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1、Changes in groundwater induced by water diversion in the Lower Tarim River,Xinjiang Uygur, NW China: Evidence from environmental isotopes and water chemistry（由引水調(diào)度引起的塔里木河下游地下水變化的研究, 中國西北新疆維吾爾自治區(qū) :基于環(huán)境同位素和水化學(xué)）匯報人：導(dǎo) 師： 專 業(yè)：Literatures Review2Literatures SourceArticle structure 1、Title and author 2、Sum

2、maryPhase 4Phase 3Phase 2Phase 11、Introduction 2、Background 1、Sampling 2、Analyses 1、Results and Discussion 2、Conclusions3、references12334435 Summary Contents Introduction and Background Sampling and AnalysesResults and Discussion Conclusions51. Summary1、提出問題:The Lower Tarim River in NW China is unde

3、r severe ecosystem degradation due to stopped stream flow and diminished groundwater recharge. Since year 2000, eight water diversions from the upper streamand from the neighboring KaiduKongque River have been implemented to alleviate the ecosystem disaster.中國西北部塔里木河下游面臨嚴(yán)重生態(tài)退化是由于河流斷流和地下水補給減少造成的。自200

4、0年以來, 通過從鄰近的開都和孔雀河等河流上游的八次引水調(diào)度已經(jīng)緩解塔里木河生態(tài)環(huán)境問題。71. Summary3、研究結(jié)果:Remarkable changes have been induced by the water diversions as follows：(1) The observed response of riparian groundwater system includes general decrease in total dissolved solid (TDS) and rise of water table. Greater rise of water tabl

5、e occurs near the river bank.沿河岸地下水系統(tǒng)觀察結(jié)果包括:總?cè)芙夤腆w(TDS)減少和水位上升。更大的地下水位上升發(fā)生在河岸附近。(2) Tritium data show that the extent of modern recharge (since1960s), including that from the diverted water, is limited to 600m from the riverbank at the upper segments and 200 m at the lower ones.氚數(shù)據(jù)顯示,現(xiàn)代水補給范圍(since196

6、0s),包括從轉(zhuǎn)移水,僅限于上游河岸600米內(nèi)部分和下游200米內(nèi)。81. Summary(3) Stable isotopes show that groundwaters are enriched in heavy isotopes and are plotted in parallel to the meteoric water line, attributed to evaporation during recharge.穩(wěn)定同位素表明,地區(qū)地下水重同位素豐富,并與大氣降水線平行,歸因于蒸發(fā)。(4) Groundwater is generally of NaMgClSO4 type

7、and is formed by dissolution of minerals. The salinity of groundwater is mainly affected by that of the diverted water and of the local antecedent groundwater, salts in the unsaturated zone, evapotranspiration during recharge.地下水一般由Na-Mg-Cl-SO4類型和溶解的礦物質(zhì)組成。地下水鹽度主要是受轉(zhuǎn)移水和當(dāng)?shù)厍捌诘叵滤?在非飽和區(qū)的鹽度,蒸散發(fā)影響。102、Intr

8、oduction and Background Water diversionGeneral settingHydrogeologyClimateEcosystem degradationIntroduction and Background112、Introduction and Background Introduction: Under the dual impacts of anthropogenic activities and climate change, a common scenario in arid and semiarid catchments, particularl

9、y in the lower reaches of them, is severe ecological degradation, such as death of vegetation, intensified groundwater salinization, soil salinization and desertification, etc.介紹：人為活動和氣候變化的雙重影響下,一個常見的場景在干旱和半干旱區(qū),特別是在下游,是嚴(yán)重的生態(tài)退化,如植被死亡,加劇地下水鹽漬化、土壤鹽漬化、沙漠化等。 12Background:1、General settingThe Tarim River

10、Basin is located in the south of Xinjiang, NW China. It has an area of 1.04x106 km2 and is flanked by the Tianshan Mountains to the north and by the Kunlun Mountains to the south (Fig. 1).2、HydrogeologyThe occurrence of groundwater is similar between the Southern Tianshan watershed and Northern Kunl

11、un watershed. The sink of the two groundwaters systems is centered in the south of the Tarim River. The diluvial aquifer from the northern mountains is composed of sand deposits some 100300 m thick forming an unconfined aquifer in which the present day water table ranges between 20 m and 200 m below

12、 surface (Fig. 2). 2、Introduction and Background 14Fig.2 Hydrogeological cross section in the Middle Tarim River, see Fig. 1 for the location15Background:3、ClimateThe Lower Tarim River is dominated by typical continental temperate arid climate.4、Ecosystem degradationUnder the impact of anthropogenic

13、 activities, runoff of three source streams (Aksu River, Hotan River and Yarkant River) to the Tarim River has decreased gradually in the last 50 years due to extensive oasis agriculture with increasing water utilization. With gradually decreased inflow to the Tarim River, proportion of water consum

14、ption in the upper and middle reaches increased gradually from 1970s to 1990s, while flow to the lower reaches reduced significantly (Table 1). The groundwater depth has increased to 812 m. 2、Introduction and Background 17Fig. 3 Sampling locations 18 Table 2 Statistics of eight water diversions193.S

15、ampling and Analyses采樣點布置及前期準(zhǔn)備穩(wěn)定同位素測定方法及標(biāo)準(zhǔn)18O, H, H 穩(wěn)定同位素測量八次引水后塔里木河流域下游地下水的物理化學(xué)變化規(guī)律及特征水化學(xué)測定方法及標(biāo)準(zhǔn)采樣方法及具體實施步驟水化學(xué)離子色譜法測定地下水位、位置,水溫、pH值、TDS和電導(dǎo)率測定20Sampling：Groundwater samples were collected from boreholes at varying distances from the riverbed along nine groundwater monitoring transects, namely: Akdun

16、 (A), Yahopumarhan (B), Yengsu (C), Abudali (D), Karday (E), Tugmailai (F), Aragan (G), Yikanbujima(H), and Kargan (I) (Fig. 3), respectively.Method：The soil samples were obtained using a hollow-stem hand auger with interchangeable 1.5 m aluminum rod from three profiles(5.87.7 m depth, SP1 and SP2 i

17、n section C and SP4 in section G, Figs. 3 and 4). Bulk soil samples of 400 g were collected at intervals of 0.25 m. Samples were homogenized over the sampled interval and immediately sealed in polyethylene bags. 3.Sampling and Analyses21Method：Gravimetric moisture content was determined by drying a

18、minimum of 80 g of soil at 110 C for 12 h. To determine chloride content, double deionisedwater (40mL) was added to the oven-dried soil sample (40 g) . Samples were agitated on a reciprocal shaker table for 8 h. The supernatant was filtered through 0.45 lm filters. Chloride was then analyzed by ion

19、chromatography.The chloride concentration of the soil solution is then calculated by dividing the measured concentration by gravimetric moisture content and by multiplying the mass ratio of solution to oven dry soil.3.Sampling and Analyses22 Table3 Site measurements and isotopic composition of surfa

20、ce waters.Analyses：24 4.Results and discussionPhase 1Phase 2Phase 3Tritium and stable isotopeanalysisHydrochemical characteristicsWater table andTDS change25 Fig.4 The precipitation tritium input from 1952 to 2007 and the decayed value for 2007.The results show a tritium content decrease from 2586 T

21、U (1963) to 2030 TU(2007). Using an exponential decay equation, the decayed tritium contents for 2007 in precipitation, which would represent tritium concentrations in groundwater that had infiltrated between 1952 and 2007, ranges from 50 TU to 225 TU from 1962 to 1966, and ranges from 10 to 35 TU f

22、rom 1957 to 2007 (Fig. 4). Therefore, groundwater with tritium content less than 10 TU is regarded as pre-modern water, or at least most part is pre-modern water when mixing with modern water is considered.Tritium analysis27Fig. 6 The stable isotopes in the water reservoirs in the lower reaches are

23、enriched in heavy isotopes due to evaporation: the Qiala Water Reservoir has the 18O of 4.6 and the Daxihaizi Water Reservoir has the 18O of 3.6 due to extended evaporation. The residual waters collected from the river bed at the Lower Tarim River show 18O from 2.0 to 3.5 and 2H from 17.1 to 5.8, as

24、 a consequence of intensive evaporation.Stable isotope analysis in surface watersFig. 6 Stable isotopic composition for surface waters and groundwaters28The modern and pre-modern groundwaters exhibit a similar behavior to fall in slight parallel to the meteoric water line, but enriched relative to t

25、he recharging river water. The phenomenon is commonly observed in dry climate and attributed to evaporation during river recharge to the riparian groundwater system in a rather uniform manner.Fig. 7 Stable isotopic composition for surface waters and groundwatersStable isotope analysis in groundwater

26、s Fig. 6 Stable isotopic composition for surface waters and groundwaters29piper三線圖以三組生要的陽離子(Ca,Mg,Na和K)和陰離子(C1,S04 ,HCO3和CO3)的每升毫克當(dāng)量的百分?jǐn)?shù)來表示。每圖包括三個部分，在左下方和右下方分別為二張等腰三角形域，中間上方夾著一張菱形域(圖1)，每域的邊長均按100等分讀數(shù)。在左下方的等腰三角形域，三個主要陽離子反應(yīng)值的百分?jǐn)?shù)按三線座標(biāo)用一個單點表示。在右下方的等腰三角形域，陰離子亦用同樣方法表示。這樣，圖上所作的二單點表示了地下水中某些溶解物質(zhì)的相對濃度。然后通過這二個

27、單點平行三角形外邊作射線，于菱形域內(nèi)相交一點。這一點通?？梢哉f明地下水總的化學(xué)性質(zhì)并用陰陽離子對表示地下水的相對成分。Hydrochemical characteristics30The water type conversion from CaMgHCO3SO4 with low TDS in source stream to NaMgClSO4 with high TDS in the lower reaches of the basin and fluoride concentration evolution show the one of the most typical water

28、evolution of arid water system, going along with evaporation and dissolution.Fig. 7 Piper trigraph for surface waters（a） and groundwaters（b）Hydrochemical characteristics（a）（b）31TDS in the groundwater within 600 m to the river bed ranges from 0.8 g/L (E3) to 3.7 g/L. (C1) with an average of 1.6 g/L,

29、except for section I, which is located in the terminal of the water flow and salt with very high TDS. Beyond the distance, TDS in groundwater is also high except for sample G5. Fig. 8 TDS distribution (g/L) in the Lower Tarim RiverHydrochemical characteristics32The strong correlations between Na and

30、 Cl (r = 1.00) and an approximately 1:1 trend (Fig. 9 a) suggest Na and Cl mainly comes from halite. Ca and Mg have strong correlations with SO4 (0.97,1.00) and relatively weak with HCO3 (0.77, 0.84). The equivalent ratios for (Ca + Mg) against HCO3 are more than 1 (Fig. 9b), suggesting that, beside

31、s dissolution of carbonates, dissolution of sulfate (CaXMg (1-X) SO4) contributes the additional (Ca + Mg) when concentration of (Ca + Mg) increases with that of SO4.Such a pattern indicates that saturation of a relevant salt controls the concentration of the respective ions.Fig. 9 Ionic ratio for t

32、he groundwaters.Groundwater saliization mechanism33Fig. 10 shows the chloride concentration in dry soil,appearing to be highly variable. The SP1 has less chloride in the whole profile, ranging from 24 to 862 mg/kg, compared to the SP2 and SP4, which show maximum chloride concentration of 4416 mg/kg

33、(2.052.30 m depth) and 11,925 mg/kg (0.351.00 m depth), respectively.Fig. 10 Moisture and chloride content for the three soil profiles34Fig.11 Water tables and TDS changes at certain groundwater monitoring section in the Lower Tarim River under water diversions35The variations of water tables have t

34、he following characteristics:before the water diversion, the water tables were similar at each section and the flow field was stable; after the water diversion, the water tables rose to different extent. The closer to the river bed, the faster the groundwater table rose. The unstable infiltration ta

35、kes place at river bed, as a result, the high groundwater hydraulic head moves towards both river-sides.Changes of TDS in groundwaters show the following characteristics:TDS in groundwater from sections B and C has increased after the first diversion; after the second and third water diversions,TDS

36、in groundwaters from all sections has decreased. The TDS for samples C7 (w8, 850 m away from the river) tempestuously increased from 4.57 g/L to 22.37 g/L after the fourth water diversion, to 15.32 g/L in August, 2007.Water table and TDS change36Fig. 12 The variation of groundwater table (m) before

37、water diversion and after the eighth water diversion (a) and groundwater depth (m) in the Lower Tarim River (August,2007).The variation of groundwater table between that before water diversion (05/2000) and after the eighth the water diversion (08/ 2007) and the groundwater depth (08/2007) are plott

38、ed in Fig. 15 using the Inverse Distance Weighting Method.4.Results and discussion37The scopes of water tables rise are wider than modern recharge limit, due to water head pressure transfer. Since the vegetation coverage exhibits a continued declining trend with dropping water table and modern water

39、 recharge scope in the area, Niu and Li (2008) concluded there was 7345 hm2 increased vegetation area from 2000 to 2006 after water diversion based on satellite images of the main area where vegetation distributed in the Lower Tarim River. However, the groundwater depth suitable for the growth of P.

40、 euphratica is less than 5 m in the Lower Tarim River, If the target of the ecological restoration is to maintain the vegetation dominated by P. euphratica, the optimal groundwater depth would be less than 5 m. However, the territory with the suitable groundwater depth is narrow, within 200 m from t

41、he river bed and becomes even narrower towards downstream4.Results and discussion381、The isotopic composition of shallow groundwater forms a trend line that is almost in parallel to the GMWL but is enriched in heavy isotopes compared with the recharging river water. This can be attributed to evapora

42、tion during the river recharge to the riparian groundwater system in a rather uniform manner.淺層地下水的同位素組成,形成一個趨勢線,幾乎是平行于GMWL，與河水相比重同位素值更大。歸因于河水補給地下水系統(tǒng)過程間的蒸發(fā)作用。2、Tritium data show that the extent of modern recharge (since 1960) is limited to 600200 m from the river bank with a descending trend towards downstream.氚數(shù)據(jù)顯示,現(xiàn)代(1960年以來)補給的程度是有限的,距離河岸600 - 200米范圍內(nèi)，往下游呈下降趨勢3、Water table has risen after the eight wa