Investigation of Geochemical Characteristics and Controlling Processes of Groundwater in a Typical Long-Term Reclaimed Water Use Area

1. Introduction

Water scarcity has been a great threat to socioeconomic development as well as ecology in many parts of the world, especially in arid and semi-arid regions [1,2,3,4]. Due to the limited availability of surface water resources and precipitation, groundwater becomes the indispensable source of freshwater for various purposes such as drinking, irrigation and industry [5,6]. Long-term overexploitation has led to sharp decline of groundwater levels in many countries [7]. In order to alleviate shortages, non-conventional water resources such as wastewater and reclaimed water have been widely used for agricultural irrigation and as landscape water for decades [1,8,9].

However, wastewater and reclaimed water often have higher concentrations of major ions, heavy metals, nitrogen, phosphorus and other nutrients compared to freshwater [10]. Their usage may pose risks to environmental quality and human health [1]. Many researches have been conducted to reveal the potential influences of wastewater and reclaimed water usage on plants, soil and groundwater [2,9,10,11,12,13,14,15]. Generally, wastewater and reclaimed water usage can provide significant economic and ecological benefits [13]. Their reliable sources of nutrients can help to reduce the cost of fertilizer in agriculture and also increase the crop yield [16]. In addition, the usage of wastewater and reclaimed water in agriculture can not only reduce the consumption of groundwater resource, but also increase groundwater recharge. However, negative effects are also observed. Salt, heavy metals and other pollutants tend to accumulate in soil with long-term wastewater and reclaimed water irrigation [17], and result in soil structure deterioration [18,19,20]. Moreover, heavy metals are found to potentially enrich in corps and pose health risk to humans [21,22]. Long-term irrigation with wastewater and reclaimed water also leads to pollutants transfer downward [23], threatening the groundwater quality and enhancing the complexity of groundwater chemistry governing mechanisms [9,12]. Therefore, understanding groundwater hydrogeochemical characteristics and their controlling factors in wastewater and reclaimed water used area is essential for managing and protecting groundwater quality and providing guidance for the usage of wastewater and reclaimed water.

Beijing, one of the cities in the world with the greatest water shortage, has used wastewater since the 1950s and reclaimed water since 2003. More than 2 × 10⁸ m³ of reclaimed water has been used for agricultural purpose since 2008 [12]. Reclaimed water is also widely used as landscape water to recover wetlands and dry rivers. Thus, it is necessary to get insight into the influences of their usage on groundwater. Considering the chemical composition of reclaimed water in Beijing [14,24], groundwater is potentially polluted by salt, nitrogen, heavy metals and organic pollutants. Previous research demonstrated that heavy metals and organic pollutants have low possibilities to constitute pollution to groundwater [14,17,25,26], but salt and nitrogen pollutants should be paid extra attention [12,27]. Although scholars have reported the spatial variation of groundwater quality in terms of salt and nitrogen pollutants [26,27], and also discussed the influences caused by the leakage of reclaimed water river on soil and groundwater quality in long-term wastewater and reclaimed water use areas in Beijing [9,14,15]. The regional groundwater hydrochemical characteristics and governing mechanisms are still poorly known. The objectives of this research are to investigate regional groundwater geochemical characteristics, and to address the controlling factors of groundwater chemistry in typical long-term reclaimed water use areas in Beijing.

2. Materials and Methods

2.1. Description of the Study Area

The study area is located in the southern part of the Beijing Plain, China (Figure 1). This area extends between longitudes of 116°13′–116°43′ E and latitudes of 39°26′–39°50′ N, encompassing an area of 1036 km². It belongs to a zone of temperate continental monsoon climate. The mean annual temperature is 11.6 °C. The mean annual precipitation 556 mm [28], with more than 70% occurring in the rainy season spanning June to September. While the mean annual potential evaporation is 1800 mm, which is more than three times of the mean annual precipitation.

The whole territory of the study area lies in the downstream part of the Yongding River alluvial-proluvial plain (Figure 1). The average elevation of this area ranges from 14 m to 52 m above sea level with the terrain gradually inclining along the northwest to southeast direction. Quaternary deposits formed by the alluvial-proluvial sediments of Yongding River are the main water-bearing media. Its thickness increases from 50 m to 300 m with the lithology changing from coarse sand to fine and sandy clay from northwest to southeast (Figure 2). A thick and continuous clay layer is observed at a depth of 100 m [29]. Groundwater above of this layer is regarded as shallow groundwater (SGW), and that below it is defined as deep groundwater (DGW). Groundwater regionally flows from northwest to southeast with its depth varying from 13 m to 35 m. The major recharge patterns are precipitation infiltration, lateral inflow, surface-water body leakage and irrigation infiltration. The main discharge components include lateral outflow and artificial abstraction.

The northern part of the study area, including Xihongmen, Jiugong, Yizhuang, Yinghai and Daxing (Figure 1), is mainly covered by urban land type, and other areas are covered by agricultural land type. There are two wastewater treatment plans (WTP), named Xiaohongmen WTP and Huangcun WTP, located in the study area. Due to the shortage of water resources, wastewater has been reused for agricultural irrigation since the 1960s, and was gradually replaced by reclaimed water from the aforementioned WTP after 2003 [26]. Reclaimed water is also widely used for surface-water landscapes such as Niantan Park, the largest wetland park in the study area.

2.2. Sample Collection and Analysis

A total of 91 samples were collected from 26 SGW boreholes and 21 DGW boreholes in April (dry season) and September (rainy season) 2016. The locations of sampling sites were shown in Figure 1. All boreholes were pumped for more than 10 min to remove the stagnant water before sampling and field testing. Samples for laboratory analysis were collected in 2.5 L clean plastic bottles that had been thoroughly pre-washed with the water to be sampled. The temperature (T), electrical conductance (EC), total dissolved solids (TDS) and pH were measured on site using a multi-parameter device (Multi 350i/SET). The other chemical indices including cations (Na⁺, K⁺, Ca²⁺, Mg²⁺, NH₄⁺) and anions (Cl⁻, SO₄²⁻, HCO₃⁻, NO₃⁻, NO₂⁻) were analyzed in the Laboratory of Groundwater Sciences and Engineering of the Institute of Hydrogeology and Environmental Geology, Chinese Academy of Geological Sciences. The laboratory analysis were conducted fallowing the analytical procedures described by Huang, et al. [30]. The ionic balance error of all samples were within a limit of ±5%.

3. Results and Discussion

3.1. Groundwater Chemistry

Groundwater chemistry involves enormous vital information on suitability for domestic, irrigational and industrial purposes [31], and is very helpful in understanding and identifying the processes governing the hydrochemical quality of groundwater [32,33]. Statistical summary of the hydrogeochemical data of both SGW and DGW during the dry and rainy seasons is presented in the

Table 1. Statistical descriptions of chemical parameters in shallow and deep groundwater. Groundwater (GW); temperature (T); electrical conductance (EC); total dissolved solids (TDS).

Shallow GW	Dry Season					Rainy Season
	Min	Max	Mean	SD 1	C.V. (%) 2	Min	Max	Mean	SD 1	C.V. (%) 2
T (°C)	9.5	19.1	14.7	2.7	18.08	13.0	23.5	19.5	2.8	14.53
pH	7.10	7.60	7.30	0.15	2.10	7.10	7.90	7.40	0.17	2.34
EC (μS/cm)	585	1716	1175	279	23.76	547	1794	1174	311	26.46
TDS (mg/L)	389	1140	782	208	26.54	337	1194	792	255	32.24
K (mg/L)	1.26	3.24	2.06	0.55	26.85	1.03	2.92	1.78	0.53	29.79
Na (mg/L)	20.4	196.0	89.7	36.0	40.19	13.6	104.0	53.2	24.6	46.13
Ca (mg/L)	38.9	172.0	103.6	35.1	33.85	40.1	172.0	105.5	37.0	35.07
Mg (mg/L)	16.9	135.0	60.7	25.3	41.68	17.0	130.0	58.5	22.7	38.79
Cl (mg/L)	11.0	302.0	107.1	64.4	60.10	17.6	280.0	86.4	61.0	70.59
SO4 (mg/L)	25.5	261.0	110.8	67.2	60.64	28.5	186.0	93.1	50.6	54.38
HCO3 (mg/L)	282.0	785.0	536.1	127.1	23.72	255.0	728.0	510.8	122.8	24.03
NO3 (mg/L)	0.10	34.00	6.00	8.80	146.79	0.00	27.00	5.02	6.91	137.87
NO2 (mg/L)	0.001	0.014	0.002	0.003	156.27	0.000	0.044	0.003	0.009	330.38
NH4 (mg/L)	0.01	0.19	0.03	0.06	164.08	0.00	0.63	0.04	0.13	325.07
Deep GW	Dry Season					Rainy Season
	Min	Max	Mean	SD 1	C.V. (%) 2	Min	Max	Mean	SD 1	C.V. (%) 2
T (°C)	12.5	18.1	15.3	1.7	11.08	15.5	22.5	19.1	2.2	11.29
pH	7.30	7.70	7.51	0.10	1.36	7.30	8.00	7.68	0.19	2.46
EC (μS/cm)	526	1228	634	167	26.33	531	836	605	76	12.53
TDS (mg/L)	309	800	389	118	30.33	298	554	361	54	14.97
K (mg/L)	1.23	2.84	1.97	0.43	21.66	1.02	3.75	1.57	0.66	42.16
Na (mg/L)	21.5	163.0	59.6	31.6	53.05	13.2	73.2	31.6	16.9	53.49
Ca (mg/L)	29.1	96.3	51.9	13.9	26.70	32.1	88.7	52.9	14.2	26.87
Mg (mg/L)	15.0	71.4	26.9	12.3	45.99	12.7	31.5	20.2	5.3	26.43
Cl (mg/L)	7.7	95.3	25.5	20.0	78.31	9.2	50.7	22.2	11.8	53.09
SO4 (mg/L)	23.4	94.4	52.7	20.5	39.02	21.5	81.3	48.9	16.8	34.36
HCO3 (mg/L)	206.0	650.0	328.1	111.8	34.06	227.0	348.0	284.1	31.0	10.92
NO3 (mg/L)	0.10	7.41	1.27	1.59	125.13	0.01	5.35	1.13	1.22	107.92
NO2 (mg/L)	0.001	0.005	0.001	0.001	129.04	0.001	0.003	0.001	0.001	92.47
NH4 (mg/L)	0.01	0.18	0.02	0.04	186.24	0.01	0.10	0.02	0.03	129.04

Notes: ¹ SD: Standard Deviation; ² C.V. (%): Coefficient of Variation.

.

As shown in Table 1, groundwater temperature ranges from 9.5 °C to 19.1 °C for SGW and between 12.5 °C and 18.1 °C for DGW during the dry season, and varies from 13.0 °C to 23.5 °C for SGW and between 15.5 °C and 22.5 °C for DGW during the rainy season. The temperature of groundwater presents a slight increase trend from the dry season to the rainy season. The pH values of both SGW and DGW in the study area are in the range of 7.1–8.0, indicating alkaline nature. The EC values of SGW varies from 585 μS/cm to 1716 μS/cm with an average of 1175 μS/cm during the dry season, and 547 μS/cm to 1794 μS/cm with an average of 1174 μS/cm during the rainy season. That of DGW ranges between 526 μS/cm and 1228 μS/cm with an average of 634 μS/cm, and from 531 μS/cm to 836 μS/cm with an average of 605 μS/cm. According to the classification of groundwater based on EC (fresh: <1500 μS/cm; brackish: 1500–3000 μS/cm; saline: >3000 μS/cm) [34], most of groundwater samples in the study area are fresh water, and only S2 and S17 fall under the brackish water category. The variation of EC shows a slight decrease trend for both SGW and DGW from the dry season to the rainy season. TDS values of SGW are in the range of 389–1140 mg/L, with an average of 782 mg/L during the dry season, and ranging between 547 mg/L to 1794 mg/L with an average of 792 mg/L during the rainy season. For the DGW, TDS values range from 309 mg/L to 800 mg/L with an average of 389 mg/L during the dry season, and between 298 mg/L and 554 mg/L with an average of 361 mg/L during the rainy season. The TDS values of DGW are lower than that of SGW during both seasons, indicating that the quality of DGW is better than that of SGW in term of the salinity. The seasonal variation of TDS for SGW is not significant, while that for DGW shows a slight decrease trend.

The average concentration of major ions during the dry season are in the following order: Ca²⁺ > Na⁺ > Mg²⁺ > K⁺ and HCO₃⁻ > SO₄²⁻ > Cl⁻ for SGW, and Na⁺ > Ca²⁺ > Mg²⁺ > K⁺ and HCO₃⁻ > SO₄²⁻ > Cl⁻ for DGW. The order changed to Ca²⁺ > Mg²⁺ >Na⁺ > K⁺ and HCO₃⁻ > Cl⁻ > SO₄²⁻ for SGW, and Ca²⁺ > Na⁺ > Mg²⁺ > K⁺ and HCO₃⁻ > SO₄²⁻ > Cl⁻ for DGW during the rainy season. All major ions for both SGW and DGW shows a seasonal variation of decrease. In addition, the content of NO₃⁻, NO₂⁻ and NH₄⁺ in SGW and DGW also presents a decrease trend from the dry season to the rainy season (Table 1). This seasonal decrease trend of cations and anions, which coincides with the seasonal variations of EC and TDS, is possibly the result of a dilution effect caused by fresh recharging water, mainly precipitation, in the rainy season [35].

As TDS is a comprehensive parameter reflecting major ion chemistry of groundwater [36], and nitrate is an important index indicating groundwater quality deterioration caused by anthropogenic sources [37], these two parameters are selected to explore the spatial variation of groundwater hydrochemistry. As displayed in Figure 3, TDS values of SGW are greater than that of DGW during both seasons. For SGW, the high values of TDS are mainly distributed at the northwest part of the study area, which is the urban area of Daxing District, Beijing, during both the dry and rainy seasons. In addition, S2 and S17 are found with relative high TDS values (>1000 mg/L) during both seasons. Compared to SGW, DGW has a relative low TDS value (all less than 800 mg/L) during the dry and rainy seasons. Apart from D3 in the south area, the relative high TDS values of DGW are found in the northwest area, consistent with the high TDS values distribution area of SGW. All of the above suggests that urbanization is a factor impacting the groundwater chemistry.

As presented in Figure 4, the high nitrate concentration of SGW and DGW during both seasons are distributed in the urban area northwest of the study area. Generally, natural nitrate concentration is lower than 10 mg/L, any value exceeding this is regarded as pollution caused by external factors [38]. Therefore, the chemistry of SGW at the northwest of the study area is influenced by the anthropogenic activities in some degree. Although, the highest nitrate concentration of DGW is lower than the geochemical limit (10 mg/L), the relative high nitrate values are located at the same regions with that of SGW, where the main urban part of the study area is located, indicating their anthropogenic sources of nitrogen.

3.2. Hydrogeochemical Facies

Piper diagram [39] has been introduced to understand the groundwater chemistry and identify hydrogeochemical facies in the study area. All groundwater samples, including both shallow and deep groundwater during the dry and rainy seasons, are plotted in Figure 5. The left ternary diagram of Figure 5 shows that about 58% and 69% of samples for SGW and DGW, to be of [Ca²⁺] type, respectively; 35% and 2% of samples for SGW and DGW, were identified as [Mg²⁺] type, respectively, and; 8% and 29% of samples for SGW and DGW, were of [Na⁺] type, respectively. As indicated in the right ternary diagram, all the samples of both SGW and DGW are dominated by [HCO₃⁻] type. Thus, groundwater in the study area is mainly Ca-HCO₃ type, followed by mixed types (including mixed Ca-Na-HCO₃ type and mixed Ca-Mg-HCO₃ type) (Figure 5).

To further understand the variation and distribution of groundwater chemical facies, water types of both SGW and DGW, during the dry and rainy seasons, are shown in Figure 6, and the percentages of each water type are summarized in

Table 2. Percentage of different water types of shallow and deep groundwater.

	Percent	Shallow GW		Deep GW
Water Type		Dry Season	Rainy Season	Dry Season	Rainy Season
Ca-HCO3		73.08%	95.83%	85.00%	100.00%
Na-Cl
Mixed Ca-Na-HCO3		3.85%		15.00%
Mixed Ca-Mg-Cl		23.08%	4.17%
Ca-Cl
Na-HCO3

. As seen in Figure 6, most of the area is dominated by Ca-HCO₃ type for both shallow and deep groundwater during the dry and rainy seasons.

For shallow groundwater, three and two hydrogeochemical facies are found during the dry and rainy seasons, respectively (Figure 6a,b). Ca-HCO₃ type water samples account 73.1% for the shallow groundwater during the dry season, and mixed Ca-Mg-Cl type water comes to the second with the percentage of 23.1%, followed by the mixed Ca-Na-HCO₃ type with the percentage of 3.85% (Table 2). The only one sample (S19) of mixed Ca-Na-HCO₃ type is found located in the eastern part of the study area. While all the mixed Ca-Mg-Cl type samples are located at the northwestern area, which is the urban area of Daxing District, Beijing. It seems that spatial variation of hydrogeochemical facies of shallow groundwater is related to land use type. Figure 6a,b also showed that hydrogeochemical facies changed from the dry season to the rainy season. The water of S19, which is of Ca-Na-HCO₃ type during the dry season, changed to be of Ca-HCO₃ type during the rainy season, while four out of the six mixed Ca-Mg-Cl type water changed to be of Ca-HCO₃ type. The only two remain mixed Ca-Mg-Cl type water are located at the downstream from the urban area of Daxing District. All of the above indicates that the quality of shallow groundwater evolves slightly fresher from the dry season to the rainy season.

As can been seen in Figure 6 and Table 2, the overall quality of DGW is better than that of SGW. During the dry season, about 85% of DGW samples are of Ca-HCO₃ type, and the other 15% of samples are of mixed Ca-Na-HCO₃ type. The Ca-Na-HCO₃ type water (D13, D15, D17) mainly distributes at the eastern part of the study area, which is basically consistent with the distributing area of Ca-Na-HCO₃ type water (S19) for SGW during the dry season. It is worth noting that the water type of DGW in the urban area is of Ca-HCO₃ type rather than mixed Ca-Mg-Cl type, indicating that the water type of DGW in the urban area has not significantly altered by the anthropogenic activities yet. Deep groundwater has similar seasonal variation tendency of hydrogeochemical facies with shallow groundwater. All of the three mixed Ca-Mg-Cl type water (D13, D15, D17) changed to the Ca-HCO₃ type water from the dry season to the rainy season. This change is possibly caused by the increase of the water recharge amount during the rainy season [40].

3.3. Mechanisms Controlling Groundwater Chemistry

3.3.1. Natural Factors

Gibbs diagrams, which are constructed by plotting ratios of Na⁺/Na⁺ + Ca²⁺ and Cl⁻/(Cl⁻ + HCO₃⁻) versus TDS [41], are widely used to identify natural processes, such as precipitation, rock-water interaction, evaporation/ crystallization, governing groundwater geochemistry [33,42,43]. As seen in Figure 7, all samples of both shallow and deep groundwater for both seasons are plotted in the rock dominance area, indicating that water-rock interaction is the main natural fundamental sources of groundwater chemical constituents in the study area. Evaporation was observed to have less contribution to the dissolved chemical constituents of groundwater during both dry and rainy seasons.

To further understand the details of rock water interaction in the study area, some ratio plots of major ions were conducted (Figure 8). The relation of Na⁺ versus Cl⁻ of both shallow and deep groundwater for both seasons are demonstrated in Figure 8a. Generally, if Na⁺ in groundwater is originated from the halite dissolution (1), then the molar ratio of Na⁺/Cl⁻ should be approximately equal to 1. While if the ratio is greater than 1, Na⁺ is mainly contributed by silicate weathering (2), whereas less than 1 indicates derivation from anthropogenic sources [43]. In this study, nearly all deep groundwater samples and most of the shallow groundwater samples during both seasons are with the ratio greater than 1, implying that silicate weathering (2) is an important source of sodium in shallow and deep groundwater [44]. Halite dissolution (1) is also one of the sources of sodium and chloride for both shallow and deep groundwater as some samples are observed with the ratio approximately equal to 1. This is confirmed by the Saturation Index (SI) of halite (Figure 9). In addition, it is worth to note that part of shallow groundwater samples are with the ratio less than 1, indicating the chemical constituents of shallow groundwater are contributed by anthropogenic sources in some degree.

$$\mathrm{NaCl}\to {\mathrm{Na}}^{+}+{\mathrm{Cl}}^{-}$$

(1)

$$2{\mathrm{NaAlSi}}_3{\mathrm{O}}_8+2{\mathrm{CO}}_2+11{\mathrm{H}}_2\mathrm{O}\to 2{\mathrm{Na}}^{+}+{\mathrm{Al}}_2{\mathrm{Si}}_2{\mathrm{O}}_5{\left(\mathrm{OH}\right)}_4+3{\mathrm{H}}_4{\mathrm{SiO}}_4+2{\mathrm{HCO}}_3^{-}$$

(2)

The relation of Ca²⁺ and SO₄²⁻ is shown in Figure 8b. It is observed that Ca²⁺ increases with SO₄²⁻ in both shallow and deep groundwater, suggesting that these two ions may derive from the dissolution of gypsum and anhydrite (3, 4). The mineral equilibrium calculation results (SI_gypsum < 1, SI_anhydrite < 1) (Figure 9) indicate that all samples are under-saturated with the respect of gypsum and anhydrite, confirming the potential contributes of these two minerals dissolution. While the phenomenon that samples of both shallow and deep groundwater fall above the 1:1 line (Figure 8b), implying that Ca²⁺ and SO₄²⁻ are also included in some other different geochemical processes besides aforementioned processes [33].

$${\mathrm{CaSO}}_4\to {\mathrm{Ca}}^{2+}+{\mathrm{SO}}_4^{2-}$$

(3)

$${\mathrm{CaSO}}_4·2{\mathrm{H}}_2\mathrm{O}\to {\mathrm{Ca}}^{2+}+{\mathrm{SO}}_4^{2-}+2{\mathrm{H}}_2\mathrm{O}$$

(4)

The relationship between Ca²⁺ + Mg²⁺ and HCO₃⁻ can reveal the source of calcium and magnesium of groundwater [33]. If the Ca²⁺ and Mg²⁺ only derive from the dissolution of carbonate, the (Ca²⁺ + Mg²⁺)/HCO₃⁻ molar ratio would be about 0.5. In this study, nearly all samples have higher ratios (>0.5) (Figure 8c), signifying the existence of additional sources of Ca²⁺ and Mg²⁺ and less contribution of Ca²⁺ and Mg²⁺ by carbonate dissolution [45]. This confirmed by the SI of calcite and dolomite (Figure 9), showing that majority of the samples of both shallow and deep groundwater are over-saturated with respect to the calcite and dolomite.

The diagram of (Ca²⁺ + Mg²⁺) versus (HCO₃⁻ + SO₄²⁻) were constructed to determine the mineralization processes (Figure 8d). The data that fall along the 1:1 line indicate contribution of dissolution of carbonates and sulfate minerals, and the data lying above and below the 1:1 line signify additional influences of the reverse cation-exchange process (5) and cation-exchange process (6), respectively [3]. As shown in Figure 8d, most of the data fall along the 1:1 line suggesting the weathering of carbonates and sulfate minerals. As discussed above, the contribution of carbonates weathering is less, so the dissolution of sulfate minerals (such as gypsum and anhydrite) is the main contribution. In addition, nearly all deep groundwater samples are observed to lie below the 1:1 line, suggesting the effects of cation-exchange process (6) on deep groundwater. However, some shallow groundwater samples fall above the equiline and some lie below the line, showing the contribution of the reverse cation-exchange process (5) and cation-exchange process (6) in the shallow groundwater in different area.

$$2{\mathrm{Na}}^{+}+{\mathrm{CaX}}_2\to {\mathrm{Ca}}^{2+}+2\mathrm{NaX}$$

(5)

$${\mathrm{Ca}}^{2+}+2\mathrm{NaX}\to 2{\mathrm{Na}}^{+}+{\mathrm{CaX}}_2$$

(6)

Chloro-alkaline indices, including CAI-1 and CAI-2, were introduced to examine the influences of cation-exchange processes on groundwater chemistry (Figure 10). These two indices are expressed as Equations (7) and (8) (all ions are expressed in meq/L) [46]. The aforementioned indices would be negative values if the hydrochemistry is dominantly affected by the normal cation-exchange process (6). On the other hand, if reverse cation-exchange process (5) takes place, these two indices would show positive values. Nearly all deep groundwater samples showed negative CAI (Figure 9), confirming the results of Figure 8d that cation-exchange process (6) occurs in deep groundwater. Some shallow groundwater samples are observed with negative CAI and others are with positive CAI, indicating cation-exchange process (6) and reverse cation-exchange process (5), respectively. This is consistent with the conclusion of Figure 8d.

$$\mathrm{CAI}-1=\frac{{\mathrm{Cl}}^{-}-\left({\mathrm{Na}}^{+}+{\mathrm{K}}^{+}\right)}{{\mathrm{Cl}}^{-}}$$

(7)

$$\mathrm{CAI}-2=\frac{{\mathrm{Cl}}^{-}-\left({\mathrm{Na}}^{+}+{\mathrm{K}}^{+}\right)}{{\mathrm{HCO}}_3^{-}+{\mathrm{SO}}_4^{2-}+{\mathrm{CO}}_3^{-}+{\mathrm{NO}}_3^{-}}$$

(8)

3.3.2. Human Activities

The contributions of human activities to groundwater chemistry are complex and uncertain, and hard to determine [9,45]. Nitrate, which is mainly originated from multiple anthropogenic sources, is widely used to indicate the effects of human activities on groundwater chemistry [47,48]. In this study, the concentration of NO₃⁻ in sallow groundwater shows an increasing trend with the increase of Cl⁻ content (Figure 11a), indicating the similar sources of these two ions [49]. Cl⁻ is commonly derived from anthropogenic inputs as well as halite dissolution. Thus, the positive relation between NO₃⁻ and Cl⁻ signifies their anthropogenic inputs. This is also confirmed by the positive correlation of TDS with (NO₃⁻ + Cl⁻)/HCO₃⁻ (Figure 11b).

As can be seen in Figure 4 and Figure 11, the high NO₃⁻ contents (exceeding geochemical limit 10 mg/L: S5, S6, S7, S16, S26) are only observed in shallow groundwater in the urban area during both seasons, implying that anthropogenic inputs such as domestic wastewater have a certain of influences on the chemistry of shallow groundwater in the urban area. This is also evidenced by the spatial distribution of water type of shallow groundwater (Figure 6a,b), of which Ca-Mg-Cl type for urban area while Ca-HCO₃ and Ca-Na-HCO₃ type for rural area. Urban anthropogenic wastes inputs are also found responsible for the relative higher NO₃⁻ content for the deep groundwater in the urban area (D6) in contrast with that in the rural area as the result of thin aquitards, but the influence is very limited. In the rural area (mainly agricultural area irrigated with reclaimed water), the nitrite content of shallow groundwater presents a poor correlation with the Cl⁻ (the Pearson correlation coefficient is 0.118 for dry season and 0.383 for rainy season), suggesting human activities such as reclaimed water irrigation and reclaimed water river leakage have very limited influences on the shallow groundwater quality. This is possibly related to the thick aquitards above the water level. As a result, the NO₃⁻ contents of all shallow groundwater are below the geochemical limit 10 mg/L (Figure 11a). Deep groundwater in the rural area also have very low nitrite content (all below 10 mg/L). NO₃⁻ contents show nearly no variation with the increase of Cl⁻ contents (Figure 11), demonstrating that the chemistry of deep groundwater in the rural area is not affected by anthropogenic pollutions.

4. Conclusions

Reclaimed water has been widely used in many arid and semi-arid regions around the world to mitigate water crises. In the present study, hydrogeochemical characteristics of groundwater in a long-term reclaimed water use area in Beijing were investigated, and the controlling processes of groundwater chemistry were also discussed in detail. The summarized conclusions are as follows.

Groundwater, including shallow groundwater and deep groundwater, is mainly naturally alkaline freshwater in the study area. The average concentration of all ions in deep aquifers are lower than that in shallow aquifers throughout the year, resulting in fresher and better quality deep groundwater. Moreover, the values of most indices of groundwater decrease from the dry season to the rainy season in both shallow and deep aquifers as the results of dilute effects in the rainy season. In terms of hydrogeochemical facies, both shallow groundwater and deep groundwater are mainly Ca-HCO₃ type, followed by mixed types such as mixed Ca-Na-HCO₃ type and mixed Ca-Mg-HCO₃ type. The hydrogeochemical facies of both shallow and deep groundwater were observed with a desalination change that water types evolved from mixed types in the dry season to Ca-HCO₃ type in the rainy season.

The chemistry of groundwater in the study area is affected by natural processes as well as human activities. Water-rock interactions such as dissolutions of silicate, halite, gypsum, anhydrite and cation exchange are the dominant natural processes controlling the chemical composition of groundwater in both aquifers and both seasons. While the influences of human activities is related to the hydrogeological condition. The urban area with the thin aquitard is observed as having obvious influences of anthropogenic inputs on groundwater chemistry, especially for shallow aquifers, while the existence of thick aquitards in rural areas greatly reduces or even eliminates the potential negative effects of reclaimed water usage on groundwater chemistry. Thus, hydrogeological condition should be taken into account when using reclaimed water for agricultural irrigation and landscape purpose.