河海大学学报(自然科学版)
河海大學學報(自然科學版)
하해대학학보(자연과학판)
JOURNAL OF HOHAI UNIVERSITY (NATURAL SCIENCES)
2009年
6期
650-654
,共5页
谭忠成%陆宝宏%汪集旸%孙营营
譚忠成%陸寶宏%汪集旸%孫營營
담충성%륙보굉%왕집양%손영영
氢氧稳定同位素%降雨%径流%钙离子%电导率%五道沟试验场
氫氧穩定同位素%降雨%徑流%鈣離子%電導率%五道溝試驗場
경양은정동위소%강우%경류%개리자%전도솔%오도구시험장
stable hydrogen and oxygen isotopes%precipitation%runoff%calcium ion%electric conductivity%Wudaogou Hydrological Experimental Catchment
在淮北平原区五道沟水文水资源试验场,对降雨径流中的氢氧稳定同位素组成变化的特点及控制平原区河道径流组分划分的一些流域水文因素进行了同位素示踪实验研究.结果表明,实验期间降雨中的δ(~(18)O)(-0.918%～-0.518%)及δ(~2H)(-5.064%～-2.310%)的变幅较大,并随雨强的降低而增大;1,3,6号测井地下水的δ(~(18)O)(或δ(~2H))主要与补给区水源及降雨的δ(~(18)O)(或δ(~2H))有关,其对降雨入渗补给的响应较慢,有明显的滞后效应;IR自记井及S4抽水井由于受抽水灌溉等人类活动的持续影响,δ(~(18)O)(或δ(~2H))明显偏负,表明有来自深部潜水的补给.此外,流域出口断面河水的δ(~(18)O)(或δ(~2H))受平原型流域较强均化作用的影响,其变幅远远小于降雨的δ(~(18)O)(或δ(~2H))变幅,在使用同位素方法划分河道径流组分时,需要考虑降雨到形成河道径流的传输时间.
在淮北平原區五道溝水文水資源試驗場,對降雨徑流中的氫氧穩定同位素組成變化的特點及控製平原區河道徑流組分劃分的一些流域水文因素進行瞭同位素示蹤實驗研究.結果錶明,實驗期間降雨中的δ(~(18)O)(-0.918%～-0.518%)及δ(~2H)(-5.064%～-2.310%)的變幅較大,併隨雨彊的降低而增大;1,3,6號測井地下水的δ(~(18)O)(或δ(~2H))主要與補給區水源及降雨的δ(~(18)O)(或δ(~2H))有關,其對降雨入滲補給的響應較慢,有明顯的滯後效應;IR自記井及S4抽水井由于受抽水灌溉等人類活動的持續影響,δ(~(18)O)(或δ(~2H))明顯偏負,錶明有來自深部潛水的補給.此外,流域齣口斷麵河水的δ(~(18)O)(或δ(~2H))受平原型流域較彊均化作用的影響,其變幅遠遠小于降雨的δ(~(18)O)(或δ(~2H))變幅,在使用同位素方法劃分河道徑流組分時,需要攷慮降雨到形成河道徑流的傳輸時間.
재회북평원구오도구수문수자원시험장,대강우경류중적경양은정동위소조성변화적특점급공제평원구하도경류조분화분적일사류역수문인소진행료동위소시종실험연구.결과표명,실험기간강우중적δ(~(18)O)(-0.918%～-0.518%)급δ(~2H)(-5.064%～-2.310%)적변폭교대,병수우강적강저이증대;1,3,6호측정지하수적δ(~(18)O)(혹δ(~2H))주요여보급구수원급강우적δ(~(18)O)(혹δ(~2H))유관,기대강우입삼보급적향응교만,유명현적체후효응;IR자기정급S4추수정유우수추수관개등인류활동적지속영향,δ(~(18)O)(혹δ(~2H))명현편부,표명유래자심부잠수적보급.차외,류역출구단면하수적δ(~(18)O)(혹δ(~2H))수평원형류역교강균화작용적영향,기변폭원원소우강우적δ(~(18)O)(혹δ(~2H))변폭,재사용동위소방법화분하도경류조분시,수요고필강우도형성하도경류적전수시간.
The characteristics of stable hydrogen and oxygen isotopes of precipitation-runoff components and some factors controlling the partitioning of different water sources of streamflows were investigated for a precipitation event in the Wudaogou Hydrological Experimental Catchment on the Huaibei Plain of China. The analytic results show that the values of the isotopic composition δ(~(18)O)( -0.918% ～ -0.518%) and δ(～２H)( -5.064% ～ -2.310%) of precipitation have large ranges of variation, and increase with the decrease of the precipitation intensity. The values of δ(~(18)O) (or δ(~2H)) forgroundwater from holes 1, 3 and 6 mainly relate to those of δ(~(18)O) (or δ(~2H)) for the groundwater recharge sources and precipitation in the area. They show a slow response to the precipitation infiltration and there exists a time lag effect. Well IR and pumping well S4 have been continuously influenced by human activities such as pumping and irrigation. The values of δ(~(18)O) (or δ(~2H)) are relatively negative, indicating the recharge of deep groundwater. In addition, the values of δ(~(18)O) (δ(~2H)) of river water at the outlet have a smaller range of variation than those of the precipitation owing to the homogenization of the plain-type catchment. It is suggested that the transfer time for the precipitation to form the streamflow should be considered in the application of isotopic methods to divide components of streamflow.
