Hydrochemistry and Isotope Hydrology for Groundwater Sustainability

Hindawi Geoﬂuids Volume 2017, Article ID 7080346, 19 pages https://doi.org/10.1155/2017/7080346

Research Article Hydrochemistry and Isotope Hydrology for Groundwater Sustainability of the Coastal Multilayered Aquifer System (Zhanjiang, China) Pengpeng Zhou,1 Ming Li,2 and Yaodong Lu3 1

Key Laboratory of Shale Gas and Geoengineering, Institute of Geology and Geophysics, Chinese Academy of Science, No. 19 Beitucheng West Road, Chaoyang District, Beijing 100029, China 2 Appraisal Center for Environment and Engineering, Ministry of Environmental Protection, No. 28 Anwaibeiyuan Road, Chaoyang District, Beijing 100012, China 3 The First Hydrogeological Team, Guangdong Geological Bureau, Kangning Road, Chikan District, Zhanjiang 524049, China Correspondence should be addressed to Pengpeng Zhou; [email protected] Received 18 May 2017; Accepted 13 September 2017; Published 19 October 2017 Academic Editor: Tobias P. Fischer Copyright © 2017 Pengpeng Zhou et al. This is an open access article distributed under the Creative Commons Attribution License, which permits unrestricted use, distribution, and reproduction in any medium, provided the original work is properly cited. Groundwater sustainability has become a critical issue for Zhanjiang (China) because of serious groundwater level drawdown induced by overexploitation of its coastal multilayered aquifer system. It is necessary to understand the origins, material sources, hydrochemical processes, and dynamics of the coastal groundwater in Zhanjiang to support its sustainable management. To this end, an integrated analysis of hydrochemical and isotopic data of 95 groundwater samples was conducted. Hydrochemical analysis shows that coastal groundwater is fresh; however, relatively high levels of Cl− , Mg2+ , and total dissolved solid (TDS) imply slight seawater mixing with coastal unconfined groundwater. Stable isotopes (𝛿18 O and 𝛿2 H) values reveal the recharge sources of groundwater in the multilayered aquifer system. The unconfined groundwater originates from local modern precipitation; the confined groundwater in mainland originates from modern precipitation in northwestern mountain area, and the confined groundwater in Donghai and Leizhou is sourced from rainfall recharge during an older period with a colder climate. Ionic relations demonstrate that silicate weathering, carbonate dissolutions, and cation exchange are the primary processes controlling the groundwater chemical composition. Declining trends of groundwater level and increasing trends of TDS of the confined groundwater in islands reveal the landward extending tendency of the freshwater-seawater mixing zone.

1. Introduction Increases of both population and water demand in coastal areas have made groundwater an important water resource for coastal regions; however, coastal groundwater is vulnerable to overexploitation and contamination [1, 2]. Therefore, sustainable management of coastal groundwater has become a critical issue [3]. Understanding the hydrochemical characteristics of coastal groundwater could provide guidance for sustainable groundwater management [4–6]. The characteristics of groundwater chemistry are primarily influenced by recharge water chemistry, water-rock interactions, solute transport, and chemical processes occurring along the flow paths [6–10]. By analyzing the hydrochemical

and isotopic data together with considering the hydrogeological conditions, the origins, chemical compositions, and dominating hydrochemical processes (e.g., water-rock interactions, evaporation, and mixing between different water) of groundwater in aquifers can be assessed comprehensively [11– 14]. In hydrogeological studies about the coastal groundwater management, analysis of the hydrochemistry and hydrogenoxygen isotopes data has been used widely to determine the hydrogeological conditions, such as groundwater recharge sources, recharge rates, and flow patterns [15–20]. The application of chemistry and hydrogen-oxygen isotopes can be used also to identify processes of groundwater salinization induced by seawater intrusion [21–25]. In addition, many

2 other isotopes (e.g., radium, carbon, chlorine, boron, and strontium) have been used as tracers for characterizing the hydrogeological conditions and hydrochemical processes in coastal aquifers, specifically identifying submarine groundwater discharge and describing seawater intrusion [10, 13, 26, 27]. This study focused on the coastal multilayered aquifer system (including three layers of aquifer and two layers of aquitard) of Zhanjiang, which is located in the southwest of Guangdong Province, China (Figure 1). The groundwater in the middle and deep confined aquifers (Figure 2) has been the sole source of drinking water for the population of the city of Zhanjiang since the 1960s. According to the water resources bulletin of Zhanjiang, groundwater pumping amount has been about 2.2 × 108 m3 /a for the resident population and local industry in recent years. Because of this intense exploitation of groundwater, the confined groundwater level has dropped to about 20 m below sea level since the 1990s [28, 29] (Figures 3(b) and 3(c)). Recent investigations have shown that the groundwater in this multilayered aquifer system remains fresh, but parts of the unconfined groundwater in island areas (e.g., Donghai and Naozhou) and small parts of the confined groundwater in Naozhou island have suffered seawater intrusion [30–33]. It is a concern that the confined groundwater in Zhanjiang city will be risky in suffering from seawater intrusion in the future. Therefore, it is necessary and urgent to conduct a research to identify the origins, mineralization processes, and hydrochemical dynamics of the coastal groundwater to assess the risk of seawater intrusion. The main objective of this study is to identify the origins, material sources, and hydrochemical processes of the groundwater in the coastal multilayered aquifer system of Zhanjiang through integrated analysis of hydrochemical and isotopic data. In addition, the risk of seawater intrusion into the confined groundwater is assessed by analysis of the dynamic data of groundwater level and hydrochemistry. The results will contribute to generate scientific information for the local coastal hydrogeology and be supportive for the sustainable management of the groundwater in this multilayered aquifer system.

2. Study Area and Its Hydrogeology Condition Zhanjiang city with a land area of 1491 km2 is located in southwestern Guangdong, China (Figure 1). The topography is high in the northwest and low in the south. The average annual precipitation and evaporation are 1347 and 1774 mm, respectively [29, 32]. The geology of the study area mainly consists of continental and marine sediments of upper Tertiary-Quaternary age overlying a basement of muddy sandstone of Cretaceous age (K2 ). According to earlier geological investigation [29, 35, 36], the sedimentary formations are characterized by five stratigraphic units, which include Holocene stratum (sand and clay), Beihai Group of middle Pleistocene age (Q2 b, sand with gravel in the lower portion and clayey sand in the upper portion), Zhanjiang Group of lower Pleistocene age (Q1 z, coarse sand with gravel and scattered lenses of clay), Xiayang Group of Pliocene age (N2 x, medium to coarse sand

Geofluids with gravel and thin layers or scattered lenses of clay), and Weizhou Group of Miocene age (N1 w, silty sand and fine sand with clay). These geological formations are intercalated with basalt and pyroclastic rock. The sediments mentioned above constitute the multilayered aquifer system that includes three aquifers (the unconfined aquifer, the middle confined aquifer, and the deep confined aquifer) separated by clay layers (aquitards) (Figure 2). The unconfined aquifer is about 30-m thick and is composed of deposits of Holocene age, Beihai Group of middle Pleistocene age, and upper portion of Zhanjiang Group of lower Pleistocene age. This aquifer overlies a thick layer of clay that extends laterally under the seabed. The hydraulic conductivity (𝐾) of this unconfined aquifer is 5–25 m/d. Because exploitation of the unconfined groundwater is scattered and intermittent, the groundwater flow field remains an approximately natural flow regime with the water table above the mean sea level (Figure 3(a)). The groundwater, which is recharged mainly by rainfall infiltration and discharged through evaporation and runoff to the ocean, flows radially from the watershed to the ocean (Figures 2 and 3(a)). The middle confined aquifer is composed of Zhanjiang Group deposits of lower Pleistocene age (Q1 z), with thickness of about 120 m and hydraulic conductivity (𝐾) of 20–60 m/d. Induced by overexploitation, the groundwater level of this confined aquifer has dropped to −24 to 16 m (Figure 3(b)). The deep confined aquifer is composed of Xiayang Group deposits of Pliocene age (N2 x), with 𝐾 of 20–50 m/d. The groundwater level of the deep confined aquifer has dropped to −22 to −4 m (Figure 3(c)). These two confined aquifers are recharged mainly via lateral runoff and they are discharged by pumping.

3. Sampling and Analysis Method To investigate the hydrochemistry of the groundwater in the multilayered aquifer system of Zhanjiang, 3 times of groundwater sampling activities were conducted from March 2009 to March 2011. As shown in Figure 1 and Table 1, a total of 95 groundwater samples were collected from public supply wells. These comprised 22 samples from the unconfined aquifer (depth < 30 m, sample numbers starting with Q), 35 samples from the middle confined aquifer (50 < depth < 140 m, sample numbers starting with Z), and 38 samples from the deep confined aquifer (depth > 200 m, sample numbers starting with S). All samples were filtered through membranes (0.45-𝜇m pore size) and stored in high-density polyethylene bottles, which were pretreated using deionized water and rinsed using sampled water. Then, the samples were preserved and acidified with HNO3 for cation analysis. All bottles were sealed with wax to ensure a watertight seal. The total dissolved solid (TDS), temperature, and pH were measured in situ using a portable multiparameter water analyzer (Hach, Sension156). The concentration of HCO3 − was also determined in the field via titration on the day of sampling. The major cations (K+ , Ca2+ , Na+ , and Mg2+ ) were analyzed by Inductively Coupled Plasma Mass Spectrometry (ICP-MS, pHPerkin-Elmer Sciex Elan DRC-e) at the Institute of Geology and Geophysics, Chinese Academy

Geofluids

3 N

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Beijing China Guangdong Province Guangdong

(km)

South China sea

1000

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(a) Hong Kong

Study area

South China sea

(km) 0

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S8 Z9

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S12

S2 Z7 S6 Z6 S5 S4 Z5 Q6

Q3 S9

Z1 Z1

Q7 S1

S11

1

Z4

Q4

Z11 S7

Sampling site of the unconfined groundwater Sampling site of the middle confined groundwater Sampling site of the deep confined groundwater Samples of the unconfined groundwater (observed by Zhang et al. [34]) Samples of the confined groundwater (observed by Zhang et al. [34])

20

S3

Hydrogeology cross-section

B

Z10 Q9 Z13 S14 Z14 S10

Q2 Donghai island

7 14 6

Z12 1

S13

Leizhou

7 6 41 14 18 1 3 20 38 45 30 21 34 22 28 26 23

0

(km) 4 (c)

8

Naozhou

41

18

3

20

Naozhou 38

30

45 21

34 28

22

26

23 (d)

Figure 1: Location map of Zhanjiang (Line A-B illustrates the location of the hydrogeological cross-section displayed in Figure 2).

4

Geofluids Precipitation infiltration A 52 S60

B Withdrawals

L34-1

１4

0

L12

L16

①

１2 ＜

S19

L30

Sk7 Sk10

L19

South China sea

１1 z

(m)

−100

②

−200 ③

．2 Ｒ −300

Є 2-3 ．1 Ｑ

−400 ＋2

476.0 Ｇ

(km) 0

5

Holocene (sand) Holocene (sandy clay) Beihai group of middle Pleistocene age １2 ＜ (sand with gravel) Zhanjiang group of lower Pleistocene age １1 Ｔ (coarse sand with gravel) Xiayang group of Pleistocene age ．2 Ｒ (medium to coarse sand with gravel)

1065.3 Ｇ

884.4 Ｇ

Upper cretaceous age ＋2 (muddy sandstone) Middle-upper Cambrian age Є 2-3 (metamorphic sandstone) L30

Clay Borehole Aquifer boundary

①

Unconfined aquifer

860.8 Ｇ

＋2

②

Middle confined aquifer

③

Deep confined aquifer Aquitard (clay layer) Groundwater flow Leakage

Weizhou group of Miocene age ．1 Ｑ (silty-fine sand)

Figure 2: Hydrogeological cross-section (Line A-B in Figure 1) of the study area.

of Sciences (IGGCAS). The anions (Cl− , SO4 2− , and NO3 − ) were measured by Ion Chromatography System (Dionex, ICS-1500) at IGGCAS. Dissolved silica (SiO2 ) was analyzed by spectrophotometry using the molybdate blue method. The charge balance (𝐸 = (∑ 𝑚𝑐 − ∑ 𝑚𝑎 )/(∑ 𝑚𝑐 + ∑ 𝑚𝑎 ) × 100%, where 𝑚𝑐 is the milligram equivalent of the cations and 𝑚𝑎 is the milligram equivalent of the anions) varied from −4.97% to 4.95% (within ±5%), with an average of −1.84% (within ±5%). This balance number can indicate the accuracy of the data. The analyses of stable oxygen (18 O), hydrogen (2 H), and sulfur (34 S) isotopes were conducted using mass spectrometers (Finigan MAT 253 for 18 O-2 H and Delta S for 34 S) at the Stable Isotope Laboratory, IGGCAS. The isotope ratios (𝛿18 O, 𝛿2 H, and 𝛿34 S) were given in the usual 𝛿-units calculated with respect to standard sample: 𝛿sample = ((𝑅sample /𝑅standard ) − 1) × 1000(‰), in which 𝑅sample and 𝑅standard represent the ratio of heavy to light isotopes of the sample and standard,

respectively. The results of the stable isotope are shown in Table 2. In this study, first, according to the groundwater chemical and isotopic data (Tables 1 and 2), statistical analyses (including general statistics and Pearson correlation analysis) and Piper diagram were used to illustrate the general hydrochemical characteristics (e.g., groundwater composition, dominating ions, and groundwater type) (Table 3 and Figure 4) and to assess the correlation between the hydrochemical compositions (Table 4) in the groundwater of this multilayered aquifer system. Second, isotope analyses, Gibbs plots, and bivariate analyses of the compositions were conducted to determine the origins, controlling physical/chemical processes and material sources of the groundwater. Third, based on the understanding of the groundwater origins and the controlling processes, the groundwater dynamics were analyzed to assess the risk of seawater intrusion into this coastal aquifer system.

Geofluids

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Depression cone of the confined groundwater

Depression cone of the confined groundwater

Observation well of the unconfined aquifer

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Observation well of the middle confined aquifer

Groundwater level

−8

Groundwater level

(a)

(b)

L24-3

−8

Observation well of the deep confined aquifer Groundwater level (c)

Figure 3: Groundwater level contour maps for the multilayered aquifer system: (a) the unconfined aquifer, (b) the middle confined aquifer, and (c) the deep confined aquifer.

4. Results 4.1. Groundwater Hydrochemistry. Understanding the characteristics of groundwater chemistry is the base to identify the groundwater origins and the hydrochemical processes occurring in the aquifer. The hydrochemical data of groundwater in the multilayered aquifer system of Zhanjiang are presented in Table 1, and the statistical results of those data are presented in Table 3. As shown, the TDS of the unconfined groundwater varies from 149 mg/L to 823.39 mg/L with a mean value of 360.28 mg/L; that of the middle confined groundwater ranges from 64.31 mg/L to 252.94 mg/L with an average value of 124.47 mg/L; and that of the deep confined groundwater changes from 99.52 mg/L to 325.98 mg/L with a mean value of 158.01 mg/L. These low values of TDS indicate that the groundwater in this aquifer system is mainly fresh (TDS < 1000 mg/L). According to the hydrogeological conditions of this aquifer system, it can be concluded that the approximately natural flow regime of the water table above the mean sea level (Figure 3(a)) is the primary reason why most of the unconfined groundwater has not become salinized. Furthermore, the confined aquifer’s roof with extremely low permeability prevents seawater intrusion into the confined groundwater. The pH value of the unconfined groundwater varies from 4 to 8.25 with an average value of 6.04; that of the middle confined groundwater changes from 4.15 to 7.34 with an average value of 6.25; and that of the deep confined groundwater ranges from 5.34 to 7.81 with an average value of 6.72. Therefore, the groundwater is generally acidity. The average concentrations of major cations in the unconfined and the middle confined groundwater follow the order of

Na+ > Ca2+ > K+ > Mg2+ , and those of the major anions follow the order of HCO3 − > Cl− > SO4 2− > NO3 − (Table 3). The average concentrations of major cations in the deep confined groundwater follow the order of Na+ > K+ > Ca2+ > Mg2+ , and those of the major anions follow the order of HCO3 − > SO4 2− > Cl− > NO3 − (Table 3). The relations between the major ions and TDS are useful for interpreting the major hydrogeochemical evolution processes occurring in the aquifer and for deducing the material sources of the ions in the groundwater [37–39]. In this study, correlation coefficients were calculated to represent the relations between TDS and the major ions (Na+ , K+ , Ca2+ , Mg2+ , HCO3 − , NO3 − , Cl− , and SO4 2− ). As shown in Table 4, the correlations between TDS and the major ions are not strong (correlation coefficients < 0.900), which indicates no single ion can take dominant role in groundwater mineralization. This result also implies that the dissolution of various minerals together constitutes the groundwater composition. 4.2. Groundwater Types. Piper diagram can help to understand the groundwater type and the potential hydrochemical processes controlling groundwater chemistry [40]. According to the concentrations of major ions shown in Table 1, the Piper plot was made (Figure 4). As shown, the unconfined and middle confined groundwater show a relatively large range in the rhombus area (areas I and II). The unconfined groundwater is characterized by HCO3 -Ca⋅Na, HCO3 ⋅Cl-Ca⋅Na, Cl⋅SO4 -Na⋅Ca, and Cl-Na⋅Ca⋅Mg hydrochemical types. With comprehensive consideration of the

Q1 Q2 Q3 Q4 Q5 Q6 Q7 Q1 Q2 Q3 Q4 Q5 Q6 Q7 Q8 Q1 Q2 Q3 Q4 Q5 Q6 Q7 Z1 Z2 Z3 Z4 Z5 Z6 Z7 Z8 Z9 Z10 Z11

Sample number

Mar 2009

Mar 2010

Mar 2011

Mar 2009

Unconfined aquifer

Unconfined aquifer


Sampling time

Unconfined aquifer

Aquifer

Ca2+ (mg/L) 17.86 15.4 12.91 77.37 52.58 105.15 18.36 13.89 41.66 27.78 70.42 25.54 76.39 15.37 9.42 13.21 43.51 28.84 33.57 29.82 74.29 16.61 7.43 3.47 7.24 4.47 10.9 4.57 6.49 2.48 7.94 8.44 7.43

Mg2+ (mg/L) 6.91 70.67 5.71 23.75 6 15.64 8.42 6.32 21.65 1.8 19.55 4.81 23.75 8.13 8.81 7.4 22.82 4.45 8.51 16.2 21.04 7.7 3.32 1.2 3.61 4.51 6.32 4.81 4.81 3.91 6.01 7.22 2.71

Na+ (mg/L) 31.24 17.74 51.38 46.58 27.12 101.81 28.26 29.93 105.21 26.17 37.78 46.13 93.39 20.82 10.06 32.03 105.67 21.27 6.54 16.2 78.99 19.69 11.43 7.56 3.97 20.02 11.42 8.14 7.94 5.35 8.87 12.62 20.63

K+ (mg/L) 6.45 45.63 6.59 146.6 13.68 41.68 1.4 7.19 14.93 13.06 22.63 14.34 120.75 1.77 3.39 8.09 17.54 13.73 23.22 13.53 15.84 1.82 10.04 1.8 7.28 8.01 6.43 4.62 4.62 3.66 1.45 9.36 6.09 61.02 5.98 46.13 22.33 80.36 5.45 58.56 7.44 68.46 44.67 93.79

5.34 54.25 142.37 110.09 162.68

69.33

9.39 5.39 52.54 195.57 118.26 131.38

HCO3 − (mg/L) 13.42 5.98 171.16 206.86 145.84 324.44

Cl− (mg/L) 49.77 183.35 19.21 111.77 32.29 154.56 40.16 50.16 193.66 34.24 88.16 28.25 186.75 29.1 8.44 53.39 203.94 27.12 10.48 17.74 137.4 28.89 12.23 12.23 2.62 27.93 10.49 13.08 6.1 7.87 5.25 28.82 6.98 SO4 2− (mg/L) 35.64 58.26 14.26 160.47 29.73 85.59 67.77 34.49 116.52 30.93 26.13 36.84 172.38 74.88 19.34 46.88 60.9 44.52 30.02 45.59 115.99 70.27 2.4 8.31 13.06 26.13 4.75 36.09 7.11 23.77 2.4 19.02 1.2 0.2

0.1

1.5

0.3

NO3 − (mg/L) 45 100 0.5 95 40 32.5 30 12.5 55 30 75 40 80 2 5 35 120 32.5 2 18 50 10 0.1 3

Table 1: Hydrochemical data of groundwater in the multilayered aquifer system of Zhanjiang. SiO2 (mg/L) 12.93 10.49 25.65 13.92 8.92 10.91 11.05 12.93 8.75 9.65 8.37 9.34 3.93 11.17 9.62 13.43 15.26 9.11 11.81 15.46 3.83 10 23.69 14.62 41.83 29.09 43.35 27.57 35.08 24.42 29.31 23.68 27.16

TDS (mg/L) 216.32 532.23 222.45 783.93 283.76 710.27 207.7 202.04 563.74 200.06 453.44 264.51 823.39 164.34 149 213.4 593.6 208.86 200.16 187.8 579.21 166.04 113.88 64.31 109.88 136.88 138.67 132.44 110.47 76.46 97.49 144.74 120.72

5.3 5.06 7.55 8.14 7.03 7.27 4.08 5 4.87 6.43 8.25 7.15 6.72 4 5.52 4.36 4.65 6.26 7.15 6.89 7.01 4.1 6.7 5.4 6.49 6.1 6.78 5.36 6.4 5.55 7.34 6.25 7.19

pH

𝑇 (∘ C) 23 26 23 22 25 22 23 23 27 26 22 22 22 25 23 22 25 23 25 23 21 26 28 27 30 27 28 27 28 26 27 28 29.5

6 Geofluids

Z1 Z2 Z3 Z4 Z5 Z6 Z7 Z8 Z9 Z10 Z11 Z12 Z13 Z14 Z1 Z2 Z4 Z5 Z6 Z7 Z8 Z9 Z10 Z11 S1 S2 S3 S4 S5 S6 S7 S8 S9 S10 S11 S12

Sample number

Mar 2010

Mar 2011

Mar 2009


Deep confined aquifer

Sampling time


Aquifer

Ca (mg/L) 9.92 2.48 3.97 3.47 11.91 4.97 9.42 2.97 8.44 9.92 7.43 9.13 8.46 5.8 8.32 3.43 4.89 9.78 4.24 22.48 2.44 7.82 22 4.41 2.97 3.47 4.47 10.33 2.97 6.45 36.21 9.92 22.81 22.87 4.97 4.97

2+

Mg (mg/L) 3.61 1.51 2.41 3.32 5.42 4.2 5.12 2.41 5.71 7.22 2.41 8.11 6.72 4.04 4.43 1.48 3.56 8.3 5.93 3.85 4.74 5.64 10.07 2.07 2.11 3.01 4.51 4.2 2.41 3.61 3.9 4.51 9.93 5.41 3.6 3.3

2+

Na+ (mg/L) 13.67 6.96 7.98 18.71 13.39 8.65 7.51 6.16 9.14 14.81 20.39 6.23 6.44 9.88 10.91 8.91 21.82 11.64 8.24 6.26 7.63 9.58 24.12 18.43 10.82 9.32 19.51 4.67 6.96 8.66 25.25 14.71 44.18 12.4 11.7 7.1

K+ (mg/L) 9.01 2.53 8.61 6.78 6.73 4.62 4.32 4.48 1.63 10 6.75 5.9 4.21 2.74 10.14 2.93 8.16 7.37 5.68 4.74 4.54 1.88 4.27 5.53 11.99 12.34 10.76 8.09 10.17 9.81 14.67 7.04 45.49 10.97 10.15 10 16.29 86.77 7.52 92.2 8.12 67.79 35.27 67.79 49.12 55.04 92.26 65.47 49.28 67 69.56 90.8 247.07 132.47 64.01 53.58

77.37 5.86 61.56 7.32 67.12 52.24 93.42 58.22 53.37 35.61 61.14

HCO3 − (mg/L) 56.4 5.86 47.46

Table 1: Continued. Cl− (mg/L) 26.05 8.58 4.29 38.04 9.5 13.83 6.69 9.43 4.32 31.69 5.99 10.2 8.99 10.74 18.36 13.12 35.88 10.49 14.36 7.87 13.12 3.51 72.64 8.76 5.25 1.74 3.51 4.36 2.62 3.51 37.54 4.36 28.82 6.1 2.62 0.89 SO4 2− (mg/L) 5.96 12.82 5.96 22.57 15.47 34.24 13.06 19.02 7.11 11.91 1.2 22.1 18.06 16.94 7.01 9.37 22.24 14.07 38.18 12.87 24.59 7.01 21.09 4.71 7.11 13.06 7.11 2.4 5.26 8.31 51.1 1.2 11.91 1.2 10.71 13.06 0.3 0.5

3 4

0.2 1

0.3

1 5

0.1

15 0.1

0.3 0.1 0.3 0.1 0.2

0.1

2

NO3 − (mg/L) SiO2 (mg/L) 13.28 16.52 43.28 25.3 38.34 28.01 39.73 24.75 40.19 22.23 26.88 26.84 30.89 29.42 18.02 17.91 37.21 46.38 39.64 43.85 26.7 48.13 10.9 54.11 26.9 25.91 32.95 46.16 40.95 45.94 9.89 34.39 26.26 31.03 54.93 50.26

TDS (mg/L) 125.48 68.53 110.46 124.5 143.7 119.25 124.62 74.6 110.79 146.77 119.44 138 149 150 126.48 73.4 145.36 155.88 151.46 155.07 89.65 119.08 252.94 136.02 100.69 101.03 131.77 117.82 131.82 127 239.1 126.22 323.46 159.68 135.68 124.01 6.69 5.65 6.59 4.15 6.8 5.55 6.6 5.59 6.95 6.52 7.05 6.67 6.34 6.44 6.7 4.38 5.78 6.66 5.62 6.8 5.52 6.83 6.37 6.94 6.51 6.4 6.99 6.84 6.56 6.74 6.3 7.15 6.14 7.3 6.7 6.48

pH

𝑇 (∘ C) 26 28 29 27 29 27 25 27 26 27 30 29 28 28 26 24 27.5 29 25 26 25 27 25 30 32 32 32 32.5 30 30 33 31 31 31 32.5 32

Geofluids 7

S1 S2 S3 S4 S5 S6 S7 S8 S9 S10 S11 S12 S13 S14 S1 S2 S3 S4 S5 S6 S7 S8 S9 S10 S11 S12

Sample number

Mar 2010

Mar 2011


Sampling time


Aquifer

Ca2+ (mg/L) 2.97 2.97 5.95 4.91 2.48 3.97 10.09 9.42 16.87 12.55 12.37 5.95 6.48 7.53 2.93 2.44 9.78 4.89 3.43 4.86 53.35 14.24 14.67 14.17 3.43 6.35

Mg2+ (mg/L) 2.11 2.11 3.3 5.66 2.7 4.2 6.62 4.52 13.22 8.72 2.71 3.61 5.65 5.19 2.08 3.56 3.26 4.74 6.22 3.85 7.41 5.03 13.63 8.3 3.26 5.33

K+ (mg/L) 13.56 13.4 10.44 9.76 10.16 9.91 6.95 8.19 47.81 4.73 12.32 9.97 8.7 14 16.8 12.25 10.28 9.48 4.79 12.28 7.37 10.35 4.85 10.08 11.54 9.94 HCO3 − (mg/L) 54.4 52.33 90.49 69.93 55.47 62.19 176.59 94.89 249.57 97.82 67.12 67.59 61.36 127.83 51.5 53.25 98.97 81.34 5.09 63.7 147.79 98.97 221.33 116.72 65.11 65.45

Table 1: Continued. Na+ (mg/L) 10.89 7.39 20.04 10.61 7.79 9.03 54.47 14.7 46.88 15.87 3.97 9.74 26.06 23.17 10.4 7.37 19.71 10.65 8.23 9.25 12.71 9.78 46.12 17.75 12.31 9.29

Cl− (mg/L) 5.99 3.44 6.91 4.36 0.85 3.44 18.82 3.44 27.65 17.3 3.47 4.29 19.86 2.54 5.25 3.51 7.02 4.36 17.51 2.62 28.89 3.51 21.5 10.49 3.51 15.74 SO4 2− (mg/L) 8.31 5.96 8.31 12.97 3.55 9.51 14.26 2.4 16.62 8.31 7.11 8.31 18.37 6.88 14.07 8.37 8.21 1.15 23.26 9.37 12.87 5.86 7.01 22.24 7.01 2.35 0.2 0.75 0.2

11 4

0.1

0.3 0.2

0.3 0.2

0.2 0.8 1 0.3 0.1 0.1

NO3 − (mg/L) 0.1 SiO2 (mg/L) 27.16 26.17 30.05 43.44 33.57 53.8 24.89 35.71 25.24 48.76 52.93 51.69 32.23 47.28 34.44 29.68 46.66 54.13 40.4 60.03 23.12 46.76 32.22 36.83 60.05 31.92

TDS (mg/L) 110.74 99.52 133.04 132.83 103.84 132.76 226.26 126.46 325.98 170.26 133.09 134.54 214 195 120.82 102.04 161.08 134.54 163.5 140.22 231.54 150.36 281.44 196.66 142.08 123.66

6.64 6.42 6.97 6.74 6.7 6.7 7.81 7.14 6.12 6.72 6.87 6.75 6.68 7.23 6.58 6.42 7.12 6.68 5.34 6.73 7.66 6.99 6 7.03 6.68 6.62

pH

𝑇 (∘ C) 31 32 32 33 30 31 33 30 32.5 31 31.5 31 30 31 32 32 32.5 33 31 31 33 31 35 31 32 32

8 Geofluids

Geofluids

9

Mar 2010

+＃ 2 4 −

３／

− 3

＃／ +（

－Ａ 2+

2 3 −

6.52

＃／

＃Ｆ−

＃；2+ Unconfined groundwater Middle confined groundwater Deep confined groundwater

12.38 13.28

Figure 4: Piper plots of chemical compositions of the coastal groundwater of Zhanjiang. −30

I

−40

17.26

complicated hydrochemical types and relatively high levels of Cl− , Mg2+ , and TDS (i.e., samples Q2, Q4, and Q6, Figure 1 and Tables 1 and 3) of the unconfined groundwater, it can be concluded that slight seawater mixing occurs in the unconfined groundwater near the coastline but that seawater intrusion is still in the initial phase [32]. The middle confined groundwater is characterized by HCO3 Ca⋅Mg⋅Na, Cl⋅HCO3 -Na⋅Ca, and Cl⋅SO4 -Na⋅Ca⋅Mg hydrochemical types. The low TDS values and complicated hydrochemical types of this confined groundwater suggest that water-rock interactions (e.g., mineral dissolution or cation exchange) might occur in the middle confined aquifer. Figure 4 also shows that the deep confined groundwater samples, which are distributed mainly in the bottom-left corner of rhombus area (II), are mainly represented by HCO3 -Na⋅Ca(Mg) hydrochemical type, indicating that deep confined groundwater naturally evolves without any intensive hydrogeochemical process or anthropogenic impact. 4.3. 𝛿18 O and 𝛿2 H Compositions. The stable oxygen (18 O) and hydrogen (2 H) isotopes of groundwater samples are related to the recharge sources, flow paths, and residence times of groundwater. The method of isotope analysis has been used widely in many hydrogeological studies [4, 5, 41, 42]. The

2 （ (% ₀)

−50.1 −49.6 −50.1 −46.5 −53.8 −54.6

II

2−

−7.16 −7.34 −7.45 −7.01 −7.09 −6.9

Mar 2010

I

３／ 4

−44 −48.4 −45.7 −44.8 −46.8 −43.6 −46.1 −51.6 −51.9 −52.9

2+

−6.42 −7.4 −6.7 −6.94 −6.91 −6.58 −7 −6.71 −7.42 −7.05

Ａ +－

−43.7 −38.4 −45.8 −46.5 −39.8 −41.5 −38.8 −45.4

2+

Mar 2010

−6.93 −5.56 −7.05 −6.93 −5.92 −6.49 −5.9 −6.93

𝛿34 S (‰)

+


H (‰)

+＋

S2 S3 S6 S7 S13 S14


2

O (‰)

+

Z2 Z4 Z6 Z7 Z8 Z9 Z11 Z12 Z13 Z14

Unconfined aquifer

18

Sampling time

．；

Q1 Q2 Q3 Q4 Q5 Q6 Q7 Q8

Aquifer

＃；

Sample number

Ｆ−

Table 2: Isotope data of groundwater in the multilayered aquifer system of Zhanjiang.

−50

−60 −8

II

−7

−6 18 ／ (% ₀)

Unconfined groundwater Middle confined groundwater Deep confined groundwater

−5

−4

LMWL (Hong Kong) LMWL (Haikou) GMWL

Figure 5: Stable isotope compositions of groundwater in the multilayered aquifers of Zhanjiang.

analysis results of 𝛿18 O and 𝛿2 H are shown in Table 2 and Figure 5. According to the monthly rainwater data obtained from the GNIP (Global Network of Isotopes in Precipitation) of the IAEA (International Atomic Energy Agency), the local meteoric water lines (LMWLs) of Hong Kong and Haikou weather stations were calculated as 𝛿2 H = 8.28𝛿18 O + 12.78 and 𝛿2 H = 7.50𝛿18 O + 6.18, respectively. Then, these two LMWLs were used as the LMWL of Zhanjiang. As shown in Figure 5 and Table 2, the isotopic compositions of 𝛿2 H and

10

Geofluids Table 3: Statistical results of groundwater chemistry data of the multilayered aquifer system of Zhanjiang.

Unconfined aquifer Middle confined aquifer Deep confined aquifer

Minimum Maximum Average Minimum Maximum Average Minimum Maximum Average

Ca2+ Mg2+ Na+ K+ HCO3 − Cl− SO4 2− NO3 − SiO2 TDS (mg/L) (mg/L) (mg/L) (mg/L) (mg/L) (mg/L) (mg/L) (mg/L) (mg/L) (mg/L)

pH

𝑇 (∘ C)

(Na + K)/Cl

9.42 105.15 37.27 2.44 22.48 7.40 2.44 53.35 9.78

4 8.25 6.04 4.15 7.34 6.25 5.34 7.81 6.72

21 27 23.59 24 30 27.31 30 35 31.67

0.38 4.44 1.58 0.57 6.28 2.22 0.91 25.03 6.95

1.8 70.67 14.55 1.2 10.07 4.59 2.08 13.63 4.93

6.54 105.67 43.36 3.97 24.12 11.30 3.97 54.47 16.04

1.4 146.6 25.18 1.45 10.14 5.63 4.73 47.81 12.14

5.34 8.44 14.26 324.44 203.94 172.38 106.91 76.77 62.61 5.45 2.62 1.2 93.79 72.64 38.18 47.24 14.86 14.62 5.09 0.85 1.15 249.57 37.54 51.1 90.33 9.15 10.13

0.5 120 41.36 0.1 15 1.64 0.1 11 1.21

3.83 25.65 11.21 10.9 54.11 30.52 9.89 60.05 38.28

149 823.39 360.28 64.31 252.94 124.47 99.52 325.98 158.01

Table 4: Correlation matrix between TDS and the major ions. Unconfined aquifer (𝑛 = 22) Ca2+ Mg2+ Na+ K+ HCO3 − Cl− SO4 2− NO3 − TDS Middle confined aquifer (𝑛 = 35) Ca2+ Mg2+ Na+ K+ HCO3 − Cl− SO4 2− NO3 − TDS Deep confined aquifer (𝑛 = 38) Ca2+ Mg2+ Na+ K+ HCO3 − Cl− SO4 2− NO3 − TDS

Ca2+

Mg2+

Na+

K+

HCO3 −

Cl−

SO4 2−

NO3 −

TDS

1 0.188 0.635 0.601 0.734 0.561 0.595 0.451 0.814

1 0.185 0.406 −0.141 0.693 0.346 0.670 0.570

1 0.314 0.196 0.801 0.580 0.503 0.766

1 0.351 0.481 0.758 0.566 0.774

1 −0.036 0.222 −0.126 0.356

1 0.649 0.798 0.881

1 0.473 0.788

1 0.760

1

1 0.554 0.204 0.098 0.550 0.348 −0.173 −0.012 0.715

1 0.085 0.096 0.193 0.391 0.262 −0.194 0.704

1 0.368 0.237 0.648 −0.111 −0.081 0.518

1 0.204 0.294 −0.049 −0.312 0.290

1 −0.239 −0.707 −0.339 0.272

1 0.305 0.152 0.632

1 −0.022 0.217

1 −0.119

1

1 0.431 0.300 0.181 0.503 0.713 0.392 0.795 0.606

1 0.727 0.388 0.826 0.661 0.146 0.267 0.844

1 0.468 0.845 0.656 0.272 −0.018 0.849

1 0.584 0.381 0.162 −0.143 0.569

1 0.564 0.003 0.365 0.851

1 0.630 0.464 0.835

1 0.143 0.425

1 0.463

1

𝛿18 O of the unconfined groundwater vary from −38.40‰ to −46.50‰ (average: −42.07‰) and from −5.56‰ to −7.05‰ (average: −6.40‰), respectively. The isotopic compositions of 𝛿2 H and 𝛿18 O of the middle confined groundwater vary from −43.60‰ to −52.90‰ (average: −47.58‰) and from

−6.42‰ to −7.42‰ (average: −6.91‰), respectively. The isotopic compositions of 𝛿2 H and 𝛿18 O of the deep confined groundwater vary from −46.50‰ to −54.62‰ (average: −50.79‰) and from −6.90‰ to −7.45‰ (average: −7.16‰), respectively.

Geofluids

5. Discussions 5.1. Origin of the Groundwater. For the unconfined groundwater, as shown in Figure 5, all samples (except Q2, Figure 1) plot along the global meteoric water line (GMWL) [43] and LMWL, indicating that the unconfined groundwater is mainly of meteoric origin. In comparison with the other groundwater samples, sample Q2 is relatively enriched in stable isotopes, it deviates slightly from the LMWL (part I in Figure 5), and it is characterized by comparatively high levels of TDS (563.74 mg/L) and a low water table (2.55 m). This might imply that this sample is influenced either by relatively intense evaporation or by slight mixing with seawater in the area near the coastline. For the middle and deep confined groundwater, as shown in Figure 5, the distribution of the confined groundwater samples presents a pattern: the deeper the aquifer depth is, the more depleted the isotopic data are. This pattern may imply that the hydraulic connection between this two confined aquifers is relatively weak. The samples collected in the mainland area (i.e., Zhanjiang city area) are mainly located along the GMWL and LMWL, indicating that the confined groundwater in the mainland area is of meteoric origin. However, the relatively more depleted isotopic data compared to those of the unconfined groundwater implies that meteoric recharge to the confined groundwater is sourced from the mountain area of the north and northwest area, where the precipitation’s isotopic data are more depleted. Meanwhile, the confined groundwater flow fields (Figures 3(b) and 3(c)) certify the occurrence of recharge from the northern and northwestern areas. In addition, the confined groundwater samples collected in the southern and southwestern areas (samples Z13, Z14, and S14 in Donghai and samples Z12 and S13 in Leizhou, Figure 1) are characterized by more depleted isotopic data than samples of the mainland area. These samples deviate significantly from the LMWL and they are distributed to the bottom-left of the LMWL (part II in Figure 5). This indicates that the confined groundwater of the Donghai and Leizhou areas is sourced from rainfall recharge during an older period with a colder climate. From the sulfur isotopes (𝛿34 S) of the groundwater in Donghai (Table 2), it can be concluded that the 𝛿34 S values in groundwater become more enriched with increasing depth. This trend of enrichment of 𝛿34 S values in the confined fresh groundwater of Donghai also demonstrates that the confined groundwater of island is palaeowater. According to the recharge pattern of the confined groundwater in the southern and southwestern areas (Figures 3(b) and 3(c)), we consider that the palaeowater stored in the confined aquifers of Donghai and Leizhou will flow toward Zhanjiang through lateral flow because of the intensive groundwater pumping of recent years. In conclusion, the unconfined groundwater is recharged by local modern precipitation. However, the confined aquifers are recharged by precipitation in northern and northwestern mountain areas and by palaeowater sourced originally from rainfall infiltration during an older time with a colder climate.

11 5.2. Controlling Processes and Material Sources of Groundwater Chemistry. To quantitatively study the controlling processes and material sources of the groundwater in Zhanjiang, Gibbs plots and bivariate analyses of the ionic relations were discussed in this section. 5.2.1. The Dominating Hydrochemical Process. Gibbs plots (i.e., a TDS versus Na/(Na + Ca) graph and a TDS versus Cl/(Cl + HCO3 ) graph) can be used to determine the primary hydrochemical processes (e.g., atmospheric precipitation, rock weathering, and evaporation) controlling groundwater chemistry [44]. According to the hydrochemical data (Table 1), Gibbs plots were made as Figure 6. Those plots indicate that rock weathering is the major mechanism controlling the groundwater chemistry of the multilayered aquifer system of Zhanjiang. This conclusion is coincident with the results deduced from the analysis of groundwater hydrochemistry and groundwater types. 5.2.2. Dissolution Material and Dissolution Process. To identify the dominant mineral in the rock weathering process in this aquifer system, molar ratio bivariate plots of Nanormalized Ca, Mg, and HCO3 were made [45, 46]. As shown in Figure 7, the groundwater of the multilayered aquifer system is mainly influenced by silicate weathering and carbonate dissolution, especially for the confined groundwater. The milligram equivalent ratio of (Na+ + K+ )/C1− can be an indicator of the sources of cations and of the occurrence of silicate weathering, where a ratio greater than 1 implies Na+ released from silicate weathering and a ratio of 1 indicates halite dissolution [47]. As shown in Table 3, the (Na+ + K+ )/C1− ratio values of the unconfined groundwater vary from 0.38 to 4.44 with an average value of 1.58; those values of middle confined groundwater range from 0.57 to 6.28 with an average value of 2.22; those values of deep confined groundwater change from 0.91 to 25.03 with average value of 6.95. These averages (Na+ + K+ )/C1− ratio > 1 indicate the derivation of Na+ and K+ from silicate weathering. Moreover, the increase of the (Na+ + K+ )/Cl− ratio with groundwater depth reveals that the silicate weathering in the confined aquifer is more remarkable than in the unconfined aquifer. Furthermore, the relatively higher concentration of SiO2 (Table 3) in confined groundwater verifies evident silicate weathering in confined aquifers. The scatter plot of C1− versus Na+ + K+ (Figure 8(a)) shows that the unconfined groundwater samples are distributed along the 1 : 1 line (or on either side of this line), which implies that ions (Na+ and K+ ) are mainly resultant from the silicate weathering and halite dissolution. Conversely, most samples of the confined groundwater fall below the 1 : 1 line, indicating that silicate weathering is the primary hydrochemical process in the confined aquifers. In addition, as shown in Figure 8(a), the excess of (Na+ + K+ ) over C1− also implies that cation exchange may occur in the confined aquifers. The plot of (HCO3 − + SO4 2− ) versus (Ca2+ + Mg2+ ) (Figure 8(b)) shows that most samples of fresh unconfined groundwater fall along the 1 : 1 line and that some samples

12

Geofluids

100,000

10,000

1,000

TDS (mg/L)

TDS (mg/L)

10,000

Ev do apo m ra in tio an n ce

Ev do apo m ra in tio an n ce

100,000

100

1,000

100

Rock weathering dominance

Rock weatheringg dominance

n tio ita ce ip an ec in Pr om d

n tio ita ce ip an ec in Pr om d

10

10

1

1 0

0.2

0.4

0.6

0.8

0

1

Na/(Na + Ca)

0.2

0.4 0.6 0.8 Cl/(＃Ｆ + （＃／3 )

1



Figure 6: Gibbs plots of the major ions in the coastal groundwater of Zhanjiang.

100

10

Carbonate dissolution 10

Carbonate dissolution

Silicate weathering

Silicate weathering

Mg/Na

（＃／3 − /Na

1

1

0.1 0.1 Evaporite dissolution

Evaporite dissolution 0.01 0.01

0.1

1 Ca/Na

Unconfined groundwater Middle confined groundwater Deep confined groundwater (a)

10

100

0.01 0.01

0.1

1

10

100

Ca/Na Unconfined groundwater Middle confined groundwater Deep confined groundwater (b)

Figure 7: Bivariate plots of molar ratio. (a) Na-normalized Ca versus Na-normalized HCO3 . (b) Na-normalized Ca versus Na-normalized Mg.

Geofluids

13 8

8

1 : 1 line

1 : 1 line

6 ３／4 2− + （＃／3 − (meq/L)

＃Ｆ− (meq/L)

6

4

4

2

2

0

0 0

2

4

6

8

10

0

2

．；+ + ＋+ (meq/L) Unconfined groundwater Middle confined groundwater Deep confined groundwater

4 6 ＃；2+ + －Ａ2+ (meq/L)

8

10


(a)

(b)

5 1 : 1 line

（＃／3 − (meq/L)

4

3

2

1

0 0

2

4 6 ＃Ｆ− + ３／4 2− (meq/L)

8

10

Unconfined groundwater Middle confined groundwater Deep confined groundwater (c)

Figure 8: Bivariate plots of ionic relation. (a) Cl− versus Na+ + K+ . (b) SO4 2− + HCO3 − versus Ca2+ + Mg2+ . (c) HCO3 − versus (Cl− + SO4 2− ).

fall below the 1 : 1 line, which indicates that the combined dissolutions of carbonate and silicate are the main sources of Ca2+ and Mg2+ in the unconfined groundwater [48]. Most samples of the confined groundwater fall above the 1 : 1 line, which demonstrates that silicate weathering is the main source of Ca2+ and Mg2+ in the confined groundwater [9, 49– 51]. The deficiency of Ca2+ + Mg2+ (Figure 8(b)) and the

excess of Na+ (Figure 8(a)) indicate the occurrence of cation exchange in the confined aquifers. The plot of HCO3 − versus (Cl− + SO4 2− ) (Figure 8(c)) shows that the groundwater samples of the unconfined and middle confined aquifers are distributed on both sides of the 1 : 1 line, which implies that carbonate and evaporite dissolutions are also the main material sources of

14

Geofluids

(Na+ , K+ , Ca2+ , Mg2+ ) silicates + H2 CO3 −

+

+

󳨀→ H4 SiO4 + HCO3 + Na + K + Ca

2+

5

0 Chloroalkaline index (CAI)

the chemical compositions of the unconfined and middle confined groundwater. The groundwater samples of the deep confined aquifer mainly plot above the 1 : 1 line, indicating that carbonate dissolution is another material source of the chemical composition of the deep confined linebreak groundwater. In conclusion, silicate weathering is the dominant process influencing the material source of ions (Na+ , K+ , Ca2+ , and Mg2+ ) in the coastal aquifer system of Zhanjiang. Carbonate and evaporite dissolutions also contribute to the groundwater compositions. With the dissolution by carbonic acid (H2 CO3 ), the general reaction of silicate weathering is

−5

−10

−15

−20

+ Mg

2+

(1)

+ Clay

−25

0

200

400 600 TDS (mg/L)

800

1,000

See [9]. Unconfined groundwater Middle confined groundwater Deep confined groundwater

Figure 9: Plot of the chloroalkaline index (CAI) versus TDS of the groundwater in the multilayered aquifers of Zhanjiang. 2

＃；2+ + －Ａ2+ − ３／4 2− − （＃／3 − (meq/L)

5.2.3. Ion Exchange. As described in Section 5.2.2, most of the confined groundwater samples show an excess of Na+ over Cl+ and a deficiency of Ca2+ + Mg2+ over HCO3 − + SO4 2− , which may indicate the contribution of cation exchange to the groundwater composition [39, 52]. The chloroalkaline index (CAI) of the groundwater samples can be an indicator of the type and the intensity of the ion exchange reactions between the groundwater and the aquifer matrix [53]. The CAI is calculated using the following formulae: CAI = [Cl− − (Na+ + K+ )]/Cl− . Positive and negative values of the CAI indicate reverse cation exchange (2Na+ + Caclay → Ca2+ + 2Naclay ) and cation exchange (Ca2+ + 2Naclay → 2Na+ + Caclay ), respectively. As shown in Figure 9, the CAI values of the confined groundwater, especially that of the deep confined groundwater, are mainly negative, supporting the assumption of the occurrence of cation exchange in the confined aquifers. Meanwhile, the absolute value of the CAI can reflect the intensity of the cation exchange reactions. Figure 9 shows that the absolute CAI values of the deep confined groundwater are greater than the values of the middle confined groundwater, which means that the cation exchange reaction in the deep confined aquifer is more intense than in the middle confined aquifer. In addition, to further investigate the occurrence of cation exchange in the confined aquifers, a bivariate plot of (Ca2+ + Mg2+ − HCO3 − − SO4 2− ) versus (Na+ − Cl− ) can be used [54]. If cation exchange is an important process controlling the groundwater chemistry, the groundwater samples will fall in the lower-right quadrant of this diagram and along a line with a slope of −1. According to the chemistry data, plot of (Ca2+ + Mg2+ −HCO3 − −SO4 2− ) versus (Na+ − Cl− ) was made (Figure 10). Figure 10 shows that most of the deep confined groundwater samples showed an excess of Na+ over Cl− and a deficiency of Ca2+ + Mg2+ over HCO3 − + SO4 2− and that they mainly lie along the line with a slope of −1. Thus, it can be concluded that cation exchange occurs in the confined aquifer.

0

−2

1 : −1 line −4 −2

0 2 ．；+ − ＃Ｆ− (meq/L)

4

Middle confined groundwater Deep confined groundwater

Figure 10: Plot of (Ca2+ + Mg2+ − HCO3 − − SO4 2− ) versus (Na+ − Cl− ).

5.2.4. Anthropogenic Input. In an area with considerable demand for groundwater, anthropogenic activity is always an important factor regarding groundwater quality. The concentrations of NO3 − can reflect the influence of anthropogenic activity on groundwater chemistry. In this study, the NO3 − concentrations in the samples of the unconfined

Geofluids

15

300

9 200 6 100

3

2008

2009

2010

2011

Groundwater level (m)

12

0

0

400

Precipitation (mm)


15

−4 −8 −12 −16

0

2008

2009

2010

2011

Year

Year Precipitation J18 J9

L38-1(B) L8-1(B)

L40-1(B) L39-1(B)

J20 J23 (a)

(b)


−4 −5 −6 −7 −8

2008

2009

2010

2011

Year L24-3 L25-3 (c)

Figure 11: Observed groundwater level dynamics in the multilayered aquifers during 2008–2011. (a) Groundwater level dynamics of the unconfined aquifer. (b) Groundwater level dynamics of the middle confined aquifer. (c) Groundwater level dynamics of the deep confined aquifer.

groundwater range from 0.5 to 120.0 mg/L with an average value of 41.36 mg/L, exceeding the quality standard for groundwater in China. This implies that the unconfined groundwater has been influenced by anthropogenic activities. The NO3 − concentrations in the samples of the middle and deep confined groundwater are