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完整後設資料紀錄
DC 欄位 | 值 | 語言 |
---|---|---|
dc.contributor.advisor | 賈儀平 | |
dc.contributor.author | Po-Jui Chen | en |
dc.contributor.author | 陳柏瑞 | zh_TW |
dc.date.accessioned | 2021-06-15T04:07:44Z | - |
dc.date.available | 2010-02-11 | |
dc.date.copyright | 2010-02-11 | |
dc.date.issued | 2010 | |
dc.date.submitted | 2010-02-05 | |
dc.identifier.citation | 中文部分
台灣糖業公司,1976,水井手冊,共160頁。 陳鈞嗣,2000,熱脈衝流速儀量測驗正與地層透水性試測,國立台灣大學地質學研究所碩士論文,共66頁。 朱家毅,2000,應用流速儀野外試測地層透水性垂直分布之探討,國立台灣大學地質學研究所碩士論文,共61頁。 詹淳傑,2003,利用熱脈衝流速儀量測地層透水性垂向分布之探討,國立台灣大學地質學研究所碩士論文,共68頁。 李在平,2005,熱脈衝流速儀實驗室量測結果之驗證,中國地質學會94年年會暨學術研討會大會手冊及論文摘要。 中央地質調查所,2008,臺灣山區地下水資源調查研究先期計畫97年度計畫,共166頁。 英文部分 Collar, R. J. , and P. A. Mock , 1997, Using water-supply wells to investigate vertical ground- water quality, Ground Water, v.35, no.5, p. 743-750. Hanson, R.T., and Nishikawa, T., 1996, Combined use of flowmeter and time-drawdowndata to estimate hydraulic conductivities in layered aquifer system, Ground Water, 34(1), 84-94. Hess, A.E., 1984. Use of a low velocity flowmetering the study of the hydraulic conductivity offractured rock. Canadian Geotechnical Journal 23, 69–78. Hess, A.E., 1986. Identifying hydraulically conductive fractures with a slow-velocity borehole flowmeter. Canadian Geotechnical Journal 23, 69–78. Holman, J. P., 1989, Heat Transfer, McGraw-Hill, Inc., U.S.A, p. 5-10. Javandel, I., and Witherspoon, P.A., 1969, A method of analyzing transient fluid flow inmultilayered aquifer,Water Resource Research, 5, 856-869. Maron and Lando, 1976, Fundamental physical chemistry,” Macmillan Publishing Co.,Inc. Molz, F.J., Morin R.H., Hess, A.E., Melville J.G., and Guven, O., The impeller meter for measuring aquifer permeability variations-Evaluation and comparison with other tests, Water Resources Research, 25(7), 1677-1683. Molz, F.J., and Liu, H.H., 1996, Discrimination of fractional Brownian movement and fractional Gaussian noise structures in permeability and related property distribution with range analysis, Water Resources Research, 32(8), 2601–2605. Paillet, F., 1998, Flow Modeling and Permeability Estimation Using Borehole Flow Logs in Heterogeneous Fractured Formations, Water Resources Research, 34(5), 997–1010. Paillet, F., 2004, Borehole flowmeter applications in irregular and large-diameter boreholes, Journal of Applied Geophysics, 55, 39–59. Robertson Geologging Ltd., 1997, User’s Guide for Heat Pulse Flowmeter Sonde, United Kingdom, 36 p. Rorabaugh, M.J., 1953, Graphical and theoretical analysis of step-drawdown test of artesian well, Proc Am Soc Civil Eng 79. Schlumbreger, 1989, Cased Hole Log Interpretation Principles /Applications, Schlumbreger Educational Services, U.S.A, 145p. | |
dc.identifier.uri | http://tdr.lib.ntu.edu.tw/jspui/handle/123456789/45180 | - |
dc.description.abstract | 地層的透水性為地下水文研究與工程應用的重要參數,雖然透過抽水試驗可以量測含水層的平均水力傳導係數,但是無法得知其透水性的變化;而雙封塞微水試驗的方法操作不易,而且精確度欠佳。本研究利用熱脈衝流速儀在井孔內量測地層垂直方向透水性的變化,以得知含水層透水性於垂直方向之變化。
由於井徑大小不同以及抽水量的差異會造成流速儀量測上產生誤差,因此必須針對所記錄的資料進行校正。當流體的雷諾數值大於2100 時,水流會進入亂流的狀態,流體除了向前流動外,並碎成許多漩渦,這使得熱脈衝流速儀量測結果會產生大於實際的現象;受到流速儀之幾何形狀與自然對流等因素的影響,必須透過校正式來修正量測結果,根據測量井之井徑大小不同,其校正公式也有會所差異。 本研究的試驗地點共有兩口井徑直徑皆為8 吋的地下水監測井,兩口深度不同的井分別反應第一與第二含水層之水位變化。先將抽水機置入井內上方進行定量抽水,在井管內產生穩定之向上水流,再把熱脈衝流速儀放置在兩口井內進行垂直流速的量測,並且隨深度記錄地層透水性的變化。經過資料校正之後,原本抽水造成亂流的誤差得以修正,與地層柱以及自然伽瑪資料比對後結果良好,配合中央地質調查所的抽水試驗資料,推算出當地地層垂直方向連續性的水力傳導系數變化。結果顯示,第一含水層主要的透水區段為地下15.50 公尺處附近,而第二含水層主要的透水區段為地下40.75 公尺,雖然含水層的岩性變化不大,但是透水區段的水力傳導係數可達整體含水層之平均水力傳導係數的4.5 倍之高。 | zh_TW |
dc.description.abstract | The permeability of the layer is an important parameter for groundwater research and engineering application. Although one can use pumping-test to measure average hydraulic conductivity of aquifer, one cannot obtain the permeability changes of layers. However, it is difficult to operate double packer slug test and this test is lack of accuracy. The research is measuring the permeability changes of layers on the vertical direction inside the boreholes through heat-pulse flowmeter, therefore we could obtain the data for the permeability of the aquifer changes on the vertical direction.
Due to the difference of well diameters and the amount of pump water, it will cause error when measuring through flowmeter. When Reynolds number of the fluid is bigger than 2100, the flow will enter the turbulent flow status; the fluid will be not only moving forward, but also breaking into eddies and causes the measurement result larger than the reality. Measurement result is affected by the geometric shapes of flowmeter and natural convections, we have to leverage calibration formulas to adjust the measurement results. The calibration formulas would vary by different sizes of well diameters. The study has been conducted with two wells with diameter as 8 inches but different depths to reflect the water level changes of first and second aquifer. We first pumped water at the top of the well and generated a stable upward flow, and then used heat-pulse flowmeter to measure the flow speed on the vertical direction for the two wells. We recorded the permeability of the layer changes as the depth changed. By using the calibration formula, we could correct the error caused by the turbulent flow when pumping. This has been compared with the stratigraphic column and natural gama and showed great result. Leveraging pumping water data from Central Geological Survey MOEA, we could calculate its continuous changes of hydraulic conductivity on the vertical direction. The result showed that major high permeability section of first aquifer is around below 15.50 meter and the major high permeability of second aquifer is around below 40.75 meter. Although the lithology changes of aquifer is not significant, the hydraulic conductivity of high permeability sections could be as high as 4.5 times of the average hydraulic conductivity of overall aquifer. | en |
dc.description.provenance | Made available in DSpace on 2021-06-15T04:07:44Z (GMT). No. of bitstreams: 1 ntu-99-R96224206-1.pdf: 3357500 bytes, checksum: 1dd88730af057fda476a0530b25d54b8 (MD5) Previous issue date: 2010 | en |
dc.description.tableofcontents | 摘要 vi
目錄 viii 圖目 viiiii 表目 ix 第一章 緒論 1 1.1研究動機及目的 1 1.2研究方法 2 1.3文獻回顧 3 第二章 熱脈衝流速儀之原理與操作 4 2.1熱脈衝流速儀運作原理 5 2.2流速儀現地操作及地層透水性計算 7 第三章 熱脈衝流速儀之量測流速校正 10 3.1實驗室內量測系統配置 11 3.2校正分析 13 3.3雷諾數(Reynold number)與流速校正 14 第四章 現場試驗:埔里育英國小地層透水性測勘 17 4.1觀測井概述 17 4.2水文地質 20 4.3現場試驗儀器設置 22 4.4井測記錄綜合分析 23 4.4.1 一號抽水井 23 4.4.2 二號抽水井 26 4.4.3 綜合分析 30 4.5平均水力傳導係數 31 4.6垂直地層剖面各深度之水力傳導係數 32 第五章 討論 39 5.1 環境背景水流(Ambient Flow)與形成的原因 39 5.2 井壁外裂隙對地層透水性測勘之影響 41 第六章 結論與建議 42 參考文獻 44 附錄A 育英國小抽水試驗 47 附錄B 育英國小抽水井岩心照片 49 | |
dc.language.iso | zh-TW | |
dc.title | 埔里盆地透水性垂向分佈量測 | zh_TW |
dc.title | Measurement of Hydraulic Conductivity Along the Vertical Direction in the Puli Basin | en |
dc.type | Thesis | |
dc.date.schoolyear | 98-1 | |
dc.description.degree | 碩士 | |
dc.contributor.oralexamcommittee | 黃燦輝,鄧茂華,王泰典 | |
dc.subject.keyword | 熱脈衝流速儀,水力傳導係數,含水層, | zh_TW |
dc.subject.keyword | Heat-pulse Flowmeter,Hydraulic Conductivity,Aquifer, | en |
dc.relation.page | 51 | |
dc.rights.note | 有償授權 | |
dc.date.accepted | 2010-02-05 | |
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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