研究生: |
劉興智 Liu, Hsing-Chih |
---|---|
論文名稱: |
臺灣中部集集攔河堰附近應力演化史之初探 Preliminary Study of Stress Evolution near the Chi-Chi Dam, Central Taiwan |
指導教授: |
葉恩肇
Yeh, En-Chao |
口試委員: |
葉恩肇
Yeh, En-Chao 李建成 Lee, Jian-Cheng 陳柔妃 Chen, Rou-Fei |
口試日期: | 2021/06/28 |
學位類別: |
碩士 Master |
系所名稱: |
地球科學系 Department of Earth Sciences |
論文出版年: | 2021 |
畢業學年度: | 109 |
語文別: | 中文 |
論文頁數: | 95 |
中文關鍵詞: | 斷層滑動資料 、應力演化 、層面校正 、初鄉斷層 |
英文關鍵詞: | fault slip data, stress evolution, bedding correction, ChuHsiang fault |
研究方法: | 田野調查法 |
DOI URL: | http://doi.org/10.6345/NTNU202101253 |
論文種類: | 學術論文 |
相關次數: | 點閱:112 下載:4 |
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災害性地震發生時,不僅會造成人員傷亡及財物損失,也會因為斷層的活動讓地形地貌改變。1999年的集集地震造成了近100公里的地表破裂,此次地震的主破裂面為車籠埔斷層。GPS資料顯示,車籠埔斷層上盤在集集地震的事件中產生了抬升以及錯動。此次抬升事件切穿了濁水溪,使侵蝕基準面相對向下,形成向源侵蝕,而2000年集集攔河堰的啟用,降低濁水溪下游沉積物的堆積速率,由於自然與人為的作用下,促使濁水溪自名竹大橋至集集攔河堰之間的岩層出露。由車籠埔斷層向東,此段露頭大多為單斜構造,且有少部分的淺部變形,直至集集攔河堰以西約1公里處,則出現了東北走向的初鄉斷層與其上盤向北傾沒的頂溪州背斜。這樣的淺部地表變形可能是地震所造成的岩層變形。本研究將利用斷層擦痕與古應力的分析,瞭解初鄉斷層上盤的頂溪州背斜附近的應力場特徵、隨地塊掘升的應力變化,以及大地應力的構造意義,最終建構研究區的構造演化史。
研究結果顯示本研究區內應力場先後順序為: stage 1 為正斷層應力場;stage 2 為走滑—逆斷層應力場,以西北西—東南東至西北—東南為擠壓方向;stage 3為走滑—逆斷層應力場,以北北西—南南東至北北東—南南西為擠壓方向;stage 4 為走滑—逆斷層應力場,西北—東南擠壓方向及西北—東南及東北—西南拉張方向。其中又可細分出 Substage,stage 2a 及 stage 2b 為同一應力場,但作用於兩種不同構造型態,分別為水平層面及正立褶皺;同理,stage 3a 及 stage 3b 為同一應力場,但作用於兩種不同構造型態,分別為正立褶皺及傾倒褶皺。
彙整上述結果,本研究探討各期應力場的地質意義:第1期為正斷層應力場,由地層年代與沉積環境推測,此時研究區域仍位於前緣斷層以西的前陸盆地中。第 2a 時期,地層位態仍為水平狀態,但應力場轉變為東-西擠壓,由於西部麓山帶的斷層是由東向西漸漸發展,推測 2a 的擠壓應力場可能是受蓬萊造山運動所引起。2b 時期,依然為東-西擠壓應力場,但地層已傾斜,推斷此時期初鄉斷層已經形成。3a 時期,應力場轉變為南-北擠壓應力場,由應力場與初鄉斷層走向關係判斷,此時初鄉斷層為具逆移分量的左移斷層,層面狀態為正立褶皺。3b時期,應力場依然為南-北擠壓應力場,層面狀態為傾倒褶皺,頂溪州背斜向北傾沒可能是南邊的鹿寮斷層向北推擠,使初鄉斷層與鹿寮斷層間形成東—西走向的褶皺構造。第 4 期應力場轉為東—西向擠壓,推測初鄉斷層運動方式為逆移斷層,但第4 期不單單只有逆斷層以及走向滑移應力場,還包括了局部正斷層應力場,有此正斷層應力場結果的露頭位置皆靠近頂溪州背斜軸部,推可能是縱彎褶皺外圍拉張所造成的破裂。
When a catastrophic earthquake occurs, it will not only cause casualties and property losses, but also change the terrain due to the activity of the fault. The Chi-Chi earthquake in 1999 caused nearly 100 kilometers of surface rupture. The main rupture surface of this earthquake was the Chelongpu fault. GPS data shows that the hanging wall of the Chelongpu fault was uplifted and dislocated during the Chi-Chi earthquake. This uplifting event cut through the Zhuoshui River, causing the erosion base level to be relatively downward, forming source erosion. The opening of the Chi-Chi Dam in 2000 reduced the accumulation rate of sediments in the lower reaches of the Zhuoshui River. Under the action, the outcrop between Ming-Zhu Bridge and Chi-Chi Dam were exposed. From the Chelongpu fault to the east, the outcrop in this section is a homocline structure, until about 1 km west of the Chi-Chi Dam, a NE-trending ChuHsiang fault and its hanging wall plunging northward Dingxizhou anticline appeared. Such shallow surface deformation may be caused by the deformation of the formation caused by the earthquake. This research will focus on the Dingxizhou anticline on the hanging wall of the ChuHsiang fault, and discuss the evolutionary relationship between the Dingxizhou anticline and the ChuHsiang fault. This thesis uses the analysis of fault slip data and paleostress to understand the stress field characteristics of the Dingxizhou anticline on the hanging wall of the ChuHsiang fault, the stress changes with the excavation of the block, and the tectonic significance of the geostress, and finally construct the study area History of tectonic evolution.
The research results show that the sequence of the stress field in the study area is: stage 1 is the normal fault stress field; stage 2 is the strike-slip-reverse fault stress field, with the compression direction from NW-SE east to NW-SE; stage 3 is strike-slip —reverse fault stress field, the compression direction is NW—SE to NNE—SSW; stage 4 is the strike-slip—reverse fault stress field, the NW—SE compression direction and the NW—SE and NE—SW tension direction. Among them, Substage can be subdivided. stage 2a and stage 2b are the same stress field, but act on two different structural types, namely the horizontal plane and the upright fold. Similarly, stage 3a and stage 3b are the same stress field, but Acting on two different structural types, namely upright folds and plunging folds.
Combining the above results, this study explores the geological significance of the stress fields in each period: The first period is the normal fault stress field, and from the stratigraphic age and depositional environment, it is speculated that the study area is still located in the foreland basin west of the front fault. In period 2a, the stratum is still in a horizontal state, but the stress field changes to east-west compression. Because the faults in the western piedmont belt gradually develop from east to west, it is inferred that the compression stress field in 2a may be caused by the Penglai orogenic movement. cause. During the 2b period, there was still an east-west compressive stress field, but the stratum was tilted. It is inferred that the ChuHsiang fault has been formed during this period. During the 3a period, the stress field changed to a north-south compression stress field. Judging from the relationship between the stress field and the ChuHsiang fault strike, the ChuHsiang fault is a left-moving fault with a reverse shift component, and the plane state is an upright fold. During the 3b period, the stress field was still a north-south compression stress field, and the surface state was a dumped fold. The Dingxizhou anticline tilted to the north. It may be that the Luliao fault in the south pushed northward, making the ChuHsiang fault and the Luliao fault. An east-west trending fold structure is formed between. The fourth phase of the stress field is converted to east-west compression. It is inferred that the ChuHsiang fault movement mode is a reverse fault. However, the fourth phase includes not only the reverse fault and the strike slip stress field, but also the local normal fault stress field. The outcrop positions of the normal fault stress field are all close to the axis of the Dingxizhou anticline, which may be the result of the rupture caused by the extension of the periphery of the longitudinal bending fold.
大江二郎(1938)台中州國姓油田調查報告。台灣總督府殖產局,共25頁。
中國石油公司臺探總處(1986)嘉義地質圖,比例尺十萬分之一。中國石油公司出版。
安藤昌三郎(1930)台灣苗栗油田之地質及構造。地質學雜誌,第 37卷,第 447 期,第 799-803 頁。
何春蓀(1986)臺灣地質概論-臺灣地質圖說明書。臺北:經濟部,1986,共117 頁,臺北市。
李元希、盧詩丁、石同生、饒瑞鈞(2003)集集地震南段地表破裂的變形機制—逆斷層-走向滑移斷層-走向滑移斷層板塊(TFF)三接點模式。經濟部中央地質調查所彙刊,第15期,第87-101頁。
李錫堤(1986)大地應力分析與弧陸碰撞對於臺灣北部古應力場變遷影響。國立臺灣大學地質學研究所,臺北市。
林啟文、盧詩丁、黃文正、石同生、張徽正(2000)臺灣中部濁水溪以南地區的集集地震斷層與構造分析。經濟部中央地質調查所特刊,第十二號,第89-112頁。
林朝棨(1933)關於臺灣產哺乳類化石的產出狀態。臺灣地學記事,第4卷,第 5~6 期,第 39~41 頁。
邱子軒(2018)台灣中部麓山帶晚期上新世至早期更新世前陸盆地之古沉積環境研究。國立中央大學地球科學系研究所碩士論文,桃園市。
張徽正、林啟文、陳勉銘、盧詩丁(1998)台灣活動斷層概論,五十萬分之一臺灣活動斷層分布圖說明書。經濟部中央地質調查所特刊第10號,共103頁。
陳于高、徐澔德、賴光胤、王昱、莊昀叡、陳文山(2002)階地變形和活動構造:以南投東埔蚋溪為例。中國地質學會九十一年年會論文集,第 12-14 頁。
陳正旺(2005)車籠埔斷層周圍岩石力學特性之初探。臺灣大學土木工程研究所碩士論文,台北。
陳冠豪(2020) 由縮減應力張量計算應力規模之可行性分析。
陳華玟、陳勉銘及石同生(2004)南投圖幅及說明書,五萬分之一臺灣地質圖。第三十一號。經濟部中央地質調查所出版。
鳥居敬造(1935)東勢圖幅及說明書(比例尺五萬分之一)。臺灣總督府殖產局出版第 732 號,共 26 頁。
游能悌、鄧屬予(1996)臺灣北部中上中新統的岩相與沉積循環。地質,15卷,2期,第29-60頁。
黃鑑水、張憲卿、劉桓吉(1994)台灣南部觸口斷層地質調查與探勘。經濟部中央地質調查所彙刊,第9號,第29-50頁。
黃鑑水、謝凱旋、陳勉銘(2000)五萬分之一台灣地質圖說明書,埔里地質圖說明書。經濟部中央地質調查所。
經濟部中央地質調查所(1999)大尖山斷層沿線地表破裂分布圖,比例尺二萬五千分之一。經濟部中央地質調查所出版。
經濟部中央地質調查所(2000)九二一地震地質調查報告。
劉桓吉、李錦發(1998)雲林圖幅及說明書,五萬分之一臺灣地質圖。第三十八號。經濟部中央地質調查所出版。
黎明工程顧問股份有限公司((2001)) 集集攔河堰初次使用安全評估報告。
謝凱旋、黃敦友(2003)台灣第三系的地層層序。台灣礦業,第 55卷,第 4 期,第 17-32 頁。
Anderson, E. M. (1951). The Dynamics of Faulting, Etc. (Revised.). Edinburgh, London.
Angelier, J. (1994). Fault Slip Analysis and paleostress reconstruction. In P. L.
Angelier, J., Barrier, E., and Chu, H. T. (1986). Plate collision and paleostress trajectories in a fold-thrust belt: The foothills of Taiwan. Tectonophysics, 125(1-3), 161-178. DOI: http://doi.org/10.1016/0040-1951(86)90012-0
Bott, M. H. P. (1959). The mechanics of oblique slip faulting. Geol.Mag.,96, 109-11.
Brace, W. F. and Bombolakis, E. G.(1963) A Note on Brittle Crack in Compression. Journal of Geophysical Research. volume68, issue12,p3709-3713.
Chen, W.- S., Ridgway, K. D., Horng, C. -S., Chen, Y.- G., Shea, K.- S., and Yeh, M.- G. (2001). Stratigraphic architecture, magnetostratigraphy, and incisedvalley systems of Pliocene-Pleistocene collisional marine foreland basin of Taiwan. Geological Society of America Bulletin, 113, 1249–71.
Covey, M. (1984). Lithofacies analysis and basin reconstruction, PlioPleistocene western Taiwan foredeep. Petroleum Geology of Taiwan, 20, 53-83.
Gibbard, P.L., and Head, M.J. (2009) The definition of the Quaternary System/Era and the Pleistocene Series/Epoch. Quaternaire, 20/2, 125-133.
Horii. H and Nasser, N.(1986) Brittle Failure in Compression: Splitting, Faulting and Brittle –Ductile Transition. Philosophical Transactions of The Royal Society A Mathematical Physical and Engineering Sciences. A 319,337-374.
Lajtai, E. Z.(1971) A theoretical and experimental evaluation of the Griffith theory of brittle fractures. Tectonophysics11, 129-156.
Lin, A. T., and Watts, A. B. (2002). Origin of the West Taiwan Basin by orogenic loading and flexure of a rifted continental margin. Journal of Geophysical Research, 107 (B9), 2185.
Lin, A. T., Watts A. B., and Hesselbo, S. P. (2003). Cenozoic stratigraphy and subsidence history of the South China Sea margin in the Taiwan region. Basin Research, 15, 453-478.
Ma, K.- F., Lee, C.- T., and Tsai, Y.- B. (1999). The Chi-Chi, Taiwan earthquake: Large surface displacements on an inland thrust fault. EOS, Transactions, American Geophysical Union, 80, 605.
Nagel, S., Castelltort, S., Wetzel, A., Willett, S. D., Mouthereau, F., and Lin, A. T. (2013). Sedimentology and foreland basin paleogeography during Taiwan arc continent collision. Journal of Asian Earth Sciences, 62, 180-204.
Pollard, D.D. and Segall, P.(1987) Theoretical displacements and stresses near fractures in rock: with applications to faults, joints, veins, dikes, and solution surfaces. In, B.K. Atkinson (Ed.), Fracture Mechanics of Rock. Academic Press, London, p. 277-349.
Richard H. Sibson, Francois Robert, K. Howard Poulsen(1988) High-angle reverse faults, fluid-pressure cycling, and mesothermal gold-quartz deposits. Geology, no. 6.
Seno, T. (1977). The instantaneous rotation vector of the Philippine Sea plate relative to
Simoes, M., Avouac, J. P. and Chen, Y. G. (2007). Slip rates on the Chelungpu and Chushiang thrust faults inferred from a deformed strath terrace along the Dungpuna river, west central Taiwan, Journal of Geophysical Research: Solid Earth, Vol. 112(B3).
Suppe, J. (1980) Imbricated structure of western foothills belt, southcentral Taiwan. Petrol. Geol. Taiwan, 17, 1–16.
Suppe, J. (1983)Geometry and kinematics of fault-bend folding. Am. J. Sci. 283, 684-721.
Teng, L. S. (1987). Stratigraphic records of the late Cenozoic Penglai Orogeny of Taiwan. Acta Geologica Taiwanica, 25, 205-–224.
Teng, L. S. (1990). Geotectonic evolution of late Cenozoic arc-continent collision in tTaiwan. Tectonophysics, 183(1-4), 57-76.
Teng, L. S., Wang, Y., Tang, C. -H., Huang, C.- Y., Huang, T. -C., Yu, M. -S., and Ke, A. (1991) Tectonic aspects of the Paleogene depositional basin of northern Taiwan. Proceedings of the Geological Society of China, 34, 313-336.
the Eurasian plate. Tectonophysics, 42(2-4), 209–226.
Wang, C.- Y., Li, C.- L., Su, F.- C., Leu, M.- T., Wu, M.- S., Lai, S.- H., and Chern, C.- C.(2002). Structural mMapping of the 1999 Chi-Chi Earthquake Ffault, Taiwan by Sseismic Rreflection Mmethods. Terrestrial, Atmospheric Oceanic Sciences, Vol. 13(3), 16.
Yang, K. M., Huang, S. T., Wu, J. o. C., Ting, H. H., Mei, W. W., Lee, M., Hsu, H. H. and Lee, C. J. (2007). 3D geometry of the Chelungpu thrust system in central Taiwan: Its implications for active tectonics", Terrestrial, Atmospheric Oceanic Sciences, Vol. 18(2), pp. 143.
Yu, H.-S., and Chou, Y.-W. (2001). Characteristics and developmentof the flexural forebulge and basal unconformity of western Taiwan foreland basin. Tectonophysics, 333, 277-291.
Yu, N. T., and Teng, S. L. (1996). Facies characteristics and depositional cycles of middle and upper Miocene strata of the Western Foothills, northern Taiwan. Ti-Chih, 15, 29–-60.
Yu, S. B., Chen, H. Y., & Kuo, L. C. (1997). Velocity field of GPS stations in the Taiwan area. Tectonophysics, 274(1), 41–59.
Yu, S.- B., Kuo, L.- C., Hsu, Y.- J., Su, H.- H., Liu, C.- C., Hou, C.- S., Lee, J.- F., Lai, T.- C., Liu, C.-C., and Liu, C.-L. (2001). Preseismic deformation and coseismic displacements associated with the 1999 Chi-Chi, Taiwan, earthquake", Bulletin of the Seismological Society of America, Vol. 91(5), pp. 995-1012.
Yue, L.- F., and J. Suppe (2014), Regional pore-fluid pressures in the active western Taiwan thrust belt: A test of the classic hubbert–rubey fault-weakening hypothesis, Journal of Structural Geology, 69, 493–-518.
Žalohar, J., and Vrabec, M. (2007). Paleostress analysis of heterogeneous fault-slip data:The Gauss method. Journal of Structural Geology, 29(11), 1798–-1810. DOI: http://doi.org/10.1016/j.jsg.2007.06.009