• 자원환경지질
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• 제9권4호
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• pp.177-212
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• 1976

Shap 화강암체내(花崗岩體內)에는 함휘수연(含輝水鉛) 석영맥(石英脈)들이 잘 발달(發達)하며 이들맥(脈)에는 기타 류화진물도 수반된다. 본(本) 연구는 본(本) 화강암(花崗岩)에 관(關)한 지화학적연구와 휘수연석(輝水鉛石)의 광화작용(鑛化作用)에 관(關)한 예비연구로서 반암동진상과도 비교 검토하였다. 즉 모암(母岩)에서의 주성분(主成分)및 부성분진물의 원소(元素)와 모암(母岩)의 변질(變質)과 맥(脈)의 변질(變質) 그리고 주(主)로 열수(熱水) 변질(變質)과 관계(關係)된 휘수연석(輝水鉛石)의 광화작용(鑛化作用)에 대(對)하여 연구하였다. 휘수연석(輝水鉛石)의 광화작용(鑛化作用)과 기타 휘창연석(輝蒼鉛石)과 황동석(黃銅石)과 같은 광물(鑛物)의 광화작용(鑛化作用)은 특히 맥(脈)과 인접한 열수변질작용(熱水變質作用)과 밀접한 관계(關係)가 있으며 정장석(正長石)의 변질작용(變質作用)이 우세한 곳에 이들 광화작용(鑛化作用)이 우세하다. 변질작용(變質作用)과 광화작용(鑛化作用)의 pattern이 구별되고 이 pattern은 변질작용(變質作用)과 광화작용(鑛化作用)의 순서와도 일치(一致)하는 몇개의 뚜렷한 대(帶)를 형성한다. 맥(脈)과 세맥(細脈)들과 이들의 변질(變質)은 동심원상대(同心園狀帶)로 더욱 세분(細分)될수 있다.

• 자원환경지질
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• 제28권6호
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• pp.613-621
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• 1995

한국의 상동광상을 비롯한 일본, 미국, 구러시아 등지의 중석광상은 백악기 후기에 형성되었다. 그러나 세계 매장량의 반을 차지하는 중국의 중석광상은 쥬라기 후기로부터 백악기 초기에 형성되었다. 백악기 후반의 중석광상에서는 휘수연의 광화작용이 중석광화작용과 밀접히 수반되는 한편 중국의 중석광상에서는 휘수연 뿐만 아니라 주석도 밀접한 수반관계를 보인다. 중국의 중석광상은 세계 매장량의 과반수를 차지하기 때운에 이들의 산상은 다양하며 대체로 세계 중석광상의 성인을 대표하고 있다고 하겠다. 한국의 경우 90% 이상의 생산량을 보인 상동광상에서는 휘수연석이 부산물로 생산되었다. ppm 단위의 주석이 감지되지만 실제 석석은 상동광체에서 관찰되지 않았다. 수집된 기존 자료를 확인하기 위해 중국의 모평광상과 한국의 대화광상을 비교해 보았다. 두 광상의 석영맥에서 산출되는 광물은 거의 유사하나 특이한 점은 중국 모평에서는 진발다이트와 석석이 다량 산출된다는 점이다. 모평광상의 휘수연-석영맥중 채취한 진발다이트와 백운모의 연령은 181.1 Ma와 167.8 Ma 이고, 대화의 휘수연-석영맥중 백운모는 80.9 Ma와 80.2 Ma를 각각 얻었다. 한국의 백악기 후기 마그마로부터 공급된 중석 광화용액 중에는 주석이 중국처럼 그 양이 증가하여 중석광화작용에 후속되리만큼 충분히 공급되지 않았기 때문에 한국의 중석광상에서는 주석이 수반되지 않았다고 추정된다.

• 자원환경지질
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• 제25권3호
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• pp.283-296
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• 1992

The Keumryeong deposits is a low grade copper deposits in which copper minerals form disseminated grains and thin veinlets in felsic volcanics seem to be dacite. Alteration of the volcanics consists mainly pervasive propylitization and silicification. Potassic alteration characterized by biotite developed locally adjacent to southwestern contact of granodiorite body. Principal sulfide minerals in altered zone are mainly pyrite and lesser chalcopyrite. Chalcopyrite content in potassic zone is relatively higher than that of surrounding propylitized zone. Pyrite and chalcopyrite accompanies magnetite, molybdenite, sphalerite, pyrrhotite, arsenopyrite, pentlandite, marcasite, hematite, ilmenite, rutile, bismuthinite and native Bi as disseminations, veinlets and knots. Granodiorite body is propylitized and contains veinlets of pyrite, chalcopyrite and molybdenite. Fluid inclusions in sulfide-bearing quartz veinlets and quartz grains of felsic volcanics and granodiorite in altered zone consist of liquid-rich, vapor-rich, $CO_2-bearing$ and halite-bearing inclusions. These four types of inclusion intimately associated on a microscopic scale and indicate condensing or boiling of ore fluid during mineralization. Homogenization temperature of coexisting fluid inclusions are mostly in the range of 350 to $450^{\circ}C$. High salinity fluid contains 28.6 to 48.4 weight percent NaCI equivalent and moderate salinity fluid cotains 0.5 to 12.5 weight percent NaCl equivalent. Pressure estimated from $CO_2$ mole fraction of $CO_2-bearing$ inclusion range 160 to 375 bars. The Kigu copper deposits is a fissure filling copper vein developed 500 m south from the Keumryong deposits. Mineralogy and fluid inclusion data of the Kigu deposits are similar to that of the Keumryeong deposits. Homogenization temperature of fluid inclusions from the Kigu deposits are reasonable agreement with temperature estimated from sulfidation curve of cubanite-chalcopyrite-pyrite-pyrrhotite and pyrite-pyrrhotite mineral assemblages. Not only mineral occurrence and wall rock alteration in the Keumryeong deposits but also fluid inclusion data such as temperature, salinity, pressure and boiling evidences are similar to those of porphyry copper deposits.

• 자원환경지질
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• 제5권3호
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• pp.145-150
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• 1972

This report is written for presenting a principal theme of study about. the origin of Sangdong ore deposit in details, being an aid to find new ore bodies, on the basis of mineralogical charactor and geological feature. Main vein in Sandgong mine has characteristic zonal distribution and localization of minerals. 3 kinds of minerals, that are quartz, hornblende, diopside, form systematically their each rich zones. Other minerals like plagioclase, native bismuth, sphene, molybdenite and wolframite are developed locally. According to the zonal distribution and localization of the minerals, the authors presume that mineralizing agents which changed interbedded limestones into ore bodies act and come up from non-exposed igneous body in the direction perpendicular to the platy main vein. That non-exposed igneous body, presumed, might be extended from the exposed igneous bodies in the southern part of Sangdong mine.

• 자원환경지질
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• 제21권3호
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• pp.309-318
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• 1988

한국(韓國)에는 330여종(余種)의 광물(鑛物)이 기재(記載)되였으며, 기중(其中) 50여종(余種)이 광물자원(鑽物資源)으로 산출되고 있다. 1986년도(年度)에는 은(銀), 연(鉛), 중석(重石), 휘수연석(輝水鉛石), 요업광물(窯業鑽物), 석회석(石灰石) 및 흑연등(黑鉛等) 14종(種)의 광산물을 수출(輸出)한 바 있다. 또한 최근(最近) 5년간(年間)(1982-1986) 국민총생산중 광업부문(鑛業部門)이 차지하는 비율(比率)은 1.5%를 지속하고 있다.

• 암석학회지
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• 제11권2호
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• pp.90-102
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• 2002

홍천 철-희토류광체는 자철석, 안케라이트, 능철석, 마그네사이트, 스트론티아나이트가 주구성광물이며 모나자이트, 콜롬바이트, 퍼구소나이트, 인회석 아지린휘석, Na-앰피볼. 황철석 황동석 중정석등이 부구성광물들이다. 광체주변부는 Na교대작용에 의하여 페나이트화(fenitization) 되었으며 순수 알바이트와 Na-앰피볼로 구성된다. 희토류광의 주구성광물은 모나자이트 ($Ce_{0.49}$ $La_{0.31}$ $Pr_{0.14}$ $Nd_{0.03}$$Gd_{0.03}$ $PO_4$이며, 스트론티아나이트 $Ca_{0.02-0.16}$ $Sr_{0.84-0.98}$ $CO_3$와 미르메키틱 조직을 보이고 앤케라이트등의 탄산염광물들에 의하여 용식되어있다. 광물 정출순서는 미세균열발달 유무에 의하여 전기와 후기로 나누어지며, 그중 전기광물은 용액내에 축적된 $CO_2$개스로 인한 파쇄작용 때문에 미세균열이 형성되어 있다. 자철석, 안케라이트, 마그네사이트, 모나자이트, 인 회석들이 전기 정출광물들이며, 콜롬바이트, 퍼구소나이트, 능철석, 희수연석등은 미세균열이 없는 후기광물들이다. 그러나 안케라이트, 마그네사이트, 모나자이트, 스트론티아나이트, 중정석, 황철석은 전기에서부터 후기까지 연속적으로 수반되며 이들은 미세균열이 잘 발달된 것들과 없는 것들이 복합적으로 관찰되어진다. 다양한 탄산염광물, 자철석, 희토류광물인 모나자이트, 퍼구소나이트, Sr 함유광물인 스트론티아나이트, Nb광물인 콜롬바이트가 출현하는 것으로 대표되는 광물조합및밌 광물화학, 모나자이트와 안케라이트의 미르메키틱 광물조직, 광체주변부를 따라 형성된 페나이트들은 홍천 철-희토류광상이 탄산염암멜트에서 형성되었고 암석은 후기 철질-탄산염암 또는 안케라이트-탄산염암임을 강력히 시사한다.

• 자원환경지질
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• 제7권2호
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• pp.45-62
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• 1974

Scheelite deposits in Sangdong mine are divided into three parallel vein groups, namely "Hanging-wall vein" which is located in the lowest parts of Pungchon Limestone, "Main vein" the most productive vein replaced a intercalated limestone bed in Myobong slate, "Foot-wall veins" a group of several thin veins parallel to main vein in Myobong slate. Besides the above, there are many productive quartz veins imbedded in the above veins and Myobong slate. Molybdenite and wolframite are barren in the former three veins group but associates only in quartz veins. Both main vein and foot-wall veins show regular zonal distribution, quartz rich zone in the center, hornblende rich zone surrounding the quartz rich zone and diopside rich zone in the further outside to the marginal parts of the vein. According to the distribution of three main minerals, quartz, hornblende and diopside the main vein can be divided into three zones which are in turn grouped into 7 subzones by distinct mineral paragenesis. They are summerized as follows: A. Diopside rich zone: 1. garnet-diopside.fl.uorite subzone 2. diopside-zoisite-quartz subzone 3. diopside-plagioclase subzone B. Hornblende rich zone: 4. hornblende-diopside-quartz subzone 5. hornblende-quartz-chlorite subzone 6. hornblende-plagioclase-quartz.sphene subzone C. Quartz rich zone: 7. quartz-mica-chlorite subzone The foot-wall veins can similarly be divided by mineral paragenesis into 3 zones, 6 subzones as follows: A. diopside rich zone: 1. garnet-diopside-quartz.fl.uorite subzone 2. garnet-diopside-wollastonite subzone B. Hornblende rich zone: 3. quartz-hornblende-chlorite subzone 4. hornblende-plagioclase-quartz subzone 5. hornblende-diopside-quartz subzone C. Quartz rich zone: 6. quartz-mica subzone The hanging-wall vein is generally grouped into 9 subzones by the mineral paragenesis which show random distribution. They are as follows: 1. diopside-garnet-fluorite subzone 2. diopside-zoisite-quartz subzone 3. diopside-hornblende-quartz-fluorite subzone 4. wollastonite-garnet-diopside subzone 5. hornblende-chlorite-quartz subzone 6. quartz-plagioclase-hornblende-sphene subzone 7. quartz-biotite subzone 8. quartz-calcite subzone 9. calcite-altered minerals subzone Among many composing minerals, garnet specially shows characteristic distribution and optical properties. Anisotropic and euhedral grossularite is generally distributed in the hanging wall vein and lower parts of the main vein, whereas isotropic and anhedral andradite in the upper parts of the main vein. Plagioclase (anorthite) and sphene are distributed ony near the foot-wall side of the aboveveins. wollastonite is a characteristic mineral in upper parts of the hang-wall vein. Molybdenite is distributed in the upper parts of quartz veins and wolframite in lower parts of quartz veins.

• 자원환경지질
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• 제27권1호
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• pp.11-28
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• 1994

The Anyang Feldspar Mine is located in Seoksu Dong, Anyang City, Kyeonggi Do, Korea and has a long exploitation record that is once produced high grade sodium feldspars, for glaze. Geologically, This area is mainly composed of Mesozoic Jurassic biotite granite (Anyang granite) which intruded Precambrian Kyeonggi Gneiss Complex outcroped near the mining area. The deposit is localized on the southwest hill side of Anyang granite batholith and is confined in hydrothemal alteration zone formed by sodium-rich alkali hydrothermal fluids along the fractures of leucocratic granite showing later differentiation facies in the biotite granite. The hydrothermal alteration is characterized by albitization, sericitization, and desilication. The microscopic observation and EPMA, XRD analysis of the feldspar ores show that major minerals are albite and quartz and accessory minerals are orthoclase and sericite, and they are rarely associated with perthite, fluorite, zircon, kaolinite, molybdenite, microcline and iron-oxide. In the REE pattern, the strong negative Eu anomalies of the feldspar ores indicate the influence of feldspar fractionation and show similiar pattern of the host leucocratic granite. The filling temperature of quartz crystals in ore zone ranges from $276^{\circ}C$ to $342^{\circ}C$, and it is inferred that the alteration occurred by the hypothermal solution.

• 자원환경지질
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• 제31권5호
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• pp.375-388
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• 1998

The purpose of this study is to investigate the ore genesis and occurrence of the Wondong polymetallic mineral deposits. The Pb-Zn, Fe and W-Mo mineralizations are found in skarn zones which formed mainly in or along the fault shear zones with the $N25-40^{\circ}W$ and $N10-50^{\circ}E$ directions, whereas the Cu-Mo mineralization is appeared hydrothermal replacement zone. The skarn minerals consist mainly of garnet and epidote, which were the last alteration phases between pneumatolytic and hydrothermal stages. The mineral paragenesis toward the late stage are as follows: arsenopyrite, scheelite, magnetite, pyrite, pyrrhotite, sphalerite, galena, chalcopyrite and molybdenite. Average ore grades are 0.33 g/t Au, 46.29 g/t Ag, 0.06% Cu, 4.4% Pb, 2.61% Zn and 29.39% Fe in tunnels, and 0.31 % Cu, 0.52% Pb, 6.29% Zn, 29.29% Fe, 0.03% Mo and 0.12% $WO_3$ in drill cores. Fluid inclusion data shows that Type I (liquid-rich), Type II (vapor-rich) and Type III (halite-bearing) inclusions are coexisted and their homogenization temperatures are quite similar. This indicates that boiling conditions have been reached during the mineralization. It is also likely that the ore solutions were evolved through the mixing between magmatic and meteoric waters. Rhyolite and quartz porphyry far the mineralization probably are not responsible of the Wondong polymetallic mineral deposits.

• 암석학회지
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• 제8권1호
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• pp.46-55
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• 1999

Fluid inclusions in granite and hydrothermal quartz indicate that three fluids have affected the Sannae granite. The earliest fluid is represented by three-phase aqueous fluid inclusions with high salinity (38 to 46 wt.% NaCl equiv.). It was exsolves from a crystallizing melt and trapped at a relatively high-pressure condition. The secong fluid is represented by two-phase aqueous fluid inclusion with low entectic temperatures (< $-40^{\circ}C$). low- to moderate salinity (3 to 24.0 wt.% NaCl equiv.) and high homogenization temperatures$ ($309^{\circ}C$$473^{\circ}C$)($. This fluid was trapped at higher pressures than 300-500 bars and precipitated molybdenite and wolframite in quartz veins. It was probably generted by fluid-host rock interactions since they show a wide range of salinity within a narrow range of homogenization temperatures. The final fluid is represented by an aquenous fluid boiling that separated into high-salinity (34-38 wt.% NaCl equiv.) and low-salinity fluid (0 to 8.7 wt.%) at $303-376^{\circ}C$ and 50-150 bars. These boiling fluids precipitated euhedral quartz in miarolitic cavities. The compositions of the final fluid was rather complex in the $H_2$O-NaCl-KCI-$FeCl_2$ system. The Sannae granite was a locus for repeated fluid events including magmatic fluids during the final stage of crystallization, the convection of hydrothermal fluids causing a fluid ascending, fluid boiling, and the local W-Mo mineralization and formation of miarolitic cavities due to thermal, tectonic and compositional properties of the felsic granite.