• Proceedings of the KSEEG Conference
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• 2005.04a
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• pp.320-323
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• 2005

• Proceedings of the KSEEG Conference
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• 1999.04a
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• pp.345-345
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• 1999

• Proceedings of the KSEEG Conference
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• 1999.04a
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• pp.194-194
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• 1999

• Economic and Environmental Geology
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• v.55 no.5
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• pp.541-550
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• 2022

A pre-existing landform is created by weathering and erosion along the bedrock fault and the weak zone. A neotectonic landform is formed by neotectonic movements such as earthquakes, volcanoes, and Quaternary faults. It is difficult to clearly distinguish the landform in the actual field because the influence of the tectonic activity in the Korean Peninsula is relatively small, and the magnitude of surface processes (e.g., erosion and weathering) is intense. Thus, to better understand the impact of tectonic activity and distinguish between pre-existing landforms and neotectonic landforms, it is necessary to understand the development process of pre-existing landforms depending on the bedrock characteristics. This study used a two-dimensional numerical landscape evolution model (LEM) to study the spatio-temporal development of landscape according to the different erodibility under the same factors of climate and the uplift rate. We used hill-slope indices (i.e., relief, mean elevation, and slope) and channels (i.e., longitudinal profile, normalized channel steepness index, and stream order) to distinguish the difference according to different bedrocks. As a result of the analysis, the terrain with high erosion potential shows low mean elevation, gentle slope, low stream order, and channel steepness index. However, the value of the landscape with low erosion potential differs from that with high erodibility. In addition, a knickpoint came out at the boundary of the bedrock. When researching the actual topography, the location around the border of difference in bedrock has only been considered a pre-existing factor. This study suggested that differences in bedrock and various topographic indices should be comprehensively considered to classify pre-existing and active tectonic topography.

• Proceedings of the KSEEG Conference
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• 2003.04a
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• pp.302-305
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• 2003

진안-장수지역 (이하 본 역)은 한반도를 구성하는 중요한 지괴인 영남육괴 지리산지역의 북서부와 옥천지향사대의 동남연변부에 위치한 곳으로 두 지괴의 경계면을 따라 압쇄작용으로 형성된 순창전단대가 분포하며 지질시대와 암석학적 특징이 상이한 여러 화성암체가 나타난다. 본 연구지역의 지질은 지리산 편마암복합체를 기반으로 선캠브리아기의 변성퇴적암류, 신암리섬암, 장수화강편마암, 선각산화강편마암 그리고 쥬라기의 대성리엽리상화강암, 순창엽리상화강암과 남원화강암으로 구성된다. (중략)

• Proceedings of the KSEEG Conference
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• 2007.04a
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• pp.421-424
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• 2007

• Proceedings of the Korean Environmental Sciences Society Conference
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• 2004.05a
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• pp.58-60
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• 2004

• Proceedings of the Korea Water Resources Association Conference
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• 2023.05a
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• pp.153-153
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• 2023

골프장 건축 시 하부지반 구축을 위해 사용하는 잔석의 산화로 인해 중금속 용출이 발생할 수 있다. 용출된 중금속으로 인근 농업지역이 오염될 경우 인간의 식생활에 직접적인 영향을 미쳐 인체건강에 악영향을 끼칠 수 있다. 특히, 망간의 경우 식품을 통해 과다섭취할 경우 정신착란, 운동실조 등 다양한 신경학적 문제를 발생시키기 때문에 망간 오염에 대한 조사 및 관리는 필수적이다. 따라서, 본 연구는 최근 골프장이 건설된 부산시 일광 회룡리 일대 농업지역에서 망간 오염 평가를 위해 지표수, 퇴적물, 벼 작물을 채취하여 망간 농도 분석을 수행하였다. 골프장 유출조부터 시작되는 관개수로에서 지표수와 퇴적물 시료를 약 20 m 간격으로 채취하였으며, 관개수로의 구조에 따라 논을 4개의 구역(Area 1 - 4)으로 구분하여 논 토양과 벼 작물을 채취하였다. 벼 작물의 경우 뿌리, 줄기, 곡물 부분으로 나누어 채취하였으며, 퇴적물과 논 토양은 시료 내 존재하는 망간의 형태를 확인하기 위해 연속추출법을 통해 분석하였다. 분석 결과 지표수의 망간 농도는 골프장 유출조에서 하류로 갈수록 감소하는 경향을 보였으며, 하류에서의 망간농도는 상류에 비해 최대 88% 감소하였다. 퇴적물의 망간 농도는 논으로 연결되는 지점에서 20,000 mg/kg 이상의 높은 농도를 보였으며, 농업이 진행 중인 3, 5, 7월은 최대 약 25,000 mg/kg의 농도를 보였으나, 농업이 끝난 9월에는 최대 약 3,500 mg/kg으로 상대적으로 낮은 농도를 보였다. 논 토양의 망간 농도는 관개수로와 첫 번째로 연결되는 Area 1에서 1,600 mg/kg으로 측정되었으며, 이는 EPA에서 권고한 논 토양 망간 기준 1,000 mg/kg을 초과하는 농도로 확인되었다. 또한, 식물이 사용할 수 없는Residual 형태의 망간 농도는 변화가 없었으나, 식물이 사용 가능한 Acid soluble, Reducible, Oxidizable 형태의 망간 농도는 추수기 이후 80% 이상 감소하였다. 벼 작물의 곡물 망간 농도는100 - 200 mg/kg으로 USDA에서 발표한 쌀 곡물 망간 농도의 평균인 5 mg/kg보다 약 20배 이상 높게 검출되었다. 본 연구 결과를 통해 골프장 유출조로부터 발생하는 망간오염을 식별하고 주변 농업지역에 미치는 영향을 확인할 수 있었으며, 추후 골프장 운영으로 인한 환경오염에 대한 관리가 필요할 것으로 생각된다.

• Proceedings of the Korean Environmental Sciences Society Conference
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• 2020.10a
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• pp.207-207
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• 2020

• The Journal of the Petrological Society of Korea
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• v.21 no.2
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• pp.129-150
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• 2012

The tectonic evolution of the Central Ogcheon Belt has been newly analyzed in this paper from the detailed geological maps by lithofacies classification, the development processes of geological structures, microstructures, and the time-relationship between deformation and metamorphism in the Ogcheon, Cheongsan, Mungyeong Buunnyeong, Busan areas, Korea and the fossil and radiometric age data of the Ogcheon Supergroup(OSG). The 1st tectonic phase($D^*$) is marked by the rifting of the original Gyeonggi Massif into North Gyeonggi Massif(present Gyeonggi Massif) and South Gyeonggi Massif (Bakdallyeong and Busan gneiss complexes). The Joseon Supergroup(JSG) and the lower unit(quartzose psammitic, pelitic, calcareous and basic rocks) of OSG were deposited in the Ogcheon rift basin during Early Paleozoic time, and the Pyeongan Supergroup(PSG) and its upper unit(conglomerate and pelitic rocks and acidic rocks) appeared in Late Paleozoic time. The 2nd tectonic phase(Ogcheon-Cheongsan phase/Songnim orogeny: D1), which occurred during Late Permian-Middle Triassic age, is characterized by the closing of Ogcheon rift basin(= the coupling of the North and South Gyeonggi Massifs) in the earlier phase(Ogcheon subphase: D1a), and by the coupling of South China block(Gyeonggi Massif and Ogcheon Zone) and North China block(Yeongnam Massif and Taebaksan Zone) in the later phase(Cheongsan subphase: D1b). At the earlier stage of D1a occurred the M1 medium-pressure type metamorphism of OSG related to the growth of coarse biotites, garnets, staurolites. At its later stage, the medium-pressure type metamorphic rocks were exhumed as some nappes with SE-vergence, and the giant-scale sheath fold, regional foliation, stretching lineation were formed in the OSG. At the D1b subphase which occurs under (N)NE-(S)SW compression, the thrusts with NNE- or/and SSW-vergence were formed in the front and rear parts of couple, and the NNE-trending Cheongsan shear zone of dextral strike-slip and the NNE-trending upright folds of the JSG and PSG were also formed in its flank part, and Daedong basin was built in Korean Peninsula. After that, Daedong Group(DG) of the Late Triassic-Early Jurassic was deposited. The 3rd tectonic phase(Honam phase/Daebo orogeny: D2) occurred by the transpression tectonics of NNE-trending Honam dextral strike-slip shearing in Early~Late Jurassic time, and formed the asymmetric crenulated fold in the OSG and the NNE-trending recumbent folds in the JSG and PSG and the thrust faults with ESE-vergence in which pre-Late Triassic Supergroups override DG. The M2 contact metamorphism of andalusite-sillimanite type by the intrusion of Daebo granitoids occurred at the D2 intertectonic phase of Middle Jurassic age. The 4th tectonic phase(Cheongmari phase: D3) occurred under the N-S compression at Early Cretaceous time, and formed the pull-apart Cretaceous sedimentary basins accompanying the NNE-trending sinistral strike-slip shearing. The M3 retrograde metamorphism of OSG associated with the crystallization of chlorite porphyroblasts mainly occurred after the D2. After the D3, the sinistral displacement(Geumgang phase: D4) occurred along the Geumgang fault accompanied with the giant-scale Geumgang drag fold with its parasitic kink folds in the Ogcheon area. These folds are intruded by acidic dykes of Late Cretaceous age.