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| DC 欄位 | 值 | 語言 |
|---|---|---|
| dc.contributor.advisor | 陳宏宇 | |
| dc.contributor.author | Ming-Hsiang Lu | en |
| dc.contributor.author | 呂名翔 | zh_TW |
| dc.date.accessioned | 2021-06-13T00:42:00Z | - |
| dc.date.available | 2007-07-31 | |
| dc.date.copyright | 2007-07-31 | |
| dc.date.issued | 2007 | |
| dc.date.submitted | 2007-07-25 | |
| dc.identifier.citation | 中文部分
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| dc.identifier.uri | http://tdr.lib.ntu.edu.tw/jspui/handle/123456789/29132 | - |
| dc.description.abstract | 本研究利用SPOT衛星影像，判釋新武呂溪流域於6個颱風時期及2次地震事件後的崩塌地分布狀況，並以溪流內之實測流量、雨量、輸砂量，以及DTM的地形分析，岩石的強度、不連續面分布等資料，來探討流域內的山崩和輸砂量在颱風與地震事件中的相對應關係。
研究結果顯示，六個颱風時期的山崩崩塌率介於0.84%到1.94%之間，崩塌率、新生率及重現率，都是以成功地震後之敏督利颱風為最高、分別為1.94%、72.3%、66.5%。區域內山崩最高點的高程，大多分布於1500至2500公尺之間，在成功地震後有繼續往山頂發展的趨勢；山崩的坡度分布變化並不顯著，大多分布於30°至50°之間，但是在坡度陡峭的邊坡，其崩塌率出現明顯的上昇。在本區域的四個地層單位中，由於畢祿山層具有最低的岩石強度，平均34MPa，因此其崩塌率最高，介於1.74%至2.56%之間；相對的，在大南澳片岩大理岩段具有最高的岩石強度，平均102MPa，所以其崩塌率較低，為0.56%至1.34%之間；大南澳片岩混合片岩段的單位體積節理數最多，平均為 47.3N/m3，山崩的重現率也最大，介於57.3%至72..5%之間，兩者間具有一定程度的相關性。 本區域之常態化差異植生指標(NDVI)，分布於0.44至0.53之間，區域內各事件的崩塌率與植生指標之間的對應關係並不明顯。在輸砂量的統計方面，利用新武呂溪流域1979至2005年的實測值，以平均法和率定曲線法估算，可以得知平均年輸砂量約在7.8至15.2百萬噸之間。輸砂量主要是由颱風暴雨事件所供應，單一事件的輸砂量約佔全年輸砂量的6.6%至25.3%。在單位流量輸砂濃度的變化方面，集集地震後之量測值比地震前增加了2.58倍，在成功地震後又再增加了1.18倍，此結果顯示持續的地震事件，使得集水區內之地質材料變得更加鬆散，不僅崩塌率上升，進而提高了逕流的沖刷能力，並帶走更多的沉積物。 | zh_TW |
| dc.description.abstract | The hydraulic measurement, geomorphologic changes and geomaterial characteristics are utilized to analysis their relationships in their study. The various images of SPOT satellite were selected to count the landslide ratio in six typhoons and two earthquakes events along the catchment of the Sinwulyu River form 1996 to 2006.
The investigated results show that the landslide ratio ranges from 0.84% to 1.94% during the different disaster event. After the Chen-Gong earthquake (ML=6.6), the following Typhoon Mindulle resulted in heavy landsliding, including 1.94% of landslide ratio, 72.3% of new generative ratio and 66.5% of reactive ratio in the catchment. The elevation of most landslides ranges from 1500 to 2500 meters and keep rising after Chen-Gong earthquake. Besides, the landslides converge in the steep slopes ranging from 30° to 50°. The uniaxial compressive strength (UCS) of the Bilushan Formation is the lowest around 34MPa in all rock units, and the landslide ratio in the Bilushan Formation, ranging from 1.74% to 2.56%, is the highest. Comparatively, 102MPa of UCS in the Dananao formation is the highest and the landslide ratio in the Dananao formation, ranging from 0.56% to 1.34%, is the lowest. The Dananao formation has 47.3N/m3 of the joint number that causes the highest reactive ratio, ranging from 57.3% to 72.5%. There is a positive linear relationship and the statistically significance between the reactive landslide ratio and the joint numbers. The Normalized Difference Vegetation Index (NDVI) in this region ranges from 0.44 to 0.53. There is week significance between landslide ratio and NDVI. The annual sediment discharge ranges from 7.8 Mt/y to 15.2 Mt/y by using the calculation of average method and rating curve method from 1979 to 2005. The sediment discharge in the period of rainstorm events occupied 6.6% to 25.3% of annual sediment discharge. The concentration of discharge increased 2.58 times in post Chi-Chi earthquake, and further increased 1.18 times after Chen-Gong earthquake. This result demonstrates that the colluvial sediments of hillslope resulted from the successive earthquakes not only caused the increasing of landslide ratio, but the rising of sediment discharge increased. | en |
| dc.description.provenance | Made available in DSpace on 2021-06-13T00:42:00Z (GMT). No. of bitstreams: 1 ntu-96-R94224209-1.pdf: 2697198 bytes, checksum: 6c4dd2861ee68fcee8b0c1e6cf9f65d2 (MD5) Previous issue date: 2007 | en |
| dc.description.tableofcontents | 中文摘要…………………………………………………………………………… I
英文摘要…………………………………………………………………………… II 目錄………………………………………………………………………………… IV 圖目錄……………………………………………………………………………… VII 表目錄……………………………………………………………………………… X 第一章 緒論……………………………………………………………….. 1 1.1 研究動機與目的………………………………………………. 1 1.2 地理位置與交通狀況…………………………………………. 1 第二章 前人研究………………………………………………………….. 4 2.1 山崩特性………………………………………………………. 4 2.2 輸砂量與侵蝕率………………………………………………. 7 2.3 常態化差異植生指標…………………………………………. 10 第三章 區域概況………………………………………………………….. 13 3.1 地形概況………………………………………………………. 13 3.2 地質概況………………………………………………………. 15 3.3 水文及氣候概況………………………………………………. 19 3.4 地震與颱風事件………………………………………………. 21 第四章 研究方法………………………………………………………….. 25 4.1 野外調查………………………………………………………. 25 4.1.1 露頭量測與記錄………………………………………………. 25 4.1.2 現地施密特錘試驗..................................................................... 27 4.1.3 樣品採集………………………………………………………. 27 4.2 室內試驗………………………………………………………. 28 4.2.1 自然物理性質試驗……………………………………………. 28 4.2.2 岩石力學性質試驗……………………………………………. 28 4.2.2.1 超音波試驗……………………………………………………. 28 4.2.2.2 單軸抗壓試驗…………………………………………………. 28 4.2.2.3 抗張強度試驗…………………………………………………. 28 4.2.2.4 點荷重試驗……………………………………………………. 29 4.3 崩塌地判釋……………………………………………………. 29 4.4 輸砂量估算……………………………………………………. 30 4.4.1 年輸砂量估算…………………………………………………. 30 4.4.2 暴雨事件輸砂量估算…………………………………………. 31 4.5 常態化差異植生指標分析……………………………………. 33 第五章 試驗結果………………………………………………………….. 35 5.1 單位體積節理數統計…………………………………………. 35 5.2 自然物理性質…………………………………………………. 36 5.3 岩石傳波速度…………………………………………………. 39 5.4 岩石抗壓強度…………………………………………………. 40 5.4.1 單軸抗壓強度…………………………………………………. 40 5.4.2 施密特錘強度…………………………………………………. 42 5.4.3 點荷重強度……………………………………………………. 43 5.4.4 平均抗壓強度…………………………………………………. 45 5.5 岩石抗張強度…………………………………………………. 46 第六章 山崩特性與影響因素…………………………………………….. 48 6.1 崩塌地統計……………………………………………………. 48 6.2 山崩特性分析…………………………………………………. 50 6.3 山崩與地形的關係……………………………………………. 53 6.3.1 山崩的高程分佈………………………………………………. 53 6.3.2 山崩的坡度分佈………………………………………………. 55 6.3.3 山崩的坡向分佈………………………………………………. 56 6.4 山崩與水文狀況的關係………………………………………. 58 6.4.1 河川密度對崩塌率的影響……………………………………. 58 6.4.2 河流侵蝕與崩塌率的關係……………………………………. 60 6.5 山崩與岩層的關係……………………………………………. 62 6.5.1 岩石強度對山崩的影響………………………………………. 62 6.5.2 單位體積節理數對山崩的影響………………………………. 63 6.6 颱風降雨對山崩的影響………………………………………. 65 6.7 山崩與植生指標的對應關係…………………………………. 70 第七章 輸砂量估算及討論……………………………………………….. 73 7.1 年度輸砂量估算………………………………………………. 73 7.2 暴雨事件輸砂量………………………………………………. 79 7.3 地震前後輸砂量變化…………………………………………. 81 7.4 雨量對輸砂量的影響…………………………………………. 82 7.5 輸砂量與崩塌率的關係………………………………………. 84 第八章 結論……………………………………………………………….. 86 參考文獻 …………………………………………………………………….. 88 附錄一 施密特錘強度換算表…………………………………………….. 95 附錄二 自然物理性質試驗方法………………………………………….. 96 附錄三 岩石風化程度分級表…………………………………………….. 98 附錄四 岩石試驗規範…………………………………………………….. 99 附錄五 SPOT衛星影像資料……………………………………………… 101 附錄六 泰利颱風後之SPOT衛星影像 102 附錄七 崩塌地數化成果………………………………………………….. 103 附錄八 打荻公式之K與r的對應關係………………………………….. 105 附錄九 各年度率定曲線關係式………………………………………….. 106 附錄十 各颱風事件的水文資料………………………………………….. 107 附錄十一 自然物理性質試驗數據………………………………………….. 108 附錄十二 單壓強度試驗數據……………………………………………….. 110 附錄十三 施密特錘試驗數據……………………………………………….. 111 附錄十四 點荷重試驗數據………………………………………………….. 112 附錄十五 抗張試驗數據…………………………………………………….. 113 | |
| dc.language.iso | zh-TW | |
| dc.subject | 輸砂量 | zh_TW |
| dc.subject | 山崩 | zh_TW |
| dc.subject | 颱風 | zh_TW |
| dc.subject | 地震 | zh_TW |
| dc.subject | 岩石強度 | zh_TW |
| dc.subject | 常態化差異植生指標 | zh_TW |
| dc.subject | earthquake | en |
| dc.subject | landslide | en |
| dc.subject | typhoon | en |
| dc.subject | NDVI | en |
| dc.subject | sediment discharge | en |
| dc.subject | rock strength | en |
| dc.title | 新武呂溪流域的山崩與輸砂量在地震與颱風事件中的相對應關係 | zh_TW |
| dc.title | The relationships between landslide and sediment discharge in the periods of earthquake and typhoon events along the catchment of the Sinwulyu River | en |
| dc.type | Thesis | |
| dc.date.schoolyear | 95-2 | |
| dc.description.degree | 碩士 | |
| dc.contributor.oralexamcommittee | 林曉武,洪銘堅,侯秉承 | |
| dc.subject.keyword | 山崩,颱風,地震,岩石強度,常態化差異植生指標,輸砂量, | zh_TW |
| dc.subject.keyword | landslide,typhoon,earthquake,rock strength,NDVI,sediment discharge, | en |
| dc.relation.page | 113 | |
| dc.rights.note | 有償授權 | |
| dc.date.accepted | 2007-07-25 | |
| dc.contributor.author-college | 理學院 | zh_TW |
| dc.contributor.author-dept | 地質科學研究所 | zh_TW |
| 顯示於系所單位： | 地質科學系 | |
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