臺灣博碩士論文加值系統

一般而言，重要的地體運動多伴隨著大量的岩漿活動，而其溫度、壓力及地化條件控制了岩漿的性質，故火成岩成了研究地體運動的一個重要櫥窗。過去的研究在概念上多基於岩石成因與地體運動間的關聯性，尚無法探討岩漿活動「熱源」的主要機制，在本研究中即針對熱源，來解釋岩漿活動的開始、演化及消滅。大陸東南燕山期以來之岩漿活動之縱、橫軸皆達一千公里之尺度，加上其傳統地質的研究已有基礎，這正是數值方法的最佳研究標的。基本上，本研究利用地函熱對流模式及熱傳導模式的數值方法，來分別模擬上部地函及岩石圈的熱運動，雖然數值方法仍存在著一些不確定性，但其模擬結果，就消極的觀點，可去除不合理的定性模式，反過來說，合理的模式應能通過數值方法的檢驗。
根據地函熱對流模擬的結果，過去許多地質學者所主張由古太平洋方向所引發的低角度隱沒模式，是無法提供熱源以產生足夠的基性岩漿底侵，亦無法造成早燕山期花崗岩漿的活動。地函加熱模式之熱源來自於下部地函，其岩石圈並未直接受到地體運動應力的影響，故岩石圈厚度在此模式中不會有大量的減薄作用。此一機制不僅彌補直接肇因地函柱的缺陷，尚可用來解釋早燕山期花崗岩漿的活動；至於引發地函加熱的機制，則與峨眉山玄武岩地函柱的活動有關。
若考慮花崗岩漿活動與玄武岩漿活動的消長關係，並利用相關的熱傳導模式，證明了加厚的下部岩石圈拆層可造成玄武岩漿底侵下部地殼，進而融熔下部地殼產生花崗岩漿之活動，這樣的模式可合理的解釋晚燕山期大量I型花崗岩漿的形成，而其殘餘物質在更高的地溫條件下，再融熔為更高溫的A型花崗岩漿。由於底侵的玄武岩漿為花崗岩漿的主要熱源，一旦開始發生雙模式火山活動，即代表玄武岩漿不再底侵，故可推論花崗岩漿活動會在短時間內停止。

Generally, the study of igneous rocks is the key to interpret the magmatism in association with plate tectonics. In many cases, their petrogenetic models are based on the relationship between the time of magmatic activities and temperature-pressure-geochemical conditions. However, this kind of studies is not able to reveal the heat source, which is the major controlling factor on the generation, evolution and extinction of the magmatism. To remedy, the numerical method is implemented. The Yanshanian and the successive magmatic activities in SE China have extraordinary dimensions up to a thousand kilometers in two major axes and sufficient basic geological knowledge have been conducted already. It is the best target to use numerical method for the simulation of heat source. In this study, the models of mantle thermal convection and heat transport are conducted to simulate the geothermal evolution in the lithosphere and the upper mantle underneath. Although the uncertainty of numerical method did exist, it is, at least, applicable to eliminate some unreasonable models. This means that a plausible model should be successful to commit the physical constraints.
Previous investigations have proposed that the paleo-Pacific subduction with very low angle slab is responsible for the early Yanshanian magmatism. In the point view of heat source, this mechanism cannot provide adequate energy to generate voluminous basaltic magmas in the mantle and, subsequently, there is no granitic magma generated from basaltic underplating. A heated mantle model is here proposed to overcome the difficulty about the heat source. At the same time, this model would not severely denude the lithosphere, which is conformable with the very limited basaltic magmatisms. Consequently, the tectonics responsible for triggering mantle heating is probably related to a core-mantle-boundary plume stopping at the interface of upper mantle and lower mantle due to the spinel-perovskite transition.
To take account of the interaction between granitic magmatism and basaltic magmatism at late Yanshanian stage, the underplating of basaltic magmas triggered by lithospheric delamination is plausible to generate I-type granitic magma. Subsequently, the dehydrated residual material may be remelted into A-type granitic magmas due to continuous underplating of basaltic magmas. These can be demonstrated by numerical heat transport modeling. However, the underplating of basaltic magma is the major heat source of the granitic magmatism. Therefore, while the basaltic magmas fail to be trapped within the middle-lower crust level, the granitic magmatism should be terminated. This can be defined with the appearance of bimodal volcanism.

中文摘要I
英文摘要III
目錄V
圖目IX
表目XII
第一章緒綸1
1.1研究動機1
1.2數值方法2
1.3研究目標3
1.4地質背景5
1.5前人研究9
第二章研究方法及工具11
2.1概述11
2.2地函熱對流模式14
2.2.1基礎流體力學14
2.2.2地函熱對流模式之基本假設16
2.2.3控制方程式無因次化（non-dimensionalization）18
2.2.4地質材料之形變特性（rheology）20
2.2.5地函熱對流之特性25
2.3熱傳導模式28
2.3.1概述28
2.3.2岩石圈與軟流圈之邊界29
2.3.3熱傳導模式控制方程式33
2.4計算流體力學之解法34
2.4.1處罰函數法36
2.4.2增強拉格蘭芝法37
2.4.3流線函數法38
2.5數值方法42
2.5.1有限差分法42
2.5.2有限元素法45
2.6研究工具46
2.7研究工具48
第三章早燕山期熱歷史51
3.1早燕山期火成活動概述51
3.2隱沒模式52
3.2.1隱沒模式概述53
3.2.2隱沒模式測試56
3.2.2.1控制方程式及求解程序56
3.2.2.2參數設定59
3.2.2.3網格系統及邊界條件63
3.2.2.4初始條件68
3.2.2.5模擬結果71
3.2.3討論77
3.3地函加熱模式80
3.3.1模式建立81
3.3.1.1基礎模式81
3.3.1.2網格系統及邊界條件83
3.3.1.3初始條件86
3.3.1.4模擬結果90
3.3.2模擬討論94
第四章晚燕山期熱歷史99
4.1晚燕山期火成活動概述99
4.2晚燕山晚期岩漿活動熱傳導模式99
4.2.1控制方程式及求解程序102
4.2.2前人研究108
4.2.3晚燕山晚期花崗岩109
4.2.4模式建立112
4.2.4.1初始地溫條件114
4.2.4.2基性岩漿底侵厚度117
4.2.4.3基性岩漿底侵時間118
4.2.4.4基性岩漿底侵深度119
4.2.4.5基性岩漿底侵溫度120
4.2.4.6地殼剝蝕與岩石圈減薄120
4.2.4.7網格系統及邊界條件121
4.2.5模擬結果122
4.2.6討論127
4.2.6.1I型花崗岩漿之生成127
4.2.6.2岩漿活動之休止期128
4.2.6.3A型花崗岩及雙模式火成活動期129
4.2.6.4基性岩脈活動期130
4.2.7結論131
4.3漳州複式岩體熱傳導模式133
4.3.1控制方程式及求解程序138
4.3.2測試模擬139
4.3.3初始地溫梯度141
4.3.4岩體厚度143
4.3.5侵入時間144
4.3.6侵位深度145
4.3.7模式參數146
4.3.8網格系統及邊界條件147
4.3.9模擬結果149
4.3.9.1邊界測試149
4.3.9.2地表熱流150
4.3.9.3模擬冷卻歷史152
4.3.10討論158
4.3.10.1祖地岩體冷卻歷史158
4.3.10.2長泰岩體冷卻歷史159
4.3.10.3古農岩體冷卻歷史161
4.3.10.4延緩古農岩體冷卻歷史之熱事件162
4.3.10.5敏感度分析166
4.3.11結論166
第五章總結169
參考文獻171
附錄A符號說明183
附錄B冪次非牛頓流體之黏滯係數185
附錄C晚燕山晚期A型花崗岩熱傳導模式程式碼187
附錄D漳州複式岩體熱傳導模式程式碼197

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