Can clay minerals account for the behavior of non-asperity on the subducting plate interface?
© Katayama et al. 2015
Received: 6 May 2015
Accepted: 2 October 2015
Published: 9 October 2015
Seismicity along the subducting plate interface shows regional variation, which has been explained by the seismic asperity model where large earthquakes occur at strongly coupled patches that are surrounded by weakly coupled regions. This suggests that the subduction plate interface is heterogeneous in terms of frictional properties; however, the mechanism producing the difference between strong and weak couplings remains poorly understood. Here, we propose that the heterogeneity of the fluid pathway and of the spatial distribution of clay minerals plays a key role in the formation of non-asperity at the subducting plate interface. We use laboratory measurements of frictional properties to show that clay minerals on a simulated fault interface are characterized by weak and slow recovery, whereas other materials such as quartz show relatively quick recovery and thereby strong coupling on the fault surface. Aqueous fluids change the mineralogy at the plate interface by producing clay minerals due to hydrate reactions, suggesting that the hydrated weakly coupled regions act as a non-asperity and form a barrier to rupture propagation along the plate boundary at the depths of seismogenic zone.
KeywordsFrictional healing Clay minerals Seismic asperity Subducting plate interface
A plate-boundary earthquake at a subduction zone represents the slip between the subducting and overriding plates, and therefore, differences in the level of seismicity can be attributed to differences in the strength of mechanical coupling at the subducting plate interface (Kanamori 1986). Strongly coupled regions are termed asperity, which ultimately released seismic energy through large megathrust earthquakes due to slip concentration, whereas the weakly coupled regions are known as non-asperity and show slow and continuous slip (e.g., Lay et al. 1981; Beroza and Ide 2011). This asperity model suggests that the subduction plate interface is heterogeneous in terms of the strength of mechanical coupling; however, the mechanism that generates the spatial difference between strong and weak couplings remains unclear.
Laboratory experiments have shown that the frictional strength of fault materials under stationary contact increases with holding time, and this healing process is likely to make an important contribution to the recovery of fault strength during the period between successive seismic cycles (e.g., Marone 1998; Beeler et al. 2001). This recovery process could be different in fault materials, such as reported for the San Andreas Fault, which shows weak or no frictional healing due to the presence of clay minerals, resulting in the mechanical weakness of this active tectonic fault (Carpenter et al. 2011). The alteration of materials at the plate interface by aqueous fluids could form clay minerals, which could in turn contribute to a weakening of the mechanical coupling at the subducting plate interface. To test this hypothesis, we systematically measured the frictional healing of clay minerals in the presence of water, on which basis we examine whether the frictional properties of clays can account for the weakly coupled regions at the subducting plate interface.
Chlorite and saponite are common alternation products of basaltic rocks (e.g., Kameda et al. 2011), and illite is frequently recognized in the pelagic sediments that cover oceanic crust (e.g., Underwood 2007). We therefore used these clay minerals for frictional experiments to examine time-dependent frictional healing. Rochester shale was used as the illite-rich simulated gouge. This shale contains 60 % illite, 9 % kaolinite, 20 % quartz, and minor plagioclase (Saffer and Marone 2003). The saponite and chlorite samples are monomineralic. The saponite samples were synthesized by Kunimine Industries, Japan, and the chlorite samples were collected as clinochlore megacryst from the Korshunovskoe mine, Russia. We also tested quartz powder for comparison with the clay minerals. Illite and chlorite were prepared by crushing in a disk mill to produce powders with grain size <75 μm. These powders, along with the original powders of saponite and quartz with grain <50 μm, were used for the friction experiments. These samples were kept in a desiccator at 70 °C for 48 h before experiments. Each of the powdered materials (2.0–2.5 g) was sandwiched between blocks; the thickness of the simulated gouge layer was approximately 0.5 mm in each experiment.
We conducted a series of slide-hold-slide frictional experiments using a biaxial frictional testing machine at Hiroshima University, Japan. The powdered samples were placed on the simulated fault surface between gabbro blocks, and two side blocks and central block were placed together to produce a double-direct shear configuration (Additional file 1: Figure S1). A normal stress of 15 MPa was applied via a hydraulic press on the side blocks, and then shear stress was applied by advancing the central block downward at a constant velocity of 3 μm/s. Similar experiments were reported for serpentine gouge in Katayama et al. (2013). The electromagnetic transducer monitored axial displacement, which was corrected by the machine stiffness (4.4 × 108 N/m). The total axial displacement was limited to 20 mm in our assembly (Additional file 1: Figure S1), and we usually started the slide-hold-slide test after 10 mm displacement achieving the steady-state friction. Mechanical data were recorded by data logger (KYOWA EDX-100A) with a sampling rate of 10 Hz. The friction coefficient was calculated from the shear stress divided by the normal stress, assuming zero cohesion. In addition to dry conditions, we performed frictional experiments under wet environments using a water tank to assess the effect of water on frictional healing, where water chemistry was controlled by pure (distilled) water or 0.5 mol/L NaCl solution.
In the experiments, the axial loading was interrupted for periods ranging from 10 to 3000 s after steady-state friction, and we measured the difference between the steady-state friction and the peak friction after each holding period. Friction under stationary contact is known to increase with the logarithm of time as follows: μ(t) = μ 0 + b log(t), where μ 0 is the friction at the beginning of stationary contact, t is holding time, and b is the healing rate (Marone 1998).
Condition and result of frictional experiments
Dry or wet
Normal stress (MPa)
Loading velocity (μm/s)
Wet (pure water)
Wet (0.5 M NaCl)
Wet (pure water)
Wet (0.5 M NaCl)
Wet (pure water)
Wet (0.5 M NaCl)
Wet (pure water)
Wet (0.5 M NaCl)
After each holding period, the peak friction decayed to the steady-state friction when the axial piston was advanced. Quartz displays oscillatory and transient variation in frictional behavior at times after the peak friction has been attained, whereas the experiments on clay minerals show a continuous decay from peak friction to the steady-state value (Fig. 3). The transient distance from the peak to steady-state friction seems to be systematically different between quartz and clay minerals, in which clay minerals tend to exhibit a large slip-weakening distance.
Mechanism of frictional healing of clay minerals
Our experiments indicate that frictional healing varies with mineralogy in the simulated faults. In particular, clay minerals are characterized by a low healing rate. Similar weak healing has been reported in clay-rich natural fault materials from the San Andreas Fault (Carpenter et al. 2011) and from the Zuccale Fault in central Italy (Tesei et al. 2012). Serpentines, the products of mantle hydration, have also been reported to exhibit a low healing rate and large slip-weakening distance (Katayama et al. 2013).
The time-dependent healing of frictional strength is thought to result from changes in the contact area along a fault surface (Dietrich 1972). At the microscopic scale, it is the normal stress applied at a contacting asperity that represents the actual contact area on a fault surface, meaning that the local stress can be significantly higher than the macroscopic stress, resulting in creep at the point contact. The area of indentation has been observed to increase with the logarithm of time (e.g., Dieterich and Conrad 1984), and the evolution of contacting asperities has been directly observed in optically transparent materials (Dietrich and Kilgore 1994). This indicates that the observed difference in healing between quartz and clay minerals could be caused by the creep strength of clay minerals, in which clay minerals are characterized by a markedly small yielding stress, several orders of magnitude smaller than that of quartz (Shen et al. 2004). Although the weak creep strength of clay minerals means that their real contact area can easily increase over time, the shear stress needed to break the contact could be much smaller than that for quartz. The rapid growth of creeping asperities in clay-rich faults causes a near saturation in contact surface area after only a short period of time. This mechanism could explain the low healing rate in the simulated clay faults.
The healing tests of clay minerals are also characterized by the relatively large transient distance after peak to steady-state friction. The sliding of fault surface after stational holding results in the asperity contact of prior state to be removed, and the new population of contact reaches to a steady state after slip over a characteristic distance. This suggests that the transient distance from peak to steady-state frictions relates to the actual contact dimension (e.g., Scholz 2002). The relatively large slip-weakening distance found in clay minerals is therefore attributed to the extended real contact area.
As temperature increases along subduction, healing processes might be enhanced by thermally activated creeping, particularly under hydrothermal conditions. Nakatani and Scholz (2004) conducted experiments under hydrothermal conditions to examine the frictional healing of quartz. They showed that the frictional healing under hydrothermal conditions is controlled mainly by fluid-assisted solution transfer processes. Although the pressure solution creep is unlikely to operate in our room temperature experiments, it might be important for healing processes in natural fault zones.
Implications for the subducting plate interface
Clay minerals are frequently observed in the sediment layers of incoming plates into subduction zones and are commonly recognized in drill cores recovered from accretionary prisms (e.g., Underwood 2007). In the shallow part of a subduction zone, the plate boundary is poorly coupled due to the presence of unconsolidated sediments, meaning that earthquakes are rare in these regions. However, slip along the subducting plate can occasionally occur at close to the trench, which generates tsunami by seafloor displacement (e.g., Satake and Tanioka 1999). Although regions predominated by clay minerals cannot accumulate a large elastic strain, the frictional weakness of such layers might enhance the rupture propagation at shallow parts of subduction zones. In fact, the samples recovered from the Japan trench show a dynamic weakening during high-velocity rotary experiments, which can explain shallow slip and heat anomalies in the slip zone during the Tohoku-oki earthquake (Ujiie et al. 2013).
Along subduction zones, the layer of clay minerals becomes dehydrated as temperature increases (e.g., Moore and Vrolijk 1992), and this layer is also trapped by hanging-wall crust due to tectonic erosion (e.g., Hilde 1983). Seismic reflection surveys show that the decollement step-down to the top of the subducting oceanic basement in the Nankai accretionary wedge due to underplating of the sediment layer (Park et al. 2002). Consequently, it is possible that the hydration state of relatively deep plate boundaries and seismogenic zones is controlled mainly by fluid supply and migration from the subducting oceanic crust (e.g., Hyndman and Peacock 2003). Seismic velocities and attenuation beneath the forearc regions of northeast Japan indicate a highly heterogeneous fluid distribution along the plate boundary that may be spatially correlated with the occurrence of repeated large earthquakes (Zhao 2015).
Our experimental results indicated that the recovery of fault strength differs according to materials, in which clay minerals show weak and slow recovery. In the regions of extensively hydrated plate boundaries that produce abundant clay minerals such as chlorite, a large elastic strain is difficult to accumulate and does not generate large thrust earthquakes, whereas the regions escaped from the hydration reactions could result in a strong mechanical coupling that acts as a seismic asperity. The descending plate undergoes changes in mineralogy at certain pressures and temperatures; however, these mineralogical transformations cannot explain the lateral heterogeneity in coupling along the plate interface. The subduction of seamounts may explain such variations in coupling (Cloos 1992; Scholz and Small 1997). However, Wang and Bilek (2011) suggested that subducted seamounts are mostly aseismic and produce numerous small earthquakes, indicating that the regions containing subducted seamounts are unlikely to be locked; instead, they release strain energy by slip on complex fracture systems. This behavior is probably due to the relatively high permeability around seamounts inferred from heat flow data (Hutnak et al. 2008). Audet and Schwartz (2013) proposed that the spatial distribution of fluid supply is a consequence of the complex hydrological structure of oceanic crust and is related to the geometry of palaeospreading ridges. Irregularities in seafloor topography could also contribute to heterogeneity in fluid pathways along subduction interfaces. Hydration reactions result in a progressive change in mineralogy at the plate interface. The frictional properties of a fault zone depend on the amount of clay minerals, as friction coefficient decreases with increasing clay content (Tembe et al. 2010). Consequently, the boundary between extensively hydrated and unaltered regions may display a transitional behavior. Moreover, in addition to mineralogical variations, pore fluid pressure plays a key role in controlling the occurrence of slip at the subducting plate interface (e.g., Seno 2003).
In this study, we focused mainly on the recovery process of fault strength; however, the velocity dependence of friction is another important parameter that controls whether a fault has potential for seismic or aseismic slip. Velocity-weakening behavior is known to accelerate slip propagation that is potentially unstable and may cause a rupture to propagate, as opposed to the self-stabilizing behavior of velocity-strengthening materials (e.g., Scholz 1998). Most clay minerals exhibit velocity-strengthening behavior at room temperature (Saffer and Marone 2003; Ikari et al. 2007; Moore and Lockner 2007). However, complex behavior of velocity dependence of clay minerals has been reported at elevated temperatures, in which velocity-weakening behavior is found at intermediate temperatures for illite-rich gouges, whereas velocity-strengthening behavior occurs predominantly at lower and higher temperatures (den Hartog et al. 2012). Further experiments are needed to test whether such behaviors are common in other clay minerals.
In our experiments, the fault strength showed a strong dependence on mineralogy, suggesting the importance of mineralogy in controlling mechanical coupling of the subducting plate interface. Since phase transformations cannot explain the spatial distribution of earthquakes along subduction zone, fluid supply and the products of hydration reactions could be key factors controlling regional variations in seismic coupling. This possibility is supported by the observed patterns of seismic velocities and attenuation in subduction zones, which indicate a highly heterogeneous fluid distribution along the plate boundary (Zhao 2015). Recent advances in seismic imaging allow the detailed structure and fluid pressure along the subduction zone to be monitored (Kodaira et al. 2004; Tsuji et al. 2008), and such monitoring of fluid pressure and movement may further help to determine the strength of coupling at the subducting plate interface.
We thank T. Shimamoto and K. Okazaki for technical advice and W. Tanikawa for the materials for the friction experiments. Comments by J. C. Moore and two anonymous reviewers helped to improve the manuscript. This study was supported by the Japan Society for the Promotion of Science and a Grant-in-Aid of Science Research on the Innovative Area of “Geofluids”.
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- Ariyoshi K, Matsuzawa T, Hasegawa A (2007) The key frictional parameters controlling spatial variations in the speed of postseismic-slip propagation on a subduction plate boundary. Earth Planet Sci Lett 256:136–146. doi:10.1016/j.epsl.2007.01.019 View ArticleGoogle Scholar
- Audet P, Schwartz SY (2013) Hydrologic control of forearc strength and seismicity in the Costa Rican subduction zone. Nat Geosci 6:852–855. doi:10.1038/ngeo1927 View ArticleGoogle Scholar
- Beeler NM, Hickman SH, Wong T (2001) Earthquake stress drop and laboratory-inferred interseismic strength recovery. J Geophys Res 106:30701–30713. doi:10.1029/2000JB900242 View ArticleGoogle Scholar
- Beroza GC, Ide S (2011) Slow earthquakes and non-volcanic tremor. Annu Rev Earth Planet Sci 39:271–296. doi:10.1146/annurev-earth-040809-152531 View ArticleGoogle Scholar
- Carpenter BM, Marone C, Saffer DM (2011) Weakness of the San Andreas Fault revealed by samples from the active fault zone. Nat Geosci 4:251–254. doi:10.1038/ngeo1089 View ArticleGoogle Scholar
- Cloos M (1992) Thrust-type subduction-zone earthquakes and seamount asperities: a physical model for seismic rupture. Geology 20:301–304. doi:10.1130/0091-7613 View ArticleGoogle Scholar
- den Hartog SAM, Peach CJ, de Winter DAM, Spiers CJ, Shimamoto T (2012) Frictional properties of megathrust fault gouges at low sliding velocities: new data on effects of normal stress and temperature. J Struct Geol 38:156–171. doi:10.1016/j.jsg.2011.12.001 View ArticleGoogle Scholar
- Dietrich JD (1972) Time-dependent friction in rocks. J Geophys Res 77:3690–3697. doi:10.1029/JB077i020p03690 View ArticleGoogle Scholar
- Dieterich JH, Conrad G (1984) Effect of humidity on time- and velocity-dependent friction in rocks. J Geophys Res 89:4196–4202. doi:10.1029/JB089iB06p04196 View ArticleGoogle Scholar
- Dietrich JH, Kilgore B (1994) Direct observation of frictional contacts: new insights for state-dependent properties. Pure Appl Geophysi 143:283–302. doi:10.1007/BF00874332 View ArticleGoogle Scholar
- Dixon TH, Moore JC. The seismogenic zone of subduction thrust faults: introduction. The seismogenic zone of subduction thrust faults. In: Dixon T, Moore C, editors. New York: Columbia Univ. Press; 2007. p. 2–14.Google Scholar
- Heki K, Miyazaki S, Tsuji H (1997) Silent fault slip following an interplate thrust earthquake at the Japan trench. Nature 586:595–598. doi:10.1038/386595a0 View ArticleGoogle Scholar
- Hilde T (1983) Sediment subduction versus accretion around the pacific. Tectonophysics 99:381–397. doi:10.1016/0040-1951(83)90114-2 View ArticleGoogle Scholar
- Hutnak M, Fisher AT, Harris R, Stein C, Wang K, Spenelli G, Schindler M, Villinger H, Silver E (2008) Large heat and fluid fluxes driven through mid-plate outcrops on ocean crust. Nat Geosci 1:611–614. doi:10.1038/ngeo264 View ArticleGoogle Scholar
- Hyndman RD, Peacock SM (2003) Serpentinization of the forearc mantle. Earth Planet Sci Lett 212:417–432. doi:10.1016/S0012-821X(03)00263-2 View ArticleGoogle Scholar
- Ikari MJ, Saffer DM, Marone C (2007) Effect of hydration state on the frictional properties of montmorillonite-based fault gouge. J Geophys Res 112:B06423. doi:10.1029/2006JB004748 Google Scholar
- Kanamori H (1986) Rupture process of subduction-zone earthquakes. Annu Rev Earth Planet Sci 14:293–322. doi:10.1146/annurev.ea.14.050186.001453 View ArticleGoogle Scholar
- Katayama I, Iwata M, Okazaki K, Hirauchi K. Slow earthquakes associated with fault healing on a serpentinized plate interface. Sci Rep 2013; 3: doi:10.1038/srep01784.
- Kameda J, Ujiie K, Yamaguchi A, Kimura G (2011) Smectite to chlorite conversion by frictional heating along a subduction thrust. Earth Planet Sci Lett 305:161–170. doi:10.1016/j.epsl.2011.02.051 View ArticleGoogle Scholar
- Kodaira S, Iidaka T, Kato A, Park OA, Iwasaki T (2004) High pore fluid pressure may cause silent slip in the Nankai trough. Science 304:1295–1298. doi:10.1126/science.1096535 View ArticleGoogle Scholar
- Lay T, Kanamori H, Ruff L (1981) The asperity model and the nature of large subduction zone earthquake occurrence. Earthquake Prediction Res 1:3–71Google Scholar
- Marone C (1998) Laboratory-derived friction laws and their application to seismic faulting. Annu Rev Earth Planet Sci 26:643–696. doi:10.1146/annurev.earth.26.1.643 View ArticleGoogle Scholar
- Moore JC, Vrolijk P (1992) Fluids in accretionary prisms. Rev Geophys 30:113–135. doi:10.1029/92RG00201 View ArticleGoogle Scholar
- Moore DE, Lockner DA. Friction of the smectite clay montmorillonite. The Seismogenic Zone of Subduction Thrust Faults. In: Dixon T, Moore C, editors. New York: Columbia Univ. Press; 2007. p. 317–345.Google Scholar
- Morrow CA, Moore DE, Lockner DA (2000) The effect of mineral bond strength and adsorbed water on fault gouge frictional strength. Geophys Res Lett 27:815–818. doi:10.1029/1999GL008401 View ArticleGoogle Scholar
- Nakatani M, Scholz C (2004) Frictional healing of quartz gouge under hydrothermal conditions: 1. Experimental evidence for solution transfer healing mechanism. J Geophys Res 109:B07201. doi:10.1029/2001JB001522 Google Scholar
- Park J, Tsuru T, Takahashi N, Hori T, Kodaira S, Nakanishi A, Miura S, Kaneda Y (2002) A deep strong reflector in the Nankai accretionary wedge from multichannel seismic data: Implications for underplating and interseismic shear stress release. J Geophys Res 107:B42061. doi:10.1029/2001JB000262 Google Scholar
- Saffer DM, Marone C (2003) Comparison of smectite- and illite-rich gouge frictional properties: application to the updip limit of the seismogenic zone along subduction megathrusts. Earth Planet Sci Lett 215:219–235. doi:10.1016/S0012-821X(03)00424-2 View ArticleGoogle Scholar
- Sakuma H (2013) Adhesion energy between mica surfaces: Implications for the frictional coefficient under dry and wet conditions. J Geophys Res 118:6066–6075. doi:10.1002/2013JB010550 View ArticleGoogle Scholar
- Satake K, Tanioka Y (1999) Sources of tsunami and tsunamigenic earthquakes in subduction zones. Pure Appl Geophys 154:467–483. doi:10.1007/978-3-0348-8679-6_5 View ArticleGoogle Scholar
- Scholz CH (1998) Earthquakes and friction laws. Nature 391:37–42. doi:10.1038/34097 View ArticleGoogle Scholar
- Scholz CH (2002) The mechanics of earthquakes and faulting, 2nd edn. Cambridge Univ, Press, UKView ArticleGoogle Scholar
- Scholz CH, Small C (1997) The effect of sea-mount subduction on seismic coupling. Geology 25:487–490. doi:10.1130/0091 View ArticleGoogle Scholar
- Seno T (2003) Fractal asperities, invasion of barriers, and interplate earthquakes. Earth Planets Space 55:649–665. doi:10.1186/BF03352472 View ArticleGoogle Scholar
- Shen L, Phang Y, Chen L, Liu T, Zeng K (2004) Nanoindentation and morphological studies on nylon 66 nanocomposites. I. Effect of clay loading. Polymer 45:3341–3349. doi:10.1016/j.polymer.2004.03.036 View ArticleGoogle Scholar
- Tembe S, Lockner DA, Wong T (2010) Effect of clay content and mineralogy on frictional sliding behavior of simulated gouges: binary and ternary mixtures of quartz, illite, and montmorillonite. J Geophys Res 115:B03416. doi:10.1029/2009JB006383 Google Scholar
- Tesei T, Collettini C, Carpenter BM, Viti C, Marone C (2012) Frictional strength and healing behavior of phyllosilicate-rich faults. J Geophys Res 117:B09402. doi:10.1029/2012JB009204 Google Scholar
- Tsuji T, Tokuyama H, Pisani PC, Moore G (2008) Effective stress and pore pressure in the Nankai accretionary prism off the Muroto Peninsula, southwestern Japan. J Geophys Res 113:B11401. doi:10.1029/2007JB005002 View ArticleGoogle Scholar
- Ujiie K, Tanaka H, Saito T, Tsutsumi A, Mori JJ, Kameda J, et al (2013) Low coseismic shear stress on the Tohoku-oki megathrust determined from laboratory experiments. Science 342:1211–1214. doi:10.1126/science.1243485 View ArticleGoogle Scholar
- Underwood MB. Sediment inputs to subduction zones: why lithostratigraphy and clay mineralogy matter. The seismogenic zone of subduction thrust faults. In: Dixon T, Moore C, editors. New York: Columbia Univ. Press; 2007. p. 42–85.Google Scholar
- Wang K, Bilek SL (2011) Do subducting seamounts generate or stop large earthquakes? Geology 39:819–822. doi:10.1130/G31856.1 View ArticleGoogle Scholar
- Zhao D (2015) The 2011 Tohoku earthquake (Mw 9.0) sequence and subduction dynamics in Western Pacific and East Asia. J Asian Earth Sci 98:26–49. doi:10.1016/j.jseaes.2014.10.022 View ArticleGoogle Scholar