# Sources Identification of Nitrogen Using Major Ions and Isotopic Tracers in Shenyang, China

Authors: Huan Huang; Mingzhu Liu; Junjie Wang; Jiangtao He; Honghan Chen
Journal: Geofluids
 (2018)

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## Abstract

Stable isotopes are natural tracers that can provide quantitative information about the surface water/groundwater interactions and sources of pollutants in water. In this study, we measuredδ18Owater and δ2Hwater and δ18Onitrate and δ15Nnitrate of the samples from the Hun River and groundwater in Shenyang City, China, where the water from the Hun River has a strong discharge and recharge connection with the groundwater. δ18Owater and δ2Hwater were used to determine the amount of surface water that was discharged into groundwater, while δ18Onitrate and δ15Nnitrate were employed to determine the sources of nitrate and ammonium in groundwater, which are the main contaminants in the study area. The reducing environment in groundwater may result from the prevailing iron and manganese, occurring from weathering of minerals and rocks, which prevents the ammonium being oxidized into nitrate. Results show that the amount of recharge from the Hun River into groundwater accounts for around 55.56–86.60% of the total groundwater in the dry season, and the ratio changed to 30.97–63.79% in the wet season. Multiproxy analysis (stable isotope analyses in combination with chemical and hydrogeological data of the study area) indicates that human activities, such as manure and sewage discharge, are the prevailing source of nitrogen in the waters.


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## Body

## 1. Introduction

Nitrogen pollution is an increasingly serious problem of groundwater in the riparian wellhead area of the Hun River. On the basis of the monitoring data of groundwater quality, nitrogen pollution has been found in most monitoring wells. Some water source wells have to be suspended, because the nitrogen content in groundwater exceeds the threshold in the Standard for Groundwater Quality (GB/T14848-93) in China. There are many sources of nitrogen pollution, and different sources cause different degrees of nitrogen pollution to groundwater. The groundwater source near the river plays an important role in the water supply in Shenyang. Therefore, it is of great significance to identify the source of groundwater nitrogen pollution and its contribution level and to carry out the targeted pollution control work and protect the groundwater resources.Groundwater and surface water (such as rivers and lakes) are important components of the hydrological cycle, and they interact with each other in a variety of physiographic and climatic landscapes in the hydrologic system. Water quality and quantity from one component may have an influence on the other component in the hydrological cycle. Therefore, it is necessary to understand the basic principles of interactions between them, as well as spatial and temporal transformation rules of water quantity and quality between groundwater and surface water. These understandings will be of theoretical and practical significance with regard to assessment of water quantity and quality and further lead to the remediation, treatment, and prevention of water pollution [1–4].The interaction between river water and groundwater is related to factors such as geography, landform, and rock characteristics of the water-bearing stratum, which are changing with seasons. In time and space, the transformation of groundwater and river water forms an indivisible complex system. Therefore, the chemical composition of water may be due to its long-term interaction with the surrounding environment in the water cycle. Moreover, water quality changes are usually caused by more complex interactions [3, 5–10]. Accordingly, the chemical composition of water can reflect its source information and evolution history to a certain extent, which will provide an effective tracing method for the study of the interaction between groundwater and surface water [11, 12]. Researchers in different disciplines, such as geologists, hydrologists, and ecologists, are developing a more comprehensive conceptualization of groundwater and surface water interactions [13]; for example, Levy and Xu [14] review and compare methods to describe groundwater and surface water interactions at different scales and show typical applications in South Africa. Hayashi and Rosenberry [15] provide a comprehensive review for the effect of groundwater exchange on the hydrology and ecology of surface water. This work attempts to investigate the broader, multidisciplinary perspective of groundwater and surface water interactions, starting from some underlying prerequisites for comprehending environmental systems. To this end, we evaluate the hydrologic and water quality data for the Hun River basin, Shenyang city, China, to better understand the interactions between groundwater and surface water.The main objective of the study was to identify the source(s) of nitrogen contamination in groundwater along the Hun River, Shenyang, China. To this end, the interactions between the Hun River and groundwater are analyzed with respect to the hydrogeology conditions of the site.δ18Owater and δ2Hwater and δ18Onitrate and δ15Nnitrate were measured from the Hun River and groundwater to determine the amount of surface water that was discharged into groundwater as well as to track back the sources of the main contaminant. The approaches presented in this paper provide a framework for evaluating the importance of the interactions between groundwater and surface water in a human-natural coupled watershed.


## 2. Geological Setting

### 2.1. Description of Site

The study area lies in Shenyang city, Liaoning province, China, within latitudes 41°42′00″~41°47′30″ and longitudes 123°15′00″~123°30′00″ in the northeast of China. It is located between the Xi River and the Hun River and covers an area of about 36 km2 (Figure 1). The northern part of the study area was mainly residential and industrial land, which has a high intensity of contaminating sources. The south of the research area was the farmland and the green land with a relatively high intensity of contamination source.Figure 1
Location map of the study area. Modified from L. Y. Liu et al. [20].


### 2.2. Geology and Hydrogeology Conditions

The study area is located in the first terrace of the Hun River alluvial-proluvial fan. The groundwater system consists of the phreatic aquifer and the leaky confined aquifer (Figure2). The phreatic aquifer is composed mainly of medium sand and medium-coarse sand (hydraulic conductivity of ca. 7 × 10−4 m·s−1 [16]). The thickness of the phreatic aquifer is ca. 15 m. The leaky confined aquifer is located below ca. 16 m from the surface, mainly composed of medium sand and medium-fine sand, with a thickness of ca. 15 m. For the aquitard, it is located ca. 40 m below ground surface and composed mainly of clay and silty clay (hydraulic conductivity of ca. 8 × 10−11 m·s−1 [16]). The groundwater table ranges from 10 to 12 m below ground surface, and the thickness of the aquitard is 4–6 m.Figure 2
Hydrogeologic profile of the region near the Hun River. Modified from Hou et al. [16].


## 2.1. Description of Site

The study area lies in Shenyang city, Liaoning province, China, within latitudes 41°42′00″~41°47′30″ and longitudes 123°15′00″~123°30′00″ in the northeast of China. It is located between the Xi River and the Hun River and covers an area of about 36 km2 (Figure 1). The northern part of the study area was mainly residential and industrial land, which has a high intensity of contaminating sources. The south of the research area was the farmland and the green land with a relatively high intensity of contamination source.Figure 1
Location map of the study area. Modified from L. Y. Liu et al. [20].


## 2.2. Geology and Hydrogeology Conditions

The study area is located in the first terrace of the Hun River alluvial-proluvial fan. The groundwater system consists of the phreatic aquifer and the leaky confined aquifer (Figure2). The phreatic aquifer is composed mainly of medium sand and medium-coarse sand (hydraulic conductivity of ca. 7 × 10−4 m·s−1 [16]). The thickness of the phreatic aquifer is ca. 15 m. The leaky confined aquifer is located below ca. 16 m from the surface, mainly composed of medium sand and medium-fine sand, with a thickness of ca. 15 m. For the aquitard, it is located ca. 40 m below ground surface and composed mainly of clay and silty clay (hydraulic conductivity of ca. 8 × 10−11 m·s−1 [16]). The groundwater table ranges from 10 to 12 m below ground surface, and the thickness of the aquitard is 4–6 m.Figure 2
Hydrogeologic profile of the region near the Hun River. Modified from Hou et al. [16].


## 3. Sampling and Methodology

Sampling conditions were shown in Table1. The shallow well refers to the sampling well located in the phreatic aquifer, and the deep well refers to the sampling well located in the leaky confined aquifer. All water samples were collected in 50 mL high-density polyethylene bottles which were cleaned with detergent first, then with 10% nitric acid, and finally rinsed several times with distilled water. This procedure was carried out to ensure that the sample bottles we used were all free from contaminants.Table 1
Sampling conditions in different periods.
Sampling time
March 2011
June 2011
September 2012
Deep wells
29
49
27
Shallow wells
9
20
24
Surface water
7
10
7
Soil samples
0
0
13In order to obtain the fresh aquifer samples for analysis, every borehole at the sampling point was pumped for about 5 minutes to purge the aquifer of stagnant water. Samples were initially collected in a sterilized bucket immediately after purging the aquifer and quickly transferred into the sampling bottles. Samples were taken in duplicate for major ion and stable isotope analyses. Some basic parameters of groundwater were measured directly in the field, including the temperature, pH, dissolved oxygen (DO), total dissolved solid (TDS), and electrical conductivity (EC). Samples earmarked for major ion analyses were filtered on-site through 0.45 mm cellulose filters with the aid of a hand-operated vacuum pump. The samples were kept in the refrigerator until they were transported to the laboratory for chemical analysis.The major ions in the water at each sampling point were analyzed using a Dionex-120 ion chromatograph from the Laboratory of Environmental Chemistry, China University of Geosciences (Beijing). The accuracy of the analyses was estimated from the charge balance error (Freeze and Cherry, 1979), which is within ±5% for all samples.The stable hydrogen (2H) and oxygen (18O) isotopes in water collected in June 2011 (47 water samples) and September 2012 (54 water samples) were measured by a Picarro Isotopic Water Analyzer in the Water and Water-Rock Reactions Isotope Laboratory, Institute of Geology and Geophysics, Chinese Academy of Sciences. The isotopic results of 2Hwater and 18Owater were reported as δ2Hwater and δ18Owater (δ=Rsample/Rstandard−1∗1000) in per mil (‰) data with the Vienna Standard Mean Ocean Water (VSMOW) standard. The analytical precision is ±0.2‰ and ±0.02‰ for δ2Hwater and δ18Owater, respectively.The stable isotopes of nitrogen (15N) and oxygen (18O) of nitrate in 26 water samples collected in June 2011 were analyzed in the Ministry of Land and Resources of Karst Geology Environmental Supervision and Testing Center using the anion exchange technique. The method for removing all O-bearing compounds from samples except NO3− and for removing the interference from other components to nitrogen measurement were based on a former paper reported by Silva et al. [17]. The stable isotopes of nitrogen (15N) and oxygen (18O) of nitrate in 28 water samples and 11 soil samples collected in September 2012 were measured with the Isotope Mass Spectrometer MAT253 at the Soil and Environment Analysis and Testing Center, Nanjing Institute of Soil Sciences, Chinese Academy of Sciences, according to the method of Brand [18]. The 15N results were reported as δ15Nnitrate relative to air in per mil (‰) data. The analytical precision of δ15Nnitrate and δ18Onitrate was about 0.05‰ and 0.5‰, respectively.


## 4. Results and Discussion

### 4.1. Hydrochemistry Analysis

The statistical results of the chemical index of the samples of groundwater and surface water are shown in Tables2 and 3. The variation range of pH in groundwater (both the southern and northern side of the study area) was 5.94–7.41, and the majority of the samples were within natural pH range of 6.50–8.50. The pH of surface water (Hun River) varied from 7.14 to 8.20 with a mean of 7.60, which was generally higher than the values in the groundwater. Lower pH of the water in the study area might be associated with CO2 produced by microbial respiration in the surface soil [19] or associated with local precipitation infiltration [20, 21]. The EC results in groundwater ranged from 511.50 to 1783.00 μS·cm−1, while the values for surface water ranged from 877.20 to 1231.90 μS·cm−1. The standard of drinking water for EC values in the World Health Organization (WHO) was between 500 and 1500 μS·cm−1 (Rodier, 1996), and some samples in both groundwater and the Hun River were higher than the standard value. From 2001 to 2005, nearly 400,000 tons of domestic sewage water and a portion of industrial waste water were discharged into the Shenyang section of the Hun River without treatment every day (Lin et al., 2007); the polluted river recharged the aquifer and may lead to the increase of EC value. The relative errors of charge balance for all the elements in groundwater and river in June 2011 were −1.53% and −1.49%, respectively, and those for March 2011 were 4.71% and 5.67%, respectively.Table 2
Statistical summary of hydrochemical data in the Shenyang areas, March 2011. All units are in mg·L−1, except for electrical conductivity (EC, μS·cm−1).
Parameter
Groundwater
The Hun River
Southern side
Northern side
Mean
Max
Min
Mean
Max
Min
Mean
Max
Min
pH
7.08
7.41
6.45
6.44
6.85
5.94
7.60
8.20
7.14
EC
628.86
1035.00
511.50
1170.53
1783.00
650.60
1231.90
1652.00
877.20
Ca
61.79
111.00
34.00
4.13
9.00
1.50
81.81
91.00
70.00
Mg
19.16
35.00
1.00
41.53
85.00
18.00
25.54
32.00
20.00
Na
48.09
70.83
29.92
71.13
113.90
33.43
110.84
182.20
50.69
K
3.66
5.86
2.49
4.04
6.92
2.24
7.22
8.48
4.20
Fe
1.13
5.16
0.06
2.62
23.86
0.13
1.59
4.93
0.99
Mn
1.25
2.46
0.15
2.00
4.04
0.21
0.45
2.29
0.45
NH4-N
2.55
12.11
0.03
0.14
0.68
0.03
12.12
19.00
6.09
Cl
55.58
83.00
30.00
126.73
204.00
53.00
175.18
271.00
102.00
HCO3
189.77
259.16
98.13
153.97
236.47
70.45
201.29
228.97
178.65
NO3-N
9.11
76.27
0.71
137.73
401.02
13.55
2.70
5.61
1.20
SO4
86.96
55.69
154.47
147.86
201.07
75.98
122.70
150.03
96.39Table 3
Statistical summary of hydrochemical data in the Shenyang areas, June 2011. All units are in mg·L−1, except for electrical conductivity (EC, μS·cm−1).
Parameter
Groundwater
The Hun River
Southern side
Northern side
Mean
Max
Min
Mean
Max
Min
Mean
Max
Min
pH
6.86
7.32
6.15
6.61
7.06
6.22
7.26
7.36
7.02
EC
690.18
1033.00
546.50
1356.37
2871.00
619.7
962.15
1399.0
474.8
Ca
72.59
114.20
47.65
130.67
270.20
59.93
53.99
59.62
49.97
Mg
17.34
27.75
11.77
34.78
52.64
12.98
12.86
15.96
11.77
Na
52.19
67.34
33.66
81.89
132.10
38.98
30.71
35.48
27.61
K
4.84
6.90
2.72
7.00
40.41
1.92
4.87
5.38
4.12
Fe
0.89
6.49
0.02
1.21
11.79
0.03
0.35
0.61
0.19
Mn
1.68
3.17
0.02
3.36
9.48
0.04
2.12
6.39
0.43
NH4-N
1.10
4.79
0.06
2.51
17.53
0.03
0.07
0.12
0.05
Cl
61.01
104.60
44.88
136.87
287.62
48.66
46.26
55.33
40.38
HCO3
214.38
281.14
123.17
268.22
527.50
93.71
143.27
123.20
179.40
NO3-N
38.71
102.71
2.58
135.29
338.24
6.23
2.79
4.37
1.77
SO4
92.34
142.32
58.13
174.44
500.32
28.56
75.21
78.19
73.39From 2001 to 2005, the concentration of ammonium nitrogen (abbreviated as NH4+-N) in the river water was as high as 9.72 mg·L−1 to 22.35 mg·L−1 (Lin et al., 2007). A high level of NH4+-N in moving water indicated some kind of contaminant entering the water. The Hun River of the study area was characterized by high levels of ammonium nitrogen concentrations, and all surface water samples exceeded the 0.5 mg·L−1 limit specified by the WHO drinking water standard. The Hun River was close to heavily fertilized fields, and therefore, the manure and sewage discharged into the Hun River might contain a higher ammonium nitrogen.In March 2011, the content of NH4+-N in the water samples of the southern part was larger than that in the northern part. The content of NH4+-N in the Hun River had reached 6.09–12.12 mg·L−1, and the groundwater sampling points of high concentration were located at the riverside. The groundwater level is lower than the river level due to the exploitation of water source wells. Therefore, it can be speculated that the ammonia in groundwater comes from the Hun River. In addition, fertilizers containing ammonium sulfate, (NH4)2SO4, or ammonium nitrate, NH4NO3, might also result in a high level of ammonium ions in the samples. The most serious contaminants in the groundwater were NH4+-N, ranging from 0.02 to 24 mg·L−1, which was followed by NO3−-N (0.16–71.50 mg·L−1), TFe (0.05–12.92 mg·L−1), and Mn2+ (0.15–9.92 mg·L−1). NH4+-N, NO3−-N, TFe, and Mn2+ concentrations at some locations exceeded the 0.5 mg·L−1 (NH4+-N), 11 mg·L−1 (NO3−-N), 0.3 mg·L−1 (TFe), and 0.1 mg·L−1 (Mn2+) limits specified by the WHO drinking water standard. The study area was a primary high iron and manganese groundwater zone [22]. The iron and manganese minerals in the study area were goethite, siderite, and rhodochrosite and contained a small amount of pyrite, magnetite, and pyrolusite [23]. The most common sources of Fe2+, Fe3+, and Mn2+ in groundwater were likely occurring naturally, from weathering of iron and manganese oxide minerals. However, industrial effluent, sewage, and landfill leachate might also contribute to Fe2+, Fe3+, and Mn2+ in groundwater [24, 25].


### 4.2. Groundwater Recharge

The geophysical investigation results showed that there was a close hydraulic connection between the phreatic aquifer in the study area and the Hun River. About 1 million cubic meters of groundwater were pumped every day from the Hun River aquifer for urban water supply, and a groundwater depression cone was formed, which causes continuous recharge of the river water to the phreatic aquifer. The phreatic aquifer and leaky confined aquifer are the main layers for groundwater exploitation in the area, and there is close hydraulic connection between the two aquifers [26]. The geophysical investigation results also revealed that there was a connection between the Hun River and the aquifer 60 m below the surface in the riverside area. As for the water quality, the Hun River, with a long history of pollution, also had a close relationship with groundwater. For example, the nitrogen concentration in groundwater was high, and a large portion was from the seepage of the Hun River, which had already been polluted by the manure and sewage and runoff from heavily fertilized fields, causing the river water to continuously recharge the phreatic aquifer.


### 4.3. Isotopic Compositions of Groundwater and the Hun River

Differences in the content ofδ2Hwater and δ18Owater of groundwater, rainfall, and surface water were used to determine the mixing processes in the groundwater flow system in the study area. δ2Hwater and δ18Owater data typically were plotted on a diagram showing δ2Hwater versus δ18Owater relative to VSMOW. Mean annual values of δ2Hwater and δ18Owater in precipitation collected at many locations around the world plot along a line with a slope of 8 and an intercept of +10 (δ2H = 8δ18O + 10), commonly referred to as the global meteoric water line (GMWL) [27]. The variability in isotopic composition of rainfall from one site to another is a function of several factors, including storm-track origin, rainfall amount and intensity, atmospheric temperature, and the number of evaporation and condensation cycles [28]. The stable isotopic composition of water relative to the GMWL revealed important information on groundwater recharge patterns, the origin of waters in hydrologic systems, and mixing of groundwater and surface water.The exchange of water between river and aquifer could be traced by the difference in stable isotope composition between the regional groundwater and the river water. The results of stable isotope (Tables4 and 5) showed clear mixing between shallow groundwater and surface water in the basin. In groundwater, the mean values of δ2Hwater and δ18Owater for the dry season (June 2011) were −8.87 and −65.12‰, respectively, and those for the wet season (September 2012) were −8.79 and −65.64‰, respectively; because of the lag of river and precipitation recharge, the isotope content in the dry and wet periods is not significantly different. But in the Hun River, the mean values of δ2Hwater and δ18Owater for the dry season (June 2011) were −9.16 and −65.79‰, respectively, and those for the wet season (September 2012) were −9.54 and −70.25‰, respectively. The values of δ2Hwater and δ18Owater in the wet season were −0.38‰ and −4.46‰ higher, respectively, than those in the dry season. Generally, the stable isotopic compositions of precipitation decrease with decreasing temperature and with increasing rainfall amount [29]. The results showed that the effect of precipitation amount was significant, and the stable isotope composition of precipitation decreased with the increase of rainfall amount and air temperature.Table 4
Statistical summary ofδ18Owater (‰) and δ2Hwater (‰) values of groundwater and river water in the study area.
Groundwater
The Hun River
Dry season
Wet season
Dry season
Wet season
δ18O (‰)
δ2H (‰)
δ18O (‰)
δ2H (‰)
δ18O (‰)
δ2H (‰)
δ18O (‰)
δ2H (‰)
Mean
−8.87
−65.12
−8.79
−65.64
−9.16
−65.79
−9.54
−70.25
Maximum
−7.82
−58.77
−6.90
−55.30
−8.90
−64.3
−9.14
−67.60
Minimum
−9.73
−70.24
−13.85
−103.2
−9.39
−66.92
−9.87
−72.30Table 5
Statistical summary ofδ18Onitrate (‰) and δ15Nnitrate (‰) values of groundwater and river water in the study area.
Groundwater
The Hun River
Dry season
Wet season
Dry season
Wet season
δ18O (‰)
δ15N (‰)
δ18O (‰)
δ15N (‰)
δ18O (‰)
δ15N (‰)
δ18O (‰)
δ15N (‰)
Mean
10.87
6.17
5.04
9.74
13.05
3.25
3.16
5.70
Maximum
14.08
13.22
15.02
24.85
15.96
3.87
13.31
7.26
Minimum
7.36
−3.14
−18.36
−7.26
10.13
2.63
−10.36
3.80In Figures3(a) and 3(b) (the size of the symbols represents the perpendicular distance of the sampling site measured from the Hun River), both δ18Owater and δ2Hwater of the groundwater and surface water were located slightly lower than the local meteoric water line (LMWL), these suggesting that there was evaporation in the basin, and the groundwater was a mixture of river water and precipitation, and the influence of the river water recharge was greater than that of the infiltration.Figure 3
Plot ofδ2Hwater and δ18Owater for shallow groundwater, deep groundwater, and surface water samples collected in the study region: (a) dry season; (b) wet season.
(a)
(b)In Figure3, the distribution of deep groundwater and shallow groundwater was approximately the same, which was further consistent with the closely hydraulic connection between the two layers of aquifer. The points representing shallow groundwater were closer to the LMWL, and the phenomenon was more obvious in Figure 3(b) (wet season). This means that the phreatic aquifer was more affected by rainfall than the leaky confined aquifer. The values of δ18Owater and δ2Hwater of the points far away from the river bank (larger symbols) were higher than those near the Hun River (smaller symbols). This indicates that the groundwater in the riverside area is more affected by the river. It receives the recharge of the Hun River, and the isotopic enrichment occurs at a distance from the river.


### 4.4. Mass Balance of Isotopic Compositions of Groundwater

Different stable isotopic compositions of2Hwater and 18Owater in groundwater were used to identify the mixing progress in the study area. The variability in isotopic composition of rainfall from one site to another is a function of several factors, including storm-track origin, rainfall amount and intensity, atmospheric temperature, and the number of evaporation and condensation cycles [28]. The stable isotopic composition of water relative to the GMWL revealed important information on groundwater recharge patterns, the origin of waters in hydrologic systems, and mixing of groundwater and surface water [30, 31].The isotopic composition of groundwater is equivalent to the average weighted value of recharge sources. Therefore, there are deviations in isotope ratios between groundwater and precipitation. Understanding the transfer function of precipitation to groundwater is crucial to the study of groundwater sources. The transfer function can provide basic information of recharge mechanism [32].Groundwater in the study area was recharged by rainfall and river water. In the study of basin water balance, it was important to assess the actual recharge of groundwater by rainfall and river water. The stable isotopes of groundwater were determined by the percentage of recharge from the relevant sources. It is assumed that the groundwater in the vicinity of the study area is a mixture of the Hun River and the precipitation. Based on the mass balance calculation of oxygen and hydrogen isotopes, the contribution percentage of each recharge source to groundwater in the study area could be evaluated by the following equation:(1)GVP+VR=PVP+RVR,G=PVPVP+VR+RVRVP+VR=P1−X+RX,X=G−PR−P×100%,where P is the precipitation stable isotope value, R is the river water stable isotope value, G is the groundwater stable isotope value, Vp is the amount of precipitation, VR is the amount of river water, X is the recharge proportion of river water, and 1−X is the recharge proportion of precipitation.According to the groundwater level in June 2011, two profiles were chosen to calculate the recharge of groundwater from the Hun River. The values ofδ2Hwater and δ18Owater in river water and rain were used as the endpoints for calculating groundwater recharge. Using the results of δ2Hwater and δ18Owater in groundwater, river, and rain samples (Section I and II in Table 6), the recharge ratios of the Hun River to the groundwater are 55.56%–86.60%, respectively, and average value is 74.04%.Table 6
The recharge ratios of the Hun River to the groundwater.
Section
Point
Distance from Hun River (km)
G (‰)
R (‰)
P (‰)
θ (%)
I
LG18
1.02
δ18O
−8.69
−9.14
−7.59
70.97
δ2H
−52.44
−66.92
−64.98
86.60
II
ZK05
0.66
δ18O
−8.49
−9.21
−7.59
55.56
δ2H
−52.44
−65.7
−63.45
83.03
III
JS23-1
0.41
δ18O
−8.80
−9.87
−8.32
30.97
δ2H
−54.90
−71.90
−64.90
58.82
IV
LG42-2
0.47
δ18O
−8.88
−9.79
−8.32
38.10
δ2H
−54.90
−72.30
−66.00
63.79For September 2012, two profiles were chosen according to the groundwater level. Using the results ofδ2Hwater and δ18Owater in groundwater, river, and rain samples (Section III and IV in Table 6) the recharge ratios of the Hun River to groundwater are 30.97%–63.79%, respectively, and average value is 47.92%.The recharge ratios of the Hun River to the groundwater in the dry season were about 55.56%–86.60%, and the ratio in the wet season was about 30.97%–63.79%. The difference in recharge ratio between the two seasons may be caused by seasonal variations and changes in groundwater exploitation intensity in the water source wells. In June 2011, the water source wells were in the mining state, and when the sample was taken in September 2012, the water source wells were almost not in use.


### 4.5. Source Identification of Groundwater Nitrogen Contamination

A key objective was to identify the sources of nitrogen pollution in the groundwater. Isotopic composition can be used to identify sources of groundwater contamination. Because different sources of NO3− have different δ15Nnitrate and δ18Onitrate values, we identified the major contaminant source of NO3− in groundwater by detecting the NO3− isotopic composition in this study. Figure 4 shows the δ15Nnitrate and δ18Onitrate values for the sample in the study area and the typical ranges for the major possible sources of NO3− [33, 34]. The main source of nitrogen could be attributed to the manure and septic waste by human activities, and the distribution of various nitrogen sources is shown in Figure 5. By using an isotopic source apportionment model based on the bias analysis of SIAR, Wang (2016) also found that the contribution rate of manure and sewage contamination is much higher than that of the other sources, reaching 76%–86% in the northern part of the study area.Figure 4
Dual-isotope method for nitrate source attribution in groundwater, September 2012. Modified from Fenech et al. [33].Figure 5
Nitrogen source spatial distribution in groundwater, September 2012.In addition, soil samples were collected for the analysis of nitrogen and oxygen isotopes. Figure6 shows the δ15Nnitrate versus δ18Onitrate values for soil samples and different sources. It indicates that in the soil, δ15Nnitrate values range from −10‰ to +15‰.Figure 6
Dual-isotope method for nitrate source attribution in soil, September 2012. Modified from Fenech et al. [33].The location of the soil samples and the actual utilization of land showed in Figure7 indicates that soil samples affected by manure and sewage were mainly distributed in the northwest of the study area. This was consistent with the analysis above; that is, groundwater pollution mainly results from manure and sewage infiltration [20, 21]. Nitrate in soil, originating from ammonium contained in soil input by fertilizers and precipitation, is mainly located in the southern part of the study area. This is consistent with the actual situation in the south area, mainly for farmland and green land.Figure 7
Sample point distribution and its nitrate source of soil samples in September 2012.


## 4.1. Hydrochemistry Analysis

The statistical results of the chemical index of the samples of groundwater and surface water are shown in Tables2 and 3. The variation range of pH in groundwater (both the southern and northern side of the study area) was 5.94–7.41, and the majority of the samples were within natural pH range of 6.50–8.50. The pH of surface water (Hun River) varied from 7.14 to 8.20 with a mean of 7.60, which was generally higher than the values in the groundwater. Lower pH of the water in the study area might be associated with CO2 produced by microbial respiration in the surface soil [19] or associated with local precipitation infiltration [20, 21]. The EC results in groundwater ranged from 511.50 to 1783.00 μS·cm−1, while the values for surface water ranged from 877.20 to 1231.90 μS·cm−1. The standard of drinking water for EC values in the World Health Organization (WHO) was between 500 and 1500 μS·cm−1 (Rodier, 1996), and some samples in both groundwater and the Hun River were higher than the standard value. From 2001 to 2005, nearly 400,000 tons of domestic sewage water and a portion of industrial waste water were discharged into the Shenyang section of the Hun River without treatment every day (Lin et al., 2007); the polluted river recharged the aquifer and may lead to the increase of EC value. The relative errors of charge balance for all the elements in groundwater and river in June 2011 were −1.53% and −1.49%, respectively, and those for March 2011 were 4.71% and 5.67%, respectively.Table 2
Statistical summary of hydrochemical data in the Shenyang areas, March 2011. All units are in mg·L−1, except for electrical conductivity (EC, μS·cm−1).
Parameter
Groundwater
The Hun River
Southern side
Northern side
Mean
Max
Min
Mean
Max
Min
Mean
Max
Min
pH
7.08
7.41
6.45
6.44
6.85
5.94
7.60
8.20
7.14
EC
628.86
1035.00
511.50
1170.53
1783.00
650.60
1231.90
1652.00
877.20
Ca
61.79
111.00
34.00
4.13
9.00
1.50
81.81
91.00
70.00
Mg
19.16
35.00
1.00
41.53
85.00
18.00
25.54
32.00
20.00
Na
48.09
70.83
29.92
71.13
113.90
33.43
110.84
182.20
50.69
K
3.66
5.86
2.49
4.04
6.92
2.24
7.22
8.48
4.20
Fe
1.13
5.16
0.06
2.62
23.86
0.13
1.59
4.93
0.99
Mn
1.25
2.46
0.15
2.00
4.04
0.21
0.45
2.29
0.45
NH4-N
2.55
12.11
0.03
0.14
0.68
0.03
12.12
19.00
6.09
Cl
55.58
83.00
30.00
126.73
204.00
53.00
175.18
271.00
102.00
HCO3
189.77
259.16
98.13
153.97
236.47
70.45
201.29
228.97
178.65
NO3-N
9.11
76.27
0.71
137.73
401.02
13.55
2.70
5.61
1.20
SO4
86.96
55.69
154.47
147.86
201.07
75.98
122.70
150.03
96.39Table 3
Statistical summary of hydrochemical data in the Shenyang areas, June 2011. All units are in mg·L−1, except for electrical conductivity (EC, μS·cm−1).
Parameter
Groundwater
The Hun River
Southern side
Northern side
Mean
Max
Min
Mean
Max
Min
Mean
Max
Min
pH
6.86
7.32
6.15
6.61
7.06
6.22
7.26
7.36
7.02
EC
690.18
1033.00
546.50
1356.37
2871.00
619.7
962.15
1399.0
474.8
Ca
72.59
114.20
47.65
130.67
270.20
59.93
53.99
59.62
49.97
Mg
17.34
27.75
11.77
34.78
52.64
12.98
12.86
15.96
11.77
Na
52.19
67.34
33.66
81.89
132.10
38.98
30.71
35.48
27.61
K
4.84
6.90
2.72
7.00
40.41
1.92
4.87
5.38
4.12
Fe
0.89
6.49
0.02
1.21
11.79
0.03
0.35
0.61
0.19
Mn
1.68
3.17
0.02
3.36
9.48
0.04
2.12
6.39
0.43
NH4-N
1.10
4.79
0.06
2.51
17.53
0.03
0.07
0.12
0.05
Cl
61.01
104.60
44.88
136.87
287.62
48.66
46.26
55.33
40.38
HCO3
214.38
281.14
123.17
268.22
527.50
93.71
143.27
123.20
179.40
NO3-N
38.71
102.71
2.58
135.29
338.24
6.23
2.79
4.37
1.77
SO4
92.34
142.32
58.13
174.44
500.32
28.56
75.21
78.19
73.39From 2001 to 2005, the concentration of ammonium nitrogen (abbreviated as NH4+-N) in the river water was as high as 9.72 mg·L−1 to 22.35 mg·L−1 (Lin et al., 2007). A high level of NH4+-N in moving water indicated some kind of contaminant entering the water. The Hun River of the study area was characterized by high levels of ammonium nitrogen concentrations, and all surface water samples exceeded the 0.5 mg·L−1 limit specified by the WHO drinking water standard. The Hun River was close to heavily fertilized fields, and therefore, the manure and sewage discharged into the Hun River might contain a higher ammonium nitrogen.In March 2011, the content of NH4+-N in the water samples of the southern part was larger than that in the northern part. The content of NH4+-N in the Hun River had reached 6.09–12.12 mg·L−1, and the groundwater sampling points of high concentration were located at the riverside. The groundwater level is lower than the river level due to the exploitation of water source wells. Therefore, it can be speculated that the ammonia in groundwater comes from the Hun River. In addition, fertilizers containing ammonium sulfate, (NH4)2SO4, or ammonium nitrate, NH4NO3, might also result in a high level of ammonium ions in the samples. The most serious contaminants in the groundwater were NH4+-N, ranging from 0.02 to 24 mg·L−1, which was followed by NO3−-N (0.16–71.50 mg·L−1), TFe (0.05–12.92 mg·L−1), and Mn2+ (0.15–9.92 mg·L−1). NH4+-N, NO3−-N, TFe, and Mn2+ concentrations at some locations exceeded the 0.5 mg·L−1 (NH4+-N), 11 mg·L−1 (NO3−-N), 0.3 mg·L−1 (TFe), and 0.1 mg·L−1 (Mn2+) limits specified by the WHO drinking water standard. The study area was a primary high iron and manganese groundwater zone [22]. The iron and manganese minerals in the study area were goethite, siderite, and rhodochrosite and contained a small amount of pyrite, magnetite, and pyrolusite [23]. The most common sources of Fe2+, Fe3+, and Mn2+ in groundwater were likely occurring naturally, from weathering of iron and manganese oxide minerals. However, industrial effluent, sewage, and landfill leachate might also contribute to Fe2+, Fe3+, and Mn2+ in groundwater [24, 25].


## 4.2. Groundwater Recharge

The geophysical investigation results showed that there was a close hydraulic connection between the phreatic aquifer in the study area and the Hun River. About 1 million cubic meters of groundwater were pumped every day from the Hun River aquifer for urban water supply, and a groundwater depression cone was formed, which causes continuous recharge of the river water to the phreatic aquifer. The phreatic aquifer and leaky confined aquifer are the main layers for groundwater exploitation in the area, and there is close hydraulic connection between the two aquifers [26]. The geophysical investigation results also revealed that there was a connection between the Hun River and the aquifer 60 m below the surface in the riverside area. As for the water quality, the Hun River, with a long history of pollution, also had a close relationship with groundwater. For example, the nitrogen concentration in groundwater was high, and a large portion was from the seepage of the Hun River, which had already been polluted by the manure and sewage and runoff from heavily fertilized fields, causing the river water to continuously recharge the phreatic aquifer.


## 4.3. Isotopic Compositions of Groundwater and the Hun River

Differences in the content ofδ2Hwater and δ18Owater of groundwater, rainfall, and surface water were used to determine the mixing processes in the groundwater flow system in the study area. δ2Hwater and δ18Owater data typically were plotted on a diagram showing δ2Hwater versus δ18Owater relative to VSMOW. Mean annual values of δ2Hwater and δ18Owater in precipitation collected at many locations around the world plot along a line with a slope of 8 and an intercept of +10 (δ2H = 8δ18O + 10), commonly referred to as the global meteoric water line (GMWL) [27]. The variability in isotopic composition of rainfall from one site to another is a function of several factors, including storm-track origin, rainfall amount and intensity, atmospheric temperature, and the number of evaporation and condensation cycles [28]. The stable isotopic composition of water relative to the GMWL revealed important information on groundwater recharge patterns, the origin of waters in hydrologic systems, and mixing of groundwater and surface water.The exchange of water between river and aquifer could be traced by the difference in stable isotope composition between the regional groundwater and the river water. The results of stable isotope (Tables4 and 5) showed clear mixing between shallow groundwater and surface water in the basin. In groundwater, the mean values of δ2Hwater and δ18Owater for the dry season (June 2011) were −8.87 and −65.12‰, respectively, and those for the wet season (September 2012) were −8.79 and −65.64‰, respectively; because of the lag of river and precipitation recharge, the isotope content in the dry and wet periods is not significantly different. But in the Hun River, the mean values of δ2Hwater and δ18Owater for the dry season (June 2011) were −9.16 and −65.79‰, respectively, and those for the wet season (September 2012) were −9.54 and −70.25‰, respectively. The values of δ2Hwater and δ18Owater in the wet season were −0.38‰ and −4.46‰ higher, respectively, than those in the dry season. Generally, the stable isotopic compositions of precipitation decrease with decreasing temperature and with increasing rainfall amount [29]. The results showed that the effect of precipitation amount was significant, and the stable isotope composition of precipitation decreased with the increase of rainfall amount and air temperature.Table 4
Statistical summary ofδ18Owater (‰) and δ2Hwater (‰) values of groundwater and river water in the study area.
Groundwater
The Hun River
Dry season
Wet season
Dry season
Wet season
δ18O (‰)
δ2H (‰)
δ18O (‰)
δ2H (‰)
δ18O (‰)
δ2H (‰)
δ18O (‰)
δ2H (‰)
Mean
−8.87
−65.12
−8.79
−65.64
−9.16
−65.79
−9.54
−70.25
Maximum
−7.82
−58.77
−6.90
−55.30
−8.90
−64.3
−9.14
−67.60
Minimum
−9.73
−70.24
−13.85
−103.2
−9.39
−66.92
−9.87
−72.30Table 5
Statistical summary ofδ18Onitrate (‰) and δ15Nnitrate (‰) values of groundwater and river water in the study area.
Groundwater
The Hun River
Dry season
Wet season
Dry season
Wet season
δ18O (‰)
δ15N (‰)
δ18O (‰)
δ15N (‰)
δ18O (‰)
δ15N (‰)
δ18O (‰)
δ15N (‰)
Mean
10.87
6.17
5.04
9.74
13.05
3.25
3.16
5.70
Maximum
14.08
13.22
15.02
24.85
15.96
3.87
13.31
7.26
Minimum
7.36
−3.14
−18.36
−7.26
10.13
2.63
−10.36
3.80In Figures3(a) and 3(b) (the size of the symbols represents the perpendicular distance of the sampling site measured from the Hun River), both δ18Owater and δ2Hwater of the groundwater and surface water were located slightly lower than the local meteoric water line (LMWL), these suggesting that there was evaporation in the basin, and the groundwater was a mixture of river water and precipitation, and the influence of the river water recharge was greater than that of the infiltration.Figure 3
Plot ofδ2Hwater and δ18Owater for shallow groundwater, deep groundwater, and surface water samples collected in the study region: (a) dry season; (b) wet season.
(a)
(b)In Figure3, the distribution of deep groundwater and shallow groundwater was approximately the same, which was further consistent with the closely hydraulic connection between the two layers of aquifer. The points representing shallow groundwater were closer to the LMWL, and the phenomenon was more obvious in Figure 3(b) (wet season). This means that the phreatic aquifer was more affected by rainfall than the leaky confined aquifer. The values of δ18Owater and δ2Hwater of the points far away from the river bank (larger symbols) were higher than those near the Hun River (smaller symbols). This indicates that the groundwater in the riverside area is more affected by the river. It receives the recharge of the Hun River, and the isotopic enrichment occurs at a distance from the river.


## 4.4. Mass Balance of Isotopic Compositions of Groundwater

Different stable isotopic compositions of2Hwater and 18Owater in groundwater were used to identify the mixing progress in the study area. The variability in isotopic composition of rainfall from one site to another is a function of several factors, including storm-track origin, rainfall amount and intensity, atmospheric temperature, and the number of evaporation and condensation cycles [28]. The stable isotopic composition of water relative to the GMWL revealed important information on groundwater recharge patterns, the origin of waters in hydrologic systems, and mixing of groundwater and surface water [30, 31].The isotopic composition of groundwater is equivalent to the average weighted value of recharge sources. Therefore, there are deviations in isotope ratios between groundwater and precipitation. Understanding the transfer function of precipitation to groundwater is crucial to the study of groundwater sources. The transfer function can provide basic information of recharge mechanism [32].Groundwater in the study area was recharged by rainfall and river water. In the study of basin water balance, it was important to assess the actual recharge of groundwater by rainfall and river water. The stable isotopes of groundwater were determined by the percentage of recharge from the relevant sources. It is assumed that the groundwater in the vicinity of the study area is a mixture of the Hun River and the precipitation. Based on the mass balance calculation of oxygen and hydrogen isotopes, the contribution percentage of each recharge source to groundwater in the study area could be evaluated by the following equation:(1)GVP+VR=PVP+RVR,G=PVPVP+VR+RVRVP+VR=P1−X+RX,X=G−PR−P×100%,where P is the precipitation stable isotope value, R is the river water stable isotope value, G is the groundwater stable isotope value, Vp is the amount of precipitation, VR is the amount of river water, X is the recharge proportion of river water, and 1−X is the recharge proportion of precipitation.According to the groundwater level in June 2011, two profiles were chosen to calculate the recharge of groundwater from the Hun River. The values ofδ2Hwater and δ18Owater in river water and rain were used as the endpoints for calculating groundwater recharge. Using the results of δ2Hwater and δ18Owater in groundwater, river, and rain samples (Section I and II in Table 6), the recharge ratios of the Hun River to the groundwater are 55.56%–86.60%, respectively, and average value is 74.04%.Table 6
The recharge ratios of the Hun River to the groundwater.
Section
Point
Distance from Hun River (km)
G (‰)
R (‰)
P (‰)
θ (%)
I
LG18
1.02
δ18O
−8.69
−9.14
−7.59
70.97
δ2H
−52.44
−66.92
−64.98
86.60
II
ZK05
0.66
δ18O
−8.49
−9.21
−7.59
55.56
δ2H
−52.44
−65.7
−63.45
83.03
III
JS23-1
0.41
δ18O
−8.80
−9.87
−8.32
30.97
δ2H
−54.90
−71.90
−64.90
58.82
IV
LG42-2
0.47
δ18O
−8.88
−9.79
−8.32
38.10
δ2H
−54.90
−72.30
−66.00
63.79For September 2012, two profiles were chosen according to the groundwater level. Using the results ofδ2Hwater and δ18Owater in groundwater, river, and rain samples (Section III and IV in Table 6) the recharge ratios of the Hun River to groundwater are 30.97%–63.79%, respectively, and average value is 47.92%.The recharge ratios of the Hun River to the groundwater in the dry season were about 55.56%–86.60%, and the ratio in the wet season was about 30.97%–63.79%. The difference in recharge ratio between the two seasons may be caused by seasonal variations and changes in groundwater exploitation intensity in the water source wells. In June 2011, the water source wells were in the mining state, and when the sample was taken in September 2012, the water source wells were almost not in use.


## 4.5. Source Identification of Groundwater Nitrogen Contamination

A key objective was to identify the sources of nitrogen pollution in the groundwater. Isotopic composition can be used to identify sources of groundwater contamination. Because different sources of NO3− have different δ15Nnitrate and δ18Onitrate values, we identified the major contaminant source of NO3− in groundwater by detecting the NO3− isotopic composition in this study. Figure 4 shows the δ15Nnitrate and δ18Onitrate values for the sample in the study area and the typical ranges for the major possible sources of NO3− [33, 34]. The main source of nitrogen could be attributed to the manure and septic waste by human activities, and the distribution of various nitrogen sources is shown in Figure 5. By using an isotopic source apportionment model based on the bias analysis of SIAR, Wang (2016) also found that the contribution rate of manure and sewage contamination is much higher than that of the other sources, reaching 76%–86% in the northern part of the study area.Figure 4
Dual-isotope method for nitrate source attribution in groundwater, September 2012. Modified from Fenech et al. [33].Figure 5
Nitrogen source spatial distribution in groundwater, September 2012.In addition, soil samples were collected for the analysis of nitrogen and oxygen isotopes. Figure6 shows the δ15Nnitrate versus δ18Onitrate values for soil samples and different sources. It indicates that in the soil, δ15Nnitrate values range from −10‰ to +15‰.Figure 6
Dual-isotope method for nitrate source attribution in soil, September 2012. Modified from Fenech et al. [33].The location of the soil samples and the actual utilization of land showed in Figure7 indicates that soil samples affected by manure and sewage were mainly distributed in the northwest of the study area. This was consistent with the analysis above; that is, groundwater pollution mainly results from manure and sewage infiltration [20, 21]. Nitrate in soil, originating from ammonium contained in soil input by fertilizers and precipitation, is mainly located in the southern part of the study area. This is consistent with the actual situation in the south area, mainly for farmland and green land.Figure 7
Sample point distribution and its nitrate source of soil samples in September 2012.


## 5. Conclusions

In this paper, we used multiproxy analysis encompassing environmental isotopes and hydrochemical data to investigate the interactions between surface water and groundwater, as well as to identify the source of nitrogen contamination in groundwater in Shenyang city, China. Our work leads to the following major conclusions.(1)
Water from the Hun River with an enriched isotopic signature moves downwards and laterally and mixes with the lower-gradient groundwater. The use ofδ2Hwater and δ18Owater in surface water and groundwater indicated that river water accounted for around 55.56%–86.60% of the total groundwater recharge in the dry season, and the ratio changed to 30.97%–63.79% in the wet season. The huge supply of groundwater indicates that groundwater is highly susceptible to contamination from land surface activities.
(2)
Stable isotope analyses combined with the chemical and hydrogeological data from this study site indicate that the human activities, such as manure and sewage discharge, are the prevailing source of nitrogen in the waters. This will be useful for future management and decisions to control pollution sources and protect groundwater quality.



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*Source: 8683904-2018-08-23.xml*