Effect of normal stress on the frictional behavior of brucite: application to slow earthquakes at the subduction plate interface in the mantle wedge
- 1Department of Earth and Planetary Science, School of Science, University of Tokyo, Bunkyo, 113-0033 Tokyo, Japan
- 2Department of Ocean Floor Geoscience, Atmosphere and Ocean Research Institute, University of Tokyo, Kashiwa, 277-8564 Chiba, Japan
- 3Department of Earth and Planetary Systems Science, Hiroshima University, Higashi–Hiroshima, 739-8526 Hiroshima, Japan
- 4Research Center for Functional Materials, National Institute for Materials Science, Tsukuba, 305-0044 Ibaraki, Japan
Correspondence: Hanaya Okuda (firstname.lastname@example.org)
We report the results of friction experiments on brucite under both dry and wet conditions under various normal stresses (10–60 MPa). The final friction coefficients of brucite were determined to be 0.40 and 0.26 for the dry and wet cases, respectively, independent of the normal stress. Under dry conditions, velocity-weakening behavior was observed in all experiments at various normal stresses. Under wet conditions, velocity weakening was observed at low normal stress (10 and 20 MPa), whereas velocity strengthening was determined at a higher applied normal stress. Microstructural observations of recovered experimental samples indicate localized deformation within a narrow shear band, implying that a small volume of brucite can control the bulk frictional strength in an ultramafic setting. Among serpentinite-related minerals, weak and unstable frictional behavior of brucite under hydrated mantle wedge conditions may play a role in slow earthquakes at the subduction plate interface in the mantle wedge.
Serpentinite is generated by the hydration of ultramafic rocks and has various mineral compositions depending on temperature–pressure conditions of the MgO–SiO2–H2O system (Evans et al., 2013). As serpentinite has been observed in various important tectonic settings and is considered to contribute to the weakness of serpentinite-dominant areas, the frictional properties of serpentinite have been investigated for several decades (see Guillot et al., 2015, and Hirth and Guillot, 2013, for a review). A large volume of serpentinite is located in mantle wedges in which olivine-rich rock of the upper mantle is hydrated by slab-derived water and composes the subduction plate interface, as suggested by geological and seismological studies (Bostock et al., 2002; Christensen, 2004; Guillot and Hattori, 2013; Hyndman and Peacock, 2003; Kawahara et al., 2016; Kawakatsu and Watada, 2007; Mizukami et al., 2014; Peacock and Hyndman, 1999; Reynard, 2013). Because of the mechanical weakness of serpentinite, the relationship between the presence of serpentinite and the aseismic behavior below the downdip limit of seismogenic zones has been argued (Hyndman and Peacock, 2003; Oleskevich et al., 1999). However, many recent observations have indicated that slow earthquakes, such as episodic tremor and slip (ETS), slow-slip events (SSEs), and low-frequency earthquakes (LFEs), occur at the depth of the mantle wedge in various subduction zones (Audet and Kim, 2016; Obara, 2002; Obara and Kato, 2016; Rogers and Dragert, 2003; Shelly et al., 2006). As slow earthquakes can trigger or be triggered by huge megathrust earthquakes (Obara and Kato, 2016), the nucleation processes of slow earthquakes are important for understanding seismic activities at subduction zones.
Recent seismological and geological studies have revealed that a layer several hundred meters to kilometers wide is serpentinized and foliated along subduction plate interfaces, and the deformation of this serpentinite layer is likely to relate to slow earthquakes at the depth of the mantle wedge (Bostock et al., 2002; Calvert et al., 2020; DeShon and Schwartz, 2004; Dorbath et al., 2008; Kawakatsu and Watada, 2007; Nakajima et al., 2009; Ramachandran and Hyndman, 2012; Tarling et al., 2019). Within this foliated serpentinite layer, both meta-ultramafic and meta-sedimentary blocks are present, and metasomatic reactions occur at the boundary between these blocks and the serpentinite matrix (Guillot et al., 2015; Tarling et al., 2019). Such a block-in-matrix structure exhibits complex rheological behavior such that shear stress is controlled by both ductile and brittle deformations of block and matrix depending on the strain rate (Fagereng and den Hartog, 2017; den Hartog and Spiers, 2014; Niemeijer and Spiers, 2007; Tarling et al., 2019). Thus, understanding the deformation properties of both the block and matrix is essential to constraining how the subduction plate interface behaves and generates slow earthquakes. This was also underlined by a geological study on the Livingstone Fault, New Zealand (Tarling et al., 2019), which found that the cataclastic slip surface was coated by scaly serpentinite, suggesting that the deformation process of serpentinite is important for brittle deformation and widespread ductile deformation at the subduction plate interface.
In addition, nearly lithostatic pore pressure conditions, which lead to low effective normal stress conditions, have been inferred based on seismic velocity structures at the plate interfaces of several subduction zones where slow earthquakes coincidently occur in regions such as Cascadia, SW Japan, central Mexico, and Hikurangi (Audet et al., 2009; Audet and Kim, 2016; Eberhart-Phillips and Reyners, 2012; Matsubara et al., 2009; Shelly et al., 2006; Song and Kim, 2012). This low effective normal stress condition may be correlated with slow earthquakes because frictional deformation becomes dominant, rather than viscous deformation, in terms of shear strength (French and Condit, 2019; Gao and Wang, 2017). Furthermore, the low effective normal stress condition seems favorable for the nucleation of slow earthquakes (Liu and Rice, 2007, 2009; Rubin, 2008; Segall et al., 2010) and is also consistent with smaller stress drops than regular earthquakes (Ide et al., 2007; Rubinstein et al., 2007, 2008; Schmidt and Gao, 2010). Thus, the frictional properties of serpentinite under low effective normal stress conditions likely play an important role in slow earthquakes at the subduction plate interface near the mantle wedge.
Serpentinite in the mantle wedge is mainly composed of an antigorite–olivine assemblage in warm subduction zones like Cascadia, whereas a brucite–antigorite assemblage dominates in the case of cold subduction zones such as that in NE Japan (Peacock and Hyndman, 1999). Because fluids from subducting slabs have a high SiO2 content, talc is stable in the vicinity of slab–mantle boundaries (Hirauchi et al., 2013; Peacock and Hyndman, 1999). Serpentinite is made up of serpentinite-related minerals, such as antigorite, brucite, and talc, and as those minerals show different frictional behavior, the frictional properties of each mineral should be understood to interpret the mechanical behavior of bulk serpentinite. Many previous experimental studies investigated the frictional properties of antigorite and talc (Hirauchi et al., 2013; Moore et al., 1997; Moore and Lockner, 2007, 2008; Okazaki and Katayama, 2015; Reinen et al., 1994; Sánchez-Roa et al., 2017; Takahashi et al., 2007; Tesei et al., 2018). However, brucite has rarely been considered in previous studies, as it is challenging to detect brucite under natural conditions because of its fine-grained nature (Hostetler et al., 1966). Brucite is not thermodynamically stable when the slab-derived water contains high SiO2 content, and the mantle wedge may undergo silica metamorphism (Manning, 1997; Peacock and Hyndman, 1999). However, geological works on exhumed mantle wedge regions suggest that silica metamorphism has not occurred widely within the shallow mantle wedge because talc zones and metasomatic reactions are often limited in the narrow part near the meta-sedimentary rocks (Angiboust and Agard, 2010; D'Antonio and Kristensen, 2004; French and Condit, 2019; Guillot et al., 2009; Kawahara et al., 2016; Mizukami et al., 2014; Nagaya et al., 2020; Reynard, 2013; Tarling et al., 2019). These observations indicate that the serpentinite layer at the subduction plate interface may contain brucite because of low silica metamorphism as brucite itself has sometimes been found (Kawahara et al., 2016; Mizukami et al., 2014). Hydrothermal experiments also support the finding that SiO2 is effectively consumed and brucite can stably exist with antigorite (Oyanagi et al., 2015, 2020). Although deformation may localize at the metasomatic region (Hirauchi et al., 2013; Tarling et al., 2019), the foliated structure of the serpentinite matrix implies that the serpentinite layer still accompanies some portion of deformation at the subduction plate interface. Furthermore, as brucite is a sheet-structure mineral, which often shows a low friction coefficient due to weak interlayer bonding, its frictional behaviors may play a role in earthquakes at the serpentinite layer (Moore et al., 2001; Moore and Lockner, 2004).
Only a few previous experimental studies under high normal stress conditions of 100 or 150 MPa have been conducted on the frictional properties of brucite. It was shown that brucite has friction coefficients of 0.40–0.46 (dry) or 0.28 (wet), which are lower than those of antigorite (Moore and Lockner, 2004, 2007; Morrow et al., 2000). Regarding the velocity dependence, significant stick-slip behavior has been observed for dry brucite at both room and high temperature, implying velocity-weakening behavior. Conversely, wet brucite shows velocity-strengthening behavior at room temperature, which gradually changes to velocity weakening with increasing temperature (Moore et al., 2001; Moore and Lockner, 2007). The friction coefficient of a serpentinite gouge can be lowered by approximately ∼ 10 %–15 % due to the presence of brucite (Moore et al., 2001). The weakness and velocity-weakening behavior of brucite under certain conditions might affect nucleation processes of slow earthquakes at the subduction plate interface in mantle wedges because velocity-weakening behavior is likely to relate to slow earthquakes as proposed in previous studies. Dilatancy hardening in the velocity-weakening system (Rubin, 2008; Segall et al., 2010), slip weakening (Ikari et al., 2013), the transition from a velocity-weakening to velocity-strengthening system at a cutoff velocity (den Hartog et al., 2012; Matsuzawa et al., 2010; Shibazaki and Iio, 2003), and slow stick-slip (Leeman et al., 2016, 2018; Okazaki and Katayama, 2015) are proposed as mechanisms that generate slow earthquakes. Most of them require the velocity-weakening system to nucleate earthquakes, especially for seismologically detected events like LFEs; therefore, the velocity-weakening behavior of brucite can be suggestive of slow earthquakes at the subduction plate interface.
However, the frictional behavior of brucite at low effective normal stress has not been studied in spite of its potential relationship to slow earthquakes. In this study, we experimentally investigated the frictional behavior of brucite at various effective normal stresses ranging from 10 to 60 MPa to understand the effect of brucite on the seismic activities at the subduction plate interface in hydrated mantle wedges.
2.1 Friction experiment
2.1.1 Sample preparation
Brucite nanoparticles with a grain size of 70 nm chemically synthesized by the FUJIFILM Wako Pure Chemical Corporation were used for the friction experiments to simulate its fine-grained nature (Fig. 1). The synthetic samples had a purity of 99.9 % (data from the FUJIFILM Wako Pure Chemical Corporation).
A biaxial testing machine at Hiroshima University, Japan, was used for all friction experiments in this study (Noda and Shimamoto, 2009). There are two gouge layers between three gabbro blocks (Fig. 1). The surfaces in contact with gouges were roughened before the experiments using carborundum (grit 80) to prevent slip between the blocks and sample. All brucite samples were dried in a vacuum oven overnight under 120∘ before the experiments. This temperature was selected to remove adsorbed water and prevent the dehydroxylation of brucite into periclase (MgO). For the dry experiments, the brucite powder was quickly sandwiched between the blocks to form the gouge after removing it from the vacuum oven, and the blocks with samples were then put in the testing machine. For the wet experiments, dried brucite was mixed with distilled water before placing it in the gouges and then sandwiched between blocks.
a All parameters (a, b, and dc) used for the velocity step tests are listed in Table S1. b Value at a shear displacement of 18 mm. c Shear loading was stopped before the peak friction coefficient was reached. d Shear loading was stopped shortly after the peak friction coefficient was reached. e Stick-slip behavior was observed, and the a–b value was determined by Eq. (5). NA: not available.
2.1.2 Experimental procedures
Normal stress was horizontally applied to the side blocks, and shear stress was applied vertically by pushing the center block downward (Fig. 1). Before applying shear stress, the desired normal stress was applied to the blocks for 1 h to prevent an effect of the compaction of the gouge during shear deformation (nominally precompaction). For the wet experiments, the blocks and gouges were placed in a tank filled with distilled water for 1 h under a normal stress of 250 kPa before the precompaction with the desired normal stress such that water-wet conditions were achieved. Note that we did not have a mechanism to prevent the gouge from squeezing out for the wet experiment; therefore, the gouge thickness for wet experiments becomes narrower than that for dry ones. After the precompaction, shear stress was applied with a constant load point velocity of 3 µm s−1. Velocity step tests were repeatedly conducted after the shear displacement reached 10 mm by abruptly increasing the load point velocity to 33 µm s−1 and decreasing it to 3 µm s−1 after a shear displacement of 1 mm (Fig. 2). The normal stress conditions of 10, 20, 40, and 60 MPa were tested for both the dry and wet cases to study the influence of effective normal stress. In addition, several experiments were conducted with different total shear displacements to investigate the evolution of the gouge microstructure in both the dry and wet experiments (Table 1).
2.2 Data analysis
2.2.1 Mechanical data
The friction coefficient μ was calculated from the ratio of the shear stress to the normal stress. Note that cohesion stresses were 0.36 and 0.47 MPa for dry and wet cases, respectively, calculated by linear regression of the shear stress and normal stress of all the experiments. Because the obtained cohesion stresses were too small to affect the friction coefficients, the cohesion stress was not considered in this study. The shear displacement was corrected using the stiffness of the testing machine (4.4 × 108 N m−1). The velocity step tests were analyzed using the rate- and state-dependent friction (RSF) law (Dieterich, 1979; Ruina, 1983). Before conducting the following analyses, the friction coefficient vs. the displacement curve was detrended for the slip-weakening trend, which was obtained from the friction data in the second half of each velocity step of 500 µm shear displacement. Detrended data were fitted to the following the RSF law:
where a, b1, and b2 are nondimensional parameters, μ0 is the steady-state friction coefficient before the velocity step, V0 and V are the sliding velocities before and after the velocity step, dc1 and dc2 are the characteristic slip distances, and θ1 and θ2 are the state variables. We estimated the effect of elastic interaction due to the machine stiffness on V using the following relationship:
where Vlp is the load point velocity, which was abruptly changed, and k is the system stiffness, which was treated as an unknown parameter (in µm−1). The Dieterich (aging) law (Dieterich, 1979; Marone, 1998; Ruina, 1983) was used for the state variable in this study.
A MATLAB code, RSFit3000, developed to fit the velocity step and slide–hold–slide tests (Skarbek and Savage, 2019) was used for the analyses of velocity step tests. The second variables b2, θ2, and dc2 (Blanpied et al., 1998) were only introduced when the experimental data were poorly fitted (upsteps of HTB575 and HTB598; Fig. 4); otherwise, b2 and θ2 were treated as 0. The value of a–b ( or a−b1) was then calculated for each step, which describes the instability of the simulated fault: the state of the fault is defined as velocity strengthening and stable when a–b is positive, whereas it is defined as velocity weakening and potentially unstable when a–b is negative. Note that dc values for the velocity steps whose velocities decreased from 33 to 3 µm s−1 (downsteps) are larger than those for the velocity steps whose velocities increased from 3 to 33 µm s−1 (upsteps). Because we chose to use the Dieterich (aging) law to fit the RSF law, dc reflects the diameter of the contact area between grains (Dieterich, 1979; Ruina, 1983). When the load point velocity is 3 µm s−1, the lifetime of one contact area is longer than that with a load point velocity of 33 µm s−1. Therefore, the contact diameter, dc, for the load point velocity of 3 µm s−1 (downsteps) is larger than that for 33 µm s−1 (upsteps). In addition, dc is also considered to reflect the shear localization (Marone and Kilgore, 1993); when the shear localizes, dc decreases. Hence, the difference in dc has qualitative information on the shear localization within the gouge. Although there are still debates on the choice of constitutive laws (Bhattacharya et al., 2015, 2017; Marone, 1998), as all constitutive laws give the same result for a–b, we calculated the value of a–b by using separately obtained a and b with the aging law. The focus of this study will be the a–b value because it plays an essential role in the nucleation process of earthquakes. However, other parameters like dc and stiffness are also important to the nucleation process, and therefore those parameters should be assessed in future studies.
When the system is velocity weakening, which is when a–b is negative, it starts to vibrate automatically (stick-slip) when the system stiffness is lower than a critical stiffness, whereas conditionally stable sliding is achieved when the system stiffness is higher than a critical stiffness. The critical stiffness kc can be described as follows when quasi-static stick-slip behavior is assumed:
where N is the effective normal stress (Ruina, 1983). Thus, as the effective normal stress N applied to the velocity-weakening system increases, the system starts to show stick-slip behavior. In other words, the occurrence of stick-slip represents the system being velocity weakening. We determined the a–b value for dry experiments with normal stresses of 40 and 60 MPa by simply comparing the averaged friction coefficients during the stick-slip behavior for two velocities based on the following relationship:
where Δμss and Δln V are variations in the steady-state friction coefficient and the sliding velocity in the log scale, respectively. In this case, a, b, and dc cannot be determined.
In the case of sheet-structure minerals, the friction between basal planes of the crystals (the (0001) plane for brucite) is thought to be significant due to their weak bonding. The shear surfaces of the samples recovered from friction experiments using sheet-structure minerals often show smooth surfaces composed of platy particles aligned parallel to the sliding direction (Moore and Lockner, 2004). Further, according to the experiments with natural samples, the aligned platy particles of interconnected talc were reported to contribute to the low friction coefficient of low-angle normal faults (Collettini et al., 2009).
Because these experiments indicate that the crystal orientation within the gouge has a significant effect on the friction coefficients of sheet-structure minerals, observations of thin sections of recovered samples were conducted after the experiments (Table 1) to investigate the effects of the deformation structures and crystal orientation within the gouges on the frictional behavior. After the experiment, we impregnated the gouge and the blocks with epoxy resin to keep the deformation structures within the gouge. Thin sections parallel to the shear direction and normal to the gouges with a thickness of 30 µm were prepared from the impregnated samples. A scanning electron microscope (SEM; JEOL JXA-8900; Atmosphere and Ocean Research Institute, University of Tokyo, Japan) was used to observe the microstructures of the gouges. An accelerating voltage of 15 kV and a beam current of 10.0 nA were used for all backscattered electron (BSE) observations. The crystal orientation was determined with a polarizing microscope at the University of Tokyo, Japan.
3.1 Mechanical behaviors
3.1.1 Friction coefficients
In general, both dry and wet experiments show high friction coefficients at a shear displacement of 1.5–2 mm (hereafter peak friction coefficients), followed by slip-weakening trends with a shear displacement of about 10 mm towards steady state (Figs. 2 and S1 in the Supplement). The final friction coefficients at a shear displacement of ∼ 20 mm for dry and wet conditions under all normal stress conditions were 0.40 ± 0.04 and 0.26 ± 0.03, respectively (Table 1). These final friction coefficients are mostly independent of the applied normal stress (Fig. 3) and consistent with previous experimental results: 0.38–0.46 and 0.28 for dry and wet brucite, respectively, at an applied normal stress of 100 MPa at room temperature (Moore and Lockner, 2004, 2007). The friction coefficient for dry experiments is also close to the theoretical value of 0.30 ± 0.03 (Okuda et al., 2019). Note that the peak friction coefficient of wet brucite at an effective normal stress of 60 MPa is high because of sudden stress drops in the initial stage of the shear displacement (Fig. S1). As these data may include some experimental artifacts, we do not use this peak value for 60 MPa normal stress in this study.
3.1.2 Velocity dependencies
For wet experiments, negative a–b values were observed at low normal stresses of 10 and 20 MPa (Fig. 4a and b). However, the a–b values became almost neutral at 40 MPa and positive at 60 MPa. A positive a–b value was consistent with previous experiments on wet brucite at an effective normal stress of 100 MPa (Moore et al., 2001; Moore and Lockner, 2007). The a–b values obtained for the upsteps and downsteps insignificantly differ (Fig. 4a and b). In the experiments with normal stress conditions of 20, 40, and 60 MPa, the constitutive parameter a is almost constant at 0.0054 for both upsteps and downsteps, whereas b decreases from 0.0064 to 0.0042 and from 0.0076 to 0.0040 for upsteps and downsteps, respectively, as the normal stress increases (Fig. 4e and f). Accordingly, we concluded that the decrease in b induces the transition from negative to positive a–b. The dc values at different effective normal stresses insignificantly differ (Fig. 4c and d).
For dry experiments, negative a–b values were obtained at all normal stress conditions (Fig. 4a and b). When the normal stress was higher than 40 MPa, stick-slip behavior was observed. This unstable stick-slip behavior was also reported in the case of a dry experiment at a higher normal stress of 100 MPa (Moore and Lockner, 2004; Morrow et al., 2000). No information on a, b, and dc values for 40 and 60 MPa experiments was obtained because of the stick-slip behavior. As shown in wet conditions, larger dc values were observed for the downsteps (Fig. 4c and d). Note that the second variables b2 and dc2 were introduced in two experiments (HTB575 and HTB598). However, their effects on the earthquake nucleation process, meaning the a–b value, are small because the b2 values are much smaller than b1, although the dc2 value is much larger than dc1 (Fig. 4e and Table S1 in the Supplement).
The constitutive parameters a and b as well as the critical slip distance dc of the dry and wet experiments significantly differ. The a, b, and dc values of the wet experiments are larger than those of the dry experiments (Fig. 4). The critical slip distances dc of the upsteps and downsteps under wet conditions were 5–15 times and 3–4 times larger, respectively, than those under dry conditions.
3.2.1 Evolution of deformation structures
As all samples (both dry and wet) showed a peak value followed by a transition into the steady state, we chose shear displacements before the peak friction coefficient (pre-yield), after the peak friction coefficient (post-yield), and in the steady state (10 mm) to study the evolution of the deformation structures. Note that the steady state may not be achieved at a shear displacement of 10 mm, but as the final friction coefficients were similar to the friction coefficients at 10 mm shear displacement, here we used the term “steady state” and considered the idea that the microstructure at 10 mm shear displacement might be consistent with the steady state. We followed the description of the microstructure of a sheared gouge by Logan et al. (1979). The results for the dry and wet experiments are shown in Figs. 5 and 6, respectively.
Before the shear loading, no shear structure was observed (Fig. 5a). When the shear force was loaded, the Riedel shear propagated in the pre-yield regime, and the gouge thickness decreased rapidly at first (Figs. 5b and 6a). Subsequently, boundary shear started to develop post-yield (Figs. 5c and 6b). In the steady state, boundary shear was created, and the Riedel shear tilted subparallel to the boundary shear (Figs. 5d and 6c). The surfaces of the gabbro blocks were filled with brucite, and the boundary shear was much smoother than the original block surface. These observations are consistent with previous studies (Haines et al., 2013; Kenigsberg et al., 2019, 2020; Logan et al., 1992; Marone, 1998), although a clear Y shear and P foliation were not observed in this study. The gouge thickness remained almost constant post-yield and at steady state, suggesting that the deformation may localize parallel to the shear deformation, i.e., parallel to the boundary shear. The thickness of the entire gouge in the steady state was 400 and 150 µm in the dry and wet cases, respectively (Figs. 5d and 6c). The narrow thickness of the gouge in the wet case may result from leakage of the sample during the experiment, but we did not have a mechanism to prevent the gouge from leaking out. The difference in the entire gouge thickness may not affect the overall frictional characteristics because both dry and wet cases showed Riedel shear development at first, followed by boundary shear development. Observation of grain contact is needed for clarification, but it was not possible in this study because the grains were very small (70 nm in diameter).
3.2.2 Crystal orientation
Because brucite has a negative elongation (Berman, 1932) and its birefringence is 0.014–0.020 (Deer et al., 2013), the interference color of brucite under crossed nicols with a sensitive color plate inserted becomes second-order blue or first-order yellow when the c axis of brucite is normal or parallel to the X′ direction of the sensitive color plate, respectively.
In the dry sample (HTB601; Fig. 7a and b), a second-order blue line can be observed parallel to the smooth boundary shear, implying that the basal (0001) plane of the brucite particles is aligned along the boundary shear parallel to the shear direction. We did not observe any alignment along the Riedel shears, suggesting that deformation along the Riedel shears cannot be dominant at the steady state. Based on the magnified view, the brucite particles are oriented within 10 µm around the boundary shear (Fig. 7b). Because the purple area indicates that the brucite particles are randomly oriented, the shear strain can be localized within a thickness of 10 µm. Hereafter, we call this oriented area the “shear band.” In the wet samples, the crystals are also oriented along the boundary shear (Fig. 7c and d). The thickness of the shear band is 20 µm (Fig. 7d), which is a little wider than that for the dry experiments. This observation is consistent with the relationship between the shear localization and dc value (Marone and Kilgore, 1993): the degree of shear localization for the dry sample is higher than that for the wet sample, and dc for dry sample was smaller than for the wet sample (Fig. 4). Note that detailed transmission electron microscopy is required in future studies to confirm the crystal orientation and shear band thickness, as shown in previous studies (Verberne et al., 2014a; Viti, 2011).
4.1 Mechanical weakness of a small amount of brucite
Based on the microstructural observations in Sect. 3.2, the boundary shear is smooth, filling the rough surface of the gabbro block as a “fault mirror” (Siman-Tov et al., 2013). The brucite particles are aligned along the boundary shear, suggesting that the deformation within the narrow shear band is responsible for most of the deformation of the gouge during the steady state. In addition, the constant gouge thickness during the steady state suggests that gouge deformation occurs parallel to the shear direction, consistent with shear deformation localized within the shear band.
Because previous studies showed that a smooth slip surface reduces the friction coefficient compared to a roughened slip surface (Anthony and Marone, 2005), the development of the smooth boundary shear observed in this study would reduce the friction coefficient with increasing shear displacement (Haines et al., 2013). In addition, the slip between the basal planes of sheet-structure minerals also plays an important role for weak friction because the friction between single crystals of sheet-structure minerals has a lower friction coefficient than that of powdered samples (Horn and Deere, 1962; Kawai et al., 2015; Niemeijer, 2018; Okamoto et al., 2019). Based on the observed alignment of the basal plane of brucite within the shear band, the friction between the basal planes of brucite crystals might enhance the weak friction of brucite. Because the preferred planes of nanoparticles tend to be aligned even when the velocity is low (Verberne et al., 2013, 2014b), nanoparticles could contribute to the slip-weakening behavior. Based on these phenomena, we conclude that the mechanical weakness of brucite observed in this study is likely derived from the smooth boundary shear of fine brucite particles and alignment of the basal plane of brucite parallel to the boundary shear.
The results of several previous experimental studies showed that the friction coefficient of a mixture of strong and weak materials inversely correlates with the volume of the weak materials (Giorgetti et al., 2015; Logan and Rauenzahn, 1987; Moore and Lockner, 2011; Niemeijer and Spiers, 2007; Shimamoto and Logan, 1981; Takahashi et al., 2007; Tembe et al., 2010). Based on the maximum amount of brucite in serpentinite, which is ∼ 20 vol. % (Kawahara et al., 2016; Moore et al., 2001), the expected friction coefficient of the antigorite–brucite mixture is 0.53, assuming a simple linear mixing law between the wet friction coefficients of 0.6 for antigorite and 0.26 for brucite. This value is not small, but the bulk friction coefficient of the mixture will decrease if weak brucite crystals are interconnected with each other. The microstructural observations showed that the shear band is less than 50 µm wide (Sect. 3.2.2; Fig. 7); therefore, a narrow network of brucite can decrease the bulk strength. The results of a recent petrographic study of a hydrated paleo-mantle wedge revealed brucite thin films parallel to antigorite particles, suggesting the significant role of brucite in the development of the sheared structure of the antigorite–brucite assemblage in the hydrated mantle wedge (Mizukami et al., 2014). Because the maximum thickness of the brucite film in the antigorite–brucite assemblage is several hundred micrometers (Kawahara et al., 2016; Mizukami et al., 2014), which is larger than 50 µm, brucite has the potential to drastically weaken the bulk strength of serpentinite.
4.2 Application to the mantle wedge conditions
When we consider the effect of brucite on the seismic activities in the mantle wedge, the effect of temperature should be taken into account because all our experiments were conducted under room-temperature conditions. According to previous experiments on brucite under hydrothermal conditions in which the temperature was varied, the friction coefficient and the a–b values decrease with increasing temperature (Moore et al., 2001; Moore and Lockner, 2007). Because a nearly neutral a–b value was observed at an effective normal stress of 150 MPa and a temperature of 340∘ (Moore et al., 2001), brucite shows unstable behavior under a wide range of temperature–pressure conditions, especially at low effective normal stress. Based on the estimated frictional properties of brucite under mantle wedge conditions, we compared brucite to other mineral phases to interpret the earthquake processes within the mantle wedge (Fig. 8).
In the mantle wedge, ultramafic minerals such as olivine transform into serpentine minerals, such as antigorite, talc, and brucite, due to hydration. In cold subduction zones, such as beneath NE Japan, likely containing brucite under the temperature–pressure conditions of the mantle wedge, the thermodynamically stable mineral assemblages are lizardite–brucite (Liz–Brc) at depths shallower than 50 km and antigorite–brucite (Atg–Brc) under deeper and warmer conditions (Peacock and Hyndman, 1999). Previous experimental studies on antigorite suggested potential seismic activities due to the unstable frictional behavior of antigorite at high temperatures above 450 ∘C (Okazaki and Katayama, 2015; Takahashi et al., 2011) at which crustal (granitic) rock shows stable friction (Fig. 8), whose friction coefficient (0.5–0.7) is not as low as that of brucite (Fig. 8). Although lizardite, which thermodynamically destabilizes at ∼ 200 ∘C, potentially shows unstable frictional behavior at low temperature (Moore et al., 1997), its friction coefficient is 0.4–0.5, which is lower than that of antigorite but higher than that of brucite (Fig. 8). Therefore, antigorite and lizardite are not preferably deformed if other weaker minerals, such as brucite, are present in continuous fault strands in which the deformation localizes.
Another candidate for such a weak mineral stable under mantle wedge conditions is talc. Talc has a low friction coefficient of 0.1–0.2 at low to high temperatures (Fig. 8); therefore, it might contribute to the creep behavior of the San Andreas Fault (Moore and Lockner, 2008) or weaken the slab–mantle interface (Hirauchi et al., 2013; Hyndman and Peacock, 2003). However, because talc has a stable frictional behavior at any temperature, leading to aseismic creep (Moore and Lockner, 2008; Sánchez-Roa et al., 2017), it cannot nucleate earthquakes. When we consider talc in the mantle wedge, talc is thermodynamically stable at high Si concentrations and temperature, whereas the mineral assemblage consists of brucite and antigorite when the Si content and temperature are low (Peacock and Hyndman, 1999). Talc was not widely observed in the paleo-mantle wedge exposed in the Shiraga body (central Shikoku, Japan) at temperature–pressure conditions under which the antigorite–brucite system is thermodynamically stable (Kawahara et al., 2016; Mizukami et al., 2014). Although only antigorite stably exists in the antigorite–brucite stability field when the Si content is high, brucite is widely distributed in the Shiraga body (∼ 10 %–15 %), suggesting low Si metasomatism in the shallow hydrated mantle wedge (Kawahara et al., 2016). Hence, brucite can stably exist within the mantle wedge rather than talc. Although talc is still significantly important for deformation at the subduction plate interface (Hirauchi et al., 2013), the possible occurrence of brucite and its weak and unstable frictional characteristics implies that brucite may be a possible control for the seismic activities at the subduction plate interface in the shallow hydrated mantle wedge.
The results of recent seismological studies showed that plate interfaces in a shallow mantle wedge have a nearly lithostatic pore pressure due to slab-derived water at various subduction zones in SE Japan, Cascadia, central Mexico, and Hikurangi (Audet et al., 2009; Audet and Kim, 2016; Eberhart-Phillips and Reyners, 2012; Matsubara et al., 2009; Shelly et al., 2006; Song and Kim, 2012). Such low effective normal stress conditions are conducive to brittle deformation rather than ductile behavior (French and Condit, 2019; Gao and Wang, 2017). Slow earthquakes in the mantle wedge of various subduction zones (Audet and Kim, 2016; Obara and Kato, 2016) might be induced by low effective normal stress because low effective normal stress conditions are conducive to the nucleation of slow earthquakes (Liu and Rice, 2007, 2009; Rubin, 2008; Segall et al., 2010). As the a–b value of brucite decreases with decreasing effective normal stress, brucite at low effective normal stress possibly causes the nucleation of slow earthquakes in the mantle wedge. On the other hand, an increase in the a–b value at higher stresses was caused by a decrease in the b value (see Sect. 3.1.2), which may be related to the saturation of the real area of contact (Saffer and Marone, 2003). As the b value can be recast as the healing rate in slide–hold–slide experiments (Ikari et al., 2016), wet brucite cannot store strain energy at the high effective normal stress condition. Notably, the possible presence of brucite-free antigorite or talc due to high Si content in the vicinity of the slab–mantle interface (Hirauchi et al., 2013; Peacock and Hyndman, 1999) might affect the partitioning of deformation (French and Condit, 2019) and the contribution of brucite to the deformation. The mechanisms of nucleation of slow earthquakes are still debated in both theoretical and experimental studies; for example, dilatancy hardening, the transition from a negative to positive a–b value, slip weakening, and slow stick-slip are all considered possible mechanisms (den Hartog et al., 2012; Ikari et al., 2013; Leeman et al., 2016, 2018; Matsuzawa et al., 2010; Okazaki and Katayama, 2015; Rubin, 2008; Segall et al., 2010; Shibazaki and Iio, 2003). As other serpentinite-related minerals show stable frictional behavior, i.e., positive a–b, friction experiments with mixtures of brucite and other minerals like talc and antigorite may provide further information on the generation of slow earthquakes. In addition, the linkage between high pore fluid pressure and effective normal stress is still debated (Hirth and Beeler, 2015; Noda and Takahashi, 2016); therefore, experiments under hydrothermal conditions with high confining pressure and high pore fluid pressure must be conducted in the future.
In this study, the influence of effective normal stress on the frictional characteristics of brucite was experimentally determined under both dry and wet conditions at room temperature. The final friction coefficients of brucite are 0.40 and 0.26 in the dry and wet cases, respectively, independently of the applied normal stress, while the peak friction coefficients are inversely correlated with the applied normal stress. In all dry experiments, velocity-weakening or stick-slip behavior was observed at every normal stress. In the wet experiments, velocity-weakening, velocity-neutral, and velocity-strengthening behaviors were observed at normal stresses of 10 and 20, 40, and 60 MPa, respectively. Combined with the previously reported temperature effect, this result suggests that brucite is weak and unstable under a wide range of temperature–pressure conditions. The microstructural observations reveal that a low friction coefficient and slip weakening from the peak to steady-state friction coefficient are due to smooth boundary shear and basal plane orientation parallel to the boundary shear. Because the deformation is concentrated within a narrow shear band with a thickness less than 50 µm, a small amount of brucite can weaken the bulk strength of the antigorite–brucite assemblage. Compared to other serpentinite minerals, brucite is the only mineral that shows both a low friction coefficient and velocity-weakening behavior. Hence, we conclude that weak, unstable brucite contributes to the nucleation of slow earthquakes in the shallow hydrated mantle wedge.
The results of all experimental data are available in the Supplement.
The supplement related to this article is available online at: https://doi.org/10.5194/se-12-171-2021-supplement.
HO conceptualized this study. HO and IK conducted the experiments. HO and HS conducted analyses before experiments. HO carried out formal analyses and microstructural analyses. HO prepared the original paper, which was reviewed and edited by all coauthors. KK was the supervisor. IK, HS, and KK designed the research project.
The authors declare that they have no conflict of interest.
This article is part of the special issue “Thermo-hydro-mechanical–chemical (THMC) processes in natural and induced seismicity”. It is a result of the The 7th International Conference on Coupled THMC Processes, Utrecht, Netherlands, 3–5 July 2019.
We thank two anonymous referees for their careful and constructive reviews. We also thank Yuta Noda and Riho Fujioka for the experiments, Hayami Ishisako for the preparation of thin sections, and Asuka Yamaguchi and Nobuhiro Ogawa for SEM observations. HO is supported by JSPS and FMSP as a research fellow.
This research has been supported by the Japan Society for the Promotion of Science (grant nos. JP20J20413, JP20H00200, JP15H02147) and the Cooperative Program (no. 114; 2019) of the Atmosphere and Ocean Research Institute, University of Tokyo.
This paper was edited by Jianye Chen and reviewed by two anonymous referees.
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