the effect of climate change on water in china
DESCRIPTION
The effect of climate change on water in China. Reporter ： Yongjian Ding. Contributors ： S. Liu, B. Ye, L. Zhao, Q. Zhao, Z. Wang, G. Yang. State Key Laboratory of Cryospheric Sciences Cold and Arid Regions Environmental and Engineering Research Institute, CAS. 21. Jun. 2011, Tehran. - PowerPoint PPT PresentationTRANSCRIPT
The effect of climate change on water in China
Reporter ： Yongjian Ding
21. Jun. 2011, Tehran
Contributors： S. Liu, B. Ye, L. Zhao, Q. Zhao, Z. Wang, G. Yang
State Key Laboratory of Cryospheric Sciences
Cold and Arid Regions Environmental and Engineering Research Institute, CAS
1. Climate change and hydrological regime
2. The effect of Cryosphere change
3. Management for water resources and ecosystem in West China
Annual discharge in main rivers over China during 1951-2008
The most river show discharge decrease except for Xinjiang region, Yaluzangbu and downstream of Yangtze River
资料收集中
y = 5. 8981x - 8855
R2 = 0. 0752
2,000
2,200
2,400
2,600
2,800
3,000
3,200
3,400
3,600
1950 1960 1970 1980 1990 2000
(m年平均流量
3 /s)
新疆总量
y = -1.5181x + 3637. 3
R2 = 0.0171
200
300
400
500
600
700
800
900
1,000
1,100
1950 1960 1970 1980 1990 2000
(m年平均流量
3 /s)
唐乃亥
y = -16.362x + 33484
R2 = 0. 3681
200
700
1, 200
1, 700
2, 200
2, 700
1950 1960 1970 1980 1990 2000
(m年平均流量
3 /s)
三门峡
y = 6.0626x + 16516
R2 = 0. 0006
15, 000
20, 000
25, 000
30, 000
35, 000
40, 000
45, 000
1950 1960 1970 1980 1990 2000
(m年平均流量
3 /s)
大通
y = -2.5902x + 5595. 7
R2 = 0.0421
200
300
400
500
600
700
800
1950 1960 1970 1980 1990 2000
(m年平均流量
3 /s)
昌都
y = 0.2714x + 7314
R2 = 2E-06
3,000
5,000
7,000
9,000
11,000
13,000
15,000
1950 1960 1970 1980 1990 2000
(m年平均流量
3 /s)
奴下
y = -14.674x + 42749
R2 = 0.0283
10,000
11,000
12,000
13,000
14,000
15,000
16,000
17,000
18,000
19,000
1950 1960 1970 1980 1990 2000
(m年平均流量
3 /s)
宜昌 y = -8. 941x + 40243
R2 = 0.0028
15,000
17,000
19,000
21,000
23,000
25,000
27,000
29,000
31,000
33,000
1950 1960 1970 1980 1990 2000
(m年平均流量
3 /s)
汉口
y = -27.66x + 55700
R2 = 0.5247
0
500
1,000
1,500
2,000
2,500
3,000
3,500
1950 1960 1970 1980 1990 2000
(m年平均流量
3 /s)
利津
y = - 3. 303x + 7203. 8
R2 = 0. 0267
0
500
1, 000
1, 500
2, 000
1950 1960 1970 1980 1990 2000
(m年平均流量
3/s
) 江桥y = - 9. 0332x + 19217
R2 = 0. 089
0
500
1, 000
1, 500
2, 000
2, 500
3, 000
1950 1960 1970 1980 1990 2000
(m年平均流量
3/s
) 哈尔滨
0
10
20
30
40
50
60
70
80
1950 1960 1970 1980 1990 2000
(m年平均流量
3 /s)
杂木寺
莺落峡
昌马堡
y = - 1. 9976x + 4049. 1
R2 = 0. 2118
0
50
100
150
200
250
300
350
1950 1960 1970 1980 1990 2000
(m年平均流量
3/s
)
铁岭
y = -0. 7206x + 1440.8
R2 = 0. 7199
-10
0
10
20
30
40
50
60
1950 1960 1970 1980 1990 2000
(m年平均流量
3 /s)
石闸里
y = -1. 2941x + 2590.3
R2 = 0. 43440
20
40
60
80
100
120
140
160
1950 1960 1970 1980 1990 2000
(m年平均流量
3 /s)
观台
y = -0.4705x + 1222. 4
R2 = 0.0017
0
100
200
300
400
500
600
700
800
1950 1960 1970 1980 1990 2000
(m年平均流量
3 /s)
王家坝
y = -6.49x + 13678
R2 = 0.02
0
500
1, 000
1, 500
2, 000
2, 500
1950 1960 1970 1980 1990 2000
(m年平均流量
3 /s)
蚌埠
y = - 0. 9127x + 8414. 4
R2 = 0. 0001
0
2, 000
4, 000
6, 000
8, 000
10, 000
12, 000
1950 1960 1970 1980 1990 2000
(m年平均流量
3/s
)
梧州
The trend of annual precipitation during 1951-2004 over China （ mm/10a)
The precipitation show consistent increase in West China
80 90 100 110 120 130
20
30
40
50
-50
-40
-30
-20
-10
0
10
20
30
40
50
60
70
80
90a. Tota l trend of precip itation from Jan. to Jul. during 1951-2003 over China (% )
The precipitation from Aug. and Dec. is decrease in most regions of China
80 90 100 110 120 130
20
30
40
50
-15
-10
-5
0
5
10
15
20
25
30Trend of precip itation from Aug. to D ec. during 1951-2003 (% /10a)
The trend of precipitation (a) from Jan to Jul. and (b) from Aug. to Dec during 1951 －2003
The monthly precipitation change over China during 1951-2003
-150
-100
-50
0
50
100
150
Jan Feb Mar Apr May Jun Jul Aug Sep Oct Nov Dec
流量变化趋势
(%
)
唐乃亥 花园口宜昌 大通哈尔滨 Komsomolsk奴下
The month discharge trends at Yellow, Yangtze and other River during 1951-98
Water use
Reservoirs regulation
The monthly discharge shows negative trends in later year in most rivers
Annual change of dischare for Xingjiang and upper reach of Yellow River
Negative relationship between XJ and UHR
2000
2200
2400
2600
2800
3000
3200
3400
1950 1960 1970 1980 1990 2000
/m
新疆总径流
3 s-1
0
200
400
600
800
1000
1200
/m
黄河径流
3 s-1
新疆总径流黄河径流
( )多项式 黄河径流 ( )多项式 新疆总径流
(a)
R=- 0. 31α >95％
- 0. 8
- 0. 6
- 0. 4
- 0. 2
0
0. 2
0. 4
0. 6
1950 1960 1970 1980 1990 2000
年
新疆总径流距平累积
- 1. 5
- 1. 0
- 0. 5
0. 0
0. 5
1. 0
1. 5
2. 0
2. 5
黄河径流距平累积新疆 黄河(b)
R=- 0. 94
0
200
400
600
800
1, 000
1, 200
1, 400
1, 600
J an Feb Mar Apr May J un J ul Aug Sep Oct Nov Dec
(m3/
s)月平均径流
1956-861987-2000
The monthly discharge average before and after 1987 at upper Yellow River
The hydrological regime has shifted from two peaks to one
peak due to precipitation decrease in fall
Relationship among discharge of upper Yellow River and other main rivers in west China
15
20
25
30
35
40
45
50
55
70 80 90 100 110
<-0.3-0.3~-0.2-0.2~00~0.20.2~0.4>0.4?<0.05
positive
negagive
Relationship between discharge at upper Yellow River and Northwest Pacific monsoon index
It shows East Asian monsoon impact Strongly on runoff at upper Yellow River
0
200
400
600
800
1000
1200
1945 1955 1965 1975 1985 1995 2005
/m流量
3 s-1
- 4. 0
- 3. 0
- 2. 0
- 1. 0
0. 0
1. 0
2. 0
季风指数
黄河径流西北太平洋季风指数
( a)
R=0. 42α >99%
- 1. 5- 1. 0- 0. 50. 00. 51. 01. 52. 02. 53. 0
1945 1955 1965 1975 1985 1995 2005
年
径流距平累积
- 4
- 3
- 2
- 1
0
1
2
3
4
季风指数累积
径流季风指数
( b)
R=0. 84α >99. 99%
East Asian monsoon Southwest monsoon
Vector diagram of summer wind velocity at 600mb during 1951-2008
Westerly influences obviously on rivers in
Xingjiang and Xizang, and
monsoon influences strongly on Yellow river and Yangtze
river
Global temperature change over 100 year（ Jones, 2003）
-0. 8
-0. 6
-0. 4
-0. 2
0. 0
0. 2
0. 4
0. 6
0. 8
1850 1870 1890 1910 1930 1950 1970 1990
全球平均温度距平
-0. 4
-0. 2
0. 0
0. 2
0. 4
0. 6
0. 8
1940 1950 1960 1970 1980 1990 2000
全球平均温度距平
降温期 升温期
8 0 9 0 1 0 0 1 1 0 1 2 0 1 3 0
20
30
40
50
-0 .4
-0.3
-0.2
-0.1
0.0
0.1
0.2
0.3
0.4
0.51850-2003
Warm-dry/cool-wet
Warm-wet/cool-dry
Relationship between global mean temperature and annual precipitation(1950-2003)
It shows regional change feature of precipitation in China with global warming
Combination of dry-wet conditions for temperature rising period and declining period
暖湿/冷干暖干/冷湿混合
8 0 9 0 1 0 0 1 1 0 1 2 0 1 3 0 1 4 0
20
30
40
50
Warm-wet/cool-dryWarm-dry/cool-wet
mixed
Mean summer wind speed at 500mb toward latitude during 1951-2008
Warm-wet/cool-dry areas in southeast and southwest is corresponding to two higher centers of latitude wind
Mean summer wind speed at 500mb toward longitude during 1951-2008
Warm-wet/cool-dry areas in north is corresponding to higher center of longitude wind, i.e.westerly controled area
Response of runoff to climate change： warm-wet/cool-dry
暖湿/冷干暖干/冷湿混合
8 0 9 0 1 0 0 1 1 0 1 2 0 1 3 0 1 4 0
20
30
40
50
190
210
230
250
270
290
310
330
350
1950 1960 1970 1980 1990 2000
(m年平均流量
3 /s)
伊犁河卡甫其海站
700
750
800
850
900
950
1000
1050
1100
1950 1960 1970 1980 1990 2000
(m年平均流量
3 /s)
雅鲁藏布江如下站
400
900
1400
1900
2400
2900
1950 1960 1970 1980 1990 2000
(m年平均流量
3 /s)
松花江哈尔滨站
5000
10000
15000
20000
25000
30000
1950 1960 1970 1980 1990 2000
(m年平均流量
3 /s)
—长江下游宜昌 大通站之间
Response of runoff to climate change： warm-dry/cool-wet
暖湿/冷干暖干/冷湿混合
8 0 9 0 1 0 0 1 1 0 1 2 0 1 3 0 1 4 0
20
30
40
50
200
300
400
500
600
700
800
900
1000
1100
1950 1960 1970 1980 1990 2000
(m年平均流量
3 /s)
黄河上游唐乃亥站
200
400
600
800
1000
1200
1400
1950 1960 1970 1980 1990 2000
(m年平均流量
3 /s)
长江支流汉江安康站
Response of runoff to climate change：mixed zone
暖湿/冷干暖干/冷湿混合
8 0 9 0 1 0 0 1 1 0 1 2 0 1 3 0 1 4 0
20
30
40
50
100
150
200
250
300
350
1950 1960 1970 1980 1990 2000
(m年平均流量
3 /s)
新疆南部叶尔羌河卡群站
10000
11000
12000
13000
14000
15000
16000
17000
18000
19000
1950 1960 1970 1980 1990 2000
(m年平均流量
3 /s)
长江宜昌站
2000
3000
4000
5000
6000
7000
8000
9000
10000
11000
12000
1950 1960 1970 1980 1990 2000
(m年平均流量
3 /s)
珠江梧州站
0
100
200
300
400
500
600
700
800
1950 1960 1970 1980 1990 2000
(m年平均流量
3 /s)
淮河王家坝站
Permafrost
Seasonal frozen ground
Instant frozen ground
No frozen ground
Area ：4.2×106km2
(44% of China area)
SWE ： 75km3
Stable
No Snow
Unstable
Number: 46377
Area ： 59425km2
Volume: 5600km3
(5 times of Yangtze River discharge)
Area ： 2.2×106km2
(23% of China area)
Ground ice:9500km3
Glacier Permafrost Snow cover
The cryosphere in China
中国是中、低纬度地区冰冻圈最发育的国家之一
Glacier Change in last 50 year.
(1). First glacier inventory over China (1960-1970’s)
(Shi et al., 2008)
(2). Second glacier Inventory using remote sensing data during 2000’s)
Glacier Change in last 50 year.
The glacier area change in China during last 50 years (Ding et al., 2006; Liu et al., 2006a, b; Ren et al., 2006; Xiao et al., 2007; Pu et al., 2007; He et al., 2008)
The glacier area reduced by 16.4% in past 50 years in China (0.46%/a) The glacier retreat has large special various. The glacier retreat is smaller in center Tibet Plateau than the area around
the Tibet Plateau
Permafrost Change in last 50 year.
Permafrost distribution map with elevation in Central Asia and and locations of boreholes (Zhao et al., 2010)
Permafrost monitor
Permafrost Change in last 50 year.
Permafrost Change
The thermal state of the active layer at sites along the Qinghai–Tibet Highway: (a) mean annual ground temperature (MAGT) at the bottom of theactive layer (TTOP); (b) MAGT at 50 cm below surface (MAGT50); (c) active-layer thickness (ALT).
temperature at the bottom of active layer
mean annual ground temperature at 50cmm
active-layer thickness
Permafrost Change in last 50 year.
Permafrost Change
Lower altitudinal limit of permafrost change (M)
The temperature at the bottom of active layer has increased between 0.02 and 0.19 /a℃
The Active layer increased about 4cm/a during 1999-2007
Lower altitudinal limit of permafrost has increased by 40-80m during last 40a
Snow Cover Change in last 50 year.
Snow Cover Change
The map of annual maximum snow water equivalent over China
(Che et al., 2004)
Xinjiang Northea
st
Tibet Plateau
There is three snow cover regions in China
(1) Xinjiang
(2) Norhteast China
(3) Qinghai-Xizang Plateau
Snow Cover Change in last 50 year.
Snow Cover Change
Xinjiang: Snow cover has no obvious change during 1951-1997
Qinghai-Xizang Plateau: Snow cover has obvious increase
Northwest China: Snow cover has slight increase
An
nu
al c
um
ula
tive
sn
ow
dep
th (
m)
（ Qin Dahe ， 2005 ； Ding Yongjan, 2009)
The effects of cryosphere change in China
Glacier change effect on the Arid interior River
Permafrost change effect on ecosystem in cold region
disaster and carbon cycle
Snow and permafrost strongly affect on climate over China
Water
Ecosystem
Environment
Climate
The effects of cryosphere change in China
Glacier change effect on the Arid interior River
Permafrost change effect on ecosystem in cold region
disaster and carbon cycle
Snow and permafrost strongly affect on climate over China
Water
Ecosystem
Environment
Climate
The report focused on the effects on water and ecosystem
Cryosphere in China
Indus
River
Gan
ges
Yaluzangbu/ Brahmaputra R.
Yenisey R.
Yellow R.Nu/Salween R.
Langcang/Mekong
Balkhash L./ YIli River
Ob R./ Irtysh R.
Large rivers in Asia are from the Cryosphere in China
Cryosphere and Water
Yangtze R.
The Cryosphere change strongly affects on water resources in arid regions in China
The snowmelt contributs to more than 38% of water in West China
Glacier runoff contributs to 25-29% of the discharge in mountain regions
in northwest arid China
Glacier runoff contributs up to 40 ％ of river discharge in Tarim Basin
Glacier strongly regulates the river discharge
Gla
cier
run
off
Time
Cryosphere and Water
0. 0
0. 5
1. 0
1. 5
2. 0
2. 5
0 10 20 30 40 50Gl aci er coverage (%)
Rati
o be
twee
n ru
noff
var
ianc
ean
d pr
ecip
itat
ion
vari
ance
(Cvr
/Cvp
)
Cryosphere Grass/Forest Oasis Desert
Tail-end lake
Glacier
Permafrost
The effect of cryosphere change on hydrology and ecosystem
How the Glacier runoff affects
river discharge?
How the permafrost influences on the hydrology and ecosystem?
What is the influence of snow cover?
Focus
Method
Field observation
Simulation Statistics
RS 、 GIS 、 GPS
+
Base
Technique
Method
0
100
200
300
400
500
600
700
800
900
1000
1980 1985 1990 1995 2000
(m流量
3 /s)
月径流观测值改进后的模拟值原模型的模拟值
(1980-2004)阿克苏协合拉水文断面模拟结果
Akesu Urumqi RIver Shule River
Dongkemadi in Yangtze River Source
(1). The effect of glacier change in hydrology
BoundaryDEM
R and B
2000
2500
3000
3500
4000
4500
5000
200 400 600
(mm)降水量
0 50 100
Gl aci er area
R and B for whole basin∆S
iiBSB
iiRSR
DDM in basin
2000
2500
3000
3500
4000
4500
5000
-300 0 300 600
A, B ( mm)
Observed data T P A and B
Degree-day factor(DDF)
0.5-9.02000
3000
4000
5000
- 20 0 20
T(℃)
2000
2500
3000
3500
4000
4500
5000
200 400 600
P (mm)
B
AKt Kp
Ablation：
ii DDTDDFA B ： iii APsB
Runoff ： iii AR Pr
Degree-day model (DDM) in site
)( 00 ZZKtTT ii Temp. ：)( 00 ZZKpPP ii Prec. ：
Estimation of glacier runoff
The simulated Glacier runoff and observed runoff at river outlet in 4 main branches in
Tarim Basin
40
80
120
160
200
240
280
320
1960 1970 1980 1990 2000 2010
An
nu
al R
un
off
/108 m
3
River runoff Glacier runoff
The river runoff has increased by 22% during 1962-2008
2/3 of increased part are from glacier runoff increase
(Liu et al., 2006)
The effect of glacier runoff change -Tarim Basin
The projected glacier runoff by 2050 in Akesu River under different scenarios (related to runoff during 1961-1990)
The glacier runoff will increase in following 40 years in Akesu river
24
25
26
27
28
29
30
31
32
33
34
2010 2015 2020 2025 2030 2035 2040 2045 2050
Glac
ier
runo
ff(1
08 m3 )
B1 A2 A1B
Glacier in Akesu:
Mean area:2.4km2
Max Area:393km2
The effect of glacier runoff change -Akesu River
The river runoff and glacier runoff at Zhimenda station in the Yangtze River source in recent 40a
The river runoff
decreased by 13.9%
while the glacier
runoff increased by
15.2% from1961-
1990 to 1990-2000
50
100
150
200
1960 1970 1980 1990 2000
Runoff
/X108m3
Ri ver runoff
8
10
12
14
16
1960 1970 1980 1990 2000
Runoff
/X108m3
Gl aci er runoff
(Liu Shiyin, 2009)
The effect of glacier runoff change -The Yangtze River source
8
10
12
14
16
18
2000 2010 2020 2030 2040 2050
Glac
ier
runo
ff (
108m
3) A2
B15 (B1)天移动平均5 (A2)天移动平均
(Zhang Yong, 2008)
Glacier:
Mean area:2.0km2
Max Area:53km2
The glacier runoff will increase in the following 40 years in the Yangtze river source
The projected glacier runoff by 2050 in the Yangtze River source under different scenarios (related to runoff during 1961-1990)
The effect of glacier runoff change -The Yangtze River source
The accumulation and ablation during 1958-2004 in the Urumqi River source Glacier No.
1
0
100
200
300
400
500
600
700
800
900
1000
1955 1965 1975 1985 1995 2005
Accumulation and ablation (mm)
Accumul ati onAbl ati on
(Abl ati on)线性 (Accumul ati on)线性
(a) The runoff increased by 35% during 1996-2005 comparing to 1980-1995; 37% of the increased part is from precipitation increase, 63% is from glacier mass loss
(Ye Baisheng , 2005)
The effect of glacier runoff change -The Urumqi River source
The glacier runoff can reach the peak in the following 20a
More than 80% glaciers is smaller than 1km2 in the basin
The effect of glacier runoff change -The Urumqi River source
The decade mass balance during 1961-2006 in interior in Hexi Corridor
The effect of glacier runoff change -The Hexi Corridor
-350
-250
-150
-50
50
150疏勒河 党河 北大河 黑河 石羊河
物质平衡
/mm
1960s 1970s 1980s 1990s 2000s
Shule Dang Baida Hei Shiyang
Mas
s B
ala
nce
0. 00. 10. 20. 30. 40. 50. 6
2010 2015 2020 2025 2030 2035 2040 2045 2050
Glac
ier
Runo
ff(1
08 m3 )
B1
A2
A1B
The glacier runoff peak maybe already occurred under climate warming due to quick response of small glacier
The effect of glacier runoff change -The Hexi Corridor
Glacier:
Mean area:0.46km2
All glacier is smaller than 1km2
The projected glacier runoff by 2050 in the Shiyang River in Hexi Corridor under different scenarios (related to runoff during 1961-1990)
The glacier runoff peak caused by climate warming
has occurred or will soon appeared in the basin with
small glacier
The glacier runoff will continuously increase and can
not reach its peak within future 50a under climate
warming in the basin with large glacier
The effect of glacier runoff change
(2). The effect of snow cover change on hydrology
- 600
- 400
- 200
0
200
400
600
800
1000
1200
1400
1600
J an Feb Mar Apr May J un J ul Aug Sep Oct Nov Dec
Dis
cha
rge
(m3 /
s)
MeanSTDTrend
Yel l ow Ri verat Tannai hai
- 2000
- 1000
0
1000
2000
3000
4000
5000
6000
J an Feb Mar Apr May J un J ul Aug Sep Oct Nov Dec
Dis
cha
rge
(m3 /
s)
MeanSTDTrend
Brahmaputat Nuxi a
The monthly discharge change of main rivers in west China during 1951 － 2006
- 200
- 100
0
100
200
300
400
500
600
700
J an Feb Mar Apr May J un J ul Aug Sep Oct Nov Dec
Discharge (m
3 /s)
MeanSTDTrend
Yeerqi an, at Wul uwat i
- 100
0
100
200
300
400
500
J an Feb Mar Apr May J un J ul Aug Sep Oct Nov Dec
Disch
arge
(m3 /s
)
MeanSTDTrend
Al ertai at Qi ongkul e
15
20
25
30
35
40
45
50
55
70 75 80 85 90 95 100 105 110
<-20-20~-10-10~-5-5~00~55~1010~20>20α<0.05
May
Irtysh River
The effect of snowmelt runoff
The Yellow River source
Yerqiang River Yaluzangbu River
Decade-mean Monthly discharge at Aletai station in Kelan River (branch of Irtysh River during 1959-2005
The max. dicharge occured earlier due to early snowmeltThe max. dicharge also increased by 15% due to rich snowThe discharge during April-June (snowmelt season) changed from 60%
to 70% of annual dischargeThe early snowmelt lead to discharge decrease in summer, the
hydrological regime change
0
10
20
30
40
50
60
70
80
90
100
J an Feb Mar Apr May J un J ul Aug Sep Oct Nov Dec
Disc
harg
e (m
3 /s)
1960s
1970s
1980s
1990s
2001- 2005
(Shen Yongping, 2007)
The effect of snowmelt runoff
(3). The effect of permafrost degradation on hydrology and ecosystem
The hydrological regime in rivers in Siberia with different coverage of permafrost (CP)
Permafrost and hydrology
The CP strongly influence on the hydrological regime
High CP, high peak flow and low basin flow
0
10
20
30
40
50
60
70
J an Feb Mar Apr May J un J ul Aug Sep Oct Nov Dec
Disc
harg
e %
（）
Anabar (CP=95%)Lena (CP=86%)Yeni sei (CP=31%)Ob (CP=7. 5%)Perchora (Cp=0%)
1
10
100
1000
0 20 40 60 80 100Coverage of Permafrost (%)
Qmax
/Qmi
n
Arcti cChi na
High CPLow CP
The Qman/Qmin v. coverage of permafrost
The hydrological regime is mostly controlled by coverage of permafrost (CP) in basin with CP higher than 60%
The permafrost degradation caused large regime change in high CP basin, but no effect on regime in low CP(<30%) basin
(Ye Baisheng, 2009)
Permafrost and hydrology
The Qmax/Qmin at Changmapu in Shulehe and at Yinluoxia in Heihe Rivers during past 60a
The climate warming, consequently permafrost degradation, causes the more flat hydrological regime
Qmax/ Qmi n= - 0. 0746x + 159. 08R2 = 0. 1237
0
2
4
6
8
10
12
14
16
18
20
1950 1960 1970 1980 1990 2000 2010
Qmax
/Qmi
n
Changmapu(CP=73%)
Qmax/ Qmi n= - 0. 044x + 98. 424R2 = 0. 1144
0
2
4
6
8
10
12
14
16
18
20
1940 1950 1960 1970 1980 1990 2000 2010
Qmax
/Qmi
n
Yi nl uoxi a (CP=58%)
Permafrost and hydrology
Arid region ：
Cryosphere
Oasis
Tail-end lake system
Cryosphere and Ecosystem
Glacier-Oasis
Glacier/Cryosphere
Oasis
Tail-end lake
Desert
Desert
Cryosphere Grass/Forest Oasis Desert
Major projects, such as
Qinghai-Tibet Railway and
high way, 3-River sources
nature reserve regions for
water and ecosystem,
Protection and Construction
of the State Ecological Safe
Shelter Zone on the Tibet
Plateau, are related to
Cryosphere 。
Qinghai-Xizang Plateaus ： Cryosphere-Ecosystem-Lake-everglade system
Tanggula Pass
Cryosphere and Ecosystem
高寒草甸
R2 = 0. 5567
30
40
50
60
70
80
90
100
0 1 2 3 4 5 6m)冻土上限（
植被覆盖度（％）
高寒草原
R2 = 0. 0469
0102030405060708090
100
0 2 4 6 8m)冻土上限（
植被覆盖度（％）
The ecosystem with rich water supply is more sensitive to permafrost degradation
The relationship between plants coverage and active layer depth in the Yellow and Yangtze River source
The type of plants and active layer depth
（ Ding Yongjian, 2009)
Permafrost and ecosystem
MeadowGrass
Co
vera
ge
（%
）
Co
vera
ge
（%
）
Active layer depth (m) Active layer depth (m)
Steppe？
The ecosystem change in the Yellow and Yangtze River sources during 1967-2008
Region高覆盖 meadow 高覆盖高寒 grass
Swamp and everglade
1967-2008
1986-2000
1967-2008
1986-2000
1967-2008
1986-2000
Yangtze -16.4 -11.3 -6.8 -3.5 -37.3 -27.3
Yellow -25.6 -21.2 -7.9 -5.5 -16.8 -13.1
Total -19.5 -8.6 -32.1
Great change, may related to permafrost degradation
Small change
(Yang Jianping, 2007)
Permafrost and ecosystem
0
2
4
6
8
10
12
14
16
- 1500 - 1250 - 1000 - 750 - 500 - 250 250 500 750 1000 1250 1500 1750 2000
Di stance f rom boundary (m)
Ratio of degradation and
improvement area
No permafrost Transi ti on Permafrost
The ratio of degradation and improvement area in permafrost, no permafrost and transition regions
The grass degradation is obvious in transition
region during 1986-2008
The ratio of degradation and improvement
area in transition region is much higher than
both permafrost region and no-permafrost
region
The permafrost distribution in Shule
River Basin in west Hexi Corridor
Permafrost and ecosystem
Relationship between dominant species and the active layer depth
The Active layer depth (m)Cyperaceae species
Gramineae species
Permafrost and ecosystem
Relationship between species number and total biomass, and the active layer depth
Upstream of the Shule River Basin
With the increase in permafrost depth, species mumber and biomass decreased in both regions.
Dongkemadi River Basin
Permafrost and ecosystem
The mechanism of response of ecosystem to the active layer depth of permafrost: the changes of soil water content
Permafrost and ecosystem
Soil
wat
er c
onte
nt（
%）
The active layer depth of permafrost
1. Climate change and hydrological regime
2. The effect of Cryosphere change
3. Management for water resources and ecosystem in West China
Tarim River
Hexi Corridor
River Sources
Main measurement for water resource and ecosystem in China
Northeast
Heihe River measurementinvestment：2001-2005:2.4 Billion 2006-2010:4.8 Billion
To protect the ecosystem in downstream of Heihe River in Hexi Corridor
River Dry-up
Ecosystem degradation
Lake shrinking
Shiyanghe River measurement
Investment(RMB)：2005－ 2010:4.3 billion
To protect the ecosystem in downstream of Shiyanghe River in Hexi Corridor
Tarim River measurement
Investment(RMB):2001-2005:10.8Billion
To protect the ecosystem in downstream of Tarim River
Tarim River downstream
Investment(RMB):2005-2010:7.5Billion
To increase water resource
Measurement:Forests and grasslandsWetlands conservationEcological migrants
Investment(RMB):2005-2010:7.5Billion
To increase water resource
Measurement:Forests and grasslandsWetlands conservationEcological migrants
desertification mouse damage
Glacier retreat Permafrost
River Source measurement in Tibet Plateau
谢谢！Thank you for
your attention ！