Identifying Groundwater Recharge Sites through Environmental Stable Isotopes in an Alluvial Aquifer

Abstract

Environmental isotope tracers have been a useful tool in providing new insights into hydrologic processes. In Mexico, there have been several studies reporting different values for ${\mathsf{\delta }}^{18}\mathrm{O}$ and ${\mathsf{\delta }}^2\mathrm{H}$ for certain geographical areas. The objective of this study is to achieve the isotopic characterization of rainfall and groundwater and to report the comprehensive understanding of groundwater flow processes around and within the Calera aquifer and, consequently, its potential recharge sites. The samples used for the stable isotope analysis (${\mathsf{\delta }}^{18}\mathrm{O},{\mathsf{\delta }}^2\mathrm{H}$) were measured using a GV-Isoprime isotope-ratio mass spectrometer at the Isotopy Laboratory of the Water Center for Latin America and the Caribbean. The $\mathsf{\delta }\mathrm{D}$ of precipitation ranged between −110.20‰ and 10.11‰, with a mean of −55.67‰ $\pm$ 27.81‰. The ${\mathsf{\delta }}^{18}\mathrm{O}$ ranged between −17.80‰ and 2.74‰, with a mean of −9.44‰ $\pm$ 4.74‰. The $\mathsf{\delta }\mathrm{D}$ of groundwater ranged between −81.92‰ and −36.45‰, with a mean of −66.05‰ $\pm$ 8.58‰. The ${\mathsf{\delta }}^{18}\mathrm{O}$ ranged between −18.26‰ and −8.84‰, with a mean of −12.35‰ $\pm$ 2.12‰. The local meteoric water line of the Zacatecas state is$\mathsf{\delta }\mathrm{D}=-2.03+5.68{\mathsf{\delta }}^{18}\mathrm{O}$. The groundwater samples were clustered into four groups. The clustering of the samples led to the finding that streamflows play a significant role in the hydrological balance as a source of local recharge to the aquifer.

1. Introduction

Environmental isotope tracers have been a useful tool in providing new insights into hydrologic processes; they integrate small-scale variability to provide an effective indication of catchment-scale processes [1]. The applications of environmental isotopes as hydrologic tracers in freshwater systems fall into two main categories according to the classification of Kendall and Doctor [1]: (i) tracers of water itself (water isotope hydrology) and (ii) tracers of the solutes in the water (solute isotope biogeochemistry).

Precipitation is an important collector of the major and minor pollutants present in the atmosphere; furthermore, it is an important component of total water resources, making it vital for irrigation, human use, as well as industrial and domestic purposes in inland regions [2,3]. The chemical composition of rainfall is determined by several mechanisms: the condensation of water vapor on cloud condensation nuclei, the capture of species inside the cloud droplets (rainout), and scavenging processes below the clouds (washout) [4,5]. Particularly, there are two factors that control the isotopic character of rainfall: (a) the temperature of condensation of the precipitation and (b) the ratio of water vapor that has already condensed into precipitation to the initial amount of water vapor in the air mass. Nevertheless, other factors such as altitude, latitude, inland distance along different storm tracks, environmental conditions at the source of the vapor, and humidity also influence the isotopic composition of precipitation [1]. Oxygen and hydrogen isotopes (${\mathsf{\delta }}^{18}\mathrm{O}$ and ${\mathsf{\delta }}^2\mathrm{H}$) can be used to determine the source of groundwater and surface waters; in nature, there is a similar systematic isotopic fractionation of stable hydrogen and oxygen; thus, their behavior in the hydrologic cycle is also similar. This similarity rises to a covariance between the stable hydrogen and oxygen isotopic concentration; the covariance was defined by Craig [6] as follows:

$$\mathsf{\delta }\mathrm{D}=8{\mathsf{\delta }}^{18}\mathrm{O}+10$$

(1)

This relation defines the Global Meteoric Water Line (GMWL), and was obtained by using a linear regression method derived from the isotopic analysis of precipitation, snow water, and river water from all over the world; most of the precipitation in the world follows this relationship [7]. The slope and the intercept of this equation are useful in understanding the systematic isotopic fractionation controlled by the hydrologic cycle [8]. The slope and intercept of the “Local Meteoric Water Line” (LMWL) for precipitation from a specific region can be different from the GMWL [8]. The intercept, which is usually called the deuterium excess parameter ($\mathrm{d}$-excess, or $\mathrm{d}$), has been used to describe different Meteoric Waterlines (MWLs), such that:

$$\mathrm{d}={\mathsf{\delta }}^2\mathrm{H}-8{\mathsf{\delta }}^{18}\mathrm{O}$$

(2)

Arid and semiarid regions account for more than a third of the world’s land surface and are characterized by receiving less than 250 mm/year of rainfall [8]. In these regions where water scarcity is a major issue, the groundwater is often the principal water supply; furthermore, in these areas, groundwater resources may be fossil resources [8,9].

In Mexico, there have been several studies reporting different values for ${\mathsf{\delta }}^{18}\mathrm{O}$ and ${\mathsf{\delta }}^2\mathrm{H}$. Kretzschmar and Frommen [10] identified the stable isotope composition for surface and groundwater samples in Baja California, based on a total of 135 samples. The authors reported significant variations in its isotopic signature depending on the type of water tested and depending on the study area; however, an LMWL was not presented. In the Gulf of Mexico area, different studies have presented LMWLs, particularly in the state of Veracruz. Lanchiet and Patterson [11] in a study made in the northern Central America report the meteoric line as $\mathsf{\delta }\mathrm{D}=7.1{\mathsf{\delta }}^{18}\mathrm{O}+6.3$. Afterwards, Goldsmith et al. [12] presented two LMWLs (2008–2009: ${\mathsf{\delta }}^2\mathrm{H}=8.36{\mathsf{\delta }}^{18}\mathrm{O}+21.0$; 2009–2010: ${\mathsf{\delta }}^2\mathrm{H}=8.10{\mathsf{\delta }}^{18}\mathrm{O}+16.6$); in the same region. Quezadas et al. [13] presented their LMWL ($\mathsf{\delta }\mathrm{D}=7.4{\mathsf{\delta }}^{18}\mathrm{O}+7.3$) with data collected from 2007 to 2012. Other investigations have been carried out in southwestern Mexico, specifically in the states of Jalisco and Colima. Hernández-Antonio et al. [14] collected stable water isotopes from 40 wells around the Guadalajara metropolitan area to explain the groundwater flow dynamics, and authors concluded that local flow is associated with the infiltration of rainwater that occurs at higher altitudes. Hartosough et al. [15] sampled multiple components of the water cycle to test for differences before and during the North American Monsoon System (NAMS) in 2003–2004 and presented two meteoric lines (pre-monsoon: $\mathsf{\delta }\mathrm{D}=7.44{\mathsf{\delta }}^{18}\mathrm{O}+3.3$; monsoon: $7.17{\mathsf{\delta }}^{18}\mathrm{O}+2.5$) for both periods.

The present study was carried out in Mexico, particularly in the northern zone of the Mexican state of Zacatecas, which is located in the central-northern part of the country. The objective of this study is to obtain the isotopic characterization of rainfall and groundwater, as well as to report the comprehensive understanding of groundwater flow processes around the Calera aquifer and, consequently, its potential recharge sites. By comparing the signatures, it is possible to identify possible groundwater recharge sites. Since isotopic meteoric lines vary with region, a local meteoric line needs to be determined. In this study, the relationship between ${\mathsf{\delta }}^{18}\mathrm{O}\left(\text{‰}\right)$ and $\mathsf{\delta }\mathrm{D}\left(\text{‰}\right)$ measured in the cumulative rainfall between each sampling time, as a time series based on samples, was collected for 2014 and 2015.

2. Materials and Methods

2.1. Study Area

The Mexican state of Zacatecas is located at the central-northern part of the country; as a semiarid region, it is characterized by low rainfall values and consequently low surface runoff, but industrial activity and agricultural irrigation take place. In this region, groundwater is the main source that sustains economic development. The climate in Zacatecas is mainly arid, and half of the population lives in rural areas; therefore, irrigated agriculture is one of the most profitable economic activities. According to CONAGUA (National Commission of Water) [16], over 130 thousand hectares are irrigated with an annual volume of 330 hm³, producing annual groundwater levels drawdowns from 1 to 5 m, due in large part to rudimentary and outdated irrigation systems with efficiencies below 45%. This fact together with the incipient increase in population has caused a higher rate of water extraction to satisfy the demand for food and services [17]. The Calera aquifer is located in the central zone of the Zacatecas state, and has an area of 2087.6 km², with a mean rainfall of 450 mm/year, resulting from a rainy season that occurs mainly between June and September and a potential evapotranspiration of 1900 mm/year. This aquifer is the main source of fresh water for agricultural and industrial activities, with an annual mean extraction of 125 mm³ [18]. The general map of the study area is shown in Figure 1.

2.2. Ordinary Least Squares Regression

The Ordinary Least Squares Regression method (OLSR) and the Reduced Major Axis (RMA) were used to determine the LMWL for Zacatecas. According to the report by Hughes and Crawford [19] for the OLSR, the slope ($a$) is given by:

$$a=\frac{{{\displaystyle \sum }}^{\text{}}xy-\frac{{{\displaystyle \sum }}^{\text{}}x{{\displaystyle \sum }}^{\text{}}y}{n}}{{{\displaystyle \sum }}^{\text{}}{x}^2-\frac{{\left({{\displaystyle \sum }}^{\text{}}x\right)}^2}{n}}$$

(3)

The intercept (b) is given by:

$$b=\frac{{{\displaystyle \sum }}^{\text{}}y}{n}-a\frac{{{\displaystyle \sum }}^{\text{}}x}{n}=\overline{y}-a\overline{x}$$

(4)

For the RMA, the slope of the line of the best fit is given by:

$$a=\frac{S_y}{S_x}={\left[\frac{{{\displaystyle \sum }}^{\text{}}{y}^2-\frac{{\left({{\displaystyle \sum }}^{\text{}}y\right)}^2}{n}}{{{\displaystyle \sum }}^{\text{}}{x}^2-\frac{{\left({{\displaystyle \sum }}^{\text{}}x\right)}^2}{n}}\right]}^{0.5}$$

(5)

The intercept is given by:

$$b=\overline{y}-a\overline{x}$$

(6)

2.3. Sampling, Preservation, and Laboratory Analysis

The rainfall samples were collected using a 20-L plastic container lined with thermal insulation and reflective paper. Likewise, heavy mineral oil was used; this mineral oil behaves as a layer floating on the rainfall water, with the aim of minimizing evaporation. The mineral oil is inert; consequently, the isotopic composition of rainfall water will not be modified by its incorporation. Precipitation and groundwater samples were collected for oxygen and hydrogen isotopic analyses from 2014 to 2015. Rainwater samples were not filtered and collected in 50-mL bottles from the plastic containers. To avoid air bubbles being trapped within, both rainwater and groundwater sample bottles were filled to the brim [20]. Then, the sample bottles were stored in cool dry ice chests away from light in accordance with IAEA (International Atomic Energy Agency) [20] guidelines. A total of 144 water samples was taken as follows: 115 groundwater samples and 29 precipitation samples; the surface water was not sampled. Groundwater was sampled through wells at a depth ranging between 65 and 125 m below the ground surface. All 29 rainwater isotope data were used to determine the local meteoric water line.

The sampling locations were chosen according to the recommendations by Kendall and Doctor; the main recommendation was to consider the elevation of the sampling locations [1]. Rainfall sampling locations and a general map of the study area are shown in

Table 1. Rainfall sampling locations (elevation values are in meters above mean sea level).

Site	Sample ID	Latitude	Longitude	Elevation (mamsl)
Fresnillo	RA1	23°10′43.77″	102°52′57.35″	2198
Villa de Cos	RA2, RA8, RA26	23°17′16.33″	102°20′29.33″	1984
La Bufa Zacatecas	RA6, RA7, RA18	22°46′43.23″	102°34′0.38″	2580
Genaro Codina	RA3, RA9, RA16	22°35′30.0″	102°39′2.68″	2330
Nueva Alianza	RA4, RA15	22°53′55.56″	102°51′33.44″	2287
Catarinas	RA11, RA12	23°6′13.80″	102°38′42.81″	2087
Trancoso	RA5, RA10, RA17	22°44′26.91″	102°22′5.07″	2200
Tanque de Guadalupe	RA13, RA23	24°33′49.27″	102°3′48.99″	1920
Estacion Camacho	RA14, RA25	24°26′26.45″	102°22′29.39″	1660
Concepción	RA19, RA21	23°59′59.7″	102°59′58.0″	1937
Rio Grande	RA20, RA28	23°49′38.02″	103°1′57.66″	1875
Sombrerete	RA24, RA29	23°23′52.90″	103°45′16.19″	2703
Juan Aldama	RA22, RA27	24°18′8.28″	103°23′7.57″	1994

. The pH, EC (electrical conductivity), and temperature were measured in the field with HACH HQ430d equipment. The standard calibration was performed with a pH buffer of pH 4.01 and pH 7.00; for EC, the calibration was performed using KCl.

The samples used for the stable isotope analysis (${\mathsf{\delta }}^{18}\mathrm{O},{\mathsf{\delta }}^2\mathrm{H}$) were measured using a GV-Isoprime isotope-ratio mass spectrometer at the Isotopy Laboratory of the Water Center for Latin America and the Caribbean, located at the Monterrey Institute of Technology and Higher Education, Nuevo León, México. Analyses for ${}^{18}\mathrm{O}$ and ${}^2\mathrm{H}$ are expressed in $\mathsf{\delta }$notation relative to the Vienna Standard Mean Ocean Water (VSMOW). The measurement precision for the stable isotopes was $\pm 0.33\text{‰}$ and $\pm 1.78\text{‰}$ for ${\mathsf{\delta }}^{18}\mathrm{O}$ and ${\mathsf{\delta }}^2\mathrm{H}$, respectively.

3. Results

3.1. Isotopic Composition of Precipitation

The isotopic signatures of 29 samples of precipitation in the Zacatecas state were analyzed. The data are presented in

Table 2. Chemical and isotopic compositions of precipitation samples collected in the Zacatecas state (isotopic values are in ‰, EC (µS/cm), T in °C, pH and d-excess.

Sample ID	δD	δ18O	pH	T	EC	d-Excess
RA1	−88.76	−13.92	7.07	12.7	143	22.60
RA2	−100.14	−16.44	7.13	12.4	178.1	31.38
RA3	−98.62	−16.22	7.54	11.4	219	31.14
RA4	−64.00	−9.50	7.76	13.3	312	12.00
RA5	−110.20	−17.80	7.77	16.7	71	32.20
RA6	−88.53	−15.32	7.5	15.2	95	34.03
RA7	−47.01	−10.16	7.4	15.6	89	34.27
RA8	−50.70	−8.40	7.6	16.2	143	16.50
RA9	−54.44	−8.84	7.78	12.9	233	16.28
RA10	−50.50	−9.92	7.6	13.2	108	28.86
RA11	−75.08	−13.20	7.4	15.3	103	30.52
RA12	−20.04	−4.70	7.5	16.2	107	17.56
RA13	−27.50	−5.10	7.6	14.9	175	13.30
RA14	−84.80	−14.03	7	15.3	169	27.44
RA15	−44.21	−6.41	7.2	16.2	143	7.07
RA16	−62.80	−10.06	7.56	12.3	101	17.68
RA17	−65.00	−12.60	7.77	17.5	78	35.80
RA18	−70.90	−12.54	7.5	15.2	194	29.42
RA19	−55.80	−11.40	7.93	16.9	101	35.40
RA20	−35.01	−6.52	7.6	16.2	111.2	17.15
RA21	−68.14	−12.37	7.07	14.3	176	30.82
RA22	−24.50	−5.35	7.4	14.3	95.2	18.30
RA23	−36.42	−6.64	7.3	14.7	85	16.70
RA24	−61.70	−11.20	7.2	15.1	82	27.90
RA25	−21.18	−3.03	7.1	16.1	138	3.06
RA26	−11.17	−1.15	7.3	14.3	179	−1.97
RA27	−53.68	−5.37	7.8	15.7	253	−10.72
RA28	−53.82	−8.44	7.3	15.2	145	13.70
RA29	10.11	2.74	7.3	16.8	158	−11.81

. The $\mathsf{\delta }\mathrm{D}$ of precipitation ranged between −110.20‰ and 10.11‰, with a mean of −55.67‰ $\pm$27.81‰. The ${\mathsf{\delta }}^{18}\mathrm{O}$ ranged between −17.80‰ and 2.74‰, with a mean of $-9.44\text{‰}\pm 4.74\text{‰}$. The $\mathrm{d}$ ranged between −11.81‰ and 35.80‰, with a mean of $19.88\text{‰}\pm 13.01\text{‰}$. The OLSR analysis showed the Local Meteoric Water Line (LMWL) for the studied region of Zacatecas state to be $\mathsf{\delta }\mathrm{D}=-2.03+5.68{\mathsf{\delta }}^{18}\mathrm{O}$ with a ${\mathrm{R}}^2=0.94$. The LMWL was plotted, and was found to have an intercept of −2.03, which is lower than the intercept of GMWL of 10. This difference may be due to the elevation of the sampling locations affecting the arrival of air masses, besides other possible influencing factors including air, temperature, secondary evaporation, moisture source, as well as the spatial and temporal variability of precipitation [21,22] (see Figure 2). The pH values of the research were measured in locations away from urban areas. The pH value reflects the acidic or alkaline degree of rainwater. The pH of rainwater in large cities is lower than that of the unpolluted area, which reflects the impact of anthropogenic activities on rainwater. The rainwater in Zacatecas state is significantly alkaline, suggesting an important effect of mineral dust from arid lands on rainwater, which is consistent with the report by Rao et al. [23].

3.2. Isotopic Composition of Groundwater and Recharge Sites

The stable isotope composition of groundwater reflects that precipitation in the recharge area seeps through the soil and the unsaturated zone to reach the water table. The potential infiltration of precipitation (only rain falling above a certain threshold rate contributes to recharge) into the soil and the unsaturated zone is, in principle, an isotopically non-fractionating process. In arid conditions, the movement of water can be upwards: water moves up in liquid and vapor phases in the unsaturated zone, eventually reaching the land surface to be lost as evaporation in the atmosphere [8]. Groundwater samples were obtained for a specific zone of Zacatecas, specifically around and within the Calera aquifer. The isotopic signatures of 115 samples of groundwater in and around the Calera aquifer were analyzed; the data are presented in the Supplementary File. The $\mathsf{\delta }\mathrm{D}$ of groundwater ranged between −81.92‰ and −36.45‰, with a mean of −66.05‰ $\pm$8.58‰. The ${\mathsf{\delta }}^{18}\mathrm{O}$ ranged between −18.26‰ and −8.84‰, with a mean of −12.35‰ $\pm$ 2.12‰. The $\mathrm{d}$ ranged between −0.85‰ and 82.94‰, with a mean of 32.76‰ $\pm$ 23.71‰. There are different multivariate methods to group the samples; one widely-used method is the Hierarchical Cluster Analysis (HCA) approach, which has been used in the clustering of groundwater samples by several investigations [24,25,26]. Nevertheless, the groundwater samples in this study are clustered into four groups. These groups were established with respect to the distance from the LMWL (see Figure 3).

3.3. Deuterium Excess

The isotopic composition of moisture in the marine atmosphere is controlled by air-sea interaction processes, and the d-excess value is fixed by these processes [27]. Figure 4 shows the statistical summaries of the d-excess values of rainwater and groundwater in the study area. The deuterium excess in precipitation and atmospheric water vapor provide information on the role of diffusive transport in the boundary layer at the evaporative source and on source temperatures that cannot be obtained from $\mathsf{\delta }\mathrm{D}$ or ${\mathsf{\delta }}^{18}\mathrm{O}$ individually available [28]. Rainwater samples in the study area present suggested d-excess values in the range of −11.81‰ and 35.80‰, with an average of 19.88‰. Of all the samples, 82.75% presented d-excess values higher than 10, which suggests the probable inputs of recycling water vapor and the contribution of possible surface flows to the rain clouds according to Fynn [29], where it was also established that low d-excess values may also have been derived from isolated local moist air masses having those characteristics. The d-excess value is a function of several factors, such as the temperature, humidity, and the isotopic characteristics of the ambient water vapor and the evaporating water.

The computed d-excess values of groundwater samples ranged between −0.85‰ and 82.94‰, with an average of 32.76‰. The average value of 32.76‰ was different from that of the local meteoric water line, making the evolutionary trend from precipitation in the study area to groundwater unclear. A higher variability of groundwater data was found, according to the research presented by Fynn et al. [29], and this variability suggests inputs from various sources and the spatial variability in the nature of the vadose zone. Variable infiltration rates are imposed by the spatial heterogeneity of the material of the vadose zone, leading to variable exposures of the infiltrated water to the effects of fractionation attending evaporation.

4. Discussion

Recharge to Aquifers

Stable isotope data can be used to evaluate possible sources of water for the Calera aquifer. All of the groundwater samples are shown in Figure 3, and they were subsequently clustered into four groups.

Groups 1 and 4 fall left on the LWML, which means this groundwater was recharged from the Calera aquifer; likely, the recharge originated in the southwest region out of the aquifer, as this area is characterized by a high density of streams and fissures and is consistent with the groundwater flow direction reported by Junez et al. [18]. Group 3 fits around the LMWL, indicating that these groundwater samples have been recharged from local precipitation. Furthermore, Figure 5 shows that these samples are closer than other samples to the streams in the study area. These streams can be classified as perched streams, as opposed to connected streams. They are hydraulically disconnected from the phreatic zone of the aquifer, which means that there is a vadose zone below the riverbed; consequently, they are losing streams and lose water mainly by outflow through the riverbed. The proximity of these groups to the streams may indicate that the streamflow represents one type of vertical recharge to the Calera aquifer, and this water can mix with other input flows in the aquifer. Besides, this group is close to the mountains, where the recharge from precipitation can appear, which is consistent with what was reported by Pacheco-Guerrero et al. [30], McCallum et al. [31], Shanafield and Cook [9], Goodrich et al. [32], and Shentis and Rosenathal [33]. Nevertheless, different types of horizontal recharge can be present in the aquifer. Two fissure systems are shown in Figure 5: shallow fissure and regional fissure systems; these fissures are potentially hydraulically connected with streams favoring the leakage from streams to the underlying unconfined aquifers. Group 2 falls right on the LWML, demonstrating that these samples have undergone some evaporation prior to infiltration [21,34].

The presence of different flow systems or mixing among them can impact the isotopic composition of the groundwater, leading to different cluster groups; there is a potential mixing of the regional groundwater system (G1, G4) with local systems (G3, G2) (Figure 6). The mixing probably results from the effect of fracture systems, as well as surface water and groundwater processes. Wassenaar et al. [35] reported groundwater data for $\mathsf{\delta }\mathrm{D}$and ${\mathsf{\delta }}^{18}\mathrm{O}$ in Mexico; two of their sample points are in the Calera aquifer; namely, two of the sampled points by Wassenar et al. are in the study area. The authors reported values of −7.3 and −10.2 for ${\mathsf{\delta }}^{18}\mathrm{O}$ and −63.2 and −73.9 for $\mathsf{\delta }\mathrm{D}$. These reported values are spatially consistent with the data reported in this investigation. The monitored altitude ranges between 1660 and 2703 mamsl, and there is not a relation found between the ${\mathsf{\delta }}^{18}\mathrm{O}$ and altitude. Other geographical parameters such as the longitude or latitude can affect the relation with the ${\mathsf{\delta }}^{18}\mathrm{O}$, which is consistent with what was reported by Liu et al. [36].

Based on the isotopic composition of groundwater and clustering, a regional geochemical conceptual model (Figure 6) was proposed along a representative cross-section of the study area. The flow patterns are presented, and different hydrogeologic environments are represented with their associated clusters. The Paleogene tertiary rhyolite allows the movement of water through the fractures; moreover, the rhyolite is covered by quaternary alluvial. The composition of the groundwater from wells settled and close to ephemeral streams is close to the rainwater composition.

5. Conclusions

Environmental isotopes in groundwater of the Calera aquifer were used to identify different sources of water contributing to the groundwater recharge. This research examined the stable isotopic composition of precipitation in the Zacatecas state and groundwater around and within the Calera aquifer. The resultant LMWL for the Zacatecas state is$\mathsf{\delta }\mathrm{D}=-2.03+5.68{\mathsf{\delta }}^{18}\mathrm{O}$. The slope and intercept values of the local meteoric water line are all lower than those of the global meteoric water line, and these differences are attributed to the continentality (~400 km away from sea), altitude (over 2000 mamsl), and the climatic conditions of the area affected by the humidity from the Pacific Ocean and the Gulf of Mexico. The d-excess values of groundwater on average seem to be higher than those of the local meteoric water line, due to groundwater having been subjected to several evaporative and infiltration processes. The clustering of the samples led to the finding that streamflow plays a significant role in the hydrological balance as a source of local recharge to the aquifer. The obtained results in this research contribute to the improvement of water management decisions with the objective of achieving an environmentally sustainable approach. In order to confirm the assumption that streamflow in the network drainage is the main groundwater recharge source, it will be necessary to examine the radioactive isotopic composition of groundwater (tritium and ${}^{14}\mathrm{C}$). The presented data offer a tool for groundwater recharge assessment in arid and semiarid regions. Future research should analyze the isotopic stable composition of streamflow and the hydraulic linkage between fissure systems and rivers.