subsurface runoff 中文意思是什麼

subsurface runoff 解釋
次表層徑流
  • subsurface : adj. 表面下的，液面下的；地下的，水面下的。n. 地面下[水面下]的部分〈巖石，土壤，水層等〉。
  • runoff : 降雨徑流
  1. On the formation mechanism, the rills were mainly formed by the concentrated action of the runoff on dyke slope, while the formation of socket mainly depended on surface runoff, subsurface flow and the existing defects within the dykes such as crack, mouse hole, fox and brocks dens

    在成因上，前者主要是降雨形成超滲地面徑流的集中對戧坡的侵蝕作用而形成；後者主要與坡面徑流、壤中流，以及土堤的薄弱點（如裂縫、鼠洞、狐1一灌洞等）有關。
  2. Thus, the next 1500 hours correspond to the base flow recession period. it is obvious that the aquifer with ampler water storage will produce larger subsurface runoff. from the above numerical simulations, one can see that the b - s model can reasonably simulate the subsurface runoff varia - tion in the two extreme conditions

    而在持續了1500 h以後入滲突然都變為0對應著實際情況中徑流的消退期，顯然儲水較多的潛水面的地下徑流比較大，而隨著退水的持續進行行，地下徑流也越來越小
  3. When soil antecedent condition is dry and the initial rainfall intensity is high, peak surface runoff also considerably lag behind that of rainfall, because of the formation of temporary relative impermeable top layer ; b ) surface runoff is controlled primarily by infiltration - excess runoff mechanism under unsaturated condition ; the major fraction of surface runoff are dominated by saturated infiltration - excess runoff response, only a small fraction by return flow mechanism when soil is saturated ; c ) subsurface flow is dominated by saturated runoff mechanism, and the duration of subsurface post the rainfall end is dependent upon rather the soil properties than the rainfall characteristics ; d ) subsurface flow intensity in cultivated soil layer ( 0 ~ 20cm ) is high up to 35mm / h when rainfall intensity is up to 120mm / h, indicating the existing of macropores and pipe flow in cultivated layer

    2 ）耕作制下紫色土的產流主要機制是： 1 ）當雨前土壤含水量未達到飽和狀態時，表面產流起始時間有明顯滯后現象，這與紫色土的快吸水性和較多非毛管孔隙密切相關；當雨前土壤較乾燥，降雨初期雨強較大時，易形成臨時相對不透水表層，表面產流峰也有明顯滯后現象。 2 ）表面徑流的產流方式主要是超滲產流，當土壤達到飽和狀態后，有四川大學博士學位論文小部分回歸流發生，但主要是飽和超滲產流發生，因為紫色土的相對不透水層和其它透水障礙層不明顯。 3 ）壤中流主要是飽和產流，與降雨過程有明顯的滯后，而且雨停后的壤中流產流歷時與降雨特徵無關。
  4. Through examination of the recession limbs of the observed hydrographs, during periods with no rain and thus no surface runoff, one can determine the value of. for this catchment, a value of 0. 8 is obtained. the simulated subsurface runoff at each grid is routed to the outlets through a unit - hydrograph method for overland flow and the linear saint - venant equation for channel flow to get the discharge at xixian station

    對所研究的流域而言，經過估算消退系數為0 . 8 .耦合著這兩種不同地下徑流機制的clm模型都可以計算出每個網格的地表地下徑流深，採用dag lohman 34 ， 35發展的匯流模型進行匯流由於是研究地下徑流，所以取每個網格的地表徑流為0 ，該模型採用單位線計算坡面匯流線性聖維南saint - venant equation進行河道匯流
  5. Next, we will apply this new versioned clm to a river basin at xixian station in the huaihe river basin. xixian station is a hydrological observation station, which covers 10190 km2. we use 11 - year from janu - ary 1980 to december 1990 observed meteorological data and runoff data including surface runoff and subsurface runoff to validate the reliability of this new subsurface model, and furthermore a quasi - steady subsurface runoff model 13, 31 bqas and dsitqsdt is also applied to this region to perform a comparison simulation

    利用包含上述地下徑流機制的clm應用到實際的流域中，選取淮河流域的息縣站所控制的流域作為實驗區域圖4 .息縣站是淮河流域的一個水文觀測站，控制面積為10190 km2 ，利用該區域11年1980年1月到1990年12月的降水氣溫等氣象資料以及徑流包括地表徑流和地下徑流資料來驗證所建立的模型的可靠性
  6. The purpose of this web site is to share my experiences with workers in any country on water logging in agricultural lands, irrigation induced soil salinity, subsurface drainage for agriculture ( horizontal and vertical ), reuse of groundwater, ground - water hydraulics, ( geo ) hydrology, rainfall and surface runoff relations, reclamation and improvement of water logged saline, salty, sodic alkaline, and acid sulphate soils, plant growth, crop production and responses as well as statistical analysis consisting of segmented linear regression and cumulative frequency distributions

    描述:探討農業耕地的水澇問題；灌溉導致的土壤鹽堿化；地表灌溉；地下水的再利用；地下水水力學；雨水與水流失的關系；淺地表排水；土壤開墾及水澇，酸性，堿性土壤的改良；片段線形回歸和累積頻數分佈的統計分析等。
  7. Subsurface runoff is obviously closely related with soil water movement in the unsaturated soil zone and dynamic change of the groundwater table. there - fore, it is necessary to develop the subsurface runoff model with a physical base associated with recharge on the aquifer and total storage in the reservoir. also a soil model with a dynamic representation of the groundwater table makes it possible and reasonable to represent a more logical subsurface runoff parame - terization

    地下徑流顯然與非飽和土壤層中的水分運動以及地下水位的動態變化密切相關，因而有必要發展考慮土壤含水量與潛水面science in china ser . d earth sciences 376中國科學d輯地球科學第36卷水分通量以及地下水位動態變化的土壤水模型相適應且具有物理意義的地下徑流模型;同時地下水位動態表示的土壤水模型也為發展更為合理的地下徑流模型創造了很好的條件
  8. Therefore, the development of the surface runoff and subsurface run - off mechanisms, and a soil moisture model that can represent the hydrological processes correctly is sig - nificant in improving land surface modeling

    因此，發展合適的地表地下徑流機制以及土壤水模型對于改進陸面水文模擬具有重要的的意義
  9. The simulations show that the subsurface runoff model can reasonably simulate the variation of the subsurface runoff during 11 years from 1980 to 1990 in this river basin, which will be useful to improving land hydraulic simulations

    結果表明:該模型合理地模擬該區域10年內基流的變化，對于改進陸面水文模擬是有意義的
  10. This model is validated by a subsurface flow separation algorithm for an ex - ample river basin, which shows that the new model can simulate the subsurface flow reasonably. keywords : subsurface runoff parameterization, boussinesq - storage equation, water storage and re - charge. hydrological processes including surface runoff, subsurface runoff, and soil water movement play a great role in land surface processes

    文中基於boussinesq - storage方程建立了同時考慮潛水面水分儲存和非飽和層水分入滲兩方面影響的地下徑流機制，並利用流域水文資料以及地下徑流分離演算法驗證了所建立模型的可靠性，結果表明該模型能夠比較合理地模擬地下徑流的變化情況
  11. 11 can be a subsurface runoff parameterization with water storage and recharge based on the boussinesq - storage equation 625 written as 11 ee sineee sine. nnnnktaxbtnnuxktbtnsknnktbtaxnnuxktbtnsknnhxtwfnxhkbwfnxhkb letting t tend to infinity, one can get the steady aquifer function hs 13 : 1 sinee. uxaxnsksnnnfnhxxhkb multiplying through by the specific yield, f, and in - tegrating with respect to x between 0 and l gives the drainable storage associated with this steady - state free surface

    下面考慮整個潛水面的一種穩定狀態，也就是是對于任意一個恆定的入滲，當時間時潛水面將達到穩定的狀態不再發生變化，這個時候顯然有， 0 ， . sntnt t ， ssqnl也就是入滲補充量等於地下徑流量
  12. Traditionally, the saturated zone is modeled as a simple lumped continuity equation :, dsitqsdt where t is time, s is the total storage in the reservoir, i is the spatially integrated volume of incoming wa - ter, and q is the discharge subsurface runoff which only depends on the total storage s. this kind of subsurface runoff model has many different parame - terizations 10 12, however it has a very common char - acteristic that the subsurface runoff is just a sin - gle - valued storage - discharge function

    對于大尺度水文模型而言，目前常常採用的是集總式的地下徑流機制，其連續性方程一般可表示為d ， dsitqst ? 1這里t是時間， s表示整個流域潛水面土壤層的飽和區域總的水分儲存量， i t表示t時刻土壤的非飽和區域向整個潛水面的水分補充量， q s表示僅依賴於水分儲存量s的地下徑流量量
  13. 5 summary a subsurface runoff model with water storage and recharge is developed in this paper based on the bous - sinesq - storage equation. the sensitivity of the model parameters is also tested. the subsurface runoff model is applied to a river basin with observed precipitation, observed air temperature data, observed runoff data, and a base flow separation algorithm in order to vali - date the model application

    5結論與討論基於boussinesq - storage方程發展了同時考慮水分儲存和入滲的地下徑流機制，分析了模型參數的敏感性，並針對淮河流域的的息縣控制站所控制的區域，利用降水徑流資料及通用的基流分離演算法進行了驗證
  14. In addition, at ncku - re study site, collections of soil water contents and data of rainfall estimate infiltration and runoff in homogeneous unsaturated soil profiles, after net fuzzy - neuro training, to analyze soil infiltration behavior and determine the infiltration and runoff of the region of the subsurface

    中文摘要本研究主要目的將現地資料含水量，運用模糊類神經網路去做訓練，在考慮降雨與土壤含水量，進行未飽和層剖面之地表入滲、逕流分析與推估。
  15. On the development process, the rills were influenced by rainfall runoff on slope, but the sockets were the result of the long - term repetitious action of rainfall and runoff and subsurface flow

    在發展過程上，前者受降雨徑流侵蝕作用時間集中；後者是在長期多次降雨形成地面徑流和壤中流侵蝕的共同作用下，逐漸發展起來。
  16. Yang and xie 9 developed a numeri - cal model for the moving boundary problem through reducing it to a fixed boundary problem by a coordi - nate transformation. it is necessary to reduce the a subsurface runoff parameterization with water storage and recharge based on the boussinesq - storage equation 623 computational cost of the groundwater model so that it can be applied to a land surface model for climate studies

    文獻9通過一個坐標變換將運動邊界問題轉化為一個固定邊界問題，進一步改進了該土壤水模型的數值計算方法，使其減少計算量，達到能在一般通用的模式中實際應用
  17. It can be seen from the temporal behavior of the three aquifers that hillslopes with a larger inclination react significantly quicker to the re - charge input and tend tend to drain faster than nearly hori - zontal aquifers. this is caused by the increasing it can therefore be estimated using a finite differ - ence approximation, ststttntlqsnt where t is a discrete change in time. so the subsurface runoff parameterization with wa - ter storage and recharge based on the boussinesq - storage equation is founded

    很顯然對于同樣的入滲強度，地下徑流深隨著坡度的增大而變化明顯，這裏面關science in china ser . d earth sciences第4期? ?田向軍等:基於boussinesq - storage方程同時考慮水分儲存和入滲的地下徑流機制379圖2模型參數的敏感性鍵的原因在於隨著坡度的增大，重力的因素起到了更大的作用
  18. Let h be the deviation of the true shape of the free surface from the shape it would hold if the water were distributed in a steady state, then 1 sine. snnaxnnnshxthxthxttfsxkbs using darcy s law and ssqnl, the discharge from the aquifer is given by 0001. xssxsxnnnnsnhqsntfkuhxhhfkuhhxhqfkuhxfsslfkttsk it is easy to get the mean subsurface runoff of this grid bqt. bqtql 626 science in china : series d earth sciences for the aquifer, the continuity equation holds. dsntlqsntdt new subsurface runoff parameterization, a synthetical recharge series is applied to some aquifers with dif - ferent parameters. firstly, the parameter is tested : three aquifers with the same following parameters are used : d 1. 5 m, k 0. 0008 m s, l 100 m, f 0. 34, p 0. 5, three different slopes are considered : 0. 002, 0. 02, 0. 05. fig

    在該模型中有三個重要的模型參數的:整個潛水面平均厚度的線性化參數d ，整個潛水面的平均坡度，以及飽和和水力傳導度k .首先考察一下該模型對于坡度的敏感性:取d 1 . 5 m ， k 0 . 0008 m s ， l 100 m ， f 0 . 34 ， p 0 . 5 .取下面三個不同的坡度0 . 002 ， 0 . 02 ， 0 . 05 .圖2 a給出是實驗給定的入滲強度的時間序列，圖2 b給出的是分別選取這三個坡度時該地下徑流機制所產生的不同的地下徑流的情況
  19. From fig. 3, one can see easily that the the stronger re - charge brings more significant subsurface runoff, and as the recharge continues, the difference between dif - ferent subsurface runoffs becomes very obvious, which is consistent with the facts. after 1500 hours, the recharges are taken to be zero

    從圖3不難看出，在初始條件完全一樣的情況下，強的降水對應的地下徑流深比較大，而且隨著降水的持續進行，地下徑流深的差異也越來越大，這顯然是與實際情形相吻合的
  20. The next work is to apply this subsurface runoff model and the soil moisture model with dynamic representation of the groundwater table to climate simulations

    進一步的工作是要把這樣的地下徑流模型與地下水位動態表示的土壤水模型應用於氣候模擬
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