• 자원환경지질
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• 제41권1호
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• pp.1-14
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• 2008

봉상 금-은광상은 백악기 안산암질 래필리응회암 내에 발달된 단층대를 충진한 석영맥광상이다. 이 광상의 광화작용은 단층-각력대에 수반되며 2시기로 구분된다. 1시기는 다시 조기와 말기로 구분되며 주된 광화시기이다. II시기는 광화작용이 관찰되지 않는다. I시기 조기는 모암변질과 천금속 황화광물이 관찰된다. I시기 말기는 금-은광물 정출시기로 자연은, 함은사면동석 및 휘안동은석과 함께 황철석, 섬아연석, 황동석 및 방연석 등의 황화광물이 관찰된다. 유체포유물 자료에 의하면, 광화I시기의 균일화온도와 염농도는 각각 $137{\sim}336^{\circ}C,\;0.0{\sim}10.6wt.%$ NaCl 로서 광화유체가 천수의 혼입에 의한 냉각과 희석이 있었음을 지시한다. 또한, 광화I시기 말기에 관찰되는 광물공생군으로부터 구한 생성온도와 황분압은 $<210^{\circ}C$과 $<10^{-15.4}$ atm를 갖는다. 황(3.4%o 기원은 화성기원과 모암내의 황에서 유래된 것으로 해석된다. 산소{2.9%o과 10.3%o(석영: 7.9%o과 8.9%o, 방해석: 2.9%o과 10.3%o)}, 수소(-75%o) 및 탄소(-7.0%o과 -5.9%o)동위원소값의 자료로 볼 때, 이 광상의 광화유체는 천수 기원의 유체가 주종을 이룬 것으로 보이며 광화작용이 진행됨에 따라 기원이 다른 천수의 혼입이 작용한 것으로 해석할 수 있다.

• 자원환경지질
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• 제47권6호
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• pp.645-655
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• 2014

금 정광으로부터 순수한 금속 형태의 Te을 얻기 위하여 소성처리, 차아염소산 용출, Fe 제거 및 전기분해실험을 수행하였다. 정광 및 소성시료에 포함되어 있는 Au, Ag 및 Te는 왕수보다 차아염소산에서 더 많이 용해된 반면에 Pb, Zn, Fe 및 Cu는 차아염소산보다는 왕수에서 더 많이 용출되었다. 전기분해하기 전, 차아염소산 용출-용액에 NaOH를 첨가한 결과 Fe가 정광시료에서 96% 제거되었지만 소성시료에서는 98% 제거되었다. 전기분해실험을 240분 동안 수행한 결과, 금속 구리가 정광시료에서 98% 회수된 반면에 소성시료에서 99%나 회수되었다. 이는 소성처리에 의하여 S가 제거되었기 때문이다. 양극 슬라임도 정광시료보다 소성시료의 전해질 용액에서 더 많이 생성되었다. 양극 슬라임을 자력선별한 결과 순수한 자연금속 형태의 텔루륨이 정광시료보다 소성시료에서 더 많이 회수되었다.

• 자원환경지질
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• 제32권6호
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• pp.561-573
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• 1999

소백산 육괴 중부지역의 선캠브리아기 변성암류에는 특징적으로 중역수형 금광상이 다수 배태된다. 연동 지역의 홍덕.대원.일생 금 광산도 이에 속하며, 단층 열극을 충진한 괴상의 석영맥 (폭 0.3~3m)으로 산출된다. 광석 광물은 매우 단순하여 주로 자류철석, 섬아연석, 방연석으로 산츨되며, 황철석, 황동석, 엘렉트럼, 사면동석, 자연창이 일부 수반된다. 유체포유물 연구결과, 광화작용은 비교적 높은 온도(240$^{\circ}$~40$0^{\circ}C$)에서 낮은 염농도 (<12 wt. % NaCl equiv.)를 갖는 $H_{2}O-CO_{2}(-CH_{4})$-NaCl계 유체로부터 진행되었다. 석영 내의 유체포유물은 단순한 액상 포유물(Type 1)과 메탄올 함유하는 $CO_2$-rich 포유물(TypeII)로 구분된다. Type II 포유물의 carbonic phase (주로 $CO_2$)의 함량은 동일 시료 내에서도 매우 다양하게 변화하면, carbonic phaseso의 메탄 함량은 대략 2~20 mole%이다. 유체포유물의 균일화온도와 염농도의 관계를 보면, 광화작용의 초기에는 $CO_2$비등을 수반한 유체 불혼화가 일어났으나, 후기에는 냉각작용이 지배적이옷음을 알 수 있다. 광화작용시의 조성 (${\delta}^{34}S_{{\Sigma}S}$=-2.1 to 2.2$\textperthousand$, $\delta$18Owater=4.7 to 9.3$\textperthousand$, $\delta$Dwater=-63 to -79$\textperthousand$ )은 광화유체가 마그마로부터 기원하였음을 지시한다. 본 연구 결과는 연동지역에 부존하는 중온형 금광상의 성인에 대하여 마그마 기원모델을 성공적으로 적용할수 있음을 확인해준다.

• 대한족부족관절학회지
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• 제23권1호
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• pp.1-5
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• 2019

Surgical treatment to restore stability in the ankle and hindfoot and prevent further degenerative changes may be necessary in cases in which conservative treatment has failed. Anatomical direct repair using native ligament remnants with or without reinforcement of the inferior retinaculum is the so-called gold standard operative strategy for the treatment of lateral ankle instability. Non-anatomical lateral ligament reconstruction typically involves the use of the adjacent peroneus brevis tendon and applies only those with poor-quality ligaments. On the other hand, anatomic reconstruction and anatomic repair provide better functional outcomes after the surgical treatment of chronic ankle instability patients compared to a non-anatomic reconstruction. Anatomical reconstruction using an autograft or allograft applies to patients with insufficient ligament remnants to fashion direct repair, failed previous lateral ankle repair, high body mass index, or generalized ligamentous laxity. These procedures can provide good-to-excellent short-term outcomes. Arthroscopic ligament repair is becoming increasingly popular because it is minimally invasive. Good-to-excellent clinical outcomes have been reported after short and long-term follow-up, despite the relatively large number of complications, including nerve damage, reported following the procedure. Therefore, further investigation will be needed before widespread adoption is advocated.

• Journal of the Korean Association of Oral and Maxillofacial Surgeons
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• 제31권3호
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• pp.248-254
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• 2005

The purpose of this study was to investigate the distribution of stress within the regenerated bone surrounding the implant using three dimensional finite element stress analysis method. Using ANSYS software revision 6.0 (IronCAD LLC, USA), a program was written to generate a model simulating a cylindrical block section of the mandible 20 mm in height and 10 mm in diameter. The $5.0{\times}11.5-mm$ screw implant (3i, USA) was used for this study, and was assumed to be 100% osseointegrated. And it was restored with gold crown with resin filling at the central fossa area. The implant was surrounded by the regenerated type IV bone, with 4 mm in width and 7 mm apical to the platform of implant in length. And the regenerated bone was surrounded by type I, type II, and type III bone, respectively. The present study used a fine grid model incorporating elements between 250,820 and 352,494 and nodal points between 47,978 and 67,471. A load of 200N was applied at the 3 points on occlusal surfaces of the restoration, the central fossa, outside point of the central fossa with resin filling into screw hole, and the functional cusp, at a 0 degree angle to the vertical axis of the implant, respectively. The results were as follows: 1. The stress distribution in the regenerated bone-implant interface was highly dependent on both the density of the native bone surrounding the regenerated bone and the loading point. 2. A load of 200N at the buccal cusp produced 5-fold increase in the stress concentration at the neck of the implant and apex of regenerated bone irrespective of surrounding bone density compared to a load of 200N at the central fossa. 3. It was found that stress was more homogeneously distributed along the side of implant when the implant was surrounded by both regenerated bone and native type III bone. In summary, these data indicate that concentration of stress on the implant-regenerated bone interface depends on both the native bone quality surrounding the regenerated bone adjacent to implant and the load direction applied on the prosthesis.

• 한국광물학회:학술대회논문집
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• 한국광물학회.대한자원환경지질학회.대한광업진흥공사 2002년도 추계 공동 심포지엄 논문집: 국내 자원의 현황과 전망
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• pp.119-136
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• 2002

Contrasts in the style of the gold-silver mineralization in geologic and tectonic settings in Korea, together with radiometric age data, reflect the genetically different nature of hydrothermal activities, coinciding with the emplacement age and depth of Mesozoic magmatic activities. It represents a clear distinction between the plutonic settings of the Jurassic Daebo orogeny and the subvolcanic environments of the Cretaceous Bulgugsa igneous activities. During the Daebo igneous activities (c.a. 200-150 (?) Ma) coincident with orogenic time, gold mineralization took place between c.a. 195 and 135 (127 ?) Ma. The Jurassic Au deposits commonly show several characteristics; prominent association with pegmatites, low Ag/hu ratios in the ore-concentrating parts, massive vein morphology and a distinctively simple mineralogy including Fe-rich sphalerite, galena, chalcopyrite, arsenopyrite, Au-rich electrum, pyrrhotite and/or pyrite. During the Bulgugsa igneous activities $(110\~50Ma)$, the precious-metal deposits are generally characterized by such features as complex vein morphology, medium to high AE/AU ratios in the ore concentrates, and diversity of ore minerals including base-metal sulfides, pyrite, arsenopyrite, Ag-rich electrum and native silver nth Ag sulfides, Ag-Sb-As sulfosalts and Ag tellurides. Vein morphology, mineralogical, fluid inclusion and stable isotope results indicate the diverse genetic natures of hydrothermal systems in Korea. The Jurassic Au-dominant deposits (orogenic type) were formed at the relatively high temperature $(about\;300^{\circ}\;to\;450^{\circ}C)$ and deep-crustal level $(4.0{\pm}1.5\;kb)$ from the hydrothermal fluids containing more amounts of magmatic waters $(\delta\;^{18}O_{H2O}\;5\~10\%_{\circ})$. It can. It can be explained by the dominant ore-depositing mechanisms as $CO_2$ boiling and sulfidation, suggestive of hypo- to mesothermal environments. In contrast, the Cretaceous Au-dominant $(l13\~68\;Ma),\;Au-Ag \;(108\~47\;Ma)$ and Ag-dominant $(103\~45\;Ma)$ deposits, which correspond to volcanic-plutonic-related type, occurred at relatively low temperature $(about\;200^{\circ}\;to\;350^{\circ}C)$ and shallow-crustal level $(1.0\{pm}0.5\;kb)$ from the ore-forming fluids containing more amounts of less-evolved meteoric waters$(\delta\;^{18}O_{H2O}\;-10\~5\%_{\circ})$. These characteristics of the Cretaceous precious-metal deposits can be attributed to the complexities in the ore-precipitating mechanisms (mixing, boiling, cooling), suggestive of epi- to mesothermal environments. Therefore, the differences of the emplacement depth between the Daebo and the Bulgugsa igneous activities directly influence the unique temporal and spatial association of the deposit styles.

• 자원환경지질
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• 제32권5호
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• pp.445-454
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• 1999

산전 금-은 광상은 석영 반암내에 반암내에 발달된 열극을 충진한 석영+방해석의 열수맥광상이다. 광화작용은 단일 시기에 형성되었으며, 시간에 따라 다음과 같이, (2) 초기, 백석 석영+황철석+유비철석+심야연석; (2)중기, 백석-투명 석영+황화광물 (황철석, 섬아연석, 황동석, 방연석)+에렉트럼+휘은석; (3)후기, 방해석+황철석+자연은의 정출이 있었다. 금-은의 주요 광화기인 중기 광화유체의 온도와 NaCl 상당 염농도는 $210^{\circ}$~$250^{\circ}C$와 4~5wt.%이고, 황분압은 -14.0~-12.2atm 으로 금-은 침전은 천수의 혼입작용에 기인한 것으로 보인다. 산소 및 수소동위원소 분석에 의하면, 광화작용이 진행되에 따라 양자 모두 감소하는 경향을 갖는다. 이는 광화작용이 진행됨에 따라 천수의 혼입이 증가하기 때문으로 해석된다.

• 대한자원환경지질학회:학술대회논문집
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• 대한자원환경지질학회 2002년도 추계 공동 심포지엄 논문집
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• pp.119-136
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• 2002

Contrasts in the style of the gold-silver mineralization in geologic and tectonic settings in Korea, together with radiometric age data, reflect the genetically different nature of hydrothermal activities, coinciding with the emplacement age and depth of Mesozoic magmatic activities. It represents a clear distinction between the plutonic settings of the Jurassic Daebo orogeny and the subvolcanic environments of the Cretaceous Bulgugsa igneous activities. Dunng the Daebo igneous activities (c.a. 200～150 (\ulcorner) Ma) coincident with orogenic time, gold mineralization took place between c.a. 195 and 135 (127 \ulcorner) Ma. The Jurassic Au deposits commonly show several characteristics; prominent association with pegmatites, low Ag/Au ratios In the ore-concentrating parts, massive vein morphology and a distinctively simple mineralogy including Fe-rich sphalerite, galena, chalcopyrite, arsenopyrite, Au-rich electrum, pyrrhotite and/or pyrite. During the Bulgugsa igneous activities (110～50 Ma), the precious-metal deposits are generally characterized by such features as complex vein morphology, medium to high Ag/Au ratios in the ore concentrates, and diversity of ore minerals including base-metal sulfides, pyrite, arsenopyrite, Ag-rich eletrum and native silver with Ag sulfides, Ag-Sb-As sulfosalts and he tellurides. Vein morphology, mineralogical, fluid inclusion and stable isotope results indicate the diverse genetic natures of hydrothermal systems in Korea. The Jurassic Au-dominant deposits (orogenic type) were formed at the relatively high temperature (about 300$^{\circ}$ to 45$0^{\circ}C$) and deep-crustal level (4.0$\pm$1.5 kb) from the hydrothermal fluids containing more amounts of magmatic waters ($\delta$$^{18}$ $O_{H2O}$; 5～10$\textperthousand$). It can be explained by the dominant ore-depositing mechanisms as $CO_2$ boiling and sulfidation, suggestive of hypo- to mesothermal environments. In contrast, the Cretaceous Au-dominant (l13～68 Ma), Au-Ag (108～47 Ma) and AE-dominant (103～45 Ma) deposits, which correspond to volcanic-plutonic-related type, occurred at relatively low temperature (about 200$^{\circ}$ to 35$0^{\circ}C$) and shallow-crustal level (1.0$\pm$0.5 kb) from the ore-forming fluids containing more amounts of less-evolved meteonc waters ($\delta$$^{18}$ $O_{H2O}$;-10～5$\textperthousand$). These characteristics of the Cretaceous precious-metal deposits can be attributed to the complekities in the ore-precipitating mechanisms (mixing, boiling, cooling), suggestive of epi- to mesothermal environments. Therefore, the differences of the emplacement depth between the Daebo and the Bulgugsa igneous activities directly influence the unique temporal and spatial association of the deposit styles.les.

• 자원환경지질
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• 제29권2호
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• pp.139-150
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• 1996

The Yucheon Bi deposits at Cheongha, Gyeongsangbugdo, is of a middle Paleogene (49 Ma) vein type, and is hosted in sandstone and shale of Banyawal formation in Cretaceous age. Based on mineral paragenesis, vein structure and mineral assemblages, two minera1ization stages were distinguished. The stage I consists of quartz with small amount of chlorite, pyrite, epidote, hal1oysite, vermiculite, serpentine and rutile associated with sericitization. The stage II is characterized by Bi minera1ization such as bismuthinite, Bi-Cu-Pb-S mineral, tetradymite, native gold, pyrite, pyrrhotite, arsenopyrite, wolframite, rutile, hematite, sphalerite, chalcopyrite, galena with alteration of sericite, chlorite, K-feldspar, albite and epidote. Fluid inclusion data indicate that fluid temperature and NaCl equivalent wt.% salinity range from 431 to $150^{\circ}C$ and from 19.2 to 0.18wt.% in the stage II. Evidence of boiling during the base-metal minera1ization indicates pressures 241 to 260 bars. Sulfur fugacity($-log\;f_{S2}$) deduced by mineral assemblages and compositions ranges from 5.1 to 5.7atm in early stage, from > 8.4 atm in middle stage and from 13.5 to 19.3 atm in late stage. It suggests that complex histories of progressive coo1ing, dilution and boiling were occurred by the mixing of the fluids. The ${\delta}^{34}S$, ${\delta}^{18}O$ and ${\delta}D$ data range from 2.5 to 3.9%, -0.5 to -4.1% and -29.7 to -47%, respectively. It indicated that hydrothermal fluids may be magmatic origin with boiling and mixing of meteoric water increasing paragenetic time.

• 자원환경지질
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• 제22권3호
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• pp.193-205
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• 1989

Regional geology of Chungil mine is composed of Cretaceous biotite granite. Chungil ore deposits are fissure filled quartz veins which developed in Cretaceous biotite granites. Mineralogic and fluid inclusion studies were undertaken to illuminate the origin of the ore deposits. Data gathered from occurrences of ore deposits and mineral paragenesis reveals that there were two major mineralization stage. The first stage is sulfides-quartz stage. The constituents of ore minerals are chalcopyrite, sphalerite, pyrrhotite with minor amount of galena, native Au, Ag, pyrite. The second stage is gangue mineral stage. Gangue minerals are quartz, fluorite and calcite. Homogenization temperature of fluid inclusions in quartz of the first and the second stage ranges from $212^{\circ}C$ to $336^{\circ}C$ and from $154^{\circ}C$ to $355^{\circ}C$ respectively. Homogenization temperature in fluorite and calcite of the second stage ranges from $127^{\circ}C$ to $252^{\circ}C$ and from $129^{\circ}C$ to $158^{\circ}C$ but these data require positive pressure corrections. Fluid inclusions in quartz of the Bongmyeong mine, Jangja the first mine and the second mine show range of homogenization temperature from $178^{\circ}C$ to $330^{\circ}C$, from $185^{\circ}C$ to $354^{\circ}C$ and from $206^{\circ}C$ to 336 respectively. The comparison of the fluid inclusion data, mineralogical component and vein attitude of the three mines with that of Chungil mine indicates that the origin of the deposits above mentioned is elucidated to be formed under similar environment. The compositions of the sphalerite in the first stage range from 16.05 mol.% FeS to 20.36 mol.% FeS.