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Effect of groundwater on the ecological water environment of typical inland lakes in the Inner Mongolian Plateau
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Abstract: To explore the causes of the ecological environment deterioration of lakes in the Inner Mongolia Plateau, this study took a typical inland lake Daihai as an example, and investigated the groundwater recharge in the process of lake shrinkage and eutrophication. Using the radon isotope (222Rn) as the main means of investigation, the 222Rn mass balance equation was established to evaluate the groundwater recharge in Daihai. The spatial variability of 222Rn activity in lake water and groundwater, the contribution of groundwater recharge to lake water balance and its effect on nitrogen and phosphorus pollution in lake water were discussed. The analysis showed that, mainly controlled by the fault structure, the activity of 222Rn in groundwater north and south of Daihai is higher than that in the east and west, and the difference in lithology and hydraulic gradient may also be the influencing factors of this phenomenon. The 222Rn activity of the middle and southeast of the underlying lake is greater, indicating that the 222Rn flux of groundwater inflow is higher, and the runoff intensity is greater, which is the main groundwater recharge area for the lake. The estimated groundwater recharge in 2021 was 3 017×104 m3, which was 57% of the total recharge to the lake, or 1.6 times and 8.1 times that of precipitation and surface runoff. The TN and TP contents in Daihai have been rising continuously, and the average TN and TP concentrations in the lake water in 2021 were 4.21 mg·L−1 and 0.12 mg·L−1, respectively. The TN and TP contents entering the lake with groundwater recharge were 6.8 times and 8.7 times above those of runoff, accounting for 87% and 90% of the total input, respectively. The calculation results showed that groundwater is not only the main source of recharge for Daihai, but also the main source of exogenous nutrients. In recent years, the pressurized exploitation of groundwater in the basin is beneficial in increasing the groundwater recharge to the lake, reducing the water balance difference of the lake, and slowing down the shrinking degree of the lake surface. However, under the action of high evaporation, nitrogen and phosphorus brought by groundwater recharge would become more concentrated in the lake, leading to a continuous increase in the content of nutrients and degree of eutrophication. Therefore, the impact of changes in regional groundwater quantity and quality on Daihai is an important issue that needs further assessment.
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Key words:
- Groundwater recharge /
- Radon isotopes /
- Nitrogen and phosphorus pollution /
- Ecological environment /
- Daihai
http://www.durridge.com/products_rad7.shtml.
②Institute of water resources for pastoral area, MWR, 2018. Study on the influence of “returning irrigation water in the basin to groundwater” on the Daihai Lake.
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Figure 5. Frequency distribution histograms of the 222Rn activity measured in Daihai and groundwater
Figure 6. Distribution characteristics of TN and TP contents in groundwater in and around Daihai
Figure 7. Distribution of 222Rn activity of Daihai Lake bottom, lake water and groundwater (a, b and d are 222Rn activity of surface and bottom lake water and groundwater, respectively, and c is the depth of lake bottom②)
Table 1. Calculation of groundwater recharge flux based on 222Rn activity
Source-sink terms Parameter Unit Value Description Atmospheric loss Radon concentration in surface lake (Cws) Bq·m−3 78.96±5.28 Measured in the field Radon concentration in air (Cair) Bq·m−3 9.61 Measured in the field Partition coefficient (α) Dimensionless 0.27 （Burnett and Dulaiova, 2003） Temperature in lake (T) °C 18.4 Measured in the field Gas transfer coefficient (k) m·d−1 0.18 （Rodellas et al. 2018） Wind speed (u) m·s−1 1.77 Measured in the field Schmidt number (Sc) Dimensionless 1064.37 （Pilson, 1998） Atmospheric loss flux (Fatm) Bq·m−2·d−1 14.03±0.96 （Macintyre et al. 1995） Radon from atmospheric loss Bq·d−1 （6.50±0.45）×108 Equation (1) Decay of radon Decay constant of radon d−1 0.181 （Wang et al. 2020） Radon inventory (I222) Bq 1.37×1010 Product of storage and the concentration of radon in lake Decay from radon Bq·d−1 （2.49±0.17）×109 Equation (1) Sediment diffusion Radon concentration in pore water (Ceq) Bq·m−3 15102.7±1744.47 Assumed to be equal to groundwater Radon concentration in bottom lake (Cwb) Bq·m−3 163.88±12.59 Measured in the field Radon molecular diffusion coefficient (Ds) cm2·s−1 4.09×10−6 （Ullman and Aller, 1982） Porosity (θ) Dimensionless 0.38 Empirical value according to lithology Sediment diffusive flux (Fdiff) Bq·m−2·d−1 37.78±4.41 （Martens et al. 1980） Radon from sediment diffusion Bq·d−1 （1.89±0.22）×109 Equation (1) Decay of radium Decay of radium d−1 1.37×10−11 （Huang, 2019） Radium inventory (I226) Bq 8.70×109 Product of storage and the concentration of radium in lake Radon from radium decay Bq·d−1 0.12±4.77×10−3 Equation (1) River input Radon concentration in river (222Rnin) Bq·m−3 337.50±102.57 Measured in the field River inflow flux (Qin) m3·d−1 7084.80±574.78 Measured in the field Radon from river input Bq·d−1 （2.39±0.75）×106 Equation (1) Groundwater input Radon concentration in groundwater (222Rngw) Bq·m−3 15102.7±1744.47 Measured in the field Groundwater recharge (Qgw) m3·d−1 8.27×104 Radon from groundwater input divided by its concentration Radon from groundwater input Bq·d−1 （1.25±0.28）×109 Equation (1) 
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