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Quartz deposition and its influence on the deformation process of megathrusts in subduction zones
© Kameda et al.; licensee Springer. 2014
- Received: 30 October 2013
- Accepted: 24 March 2014
- Published: 16 April 2014
We present a quantitative examination of the liberation and subsequent deposition of silica at the subduction zone plate interface in the Mugi mélange, an exhumed accretionary complex in the Shimanto Belt of southwest Japan. Frequency and thickness measurements indicate that mineralized veins hosted in deformed shales make up approximately 0.4% of the volume of this exposure. In addition, whole-rock geochemical evidence suggests that the net volume of SiO2 liberated from the mélange at temperatures of < 200°C was as much as 35%, with up to 40% of the SiO2 loss related to the smectite-illite (S-I) conversion reaction, and the rest attributable to the pressure solution of detrital quartz and feldspar. Kinetic modeling of the S-I reaction indicates active liberation of SiO2 at approximately 70°C to 200°C, with peak SiO2 loss at around 100°C, although these estimates should be slightly shifted toward lower temperature conditions based on X-ray diffraction (XRD) analyses of mixed-layer S-I in the Mugi mélange. The onset of pressure solution was not fully constrained, but has been documented to occur at around 150°C in the study area. The deposition in deformed shales of quartz liberated by pressure solution and the S-I reaction is probably linked to seismogenic behavior along the plate interface by (1) progressively enhanced velocity-weakening properties, which are favorable for unstable seismogenic faulting, including very-low-frequency earthquakes and (2) increasing intrinsic frictional strength, which leads to a step-down of the plate boundary décollement into oceanic basalt.
- Subduction zone
The deposition of quartz as pore-filling cement and/or veins is a common diagenetic process during burial sedimentation, and can cause dramatic modifications of bulk-rock mechanics, including changes in stiffness (Laubach et al. 2004), consolidation behavior (Karig and Morgan 1994), and frictional properties (Lockner and Byerlee 1986). In sandstone reservoirs, quartz cementation starts at approximately 90°C (McBride 1989), whereas in shales, evidence of pore-filling cementation is rare, with mineralized veining being a much more common form of quartz deposition (van de Kamp 2008). The SiO2 deposited in sandstone cements is thought to be derived from pressure solution of detrital quartz and feldspar, although some studies emphasize the importance of external SiO2 sources, such as smectite-illite transformation (S-I) reactions in accompanying shales (Hower et al. 1976; van de Kamp 2008).
At subduction margins, incoming sedimentary deposits are buried along the plate boundary thrust. The underthrusting causes these sediments to undergo several diagenetic reactions during burial. These processes might have a first-order influence on the mechanical transition from aseismic shallower deformation to unstable seismic slip in deeper parts of the subduction zone (Moore and Saffer 2001); indeed, quartz cementation and/or veining have been invoked as a cause of the formation of seismogenic plate boundaries (Byrne 1998; Moore and Saffer 2001; Moore et al. 2007). A recent friction experiment by Saito et al. (2013) suggested that lithification of the plate boundary fault due to quartz deposition can also cause very-low-frequency earthquakes (VLFE) at shallow subduction zones (less than approximately 10-km depths; e.g., Ito and Obara 2006; Obana and Kodaira 2009; Ando et al. 2012; Sugioka et al. 2012). However, the origin, timing, and volume of this cementation and/or veining have yet to be documented in detail. In on-land accretionary complexes, quartz deposition has been documented in deformed rocks that underwent diagenesis at 100°C to 120°C (Moore and Allwardt 1980). Byrne (1998) suggested that pressure solution promotes quartz cementation in these types of environments. However, as the majority of plate boundary faults are located in smectite-rich horizons (Underwood 2007), the S-I reaction could also supply significant amounts of silica, although this factor has not been assessed in previous research.
In this study, we examined the behavior of mobilized SiO2 along the subduction zone plate interface by measuring the frequency and volumetric ratio of quartz-dominated mineralized veins present within an on-land accretionary complex of the Shimanto Belt (Mugi mélange), Japan. As a possible source for such veining, we focused on the diagenetic S-I reaction in the host-rock shales. For this purpose, bulk and clay fraction mineralogy was investigated by X-ray diffraction (XRD) analyses. We also modeled possible pathways of the S-I reaction by considering the underthrusting sediments in the Nankai margin as an analog setting. Based on these results, we detail the SiO2 behavior and its mechanical consequence on plate boundary faults in subduction zones.
Analysis of vein frequency and volumetric fraction
We examined the occurrence and distribution of mineralized veins hosted in deformed shales (vein II) along a transect that includes the entire section of unit 2 of the Mugi mélange from basal basalts to uppermost terrigenous sandstones (Figure 1c). We used a caliper to measure the thickness of every vein that intersected the transect line. Although our measurement was one-dimensional (1-D), the cumulative thickness of veins along the transect is almost equivalent to the volumetric fraction in bulk rock, because the transect runs almost perpendicular to the mélange foliation, and vein II mostly occurs parallel or slightly oblique to the foliation. Basalt-hosted veins were excluded from our analysis because it was not possible to discriminate between veins formed before subduction, associated with near-ridge fluid circulation, from those formed after subduction. When estimating the volume fraction, we also excluded veins in sedimentary horizons around the basal basalt, since Sr isotope analysis suggested that some of these veins have been influenced by dehydration of the basalt (Yamaguchi et al. 2012).
We collected two shale samples (ML-01 and ML-02) from the study area (marked in Figure 1c). For bulk-rock analysis, rock chips were powdered in an agate mortar, and these powders were mounted on sample holders by side-loading to minimize the development of a preferred orientation of clay minerals. Bulk XRD patterns were obtained using a MAC Science MX-Labo with monochromatized CuK α radiation at 40 kV and 30 mA, with 1° divergence and anti-scattering slits, and a 0.15-mm receiving slit in continuous scan mode at a rate of 1°2θ per minute. Relative abundances of the constituent minerals (total clays, quartz, plagioclase, and calcite) were estimated by applying a normalization factor given by Underwood et al. (2003). However, the present analysis is not strictly quantitative because of the difference in experimental apparatus, and thus the data should be considered semi-quantitative.
Other chips were gently crushed and dispersed ultrasonically in distilled water; the clay fraction (< 2 μm) was then separated by centrifugation and soaked two times in 1 M CaCl2 solution (for more than 6 h in each treatment) to prepare Ca-saturated specimens. Suspensions of Ca-saturated specimens were dropped onto glass slides and dried in an oven at 60°C (air-dried, AD). These mounts were exposed to ethylene-glycol vapor at 60°C overnight (EG). XRD patterns for these mounts were recorded using a Rigaku Rint-2500 (Advanced Characterization Nanotechnology Platform, The University of Tokyo) with monochromatized CuK α radiation at 40 kV and 200 mA, with 0.5° divergence and anti-scattering slits, and a 0.3-mm receiving slit in continuous scan mode at a rate of 1°2θ per minute. Relative weight ratios for clay phases were estimated by applying a Biscaye's weighting factor (Biscaye 1965), which assumes a linear correlation between the peak area of the component and its abundance (1× for smectite, 4× for illite, and 2× for chlorite).
For decomposition of the 10-A peak profile, the samples were rescanned in step scan mode for 4 s every 0.02°2θ step, and obtained profiles were processed by DECOMPXR (Lanson 1997). A background was linearly interpolated from 6.5 to 10°2θ range and subtracted from the experimental pattern. Gaussian curves were composed to fit the original pattern without pattern smoothing. NEWMOD (Reynolds 1985) was used to calculate 1-D XRD patterns for mixed-layered clays.
Modeling of silica release along the plate interface during the S-I conversion reaction
The S-I reaction at the Nankai margin, as observed in several drilling holes (Steurer and Underwood 2003), was well reproduced by this kinetic expression (Saffer et al. 2008; Saffer and McKiernan 2009).
We consider the Muroto transect of the Nankai Trough as an analog setting of diagenesis for the Mugi mélange. Temperature-time history for the kinetic modeling is constructed using an underthrusting deposit at a rate of 4 cm/year in a geothermal structure modeled by Spinelli and Wang (2008). The numerical modeling of Spinelli and Wang (2008) examined the effect of fluid circulation in the upper oceanic crust on the subduction zone thermal condition, and provided two models for the Nankai margin: a cooler one with preferred hydrothermal circulation, and a warmer one with no fluid circulation. The temperature difference of the décollement between the two models at a landward distance of 100 km from the deformation front is approximately 70°C. In our kinetic calculation, we also adopted these two models in order to test how the subduction zone thermal model affects the progress of the illitization reaction. Equation 1 was solved numerically by the finite difference method. We used an S-I content value of 40 wt.% in the incoming deposit, and an initial state of 80%S at the trench of the Muroto transect (Saffer et al. 2008). A sensitivity test was also performed with respect to the plate convergence rate and initial state of %S.
The veins hosted in the matrix shales of the Mugi mélange are < 1- to 12-mm thick, with most being < 1 mm (Figure 2b). Figure 2c shows the spatial variation in vein frequency (Matsumura et al. 2003) and cumulative thickness at 1-m intervals. Veins are concentrated within sedimentary horizons near the fault zone below the basalt (Matsumura et al. 2003), with this heterogeneity also apparent in the cumulative thickness distribution. In addition, vein density is lithology-dependent, with fewer veins in horizons containing abundant sandstone and siliceous shale lenses, and more frequent veining within homogeneous shales. In total, the mineralized veins occupy approximately 0.4 vol.% of the total amount of rock (bulk rock) along the transect. This value of volume fraction is comparable to the previous estimation for veins related to shear fabrics in the Yokonami mélange, which is another exhumed tectonic mélange in the Shimanto Belt, Shikoku (approximately 1 vol.%; Hashimoto et al. 2012).
Integrated peak intensities and calculated bulk rock mineral compositions
wt.% in clay fraction*
wt.% in bulk rock**
wt.% in clay fraction
wt.% in bulk rock
Results of peak decomposition for the I-S band
Ordered S-I (low angle)
Ordered S-I (high angle)
Origin of SiO2 for mineralized veins
The majority of SiO2 in the veins observed along the transect is thought to have originated from pressure solution of detrital quartz and feldspar in deformed shales (Kawabata et al. 2007). Kawabata et al. (2007) determined the variation in whole-rock geochemistry of scaly shales in the Mugi mélange, and used a Ti-normalized isocon approach (Grant 1986) to estimate a total volume loss of 17 to 54 vol.% from the deformed mélanges during pressure solution deformation, the majority of which was fluid-mobile SiO2. However, this value represents a net volume reduction and should therefore also involve other sources, e.g., S-I or illite-muscovite reactions. In order to quantify the amount of SiO2 contributed to this volume loss by the various sources, we determined the amount of SiO2 removed by S-I reactions as follows.
This equation predicts that the S-I reaction yields 18 wt.% SiO2 from primary smectite. Boles and Franks (1979), using a different chemical composition, estimated a SiO2 loss of 23.3 wt.%, while Leder and Park (1986) suggested a loss as high as 28 wt.%. Above 200°C, the illite-muscovite conversion reaction will be enhanced and can liberate a further 17 to 23 wt.% of SiO2 from the original illite (van de Kamp 2008). Therefore, if one assumes a shale containing 50 wt.% smectite, the S-I reaction can potentially yield 9 to 14 wt.% of SiO2 from bulk sediments (18 to 28 wt.% of primary smectite) until the completion of the reaction.
At subduction margins, extensive research has quantified the mineralogy of incoming sediments (Underwood 2007). At the Nankai margin, smectite comprises some 20 to 50 wt.% of the bulk sediments within the Lower Shikoku Basin facies, which hosts the décollement-equivalent horizon, yielding a possible 4 to 14 wt.% of SiO2 mobilized by the S-I reaction.
Our XRD analyses show that the two shale samples have almost identical mineral compositions, containing approximately 35 wt.% of S-I, possibly as a product of a diagenetic reaction (Table 1). Considering previous reports on the relatively homogeneous nature of the matrix shale throughout the units (units I, II, and III; Ikesawa et al. 2005; Kawabata et al. 2007), the mineralogical properties shown here are thought to be representative of the whole units in this area. The weight fraction of 35 wt.% of S-I in the shale is almost equivalent to the smectite content in the Nankai sediments, and thus, comparable amounts of SiO2 (i.e., 4 to 14 wt.%) may have been released from the shales of the Mugi mélange. However, if we consider the net volume of SiO2 removed at temperatures of < 200°C, the isocon methods suggest a 35 wt.% loss of SiO2 from the original mudstone (Kawabata et al. 2007). This indicates that up to 40% of the total mass loss estimated by the isocon method was explained by S-I reactions, with the rest attributable to pressure solution of detrital quartz and feldspar. Liberation of as much as 14 wt.% SiO2 from the original mudstone is obviously enough to account for the observed quartz veining in the Mugi mélange, meaning that this excess SiO2 may have cemented associated sandstones, or may have left the system.
Moore and Allwardt (1980) suggested that incipient pressure solution occurs in exhumed accretionary complexes that undergo diagenesis at temperatures of 100°C to 120°C, with this process being dominant at temperatures above 200°C. Although the onset of pressure solution in the Mugi mélange has not been well constrained, pervasive pressure solution seams defined by dark cleavages are present in shales that were deformed at around 150°C (Kawabata et al. 2007). In contrast, the behavior of SiO2 mobilized during the S-I reaction can be more quantitatively assessed by kinetic modeling. Here, we reproduce S-I reaction pathways along the Nankai Trough plate interface as an analog setting for the Mugi mélange (Figure 6a). In these calculations, we assume that the initial content of smectite in the incoming deposit is 40 wt.%, and that 18 wt.% of SiO2 was liberated as a proportion of the original smectite until the end of the reaction. In addition to the results of calculations of the S-I reaction progress, Figure 6a also shows cumulative SiO2 liberation during this reaction. As the reaction proceeds, approximately 6 wt.% SiO2 is progressively released from the underthrusting deposit; Figure 6b shows the rate of SiO2 release as a function of temperature. This calculation demonstrates that the S-I reaction actively supplies SiO2 at temperatures of 70°C to 200°C, with the reaction continuing at higher temperatures. A sensitivity test indicates that the reaction temperature does not change significantly within the parameter ranges examined, while the reaction rate is highly dependent on variables such as the plate convergence rate and initial states of %S (Figure 6c,d). The temperature range for the active release of SiO2 is comparable to the estimated formation temperatures of quartz veins in the Mugi mélange (125°C to 245°C).
Comparison between kinetic prediction of S-I conversion and actual state of S-I in on-land samples
To check the validity of the kinetically predicted reaction progress of S-I conversion, the modeling results were compared with the mixed-layer S-I in the Mugi mélange. As mentioned earlier, the peak decomposition of approximately 10-Å reflection indicates that the S-I phase in the samples is ordered (R = 3) S-I of approximately 10%S. It is noted that 10%S of S-I is slightly lower than the kinetically expected value (15%S to 25%S; Figure 6a), considering the maximum paleotemperature of the Mugi mélange from vitrinite reflectance measurements (130°C to 150°C; Ikesawa et al. 2005).
Although the downhole progress of S-I conversion at the Nankai margin was successfully reproduced by the above kinetic expressions (Saffer et al. 2008), it is uncertain as to whether they are still applicable to modeling of diagenesis at great depths. In fact, K-feldspar was rarely detected by XRD in the analyzed shales, possibly because of completion of the albitization reactions of feldspars (Moore et al. 2007), and it is therefore probable that the activity ratio of K/Na in such conditions is controlled by other equilibrium states (e.g., albite-illite equilibrium). Moreover, deformation features such as mélange fabric and pervasive pressure solution cleavages are apparent in the analyzed samples. It has been inferred that the S-I reaction can be accelerated by deformation itself (e.g., Vrolijk and van der Pluijm 1999) and/or chemical anomaly of circulated fluids during deformation (e.g., Dellisanti et al. 2008). Although the sampling site of ML-01 is located in the vicinity of the basalt rock (at a distance of 5 m), close similarity of the two XRD patterns suggests that the S-I reaction may not have been affected by basalt-related deformation and/or fluids. However, both samples are involved in tectonic processes of mélange formation, and if these processes foster the rate of the conversion reaction, active SiO2 liberation will take place at a slightly lower temperature condition than the theoretical estimation.
Implications for seismogenesis at subduction zones
The second important aspect is an increase in the intrinsic frictional coefficient of the décollement, which may eventually lead to décollement step-down into the subducting oceanic basalt (Figure 7). Tectonic mélanges often include slabs or fragments of oceanic basalt, the presence of which can be explained by décollement step-down and subsequent underplating of the downgoing mélange, in addition to movement of the upper part of the basement into the overriding plate (Kimura and Ludden 1995; Kimura et al. 2011). Ikesawa et al. (2005) identified fault rocks such as cataclasites and ultracataclasites at the base of a section of incorporated basalt and argued that fracturing of basalt is a seismogenic process. The occurrence of high-velocity frictional slip on this fault has been also inferred from several lines of geological evidence, including a rapid injection of basalt-derived fluidized granular material during faulting (Ujiie et al. 2007), stretching of fluid inclusions in calcite by frictional heating (Ujiie et al. 2008), and progress of chloritization in fluidized rock due to frictional heating (Kameda et al. 2011). In addition, it is thought that sites of décollement step-down coincide with the upper aseismic-seismic transition (Matsumura et al. 2003), although the actual controls of this tectonic process are poorly understood. Progressive hardening by ongoing quartz veining and/or cementation is a possible process to increase the frictional strength of the sedimentary décollement by which fracturing can break through to relatively weak levels within the basalt (Figure 7). The initiation of active quartz deposition at temperatures of 100°C is consistent with the onset of décollement step-down at around 150°C.
This work examined the liberation and deposition processes of SiO2 in the deformed shale (the Mugi mélange in the Shimanto accretionary complex), which represents typical deformation features at subduction zone plate boundaries. XRD analysis of the rock and kinetic modeling suggest that the underthrusting of incoming sediments may rapidly foster S-I reactions to release SiO2 at temperatures from approximately 100°C. This condition is consistent with the formation temperatures of quartz veins inferred from fluid inclusion microthermometry. Moreover, the potential mass of SiO2 released during the reaction is large enough to account for the total volume of the veins in the analyzed transect. Progressive SiO2 deposition may be linked to plate boundary seismogenesis, including VLFE and décollement step-down into the oceanic basement during underplating.
We thank H. Tobin, K. Ujiie, and H. Ueda for many suggestions that improved this paper. We also thank J. Ashi and two anonymous reviewers for their careful reviews. DECOMPXR was kindly provided by B. Lanson. This work was supported by Grants-in-Aid for young scientists (24740339) from JSPS, the 'Nanotechnology Platform’ project (12024046), and Grants-in-Aid for Scientific Research on Innovative Areas (21107005) from MEXT.
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