震動予測の試み?大阪地域の3次元地盤構造モデルの作成?
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1 No. 2, p , 2002 Three-dimensional subsurface structure model beneath the Osaka Plain Haruo Horikawa 1, Kiyohide Mizuno 2, Kenji Satake 3, Haruko Sekiguchi 4, Yuko Kase 5, Yuichi Sugiyama 6, Hiroshi Yokota 7, Masaki Suehiro 8 and Arben Pitarka 9 1, 2, 3, 4, 5, 6 Active Fault Research horikawa@aist.go.jp, Center, GSJ/AIST, k4-mizuno@aist.go.jp, h. kenji.satake@aist.go.jp, haruko.sekiguchi@aist.go.jp, kase.yuko@aist.go.jp, sugiyama-y@aist.go.jp 7, 8 Hanshin, yokota@hanshin-consul.co.jp, Consultants Co., Ltd. suehiro@hanshin-consul.co.jp 9 URS CorporationURS Corporation, Arben_Pitarka@urscorp.com Abstract: We newly developed a three-dimensional subsurface structure model beneath the Osaka Plain, southwest Japan, that covers the eastern part of the Osaka sedimentary basin. The model was constructed by integrating both geophysical and geological data such as gravity anomaly, seismic reflection profiles, and borehole data. From this information we selected marine-clay beds, volcanic ashes and a geomagnetic polarity boundary as key markers, and inferred their distributions over the model area. We then estimated the seismic velocity and density of the sediment layer as a function of depth and time since deposition. The basin-floor in our model has wedge-like structures formed by repeated activity of reverse faults. Comparison of our model with other subsurface structure models shows several differences, reflecting the different amount of data. Numerical simulation of ground motions using the subsurface structure reproduced basin-induced surface waves, which were not reproduced from a flat-layered velocity structure, but synthetic waveforms are still different from the waveforms observed in the southern part of the plain. These discrepancies may result from erroneous modeling of the basin floor in the southern part. In the eastern part of the plain, body waves arrive later than observed probably because of underestimation of seismic velocity of the sediment layer. 3 Keywords: three-dimensional subsurface structure, Osaka Plain, geologic structure, basin-induced surface wave S 13 4 Kawase, 1996) Ikebe et ( al., 1970) Graves et al. ( (1998), 1993) (, 1975; Hatayama et al., 1995) 3 (1993)
2 (1993) (1997, 1999) (, ) (, 1982), 1987) (, 1998) ( 2 (Faust, 1951) 1) 2) P S S P P Fig. 1 2 (, 1982; P, 1997) S (1998) P, ( 2001) S 6.1 (2) (3)
3 3 ( Nakagawa et al., 1991) 5 Fig. 4 1 (, 1994) (, 1982) (, 2001) ( DSI (Dipole Shear Sonic Imager), 1985) (, 1998) ( PS, 1986) 6 GS-K1 (, ) (, 1997) 3 (, 1972) (1973) (1991) (1993) S (, 1998) P ( 4, 1990;, 1990) OD-1OD-9 (, 1996a) (, 1996c) (, 1996b) ( Ikebe et al., 1970) OD-8 (, 1996d) ( 8, 1996c) (, 1996e) (, 1996b) (, 1996a) 38 km OD-1OD-9 (, 1998) 58 km Fig. 1 4 Appendix A x Fig. 2 y 3 km Ma 13Ma -1 Fig km 59 Fig. 2 Fig. 2 Table 1 8 Fig. 2 Fig. 2 1 (, 1973) Fig. 2 (, 1989) (2000) (, 1994)
4 (1973) m (, 1991) 500 m, ( 1978, (, 1994;, 1995; 1998 ) Fig (1997) (, ) (1998 Fig. 3 2 y = 8 km y = 6 km (1987) 500 m 80, ( 1994) (, 1992) Fig. 2 y = 6 km 7 Ma 12 (, 1992) 45, 1997) (,, 1995; 1997) (1997) Fig. 5 (1996) Ma 12 (, 1992) (, ) 2 (, 1992)
5 3 (, Cande and Kent (1995) 1997) 2.6 my 80 (, 1982) GS-K1 (Biswas et al., 1999) (, 1996) (1977) (1998) (, 1977) GS-K1 (1977) (1984) Fig Ma -1Ma Ma -1 (, 1993) my Talwani et al. (1959) (, 1984) (1999) my 1.7 my / / ( Doblin and Savit, 1988;, 2001) (, 1997) Ma -1 (1977; 1984) Ma -1 Ma Ma -1Ma 5 Ma -1 (, 1984) Ma -1 3 my (, 1988) 0.51 my (1999) OD-1 OD-2 Fig. 3 Ma my 37 (Shackleton et al., 1990) / Ma my Ma 3 / (, 1982)
6 Fig my (, K-Ar 1970) my (Hayashidaet al., 1996) (1999) Ma 3 Shackleton et al. (1990) 21 y = 30 km Fig. 6 (b) Ma my (, 1996) Ma 10 Ma 10 9 (, 1999) (Bassinot et al., 1994) (1996) my, my 1700 m (1993) Ma 10 BT my Ma my Fig. 7 Fig. 8 / (1998) GS-K km 2 (1997) y = 15 km 2 Fig. 6 (a) (1998) (1991) (1993) 3.2 P V P (km/s) D (m) T () (1998) Ma 10 Fig m 800m
7 3 V P = 1.069T D /(D/ 800.) 0.41 (1) 800m V p V s V p V s P S V P = 1.069T D (2) n K V p V s (1998) V p n ρ S, ρ F n P S ρ ρ S V p ρ = ( 1 n)ρ S (3) P ρ = ( 1 n)ρ S + nρ F (4) V p0 (km/s) D (m) n ρ Gassmann (1951) V p0 = V p 0.355D (10) V p0 n 2 2 log 10 n = V p (11) K ˆ + Q V p ρ V s K = K S (5) K S + Q (10), (11) n Q = K F( K S K ˆ (4) ρ n ) (6) (5)(6) K K nk ( S K F ) K (8) K K ˆ K K S K F (9) V s (1996) Gassmann S 2 1) ) G G GS-K K = 5 9 p (7) V 2 p = 1 K + 4 ρ 3 G = 1 K + 4 K (8) P (5.5 km/s) ρ 5 S ρ V p K P V p P 5.5 km/s P S V s S (2.75 km/s) (2.6 g/cm 3 ) V 2 s = G ρ = G ρ = 3 K (9) 5 ρ S Q S K S K F (2002) n K (5) (6) K (4) ρ Q
8 Arben Pitarka S V S (km/s) (12) Q S = 50V S 5.1 ( Li et al., 1990) y = 32 km Fig. 9 S S Fig. 10 (1996) S S OSB Fig. 8 (1998) m S 0.7 km 0.4 km/s 0.2 km/s 1 (1999) Fig y = 24 km y = 46 km (1999) 2 (1999) (1999) (x = 15 km, y = 46 km ) 1210 m 1195 m (, 1991) 3 2 1) 2) 2) 1
9 3 Table 2 Fig. 8 ( 13.gif) P S (, 1984) (Toki et al., 1995) Fig. 8 S/N ( Hatayama et al., 1995) Hz Pitarka (1999) 3 staggered grid (2002, ) Graves (1996) P S 3 S 550 m/s S 550 m/s P S 3 1 Fig km Fig. 13ac x = 30 km 2 Fig. 13 x = 26 km y = 12 km 2 Fig. 14ad 3 4
10 CHY (x = y km = 6.92 km) 3 SKI CHY TDO (x = 9.63 y km = km) ABN (x = y = km km) Fig. 13 (b) TDO FKS (x = kmy = km) 1 15 TDO 3 SKI (x = kmy = km) 18 3 YAE (x = kmy = km) MRG (x = km, y = km) (1996) S 6.3 SKI Fig. 8 S SKI SKI S TDO 700 m Fig. 13 Fig. 13 (c) 15 1 OCU (x = y = km km) 30 AMA (x = 9.78 kmy = km) 25 SKI 18 SKI
11 3 Wessel and TYN (x = kmy = km) SRK Smith (1998) GMT (Generic Mapping Tools) (x = kmy = km) 20 3 Fig. 13 SRK Bassinot, F. C., E. Vincent, X. Quidelleur, N. J. Shackleton, and Y. Lancelot (1994) Astronomical theroy of climate and the age of the Brunhes-Matuyama magnetic reversal. Earth Planet. Sci. Lett., 126, Biswas, D. K., M. Hyodo, Y. Taniguchi, M. Kaneko, S. Katoh, H. Sato, Y. Kinugasa, and K. Mizuno (1999) Magnetostratigraphy of Plio-Pleistocene sediments in a 1700-m core from Osaka Bay, southwestern Japan and short geomagnetic events in the middle Matuyama and early Brunhes chrons. Palaeo- geography, Palaeoclimatology, Palaeoecology, 148, Cande, S. C., and D. V. Kent (1995) Revised calibration of the geomagnetic polarity timescale for the late Cretaceous and Cenozoic. J. Geophys. Res., 100, (2000) CD-ROM,. Doblin, M. B., and C. H. Savit. (1988) Introduction to 1) Geophysical Prospecting, 4th Edition, McGraw-Hill, 2) 867p. (1992), 213p. Faust, L. Y. (1951) Seismic velocity as a function of 3) depth and geologic time. Geophysics, 16, Gassmann, F. (1951) Elastic waves through a packing of spheres. Geophysics, 16, Graves, R. W. (1996) Simulating seismic wave propagation in 3D elastic media using staggered-grid 3) finite differences. Bull. Seismol. Soc. Am., 86, Graves, R. W., A. Pitarka, and P. G. Somerville (1998) Ground-motion amplification in the Santa Monica area: Effects of shallow basin-edge structure. Bull. Seismol. Soc. Am., 88, Hatayama, K., K. Matsunami, T. Iwata, and K. Irikura (1995) Basin-induced Love waves in the eastern part
12 of the Osaka basin. J. Phys. Earth, 43, Hayashida, A., H. Kamata, and T. Danhara (1996). 2, 42, Correlation of widespread tephra deposits based on paleomagnetic directions: Link between a volcanic field and sedimentary sequences in Japan.. Quaternary International, 34-36, , 43, (2002) S Q. 2002, S (1998). 2, 51, S. 2, 51, (1996). 2, 49, ,, 270 p. (1995). 2, 48, (1982) 5 2, 47, (1993), 112p.. 2, 46, (1985) 5 Kawase, H. (1996) The cause of the damage belt in Kobe:. "the basin-edge effect," constructive interference of, 103p. the direct S-wave and with the basin-induced (1973) diffracted/rayleigh waves. Seismol. Res. Lett., 67, ,. (1972) 1 5 Ikebe, N., J. Iwata, and J. Takenaka (1970) Quaternary. geology of Osaka with special reference to land (2001)., subsidence. J. Geosci. Osaka City Univ., 13, p. (1998)., 51, (1997) (1991) 1.., 97, 52, CS Li, Y. G., P. Leary, K. Aki, and P. Malin (1990) Seismic (1991) trapped modes in the oroville and San-Andreas fault. 30. zones. Science, 249, (1993)., 340p. (1984) (1998) 1/25,000 2, 37, , 28p. PS (2001).,, (1986) 5 (1998) (1977), (1994) 5, 14, (1984)., 48, , 38, (1998) OD (1991) ,
13 p. (1998) 5 (1996) p. (1997). (1997) , , (1991). 98, 473. (1999) Pitarka, A. (1999) 3D elastic finite-difference modeling of seismic motion using staggered grids with, nonuniform spacing. Bull. Seismol. Soc. Am., 89, (1978)., 51, Arben Pitarka (2002) (1994) no. 2, Shackleton, N. J., A. Berger, and W. R. Peltier (1990) An 90, alternative astronomical calibartion of the lower Nakagawa, K., K. Ryoki, N. Muto, S. Nishimura, and K. Pleistocene timescale based on ODP site 677. Ito (1991) Gravity anomaly map and inferred Transaction of the Royal Society of Edinburgh: basement structure in Osaka plain, central Kinki, Earth Sciences, 81, south-west Japan. J. Geosci. Osaka City Univ., 34, (1997) No , (1996a) 1:25,000, (1997). No (1996b) 1:25,000, ,. (1988)., 30, (1996c) 1:25,000 (1996), (1996d) 1:25,000, 69A, ,. Talwani, M., J. L. Vorzel, and M. Landisman (1959) Rapid gravity computations for two-dimensional (1996e) 1:25,000 bodies with application yo the Mendocino,. submarine fracture zone. J. Geophys. Res., 64, (1970) Fission-Track (1995), 24, (1996a) 1:25,000. 2, 48, ,. Toki, K., K. Irikura, and T. Kagawa (1995) Strong motion (1996b) 1:25,000 records in the source area of the Hyogoken-nambu earthquake, January 17, 1995, Japan. Journal of,. Natural Disaster Science, 16, (2000), 395 p., (1975). 4., (1996c) 1:25,000 (1990), , 43, (1998). 8 Wessel, P., and W. H. F. Smith (1998) New, improved
14 version of Generic Mapping Tools released. Eos, 79, (1999) 579., 105, (1987). 77, m (1973)., 79,., 48, (1993) , 47, VI 36 0' " 136 0' " ( ) X Y X 4 A1 Y x X y A1 Table A1. Coordinate values of the model region. Japanese plane rectangular coordinates* (m) Latitude and longitude X coordinate Y coordinate Latitude (North) Longitude (East) SW edge SE edge NE edge NW edge *The Japanese plane rectangular system is based on the Tokyo Geodetic Datum (1987), and the transverse Mercator projection is used in this system. The origin of the rectangular system depends on the area to be projected. In this case the origin is N and E. The SW edge is the origin of the coordinate used in the subsurface structure model A2 1 A
15 3 A2 Table A2. Data format of the file on altitude data. Name Description Type Format YINDX Coordinate value along the y axis integer* I4 XINDX Coordinate value along the x axis integer* I4 HGHT Altitude (m) real F13.2 *Actual coordinate values in the subsurface structure model are given with (XINDX-1)dx and (YINDX-1)dy, respectively. Here dx and dy are the grid interval along x-axis and y-axis, respectively, and both values are 0.1 km. Description of data format is written in Fortran style. A3 Table A3. Data format of the file on medium constants. Name Description Type Format YINDX Coordinate value along the y axis integer I3 XINDX Coordinate value along the x axis integer I4 ZINDX Coordinate value along depth* integer I4 VP P-wave velocity (m/s) integer I5 VS S-wave velocity (m/s) integer I5 DEN Density (g/cm 3 ) real F5.2 QS Q value for S-wave integer I4 *Depth of the grid point is given as (ZINDX-1)dz+dz/2-HGHT, where dz is grid interval along depth and 0.05 km. Description of data format is written in Fortran style. 1 2 Table 1. Faults used for block partitioning and their dip angles. See Fig. 2 for their locations. No. Fault name Dip angle (deg.) 1 Arima-Takatsuki tectonic line 90 2 Nobata fault system 90 3 Hirakata-Ikoma fault system 45E 4 Ikoma fault (eastern branch) 45E 5 Katano fault 45E 6 Uemachi fault system 80E 7 Sakuragawa monocline-suminoe monocline 80E 8 Rokko-touen fault system Table 2. Hypocentral parameters of the earthquake used in numerical simulation with the three-dimensional subsurface structure model. Origin time Latitude Longitude Depth Strike Dip Rake Moment (JST) (N, deg.) (E, deg.) (km) (deg.) (deg.) (deg.) magnitude 2000/8/27 13 h 13 m 13.8 s
16 堀川晴央 水野清秀 佐竹健治 関口春子 加瀬祐子 杉山雄一 横田裕 末廣匡基 Arben Pitarka 第 1 図. モデル化対象地域 ( モデル領域 ) の位置図. Fig.1. Map showing the location of study area, Osaka Plain.
17 大阪平野の 3 次元地盤構造モデルの作成 Fig. 5 第 2 図. 深層ボーリングデータと反射法地震探査測線の分布およびブロック分割. 緑色の実線は本研究で再解析した反射法地震探査測線, 緑色の破線は既往探査結果のみをモデル作成に利用した測線. 白丸と赤丸は本研究で利用したボーリングデータの取得地点を示し, 赤丸は基盤岩に達したもの. 青線はブロック分割に用いた断層の地表トレース. 断層の名称と傾斜角は第 1 表を参照. Fig. 2. Map showing the locations of boring sites, seismic reflection-survey lines, and faults used for block partitioning. Green solid lines are survey lines of which data were reanalyzed in this study, while green dashed lines are survey lines of which data were not reanalyzed but the existing results were referred. Open circles show boring sites at which basement rock was not found while red circles show boring sites that reached basement rock. Blue lines stand for the intersections of the ground surface and faults. Each numeral is attached to each fault given in Table 1.
18 堀川晴央 水野清秀 佐竹健治 関口春子 加瀬祐子 杉山雄一 横田裕 末廣匡基 Arben Pitarka 第 図. 本研究で採用した地質層序区分と年代. は海成粘土層, 鎖線はガウス 松山クロン境界を示す.
19 大阪平野の 3 次元地盤構造モデルの作成 第 4 図. 重力観測点とブーゲー異常の分布図. 観測点を で示す. 仮定した密度は 2.67 g/cm3. Fig. 4. Contours of Bouguer anomaly with observation points shown with crosses. The assumed density is 2.67 g/cm3.
20 堀川晴央 水野清秀 佐竹健治 関口春子 加瀬祐子 杉山雄一 横田裕 末廣匡基 Arben Pitarka 第 5 図. 生駒断層の反射断面. 下川ほか (1997) の探査データを再解析して得た深度変換断面に, 各基準面の同定位置を書き加えた. 測線位置は第 2 図参照. 図中の数字は速度解析によって得られた P 波速度 (m/s). Fig. 5. Reanalyzed depth-converted seismic profile across the Ikoma fault. The reflection survey was originally conducted by Shimokawa et al. (1997). Identified horizons of key beds are shown on the profile. See Fig. 2 for the survey line. Numerals in the figure stand for P-wave velocity in m/s.
21 大阪平野の 3 次元地盤構造モデルの作成 第 6 図.2 次元地質構造モデル.(a) y = 15 km, (b) y = 30 km. Fig. 6. Two-dimensional geologic structure models. (a) y = 15 km, (b) y = 30 km.
22 堀川晴央 水野清秀 佐竹健治 関口春子 加瀬祐子 杉山雄一 横田裕 末廣匡基 Arben Pitarka 第 7 図.3 次元地質構造モデルの可視化例. 大阪湾側から東を見たもの. Fig. 7. An example of visualization of the three-dimensional geologic structure model. East view from Osaka Bay.
23 大阪平野の 3 次元地盤構造モデルの作成 第 8 図. 基盤岩上面の深度分布. 灰色の部分では基盤岩が露出している. 微動観測点の位置 ( ), 波形計算の対象とした地震の震央 ( ), 波形を計算した観測点 ( ) も示した. 発震機構 ( 下半球投影 ) を右下に示す. Fig. 8. Distribution of depth to the top of basement. Basement rock is exposed at the ground surface in gray areas. The observation points of seismic micro tremor (circles) are also plotted. The epicenter of the earthquake used for calculating waveforms is shown with a star, and strong motion stations for which waveforms were calculated are indicated by inverted triangles. The focal mechanism of the earthquake is shown in the lower right with lower hemisphere projection.
24 堀川晴央 水野清秀 佐竹健治 関口春子 加瀬祐子 杉山雄一 横田裕 末廣匡基 Arben Pitarka 第 9 図.y = 32 km における S 波速度構造の断面. Fig. 9. S-wave velocity structure along y = 32 km.
25 大阪平野の 3 次元地盤構造モデルの作成 et al. et al. et al. 第 10 図. 本研究で得られた S 波速度構造 ( 実線 ) と微動探査による推定結果 ( 破線 ) との比較. 微動探査の結果は堀家ほか (1996) による.(a) OSB,(b) KWMT,(c) KNW. 各観測点の位置は第 8 図を参照. Fig. 10. Comparison of S-wave velocity structure derived in this study (solid line) and that estimated from observation of seismic micro tremor (dashed line). The results of the micro tremor observation are after Horike et al. (1996). (a) OSB, (b) KWMT, (c) KNW. See Fig. 8 for the location of each observation point.
26 堀川晴央 水野清秀 佐竹健治 関口春子 加瀬祐子 杉山雄一 横田裕 末廣匡基 Arben Pitarka 第 11 図. 基盤岩上面深度分布の比較.(a) 本研究で得られた基盤岩上面深度,(b) 宮腰ほか (1999) で得られた基盤岩上面深度,(c) 2 つの基盤岩上面深度の差. 正の値は本研究で得られた深度の方が深いことを示す. Fig. 11. Comparison of the depth to the top of basement between two models. (a) this study, (b) Miyakoshi et al. (1999), (c) difference in depth between the two models. Positive values mean that depth estimated in this study is deeper than that of Miyakoshi et al. (1999).
27 大阪平野の 3 次元地盤構造モデルの作成 第 12 図. 比較のための波形計算に用いた 1 次元水平成層地盤構造モデル. Fig. 12. Flat-layered subsurface structure used for comparison of waveforms shown in Fig. 14.
28 堀川晴央 水野清秀 佐竹健治 関口春子 加瀬祐子 杉山雄一 横田裕 末廣匡基 Arben Pitarka 第 13a 図. 速度波形のスナップショット ( 東西成分 ). 一番下の右端のコマは基盤岩上面深度を示す. スナップショット中にある黒い線は基盤岩上面深度が 0 m の位置で, 盆地端にあたる. Fig. 13a. Snapshots of particle velocity (EW component). The lowest right panel shows the depth to the top of basement (same as Fig. 8). Black lines in each snapshot delineate the basin edges, where the depth to the top of basement is 0 m.
29 大阪平野の 3 次元地盤構造モデルの作成 第 13b 図. 速度波形のスナップショット ( 南北成分 ). Fig. 13b. Snapshots of particle velocity (NS component).
30 堀川晴央 水野清秀 佐竹健治 関口春子 加瀬祐子 杉山雄一 横田裕 末廣匡基 Arben Pitarka 第 13c 図. 速度波形のスナップショット ( 上下動成分 ). Fig. 13c. Snapshots of particle velocity (UD component).
31 大阪平野の 3 次元地盤構造モデルの作成 obs. 3D flatlayer 第 図. 観測波形と合成波形との比較 ( 大阪平野南部 ). 上 : 観測波形, 中 : 次元地盤構造モデルを使ったときの合成波形, 下 : 水平成層型の地盤構造を使ったときの合成波形. 波形は のバンドパスフィルターを通したもの. 各観測波形のトレース左側に付した数値は, 観測波形の最大振幅 を示す
32 堀川晴央 水野清秀 佐竹健治 関口春子 加瀬祐子 杉山雄一 横田裕 末廣匡基 Arben Pitarka obs. 3D flatlayer 第 図. 観測波形と合成波形との比較 ( 大阪平野西部 ). 上 : 観測波形, 中 : 次元地盤構造モデルを使ったときの合成波形, 下 : 水平成層型の地盤構造を使ったときの合成波形. 波形は のバンドパスフィルターを通したもの. 各観測波形のトレース左側に付した数値は, 観測波形の最大振幅 を示す
33 大阪平野の 3 次元地盤構造モデルの作成 obs. 3D flatlayer 第 図. 観測波形と合成波形との比較 ( 大阪平野東部 ). 上 : 観測波形, 中 : 次元地盤構造モデルを使ったときの合成波形, 下 : 水平成層型の地盤構造を使ったときの合成波形. 波形は のバンドパスフィルターを通したもの. 各観測波形のトレース左側に付した数値は, 観測波形の最大振幅 を示す
34 堀川晴央 水野清秀 佐竹健治 関口春子 加瀬祐子 杉山雄一 横田裕 末廣匡基 Arben Pitarka obs. 3D flatlayer 第 図. 観測波形と合成波形との比較 ( 大阪平野北部 ). 上 : 観測波形, 中 : 次元地盤構造モデルを使ったときの合成波形, 下 : 水平成層型の地盤構造を使ったときの合成波形. 波形は のバンドパスフィルターを通したもの. 各観測波形のトレース左側に付した数値は, 観測波形の最大振幅 を示す
断層による不連続構造を考慮した大阪堆積盆地の3次元地盤構造モデル
No. 3, p. 225-259, 2003 A three-dimensional subsurface structure model beneath the Osaka sedimentary basin, southwest Japan, with fault-related structural discontinuities 1 2 3 4 5 6 7 8 9 10 11 12 Arben
神奈川県西部山北南高感度地震観測井の掘削および孔内検層，Borehole Drilling and Physical Properties of the Yamakita-minami Seismic Observatory in Western Ka
*1 *2 *3 *4 *5 *5 *6 *6 *2 *7 *5 *4 *5 *5 *6 *6 Borehole Drilling and Physical Properties of the Yamakita-minami Seismic Observatory in Western Kanagawa Prefecture, Central Honshu, Japan Hiroki HAYASHI
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