本文選題：三大流域 + 徑流量��； 參考：《華東師范大學(xué)》2016年博士論文

【摘要】：河流通過向海輸送陸源物質(zhì)(如淡水、泥沙及其攜帶的營養(yǎng)物質(zhì))而影響河口、海岸及邊緣海。河流入海水沙通量的變化會導(dǎo)致河口海岸帶鹽度、濁度和地貌過程等的變化,從而對海岸帶功能產(chǎn)生影響。工業(yè)時(shí)期以來,特別是近幾十年來,全球氣候變化顯著,流域人類活動日益增強(qiáng)。在氣候變化和人類活動的雙重影響下,世界上許多河流入海水沙通量發(fā)生急劇變化。然而,由于氣候變化的地域差異以及流域開發(fā)程度的不同,不同河流水沙通量對氣候變化和人類活動的響應(yīng)呈現(xiàn)巨大差異。因此,開展不同流域(特別是大河流域)的相關(guān)對比研究十分必要。黃河、長江和珠江是我國最大的三條河流,也都是世界級大河(三流域合計(jì)占全球陸地總面積的約2%)。這三大流域位于典型的東亞季風(fēng)氣候區(qū)的不同緯度帶,同時(shí)也是我國乃至世界上人類活動最強(qiáng)烈的地區(qū)之一。黃河、長江和珠江入海徑流和泥沙是西太平洋沿岸最主要的淡水和泥沙來源之一。本研究以這三大流域?yàn)檠芯繉ο?基于年和月氣溫、降水量、徑流量、輸沙率系列數(shù)據(jù),采用Mann-Kendall(?)參數(shù)趨勢檢驗(yàn)法,累計(jì)距平法,最大協(xié)方差分析法,克里金插值法以及線性回歸分析等多種數(shù)學(xué)統(tǒng)計(jì)方法,分析1956年有同步系列資料以來我國三大流域的氣溫和降水量變化特征,以及氣候變化和人類活動對三大河流徑流量和輸沙率的影響。主要結(jié)果和結(jié)論如下：(1)黃河、長江、珠江三大流域氣溫和降水量變化。1956-2013年三大流域平均溫度顯著上升,平均升溫速率為0.22℃/10yr,與全球平均升溫速率(0.21℃/10yr)相近。然而,三大流域內(nèi)升溫速率存在明顯空間差異：升溫速率變化范圍為0.05-0.49℃/10yr,它隨著緯度和高程的上升呈增大趨勢,即高升溫速率主要出現(xiàn)在高緯度地區(qū)的黃河流域和高海拔的長江的源頭流域；此外,人口密集和工業(yè)發(fā)達(dá)的特大城市(例如上海)的升溫速率較周邊地區(qū)大。三大流域升溫速率還表現(xiàn)出顯著季節(jié)差異：升溫速率夏季最小(0.14℃/10yr),冬季最大(0.29℃/10yr)。近60年來三大流域升溫過程具有較顯著的階段性：以1987和1998年為轉(zhuǎn)折呈梯級升溫態(tài)勢。1956年以來三大流域平均年降水量的變化趨勢不顯著,但三大流域內(nèi)不同地域的降水量顯示出不同的變化趨勢：即中部(黃河的中下游流域,長江流域的中部地區(qū)以及珠江的西江流域)年降水量呈下降趨勢,而西北(位于青藏高原的黃河和長江西部源頭流域)、東南(長江下游及珠江的東江、北江流域)兩翼年降水量呈上升趨勢。氣溫和降水量變化的綜合分析表明,近60年來三大流域的西北和東南區(qū)域呈現(xiàn)變暖變濕趨勢,而中部區(qū)域有變暖變干趨勢。此外,三大流域降水量具有顯著的年際變化和一定的年代尺度階段性趨勢特征。(2)黃河、長江、珠江三大流域季節(jié)性氣溫和降水量與太平洋、印度洋海表溫度(Sea Surface Temperature:SS T)的年際和年代際共變關(guān)系。三大流域各季節(jié)氣溫的年際變化與SST的El Nino-Southern Oscillation (ENSO)模式變化序列相關(guān)。夏季和秋季三大流域內(nèi)大部分地區(qū)平均溫度與SST的ENSO模式變化序列呈負(fù)相關(guān),但春季和冬季平均溫度變化與SST的ENSO模式變化序列正相關(guān)。三大流域各季節(jié)降水量的年際變化同樣與SST的ENSO模式變化序列相關(guān),但不同季節(jié)降水量對SST變化的局地響應(yīng)不同。例如,SST的ENSO模式變化序列與三大流域東南區(qū)域的冬季降水量呈正相關(guān),但與夏季黃河流域的降水量呈負(fù)相關(guān)。秋季SST的ENSO模式變化序列與長江干流北部流域降水呈負(fù)相關(guān),但與長江干流南部流域降水正相關(guān)。與降水相比,季節(jié)性陸地氣溫對SST年際共變響應(yīng)的空間一致性更顯著。在年代際時(shí)間尺度上,三大流域季節(jié)性降水和氣溫與SST的Pacific Quasi-Decadal Oscillation (QDO)模式變化序列更為相關(guān)。(3)黃河、長江、珠江三大河流徑流量和輸沙率變化。1956-2013年時(shí)段,黃河徑流量呈顯著下降趨勢,珠江、長江徑流量變化趨勢均不顯著；同期三大河流輸沙率均呈顯著下降趨勢。三大河流的徑流量和輸沙率均具有明顯的(但不一定同步的)階段性變化。例如,1964-1997年黃河徑流量和輸沙率均呈顯著下降趨勢；1997-2013年黃河徑流量呈顯著上升趨勢。1998-2011年長江徑流量呈明顯下降趨勢,其它時(shí)段徑流量變化趨勢不明顯；近60年長江輸沙率的顯著下降趨勢主要開始于1984年。1956-1983年珠江徑流量和輸沙率均有上升趨勢,而1994年后二者又呈顯著下降趨勢。(4)子域(subbasin)對黃河、長江、珠江徑流量和輸沙率貢獻(xiàn)的變化。黃河水沙來源存在明顯的區(qū)域性差異,且不同子域產(chǎn)流產(chǎn)沙率隨時(shí)間變化十分顯著。1956年以來大約69%的黃河水量來自上游蘭州站以上流域,而中游流域產(chǎn)沙量約占整個(gè)流域的77%,并為整個(gè)流域貢獻(xiàn)了大約31%的徑流量。但1956年以來(特別是1985年以來)黃河中游流域產(chǎn)流和產(chǎn)沙率均呈顯著下降趨勢：例如,1956-1985年中游產(chǎn)沙量約占整個(gè)流域的86%,而1986年后降至大約68%。長江各子流域徑流量和輸沙率變化趨勢十分復(fù)雜：1956年以來源頭金沙江流域徑流量呈上升趨勢,但輸沙率呈下降趨勢；長江干流以北的岷江、嘉陵江和漢江三個(gè)子流域年徑流量呈下降趨勢(其中岷江徑流量下降趨勢達(dá)到顯著水平),輸沙率均呈顯著下降趨勢；干流以南的烏江、洞庭湖和鄱陽湖三子流域中只有烏江徑流量呈下降趨勢,而鄱陽湖和洞庭湖流域徑流量均呈上升趨勢,干流以南三子流域的輸沙率均呈下降趨勢。三峽工程運(yùn)行前的1956-2002年大約65%的長江泥沙通量來自上游流域,而2003年三峽工程運(yùn)行后大約67%的長江泥沙通量主要來自中下游流域的貢獻(xiàn)(特別是對中游干流河床的侵蝕)。1956-2013年西江對珠江徑流量和輸沙率的貢獻(xiàn)率分別高達(dá)大約77%和89%；近60年來西江、北江、東江年徑流量變化趨勢均不顯著,但輸沙率均呈下降趨勢,其中西江和東江輸沙率下降趨勢達(dá)到顯著水平。(5)氣候變化和人類活動對黃河、長江、珠江水沙通量的影響。氣候變化對三大河流徑流量和輸沙率的影響具有空間和時(shí)間差異：在空間上,降水量變化對相對干旱的黃河流域的水沙通量的影響較之對長江和珠江的影響更為明顯；在時(shí)間上,氣候變化對近60年時(shí)段的水沙通量影響不大,但對年代尺度水沙通量的階段性變化可產(chǎn)生顯著影響。例如,1975-1997年黃河徑流量和輸沙率下降大約20%歸因于降水量的減少。1998-2011年長江徑流量減少大約50%歸因于降水量的減少,另外50%主要?dú)w因于人類活動,而輸沙率的顯著下降只有大約20%歸因于降水減少。1956-1983年珠江徑流量增加主要是降水量增加引起的,降水增加也是輸沙率上升的一個(gè)重要原因；而1994-2013年珠江大約50%的徑流量下降以及20%的輸沙率下降可歸因于同期降水量減少。而氣溫變化對三大流域水沙通量的影響目前很難進(jìn)行量化。本文資料顯示,與降水量變化相比,氣溫變化對三大流域水沙通量變化的貢獻(xiàn)較小。降水量～徑流量以及徑流量～輸沙率雙累積曲線的分析表明,1956年以來三大河流的徑流量和輸沙率除了受到降水量影響外,還受到其它因素的影響(鑒于氣溫變化的影響很小,“其它因素”主要是指人類活動)。人類活動對黃河徑流和輸沙的影響以中游流域最為明顯。雖然人類活動是長江和珠江年徑流量年際變化的次要原因(主要原因是降水量變化),但它是造成三大河流輸沙率顯著下降的主要原因。人類活動對三大河流徑流量和輸沙率的影響隨時(shí)間推移呈顯著增加趨勢。例如,人類活動導(dǎo)致的黃河輸沙率下降比例在1960年代約為21%,而在2000年后達(dá)到89%。人類活動導(dǎo)致的長江輸沙率下降始于1969年(因1968年底漢江上丹江口水庫建成運(yùn)行)；2010-2013年長江輸沙率較氣候決定理論值(指基于1968年以前的降水量～徑流量和徑流量～輸沙率關(guān)系推算的輸沙率)下降了約74%(反映人類活動的影響)。人類活動導(dǎo)致的珠江輸沙率下降始于1990年代,2010-2013年珠江輸沙率較理論值減少了大約66%。在各種人類活動中,水庫建設(shè)是三大流域輸沙率呈階段性下降的主要原因。例如,1969-2013年漢江輸沙率僅為丹江水庫修建前的1956-1968年平均水平的14%。2000年二灘水庫蓄水后金沙江輸沙率較之前下降了約42%；2003年三峽水庫蓄水后長江入海泥沙通量(2003-2013年平均143 Mt/yr)僅為1956-1968年平均水平(512 Mt/yr)的28%。1997年珠江西江干流天生橋水庫以及2006年龍灘水庫蓄水后(2007-2013年)西江輸沙率僅為之前(1956-1996年)的23%(大約減少了55 Mt/yr)。流域土地利用強(qiáng)度的改變也對三大河流的水沙通量特別是輸沙率產(chǎn)生了重要影響。例如,到1980s黃河流域水土保持措施才有效發(fā)揮作用,使黃河輸沙率出現(xiàn)明顯下降趨勢。1980s以前,隨著長江流域人口增加、耕種面積擴(kuò)大,地表侵蝕加強(qiáng),流域產(chǎn)沙率呈增加趨勢,但之后隨著“長治工程”(長江流域水土流失治理工程)的逐步實(shí)施,流域產(chǎn)沙率呈下降趨勢。1980s前珠江流域大規(guī)模的毀林開荒使水土流失加劇超過水庫蓄水的影響,因此輸沙率較理論值偏大；但1990s后隨著各級水庫的運(yùn)行和水土保持措施的實(shí)施,輸沙率又下降了。此外,隨著流域人口增加和社會經(jīng)濟(jì)發(fā)展,工農(nóng)業(yè)用水需求也急劇增加,引水調(diào)水不斷加強(qiáng),因此流域耗水增多也對徑流量產(chǎn)生了一定影響。例如,2012年黃河全流域地表水耗水量(地表水取水量扣除其回歸到黃河干、支流河道后的水量)為32×109m3,甚至高于當(dāng)年黃河的入海徑流量(28×109m3)；同年珠江流域耗水量(36×109m3)約占珠江年徑流量的13%；長江流域同年耗水量占長江年徑流量的8%。但由于其它因素作用(如蒸發(fā)量減少、部分流域水土流失加重、地下水補(bǔ)充),使多種因素共同影響下的長江和珠江徑流量大小仍表現(xiàn)為主要取決于流域降水量。人類活動還對三大河流年徑流量和輸沙率的季節(jié)性分配產(chǎn)生了重要影響。近年來三大河流徑流和輸沙的洪枯季差異明顯縮小。例如,1986年龍羊峽水庫和1999年小浪底水庫蓄水后,黃河夏季徑流量和輸沙率急劇下降。1956-1959年(相對自然狀態(tài)時(shí)期)黃河最大月(8月)與最小月(1月)徑流量多年平均值比值為11：1,而2002-2013年(受到人類活動顯著影響后)最大月(7月)與最小月(4月)徑流量多年平均值比值為7：1；1956-1959年黃河最大月(8月)與最小月(1月)輸沙率多年平均值比值為495：1,而2002年后最大月(7月)與最小月(2月)輸沙率多年平均值比值僅為71：1。三峽水庫蓄水前(1956-2002年)長江最大月(7月)與最小月(1月)輸沙率多年平均值比值為42：1,而2003年后長江最大月(7月)與最小月(2月)輸沙率多年平均值比值僅為11：1。1956-1979年(相對自然狀態(tài)時(shí)期)珠江最大月(7月)與最小月(12月)輸沙率多年平均值比值為109：1,而2006年龍灘水庫蓄水后珠江最大月(6月)與最小月(2月)輸沙率多年平均值比值為54：1�？傮w上,相比于長江和珠江,黃河水沙通量對氣候變化或人類活動的影響更為敏感,反映黃河的脆弱性更高。這與黃河流域降水量較少、下墊面黃土發(fā)育等特點(diǎn)有關(guān)。此外,人類活動對研究區(qū)北部河流徑流和輸沙的影響程度較南部河流也更明顯。
[Abstract]:Rivers can affect estuaries, coastal and marginal seas by transporting land sources (such as fresh water, sediment and their nutrients). Changes in water and sand fluxes from rivers to the sea lead to changes in salinity, turbidity, and geomorphic processes in the estuarine and coastal zones. The climate change and human activity are increasing. Under the dual influence of climate change and human activity, many rivers in the world have a sharp change in the amount of water and sand in the sea. However, the response of different rivers and rivers to climate change and human activity due to the regional difference of climate change and the difference of the development degree of the river basin There are great differences. Therefore, it is necessary to carry out a comparative study of different basins (especially the great river basins). The Yellow River, the Yangtze River and the Pearl River are the largest three rivers in our country, and are also the world-class rivers (the total of the three basins are about 2% of the total land area in the world). The three stream regions are located at different latitudes of the typical East Asian monsoon climate zones, It is also one of the most intense areas of human activity in China and in the world. The Yellow River, the Yangtze River and the Pearl River are one of the most important sources of fresh water and sediment in the Western Pacific coast. This study is based on the annual and monthly temperature, precipitation, runoff and sediment transport rate based on the three major basins, using Mann-Kendall (?) parameter trend test, cumulative anomaly method, maximum covariance analysis, Kriging interpolation and linear regression analysis, and other mathematical statistics, analysis of the changes in temperature and precipitation in the three major basins of China since 1956, as well as the change of air weather and human activities to the three river flow and sediment transport rate. The main results and conclusions are as follows: (1) the temperature and precipitation in the three major basins of the Yellow River, the Yangtze River and the Pearl River have increased significantly in the three large basins in.1956-2013, and the average heating rate is 0.22 /10yr, which is similar to the global average heating rate (0.21 C /10yr). However, there are obvious spatial differences in the temperature rising rate in the three big basins: heating up The range of rate variation is 0.05-0.49 C /10yr, which increases with the rise of latitude and elevation, that is, the rising temperature rate is mainly in the the Yellow River basin of high latitudes and the source basin of the high elevation of the Yangtze River; in addition, the heating rate of densely populated and industrial megacities (such as Shanghai) is larger than that in the surrounding area. The three big basins are more than those in the surrounding areas. The heating rate also showed significant seasonal differences: the heating rate was minimum in summer (0.14 /10yr) and the maximum in winter (0.29 /10yr). The warming process of the three big basins in the last 60 years had a significant stage characteristics: the turning of the 1987 and 1998 was a cascade rising trend, and the average annual precipitation of the three big basins since.1956 was not significant, but three The precipitation in different regions of the large basin shows a different trend of change: that is, the annual precipitation in the middle and lower reaches of the Yellow River, the middle of the Yangtze River Basin and the Xijiang River Basin of the Pearl River is declining, while the Northwest (located in the the Yellow River of the Qinghai Tibet Plateau and the source basin in the west of the Yangtze River), and the Southeast (the lower reaches of the Yangtze River and the Pearl River, the North River) The annual precipitation on the two wings showed an upward trend. The comprehensive analysis of the changes in temperature and precipitation showed that the northwest and southeastern regions of the three big basins in the last 60 years showed a warming and wetting trend, while the central region had a warming and dry trend. In addition, the precipitation in the three large basins had significant annual changes and a certain trend characteristic of a certain age scale. (2 The interannual and interdecadal covariance relationship between the seasonal temperature and precipitation of the three big basins in the the Yellow River, the Yangtze River and the Pearl River and the India ocean sea surface temperature (Sea Surface Temperature:SS T). The interannual variation of the temperature in each season of the three big basins is related to the El Nino-Southern Oscillation (ENSO) model variation sequence of SST. In the summer and autumn, the three major basins in the autumn are in the middle. The average temperature in most areas is negatively correlated with the ENSO pattern variation sequence of SST, but the change of the average temperature in spring and winter is positively related to the ENSO model variation sequence of SST. The interannual variation of the precipitation in the three large basins is also related to the ENSO model variation sequence of SST, but the local response of the different seasonal precipitation to the SST changes is different. For example, the ENSO pattern change sequence of SST is positively correlated with the winter precipitation in the southeast region of the three major basins, but negatively related to the precipitation in the the Yellow River basin in summer. The ENSO model variation sequence of the autumn SST is negatively correlated with the precipitation in the northern watershed of the Yangtze River, but it is positively related to the precipitation in the southern watershed of the Yangtze River. The spatial consistency of the interannual covariant response of SST is more significant. On the interdecadal time scale, the seasonal precipitation and temperature of the three large basins are more related to the Pacific Quasi-Decadal Oscillation (QDO) model variation sequence of SST. (3) the runoff volume and sediment transport rate of the three rivers in the Yellow River, the Yangtze River and the Pearl River change in the.1956-2013 year period, and the runoff of the three rivers in the Yangtze River The trend of the runoff in the Pearl River and the Yangtze River is not significant, and the sediment transport rate of the three rivers in the same period has a significant downward trend. The runoff and sediment transport rate of the three rivers have obvious (but not necessarily synchronous) stage changes. For example, the runoff and sediment transport rate in the 1964-1997 years of the Yellow River both have a significant downward trend; 1997-2013 years. The runoff of the Yellow River has a significant upward trend in.1998-2011 years, and the runoff of the Yangtze River shows a significant downward trend. The trend of the runoff in other periods is not obvious. The significant decline trend of the sediment transport rate in the last 60 years is mainly in the Pearl River Runoff and sediment transport rate in the year.1956-1983 in 1984, while the two after 1994 showed a significant downward trend. (4) changes in the contribution of Zi Yu (subbasin) to the Yellow River, the Yangtze River, the Pearl River Runoff and the sediment transport rate. There are obvious regional differences in the source of water and sediment in the Yellow River, and the different Zi Yu yield and sediment rates vary with time. The amount of water in the Yellow River is about 69% from the upper reaches of the LanZhou Railway Station, and the sediment yield in the middle reaches of the whole stream is about the whole stream. 77% of the region has contributed about 31% of the runoff to the whole river basin, but the rate of runoff and sediment yield in the middle reaches of the Yellow River since 1956 (especially since 1985) has decreased significantly: for example, the sediment yield in the middle reaches of the 1956-1985 year is about 86% of the whole River Basin, and the runoff and sediment transport rate in the Yangtze River Basin of about 68%. after 1986 has decreased. The trend is very complicated: since 1956, the runoff of the Jinsha River basin is on the rise, but the rate of sediment transport is declining. The annual runoff of the three sub basins in the north of the Yangtze River, the Jialing River and the Hanjiang River shows a downward trend (in which the decrease trend of the Minjiang River Runoff reaches a significant level), the sediment transport rate has a significant downward trend, and the main stream is south. In the three sub basins of Wujiang, Dongting Lake and Poyang Lake, only the runoff of Wujiang is declining, while the runoff of Poyang Lake and Dongting Lake is on the rise, and the sediment transport rate of the three sub basins in the south of the main stream is decreasing. The sediment flux of the Yangtze River in the 1956-2002 year of the Three Gorges project comes from the upstream river basin, and the Three Gorges of the Three Gorges in 2003. About 67% of the Yangtze River sediment flux mainly comes from the contribution of the middle and lower reaches of the Yangtze River after the project operation (especially the erosion of the middle stream river bed). The contribution rate of the Xijiang River to the Pearl River Runoff and sediment transport rate is up to 77% and 89% respectively in.1956-2013. The Annual Runoff Trend of the West River, the North River and the Dongjiang River is not significant in the last 60 years, but the sediment transport rate is all present The decline trend is significant. (5) the influence of climate change and human activity on the water and sediment flux of the Yellow River, Yangtze River and Pearl River. The effect of climate change on the flow and sediment rate of three rivers has spatial and temporal differences: in space, the change of precipitation to the relatively arid the Yellow River Basin The effect of water and sediment flux is more obvious than that on the Yangtze River and the Pearl River; in time, the impact of climate change on the water and sediment flux in the last 60 years is not significant, but it has a significant influence on the phased changes of the water and sediment flux in the age scale. For example, the decrease of the Yellow River's runoff and sediment transport rate in 1975-1997 years is about 20% due to the decrease of.1 The decrease of the runoff of the Yangtze River by about 50% in the past 998-2011 years is attributable to the decrease of precipitation, and the other 50% mainly attributable to human activities. The significant decrease in sediment transport rate is only about 20% attributable to the decrease of precipitation in.1956-1983. The increase of the Pearl River runoff is mainly caused by the increase of precipitation, and the increase of precipitation is also an important reason for the increase of sediment transport rate; and 19 The decrease of about 50% of the Pearl River in 94-2013 years and the decrease of 20% of the sediment transport rate can be attributed to the decrease of the precipitation in the same period. The influence of the temperature change on the water and sediment flux of the three large basins is difficult to quantify. The analysis of the double cumulative curve of runoff and runoff and sediment transport rate shows that the runoff and sediment transport rate of the three rivers have been influenced by other factors in addition to the amount of precipitation since 1956. (in view of the small influence of temperature change, the other factors "mainly refers to human activities). The effect of human activities on runoff and sediment transport in the Yellow River Although the human activity is the secondary cause of annual variation in the annual runoff of the Yangtze River and the Pearl River (mainly due to the change of precipitation), it is the main cause of the significant decrease in the sediment transport rate of the three rivers. The influence of human activity on the flow rate and sediment transport rate of the three rivers is significantly increased with time. For example, the decline ratio of the Yellow River's sediment transport rate caused by human activities was about 21% in 1960s, and the decline of the Yangtze River sediment transport rate caused by 89%. human activities in 2000 began in 1969 (due to the completion of the Danjiangkou reservoir on the Han River on the Hanjiang River at the end of 1968); the 2010-2013 year sediment rate of the Yangtze River determined the theoretical value (based on the precipitation before 1968). The calculated sediment transport rate decreased by about 74% (reflecting the influence of human activity). The decline of the Pearl River transport rate caused by human activities began in 1990s, and the Pearl River transport rate in the 2010-2013 year was reduced by about 66%. in all kinds of human activities, and the construction of the reservoir is a stage of sediment transport in the three major basins. For example, in the 1969-2013 year, the rate of sediment transport in the Han River in 1969-2013 years was only 42% after the storage of the two beach reservoir at the average level of 1956-1968 years before the construction of the Danjiang Reservoir in 14%.2000, and the sediment flux of the Yangtze River to the sea (2003-2013 year average 143 Mt/yr) was only 1956-1968 years average after the water storage of the Three Gorges Reservoir in 2003. 512 Mt/yr) in 28%.1997, the sediment transport rate of the Xijiang River, the main stream of the Pearl River in the Pearl River and the Longtan Reservoir in 2006 (2007-2013 years), is only 23% (about 55 Mt/yr) of the previous (1956-1996 years). The change of the land use intensity of the river basin also has an important effect on the water sand flow rate, especially the sediment transport rate of the three major rivers. For example, to 1980s The measures of soil and water conservation in the the Yellow River basin have played an effective role, and before the obvious downward trend of the sediment transport rate in the Yellow River is.1980s, with the increase of the population of the Yangtze River Basin, the area of cultivated land is enlarged, the erosion of the surface is strengthened and the sediment yield in the river basin is increasing, but after the gradual implementation of the "Changzhi project" (the water and soil erosion control project of the Yangtze River Basin), the flow of soil and water is gradually carried out. The rate of sand production in the region shows a downward trend of.1980s before the large scale of deforestation in the Pearl River Basin, which makes the soil erosion aggravate the influence of the reservoir water storage, so the rate of sediment transport is larger than that of the theoretical value. But after the implementation of the operation of the reservoirs at all levels and the implementation of the soil and water conservation measures, the rate of sediment transport has declined again. The demand for water use in industry and agriculture has also increased rapidly, and the water diversion of water diversion has been strengthened continuously. Therefore, the increase of water consumption in the basin also has a certain effect on the runoff. For example, in 2012, the water consumption of the surface water of the whole basin of the Yellow River (the surface water quantity of the surface water is deducted to the the Yellow River dry, the water amount after the tributary channel) is 32 x 109m3, even higher than the runoff from the Yellow River in the same year. Volume (28 * 109m3); in the same year, the Pearl River Basin water consumption (36 * 109m3) accounted for 13% of the annual runoff of the Pearl River; the Yangtze River Basin consumed the same amount of water in the same year as the Yangtze River.

【學(xué)位授予單位】：華東師范大學(xué)
【學(xué)位級別】：博士
【學(xué)位授予年份】：2016
【分類號】：P467;TV143
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本文編號：1886555