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Sciences in Cold and Arid Regions Volume 6, Issue 1, February, 2014

Citation: Xu  JH, Li WH, Hong YL, et al., 2014. A quantitative assessment on groundwater salinization  in  the Tarim River  lower  reaches, Northwest China. Sciences in Cold and Arid Regions, 6(1): 44–51. DOI: 10.3724/SP.J.1226.2014.00044.   

A quantitative assessment on groundwater salinization in the Tarim River lower reaches, Northwest China

JianHua Xu 1*, WeiHong Li 2, YuLian Hong 1,

ChunMeng Wei 1, Jie Tang 1

1. The Research Center for East-West Cooperation in China, the Key Laboratory of Geographic Information Science, the Ministry of Education of PRC, East China Normal University, Shanghai 200062, China

2. State Key Laboratory of Desert and Oasis Ecology, Xinjiang Institute of Ecology and Geography, Chinese Academy of Sciences, Urumqi, Xinjiang 830011, China

*Correspondence to: JianHua Xu, Research Center for East-West Cooperation in China, East China Normal University,

Shanghai 200062, China. E-mail: jhxu@geo.ecnu.edu.cn

Received: March 15, 2013 Accepted: July 1, 2013

ABSTRACT

Based on monitored data from 840 samples, we assessed the spatial and temporal variability of groundwater salinization in the Tarim River lower reaches combining classical statistics and geostatistics. Results show that total dissolved solids (TDS) is significantly correlated with other related ions, such as Na+, Mg2+, Ca2+, Cl− and K+. TDS and underground water level have characteristics of spatial autocorrelation, both of which present the isotropic characteristic and con-form to the spherical model in each year from 2001–2009. TDS is basically greater than 1 g/L but less than 2 g/L in the Tarim River lower reaches, which indicates that salt stagnation pollution is more serious. The most serious salinization (3 g/L < TDS ≤ 35 g/L) contaminated area is mainly in the middle and lower part of the study area. Keywords: groundwater; salinization assessment; semivariogram; geostatistics; lower reaches of the Tarim River

1 Introduction

Groundwater salinization, which is commonly found in coastal, arid and semi-arid areas, refers to the enrichment of a variety of dissolved substances in groundwater under the cooperative influence of human activity and natural evolution (Karro et al., 2004; Subyani, 2005). Many factors lead to continuing groundwater salinization, such as dissolution of soluble minerals, rising groundwater level, strong evaporation, scarce precipitation, large-scale exploitation of groundwater, inappropriate agricultural irrigation and excessive use of chemical fertilizers (Chourasia and Tellam, 1992; Fisher and Mulican, 1997). The study of

groundwater salinization characteristics, material sources and influencing factors can provide a scientific basis for groundwater resource planning, utilization and management, and prevention of soil salinization.

In a number of chemical parameters, total dis-solved solids (TDS) is an important indicator that describes groundwater salinization. It is often used to characterize the regional groundwater hydrochemical characteristics. Studies (Salama et al., 1999; Wang et al., 2008) show that the higher the TDS’s value of shallow groundwater, the more serious soil saliniza-tion becomes when groundwater depth is lower than the critical depth of salt uprising. Otherwise the de-gree of soil salinization will become mild. Therefore,

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TDS is considered as one of the important ground-water salinization indicators.

In arid and semi-arid areas of Northwest China, groundwater salinization has become common forms of groundwater pollution. A variety of studies have defined groundwater salinization, and can be inter-preted as follows: along the direction of groundwater flow, chemical composition changes from the re-charge zone to discharge zone, due to an increase of TDS in the groundwater and the concentration of chemical components (Richter and Kreitler, 1993; Wen et al., 2006).

Based on monitored data from 840 samples from 2000 to 2009, this paper investigated the spatial and temporal variability of groundwater salinization in the Tarim River lower reaches by classical statistics and geostatistics.

2 Study area and data 2.1 Study area

Tarim River is located in south Xinjiang, Northwest China, with a length of 1,321 km and watershed area of 102×104 km2 (39°00'N–41°40'N, 74°30'E–88°30'E) (Zhang et al., 2005). It is one of the longest inland riv-ers around the world, and plays a key role in the de-velopment of local society and economy. The Takla-makan Desert, the second largest desert in the world, is named after the Tarim River and Kuluke Desert. It lies to the south of the river and extends across the Tarim Basin. There are Tianshan Mountains to the north of the basin and Karakorum Mountains to the south. The Tarim River lower reaches are 321 km in length from Qiala to Taitema Lake (Figure 1).

Figure 1 Location of the monitoring sites for groundwater of the Tarim River lower reaches

Downstream alluvial plain area lies in the eastern part of the Tarim Basin, and the terrain is relatively flat, with an average altitude of 825 m. Major land-form types are alluvial-diluvial, alluvial, aeolian and fluvial-lacustrine sedimentation. Simultaneously, the stratum structure is simple, mainly made up of Pleistocene and Holocene quaternary strata, and the surface lithology is dominated by sand, sub-sandy soil and clay. In addition, the aquifer in this study area is quaternary, and the lithology is single with predominantly river-lake facies fine sand and silty fine sand, and eolian sand locally. Divided by wa-ter-bearing media, it belongs to a typical chinky aq-uifer; while divided by burial condition, it belongs to a phreatic aquifer (Chen et al., 2008; Li et al., 2010;

Xu et al., 2008, 2013). Thus, the permeability and water abundance are relatively poor with the perme-ability coefficient varying from 1.2 to 4.8 m/d, and the single-orifice water inflow is less than 150 m3/(d·m). The study area is located in a disconnec-tion river, from Tikanlik to Taitema Lake, which has a warm-temperate, extremely arid climate with an-nual solar radiation of 5,692–6,360 kJ/m2. According to observations by the Tikanlik meteorological sta-tion from 1957 to 2005, average temperature, annual precipitation and annual evaporation are 10.94 °C, 34.53 mm and 2,531.45 mm, respectively. Due to years of zero flow, the groundwater table mostly dropped to 8–12 m and both the degree of salinity and mineralization are relatively high.

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2.2 Data collection and analysis

Nine groundwater monitoring sites along the Tarim River lower reaches were selected. They are Akdun (A), Yahepu (B), Yingsu (C), Abudali (D), Kardayi (E), Tugmailai (F), Alagan (G), Yiganbjima (H) and Kaogan (I). Monitoring wells, with a depth of 8–17 m, were stationed at an interval of 100 to 200 m for every monitoring site. There were 40 monitoring wells in total and they were distributed within the range of 50–1,050 m away from the watercourse. In order to analyze groundwater chemistry component change, we measured the groundwater table and collected ground-water samples regularly from each well at each site. We collected and analyzed 840 samples during the period from 2000 to 2009. The samples were stored in clean and colorless polyethylene plastic bottles, and sealed with paraffin and labeled, and placed in a shaded area until sent to the laboratory. Chemical compositions of the samples were analyzed within two days in the la-boratory. The chemical analyses included total dis-solved solids (TDS), pH, concentrations of CO3

2−, HCO3

−, Cl−, SO42−, Ca2+, Mg2+, K+ and Na+.

This study adopted an appropriate method to meas-ure each parameter. The pH was measured using a pH meter (APHA, 1995). Calcium (Ca2+) and magnesium (Mg2+) were determined using the EDTA titrimetric method (APHA, 1995). Chloride (Cl−) was determined by standard AgNO3 titration. Carbonate (CO3

2−) and bicarbonate (HCO3

−) were determined by titration with HCl (APHA, 1995). Sodium (Na+) and potassium (K+) were measured by flame photometry, while sulphate (SO4

2−) by spectrophotometer turbidimetry (APHA, 1995). Total dissolved solids (TDS) was determined by the gravimetric method (MEP PRC, 1999). 3 Methods 3.1 Classical statistics

Although groundwater salinization in the Tarim River lower reaches is affected by various factors, the correlation between groundwater salinization and pa-rameters describing chemical components can still be established, as is commonly performed in numerous studies (Xu, 2002; Tardy et al., 2004; Giridharan et al., 2008; Chenini and Khemiri, 2009; Xu et al., 2012). For the purpose of comparison, this work also con-ducted regression analysis to examine the correlation among TDS and ions. 3.2 Geostatistics

Studies have shown that groundwater chemistry parameters are typical regionalized variables, which are structural as well as stochastic (Ahmadi and

Sedghamiz, 2008; Wang et al., 2008; Wang et al., 2011). Thus, the spatial variability of groundwater salinization in the Tarim River lower reaches can be analyzed by the geostatistic method (Journel and Huijbregts, 1978; Marchant and Lark, 2004). 3.2.1 The semivariogram

In geostatistics (Journel and Huijbregts, 1978; Marchant and Lark, 2004), the regionalized variable, such as TDS or groundwater depth, is regarded as the value of a variable at a location x as a realization of a random function Z(x). This random function is as-sumed to be intrinsically stationary. This is a weak form of second-order stationarity and is met if two conditions hold. The first is that the expected value of the random function, E[Z(x)], is constant for all x. Secondly, the variance of the differences between the value of the variable at two different locations de-pends only on the lag vector separating the two loca-tions and not on absolute locations. In general, this variance may be a function of both the direction and length of the lag vector. If the regionalized variable is isotropic, the semivariogram is purely a function of the length of the vector which we denote h. Thus, the relationship between values from different locations is described by the semivariogram.

]))()([(21)( 2hxZxZEh +−=γ (1)

The semivariogram is estimated from variable

values observed at sampled points, xs, s=1, . . . , n. The method of moments estimator is the average of squared differences between observations separated by distance h as follows:

∑=

+−=)(

1

2)]()([)(2

1)(hN

iii hxZxZ

hNhγ (2)

where Z(xi) indicates the magnitude of regionalized variable, and N(h) is the total number of pairs of at-tributes that are separated by a distance h.

This study used the semivariogram to reveal the spatial variability of TDS and groundwater level in each year. 3.2.2 Kriging and Cokriging methods

Based on the semivariogram, Kriging and Cokriging can be used to estimate the values of regionalized vari-able at unsampled locations (Goovaerts, 1997).

Ordinary Kriging can mathematically be defined as given in the following:

∑=

=n

iiiX XZZ

1

* )(λ (3)

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where Z*X is the estimated value, and λi is the corre-

sponding weight of each observation Z(Xi) on the es-timation. These weights are calculated to ensure that the estimator is unbiased and the estimation variance is a minimum. The nonbias condition requires that:

⎪⎪⎩

⎪⎪⎨

⎧

=

=−

∑

∑

=

=

n

ii

iji

n

ii XXXX

1

*

1

1

),(),(

λ

γμγλ (4)

where γ(Xi, Xj) is the semivariogram between sampled point i and point j, γ(Xi, X*) is the semivariogram be-tween sampled point and estimated point, and μ is the Lagrange multiplier of minimum condition.

The general form of Cokriging equations are:

*

1 1

1

( , ) ( , )

1,0,

l

l

nv

il lv i j v uv jl i

n

ili

X X X X

l ul u

λ γ μ γ

λ

= =

=

⎧− =⎪

⎪⎨ =⎧⎪ = ⎨⎪ ≠⎩⎩

∑∑

∑ (5)

where u and v are the primary and covariate (secondary) variables, respectively. In the Cokriging method, the u and v are cross-correlated and the covariate contributes to the estimation of the primary variable. Generally, measuring the covariate is simpler than measuring the primary variable. For the Cokriging analysis, the cross semivariogram (or cross-semivariogram) should be determined in prior. Provided that there are points where both u and v have been measured, the

cross-semivariogram is estimated by:

{

}

( )

1

1( ) [ ( ) ( )]2 ( )

[ ( ) ( )]

N h

uv u i u ii

v i v i

h Z X Z X hN h

Z X Z X h

γ=

= − + ⋅

− +

∑ (6)

In order to reveal the spatial pattern of groundwater

level and TDS, the two interpolation methods, ordinary Kriging and Cokriging were used and cross-checked for interpolation test. Our results show that the accura-cy of Cokriging is higher than that of ordinary Kriging. Based on interpolation test, selecting groundwater and altitude as the first and second co-variable, we used the Cokriging method to compute the interpolation values of TDS from 2001 to 2009. 4 Results and discussion 4.1 Groundwater salinization and its related major

chemical parameters

The basic statistical parameters and the t-test re-sults for 840 samples are presented in table 1. Overall, the groundwater in the lower reaches of the Tarim River shows slight alkalinity, with a mean pH of 7.66±0.02 and a mean TDS of 5.333±0.450 g/L. As for the anions of CO3

2−, HCO3−, Cl− and SO4

2−, the contents are 0.002±0.000, 0.363±0.006, 2.047±0.233 and 1.002±0.052 g/L, respectively. Similarly, the con-tents for cations of Ca2+, Mg2+, Na+ and K+ are 0.180±0.009, 0.220±0.012, 1.299±0.140 and 0.036±0.002 g/L, respectively.

Table 1 Basic statistical analysis of groundwater salinization

Mean Std. error of mean Std. Skewness Kurtosis t Samples Sig. (2-tailed)TDS (g/L) 5.333 0.450 13.050 6.030 42.187 11.845 840 0.000 CO3

2− (g/L) 0.002 0.000 0.012 8.878 91.168 4.583 840 0.000 HCO3

− (g/L) 0.363 0.006 0.175 1.217 2.298 60.177 840 0.000 Cl− (g/L) 2.047 0.233 6.762 6.949 58.111 8.774 840 0.000 SO4

2− (g/L) 1.002 0.052 1.511 3.648 15.282 19.216 840 0.000 Ca2+ (g/L) 0.180 0.009 0.249 5.171 36.093 20.907 840 0.000 Mg2+ (g/L) 0.220 0.012 0.338 3.523 12.903 18.832 840 0.000 Na+ (g/L) 1.299 0.140 4.064 6.738 53.858 9.264 840 0.000 K+ (g/L) 0.036 0.002 0.069 6.340 43.323 15.287 840 0.000

Studies (Salama et al., 1999; Wang et al., 2008)

show that the higher the TDS’s value of shallow groundwater, the more serious soil salinization be-comes. Otherwise the degree of soil salinization will become mild. Therefore, TDS was considered as one of the important indicators for groundwater saliniza-tion in the Tarim River lower reaches.

Stepwise regression analysis was performed by taking TDS as dependent variable and other parame-ters as independent variables. The regression equation is as follows:

2 23.2598Na 5.6050Mg 3.1437Ca

1.1016K 0.3577Cl 0.0758TDS + + +

+ −

= + +

− − + (7)

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The t-test results are presented in table 2 and indi-cate that the screened independent variables are Na+, Mg2+, Ca2+, Cl− and K+. The partial regression coeffi-cient of the first four independent variables, i.e., Na+, Mg2+, Ca2+, Cl−, are all highly significant (Sig.=0.0000), as well as the independent variable, i.e., K+, shows high significance (Sig.=0.0495). This indicates that Na+, Mg2+, Ca2+, Cl− and K+ are the main chemical variables to affect TDS.

The main reason why the regression of TDS exhib-its high correlations with Na+, Mg2+, Ca2+, Cl− and K+

is that the lower reaches of the Tarim River is a salt accumulation zone, with high salt content in the soil and groundwater (Chen et al., 2005). Moreover, due to implementation of the ecological water delivery project since 2000 (Gao et al., 2007), the groundwa-ter tables in the lower reaches were uplifted and the concentrations of various chemical substances were diluted. In other words, the lower the groundwater table, the higher the salinity concentration. This re-sult is consistent with studies of Li et al. (2010) and Xu et al. (2012).

Table 2 The correlation between TDS and cations in groundwater chemical components

Dependent variable Independent variable and constant Coefficients t Sig.

TDS

Na+ 3.2598 54.8818 0.0000 Mg2+ 5.6050 64.1187 0.0000 Ca2+ 3.1437 21.6392 0.0000 Cl− −0.3577 −10.2380 0.0000 K+ −1.1016 −1.9672 0.0495

Constant 0.0758 3.3480 0.0009

4.2 Spatial variability of groundwater level and TDS

Our study shows that both groundwater level and TDS have isotropic characteristics for each year from 2001–2009, and their semivariogram conform to the spherical model as follows:

3

0 3

0

0 03( ) ( ) 02 2

hh hh C C h aa a

C C h a

γ

=⎧⎪⎪= + − < ≤⎨⎪

+ >⎪⎩

(8)

where C0 is the nugget that reflects spatial heteroge-neity caused by random factors, a is the maximum range of spatial autocorrelation, and C0+C is the sill that represent total variance.

Table 3 shows the related semivariogram parame-ters for groundwater level and TDS. Evidently, both the nugget of groundwater level and TDS are lower, which indicates that the variable error caused by sam-pling and analyzing is smaller. The maximum range of the groundwater level and TDS reached 90.3 km and 81.1 km respectively, which means that ground water level and TDS presented spatial autocorrelation char-acteristics in a larger space.

C0/(C0+C) is the ratio of the nugget and sill. The high ratio shows that the spatial variability caused by randomness is dominant. Otherwise, the low ratio shows that the dominant spatial variability is caused by configurative factors. The regionalized variable has

a strong spatial correlation when C0/(C0+C) ≤25%. It is medium when 25%< C0/(C0+C) <75%, and the spa-tial variability are low when C0/(C0+C) ≥75%.

Table 3 shows that in 2000, 2001 and 2009, C0/(C0+C) of underground water level are all greater than 25%, except for 2006. Thus, it can be seen that the underground water level shows strong spatial autocor-relation in 2002, 2003, 2004, 2005 and 2007. In the remaining years, however, underground water level shows medium spatial autocorrelation due to C0/(C0+C) greater than 25%.

4.3 The assessment of groundwater salinization

Using the Cokriging method, we selected ground-water and altitude as the first and second co-variables, TDS from 2001 to 2009 was drawn respectively. Fig-ures 2–3 shows the spatial patterns of TDS for 2006 and 2009, respectively.

Based on the results of Cokriging interpolation for TDS, according to the classification criteria of division of groundwater salinization degree proposed by Robinove et al. (1958), the assessment results of groundwater salinization in the Tarim River lower reaches from 2001 to 2009 are presented in table 4. TDS is basically greater than 1 g/L but less than 2 g/L in the Tarim River lower reaches, which indi-cates that salt stagnation pollution is more serious. The most serious salinization (3 g/L < TDS ≤35 g/L) contaminated area is mainly in the middle and lower part of the study area.

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Table 3 Semivariogram and its parameters of groundwater level and TDS

Year C0 C0+C C0/(C0+C) a (km)

Groundwater level

2000 0.126 0.389 32.39% 18.92001 0.252 0.696 36.21% 81.22002 0.122 0.496 24.60% 90.32003 0.413 2.574 16.05% 37.42004 0.455 3.282 13.86% 78.22005 0.032 3.491 0.92% 11.22006 0.216 0.513 42.11% 69.52007 0.055 2.351 2.34% 68.52008 0.698 2.485 28.09% 81.12009 0.533 1.432 37.22% 81.1

TDS

2000 0.186 0.515 36.12% 57.82001 0.293 0.734 39.92% 81.22002 0.129 0.391 32.99% 35.12003 0.051 0.752 6.78% 75.52004 0.912 1.435 63.55% 77.42005 0.603 1.043 57.81% 81.12006 0.654 1.118 58.50% 81.12007 0.643 0.997 64.49% 69.52008 0.732 1.032 70.93% 81.12009 0.594 1.263 47.03% 81.1

Figure 2 Spatial patterns of TDS in 2006

Figure 3 Spatial patterns of TDS in 2009

Table 4 The area ratio of classification of groundwater salinization level

Year Brackish water Moderate salt water Extreme salt water Brine

(1 g/L < TDS ≤3 g/L) (3 g/L < TDS ≤10 g/L) (10 g/L < TDS ≤35 g/L) (TDS >35 g/L) 2001 71.79 20.51 5.13 2.56 2002 79.49 17.95 2.56 0.00 2003 92.31 5.13 2.56 0.00 2004 85.12 5.54 7.18 2.16 2005 79.49 12.82 5.13 2.56 2006 82.05 10.26 5.13 2.56 2007 71.79 20.51 5.13 2.56 2008 71.79 20.51 5.13 2.56 2009 75.87 12.09 7.50 4.54

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The area ratio of brackish water (1 g/L < TDS ≤3

g/L) first increased, then decreased, and at last showed a smooth trend. It increased from 71.79% to 92.31% during the period of 2001 to 2003 and then smooth in the following years. The area ratio of mod-erate salt water (3 g/L < TDS ≤10 g/L) presented a decreasing trend first and then basically stabilized after short fluctuations, but with a slight upward trend in 2009. In addition to more than 7% in 2004 and 2009, the area ratio of extreme salt water (10 g/L < TDS ≤35 g/L) stabilized at around 5.1% in other years. The area proportion of brine (TDS >35 g/L) was very low, and it even was 0% in 2002 and 2003.

5 Conclusions

Temporal and spatial variability of groundwater salinization in the Tarim River lower reaches were analyzed by a combined method of classical statistics, geostatistics and geographic information system. The main findings are as follows:

(1) As one of the important indicators for ground-water salinization in the Tarim River lower reaches, TDS is related with other chemical parameters, such as Ca2+, Mg2+, Na+, K+, CO3

2−, HCO3−, Cl− and SO4

2−. There is significant correlation between TDS with other related ions, such as Na+, Mg2+, Ca2+, Cl− and K+.

(2) TDS and the underground water level have characteristics of spatial autocorrelation. Although the related parameters of the semivariogram are different, both groundwater level and TDS present isotropic characteristics and conform to the spherical model for each year during 2001–2009.

(3) TDS is basically greater than 1 g/L but less than 2 g/L in the Tarim River lower reaches, which indicates that salt stagnation pollution is more serious. The most serious salinization (3 g/L < TDS ≤35 g/L) contami-nated area is mainly in the middle and lower part of study area. The area proportion of brine (TDS >35 g/L) was very low. Acknowledgments: This work was supported by the National Basic Re-search Program of China (973 Program; No. 2010CB951003). References Ahmadi SH, Sedghamiz A, 2008. Application and evaluation of

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