Please use this identifier to cite or link to this item: http://hdl.handle.net/11455/34445
標題: Effect of Surface Vegetation Type on Soil Water Movement
地表植生類型對土壤水分移動影響之研究
作者: 林軍豪
Lin, Chun-Hao
關鍵字: watermark;土壤水分感應器;vegetation;antecedent rainfall amount;rainfall intensity;植生;土壤水分移動;降雨特性
出版社: 水土保持學系所
引用: 丁澈士、陳慶雄、卓泳良、胡雅倩、葉瑞盛(1999)不同敷蓋與覆蓋處理下對坡地土壤水份動態之研究。 第十屆水利工程研討會論文集:95-102。 何正品(1994)蓮華池森林集水區坡面土壤水分變化對降雨之反應,台灣大學森林學系防災研究室。 何國謙(2005)植物覆蓋和土壤性質與蚯蚓活動關係之研究,國立中興大學水土保持學系碩士論文。 何學哲(1998)福山地區坡面土壤水分變化之研究,台灣大學森林學研究所碩士論文。 吳嘉俊、陳智賢、鄒嘉慶(1995)不同敷蓋材料對陡坡地土壤水分變化及沖蝕控制之研究。 中華水土保持學報26(2):121-133。 吳耀琪(1990)不同覆蓋林地未飽和帶土壤水分變化之研究。台灣大學森林學研究所碩士論文。 林明義(2000)九份二山崩塌地土壤水分特性之研究。國立中興大學 水土保持學系研究所碩士論文。 林俐玲、董小萍(1996),「土壤物理學實習手冊」,國立中興大學水土保持學系。 林正錺、蘇銘燦(1986)多孔體不飽和導水度之理論計算。 中國農業化學會誌24(1):72-79。 涂展台(1999)茶園不同水土保持處理下土壤水分特性曲線之量測。 國立中興大學水土保持學系研究所碩士論文。 陳念軍(1970)滲透現象及其影響因子的研討,水土保持學報 3:18-23。 張仲民(1987)普通土壤學,國立編譯館,台北。 郭魁士(1977)土壤學。中國書局出版。 黃誌川(1999)未飽和層土壤水分移動行為之分析,國立台灣大學地理學系研究所碩士論文。 黃俊義(1981)覆蓋及敷蓋對坡地土壤保水力之影響,水土保持學報14:90-95。 黃國禎、萬鑫森(1996) 坡地植生及覆蓋下土壤水分入滲透性,屏東技術學院學報5(1):45-51。 葉正霖(2002)台灣中部溪流源頭森林集水區水文現象及特性之研究,國立中興大學水土保持學系博士論文。 萬鑫森 譯(1987)基礎土壤物理學,國立編譯館主編,茂昌圖書有 限公司發行。 劉棠瑞、蘇鴻傑(1983)森林植物生態學,台灣商務印書館。 鄭泰山(1989)水土保持草類根系之研究,國立中興大學水土保持學系碩士論文。 盧惠生、楊炳炎(1979)不同覆蓋坡地土壤滲透之探討。 中華水土保持學報10(2):111-120。 顏正平(1974)水土保持木本植物根系分佈類型研究,國立中興大學水土保持學系碩士論文。 謝 銘(2002)中部地區坡地土壤水分流動之研究,國立中興大學水土保持學系碩士論文。 Burdine, N. T. (1953). “Relative permeability calculation from size distribution data”, Am. Soc. Agri. Eng., 10:400-404. Gardner, W. (1920). The capillary potential and its relation to soil moisture content. Soil Sci. 10: 357-359. Gee, G. W., and J. W. Bander (1986). Partical-size analysis. In klute, A. ed., method of soil analysis, part 1, physical and mineralogical Methods, 2nd Ed. Am. Soc. Agronomg and Soil Sci. Madison, Wiscinsin, U.S.A. p383-411. Lewis, M. R., and W. L. Powers (1939). Study of factors affecting infiltration. Soil Sci. Soc. Am. Proc. 3: 334-337. Mualem, Y. (1976). A new model for predicting the hydraulic onductivity of unsaturated porous media. Water Resour. Res. 12: 513-522. Musgrave, G. W. (1955). How much of the rain enters the soil. U.S.D.A. yearbook, water: 151-159. Nelson, D. W., and L. E. Sommers (1975). A rapid accurate procedure for the estimation of organic carbon in soils. Proc. Indiana Acad. Sci. 84: 456-462. Tiulin. A. F. (1928). Questions on soil structure : Ⅱ Aggregate analysis as a method for determining soil structure. Perm. Agr. Exp. Sta. Dir. Agr. Chem. Rep. 2:77-122. van Genuchten, M. Th. (1980). A closed-form equation for predicting the hydraulic conductivity of unsaturated soils. Soil Sci. Soc. Am. J. 44: 892-898. Walkley, A., and I. A. Black (1934). An examination of he Degtjareff method for determining soil organic matter and a proposed modification of the chromic acid titration method. Soil Sci. 37: 29-38. Williams, J., R. E. Prebble, W. T. Williams, and C. T. Hignett (1983). The influence of texture, structure and clay mineralogy on the soil moisture characteristic. Aust. J. Soil Res. 21: 25-32. Wösten, J.H.M., and M. Th. van Genuchten (1988). Using texture and other soil properties to predict the unsaturated soil hydraulic functions. Soil Sci. Soc. Am. J. 52: 1762-1770. Yorder, R. E. (1936). A direct method of aggregate analysis and a study of the physical nature of erosion losses. J. Am. Soc. Agron. 28:337-351.
摘要: 
本研究選取九份二山兩鄰近試區,雜木林試區與堆積平台試區,架設資料收集記錄器(Dataloogger)與埋設土壤水分感應器(Watermark)以探討不同植生狀況對土壤水分移動的關係。
植被種類影響土壤水分移動的原因之ㄧ在於在於根系分佈深度的差別。雜木林試區因為有較多的木本植物,根系分佈較深,是以30cm深之土壤水分變化量不論濕季與乾季變化都要比15cm深處來得大。而堆積平台試區之主要植生為草本植物,所以淺層之土壤水分變化量較大,變化幅度由大至小排列為15cm、30cm、60cm與90cm深。
研究降雨期間土壤水分變化情形,結果發現土壤水分並沒有完全依照土壤深度向下增加,雜木林試區在4.5 mm/hr降雨強度、堆積平台試區在9 mm/hr的降雨強度下,水分會藉由腐根或土壤生物所造成的通道(Soil pipes)快速通過15cm下移至深層土壤。研究土壤退水情形發現,臨前雨量為影響退水斜率與持水時間的因子,臨前雨量與退水斜率呈負相關,而與持水時間呈正相關。

To understand the relationship between different vegetation cover and soil moisture movement, Dataloggers and Watermarks have been both set up in two experimental areas, namely, forest area and grass area.
One of the reasons that different vegetations influence soil water movement is different distribution of root system. Because there are more woody plants in forest area, the root system is distributed in deeper soil layer. No whether wet season or dry season, the soil water variation in 30 cm depth are larger than in 15 cm depth. Herb is the most vegetation cloak in grass area, so the soil water variation is huge in shallow layer of soil. Therefore, the range of soil water variation from heavy to light arrange for depth of 15cm, 30cm, 60cm, and 90cm.
In the study of the situation of soil water movement during the rainfall, it is found that soil doesn't wet downward each time. When the rainfall intensity arrived 4.5 mm/hr in forest area or 9.0mm/hr in grass area , water moved through 15 cm depth and arrived the deep soil layer. This might be caused by soil piping which mainly formed from rotten root. In the study of the soil water recession variation, It is found that antecedent rainfall amount is the major factor that affect the slope of soil water recession and the hours of soil water maintained. The antecedent rainfall amount and the slope of soil water recession are in negative relation, and the antecedent rainfall amount and the hours of soil water maintained are in positive relation.
URI: http://hdl.handle.net/11455/34445
其他識別: U0005-2508200618182500
Appears in Collections:水土保持學系

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