effects of human activities on the yangtze river
S.L. Yang, Z. Shi, H.Y . Zhao 1
, P
. Li, S.B. Dai and A. Gao
我的回忆不是我的
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Hydrology and Earth System Sciences, 8(6), 1210 1216  (2004)    ©  EGU Research Note:
Effects of  human activities on the Yangtze River suspended sediment flux into the estuary in the last century
S.L. Yang 1, Z. Shi 2, H.Y. Zhao 1, P. Li 1, S.B. Dai 1 and A. Gao 1
1State Key Lab of Estuarine and Coastal Research, East China Normal University, Shanghai 200062, China
2
School of Naval Architecture, Ocean and Civil Engineering, Shanghai Jiaotong University, 1954 Huashan Road, Shanghai 200030, China
E-mail for corresponding author: u.edu; shilunyang@hotmail
Abstract
The surface erosion area in the Yangtze River basin increased from 364×103 km 2 in the 1950s to 707×103 km 2 in 2001 due to a great increase in population. Based on the regression relationship between surface erosion area and population, the surface erosion area was predicted to be about 28
0×103 km 2 at the beginning of the 20th  century. The sediment yield, which increased by about 30% during the first six decades of the 20th  century, was closely related to the surface erosion area in this river basin. The Yangtze annual suspended sediment flux into the estuary was about 395×106 t a -1 at the beginning of the century, and this gradually increased to an average of 509×106 t a -1 in the 1960s. The increase in the suspended sediment flux into the estuary was accelerated in the 1950s and the 1960s due to the rapid increase in population and land use immediately after the Second World War and the Liberation War. After the riverine suspended sediment flux reached its maximum in the 1960s, it decreased to <206×106 t a -1 in 2003. Construction of dams was found to be the principal cause for this decreasing trend because,during the same period, (a) the riverine water discharge did not show a decreasing trend, (b) water diversion was not influential and (c)sedimentation in lakes and canals of the middle and lower reaches did not increase. The total storage capacity of reservoirs has increased dramatically over the past half century. The amount of sediment trapped in reservoirs has increased to more than half a billion t a -1. As a result, the suspended sediment flux into the estuary dramatically decreased, even though the sediment yield from many areas of the basin increased in recent decades. Human activities gradually increased the suspended sediment flux into the estuary before the 1960s and then rapidly decreased it. The last century was a period when the Yangtze suspended sediment flux into the estuary was dramatically affected by human activities.
Keywords: riverine sediment flux, human activities, surface erosion, dam, Yangtze (Changjiang) River
Introduction
Riverine sediment flux into an estuary usually governs the 100~102 year evolution of deltas (Innocenti and Pranzini,1993; Fanos, 1995; Guillen and Palanques, 1997; Barusseau et al ., 1998; Stanley and Warne, 1998; Carriquiry and Sánchez, 1999; Ly, 1980; Panin and Jipa, 2002; Yang  et al .,2003a). It also affects short-term sediment transport in the estuarine and coastal areas (Yang  et al ., 2003b; Shi, 2004).Human activities have strongly influenced the riverine sediment supply to the estuary in many rivers during the 19th and 20th centuries (Guillen and Palanques, 1997;Trenhaile, 1997; Walling, 1999; Milliman, 2001). Compared with the scientific knowledge of many rivers such as the Nile in Egypt (Fanos, 1995; Stanley and Warne, 1998), the Ebro in Spain (Guillen and Palanques, 1997; Sanchez-Arcilla  et al., 1998), the Mississippi (Coleman et al., 1998)and the Colorado River in USA (Carriquiry and Sánchez,1999), the Niger River in Niger (Abam, 1999), the Senegal River in Senegal (Barusseau et al ., 1998), the Yellow River in China (Yang et al ., 1998), and the V olta River in Ghana (Ly, 1980), less is known of the Yangtze (Changjiang),especially in terms of its history before the 1950s. The measurement of sediment flux in the Yangtze River began
in the 1950s. Although the recent decrease in Yangtze River suspended sediment load has preliminarily been revealed and related to human activities (Yang et al ., 2002), further studies are needed. The primary objective of this paper is to examine the effects of human activities on the Yangtze River
Effects of human activities on the Yangtze River suspended sediment flux into the estuary in the last century
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suspended sediment flux into the estuary in the last century.
Physical settings and data collection
The Yangtze originates from the Tibetan Plateau at an elevation of more than 5000 m. It flows eastward for 6300km before entering the East China Sea. Its catchment covers an area of 1.94×106 km 2 and currently has a population of about 400 million. Its mean annual water flux is 908×109m 3(1950 2003) and its annual suspended sediment flux is 422×106 (1951 2003). The mean annual precipitation and evapotranspiration for the basin are 1000 1400 mm and 700 800 mm respectively (Shen, 1986). The Yangtze ranks third in the world in length (Wang and Zhu, 1994), ninth in catchment area (Chen and Gupta, 2001), fourth in sediment flux and fifth in water flux (Eisma, 1998), and probably ranks first for population. The upper reaches of the river end at Yichang, 1840 km away from the estuary. The bed level of the main stream at Yichang is about 60m above the estuary, suggesting that the gradient of the trunk stream is more than one magnitude order higher in the upper reaches than in the middle and lower reaches. The upper reaches account for 52% of the catchment area. There are many lakes scattered throughout the middle and lower reaches. Among t
hem, Lake Dongting and Lake Poyang are the two largest.These lakes, especially Lake Dongting, act as sinks for riverine sediment. The tidal limit of the Yangtze estuary is
at Datong. Datong accounts for 93% of the catchment area (Fig. 1). The water and sediment fluxes at Datong are 2.04and 0.86 times that at Yichang respectively (Yang et al .,2002).
Data on water and sediment fluxes for the river were provided by the Yangtze River Water Conservancy Committee, Ministry of Water Conservancy of China. Data for population, surface erosion area and sediment yield were derived from different sources in the literature. SPSS software was employed for regression analysis.
Results and discussions
THE TIME SERIES OF ANNUAL DISCHARGE
Annual discharge was measured in 1923 1924, 1930, 1935 1937, 1948 and since 1950 at the Datong Hydrological Station. Annual discharge was therefore not available for most of the first half of the 20th century. Fortunately, annual flow discharges has been measured since 1865 at the Hankou Hydrological Station where the Hanjiang River flows into the trunk stream (Fig. 1) of the Yangtze. Alt
hough Hankou is about 500 km upstream from Datong, its annual flow is significantly correlated with the annual flow at Datong (r=0.95 P <0.001). Thus the missing annual flow discharges for Datong could be estimated by utilizing the regression
relationship for annual flow between Hankou and Datong.
Fig. 2. The Yangtze River basin in China.
S.L. Yang, Z. Shi, H.Y . Zhao 1, P . Li, S.B. Dai and A. Gao
曲高和寡的意思
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A time series of annual flow discharge at Datong was reconstructed for the whole 20th century (Fig.
2). According to this time series, the annual flow discharge increased by 1.5% from 1900 to 1949.
INCREASE IN SEDIMENT FLUX DUE TO
DEFORESTATION FROM THE 1900S TO THE 1960S
The surface erosion area in the Yangtze catchment has nearly doubled over the past five decades. The surface erosion area was estimated to be 364×103 km 2 in the 1950s (Shi, 1999;Zhang and Zhu, 2001) and 707×103 km 2 in 2001(CRWCCWCMC, 2002). The increase in surface erosion area is attributed to the increase in population. The population of the river basin was 178 million in 1949 and increased to nearly 400 million in 2001(Zhang, 2000).Assuming that 364×103 km 2 represents the surface erosion area in the mid-1950s and the increase in surface erosion was proportional to the increase in population from 1949 to 2001, the surface erosion area was estimated to be about
319×103 km 2
in 1949, and the relationship between surface erosion area (A) and population (P) is              A = 0.001748P + 9701
(1)
接受的近义词
where A represents surface erosion area in km 2 and P population. The surface erosion area at the beginning of the 20th century is estimated to be about 280×103 km 2, because the population at that time was 155 million.
Although the sediment yields measured for the gauging stations within the basin are highly variable because of natural diversity in the catchment, this variability is reduced when the data are integrated (Lu and Higgitt, 1999).Averaged over the basin, the sediment yield was 3980t km  2a  1 (Table 1). The coefficient of the independent variable A in the regression equation in Fig. 3 suggests a similar sediment yield. The very good correlation shown in Fig. 3 suggests that the differences in sediment yield among the subcatchments are very low. The total surface erosion area in Table 2 and Fig. 3 amounts to 81% of the whole
10000
15000
20000250003000035000400004500019001910
1920
1930194019501960
压强单位换算1970
1980
兼职在家可做
1990
2000
Calendar year
W a t e r  d i s c h a r g e  (m 3/s )
Fig. 1. Annual flow discharges at Datong (observed in 1923 1924, 1930, 1935 1937, 1948 and since 1950; data for the missing years were
exo个性签名estimated using the regression between flows at Datong and Hankou.
Table 1. Distribution of area of surface erosion and sediment yield among different intensity types in the Yangtze River basin in 1985(based on Shi, 1998)Intensity types of
Sediment yield rate Area of surface erosion Annual sediment yield surface erosion
surface erosion (t/km 2·a)(t km  2a  1)(103 km 2)
(106 t)
Very low-grade 500-2 500210247Low-grade    2 500-5 000190658Middle-grade    5 000-8 000103652High-grade 8 000-13 50040.8417Very high-grade >13 50018.6265Total
3980
562
2239
Effects of human activities on the Yangtze River suspended sediment flux into the estuary in the last century
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01002003004005006000
306090120
150
Area of surface erosion (103
km 2)
A n n u a l  s e d i m e n t  Y i e l d  (106 t )
Fig. 3. Regression between area of surface erosion (A) and annual
sediment yield (Y) (data in Table 2).
Table 2.  Area of surface erosion and sediment yield in subcatchments of the Yangtze in 1985Subcatchments
Area of surface Annual sediment yield Data sources
erosion  (103km 2)(106 t)
Jinshajiang R.135.4557.4Shi, 1999Jialinjiang R.92.5397Shi, 1999Hanjiang R.61.0250He, 1997Minjiang R.
49.2215Shi, 1999
Four rivers into Lake Dongting 45.3180Zhang et al ., 1999Zhang and Zhu, 2001Five rivers into Lake Poyang 35.2155Zhang et al ., 1999Tuojiang R.16.384.1Shi, 1999Wujiang R.14.695.4Shi, 1999Chishuihe R.  3.8623.6Shi, 1999
Total
453.4
1958
catchment. In Anhui Province around Datong in the lower reaches where the surface erosion area was 33.6×103 km 2(6.0% of the total catchment area), the sediment yield rate,2054 t km  2a  1 on average, was lower than those in Table 2and Fig. 3 (Zhang et al ., 1999). On the other hand, in the Three Gorges region where the surface erosion area was 34.6×103 km 2 (6.2% of the total catchment), the sediment yield rate, 5780 t km  2a  1 on average, was higher than those in Table 2 and Fig. 3. Because the surface erosion area in these two regions was only 12% of the total, the spatial variation in sediment yield rate was assumed to be low. In view of this, the regional difference in sediment yield was ignored when predicting the sediment yield before the 1950s.There will be a  natural  background sediment yield in the
catchment. Table 1 suggests that surface erosion  is defined as an area where sediment yield rate is >500 t km  2a  1. In other words, the sediment yield rate is < 500t km  2a  1 in the rest of the catchment. In the Yangtze catchment, the annual sediment yield on forestland was found to be 6 t k
m  2(Li et al ., 2002). The forest cover in the Yangtze catchment was 60 80% in the distant past and decreased to 22% in 1957 and 10% in 1986 (Zhang and Zhu, 2001). Assuming (a) the forest cover was 30% in 1900 and 25% in 1949 and (b) the average sediment yield for the remaining uncleared land is 300 t km  2a  1, the average sediment yield for the uncleared land in the basin was 196 t km  2a  1 in 1900, 211t km 2a  1 in 1949 and 219 t km  2a  1 in the 1950s, which was comparable to the corresponding sediment yield in the United States (Langbein and Schumm, 1958). Based on the above assumption and using the catchment area above Datong Hydrological Station (1.81×106 km 2), the annual sediment yield would be 196×(1810000 280000)+3980×280000=1.414×109 t in 1900, 211×(1810000 319 000) +3980×319 000=1.584×109 t in 1949, and 219×(1810000 364000)+3980×364000 =1.765×109 t in the 1950s.
Only part of the sediment derived from surface erosion enters the river system, including waterways, lakes and reservoirs. The sediment entering the river system either flows into the estuary or settles down in the river system.To estimate the missing sediment flux into the estuary before the 1950s, the amount of sediment entering the river system and the amount of sediment deposited in the river system need to be known. In the 1950s, the sediment flux into the estuary was 466×106 t a -1 and the deposition in lakes and river channels was 195×106 t a -1, on average, and deposition in reservo
irs can be effectively ignored because few dams had been constructed by then (Zhu, 2000). Therefore, the
S.L. Yang, Z. Shi, H.Y . Zhao 1, P . Li, S.B. Dai and A. Gao 1214
ratio of the sediment entering the river system to the sediment yield was (466×106 t +195×106 t) /1.765×109t =0.374, which is similar to the ratio of 0.34 from Zhu (2000). This ratio can be expected to be sensitive to changing land use. However, taking the whole catchment, the different land uses can be expected to change nearly proportionally with the total surface erosion area, and the influence on the ratio is expected to be limited. Using a ratio of 0.36, the average of this study and that of Zhu (2000), the sediment entering the river system was predicted to be 509×106 t in 1900 and 570×106 t in 1949.
The lakes and channels in the middle and lower reaches acted as an adjustor for the riverine sediment. The greater the amount of sediment supplied to them, the higher the deposition rate. The deposition was 195, 108 and y
0×106t a  1 when the sediment supplied to them was 661, 510 and y
300×106 t a  1, respectively (unpublished data of the authors), which suggests a regression equation D=0.5385S  163, r 2=0.999, P <0.001, where D (106 t a  1) is the deposition rate and S (106 t a  1) is sediment supply, respectively.According to this equation, the deposition was 111×106 t in 1900 and 144×106 t in 1949. Thus, the suspended sediment flux into the estuary was about 398×106 t a  1 in 1900 and 426×106 t a  1 in 1949, if the influence of water discharge is not considered.
In natural river systems, sediment flux is positively correlated to flow discharge (Chernicoff and Venkatakrishnan, 1995). Taking the 1.5% increase of flow discharge into account, the suspended sediment flux was predicted to be 395×106 t a -1 in 1900 and 429 in 1949,respectively. Assuming that the suspended sediment flux increased progressively from 1900 to 1949, the decadal suspended sediment flux would be as shown in Fig. 4. The sharp increase in annual sediment flux in the 1950s
(466×106 t a  1) and in the 1960s (509×106 t a  1) was likely caused by the population boom after the Second World War and the Liberation War which ended in 1949.
DECREASE IN SEDIMENT FLUX DUE TO DAM CONSTRUCTIONS SINCE THE 1970S
Dam construction in the Yangtze River basin began to flourish in the late 1950s, much later than on r
ivers of other countries such as the Nile (Fanos, 1995; Stanley and Warne,1998), the Ebro (Guillen and Palanques, 1997) and the Colorado (Carriquiry and Sánchez, 1999). Up to now, nearly 50000 dams have been constructed in the Yangtze River basin. Along with the rapid increase in the cumulative reservoir storage capacity, more and more riverine sediment was trapped in the reservoirs. For example, in the upper reaches (upstream from Yichang), the total amount of deposition in reservoirs was 2.85 and 19.1×106 t a  1 in the 1950s and the 1960s, respectively. The largest reservoir put into operation in the 20th century, the Danjiangkou Reservoir (Fig. 1), with a storage capacity of 17.45×109m 3began to impound water in 1959. From 1960 to 1994,1.41×109 m 3 of sediment was trapped by this reservoir (www.cjh, 2003), giving a mean depositional rate 53.3×106 t a  1
The total storage capacity of these reservoirs amounted to approximately 200×109 m 3 by the end of 2003. This represents 22% of the annual flow discharge into the estuary.The total amount of sediment trapped by the reservoirs was positively related to the total storage capacity (Fig. 5).Annual suspended sediment flux into the estuary has shown a significant decrease since the late 1960s (Fig. 6). Annual suspended sediment flux in the 1990s, 343×106 t a  1, was one-third lower than the annual suspended sediment flux in
250
300350400450500550
1900s 1910s 1920s 1930s 1940s 1950s 1960s 1970s 1980s 1990s
Decades
S e d i m e n t  f l u x  (106 t /a )
Fig. 4. Decadal suspended sediment flux into the estuary.

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