本論文研究台灣中南部褶皺逆衝斷層帶的區域性地質構造及活動斷層。主要的研究 方法包括整合震測資料、井下地質資料、及野外資料於層序地層分析、構造平衡剖面分 析以及構造剖面恢復分析等，此三地區包括台中車籠埔斷層附近地區，北港高區東緣和 台南高雄陸海交界及平原地區。以瞭解各不同地質構造區域的構造特徵及構造發育。 在車籠埔斷層地區，共建立數條東西向的地質構造平衡剖面及溯源剖面，並對於此 區造山變形前緣進行地質構造分析。由台灣中部的1999集集大地震破裂－車籠埔斷層的 鉆井岩心之組構分析，顯示車籠埔斷層剪切帶之變形組構特徵，主剪切帶的位置符合於 岩性及層序轉換帶之力學界限。由卓蘭層頂部為恢復基準之地質構造溯源剖面顯示車籠 埔斷層自蓬萊運動以來約有13.7公里之位移量。 在北港高區東緣及附近地區之研究，北港高區的古地形幾何形貌之不規則性（ irregularity）以及南北方向構造之不連續，為主要控制其附近各區塊地體構造發育之重要 因素。北港高區是以最高之梅山古脊為基準，分別往南北兩側逐漸傾沒，呈北陡西緩。 東西走向之梅山古脊北以草嶺斷層系統為界，南以梅山斷層系統為界。薄皮褶皺逆衝作 用受北港脊之阻擋，無法向西延伸而形成出露低角度之九芎坑逆衝斷層。草嶺斷層系統 為北港高區北緣的重要反轉斷層，此反轉斷層之主要特徵為斷層淺部為逆斷層而深部仍 維持正斷層型態。車籠埔斷層及彰化斷層淺層滑移至草嶺斷層附近消失。梅山斷層為一 重要之高角度反轉斷層，與平原區之Ｂ斷層組成北港高區南緣之重要邊界斷層。由震測 資料之斷層對比，梅山斷層與Ｂ斷層並不直接相連，而是以接力斜坡（relay ramp）之方 式形成兩者間之構造轉換帶。梅山斷層之平面分佈以盲斷層之形式延伸至民雄附近，由 恢復地層之分析，顯示梅山區塊是一完全反轉之中新世地塹盆地，此盆地形成於南莊期 之前。 在台南高雄平原地區及陸海交界處，左鎮斷層為台灣西南部麓山區之重要撕裂斷層 （tear fault），在此斷層南側之那菝林背斜、新化斷層等構造單元，以反向逆衝斷層（ backthrust）之形態出現，並與龍船構造形成重要之構造三角帶（triangle zone）系統；在 陸海交界之二仁溪口附近之淺海地區仍以反向之斷層轉折褶皺為主。此區之前陸盆地沈 積，以厚層且較鬆軟之古亭坑泥岩為主，提供中深度地下構造三角帶之發育。 在台灣西南地區造山變形前緣帶，以反轉構造或低緩的前緣隱伏背斜為主要特徵， 此研究證實變形前緣之逆衝作用已由麓山區與平原區之交會處，往西延伸至10〜15公里 處形成一南北狹長的地帶，此帶並向西南延伸至台南及高雄陸海交界地區。 This study will be focused on the analysis of regional mesoscopic structural framework as well as the analysis of active faults in central and southern Taiwan. Three areas were chosen for structure analysis in order to decipher their geometrical characteristics and sequential developments by an integrated interpretation using seismic , well log, and field-geology data. Three areas include (1) in the vicinity of the Chelungpu Fault in the Taichung area, (2) east margins of the Peikang High, and (3) south of the Peikang High in Tainan and Kaohsiung areas. Several balanced and palinspatic-restored sections are constrained by seismic data. Analysis on drill cores recovered from the 1999 Chi-Chi earthquake rupture (i.e, the Chelungpu Fault) in central Taiwan, shows that the Chelungpu Fault consists of several major shear zones and their mechanical boundaries coincide with the lithological boundaries of stratigraphic sequence. According to the analysis on palinspatic sections using top of Cholan Formation as a datum plane, it shows that there is a displacement along the fault plane of about 13.7 kilometers, at least, for the Chelungpu Fault. At the eastern edge of the Peikang High, geometrical irregularity of the basement high and the discontinuity of the tectonic trend in the north-south direction are the most important factors that control the geological development for each compartment. The Peikang High is plunged both southward and northward to form the Meishan Ridge. The east-west striking Meishan Ridge is bounded by the Tsaoling Fault system to the north and Meishan Fault to the south. The thin skin thrusting was retarded by the ridge 129 and resulted in the emergence of Chiuchungkeng Fault to form a low angle thrust. The Tsoling Fault system is an important inverted fault. This inverted fault shows reverse features in shallow part while in deeper part it remains normal fault features. Data revealed that the southern part of Chelungpu Fault nappe disappears near the Tsoling Fault. The Meishan Fault is also an important inverted fault. The B Fault and the Meishan Fault are composed of one boundary fault in the southern side of Peikang High. The Meishan fault is not directly connected to the B Fault while a relay ramp is verified as a transitional accommodation zone. The Meishan Fault is interpreted to have extended to the Minshung tonship. The Chaiyi graben is determined as a thoroughly inverted graben by the restoration method. The Chaiyi graben is judged to have occurred prior to the deposition of the Nanchuang Formation. On the coastal plain and transitional zone between offshore and land in Kaohsiung and Tainan, the Tsochen Fault is an important NW-SE trending tear fault in southwestern Taiwan. Napalin Anticline and Hsinhua Fault located at the southern side of Tsochen Fault appear as backthrusts and composed as the triangle zone near the Longchuan structure. Nearshore area near Erzenchi is characterized by fault-bend fold in a reverse direction. The foreland deposits of the Gutinkeng Formation is dominated by thick, low density mudstone which is very suitable for the development of triangle zone in the middle and deep part of subsurface. If the deformation front is defined as the appearance of buried frontal low angle thrust or the inverted faults, this study has proved that the position of deformation front has been extended westward some 10-15 kilometers from the junction between foothill and coastal plain, and the zone of front also extended to the offshore of Kaoshung and Tainan areas.
