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Geochemical and mineralogical characteristics of fault gouge in the Median Tectonic Line, Japan: evidence for earthquake slip

  • 1Email author,
  • 2,
  • 2,
  • 3,
  • 4,
  • 5, 6,
  • 7,
  • 2 and
  • 2
Earth, Planets and Space201466:36

https://doi.org/10.1186/1880-5981-66-36

  • Received: 13 November 2013
  • Accepted: 30 April 2014
  • Published:

Abstract

We carried out geochemical and mineralogical analyses on fault-zone rocks from the Anko section of the Median Tectonic Line in Nagano Prefecture, Japan, to investigate coseismic physicochemical processes in the fault zone. The latest fault zone in the Anko section contains cataclasite, fault breccia, and fault gouge of granitic composition, and brecciated basic schist. Protoliths of the granitic composition are from the Ryoke metamorphic belt and those of the basic schist from the Sambagawa metamorphic belt. X-ray diffraction analyses show a selective decrease of clay minerals coupled with an increase of amorphous phase in an intensely deformed layer of black gouge (5- to 10-cm thick). SEM observation reveals that the black gouge is characterized by a drastic reduction of grain size and abundant ultrafine particles of submicrometer to several tens of nanometers with well-rounded spheroidal shapes. These observations for the black gouge are indicative of strong mineral lattice distortion and granulation associated with earthquake slip. Geochemically, the black gouge is characterized by distinctly higher Li content and 87Sr/86Sr isotope ratio than surrounding cataclasites, breccias, and gouges, which have similar major element compositions. Model analysis reveals that the trace element composition of the black gouge is consistent with high-temperature (up to 250°C) coseismic fluid-rock interactions. Thermal and kinetic constraints indicate that there have been repeated slips on the fault at moderate depths (e.g., 600 m), although the tectonic process by which the fault zone has been uplifted and exposed in this area is not well understood.

Keywords

  • Active fault
  • Frictional heat
  • Fault gouge
  • Trace elements
  • Isotope ratios

Background

Transient frictional heating in a fault zone during earthquake slip affects the slip behavior itself. Increased temperature on a fault can induce dynamic fault weakening by processes such as pressurization of interstitial fluid by thermal expansion, known as thermal pressurization (Sibson 1973; Lachenbruch 1980; Andrews 2002), and melt lubrication (Sibson 1975; Fialko and Khazan 2005). Geochemical and mineralogical analyses of fault rocks combined with geological, structural, and geophysical observations can provide useful means for elucidating such slip-weakening processes. In the case of the Chelungpu fault in Taiwan, which slipped during the 1999 Mw 7.6 Chi-Chi earthquake (Ma et al. 1999), the slip-zone rocks show marked anomalies in both fluid-mobile trace element concentrations (Sr, Cs, Rb, and Li) and Sr isotope ratios that are consistent with fluid-rock interactions at >350°C (Ishikawa et al. 2008). Thermal signals recorded in the slip-zone minerals (Mishima et al. 2006; Hirono et al. 2007) and the low permeability of the fault zone (Doan et al. 2006; Tanikawa et al. 2009) strongly suggest that thermal pressurization took place during the earthquake (Ishikawa et al. 2008). Geochemical analyses of the slip-zone rocks accompanied with generation of pseudotachylite in an ancient megasplay fault in the Shimanto accretionary complex (Mukoyoshi et al. 2006) are also indicative of fluid-rock interactions at >350°C (Honda et al. 2011). These observations provide a key for gaining a detailed understanding of slip processes in the presence of pore fluids.

However, there have been few studies of coseismic geochemical and mineralogical processes in fault zones that have investigated both the geochemistry of high-temperature fluid-rock interactions and structural observations. Three of the previously studied faults are the Chelungpu fault (Ishikawa et al. 2008), the major thrust of the Boso accretionary complex, Japan (Hamada et al. 2011), and the ancient megasplay fault of the Shimanto accretionary complex, Japan (Honda et al. 2011). Lithology, stress, temperature conditions, maturation (repeated activity and slip accumulation) and tectonic history may influence which coseismic physicochemical processes occur in slip zones, and how they occur. The aforementioned three faults are within sedimentary rocks (mudstone and sandstone) and are considered to be branch faults from plate-subduction megathrusts or major thrusts within the accretionary prism near a megathrust (Ishikawa et al. 2008; Hamada et al. 2011; Honda et al. 2011).

In this study, we focused on a fault from the Anko section of the Median Tectonic Line (MTL) in Nagano Prefecture, Japan, an inland fault in rocks of different lithology from the previous studies. We examined the structural, geochemical, and mineralogical characteristics of the fault zone and surrounding rocks to assess the relationship of coseismic fluid-rock interactions and other physicochemical processes in the slip zone with earthquake slip.

Methods

Geological background and outcrop of the MTL at the Anko section

The MTL is a major crustal-scale fault that was first active in the Cretaceous. It has a strike length of >1,000 km and shows displacements of 200 to 1,000 km (Ichikawa 1980). The MTL is the dominant geological structure in southern Nagano Prefecture, where it strikes approximately N-S with subvertical dip and a left-lateral displacement of 60 km (Figure 1b). Collision of the Izu-Bonin arc of the Philippine Sea plate with the Eurasia plate at 27 to 15 Ma produced a counterclockwise rotation of the MTL to a NNE-SSW strike (Matsushima 1994).
Figure 1
Figure 1

Index map (a) and simplified structural map (b) in the region of the MTL in southern Nagano Prefecture.

The Anko section along the Aoki River (Figure 1b) exhibits the main boundary fault of the MTL strikes NNE-SSW with a subvertical dip, which separates the Ryoke and the Sambagawa belts (Figure 2; Kawamoto et al. 2013a). West of the boundary, the Ryoke belt rocks are cataclasites derived from granitic or gneissic mylonite and altered dark breccia. East of the boundary, the Sambagawa belt rocks are partly brecciated or cataclastic greenschist, pelitic schist, and serpentinite. However, the altered dark breccia of the Ryoke belt are displaced by a minor low-dip fault (Tanaka et al. 1996).
Figure 2
Figure 2

Simplified geological map of the Anko section of the MTL. See Figure 1 for location.

A previously unrecognized mesoscale fault, approximately 40 m west of and parallel to the main boundary fault, was exposed by floodwaters in the summer of 2010 (Figure 2). Because this fault has not been displaced by any subsequent deformations (Figure 3), we consider the fault to be the latest fault zone in the Anko section of the MTL. This fault zone contains, from east to west, orange-stained cataclasite (up to 1-m thick), gray breccia with some gouge (20- to 30-cm thick), black gouge (5- to 10-cm thick), gray-green gouge (15- to 20-cm thick), and brecciated greenschist extending to the west (Figure 3). The orange-stained cataclasite is partly brecciated with rounded clasts and is comminuted with weak foliation. The boundary between the cataclasite and the gray breccia is gradual, and the rounded clasts and elongated tails from the cataclasite are incorporated in the breccia, exhibiting a complex flow structure with isoclinal folds. The black gouge is highly foliated with a dense, closely spaced, dark network of seams. The gray-green gouge is foliated with composite planar fabrics accompanying the well-developed Riedel slip surface (R1-plane) described above. The fabrics indicate dextral shear deformation. The elongated clasts aligned with the R1-plane are derived from the adjacent gouge layers. The contact between the gray-green gouge and the brecciated greenschist is sharp and straight, corresponding to the Riedel shear Y-plane. There are serpentinite blocks within the brecciated greenschist.
Figure 3
Figure 3

Photographs of the most recently active fault zone in the Anko section of the MTL. White arrows indicate dextral sense of slip. Structural divisions of the fault-zone rocks and sampling points for mineralogical and geochemical analyses are also shown.

Sample collection

For mineralogical and geochemical investigation, we collected 12 samples from the fault zone: two from the orange-stained cataclasite, three from the gray breccia, one from the black gouge, two from the gray-green gouge, and four from the brecciated greenschist (samples FZ01 to FZ12 in Figure 3). Additional three samples were collected from the black gouge zone (samples FZ06b to FZ06d; up to 2 m from FZ06 but beyond the extent of Figure 3) for trace element and isotope analyses. We also collected some oriented samples from the fault zone for microscopic observations.

Microscopic observation

To observe the microscopic structures and fabrics in the fault zone, we used polarization microscope and scanning electron microscope (SEM: JSM-6500 F, JEOL, Tokyo, Japan) operated at an acceleration voltage of 10 kV. Thin sections were prepared to be the plane perpendicular to the mesoscopic foliation and/or structural zone boundaries. The samples for the SEM observation were prepared by being dispersed in ethanol and then dropped on the observation stage.

X-ray diffraction analysis

X-ray diffraction (XRD) with monochromatized CuKα radiation (Spectris PANalytical, X'Pert PRO MPD, Almelo, the Netherlands) was used to analyze the mineralogy of the samples. Each sample was gently powdered in an agate mortar. Part of each original sample was mixed with α-alumina (25 wt.%) for use as an internal standard. These samples were then mounted on XRD glass holders, side-loaded to minimize preferred alignment of phyllosilicates. XRD patterns were obtained with the spectrometer operated at 45 kV, 40 mA, 0.004° (Δ2θ) step width with 0.25° divergence, anti-scattering slits, and a high-speed semiconductor array detector. For quantitative determination of the mineral composition of the samples containing α-alumina, we used the RockJock program of Eberl (2003). The XRD patterns were compared with integrated XRD patterns of standard minerals stored in the RockJock program, and the weight percent of the component minerals in the samples was determined.

The XRD patterns of some samples on a zero diffraction plate, made from a single silicon crystal, were obtained under the same operating conditions at around 20° to 30° 2θ for evaluation of a broad bump caused by amorphous state.

The clay fraction (<2 μm) was separated by centrifugation from each of the bulk-powdered samples (without α-alumina). Oriented samples of the clay fraction were prepared by sedimentation onto glass slides in dry air. XRD patterns were obtained using the spectrometer operated under the same conditions as for the internal standard determinations. XRD analysis was also undertaken for the clay fraction saturated with ethylene glycol vapor. The relative abundances of kaolinite, smectite, illite, and chlorite were calculated by the method of Biscaye (1965).

Major and trace elements and Sr isotope analyses

Major element concentrations were measured with an X-ray fluorescence spectrometer (XRF: MagiX PRO, Spectris) using the conventional glass bead method. Trace-element concentrations were measured with an inductively coupled plasma mass spectrometer (ICP-MS: ELAN DRC II, Perkin Elmer) after sample decomposition with HF-HNO3. Sr isotope ratios were determined with a thermal ionization mass spectrometer (TIMS: TRITON, Thermo Finnigan, Bremen, Germany) after chemical separation of Sr using an ion-exchange resin column (Sr Resin, Eichrom, Lisle, IL, USA). Replicate analyses (N = 5) of the NIST SRM 987 Sr isotope standard during this study yielded a mean value (±2 SD) of 87Sr/86Sr = 0.710251 ± 0.000018. The trace element concentrations and Sr isotope data obtained for reference rock material Geological Survey of Japan JB-3 (Table 1) were consistent with the reported values (Geochemical reference samples database of Geological Survey of Japan: http://riodb02.ibase.aist.go.jp/geostand/).
Table 1

Major and trace element concentrations and Sr isotope ratio of the fault gouges and surrounding rocks

 

FZ01

FZ02

FZ03

FZ04

FZ05

FZ06

FZ06b

FZ06c

FZ06d

FZ07

FZ08

FZ09

FZ10

FZ11

FZ12

JB3

SiO2

67.47

66.75

67.50

70.98

72.06

62.97

   

64.23

63.31

42.09

44.57

46.57

45.89

 

TiO2

0.81

0.90

0.72

0.61

0.60

0.79

   

0.83

0.70

0.39

1.26

1.54

1.80

 

Al2O3

18.30

17.96

16.42

16.78

15.97

14.50

   

16.53

15.82

5.95

9.44

8.25

12.28

 

Fe2O3

5.02

5.69

5.41

3.89

3.24

7.65

   

6.60

5.08

13.35

14.84

13.86

14.89

 

MnO

0.09

0.10

0.12

0.09

0.06

0.13

   

0.10

0.12

0.17

0.18

0.17

0.16

 

MgO

2.33

2.49

2.90

1.94

2.21

6.84

   

3.18

2.67

33.98

22.21

20.80

15.26

 

CaO

3.20

2.93

3.78

1.98

2.12

4.13

   

2.79

5.96

3.88

6.83

7.77

7.45

 

Na2O

0.08

0.07

0.07

0.10

0.13

1.08

   

3.04

3.04

0.13

0.50

0.82

1.96

 

K2O

2.46

2.82

2.91

3.52

3.50

1.74

   

2.50

3.11

0.03

0.07

0.10

0.14

 

P2O5

0.23

0.29

0.15

0.10

0.10

0.18

   

0.20

0.19

0.03

0.09

0.12

0.18

 

Li

48.1

43.0

37.2

29.9

26.2

66.7

67.7

62.7

65.6

44.9

32.4

16.8

16.1

10.5

14.1

7.10

Be

0.958

1.15

1.19

1.09

1.33

1.52

1.41

1.52

1.84

1.34

0.926

0.179

0.230

0.409

0.344

0.612

Ti

4,330

4,770

3,860

3,400

3,300

4,070

4,360

3,930

4,490

4,680

3,720

1,920

6,650

8,420

8,340

8,300

V

97.7

111

89.0

75.8

82.9

107

109

102

117

120

100

92.1

275

282

319

406

Cr

14.5

16.8

61.3

38.5

76.1

332

384

374

324

25.1

14.6

1,740

1,090

981

591

54.8

Co

9.05

13.6

12.4

10.6

11.4

26.0

26.7

25.8

23.4

15.0

10.3

110

86.8

80.1

70.9

35.5

Ni

17.4

11.1

23.7

18.8

45.7

2,045

198

236

212

15.1

14.4

1,550

960

951

526

41.3

Cu

23.2

11.9

31.0

31.5

32.6

33.5

38.2

35.2

36.3

13.9

14.1

28.2

136

142

180

192

Zn

84.5

84.6

77.3

58.3

61.1

78.0

91.4

81.0

87.1

91.1

68.3

58.7

88.6

89.9

91.6

112

Rb

69.3

81.9

89.5

113

136

57.2

61.3

37.1

64.2

74.2

77.5

0.289

0.291

0.249

2.15

14.2

Sr

242

209

281

231

206

155

155

174

171

302

357

57.4

73.9

90.6

1,390

412

Y

10.1

12.2

13.9

17.5

17.7

16.1

19.0

18.0

18.4

10.5

12.7

3.6

11.5

13.1

18.5

23.7

Nb

7.94

9.34

12.3

14.4

13.4

10.1

10.2

9.43

10.4

9.64

8.11

0.63

2.30

3.27

6.94

1.95

Mo

0.48

0.45

1.38

0.97

1.91

0.71

1.03

0.841

0.760

0.34

0.31

1.25

0.17

1.46

1.13

1.05

Cs

19.3

23.8

23.3

30.7

72.6

18.8

22.1

12.4

18.2

14.9

15.2

0.367

0.329

0.191

0.443

0.945

Ba

197

218

243

337

329

314

241

254

328

485

506

10.0

10.0

14.0

59.0

236

La

32.6

35.1

28.8

33.7

31.8

21.8

23.4

23.1

20.9

15.8

21.4

1.20

2.70

4.40

7.30

8.22

Ce

63.4

67.9

60.0

68.9

66.1

45.1

50.2

49.0

44.4

34.4

41.9

3.10

8.20

13.3

18.9

21.0

Pr

7.00

7.20

6.58

7.41

7.22

4.98

5.68

5.51

5.12

3.96

4.67

0.454

1.34

2.15

2.75

3.15

Nd

24.6

26.8

24.8

27.6

26.6

19.4

22.3

21.1

20.1

16.2

18.1

2.50

7.40

11.1

13.9

16.0

Sm

4.25

4.79

4.80

5.15

5.00

3.84

4.47

4.16

4.21

3.17

3.61

0.680

2.38

3.10

3.80

4.13

Eu

1.16

1.27

0.98

0.99

0.96

0.94

1.01

0.983

1.05

0.76

0.89

0.25

0.81

1.08

1.33

1.33

Gd

3.31

3.79

3.85

4.26

4.06

3.36

4.15

3.94

3.83

2.73

3.04

0.835

2.68

3.28

4.24

4.70

Tb

0.435

0.512

0.565

0.588

0.590

0.485

0.593

0.551

0.549

0.382

0.437

0.126

0.411

0.504

0.660

0.730

Dy

2.22

2.64

2.86

3.29

3.43

3.11

3.51

3.37

3.21

2.18

2.48

0.797

2.61

2.89

4.02

4.72

Ho

0.378

0.443

0.529

0.637

0.657

0.581

0.696

0.669

0.651

0.426

0.431

0.142

0.472

0.559

0.772

0.900

Er

0.99

1.17

1.59

1.79

1.82

1.68

1.99

1.83

1.87

1.21

1.26

0.379

1.27

1.39

2.05

2.72

Tm

0.127

0.156

0.215

0.252

0.295

0.242

0.279

0.272

0.258

0.163

0.169

0.045

0.150

0.176

0.289

0.390

Yb

0.79

0.90

1.32

1.67

1.58

1.57

1.83

1.80

1.70

1.00

1.10

0.25

0.94

1.11

1.64

2.57

Lu

0.112

0.123

0.186

0.234

0.239

0.221

0.264

0.239

0.241

0.143

0.148

0.034

0.125

0.151

0.234

0.390

Ta

0.418

0.511

0.760

0.860

0.825

0.622

0.663

0.617

0.647

0.536

0.419

0.045

0.155

0.229

0.453

0.130

W

1.49

1.89

2.97

1.94

2.23

2.53

2.30

2.13

2.38

1.25

0.674

1.24

0.340

0.511

0.263

1.09

Tl

0.290

0.395

0.417

0.460

0.575

0.341

0.320

0.246

0.311

0.363

0.361

0.055

0.057

0.026

0.061

0.040

Pb

8.62

13.0

8.19

14.7

10.6

10.8

10.9

11.2

10.6

10.5

11.7

0.288

0.242

0.231

1.67

5.00

Th

6.44

7.43

11.8

16.3

15.8

6.46

7.29

6.88

6.55

4.05

4.55

0.049

0.155

0.251

0.680

1.34

U

0.667

0.655

1.56

1.88

1.84

1.11

1.28

1.26

1.08

0.819

0.442

0.014

0.029

0.039

0.207

0.483

87Sr/86Sr

0.707745

0.707876

0.707969

0.708416

0.708313

0.707812

0.708081

0.708114

0.707921

0.707038

0.707269

0.706611

0.704624

0.703684

0.703177

0.703420

The units for major elements and trace elements are weight percent and ppm, respectively.

Results

Microscopic structures and fabrics

The microscopic structures and fabrics of oriented samples from the fault zone were examined in thin section.

The orange-stained cataclasite is composed of abundant recrystallized quartz grains (<1 mm), which are partly displaced and fragmented by minor faults and surrounded by carbonate veins and a matrix of clay minerals (Figure 4a). The gray breccia is composed of an abundant matrix of clay minerals and carbonate cements supporting fragments of recrystallized quartz grains (Figure 4b). No intense foliation is evident in either of these rocks.
Figure 4
Figure 4

Microstructures in fault-zone rocks of most recently active fault zone in the Anko section of the MTL. (a) Orange-stained cataclasite, (b) gray breccia, (c) black gouge, (d) black gouge under cross-polarized light, (e) gray-green gouge, and (f) brecciated greenschist. c-vein, calcite vein.

In contrast, the black gouge exhibits highly intense foliation, indicated by the preferred orientation of grains (submicron to several tens of microns) of fragmented quartz, K-feldspar, plagioclase, carbonate minerals (veins), and clay minerals (Figure 4c,d). Anastomosing black seams, probably chlorite, are developed parallel to the foliation.

The gray-green gouge is composed of abundant fragmented grains of quartz, K-feldspar, and plagioclase accompanied by carbonate veins and a matrix of very fine-grained clay minerals (Figure 4e).

The brecciated greenschist shows mylonitic foliation, which is composed of amphibole porphyroclasts with tails and fish of clay minerals (Figure 4f). Very fine grains of serpentinite are locally observed in the brecciated greenschist.

SEM observation of the black gouge sample (Figure 5a,b) confirmed a drastic reduction of particle size compared with the surrounding gouge samples (Figure 5c,d). The particles in the black gouge sample ranged in size from submicrometer to several tens of nanometers and had well-rounded spheroidal shapes. However, such ultrafine particles were scarcely observed in the surrounding gouge samples.
Figure 5
Figure 5

Fine structure by SEM observation. (a, b) black gouge (FZ06), (c) gray breccia (FZ05), and (d) gray-green gouge (FZ07).

Mineralogical characteristics

XRD patterns of the bulk samples with internal standard (α-alumina) and clay fractions are shown in Figure 6, and bulk mineral compositions and clay mineral compositions, determined by the RockJock program and Biscaye analyses, respectively, are summarized in Table 2. Total percentages of minerals composited were approximately 83% to 109% except for sample FZ06 (71.8%).
Figure 6
Figure 6

XRD patterns of (a) bulk samples and (b) clay fractions of samples FZ01 to FZ12.

Table 2

Mineral compositions from X-ray diffraction data

 

FZ01

FZ02

FZ03

FZ04

FZ05

FZ06

FZ07

FZ08

FZ09

FZ10

FZ11

FZ12

RockJock's bulk mineral composition

Quartz

35.2

37.1

34.1

41.5

44.5

29.1

24.1

24.0

0.0

0.0

0.0

0.0

K-feldspar

0.0

0.0

0.0

0.0

0.0

5.0

0.0

15.4

0.0

0.3

0.0

1.2

Plagioclase

0.0

0.0

0.0

0.0

0.0

7.1

29.5

24.5

0.0

0.1

0.0

10.9

Dolomite

0.3

0.4

0.6

1.3

1.2

2.5

0.0

0.0

0.0

0.1

0.0

0.0

Ankerite

6.9

6.2

8.6

3.8

3.8

6.0

0.8

1.8

0.0

0.2

0.0

2.0

Siderite

3.3

4.1

3.8

2.9

1.2

0.0

0.4

0.1

0.0

0.0

0.0

0.0

Amphibole

0.0

0.0

0.0

0.0

0.0

0.0

0.0

0.0

3.0

31.8

50.9

28.9

Magnetite

0.0

0.0

0.0

0.0

0.0

0.0

0.0

0.0

4.3

1.0

0.0

1.4

Forsterite

0.0

0.0

0.0

0.0

0.0

0.0

0.0

0.0

3.6

0.6

0.0

0.0

Total non-clay

45.7

47.8

47.1

49.5

50.7

49.7

54.8

65.8

10.9

34.1

50.9

44.4

Serpentine

0.0

0.0

0.0

0.0

0.0

0.0

0.0

0.0

5.5

0.0

0.0

0.0

Kaolinite

19.0

15.4

11.2

6.0

2.4

0.0

0.0

1.8

0.0

0.0

0.0

0.0

Smectite

0.0

0.0

0.0

0.0

0.0

0.0

0.0

6.7

30.4

13.1

10.1

12.9

Illite

22.9

26.0

24.8

32.2

39.3

3.6

12.8

12.2

0.0

0.0

0.0

0.1

Chlorite

0.0

0.0

0.0

0.0

0.0

18.5

21.7

22.5

36.9

43.2

35.8

33.3

Total clay

41.9

41.4

36.0

38.2

41.7

22.1

34.5

43.2

72.8

56.3

45.9

46.3

Total

87.6

89.2

83.1

87.7

92.4

71.8

89.3

109.0

83.7

90.4

96.8

90.7

Biscaye's relative clay mineral composition

Kaolinite

8.5

6.8

8.5

1.7

1.8

0.0

0.0

1.5

0.0

0.0

0.0

0.0

Smectite

0.0

0.0

0.0

0.0

0.0

0.0

0.0

25.1

57.7

34.7

48.8

41.7

Illite

91.5

93.2

91.5

98.3

98.2

6.8

14.9

11.7

0.0

0.0

0.0

0.0

Chlorite

0.0

0.0

0.0

0.0

0.0

93.2

85.2

61.7

42.3

65.3

51.2

58.3

Total

100.0

100.0

100.0

100.0

100.0

100.0

100.0

100.0

100.0

100.0

100.0

100.0

The orange-stained cataclasite (FZ01 and FZ02) consists mainly of quartz, illite, and kaolinite, with small amounts of carbonate minerals (siderite and ankerite). Clay minerals are predominantly illite. The gray breccia (FZ03 to FZ05) also consists of mainly of quartz, illite, and kaolinite with small amounts of siderite and ankerite. Illite is the dominant clay mineral.

The black gouge (FZ06) consists of quartz, plagioclase, K-feldspar, chlorite, illite, and ankerite. XRD intensities for the clay fraction are relatively weak. The total mineral abundances (71.8%) estimated by the RockJock program are markedly lower in the black gouge than in the neighboring fault zone material.

The green-gray gouge (FZ07 and FZ08) also consists of quartz, plagioclase, chlorite, and illite with small amounts of ankerite and siderite. K-feldspar, kaolinite, and smectite were detected in only sample FZ08.

The brecciated greenschist (FZ09 to FZ12) consists mainly of amphibole and chlorite. Antigorite and lizardite were identified only in clasts incorporated in the schist (FZ09). Clay minerals in samples FZ09 to FZ12 are rich in chlorite.

The XRD patterns obtained by using the zero diffraction plate confirmed the presence of broad low bumps at around 20° to 30° 2θ in the black gouge sample but not in the surrounding gouge and breccia samples (Figure 7).
Figure 7
Figure 7

XRD patterns of samples on zero diffraction plates. These are compensated by subtracting the background intensity of the plate. Broad bumps at around 20° to 30° 2θ are shown by pink shading.

Geochemical characteristics and identification of protoliths

Major and trace element compositions and Sr isotope data obtained in this study are summarized in Table 1. Samples FZ01 to FZ08 (orange-stained cataclasite, gray breccia, black gouge, and gray-green gouge) show relatively high SiO2 and Al2O3 concentrations (about 63 to 71 and 15 to 18 wt.%, respectively), whereas samples FZ09 to FZ12 (brecciated greenschist) have low SiO2 concentrations and high Fe2O3 and MgO concentrations (about 42 to 47, 13 to 15, and 15 to 34 wt.%, respectively). Similar compositional contrasts between samples FZ01 to FZ08 and samples FZ09 to FZ12 are also apparent in other major and trace element concentrations (K2O, Cr, Ni, Rb, Cs, Ba, Pb, and Th) and in Sr isotope ratios (Table 1).

In the chondrite-normalized rare-earth element (REE) diagrams, samples FZ01 to FZ08 are clearly enriched in light REE (LREE), with weak to moderate negative Eu anomalies (Figure 8a). These REE patterns are typical of granitic rocks, and are consistent with those of Ryoke granites reported by Ishihara and Chappell (2007). Their high SiO2 and Al2O3 concentrations are also consistent with a diorite-granite composition.
Figure 8
Figure 8

Chondrite-normalized REE diagrams for (a) samples FZ01 to FZ08 and (b) samples FZ09 to FZ12. Chondrite values are from Sun and McDonough (1989). Data for the Ryoke granites in (a) and the Sambagawa greenschists in (b) are from Ishihara and Chappell (2007) and Honda et al. (1986), respectively.

In contrast, samples FZ09 to FZ12 are only moderately enriched in LREE. For these samples, REE patterns from La to Sm are flat or slightly depleted in La and Ce. REE concentrations of sample FZ09 are markedly lower than all other samples. These REE patterns (apart from sample FZ09) are consistent with those of normal or enriched mid-ocean ridge basalts (MORB) and MORB-type greenschists from the Sambagawa belt (Honda et al. 1986; Figure 8b). The low SiO2 and high MgO, Fe2O3, Cr, and Ni concentrations of these samples are also in accord with a basaltic origin. These observations suggest that samples FZ09 to FZ12 originated from accreted oceanic basalts. The extremely low REE concentrations of sample FZ09 can be attributed to entrainment of highly REE-depleted ultramafic clasts, which is supported by the high serpentinite content (Table 2) and very high MgO, Cr, and Ni concentrations in this sample.

The 87Sr/86Sr ratios of samples FZ01 to FZ08 (0.7070 to 0.7084) are consistent with those of Ryoke granites and gabbros reported previously (Kagami et al. 1985; Morioka et al. 2000; Okano et al. 2000; Kawamoto et al. 2013a). In contrast, samples FZ10 to FZ12 show distinctly low 87Sr/86Sr ratios (0.7032 to 0.7046), which accord with those of MORB (0.7021 to 0.7054; Hoffman 2003). The relatively high 87Sr/86Sr ratio (0.7066) obtained from sample FZ09 may reflect the involvement of an external source of Sr during serpentinization, or might be an aging effect. The high Rb/Sr ratio of this sample (0.0050, cf. 0.0015 to 0.0039 for samples FZ10 to FZ12) reflects a rapid increase with time of the 87Sr/86Sr ratio of the sample because of decay of 87Rb to 87Sr.

Thus, we concluded that the protoliths of samples FZ01 to FZ08 were the granitic rocks from the Ryoke belt and those of samples FZ09 to FZ12 were the greenschists of the Sambagawa belt.

Discussion

Anomalous mineral assemblage of the black gouge

The total mineral abundance (72%) estimated by RockJock analysis of XRD data for black gouge sample FZ06 was much lower than those of the surrounding deformed rocks (83% to 109%; Table 2). This reflects the markedly lower total clay mineral abundance (22%) of the black gouge than that of the surrounding Ryoke belt rocks (35% to 43%; Table 2). The XRD pattern of the black gouge, obtained by using the zero diffraction plate, confirmed the presence of broad low bumps at around 20° to 30° 2θ indicating the existence of amorphous phase (Figure 7). Furthermore, large amount of well-rounded spheroidal ultrafine particles ranging in size from submicrometer to several tens of nanometers, were observed only in the black gouge (Figure 5). Because weak X-ray diffraction intensity of minerals could be attributed not only to lattice distortions but also to reductions of particle size to the submicrometer to nanometer range (e.g., Lönnberg and Lundström 1994), the ‘missing’ mineral content in the XRD analysis of black gouge sample FZ06 could be attributed to the observed ultrafine particles.

Such features resemble the characteristics of the latest slip zone within the Taiwan Chelungpu fault that slipped during the 1999 Chi-Chi earthquake (Hirono et al. 2014). The transformation of clay minerals (kaolinite and chlorite-ripidolite) into fully amorphous particles of several tens of nanometers in size has been confirmed by milling experiments (Vdovic et al. 2010), and such amorphous ultrafine particles have also been produced by friction experiments using quartzite, granite, and diorite (Yund et al. 1990; Hirose et al. 2012; Hirono et al. 2013). The Chelungpu fault comprises three dominant fault zones (Hirono et al. 20062008), and the shallowest fault zone is most likely the one that slipped during the Chi-Chi earthquake because recent heating and a major stress-orientation anomaly were observed in that zone (Kano et al. 2006; Wu et al. 2007). Although aforementioned low total mineral abundance and ultrafine particles were observed in the latest slip zone of the Chelungpu fault, almost 100 wt.% total weight percentages of mineral abundance and no ultrafine particles were observed in all samples from two deeper fault zones. Hirono et al. (2014) suggested that amount of time elapsed after the 1999 Chi-Chi earthquake at the time that the samples were collected may have been insufficient for recrystallization to occur. Therefore, large amounts of ultrafine particles with weak X-ray diffraction intensity could be characteristics of the slip zone associated with the recent earthquake.

Taken together, the observations of this study and the results of previous studies suggest that anomalously low total mineral and total clay mineral abundances observed in the black gouge could be arisen from comminution during the recent earthquake.

Anomalous elemental and isotope compositions of the black gouge

The black gouge (FZ06), the most intensely deformed component of the fault zone, is developed within rocks of the Ryoke belt. To determine whether coseismic or interseismic processes are imprinted on the bulk chemical composition of sample FZ06, we need to examine the chemical heterogeneity of the original Ryoke belt rocks. The chemical composition of granitic rocks generally evolves as a result of differentiation of magma by crystal fractionation. Crystal fractionation causes systematic changes in the chemistry of the residual magma, and these changes reflect the affinities of different elements to the minerals that are crystallized. Therefore, the effect of magma differentiation on the Ryoke belt granitic rocks can be examined by using chemical variation diagrams. In Figure 9, major and trace element concentrations of the black gouge and various other samples are plotted against Ti, Nb, and Nd concentrations. The elements on the x-axis are chosen on the basis of their general solid/melt bulk distribution coefficients (or ‘incompatibility’) of elements in magmatic systems (e.g., Sun and McDonough 1989) and their fluid immobility. The data for samples FZ01 to FZ05, FZ07, and FZ08, which originated from Ryoke belt granitic rocks, show either positive or negative correlations in Figure 9. These trends (solid lines in Figure 7) are consistent with those of granitic rocks, suggesting that the chemical variations of these samples are largely inherited from the granitic source rocks, but with variable degrees of differentiation. The Sr isotope ratios of these rocks also correlate well with Nd concentrations, which can be attributed to the combined effect of magma differentiation and 87Sr/86Sr evolution with time.
Figure 9
Figure 9

Chemical variation diagrams for major and trace elements and Sr isotope ratios (a-l). These are for black gouge samples, Ryoke belt host rocks, and a Sambagawa belt rock (FZ10). Also shown are mixing lines between samples FZ10 and Ryoke belt rock sample FZ04, and for a 7:3 mixture of samples FZ04 and FZ10. Original Li value for a black gouge sample FZ06 is shown in (a) as an example of the estimated original values used in Figure 8.

The black gouge samples (FZ06, FZ06b, FZ06c, and FZ06d) are indistinguishable from other Ryoke belt samples in terms of concentrations of Ti, Nb, Nd, Cs, Ba, La, Sm, and Pb (Figure 9g,h,i,j,k). However, the black gouge samples are enriched in Li, MgO, Cr, and Ni, have a higher 87Sr/86Sr ratio, and are depleted in Rb and Sr (Figure 9a,b,c,d,e,f,l). Mg, Cr, and Ni are relatively fluid-immobile elements that are generally abundant in mafic rocks. As described in the previous section, the Sambagawa belt samples (FZ09 to FZ12) originated from basalt (with ultramafic clasts) and are highly enriched in these elements (Table 1). Thus, it is possible that the higher MgO, Cr, and Ni concentrations in the black gouge samples are the result of entrainment of small amounts of Sambagawa belt rocks. Indeed, the concentrations of MgO, Cr, and Ni (and of Sr, Cs, Ba, La, Sm, Pb, Ti, Nb, and Nd) in the black gouge samples can be explained by a source comprising about 70% Ryoke (FZ04) and 30% Sambagawa (FZ10) rocks (Figure 9). The SiO2, Al2O3, and Fe2O3 contents of the mixed product (63.1, 14.6, and 7.2 wt.%, respectively) are also comparable to those of sample FZ06 (63.0, 14.5, and 7.7 wt.%, respectively). We concluded that the chemical composition of the black gouge from this outcrop has been modified by entrainment of Sambagawa belt rocks during deformation associated with MTL activity.

Even if the effect of source-rock mixing is taken into account, the concentrations of Li and Rb and the Sr isotope ratio of the black gouge samples remain anomalous (Figure 7). Li, Rb, and Sr are known to be fluid-mobile elements, and mobilization and isotope exchange of these elements by coseismic high-temperature fluid-rock interactions has been recognized in the slip zones of the faults of Chelungpu, Boso, and Shimanto (Ishikawa et al. 2008; Hamada et al. 2011; Honda et al. 2011).

To quantify the possible enrichment or depletion of elements in the black gouge samples as a result of fluid-rock interactions, we estimated the source-rock compositions of the FZ06 samples. Here, we assumed that the original trace element composition of the precursor to the black gouge lay along the mixing line between samples FZ04 and FZ10, which best explains the fluid-immobile major and trace element characteristics of the FZ06 samples (Figure 9). Then, by assuming that Ti, Nb, and Nd were immobile during fluid-related processes, we estimated the original element concentrations in each FZ06 sample according to the mixing line (see Figure 9a). The trace element concentrations of the FZ06 samples normalized to their inferred original values are shown in Figure 10. Considering the heterogeneity of the Ryoke belt rocks (1 SD error bars in Figure 10), only the normalized values for Li, Be, Zn, W (and some Rb values), and the 87Sr/86Sr ratio deviate markedly from the inferred original values. The enrichments of Li (130% to 160%), Be (80% to 130%) and 87Sr/86Sr ratio (90 × 10−3% to 130 × 10−3%) are considerable. It is possible that these enrichments have been overestimated because of uncertainty about the composition of the Sambagawa belt rocks entrained in the black gouge. If we define the compositional anomaly as the deviation from the magma differentiation trends of the host Ryoke belt rocks (solid lines in Figure 9) rather than the deviation from the FZ04 to FZ10 mixing line, then the enrichments of Li, Be, and 87Sr/86Sr are 51% to 75%, 25% to 63%, and 57 × 10−3% to 79 × 10−3%, respectively, which are still considerably beyond the heterogeneity of the host rocks shown in Figure 10. Considering the generally low Li and Be concentrations and the low 87Sr/86Sr ratios of the Sambagawa belt rocks (Table 1), the estimated enrichments based on the magma differentiation trend should be regarded as lower limits.
Figure 10
Figure 10

Trace element and Sr isotope compositions of black gouge samples normalized to original values. Original values were estimated from mixing lines between samples FZ04 and FZ10, and Ti, Nb, and Nd concentrations of black gouge samples. Relative deviation (%) of each element concentration from the original value was calculated as follows: [(Concentration in black gouge − Original value)/Original value] × 100. Error bars indicate standard deviations from the data for Ryoke belt host rocks and are representative of the chemical heterogeneities of source rock compositions.

The above chemical characteristics of the black gouges could be produced by preferential uptake or extraction of elements associated with fluid-rock interactions. The enrichments of Li and 87Sr/86Sr observed here for MTL black gouge samples contrast strikingly with depletions of Li and 87Sr/86Sr observed in the Chelungpu fault black gouges (Ishikawa et al. 2008). These differences imply that fluid-rock interactions occurred under considerably different conditions in the two regions.

Element distribution modeling for high-temperature fluid-rock interactions

To quantify the effect of fluid-rock interaction in the black gouge, we applied the simple model of Ishikawa et al. (2008). Assuming chemical equilibrium, the solid/fluid bulk distribution coefficient (Kd) of a trace element is defined by
Kd = C s C f
(1)
where Cs and Cf are element concentrations (ppm) in the solid and fluid, respectively. Here, we assume interaction of a solid with a single batch of fluid. When we define the fluid/solid mass ratio, R, mass balance requires that
C s + R C f = C s 0 + R C f 0
(2)
where Cs0 and Cf0 are the element concentrations in the solid and fluid, respectively, prior to solid-fluid interaction. From Equations 1 and 2, we obtain
C s = Kd C s 0 + R C f 0 R + Kd
(3)

from which we can calculate the trace element concentration of the solid after interaction with the fluid.

Sr isotope ratios in solids and fluids are identical under equilibrium conditions, so the Sr isotope ratio in the solid after interaction with the fluid, (87Sr/86Sr)s, is given by
S 87 r / S 86 r s = S 87 r / S 86 r s 0 C s 0 Sr C s 0 Sr + R C f 0 Sr + S 87 r / S 86 r f 0 R C f 0 Sr C s 0 Sr + R C f 0 Sr
(4)

where (87Sr/86Sr)s0 and (87Sr/86Sr)f0 are the Sr isotope ratios in the solid and fluid, respectively, prior to solid-fluid interaction.

In our calculations, we used the estimated original values of the FZ06 samples (Figure 10 and Table 3) for Cs0 and (87Sr/86Sr)s0. For realistic calculations, however, the values of Kd, Cf0, and (87Sr/86Sr)f0 appropriate for the MTL fault are also required. Kd can be estimated on the basis of the results of a hydrothermal experiment for sediments from the Escanaba Trough by James et al. (2003). Although the MTL is not a sediment-hosted fault system, the chemical and mineral compositions of the granite-derived fault gouges of our study are similar to those of James et al. (2003) - hemipelagic-terrigeneous sediments with SiO2 = 59.3 wt.%, Al2O3 = 14.1 wt.%, Fe2O3 = 6.43 wt.%, CaO = 4.23 wt.%, and K2O = 1.96 wt.%. Thus, it is reasonable to apply the sediment-based Kd values to our model calculations. The Kd values estimated for temperatures of 100°C, 150°C, 200°C, 300°C, and 350°C are shown in Table 3. We estimated values of Cf0 and (87Sr/86Sr)f0 from the compositions of surface flows from natural mineral springs along the MTL. Spring waters from Kashio (Figure 1) are representative of those along the MTL. They are saline, with Arima-type chemical compositions (e.g., Hashizume 1984), and are thought to be derived from deep in the crust or from the subducting slab (Kawamoto et al. 2013b). Major and trace element analyses by ICP-MS and ICP-AES of spring waters from Kashio, Toyama (20 km southwest of Anko), and Yamamuro (35 km north of Anko) revealed tight linear correlations of trace element concentrations with Na concentrations (Figure 11), suggesting that these MTL fluids share similar chemical characteristics that are essentially controlled by mixing of saline end-component fluids with meteoric water. Here, we used a moderate fluid composition with a Na concentration of 1,000 ppm (Figure 11) estimated from Kashio spring water to calculate Cf0 and (87Sr/86Sr)f0 values (Table 3). The fluid so estimated is characterized by a much higher Li/Na ratio (7.3 × 10−3) than that of seawater (1.5 × 10−5).
Table 3

Parameters used for modeling of trace-element compositions and Sr isotope ratio of the black fault gouge

 

Kd

C f0

Cs0FZ06

Cs0FZ06b

Cs0FZ06c

Cs0FZ06d

100°C

150°C

200°C

250°C

300°C

350°C

(ppm)

(ppm)

(ppm)

(ppm)

(ppm)

Cs

1,800

440

180

92

59

26

0.0085

19.9

20.2

18.2

20.7

Rb

423

210

120

81

67

25

0.039

72.7

73.9

66.5

75.5

Ba

130

89

52

20

17

14

4.7

221

224

203

229

La

15,000

80,000

19,000

41,000

47,000

26,000

0.00007

22.7

23.0

21.0

23.5

Pb

10,000

13,000

4,500

1,900

350

110,000

0.00079

9.53

9.68

8.74

9.89

Sr

26

22

19

16

17

20

9.5

167

190

181

172

Sm

140,000

81,000

19,000

41,000

47,000

26,000

0.00008

4.16

4.19

4.01

4.23

Li

100

53

32

15

8.4

2.8

7.3

27.0

25.8

27.6

25.2

87Sr/86Sr

-

(87Sr/86Sr)f0

(87Sr/86Sr)s0

(87Sr/86Sr)s0

(87Sr/86Sr)s0

(87Sr/86Sr)s0

0.70917

0.70689

0.70743

0.70721

0.70701

Kd values of Cs, Rb, Ba Sr and Li are calculated from James et al. (2003). Kd values for other elements are from You et al. (1996).

Figure 11
Figure 11

Various element concentrations versus Na concentration for MTL mineral spring waters. Estimated composition of MTL fluid (Na = 1,000 ppm) used for model calculations is also shown. La and Sm values for Toyama and Yamamura samples and La values for two Kashio samples were below detection limits.

If the values of Cs0, Cf0, (87Sr/86Sr)s0, and (87Sr/86Sr)f0 are constant (Equations 3 and 4), the calculated composition of the rock after interaction with the fluid is dependent on the Kd values and the fluid/solid mass ratio R. Because Kd for each element varies as a function of temperature, the calculated composition depends on both temperature and R. The results of calculations for temperatures of 100°C, 150°C, 200°C, 250°C, 300°C, and 350°C are shown in Figure 12. These calculations indicate that Li concentrations and 87Sr/86Sr ratios would have been preferentially elevated in the black gouge by interaction with fluids at temperatures between 100°C and 250°C. The calculated compositions best fit the observed values for sample FZ06 (red solid circles in Figure 12) at 150°C and R = 7, at 200°C and R = 8, and at 250°C and R = 14. At temperatures higher than 300°C, increases of the Li deviation are restricted by the rapid decrease of KdLi with increasing temperature (Table 3). When we use the minimum values for Li and 87Sr/86Sr estimated for the FZ06 samples (red open circles in Figure 12; deviation from the magma differentiation trends of the host Ryoke belt rocks), they best fit the calculated values at 250°C and R = 4. Even if we modify the Cf0 values along the trends defined by the data for MTL fluids (Figure 11), the calculation results are essentially similar and the best-estimated R value varies according to the value of Cf0. Calculations using a suite of Kd values from experimental hydrothermal data from Nankai Trough sediments (You et al. 1996) also gave similar results. These modeling results therefore suggest that the chemical characteristics of the black gouge are a result of fluid-rock interactions at temperatures up to 250°C.
Figure 12
Figure 12

Calculated trace element and Sr isotope compositions of black gouge at 100°C to 350°C for various fluid/solid ratios (a-f). Values are normalized to original values as describe in Figure 8 caption. Red solid circles with thick error bars are average values for FZ06 samples and their standard deviations. Red open circles represent minimum Li and 87Sr/86Sr enrichments in the FZ06 samples (see text). Thin error bars represent chemical heterogeneities of source rock compositions as in Figure 8.

Our XRD analysis also shows that black gouge sample FZ06 contained K-feldspar and chlorite (Figure 6 and Table 1), which are typical secondary minerals formed by hydrothermal alteration. The development of black chlorite-bearing seams within the intense foliation in the black gouge indicate that chlorite was precipitated during or after shearing. Jefferies et al. (2006) also reported precipitation of fibrous chlorite within MTL cataclasites at the onset of grain-scale brittle deformation. These results and observations support the scenario for occurrence of high-temperature fluids in the black gouge inferred from geochemical data.

The temperatures of up to 250°C during fluid-rock interactions in the black gouge are unlikely to have been attained without earthquake-associated frictional heating or influx of a hot transient pulse of fluid, which could result from post-seismic discharge from deep rupture zones. The occurrence of fluid-induced geochemical anomaly is restricted within the black gouge zone that is characterized by a large amount of ultrafine particles and weak X-ray diffraction intensity. This strongly suggests that the high temperature resulted from earthquake slip. Although the fluid-rock interactions require some local flow or circulation of fluids, lack of extensive veins developed along the black gouge zone (Figure 3) is indicative of fluid-rock interactions induced by frictional heating, not by the hot transient pulse of fluid or hydrothermal alteration at the depths.

Kinetic evaluation of the geochemical signals recorded in the black gouge

When coseismic fluid-rock interactions take place in a fault zone, the rocks in the fault zone may not record clear geochemical signals of these interactions. This is because the duration of a single earthquake event may be shorter than the time required for such reactions to take place, particularly if reaction rates are slow because of relatively low temperatures. Thus, kinetic effects must be taken into consideration to achieve a rigorous evaluation of fluid-rock interactions during an earthquake (e.g., Ishikawa et al. 2008). The degree to which fluid-solid chemical (isotopic) equilibrium (F) is achieved according to Beck et al. (1992) is
F = 1 exp C s C f A M kt
(5)

where Cs/Cf is the ratio of a trace element concentration in the solid to that in the fluid, A/M is the ratio of solid surface area to fluid mass, k is the reaction rate, and t is time. Only limited data are available for k values associated with trace element equilibration. The reported k values for Sr isotope exchange during calcite recrystallization at 300°C, 350°C, and 400°C are 4.68 × 10−9, 2.82 × 10−8, and 1.32 × 10−7 mol m−2 s−1, respectively (Beck et al. 1992), and the extrapolated k value at 150°C is 1.62 × 10−12 mol m−2 s−1. We derived a value of 19 for Cs/Cf from the Cs0 and Cf0 values for Sr in Table 3, and estimated A/M by assuming A = 3.23 × 107 m2 m−3, the value determined by Ma et al. (2006) for fault gouge from the Chelungpu fault, and 10 MPa fluid pressure and 20% porosity.

Element partitioning within the fault zone may be controlled by complicated processes that reflect the interaction of fluids with multiple mineral phases, and it is not clear what F values we require to detect the geochemical signal derived from fluid-rock interactions. However, if the parameters we assumed here are valid, then 99%, 90%, and 50% equilibrium can be achieved at 250°C in 2.1 × 103, 1.1 × 103, and 3.3 × 102 s, respectively; at 200°C in 3.0 × 104, 1.6 × 104, and 4.9 × 103 s, respectively; and at 150°C in 7.8 × 105, 4.2 × 105, and 1.3 × 105 s, respectively. Thus, near- or quasi-equilibrium requires heat for a longer duration than can be provided by a single earthquake event, especially the durations required at temperatures of 200°C and 150°C. Although the temperature in a fault during a single earthquake event varies with time in response to frictional heating and heat conduction, because k decreases rapidly as cooling proceeds, it is likely that only the geochemical signals that represent the peak temperatures reached are recorded in the fault rocks.

Here, we have assumed that repeated earthquake events simply result in an increase of the net reaction time for fluid-rock interactions. Figure 13a,b,c shows the relationships between the number of earthquake events and the heat duration required to attain F of 0.99, 0.90, 0.50, and 0.20 at constant temperatures of 250°C, 200°C, and 150°C. Even if we assume events of relatively long duration, for example 5 min each, 90% equilibrium requires 4, 53, and 1,400 earthquake events at temperatures of 250°C, 200°C, and 150°C, respectively. Thus, it is clear that the geochemical anomaly in the black gouge requires multiple earthquake events, unless the reaction rate in the MTL fault was considerably faster than our estimates. Although the MTL activity in this area has not been well understood, if the occurrence of thousands of earthquake events in this fault zone is unrealistic, earthquake events at temperatures higher than 200°C are required.
Figure 13
Figure 13

Relationships between heat duration and number of earthquake events (a- c) and between slip displacement and depth (d-f). (a- c) F = 0.20, 0.50, 0.90, and 0.99 at temperatures of 150°C, 200°C, and 250°C. (d,e,f) These parameters are required to attain temperatures of 150°C, 200°C, and 250°C by frictional heating.

It should be noted that the achievement of fluid-rock near-equilibrium in a short time period requires very large solid surface area. For instance, if we assume smaller A of 1.0 × 106 m2 m−3, which represents the value for very fine-grained sediments, it takes much longer time, 1.4 × 104 and 2.0 × 105 s at 250°C and 200°C, respectively, to achieve 90% equilibrium with the same parameters described above. This implies that fluid-rock interactions coupled with dynamic production of ultrafine solid grains as well as frictional heating during the earthquake slip are essential to satisfy the physicochemical condition under which the high-temperature geochemical signals as observed in the black gouge become detectable.

Earthquake slip along the MTL at the Anko section

The tectonic conditions under which temperatures of 150°C to 250°C are reached during earthquake slip can be simply constrained by the relationships among depth, slip displacement, and frictional coefficient in the fault gouge. Here, we assumed 2.70 g cm−3 bulk density, 1.20 J g−1 K−1 specific heat capacity, no thermal diffusion, 30°C km−1 geothermal gradient, 15°C ground-surface temperature, and hydrostatic confining stress (normal stress on the slip zone equal to overburden stress). The combinations of depth and slip displacement required to attain temperatures of 150°C, 200°C, and 250°C for friction coefficients 0.30 and 0.15 are shown in Figure 13d,e,f. For frictional heating of 200°C to 250°C, slip displacement of more than 15 m is required at shallow depths (e.g., 200 m), whereas a shorter displacement of <10 m would attain higher temperatures at greater depth (e.g., 600 m). Considering that other recent inland earthquakes have not had displacements as large as 15 m (e.g., 2008 Wenchuan earthquake, approximately 8 m, Yagi et al. 2012;; 1999 Chi-Chi earthquake, approximately 8 m, Shin and Teng 1999 Chi-Chi earthquake, approximately 8 m, Shin and Teng ; 1999 Chi-Chi earthquake, approximately 8 m, Shin and Teng 2001), past earthquakes in the Anko section of the MTL have probably been caused by a small number of relatively short displacements (<10 m) at moderate depths (e.g., 600 m). However, there is as yet no geological evidence to explain how fault zones viewed today in outcrop have been uplifted from such depths to the surface. It can be speculated that uplift at approximately 4 mm year−1 during the Quaternary in and around the Akaishi Mountain Range (Chichibu Belt in Figure 1) caused by the Izu-Honshu collision (e.g., Dambara 1971) might have affected the Anko section of the MTL.

On the other hand, it is possible that high-temperature fluids might have triggered thermal pressurization during earthquakes in the Anko section of the MTL. An experimental evaluation by Wibberley and Shimamoto (2005) of hydraulic properties of fault-zone rocks from the Tsukide section of the MTL (Mie Prefecture) suggested that thermal pressurization likely occurred in the fault gouge there. This mechanism might also have affected the most recently active fault zone in the Anko section, but there are insufficient data on the hydraulic properties for the black gouge and surrounding rocks there to evaluate this possibility.

Conclusions

Our field and microscopic observations, mineralogical and geochemical analyses, modeling of fluid-rock interactions, and kinetic evaluation of geochemical data have shown that the black gouge within the most recently active fault in the Anko section of the MTL has been subjected to selective distortion of crystalline structure and granulation in clay minerals and high-temperature (up to 250°C) fluid-rock interactions associated with earthquake slip.

Our results demonstrate that the analytical approach and modeling we used are useful for investigations of earthquake slip, not only for sediment-hosted thrusts at subduction boundaries (Ishikawa et al. 2008; Hamada et al. 2011; Honda et al. 2011), but also for active inland granite-hosted faults. We have shown that in faults that define geological boundaries, entrainment of different types of rocks (granite versus basalt in this study) in slip zones must be taken into account during analysis and modeling. Our modeling also indicates that Arima-type fluids from depth might have been involved in earthquake slip on the MTL.

However, to more accurately evaluate the geochemistry of coseismic fluid-rock interactions on the MTL, experimental data are needed on the hydrothermal properties of black gouge from the MTL. The remarkably low abundances of total minerals and total clay minerals from XRD analyses of the black gouge probably indicate that insufficient time has elapsed since the most recent earthquake event to allow neocrystallization of clay minerals to occur. Further studies are needed on the kinetics of neocrystallization of minerals after distortion and amorphization by frictional forces.

Declarations

Acknowledgements

We thank J. Matsuoka and K. Nagaishi for their work on chemical analyses. We also thank two anonymous reviewers and Editor C. Rowe for their constructive comments. This work was supported by Grants-in Aid for Science Research from MEXT and JSPS.

Authors’ Affiliations

(1)
Kochi Institute for Core Sample Research, Japan Agency for Marine-Earth Science and Technology (JAMSTEC), 200 Monobe-otsu, Nankoku Kochi 783-8502, Japan
(2)
Department of Earth and Space Science, Graduate School of Science, Osaka University, Toyonaka, Osaka 560-0043, Japan
(3)
Oshika Museum of Japan Median Tectonic Line, Oshika, Nagano 399-3502, Japan
(4)
Faculty of Education, Tokyo Gakugei University, Koganei, Tokyo 184-8501, Japan
(5)
Department of Earth and Planetary Science, Graduate School of Science, The University of Tokyo, Bunkyo-ku, Tokyo 113-0033, Japan
(6)
Department of Natural History Science, Graduate School of Science, Hokkaido University, Kita-ku, Sapporo 060-0810, Japan
(7)
Research and Development Center for Submarine Resources, JAMSTEC, Yokosuka Kanagawa, 237-0061, Japan

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