Progressive Low-Grade Metamorphism Reconstructed from the Raman Spectroscopy of Carbonaceous Material and an EBSD Analysis of Quartz in the Sanbagawa Metamorphic Event, Central Japan

: Low-grade metamorphic temperature conditions associated with the Sanbagawa metamorphic event were estimated by the Raman spectroscopy of carbonaceous material (RSCM) in pelitic rocks and an electron backscatter diffraction (EBSD) analysis of the quartz in siliceous rocks. Analytical samples were collected from the Sanbagawa metamorphic complex, the Mikabu greenstones, and the Chichibu accretionary complex in the eastern Kanto Mountains, central Japan. Previously, low-grade Sanbagawa metamorphism was only broadly recognized as pumpellyite–actinolite facies assigned to the chlorite zone. The RSCM results indicate metamorphic temperatures of 358 ◦ C and 368 ◦ C for the chlorite zone and 387 ◦ C for the garnet zone of the Sanbagawa metamorphic complex, 315 ◦ C for the Mikabu greenstones, and 234–266 ◦ C for the Chichibu accretionary complex. From the EBSD analyses, the diameter of the quartz grains calculated by the root mean square (RMS) approximation ranges from 55.9 to 69.0 µ m for the Sanbagawa metamorphic complex, 9.5 to 23.5 µ m for the Mikabu greenstones, and 2.9 to 7.3 µ m for the Chichibu accretionary complex. The opening angles of the c -axis fabric approximate 40–50 ◦ , presenting temperatures of 324–393 ◦ C for the Sanbagawa metamorphic complex and the Mikabu greenstones. The temperature conditions show a continuous increase with no apparent gaps from these low-grade metamorphosed rocks. In addition, there exists an empirical exponential relationship between the estimated metamorphic temperatures and the RMS values of the quartz grains. In this study, integrated analyses of multiple rock types provided valuable information on progressive low-grade metamorphism and a similar approach may be applied to study other metamorphic complexes.


Introduction
The eastern Asian continent has retained a geological record of long-lived subduction from the Paleozoic through to the present day [1]. The metamorphic complex and the accretionary complex distributed in the Japanese Islands have been formed by the subduction of the oceanic plate since the Paleozoic. In particular, the Sanbagawa regional high P-T metamorphism resulted from the subduction of the Izanagi oceanic plate beneath the eastern Asian continent during the Late Cretaceous to Paleocene [2]. This metamorphism formed the Sanbagawa metamorphic complex, which is classified into chlorite, garnet, and biotite metamorphic zones based on the mineral assemblages [3,4]. The chlorite zone, which corresponds with the pumpellyite-actinolite metamorphic facies, is broadly recognized  [3,11] and (b) geological map of the eastern Kanto Mountains, modified from previous studies [3,11], showing the chert and pelitic rock sample localities. The geological transects X-X' and Y-Y' (pink lines) are shown in Figure 5.

Geological Outline
Low-grade Sanbagawa metamorphism in the Kanto Mountains is recognized in the  [3,11] and (b) geological map of the eastern Kanto Mountains, modified from previous studies [3,11], showing the chert and pelitic rock sample localities. The geological transects X-X' and Y-Y' (pink lines) are shown in Figure 5.
In addition, the metamorphic conditions have been inferred from the quartz fabrics in siliceous rocks. Chert, metachert, and siliceous schist, which were originally deposited in pelagic and deep-sea environments, occur widely in the Chichibu accretionary complex, the Mikabu greenstones, and the Sanbagawa metamorphic complex. Quartz growth is generally controlled by the strain rate, temperature, and hydrolytic weakening [14] and quartz recrystallization may be used as a piezometer during dynamic recrystallization [15,16]. In this study, the metamorphic temperature is estimated from the quartz fabrics of the opening angle (OA) of the c-axis fabric and the quartz diameter in siliceous rocks observed by an electron backscatter diffraction (EBSD) analysis.
The aim of this study is to estimate the conditions of low-grade metamorphism of the Sanbagawa metamorphic complex, the Mikabu greenstones, and the Chichibu accretionary complex based on the RSCM of pelitic rocks and quartz fabric data in the siliceous rocks. In addition, we reconstruct the tectonic setting and thermal history of the accretionary wedge along the subduction zone beneath the eastern Asian continent during the Late Cretaceous to Paleocene.
The Mikabu greenstones consist of two units, the Upper Unit and the Lower Unit, structurally separated by a fault [4]. The Upper Unit is composed of metabasalt, metagabbro, metachert, ultramafic rocks, and minor red mudstone. The Lower Unit consists mainly of phyllite and metabasalt with ultramafic rock. The Upper Unit is assigned to the main part of the Mikabu greenstones whereas the Lower Unit is interpreted as a tectonic mélange between the Upper Unit and the Sanbagawa metamorphic complex [22]. Both units are in the chlorite zone of Sanbagawa metamorphism [4]. The Mikabu greenstones are interpreted as an oceanic plateau that erupted on the Panthalassa Ocean and accreted along the eastern Asian continent during the Early Cretaceous [13]. Anorthosite accompanying metagabbro in the Upper Unit yields a zircon U-Pb age of 157 Ma that represents the eruption age of the Mikabu greenstones during the Late Jurassic [13]. Late Jurassic radiolarians occur in red mudstone in the uppermost part of the Mikabu greenstones [23]. The phengite K-Ar ages of the Mikabu greenstones range from late Early Cretaceous to Late Cretaceous [13,19].  The Chichibu accretionary complex in the study area is divided into three tectonostratigraphic units: Kashiwagi, Kamiyoshida, and Sumaizuku in ascending structural order [24]. The Kashiwagi Unit is dominated by pelagic to hemipelagic sedimentary rocks (chert, dolomitic limestone, tuffaceous shale) and basalt with black shale and minor sandstone. The Kamiyoshida Unit is composed of basalt and basaltic tuff, chert, and a broken formation of sandstone and mudstone. The Sumaizuku Unit is characterized by a mélange with chert and basalt blocks and a broken formation of sandstone and mudstone. The metamorphic grade of the Kashiwagi and Kamiyoshida units is established by the occurrence of alkali-amphibole in basalts [4,17]. Alkali-amphibole has not been reported in the Sumaizuku Unit, indicating that the unit was only subjected to very low-grade metamorphism or diagenesis. Radiolaria in mudstones indicate an Early Jurassic age for the Sumaizuku Unit, Middle Jurassic for the Kamiyoshida Unit, and Middle Jurassic to Early Cretaceous for the Kashiwagi Unit [25][26][27]. Sandstones from the Kashiwagi Unit yield Early Cretaceous detrital zircon U-Pb ages and phengite K-Ar ages [18,21]. The Chichibu accretionary complex formed during the Jurassic to Early Cretaceous.
The chlorite zone (pumpellyite-actinolite facies) assigned to a low-grade part of Sanbagawa metamorphism extends widely through the Sanbagawa metamorphic complex, the Mikabu greenstones, and the Chichibu accretionary complex [3,4]. Temperature and pressure conditions were approximately estimated to be 300-400 • C and 6-7 kbar for the higher chlorite zone of the Sanbagawa metamorphic complex and 200-300 • C and 5-6 kbar for the lower chlorite zone of the Mikabu greenstones and the Chichibu accretionary complex in the Kanto Mountains, central Japan [3,28].

Analytical Methods
Raman spectroscopy measurements were carried out on polished thin sections cut perpendicular to the foliation (i.e., XZ sections). The analyses were made at 30 sites in each thin section to encompass the full range of sample heterogeneity. A Nicolet Almega XR micro-Raman system (Thermo Fisher Scientific, Waltham, MA, USA) at Nagoya University, Nagoya, Japan, was utilized, which is equipped with a green (532 nm) Nd-YAG laser that passes through an optical microscope (Olympus, BX51, Tokyo, Japan) and employs a 100 × objective lens that produces an irradiation power of 3 mW at the sample surface. For each analysis, the Raman spectrum was acquired with a single polychrome spectrometer equipped with a 1024 × 256 pixel CCD detector. The acquisition time for each analysis was 30 s. The wave number resolution was 1 cm −1 in the spectral range measured using 2400 lines per mm grating. The first-order region of the carbonaceous material (CM) Raman spectra contains discriminative bands at around 1350 cm −1 (D1-band), 1580 cm −1 (G-band), 1620 cm −1 (D2-band), 1510 cm −1 (D3-band), and 1150 cm −1 (D4-band) for poorly ordered carbon [29][30][31]. All of the significant peak positions and band areas were resolved using the computer program Peak Fit v. 4.12 (SeaSolve Software Inc., San Jose, CA, USA).
In this study, two temperature equations were used following Mori et al. [32]. If a clear D4-band was present, the temperature equation proposed by Kouketsu et al. [8] was applied using the full width at a half maximum of the D1-band (FWHM-D1) as follows: This equation, which is applicable to the temperature range of 150-400 • C with an estimated error of ±30 • C, yielded temperatures of 231-358 • C for almost all of the samples (Table 1). If the spectrum lacked a D4-band, such as samples KR16 and KR15, the temperature equation proposed by Aoya et al. [33] was applied using the R2 ratio defined by area ratio of D1/(G + D1 + D2) as follows: This equation is applicable to the temperature range of 340-655 • C and has an estimated error of ±30 • C.
The crystallographic orientations of the quartz in siliceous rocks were measured by indexing the EBSD patterns acquired using a Hitachi SU3500 SEM equipped with an HKL EBSD Nordlys-Nano detector (Oxford Instruments, Abingdon, UK) at the Geological Survey of Japan, National Institute of Advanced Industrial Science and Technology, Tsukuba, Japan. Thin sections of 19 samples of siliceous rocks were cut parallel to the foliation and bedding and perpendicular to the stretching lineation (i.e., XY sections). Before the EBSD analysis, the thin sections were polished for several minutes with SYTON fluid using a Buehler VibroMet 2 to remove surface damage. The diffraction pattern acquisition was performed in a low-vacuum mode using an accelerating voltage of 15 keV, a working distance of 18 mm, and a specimen tilt of 70 • . The orientation data were collected using AZtec software and processed with HKL Channel 5 software. All index data in this study are presented as points with a mean angular deviation (MAD) of <1 • . The post-acquisition processing was conducted using a 10 • segmentation angle for grain modeling and a grain size cut-off of 4 pixels.

Metamorphic Temperatures from the RSCM
The metamorphic temperatures of 11 samples of pelitic rock and 3 samples of muddy part in chert were investigated using a RSCM. The pelitic rock samples were pelitic schist from the Sanbagawa metamorphic complex, phyllite from the Lower Unit of the Mikabu greenstones, and shale and mudstone from the Chichibu accretionary complex. No pelitic rocks were found in the Upper Unit of the Mikabu greenstones. The results of the RSCM analyses are presented in Table 1 and selected Raman spectra and microphotographs in Figure 3. Examples of peak separation are shown in Figure 4. The Raman spectra exhibited a clear D1-band and a D2-band and a small D4-band on the left shoulder of the D1-band for almost all of the samples (Figure 4a). The Raman spectra for the samples KR15 and KR16 were characterized by a clear D1-band and a G-band with a small D2-band (Figure 4b).
The structural change of the CM determined from FWHM-D1 is a well-known thermal indicator of very low-grade to low-grade metamorphism [34,35]. The calculated Raman spectra FWHM-D1 values increased along a geological transect ( Figure 5) from the Sanbagawa metamorphic complex to the Mikabu greenstones and the Chichibu accretionary complex. However, the FWHM-D1 values were fairly constant within the lower chlorite zone of the Chichibu accretionary complex. In almost all of the samples from the chlorite zone, a small D4-band usually appeared at around 1245 cm −1 . The D4-band did not appear in samples KR15 and KR16, reflecting their higher metamorphic grade. In addition, the D4/D1 intensity ratios of the samples from the chlorite zone showed a negative correlation with the metamorphic grade ( Figure 5).
The temperature equation by Aoya et al. [33] yielded 368 • C for sample KR15 and 387 • C for sample KR16 (Table 1). For the Sanbagawa metamorphic complex, the garnet zone sample had a calculated temperature of 387 • C and the chlorite zone samples had calculated temperatures of 358-380 • C. We applied the temperature equation by Kouketsu et al. [8] for the other samples with the D4-band. The sample from the Mikabu greenstones (Lower Unit) had a calculated temperature of 315 • C and the samples from the Chichibu accretionary complex had calculated temperatures of 231-315 • C. The calculated temperatures decreased from north to south toward structurally higher positions from the Sanbagawa metamorphic complex to the Mikabu greenstones (Lower Unit) and lastly the Chichibu accretionary complex.

Diameter and Orientation of the Quartz in Siliceous Rocks
In field observations, siliceous rocks are generally named chert, metachert, or siliceous schist according to the increase in metamorphic grade and foliation development. Chert generally occurs in the Chichibu accretionary complex, metachert in the Mikabu greenstones, and siliceous schist in the Sanbagawa metamorphic complex. Fine recrystallized quartz has recently been used as a piezometer to infer the conditions of dynamic recrystallization [15,16]. The focus in this study was on the original diameter of the quartz related to crystallization during metamorphism. The results of the EBSD analysis for the quartz in siliceous rocks are provided in Table 2 and photomicrographs and inverse pole figure (IPF) mapping are shown in Figure 6. The diameter of the quartz was calculated using the root mean square (RMS) of the quartz grains [16,36] (Figure 7). The c-axis orientations of the quartz grains were plotted in lower hemisphere equal area projections ( Figure 8). The median aspect ratio for all samples was estimated to be 1.5 to 1.7 (Table 2).             In the chlorite and garnet zones of the Sanbagawa metamorphic complex, siliceous schists are composed of crystallized quartz with a consistent size distribution of less than several millimeters, based on a microscopic observation (Figure 6a,b). Based on the IPF map, the crystallized quartz from both metamorphic zones occurred as quartz grains of < 200 µm in diameter (Figure 6a,b). The RMS values ranged from 55.9 to 69.0 µm, presenting no significant difference between the samples from the garnet zone and the chlorite zone (Figure 7). The c-axes showed weak, crossed girdle patterns [14], rotated anticlockwise by 10 • for sample KWC27, and a small circle girdle for sample KWC 25 (Figure 8).
The metacherts in the Mikabu greenstones are composed of microcrystalline quartz of < 50 µm in size on the IPF map (Figure 6c-e). The RMS of the quartz grain diameter was 23.5 µm for the Lower Unit and 9.5-12.9 µm (mean = 11.4 µm) for the Upper Unit (Figure 7). The grain size was larger in the metachert from the Lower Unit than the Upper Unit. Sample KWC14 contained a cleavage normal to bedding and fine recrystallized quartz grains were observed along the cleavage (Figure 6d). The c-axis patterns showed a weak crossed girdle rotated clockwise by 10 • for sample KWC14 and Type-I crossed girdle patterns [16] rotated anticlockwise by 10 • for samples KWC06 and KWC02 (Figure 8).
The cherts of the Chichibu accretionary complex are composed of cryptocrystalline quartz (Figure 6f-h). The quartz grains were < 20 µm in size in the Kashiwagi Unit and < 10 µm in the Kamiyoshida and Sumaizuku units. The RMS values ranged from 3.5 to 7.3 µm (mean = 6.4 µm) in the Kashiwagi Unit, 3.0 to 4.6 µm in the Kamiyoshida Unit, and were 2.9 µm in the Sumaizuku Unit (Figure 7). The RMS values of the Chichibu accretionary complex ranged from 2.9 to 7.3 µm, showing a slight increasing trend toward the structurally lower part of the complex. Quartz c-axes showed random patterns with a weak Y maximum elongated toward the X axis for samples KWC 13 and KWC12 and a Y-Z maximum for sample KWC15 (Figure 8).

Relationship between the Quartz Diameter, Opening Angle of the c-Axis Fabric, and Temperature
To investigate the relationship between the quartz diameter and metamorphic grade, we compared the quartz diameter derived from the RMS data with to the temperature derived from the RSCM data obtained from adjacent localities ( Figure 1; Table 2). The quartz diameter showed an exponential relationship with the temperature for values of 2.9-67 µm and 234-387 • C (Figure 9). This correlation is well-described by the following equation: T ( • C) = 39.7 × ln(RMS) + 204 (R 2 = 0.91).
In the dynamic recrystallization regime, quartz deformation occurs by cataclastic flow (CF) at temperatures below 280 • C, by bulging recrystallization (BLG) at temperatures of 280-400 • C, by subgrain rotation (SGR) at temperatures of 400-500 • C, and by grain boundary migration (GBM) at temperatures in excess of 500 • C [37,38]. Furthermore, numerical modeling undertaken by Piazolo et al. [39] revealed that quartz growth during dynamic recrystallization is related to temperature and the strain rate. Stipp et al. [36] also observed an increase in quartz size with temperature and the relationship can be described by an exponential function though the BLG, SGR, and GMB zones. In addition, Faleiros et al. [14] showed that the opening angle (OA) of the c-axis fabric is strongly temperaturedependent through the range of 250-1050 • C during the crystal plastic deformation of quartz, presenting the following equation for the temperature range of 250-650 • C: T ( • C) = 6.9 × OA + 48 (250 • C < T < 650 • C and OA < 87 • ). MC: metamorphic complex; AC: accretionary complex; GS: greenstones; Temp_S: temperature estimated from muddy part in siliceous rocks; Temp_P: temperature estimated from pelitic rocks; Sample_P: corresponding sample of pelitic rocks analyzed by RSCM; STDEV: standard deviation. Figure 9. Relationship between the RSCM temperature estimates and the RMS data for samples from adjacent localities.

Low-Grade Sanbagawa Metamorphism
The conditions of low-grade Sanbagawa metamorphism were reconstructed using the RSCM of pelitic rocks and an EBSD analysis of the quartz in siliceous rocks clarified in this study and reviews of previous studies.
Temperatures estimated from the RSCM data were 358 °C and 368 °C within the chlorite zone, 387 °C in the garnet zone of the Sanbagawa metamorphic rock, 315 °C for the Mikabu greenstones (Lower Unit), and generally 234-266 °C for the Chichibu accretionary complex with 306 °C for sample KWC13 from the Kashiwagi Unit, similar to the temperature estimated for the Mikabu greenstones. The estimated temperatures increased from the Chichibu accretionary complex to the Mikabu greenstones to the Sanbagawa For the samples of the Sanbagawa metamorphic rocks and the Mikabu greenstones, which showed weak c-axis girdle patterns with approximate opening angles of 40-50 • (Figure 8), a temperature range of 324-393 • C was calculated by the equation proposed by Faleiros et al. [14], which agreed well with the temperature range of 315-387 • C estimated from the RSCM data. The increase in quartz diameter was probably caused by temperature as the samples from this study were not subjected to intensive dynamic recrystallization.

Low-Grade Sanbagawa Metamorphism
The conditions of low-grade Sanbagawa metamorphism were reconstructed using the RSCM of pelitic rocks and an EBSD analysis of the quartz in siliceous rocks clarified in this study and reviews of previous studies.
Temperatures estimated from the RSCM data were 358 • C and 368 • C within the chlorite zone, 387 • C in the garnet zone of the Sanbagawa metamorphic rock, 315 • C for the Mikabu greenstones (Lower Unit), and generally 234-266 • C for the Chichibu accretionary complex with 306 • C for sample KWC13 from the Kashiwagi Unit, similar to the temperature estimated for the Mikabu greenstones. The estimated temperatures increased from the Chichibu accretionary complex to the Mikabu greenstones to the Sanbagawa metamorphic complex. However, this trend could not be confirmed for the Upper Unit of the Mikabu greenstones because the pelitic rocks necessary for the RSCM analysis were absent in this unit. The temperatures of the Sanbagawa metamorphic complex and the Mikabu greenstones were also estimated to be 324-393 • C by the OA of the c-axis fabric; however, the trend could not be confirmed.
The temperature conditions were related to the RMS of the quartz grain diameters (Figure 9). The Chichibu accretionary complex samples had RMS values of 2.9-7.3 µm, the samples of the Upper Unit of the Mikabu greenstones had RMS values of 9.5-12.9 µm, and the sample of the Lower Unit of the Mikabu greenstones had an RMS value of 23.5 µm ( Table 2). These additional data also suggest that the metamorphic temperature increased towards structurally lower positions without a large gap. The integration of the data from the RCMS and EBSD analyses helped to constrain the conditions of progressive low-grade metamorphism within the chlorite zone of the Sanbagawa metamorphic complex, the Mikabu greenstones, and the Chichibu accretionary complex.
Recent studies have provided detrital zircon U-Pb ages and phengite K-Ar ages for the Sanbagawa metamorphic complex, the Mikabu greenstones, and the Chichibu accretionary complex [12,[18][19][20][21], which can be used to understand the accretion and progressive metamorphism in the region.
The Chichibu accretionary complex was accreted to the eastern margin of the Asian continent during the Jurassic to Early Cretaceous [24]. The Kashiwagi Unit, which is the youngest unit in the Chichibu accretionary complex, has previously been assigned to the Early Cretaceous (Berriasian to Valanginian) based on radiolarian fossils from mudstone [26,27]. In addition, the detrital zircon U-Pb ages from sandstones of this unit in the eastern Kanto Mountains have a youngest single grain age (YSG) of 127 Ma and a recalculated weighted mean age of the youngest cluster (YC) of 131 Ma, suggesting a maximum depositional age of Early Cretaceous (Hauterivian to Barremian) [21]. Tominaga and Hara [13] noted that the Kashiwagi Unit and the Mikabu greenstones are closely related in the ocean plate stratigraphy. Previously, the Mikabu greenstones were thought to have originated from an oceanic plateau related to the Shatsky Rise at the nearby triple junction of the Izanagi, Farallon, and Pacific plates during the Late Jurassic [40,41]. However, Tominaga and Hara [13], based on a U-Pb age of 157 Ma from anorthosite, proposed that the oceanic plateau was formed in the central part of the Izanagi Plate and that eruption occurred in the Late Jurassic. They also concluded that the Mikabu greenstones were subducted and accreted together with the Kashiwagi Unit during the Early Cretaceous.
Tsutsumi et al. [20] examined the detrital zircon ages of psammitic schist from the Sanbagawa metamorphic complex and presented YSG ages of 95 and 91 Ma for the chlorite zone and 79 Ma for the garnet zone. Using their data, the YC ages were recalculated as 108 and 103 Ma for the chlorite zone and 84 Ma for the garnet zone. These detrital zircon ages show that the maximum depositional ages of the original clastic rocks are, at the latest, Early to Late Cretaceous (Albian to Campanian). The Sanbagawa metamorphic complex was accreted during the Late Cretaceous after the subduction of the Mikabu greenstones and the Kashiwagi Unit. In the most recent tectonic framework, based on detrital zircon chronology, most of the Sanbagawa metamorphic complex is interpreted as the deeper accreted unit of the Cretaceous Shimanto accretionary complex [42][43][44][45]. During the Late Cretaceous, large amounts of oceanic and clastic material were subducted into shallower to deeper parts of the accretionary wedge.
The timing of Sanbagawa metamorphism is inferred to be Late Cretaceous to Paleocene based on the phengite K-Ar ages of the Sanbagawa metamorphic rocks that are 84-72 Ma for the chlorite zone, 82-58 Ma for the garnet zone, 67-53 Ma for the biotite zone [19], and 82-80 Ma for the Mikabu greenstones [18,19]. The closure temperature of the K-Ar isotopic system in phengite is 350 • C [46]; therefore, the K-Ar ages from the Sanbagawa metamorphic complex samples are interpreted to be metamorphic and cooling ages. Older phengite K-Ar ages of 110 Ma [13] from the Mikabu greenstones and 117 Ma [18] from the Chichibu accretionary complex were not reset during Sanbagawa metamorphism because of its low grade (<315 • C).
The tectonic setting and history of Sanbagawa metamorphism is summarized as follows ( Figure 10). During the Early Cretaceous, the Mikabu greenstones and the Chichibu accretionary complex were accreted. In the Late Cretaceous, the protoliths of the Sanbagawa metamorphic rocks were accreted at a deep level in the wedge and the Shimanto accretionary complex was accreted at a shallow level in the wedge. Soon after accretion of the Sanbagawa metamorphic complex, during the Late Cretaceous to Paleocene, the Sanbagawa regional metamorphic event affected the Sanbagawa metamorphic complex, the Mikabu greenstones, and the Chichibu accretionary complex. lows ( Figure 10). During the Early Cretaceous, the Mikabu greenstones and the Chichibu accretionary complex were accreted. In the Late Cretaceous, the protoliths of the Sanbagawa metamorphic rocks were accreted at a deep level in the wedge and the Shimanto accretionary complex was accreted at a shallow level in the wedge. Soon after accretion of the Sanbagawa metamorphic complex, during the Late Cretaceous to Paleocene, the Sanbagawa regional metamorphic event affected the Sanbagawa metamorphic complex, the Mikabu greenstones, and the Chichibu accretionary complex.

Conclusions
Low-grade metamorphism associated with the Sanbagawa metamorphic event was investigated by the RSCM of pelitic rocks and an EBSD analysis of the quartz in siliceous rocks, yielding the following results.
1. The RSCM results indicate metamorphic temperatures of 358 °C and 368 °C for the chlorite zone and 387 °C for the garnet zone of the Sanbagawa metamorphic complex, 315 °C for the Mikabu greenstones, and 234 °C to 266 °C for the Chichibu accretionary complex. 2. From the EBSD analyses, the diameters of the quartz grains calculated from the RMS range from 55.9-69.0 μm for the Sanbagawa metamorphic complex, 9.5-23.5 μm for the Mikabu greenstones, and 2.9-7.3 μm for the Chichibu accretionary complex. In addition, the c-axis patterns of the quartz grains evolved from random to weak crossed girdle patterns from the Chichibu accretionary complex to the Sanbagawa metamorphic complex. The OA of the c-axis fabric approximate 40-50°, presenting a temperature range of 324-393 °C for the Sanbagawa metamorphic complex and the Mikabu greenstones. 3. The increase in estimated metamorphic temperatures and exponential increase in the quartz diameter from the Chichibu accretionary complex to the Mikabu greenstones and the Sanbagawa metamorphic complex, without any apparent gap, records progressive low-grade metamorphism associated with the Sanbagawa metamorphic event. 4. Integrated analyses of multiple rock types including basalts, pelitic rocks, and siliceous rocks provided valuable information on progressive low-grade metamorphism and a similar approach may be applied to study other metamorphic complexes.