Kurchatovite occurs as colorless granular crystals up to 1 mm at the Fuka mine, Okayama Prefecture, Japan. The mineral is associated with shimazakiite, calcite and johnbaumite. The Vickers microhardness is 441 kg mm−2 (50 g load), corresponding to 4½ on the Mohs’ scale. The calculated density is 3.23 g cm−3. Electron microprobe analyses of kurchatovite gave empirical formulae ranging from Ca0.987(Mg1.004Fe0.020Mn0.001)Σ1.025B1.992O5 to Ca0.992(Mg0.466Fe0.523)Σ0.989B2.013O5 based on O = 5, and kurchatovite forms a continuous solid solution in this range. The mineral is orthorhombic, Pbca, and the unit cell parameters refined from XRD data measured by a Gandolfi camera are a = 36.33(14), b = 11.204(3), c = 5.502(17) Å, V = 2239(12) Å3. It is formed by a layer of MgO6–octahedra, a layer of CaO7–polyhedral and B2O5 consisting of two BO3–triangles. The kurchatovite from the Fuka mine was probably formed by supplying Mg and Fe to shimazakiite from hydrothermal solution at a temperature between 250 to 400 °C.
Ilvaite, a hydrous calcium mixed–valent iron silicate, is found in red hematitic chert (jasper) lenses in altered basalt and an iron–manganese ore from the Sumaizuku unit (Middle Jurassic accretionary complex) of the Northern Chichibu belt, SW Japan. The jasper lenses are composed of ilvaite, andradite, stilpnomelane, riebeckite, hematite and quartz. Ilvaite in the jasper lenses shows an unusual spherical morphology (~ 100 µm in diameter) and each ilvaite spherule exhibits a foam–like microstructure with recrystallized quartz grains. Ilvaite also occurs as discrete euhedral crystals (up to 500 µm in length) in quartz segregation veins or monomineralic ilvaite veins. Ilvaite in the jasper lenses is close to the endmember composition, but the material in the iron–manganese ore is rich in Mn2+ (up to 0.84 atoms per formula unit) corresponding to manganilvaite. Thermodynamic modeling shows that the ilvaite–andradite–hematite–quartz association (ilvaite + O2 = hematite + andradite + quartz) is stable under the peak P–T conditions of the Sumaizuku unit (~ 0.35 GPa, 230–250 °C) and oxygen fugacity slightly above the hematite–magnetite buffer (log fO2 = ~ –38). Ilvaite spherules are intimately associated with colloform–textured andradite, suggesting that they probably originated from a Ca–Fe–Si colloidal precursor deposited along hydrothermal fluid conduits within the Early Permian oceanic crust, and recrystallized during subduction–related low–grade metamorphism.
Jadeite occurs as the shocked product of albite feldspar in shocked meteorites, and is one of the most common high–pressure polymorphs in shock–melt veins of meteorites. The characteristic textures of jadeite in shocked ordinary chondrites show that some of jadeite crystals were formed from originally albite feldspar by a solid–state transformation and some were crystallized from a shock–induced albite melt. Based on these textures of jadeite together with the other high–pressure mineral assemblages and their crystallization kinetics, we can estimate the impact conditions such as impact velocity and parent–body size.
Occurrence and mineralogical properties of pinkish colored epidotes that were found in core samples from a geothermal exploration well NB–1, Noboribetsu, Hokkaido, Japan are described together with estimating the formation conditions. The minerals occurred mainly as vein– and druse–fillings in volcaniclastic rocks of the Miocene Osarugawa Formation. They coexisted with brownish chlorites, K–feldspar, illite, and quartz, and associated with minor hematite, titanite, and/or apatite. The minerals were produced by local K–alteration that overprinted early–formed regional propylitization associated with ordinary greenish epidotes and chlorites. The cell parameters of pinkish epidote were: a = 8.884(6), b = 5.614(1), c = 10.149(7) Å, β = 115.5(8)°, and V = 456.9(4) Å3. The Ca2Mn3+3Si3O12(OH) contents of the pinkish epidotes were generally less than 2.4 mol%, while the Ca2Fe3+3Si3O12(OH) contents attained 28 mol%. It is considered that the low Mn contents and relatively low Fe contents resulted in giving the characteristic pinkish to pale yellow colors for epidote. Associated brownish chlorites were characterized by low total Fe and relatively high Fe3+ contents. Their formation temperatures were estimated to be 230–300 °C, using semi–empirical chlorite geothermometers. These data indicate that pinkish epidotes coexisted with brownish chlorites formed under oxidative conditions and probably low Fe contents in hydrothermal fluids.
Vol.31 (1944) No. 5 and No.6 in the predecessor journal ″The Journal of the Japanese Association of
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