臺灣博碩士論文加值系統

摘要

從陳有蘭溪流域在1996年賀伯颱風、1999年921地震、2001年桃芝颱風及2004年敏督利颱風等四個事件所進行之研究中發現，921地震後的五年內，山崩新生率上升至70%，山崩重現率下降至40%，四個事件之山崩面積機率迴歸指數均大於1.5，此意義顯示山崩類型主要為小於2000 m2之小規模山崩。從山崩最低點的機率分布也可以發現，921地震後仍有超過90%的崩塌材料堆積在山坡上。
從河流輸砂量的統計結果發現，921地震後陳有蘭溪之平均年輸砂量達37百萬噸，較地震前增加13倍，單位懸浮沉積物濃度較地震前增加4 倍以上，而桃芝及敏督利颱風期間，單位流量中之輸砂量也超過賀伯颱風的1.5倍，此意義顯示，地震後本研究區內的輸砂特性有了變化，不但平均年輸砂量上升，且在相同流量條件下，地震後之輸砂量會較地震前高。
就山崩與岩石強度之對應關係中可瞭解，921地震後南莊層之崩塌率為地震前的17倍，和社層為3.4倍，變質岩層為4.8倍，其中以南莊層崩塌率的上升幅度最大，此原因可能是南莊層之岩石平均強度不到和社層及變質岩層的2/3使然。而南莊層及和社層在921地震後之山崩重現率下降25%，變質岩層僅下降6%，此結果可能與變質岩層之不連續面的分布比例為南莊層及和社層的2倍有密切關係。
從崩塌面積的分布與車籠埔斷層距離的關係中可以發現，921地震的山崩與斷層距離超過20km後，崩塌率有明顯下降的趨勢，在桃芝颱風的山崩分布中亦可看到此現象，而敏督利颱風時，此現象已不明顯。從降雨量與山崩率的比對中可以發現，賀伯颱風時，降雨量越大的集水區，崩塌率就越高，其相關係數達0.99，但降雨量與桃芝颱風及敏督利颱風的山崩卻無此明顯的關係，此現象可以說明賀伯颱風的崩塌主要是受到降雨多寡的影響，而桃芝及敏督利颱風除了降雨量的關係外，還包括了921地震的影響。

Abstract

Examining the effects of four events -- typhoon Herb, 921-earthquake, typhoon Toraji and typhoon Mindulle -- along the catchments of Chenyoulan River, we found that newborn landslide rate increased to 70%, while the reactive landslide rate decreased to 40%. Regression exponent results show that the landslides associated with these four events were all greater than 1.5, indicating that the landslides in Chenyoulan watershed are dominated by small landslides, which tend to be less than 2000m2. Probability distribution in the upslope area at the lower most point reached by landslides shows that 90% of the landslides remained confined to hillslopes after 921-earthquake. In addition, the post-earthquake average sediment discharge was 37 Mt/yr, some 13 times the pre-earthquake amount. The post seismic unit sediment concentration also increased by 4 times in the Chenyoulan River.
The post-earthquake landslide rate for Nanchuang formation increased 17times. In contrast, the landslide rate for Hoshe formation only increased 3.4 times, and the metamorphic formation only increased 4.8 times. These results reveal that the rock strength of Nanchuang formation was smaller than that of Hoshe formation and metamorphic formation. The post-earthquake reactive landslide rate for Nanchuang formation and Hoshe formation decreased to 25%, but at the same time the metamorphic formation decreased only 6%. The controlling factor came from the discontinuities distribution, because the joints sets for Nanchuang formation and Hoshe formation were only 2/3 of the metamorphic formation.
Analysis of the correlation between landslide distribution and distance from the Chelungpu fault revealed that the 921 co-seismic landslide rates decayed more rapidly after 20 km; landslide effects of typhoon Toraji indicated similar results. The relation between accumulated rainfall and landslide rate display that during typhoon Herb the landslide rate increased with the accumulated rainfall, and the correlation coefficient reached 0.99. But during typhoon Toraji and Mindulle the landslide rate didn’t have good relation with the accumulated rainfall, the landslides during typhoon Toraji and Mindulle maybe affected by 921 earthquake.

目錄

致謝 …………………………………………………….... Ⅰ
中文摘要 ……………………………………………………... Ⅱ
英文摘要 ……………………………………………………... Ⅲ
目錄 ……………………………………………………... Ⅴ
圖目錄 ……………………………………………………... Ⅷ
表目錄 ……………………………………………………... Ⅹ

第一章 緒論………………………………………………... 1
1.1 前言………………………………………………... 1
1.2 研究動機與目的…………………………………... 2
1.3 地理位置及交通狀況……………………………... 3

第二章 文獻回顧……………………………....................... 5
2.1 地質條件與山崩及土石流的關係………………... 5
2.2 降雨與地震對山崩及土石流的影響……………... 7
2.3 山崩機率的分布……………………………........... 8
2.4 侵蝕率的變化……………………………………... 9
2.5 地表起伏與侵蝕作用……………………………... 13

第三章 研究區域概況……………………………………… 15
3.1 地質概況……………………………………............ 15
3.2 氣候及水文………………………………………… 19
3.3 地質災害事件……………………………………... 22

第四章 研究方法…………………………………………... 25
4.1 野外調查…………………………………………... 25
4.2 室內實驗室試驗…………………………………... 26
4.3 地理資訊系統分析………………………………... 30
4.4 輸砂量計算………………………………………... 32

第五章 研究方法結果……………………………………… 37
5.1 自然物理性質試驗結果………………………….... 37
5.2 傳波速度試驗結果………………………………... 41
5.3 抗壓強度試驗結果……………………………….... 42
5.4 抗張強度試驗結果………………………………... 45
5.5 崩塌地數化及統計結果…………………………... 46
5.6 輸砂量計算結果…………………………………... 47
5.7 水文分析結果……………………………………... 52
5.8 地形分析結果……………………………………... 53

第六章 山崩及輸砂量特性………………………………... 57
6.1 山崩面積機率分佈………………………………... 57
6.2 山崩最高點及最低點的機率分佈………………… 59
6.3 山崩坡度的機率分佈……………………………… 63
6.4 山崩的新生率及重現率…………………………... 64
6.5 地震前後輸砂量的變化…………………………... 67
6.6 懸浮輸砂量與河床載的關係……………………... 70
6.7 乾季與濕季之差別………………………………... 71
6.8 輸砂量統計法之比較……………………………… 73

第七章 影響山崩及輸砂量之因子………………………… 77
7.1 岩石強度與山崩的關係…………………………... 77
7.2 不連續面分布狀況與山崩的關係………………… 78
7.3 斷層距離與山崩的關係…………………………... 81
7.4 地形及水文因子與山崩的關係…………………... 82
7.5 降雨與山崩及輸砂量的關係……………………… 86
第八章 結論……………………………………………….... 91

參考文獻 …………………………………………………….... 93
附錄一 暴雨事件的雨量、流量及輸砂量………………….. 103
附錄二 單位體積節理數的估計法………………………… 106
附錄三 施密特錘試驗換算單壓強度圖…………………… 107
附錄四 自然物理性質試驗方法…………………………… 108
附錄五 點荷重試驗方法…………………………………… 110
附錄六 輸砂量估算公式…………………………................ 112
附錄七 平均年輸砂量估計結果…………………………… 113
附錄八 本研究區之坡度分布……........................................ 115
附錄九 1985至2004年颱風事件之降雨量及輸砂量……... 116
附錄十 自然物理性質試驗紀錄…………………………… 117
附錄十一 各項抗壓試驗結果………………………………… 119
附錄十二 野外露頭不連續面調查結果……………………… 122
附錄十三 輸砂量與流量的關係……………………………… 125
附錄十四 颱風及地震誘發之山崩分布……………………… 128
附錄十五 敏督利颱風期間愛玉子溪土石流監測系統資料… 129

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