• Proceedings of the Petrological Society of Korea Conference
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• 1999.06a
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• pp.75-78
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• 1999

• Proceedings of the Petrological Society of Korea Conference
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• 2000.05a
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• pp.40-40
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• 2000

• Proceedings of the Petrological Society of Korea Conference
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• 2006.05a
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• pp.39-41
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• 2006

• Proceedings of the Petrological Society of Korea Conference
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• 2009.05a
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• pp.112-114
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• 2009

• Journal of the Mineralogical Society of Korea
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• v.17 no.1
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• pp.1-9
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• 2004

Copper(II) sorbed on kaolinite (KGa-lb) was studied using electron paramagnetic resonance (EPR) and extended X-ray absorption fine structure (EXAFS) spectroscopy. The sorbed copper(II) had an isotropic EPR signal with $g_{iso}\;=\;2.19$ at room temperature. At 77 K, the isotropic signal converted to an axially symmetric anisotropic signal with $g_{\$\mid$}\;=\;2.40,\;g_{\bot}\;=\;2.08,\;and\;A_{\$\mid$}\;=\;131\;G$. These EPR results suggest that the sorbed copper(II) forms an outer-sphere surface complex with a tetragonally distorted $CuO_{6}$ octahedral structure on the kaolinite. In the sorption measurement, the amount of sorbed copper increased with increasing pH of the solution. However, the intensity of the isotropic EPR line was not directly proportional to the amount of sorbed copper. This discrepancy was resolved by assuming the formation of a surface precipitate at higher pH that is invisible by EPR. The EXAFS data confirmed the existence of the surface precipitate. The best fit for the EXAFS of the sorbed copper showed that each copper on the kaolinite had 6.8 copper neighbors located $3.08\;{\AA}$ from it, in addition to the first shell oxygen neighbors, including 4 equatorial O at $1.96\;{\AA}$ and 2 axial O at $2.31\;{\AA}$. This work shows that the local environment of the copper sorbed on the kaolinite changes as a function of pH and surface loading, and that the EPR and EXAFS are useful in studying such changes.

• Journal of the Mineralogical Society of Korea
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• v.5 no.1
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• pp.22-31
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• 1992

The Sancheong kaolin was fractionated into 9 size fractions by wet sieving, sedimentation, and centrifugation. The systematic X-ray diffraction combined with electron microscopy shows that the clay mineral composition of each size fraction is related to the original fabric of kaolin. Minerals such as halloysite (10${\AA}$), kaolinite, illite, and goethite which were formed by procipitation from solution are generally concentrated in the finer fractions, whereas verniculite which was formed by pseudomorphic transformation from other primary minerals are concentrated in the coarser factions. Kaolinits of various types which were formed by precipitation or transformation show a wide size range but they are generally concentrated in the coarser fractions. Halloysite or halloysite-kaolinite clusters in coarse fractions are the fragmentation products of the walls of original boxwork clusters in coarse fractions are the fragmentation products of the walls of original boxwork kaolin which escaped the complete dispersion even through the grinding, ultrasonic agitation, and chemical treatment. Separation of fully hydrated halloysite and kaolinite was possible by systematic wet size fractionation. The coarse-grained minerals such as vermiculite and kaolinite are usually removed during the preparation of clay fraction smaller than 2${\mu}m$, whereas the fine-grained minerals such as illite and goethite are overlooked in X-ray diffraction of the bulk samples because of their minor contents. The systematic wet size fractionation is needed for understanding of the exact mineralogy of kaolin of weathering origin.

• Proceedings of the Korean Ceranic Society Conference
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• 2000.04a
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• pp.15.1-15.1
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• 2000

• Proceedings of the Petrological Society of Korea Conference
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• 2009.05a
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• pp.32-34
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• 2009

• Journal of the Mineralogical Society of Korea
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• v.19 no.1 s.47
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• pp.39-48
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• 2006

X-ray diffaction and chemical analysis were used for mineralogical characteristics of weathering grade of granite and biotite gneiss. Granite is composed mainly of quartz, albite, and minor K-feldspar and biotite gneiss is biotite, quartz, albite. Illite and kaolinite increased in granite, and vermiculite and halloysite in biotite gneiss as increasing weathering process. The percentages of $Al{2}O_{3}$ increase but that of CaO, $Na_{2}O,\;K_{2}O$ decrease as the weathering process. $Fe_{2}O_{3}$ different from granite and biotite gneiss.

• Journal of the Mineralogical Society of Korea
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• v.7 no.1
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• pp.49-61
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• 1994

As the groundwater flows along the fractures of crystalline rocks, it will be in contact with the fracture walls mostly coated by secondary minerals which are quite different form those of host rocks. The presence of fracture-filling minerals in crystalline rocks is important on the view point of radioactive waste disposal because of their great surface reactivity. The Surichi drill hole of 200 m in depth in the Yugu area composed mainly of Precambrian gneiss was selected to study the formation process of clay minerals on the fracture wall of gneiss, and their relation with present groundwater. The water-rock interaction in fractures resulted in the formation of gibbsite and clay minerals. They are formed by two different processes : (1) Incongruent dissolution of feldspar by groundwater diffused from a fracture path into rock matrix produced smectite and illite in situ, (2) on the wall of fracture, gibbsite, kaolinite, smectite and illite are formed by precipitation of dissolved species in groundwater. They show the paragenetic sequence such as gibbsite${\leftrightarrow}$kaolinite${\leftrightarrow}$smectite or illite. The paragenetic sequence of fracture-filling minerals was controlled by increase of pH of groundwater, decrease of fracture permeability by precipitation of fillings, and immobility of alkali or alkaline earths in groundwater. The groundwater from the Surichi borehole is a $Na-HCO_{3}$ type with pH range of 8.6-9.2. The sodium and bicarbonate in groundwater would be supplied by the dissolution of albite and calcite, respectively. The saturation index of groundwater and surface water calculated by WATEQ4F indicates that gibbsite and kaolinite are under precipitation to equilibrium state, and that smectite and illite are under equilibrium to redissolution environment. The stability relation of clay minerals in the $Na_{2}O-Al_{2}O_{3}-SiO_{2}-H_{2}O$ system shows that kaolinite is stable for all waters.