Effective Storage Rates Analysis of Groundwater Reservoir With

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Water and Environment Journal. Print ISSN 1747-6585

Effective storage rates analysis of groundwater reservoir with surplus local and transferred water used in Shijiazhuang City, China Shanghai Du1,2, Xiaosi Su1,2 & Wenjing Zhang1,2

1Key Laboratory of Groundwater Resources and Environment, Ministry of Education, Jilin University, Changchun, China and 2Institute of Water Resources and Environment, Jilin University, Changchun, China

Keywords Abstract effective storage rate; fuzzy mathematics; Groundwater reservoir (GR) of both local precipitation and surplus water transferred groundwater reservoir; Hutuo River. from the Han River Basin is an effective method to prevent further lowering of the Correspondence groundwater table. In this study, when the different volumes of infiltration water X. Su, Institute of Water Resources and from the fuzzy mathematical analysis were input in the simulation, the rate at which Environment, Jilin University, Changchun the groundwater table rose ranged from 1.47 to 3.45 m/a. The effective storage rate 130021, China. Email: [email protected] (ESR) values of GR and the local reservoir was calculated, and ranged from 80.50 to 90.95% and from 49.66 to 80.90%, respectively. In GR, the ESR decreased as doi:10.1111/j.1747-6593.2012.00339.x artificial recharge increased. Comparison of the ESR values between local reservoir and GR showed that if the volume of artificial recharge water available was < 7.86 ¥ 108 m3/a, then GR was a better storage method than the local reservoir. According to our results, this situation would occur 80.30% of the time.

recharge water resources (Shivanna et al. 2004; Peter 2005). Introduction Because of the purification that occurs in the unsaturated Groundwater reservoir (GR) is a popular water resources zone, some sewage can also be used for GR (Sheng 2005). management method in China, and it refers to the water Groundwater modelling has been used to analyse and conservancy in available porous media under artificial control improve proposed GR schemes (Sanford 2002). In GR applica- for water storage and exploitation (Li 2007). An adequate tions, numerical models are used almost exclusively (Pliakas supply of good-quality water is an essential requirement for et al. 2005). the development and survival of any society. While the avail- In addition to suitable infiltration rate and water storage ability and quality of surface water is generally uncertain, GR conditions, sufficient water supply is important for effective provides a natural, reliable and often cheap way to transform regulation and storage. However, in areas where water is questionable surface water into a safe underground resource scarce, local water resources alone cannot be used to resolve (Huisman & Olsthoorn 1983). Underground storage via GR, water supply problems. Combination of local water with that where possible, may be an efficient, environmentally friendly transferred from other areas is becoming increasingly impor- solution to water storage (ASCE 2001). tant in modern city water supply systems. The source area Storage space, infiltration rate and infiltration water and supply area are usually located in different climatic resources are the main factors to be evaluated for GR. The GR zones, and precipitation changes with the different charac- concept has been extended to the storage of either treated teristics of region, which produces many uncertainties in the or untreated surface water or reclaimed wastewater in a suit- parameters of the local water and transferred water. Analysis able aquifer through a system of spreading basins, infiltration of situations with abundant and scarce water for GR will be galleries and recharge wells (Sheng 2005). Several infiltrate fundamental for the construction and administration of GR. techniques, such as injection wells, old streambeds, infiltra- In this study, a simulation model was used to provide infor- tion ponds or surface drainage system, are documented in mation on the volume of water that could be recharged into the scientific literature (Khepar et al. 2009; Bouwer 2002; Han cone of depression at Shijiazhuang, and how the level of the 2003; Pliakas et al. 2005). Local flooding from rain, storms, groundwater table would vary during infiltration. The results surplus water reservoirs and recycled water are important could be used to ensure sustainable supply of the aquifer and

Water and Environment Journal 27 (2013) 157–169 © 2012 CIWEM. 157 Effective storage rates analysis of groundwater reservoir S. Du et al. to decrease the rate at which the groundwater table is low- resources available and social demand means that there is a ering. However, Shijiazhuang and the Han River Basin are large local water shortage that will be impossible to resolve located in different climate regions, and the combined without external input. Development of the cone of depres- amount of water available from these sources is a key factor sion is shown in Figs 3 and 4. The middle section of the for the GR project in this area. Because uncertainty in the South-to-North Transfer Water Project was constructed as a infiltration rate would affect the accuracy of the simulation solution to water resources shortages on the North China model on an increased scale, a field-scale infiltration test was Plain. The South-to-North Transfer Water Project can carry carried out to solve the parameter uncertainty problem. > 100 ¥ 108 m3/a of surface water from the Han River Basin, which is a tributary of the Yangtze River, to cities such as Shijiazhuang. GR could allow full use of this diverted water to Study area resolve water shortages and environment geology prob- Shijiazhuang is the capital of Hebei Province, China (Fig. 1), lems. The excellent storage capacity of the cone of depres- and is located on the alluvial fan of the Hutuo River. The local sion and the infiltration conditions of the riverbed will be reservoir named Huangbizhuang Reservoir is located at the important in the GR project. outlet of the Hutuo River from Taihang Mountain, and is the most important hydraulic project in Shijiazhuang. The bed of the Hutuo River below the reservoir is dry all year, except Construction conditions of GR during the flood season when it receives surplus water from the local reservoir. The main components of the water trans- Boundary conditions fer network in the area are the Shijin, Yuanquan, Dongming, Because of continual overexploitation of the groundwater, Ximing and main channels of South-to-North Transfer Water the aquifer in the study area forms a relatively independent Project (Fig. 1). The main channel South-to-North Transfer groundwater basin. The western boundary is a weakly per- Water Project was constructed with the aim of resolving meable boundary, the southern and northern boundaries are water shortage problems in Beijing and the surrounding area. near the edge of the Hutuo River alluvial fan, and the eastern This channel is 1273 km long. According to the South-to- boundary is near the watershed of the groundwater. Further- North Transfer Water Project plan, 130 ¥ 108 m3 of surface more, there is a continuous clay layer at the bottom of the water could be transferred from the Yangtze River to Beijing middle Pleistocene, which forms an underground storage and other cities, including Shijiazhuang. space with excellent storage conditions. The annual precipitation in the area is 493 mm, and > 80% of this falls in the flood season from June to September (Fig. 2). During the flood season, any surplus water from the Storage capacity local reservoir acts as the main local water source of artificial Calculation of the storage capacity using the following recharge for the GR. equation is an essential first step for the development of There are two layers in the quaternary aquifer. The upper the GR: layer is Holocene-upper and middle Pleistocene phreatic aquifer, which is the dominant aquifer used to supplement m VV= ∑ μ * the water supply of Shijiazhuang. The lower layer is lower ii i=1 Pleistocene confined aquifer, and is separated from the upper 3 3 layer by a section of continuous clay. where V (m ) is the storage capacity of the GR, Vi*(m)isthe

The Shijiazhuang City has used groundwater as its main volume of vacant underground space for the i grid and mi is water source for a long time. Long-term mismanagement the specific yield of the i grid. and groundwater overdraft have formed a cone of depres- Storage capacity is determined by the specific yield, and sion at the centre of Shijiazhuang. Although earlier ground- the difference between upper and lower groundwater levels. water management slowed the lowering of the groundwater According to historical data (Du 2009), because of the rapid table from 1.60 m/a (in 1975–1985) to 1.05 m/a (in 1985– increase of water demand and groundwater overexploit 2000) (Yang 1987; Lin & Liao 1995), the cone of depression break the local balance between groundwater recharge and has been increasing. As of 2006, the cone of depression had discharge after 1980 in Shijiazhuang City, and the under- an area of 436.5 km2, and at its centre the depth of the ground constructions of the civil service had been designed groundwater table was 52.40 m. Because of the construc- 15 m below the surface in the central Shijiazhuang City, a tion of Huangbizhuang Reservoir and rapid urbanisation of natural local groundwater flow net of 30 June 1980 has been Shijiazhuang City, there was 5.32 ¥ 108 m3 groundwater chosen as the upper limit water level, and the middle Pleis- exploited in 2006, and the groundwater amount available is tocene layer was chosen as the bottom of the GR. Spatial 2.52 ¥ 108 m3/a; the large difference between the local water analysis based on geographic information system was used

Fig. 1. Location of study area.

200

150

100 Precipitation/mm 50

0 Jan. Feb. Mar. Apr. May. Jun. Jul. Aug. Sep. Oct. Nov. Dec. Fig. 2. Monthly average precipitation of study area. Month

Fig. 3. The locations of monitor wells.

in the calculation. As of 1 June 2006, the total storage Infiltration rate capacity of GR was calculated at 106.30 ¥ 108 m3, and the dewatering capacity was calculated as 33.51 ¥ 108 m3. This A section of the bed of the Hutuo River (Fig. 5) was selected demonstrates that the cone of depression has a large water as the recharge site. This section of riverbed was chosen for storage space to accommodate artificial recharge. the following reasons: the infiltration rate at this site is the

Fig. 4. Development of cone of depression.

3.00

2.50

2.00

1.50

1.00 Infiltration Rate (m/d) 0.50

0.00 024681012 Day

Fig. 6. Variation of inﬁltration rates.

Two sections were set at the entrance and exit of the infil- Fig. 5. Locations of infiltration field. tration field for measurement of the infiltration rate. The infiltration rate was calculated using the following equation: highest along the riverbed; the main transfer channel of the VQQQA=−−()12 3 middle section of the South-to-North Transfer Water Project is 3 located near this site; this site is on the edge of the cone of where V (m/d) is the infiltration rate in the riverbed, Q1 (m/d) 3 depression, which means recharge water could rapidly trans- in the volume of water flow into the field, Q2 (m /d) in the 3 fer to the dewatering aquifer; and according to groundwater volume of water flow out of field, Q3 (m /d) is the volume of quality assessments (Ye et al. 2008), this site has less con- water stored above the surface of the field and A (m2)isthe tamination in the unsaturated zone than in other sites along infiltration area. the riverbed, which means it will not reduce the quality of the The average infiltration rates of the field are presented in recharge water during GR. Fig. 6. Because of the capillary press of pores during the A field-scale infiltration test has been carried out to solve wetting process, the initial infiltration rate was 2.50 m/d, and the problem of uncertainty in the infiltration rate, which the press, decreasing with the increasing water content would affect the accuracy of the simulation model. The field rates, decreased by about 40% to 1.5 m/d almost 6 days later; infiltration test was performed at the infiltration site for over when the water occupies the pores along the vertical flow 10 days, from 19 August to 30 August 2009. The total amount path, the infiltration rate has been decreased until a steady of recharge water over this period was 1.15 ¥ 107 m3, and the state, which is stabilised around 1.4 m/d and lasts for 3 days seepage area was about 0.6 km2. during this infiltration test.

Using the infiltration rate of 1.4 m/d, and enlarging the Table 1 Fuzzy probability of abundant–scarce encounters between Han infiltration area to 3 km2 by digging the central area of the River Basin and Shijiazhuang City riverbed, we can calculate that about 10–15 ¥ 108 m3/a of Shijiazhuang City surface water could be recharged into GR. A/% B/% C/% Sum/% Han River Basin I 7.46 9.39 9.10 25.95 II 12.24 23.77 11.67 47.68 Artificial recharge source III 7.10 12.73 6.60 26.43 Sum/% 26.80 45.89 27.37 100 Artificial recharge sources are key factors in the GR construc- Notes: I, II, III means abundant years, plain years and scarce years of Han tion. In this case, the local surplus water from the local reser- River Basin, respectively; A, B, C means abundant years, plain years and voir and water transferred from the Yangtze River by the scarce years of Shijiazhuang City, respectively. South-to-North Transfer Water Project can be used for GR. The fuzzy mathematics calculation of the volume of recharge water available when encountering different combinations of abundant or scarce precipitation conditions in the two ⎧ 0125875pp≤>.%, .% ⎪ regions is described in the following section. P −12. 5 ⎪ 12.% 5<≤P 37 .% 5 ⎪ 25 μ(,pp )= ⎨ ⎪ 1375625.%<≤P .% Data and methodology ⎪887. 5 − P ⎪ 62.% 5<≤P 87 .% 5 ⎩ 25 Conditions of abundant or scarce precipitation for recharge water where m is the subjective degree of precipitation and ranges from0to1,andp is the probability that precipitation will Fuzzy mathematics was formed when the scientists studied occur. the phenomenon in natural; especially, different levels should The possibility of encountering different combinations of be divided by parameter values, which is convenient to either abundant or scarce precipitation at any moment in the researches. However, the limits for the time observation two hydrological areas can be calculated using fuzzy math- series were selected artificially, which would make it difficult ematics as follows: to describe the natural characteristics. To solve these types of problems, the fuzzy mathematics seems to be an appro- N μμ∧ priate method (Yu 2005). ∑()AB i=1 The volume of surplus water available from the local res- F ⋅ = ×100% AB N ervoir is determined by the amount of precipitation that occurs around Shijiazhuang, and the volume of transferred where F refers to the fuzzy possibility, i = 0, 1, 2. . . . ; and N is water available is determined by the amount of precipitation the length of the of precipitation event in years. in the Han River Basin. Therefore, the volume of artificial In this paper, the precipitation for each year from 1956 to recharge water was calculated using different combinations 1998 was used to analyse the possibilities of encountering of abundant and scarce precipitation in Shijiazhuang and the different combinations of abundant or scarce precipitation in Han River Basin. Because precipitation is a random process the two regions (Fig. 7). Nine combinations of either abun- with fuzzy characteristics, fuzzy mathematics was applied to dant or scarce precipitation in the local area, and the transfer evaluate the conditions of abundant precipitation. The follow- water area, are given in Table 1. According to the character- ing equations were applied: istics of the local water resources, when precipitation was scarce in both areas, the volume of surplus water was not ⎧ 1125p ≤ .% sufficient for transfer. We determined that 86.05% of the years ⎪ ⎪37. 5 − p from 1956 to 1998 had conditions that provided sufficient μ(,)pr= ⎨ 12.% 5<

Numerical model ⎧ 1875p ≥ .% ⎪ ⎪p − 62. 5 Hydrogeology conception model μ(,pd )= ⎨ 62.% 5<

2.5

Han River Basin Shijiazhuang City 2

1.5 K

0.5

0 1955 1960 1965 1970 1975 1980 1985 1990 1995 2000 Year Fig. 7. Historical precipitation processions.

Fig. 8. Boundary conditions of simulation area.

middle Pleistocene is half-conﬁned aquifer. However, the clay The western lateral boundaries are formed by the division layer between them is not continuous, and the two aquifers lines between mountainous and plains areas; and the north- can be considered as one phreatic aquifer for the purposes of ern, eastern and southern lateral boundaries are administra- this study. The continuous clay layer between the middle and tive boundaries, which are controlled by the locations of the lower Pleistocene is considered as the bottom of the aquifer. observation wells (Fig. 8).

Groundwater flow numerical model weighted recharge volume of transfer water 5.40 ¥ 108 m3/a. The monthly volumes for transfer water were similar over a In this study, groundwater modelling system was used to year, while those of surplus local water were concentrated in develop a groundwater numerical model. The study area was the flood season. divided into a grid of 25 375 500 m ¥ 500 m squares. Two types of hydrogeology boundaries are presented in Fig 8, Prediction results including the recharge boundary to the west, and the other boundaries are variable head boundaries in all other If the groundwater level as of 1 June 2006 is taken as the initial directions. water level, we can forecast that the surplus water from the The period from 1 June 2004 to 1 June 2005 was selected local reservoir and transfer water from the South-to-North for model identification, and that from 1 June 2005 to 1 June Transfer Water Project will begin to infiltrate the groundwater 2006 was selected for model validation. Each year was from 1 June 2013. The groundwater level will then recover, divided into 12 monthly stresses. and this recovery will be complete on 1 June 2020. Recharge results under conditions of continuous abun- Results and discussion dant, average or scarce precipitation were compared (Fig. 9).

Quantity of artificial recharge Groundwater level recovery According to surplus water data from the local reservoir and Variation in the groundwater level at one point near the centre transfer water data from the South-to-North Transfer Water of the cone of depression was chosen to assess the effect of Project, the volumes of water for artificial recharge could be artificial recharge. The changes in the groundwater level calculated under different encountering cases. According to throughout the forecast period and under different condi- the Huangbizhuang Reservoir office report, the local surplus tions are illustrated in Fig. 8. The groundwater levels of obser- water in abundant precipitation conditions is 3 ¥ 108 m3/a, in vation wells at the end of the forecast period are presented in average precipitation condition the local surplus water avail- Table 3, and the forecast changes in the groundwater level able is 1 ¥ 108 m3/a, and in scarce precipitation no surplus without artificial recharge are presented in comparison. water is available. Correspondingly, according to the transfer These results illustrate that the groundwater level will con- plan, there is about 5.72 ¥ 108 m3/a of water transferred from tinue to decrease until 2013. At this time, the maximum depth the South-to-North Transfer Water Project in abundant pre- of the water table is 61.77 m, which can be compared with the cipitation conditions, 5.64 ¥ 108 m3/a in average conditions surface of the land at 73.59 m. In 2013, the South-to-North and 4.64 ¥ 108 m3/a in conditions of scarce precipitation. Transfer Water Project will begin to transfer water to Shi- The volume of artificial recharge water available under jiazhuang, and this will infiltrate into the groundwater. From nine different conditions was calculated (Table 2). The 2013, we forecast that the groundwater level would increase volume of recharge water available for GR ranged from 4.64 in a manner that was dependent on the volume of artificial to 8.72 ¥ 108 m3/a. The fuzzy possibilities were taken as the recharge. The groundwater level recovery speed was calcu- weights of different precipitation conditions, and the fuzzy lated (Table 4) and ranged from 1.47 to 3.49 m/a without arti- weighted recharge water volume was calculated as ficial recharge, and from 2.28 to 4.24 m/a with artificial 6.66 ¥ 108 m3/a, which included the fuzzy weighted recharge recharge. These results illustrate the beneficial effect of arti- volume of surplus water 1.26 ¥ 108 m3/a and the fuzzy ficial recharge on the groundwater level.

Effective storage rates (ESR) Table 2 The volume of recharge water available under different Artiﬁcial recharge to groundwater will enhance the ground- conditions of abundant or scarce rainfall water level and alter the eastern boundary. When the Shijiazhuang City

ABCTable 3 Forecast results of water level at the cone of depression centre

Han River Basin I Qd 5.72 5.72 5.72 Shijiazhuang City Qs 3.00 1.00 0 A (m) B (m) C (m) sum 8.72 6.72 5.72 Han River Basin I 37.52 32.11 28.67 II Qd 5.64 5.64 5.64 II 37.21 31.99 28.30 Qs 3.00 1.00 0 sum 8.64 6.64 5.64 III 31.50 26.64 22.13 No 2013 13.06 12.28 11.82 III Qd 4.64 4.64 4.64 AR 2020 7.86 7.03 6.13 Qs 3.00 1.00 0 sum 7.64 5.64 4.64 AR, Artiﬁcial Recharge.

Fig. 9. Forecast results of groundwater level in 1 June, 2020.

Table 4 Recovery speed of water level at the cone of depression centre Shijiazhuang City

ABC

V1 (m/a) V2 (m/a) V1 (m/a) V2 (m/a) V1 (m/a) V2 (m/a) Han River Basin I 3.49 4.24 2.83 3.58 2.41 3.22 II 3.45 4.19 2.82 3.56 2.35 3.17 III 2.63 3.38 2.05 2.80 1.47 2.28

Notes: V1 means the recovery speed under no artiﬁcial recharge in 2020; V2 means the recovery speed under artiﬁcial recharge in 2020.

Fig. 9. Continued

groundwater level exceeds the level outside of GR, the of water that can be stored by GR is defined as the effective boundary will convert from an inflow to outflow boundary. stored water. The ratio between this and the volume of The outflow water could be estimated by the specific yield recharge water is the ESR. The ESR of GR was calculated with and groundwater level difference between pre- and post-GR different volumes of recharge water (Table 6). The ESRs periods. The outflow water volumes calculated under differ- ranged from 80.50 to 91.95%. Under condition I-A, the ESR ent precipitation conditions are shown in Table 5. The volume was 80.50%, and the maximum outflow water volume was

Table 7 The effective storage rates (ESR) of Huangbizhuang Reservoir 108 m3/a Year 2000 2001 2002 2003 2004 2005 2006 Flow-in 6.99 3.753 2.781 3.273 5.97 3.19 4.34 Loss 2.02 1.71 1.4 1.09 1.14 1.14 1.14 ESR/% 71.10 54.41 49.66 66.70 80.90 64.26 73.73

=+ QQAB Q

Where QA means the part of recharge water used in

smoothing the cone of depression, and QB means the other part of water. According to the Darcy’s Law, because of the lag effect of

aquifer, when we multiple the QB, the gradient increasing with

the same magnitude, which means that the QB is respectively to the volume of water discharged, the more water recharged, the more water discharged through the down-

stream boundary. In this study, the QA is a constant volume,

the percent of QA will decrease as the Q increases, which

means that the percentage of QB and the volume discharged increased, and the ESR of artiﬁcial recharge reduced. Fig. 9. Continued

Comparison of the ESR of the local reservoir Table 5 Lateral discharge of groundwater reservoir and GR Shijiazhuang City The ESRs of GR were compared with those of the upstream A B C local reservoir as an example of a surface water reservoir. (108 m3/a) (108 m3/a) (108 m3/a) According to the local reservoir data, the main losses of Han River Basin I 1.70 0.96 0.89 water occur through evaporation from the water surface and II 1.61 0.88 0.84 seepage into groundwater from the reservoir. The ESR of the III 1.28 0.65 0.42 local reservoir was calculated for each year between 2000 and 2006 (Table 7). The average ESR of the local reservoir at 65.82% (range 49.66–80.90%) was much lower than the Table 6 The effective storage rates of groundwater reservoir average ESR of GR. In contrast to the ESR of GR, as the volume Shijiazhuang City of artificial recharge increased, the ESR of the local reservoir increased. A B C The results for the local reservoir are also plotted in (%) (%) (%) Fig. 10, and intersected with the GR results at a recharge Han River Basin I 80.50 85.71 84.44 8 3 II 81.37 86.75 85.11 volume of 7.86 ¥ 10 m /a. From this three cases of optimal III 83.25 88.48 90.95 water storage were determined as follows: (a) if the volume of artificial recharge water was < 7.86 ¥ 108 m3/a, then GR is the best storage method; (b) if the volume of artificial recharge 1.70 ¥ 108 m3/a. By contrast, under condition III-C the ESR water is 7.86 ¥ 108 m3/a, then both GR and the local reservoir was 90.95% and the minimum outflow water volume was are suitable for storage; and (c) if the volume of artificial 0.42 ¥ 108 m3/a. recharge water is > 7.86 ¥ 108 m3/a, then the local reservoir The artificial recharge water and ESR had a stochastically should be used for storage. linear correlation (Fig. 10). As the volume of artificial recharge The results in Table 5 indicate that the artificial recharge water increased, the ESR decreased. This occurs because of volume will exceed 7.86 ¥ 108 m3/a in conditions I-A and I-B. the increase in the volume of artificial recharge water which According to Table 4, GR should be a superior storage would raise the groundwater levels around the recharge site. medium to the local reservoir 80.30% of the time. In consid- The volumes of artificial recharge water Q could be divided eration of the potential environmental and geological impact, into two parts: although the local reservoir would be a better storage

100

70 ESR/% 60 Hutuo River Groundwater Reservoir 50 Huangbizhuang Reservoir

40 Fig. 10. Correlation between effective storage rates (ESR) and amount of groundwater 2345678910 4 3 reservoir. Artificial Recharge Water/10 m /a

medium than GR the remaining 19.7% of the time, GR should underground dam at the discharge boundary could also still be the first choice for storage of surplus water resources. improve the ESRs of GR. The loss of water from GR through discharge boundary could be decreased or eliminated by construction of underground dams. Acknowledgement We appreciate the anonymous reviewer for their comments during the review process, which greatly improve the quality Conclusions of this paper. This work was supported by the Chinese (1) Spatial analysis showed that the dewatering aquifer National Science Fund Project (NSFC41073054) and Interdis- offered a large total storage capacity (106.30 ¥ 108 m3) and ciplinary projects funds for PhD research in Jilin University had a dewatering capacity of (33.51 ¥ 108 m3). Field tests (2011J012). showed the infiltration rate (1.4 m/d) was excellent for water storage. With this infiltration rate and an increased infiltration To submit a comment on this article please go to area (3 km2), about 10–15 ¥ 108 m3 of surface water could be http://mc.manuscriptcentral.com/wej. For further information, please injected into the underground aquifer every year. see the Author Guidelines at wileyonlinelibrary.com (2) Additionally, fuzzy mathematical analysis of the different combinations of abundant and scarce surplus water from References local and transferred sources showed that the volume of ASCE. (2001) Standard guidelines for artificial recharge of ground surplus water (4.64–8.72 ¥ 108 m3/a) was adequate for water. Environmental and Water Resource Institute, American recharge of the groundwater reservoir by GR. Simulation Society of Civil Engineering (ASCE), EWRI/ASCE 34-01, USA. results showed that this artificial recharge could effectively Bouwer, H. (2002) Artificial Recharge of Groundwater: Hydrogeol- increase the level of the groundwater table at a rate of 1.47– ogy and Engineering. Hydrogeol. J., 10 (1), 121–142. 3.45 m/a after 2013. These results indicate that GR could be Du, S.H. (2009) Simulation of artificial recharge effects in Hutuo effectively implemented in this area. River groundwater reservoir. Master Paper, Jilin University, (3) A key issue in water resource management for Shi- China. jiazhuang is whether to store surplus water in the local Han, Z. (2003) Groundwater Resources Protection and Aquifer reservoir or by GR. The ESRs of GR and the local reservoir Recovery in China. Environ. Geol., 44, 106–111. were 80.5–91.95% and 49.66–80.90%, respectively. GR was a Huisman, L. and Olsthoorn, T.N. (1983) Artificial Groundwater better use of the surplus water than the local reservoir Recharge. Pitman Advanced Publishing Program, London. Khepar, S.D., Yadas, A.K., Sondhi, S.K. and Sherring, A. (2009) when the volume of artificial recharge water available was Modeling Surplus Canal Water Releases for Artificial Recharge < 7.86 ¥ 108 m3/a. This situation should occur 80.30% of the of Groundwater through Surface Drainage Systems. Irrigat. time. Otherwise, local reservoir is the better choice, but Sci., 19, 95–100. comes with a higher cost. To further evaluate water storage Li, Y.G. (2007) Groundwater Reservoir Construction Research. in this area, reduction or elimination of water resource loss China Environmental Science Press, Beijing. via evaporation of the surface reservoir or lateral discharge Lin, X.Y. and Liao, Z.S. (1995) Groundwater Management. from the groundwater boundary should be investigated. An Geological Publishing House, Beijing.

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