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We welcome the constructive comments by Wallis and Endo () on the schematic geological cross section, mineral description, and temperature estimate of the Shiraga serpentinite mass in our paper (Fukumura, Okamoto, & Terabayashi,). As figure 1 in Wallis and Endo () provides detailed outcrop distributions, a better geological map blending data from Fukumura et al. () and Wallis and Endo () was created (Figure). ABSENCE OF ORTHOPYROXENE The absence of orthopyroxene in the Shiraga serpentinite is emphasized by Wallis and Endo (). The valuable observations by Wallis and Endo () therefore strongly support the conclusions of Fukumura et al. () because orthopyroxenes were never recognized with metamorphic olivines in the Shiraga serpentinite. [Extracted from the article]

In their recent paper 'Metamorphic olivine after dehydration embrittlement in Serpentinite: Case study from the Shiraga Serpentinite mass in the Sanbagawa high P/T metamorphic belt, central Shikoku, Japan', Fukumura, Okamoto, and Terabayashi () present information on an important relic of the mantle wedge located in the Sanbagawa belt of central Shikoku. The presence of talc and olivine in the Shiragayama body reported by Fukumura et al. () is in agreement with previous studies (e.g. Kawahara et al.,). MINERAL ASSEMBLAGES The authors report orthopyroxene (opx) in 10 of their 21 samples (table 1 in Fukumura et al.,) but provide no chemical analyses or photomicrographs to support the claim. However, such selection criteria are not mentioned in Fukumura et al. () and a comparison of the patterns of sampling locations does not suggest radically different sampling strategies in the two studies of Fukumura et al. () and Kawahara et al. (). [Extracted from the article]

The present paper reports, for the first time, the occurrence of an omphacite‐bearing mafic schist from the Asemi‐gawa region of the Sanbagawa belt (southwest Japan). The mafic schist occurs as thin layers within pelitic schist of the albite–biotite zone. Omphacite in the mafic schist only occurs as inclusions in garnet, and albite is the major Na phase in the matrix, suggesting that the mafic schist represents highly retrogressed eclogite. Garnet grains in the sample show prograde‐type compositional zoning with no textural or compositional break, and contain mineral inclusions of omphacite, quartz, glaucophane, barroisite/hornblende, epidote and titanite. In addition to the petrographic observations, Raman spectroscopy and focused ion beam system–transmission electron microscope analyses were used for identification of omphacite in the sample. The omphacite in the sample shows a strong Raman peak at 678 cm−1, and concomitant Raman peaks are all consistent with those of the reference omphacite Raman spectrum. The selected area electron diffraction pattern of the omphacite is compatible with the common P2/n omphacite structure. Quartz inclusions in the mafic schist preserve high residual pressure values of Δω1 > 8.5 cm−1, corresponding to the eclogite facies conditions. The combination of Raman geothermobarometries and garnet–clinopyroxene geothermometry gives peak pressure–temperature (P–T) conditions of 1.7–2.0 GPa and 440–540 °C for the mafic schist. The peak P–T values are comparable to those of the schistose eclogitic rocks in other Sanbagawa eclogite units of Shikoku. These findings along with previous age constraints suggest that most of the Sanbagawa schistose eclogites and associated metasedimentary rocks share similar simple P–T histories along the Late Cretaceous subduction zone. [ABSTRACT FROM AUTHOR]