博碩士論文 105624017 詳細資訊



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姓名 洪世明(Shi-Ming Hong)  查詢紙本館藏   畢業系所 應用地質研究所
論文名稱 利用孔隙率-有效應力關係曲線評估海岸山脈南段弧前盆地之地層侵蝕量
(Using porosity-effective stress relationship curve to evaluate the erosion amount of the fore-arc basin in the southern part of Coastal Range)
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摘要(中) 地層侵蝕量對於盆地演化歷史推測、造山帶演化推估、油氣成熟與遷徙的過程都是一個重要的參數。地層侵蝕量估計多使用地球物理、地球化學、地層對比等方法進行，但在海岸山脈弧前盆地(泰源與樂合盆地)，因(1)地物井測與震測資料欠缺；(2)沉積物來源主要來自中央山脈，其帶來的高變質度沉積物嚴重干擾地球化學指標之測量；(3)地層受到大範圍的抬升與侵蝕，地層對比不易等三個限制，造成單一方法推估地層侵蝕量不確定性高。本研究於泰源盆地之馬達吉達溪剖面採集五個砂岩樣本、於樂合盆地之樂合溪剖面採集三個砂岩樣本，進行孔隙率-有效應力分析得出預壓密應力，並藉此計算地層侵蝕量。孔隙率-有效應力分析的原理基於顆粒沉積物在力學壓密過程中孔隙率的變化，若樣本受化學壓密則視為無效樣本，為增加成果的可信度，本研究將孔隙率實驗之砂岩樣本製作薄片進行觀察、並引用前人在此二研究區之鏡煤素反射率資料進行古地溫分析，確立孔隙率實驗之砂岩樣本的壓密型態。孔隙率-有效應力分析所得之地層侵蝕量計算成果將以地層對比與鏡煤素反射率分析進行限縮。成果顯示，馬達吉達溪剖面利用五個有效樣本獲得了709~2,248公尺的地層侵蝕量分析成果；地層對比成果顯示此研究區之地層侵蝕量下限為562公尺；鏡煤素反射率分析顯示，在無地溫異常之條件下，地層侵蝕量為3,688公尺。樂合溪剖面僅有一個有效樣本進行孔隙率-有效應力分析，獲得了1,186~2,162公尺的地層侵蝕量分析成果，而地層對比與鏡煤素反射率分析皆無法為此研究區限縮成果，使得本研究於樂合溪剖面獲得的成果仍有不確定性。
摘要(英) Erosion amount is an important parameter for prediction of evolution history of sedimentary basin, estimation of orogenic belt growth, and the process of organic material maturation and migration. Traditionally, the estimation of erosion amount is mostly performed by geophysical, geochemical, and stratigraphic contrast. However, in the fore-arc basins of the Coastal Range (Taiyuan and Loho Basin), due to (1) lack of logging and seismic data by geophysics; (2) the source of sediments is mainly from Central Mountain Range, the highly metamorphic sediments seriously interfere the measurement of geochemical indicators. (3) The area has large-scale uplift and erosion, stratigraphic contrast is hardly to be used. These three factors result in high uncertainty in the estimation of erosion amount from any single method. In this study, five sandstone samples were collected from Madagida section of the Taiyuan Basin and three sandstone samples were collected from Loho section of the Loho Basin. By attempting porosity-effective stress analysis, we can get preconsolidation pressure of each samples and use it to calculate their erosion amount. The principle of porosity-effective stress analysis is based on mechanical compaction, if the sample was compacted by chemical reaction, it will be regarded as an invalid sample. In order to increase the credibility of the results, this study use two method to judge the compaction style of the sandstone samples: (1) thin section observation; (2) paleotemperature analysis by vitrinite reflectance. The result of calculated erosion amount will then be compared by two method: (1) stratigraphic contrast; (2) vitrinite reflectance analysis. The results show that, all five sandstone samples in Madagida section are available to attempt porosity-effective stress analysis and derive the erosion amount between 709~2,248 meters; the result of stratigraphic comparison suggest that the lower boundary of erosion amount in Madagida section is 562 meters; whereas the result of vitrinite reflectance analysis shows that, in the condition of normal geothermal condition, the erosion amount is 3,688 meters. Furthermore, in Loho section, only one sandstone sample can be used for porosity-effective stress analysis and erosion amount is estimated between 1,186~2,162 m. However, neither stratigraphic contrast nor vitrinite reflectance analysis can constrain the result from porosity-effective stress analysis, causing the result of Loho section have higher uncertainty.
關鍵字(中) ★ 海岸山脈
★ 侵蝕厚度
★ 孔隙率
★ 鏡煤素反射率		 關鍵字(英) ★ Taiwan Coastal Range
★ Erosion Amount
★ Porosity
★ Vitrinite Reflectance
論文目次 摘要...................................................i
Abstract...............................................ii
誌謝...................................................iv
目錄...................................................vi
圖目錄.................................................ix
表目錄.................................................xii

一、緒論...............................................1
1.1 研究動機、目的與論文架構...........................1
1.2 地質背景...........................................2
1.2.1 地體構造演化與沉積歷史...........................3
1.2.2 地層接觸關係與地層詳細資訊.......................8
1.3 地層侵蝕量估計方法的選擇...........................13
1.3.1 常見地層侵蝕量估計方法...........................14
1.3.2 各類方法在本研究區之可行性討論...................15

二、研究方法...........................................16
2.1 孔隙率實驗之砂岩樣本採集與薄片觀察.................16
2.1.1 沉積物受成岩作用的性質轉變.......................17
2.1.2 力學壓密與化學壓密的轉化與判斷標準...............17
2.1.3 砂岩樣本之礦物組成與岩石分類判斷依據.............21
2.1.4 孔隙率試驗之砂岩樣本採集地點.....................22
2.2 地層對比法之概念與限制.............................26
2.3 鏡煤素反射率資料引用與分析方法.....................27
2.3.1 鏡煤素反射率的演變及在地層侵蝕量推估的應用.......27
2.3.2 鏡煤素反射率在海岸山脈南段的研究.................30
2.3.3 造成鏡煤素反射率資料隨機性高的討論...............31
2.3.4 前人鏡煤素反射率樣本深度標定之疑慮...............33
2.4 根據不同圍壓下的孔隙率變化曲線決定預壓密應力.......34
2.4.1 力學壓密中有效應力對孔隙率的影響.................34
2.4.2 決定岩石樣本預壓密應力的原理及相關成果...........36
2.4.3 高圍壓孔隙率量測系統(YOKO2)原理..................39
2.4.4 YOKO2系統操作流程................................40
2.4.5 透過圍壓與孔隙壓力計算有效應力...................42
2.4.6 孔隙率-有效應力實驗資料分析方式..................43
2.4.7 單位重量測.......................................46
2.4.8 利用預壓密應力計算地層侵蝕量.....................47

三、研究成果...........................................50
3.1 孔隙率實驗樣本之薄片觀察與單位重量測...............50
3.1.1 單位重測量成果...................................50
3.1.2 礦物組成分析.....................................51
3.1.3 顆粒接觸關係.....................................52
3.1.4 石英溶液沉澱情形觀察.............................53
3.2 利用地層對比法推估地層侵蝕量的成果.................54
3.2.1 對比區域之選擇...................................54
3.2.2 對比所得之地層侵蝕量成果.........................56
3.3 引用前人Ro(%)資料推估古地溫與地層侵蝕量............57
3.3.1 碳化漂木資料的篩選與樣本深度的重新標定...........57
3.3.2 利用Ro(%)計算地層侵蝕量成果......................59
3.3.3 古地溫推估.......................................60
3.4 孔隙率-有效應力分析地層侵蝕量成果..................62
3.4.1 馬達吉達溪剖面實驗成果...........................62
3.4.2 樂合溪剖面實驗成果...............................67

四、綜合討論...........................................70
4.1 孔隙率實驗之砂岩樣本壓密型態綜合討論...............70
4.2 鏡煤素反射率分析成果討論...........................74
4.2.1 馬達吉達溪剖面...................................74
4.2.2 樂合溪剖面.......................................75
4.2.3 斷層帶對鏡煤素反射率的影響.......................76
4.3 孔隙率-有效應力分析成果討論........................77
4.3.1 馬達吉達溪剖面...................................77
4.3.2 樂合溪剖面.......................................77
4.4 樂合溪剖面之不整合面存在對本研究成果之影響.........79
4.5 綜合討論...........................................82

五、結論與建議.........................................84
5.1 結論...............................................84
5.2 建議...............................................85

參考文獻...............................................86

附錄A QFL分析數據..................................95
附錄B 孔隙率實驗之砂岩薄片影像.....................96
附錄C ?=0之孔隙率-有效應力變化趨勢.................99
附錄D 孔隙率-有效應力實驗數據......................101
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指導教授 董家鈞 蔡龍珆(Jia-Jyug Dong Loung-yei Tsai) 審核日期 2020-7-30
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