International Scholarly Research Notices

International Scholarly Research Notices / 2013 / Article

Research Article | Open Access

Volume 2013 |Article ID 930207 | https://doi.org/10.1155/2013/930207

M. Cecilia Giménez, Patricia S. Blanes, Edgar E. Buchhamer, Rosa M. Osicka, Yamila Morisio, Silvia S. Farías, "Assessment of Heavy Metals Concentration in Arsenic Contaminated Groundwater of the Chaco Plain, Argentina", International Scholarly Research Notices, vol. 2013, Article ID 930207, 12 pages, 2013. https://doi.org/10.1155/2013/930207

Assessment of Heavy Metals Concentration in Arsenic Contaminated Groundwater of the Chaco Plain, Argentina

Academic Editor: J. A. Jönsson
Received16 Jul 2013
Accepted19 Aug 2013
Published17 Sep 2013

Abstract

The occurrence and distribution of arsenic and 23 other trace elements have been investigated in groundwater from Comandante Fernández Department in the Central region of Chaco Province, Northern Argentine. The arsenic concentrations samples ranged between 0.7 to 1990 µg L−1; 91% ( ) exceeds the 10 µg L−1 World Health Organization (WHO) provisional standard limits for drinking water. Fluorine was detected in 31% of groundwater samples. Furthermore, there was found a significant correlation between As and F ( ), indicating an association in the prevalence of both elements. In addition, about 78%, 31%, 16%, 13%, and 4.5% of groundwater samples had, respectively, B, Fe, Al, Mn, and Sb exceeding Código Alimentario Argentino (CAA) guideline values. In contrast of the previously values descript, the corresponding to Cr, Be, Ni, Pb, Ag, Se, and Zn were found below the quantification limit. The presence of As and trace elements in groundwater represents an important issue because it can cause a public health problem.

1. Introduction

Among known pollutants, trace elements are widely recognized as being potentially toxic to living organisms. Water contamination with heavy metal (HM) are mainly determined by natural (i.e., weathering, erosion of bed rocks, and ore deposits) [1] and anthropogenic (i.e., mining, industries, and agriculture) processes [2].

Soils and water containing high levels of arsenic and other toxic trace elements can easily contaminate plants, animals, and human beings in contact with them, as they either produce toxic effects or accumulate in plants and thereby enter animal and human food chains [3].

Certain elements like sodium (Na), potassium (K), calcium (Ca), magnesium (Mg), iron (Fe), manganese (Mn), copper (Cu), cobalt (Co), and zinc (Zn) are essentially required by living organisms in specific concentrations but may produce toxic effects in high concentrations [2]. The main threats to human health from HM are associated with exposure to lead (Pb), mercury (Hg), cadmium (Cd) and arsenic (As), which are extremely prejudicial owing to their toxicity, long persistence, and bioaccumulative nature [4]. Their toxic effects include headache, hypertension, irritability, abdominal pain, nerve damages, liver and kidney problems, sideroblastic anemia, intellectual disabilities, fatal cardiac arrest, and carcinogenesis. These metals have been extensively studied and their effects on human health regularly reviewed by international bodies such as the WHO [5].

Long-term drinking of arsenic contaminated water can cause severe skin diseases including skin cancer; lung, bladder, and kidney cancers, and perhaps other internal tumors; peripheral vascular disease; hypertension; and diabetes [6, 7]. It also seems to have a negative impact on reproductive processes (infant mortality and weight of newborn babies) and cardiovascular diseases [8].

The occurrence of high concentrations of As and trace elements in drinking water has been recognized, over the past two or three decades, as a great public health concern in several parts of the world [6, 9]. The Chaco-Pampean plain is the largest one in Latin America and one of the largest geographic units in the world affected by As-contaminated groundwater [10]. In the Chaco plain (north of the Chaco-Pampean plain), the major source of arsenic in groundwater is chemical weathering of the rocks, and no anthropogenic sources of contamination have been reported [11].

Particularly, it has been identified that there are elevated As concentrations in groundwater and reported in different regions of Argentina such as La Pampa [1], Buenos Aires [9], Chaco [11], Cordoba [12], Santiago del Estero [13], Santa Fe [14], and Tucumán [15] Provinces. Detailed information of the arsenic concentration in the groundwater of the Central-West region of Chaco is available in recent publications; high fluorine (F) and As contents in drinking waters have also been reported [11, 16]. In addition, a positive correlation between As and F has been found ( ).

In the study area, it is necessary to carry out the research on the presence of the trace elements in groundwater which are present in concentrations higher than the WHO reference values assigned for health reasons. These elements were selected taking in view the geology of the study area and possible leaching of As and other trace metals previously reported in other areas in Chaco-Pampean plain [14, 15, 17], like vanadium, strontium, barium, chromium, uranium, molybdenum, manganese, and selenium. The residents who lives in As-contaminated areas and consume groundwater are not only exposed to As concentrations but also to high concentration of multiple metals that can cause adverse health effects.

This paper presents an integrated study on the occurrence and the distribution of arsenic and heavy metals (HM) in groundwater in the area of Comandante Fernández in the Central region of Chaco Province, Northern Argentine. In addition, the relations between arsenic occurrence and these chemical components are discussed from a chemical point of view.

2. Materials and Methods

2.1. Location of the Study Area

The study area is located in the Department Comandante Fernández, Chaco Province, Northern Argentina (Figure 1). It covers an area of 1500 km2, and approximately 0.10 million population [11]. Presidencia Roque Sáenz Peña (90000 inhabitants), located between 26°47′27′′ latitudes S and 60°26′29′′ longitudes W, is the most important town where we could find an economy based on agricultural and livestock exploitation.

This area is located within the geologic province known as the Chaco Pampean [11]. The aquifers are hosted in superposed sequences of aeolian and fluvial sediments of the tertiary and quaternary ages [18]. As there are no superficial sources of groundwater, recharge of the phreatic aquifer is produced from rainfalls, while deep aquifer recharge occurs from west to east and northwest-southeast, and it is supposed to be located in the higher parts of the sub-Andean outcrops [19, 20].

The studied zone has a semiarid and subtropical continental type climate, characterized by sultry summers and cold winters, receiving an annual precipitation of 900 mm, between November and March [21].

2.2. Sampling and Analysis

Forty-five groundwater samples were collected during May–October 2010 (a dry season), in rural and suburbs areas of the Comandante Fernández Department (Chaco Province), (Figure 1). Each sample has been collected from each tube well. Latitude and longitude of these tube wells were determined using a Garmin eTrex Legend, Global Positioning System (Garmin Ltd., UK). Specific well information, that is, the depth of the well was obtained from its owner. The sampling points were selected taking into account their spatial distribution in the area, in order to obtain an accurately representative hydrochemistry.

For all analyses, cleaning and sampling procedure involved deionized distilled water (DDW) produced by MilliQ water (Millipore Elix 5) and high-purity solvents. All glassware and polyethylene bottles were kept in 10% (v/v) HNO3 (Merk 65%) for 24 hours, rinsed out with DDI, and dried in a stove. All tube-wells samples were collected after 3 min flushing, filtered through 0.45 μm membrane filters and transferred to three different polyethylene bottles to undertake different analysis. Samples for major cations analysis (Ca2+, Mg2+, Na+, and K+) and total As were acidified with 0.06 M HCl. For trace metals analysis, samples were acidified to pH < 2 by addition of ultrapure nitric acid (Fluka). No acidified fractions were collected without headspaces in the sample bottles for measurements of anions such as Cl, , , F, and alkalinity. All the samples were kept at 4°C until analysis.

2.3. Groundwater Analyses

The physical parameters like water temperature (T), pH, and electrical conductivity (EC) were measured in situ by using a HANNA HI991301 Portable PH/EC/TDS/Temperature Meter. Na+ and K+ were determined by emission flame spectrometry (JENWAY PFP7) and Ca2+ and Mg2+ concentrations were determined by complexometric titration using ethylenediaminetetraacetic acid (0.05N EDTA). Chloride, nitrate, and fluorine ionic activity were measured with ion-selective electrodes using OAKTON CE pH/ION Mod. 510. Alkalinity was analyzed by titration method with sulfuric acid, and sulfate was measured by turbidimetric method using Spectrophotometer UV-Visible Metrolab 1700. For a better detection limit, arsenic was analyzed by hydride generation atomic absorption spectroscopy method (HGAAS) using hollow cathode lamps at 193.7 nm wavelength. The instrument quantification limit for this system was 5 μg L−1; an intermediate precision of less than ±10% was achieved. All these analyses were performed at the Laboratories of Química Analítica, Universidad Nacional del Chaco Austral, Argentina.

Total concentrations of 23 trace elements (Ag, Al, Ba, Be, B, Cd, Co, Cr, Cu, Fe, Mn, Mo, Ni, P, Pb, S, Sb, Se, Si, Sr, Ti, V, and Zn) were determined by inductively coupled plasma-optical emission spectrometry (ICP-OES), (PERKIN ELMER 5100 DV, axial, solid state detector, cross-flow nebulizer, associated with Scott Type chamber, and AS type auto sampler. The equipment was linearly calibrated from 1 to 100 μg L−1 with custom certified standard solution (Merck ICP Multielement Standard Solution XIII). values of calibration curves were >0.995, and no trend was observed in the residuals for all analyzed metals. Linearity was checked after every 10 samples using homemade control solution. If the recovery was greater than ±10%, the recalibration was performed for the concerned element. Accuracy of the procedure it has been tested by analyzing a certified reference material, NIST SRM 1643 c “Trace elements in water.” For the studied elements, bias ranged from 2 to 7%. Precision, expressed as intermediate precision was better than 9% for all analyzed elements.

2.4. Statistical Analysis

All statistical analysis of data, including maximum and minimums, means and medians, was performed using the program STATGRAPHICS 5.1 (Statistical Graphic Corporation. Manugistics Inc.; Rockville, USA). The software Rock Ware Aq.QA version 1.1.5.1 was used to construct the Piper diagrams that depicted the groundwater types.

3. Results and Discussion

3.1. Physicochemical Parameters

The physicochemical parameters determined in selecting 45 groundwater samples are shown in Table 1. Well depth ranged between 5 and 220 m, with average value of 23 m. The pH values of the assorted groundwater samples varied from 6.50 to 8.94 with average value of 7.54 indicating that the waters are generally neutral to slightly alkaline. The measured water temperatures vary from 22.6 to 27.5°C with an average of 23.8°C.


Sample IDDepth (m)pHEC (mS cm−1) Cl Na+K+Ca2+Mg2+Water type

M1307.532.6265626935123.16447.103.541.65Na–HCO3
M2187.460.9450914.418.010.4326 31.3 11.67.50Na–HCO3
M3138.087.078605103108nd1595 29.8 31.98.30Na–SO4
M486.501.7858499.1335111669110 8.965.03Na–SO4
M557.821.5568199.22092.50338 20.010.916.6Na–HCO3
M6207.110.8340821.115912.2132 13.924.511.4Na–HCO3
M7186.901.2749057.122621.2221 11.0 9.105.50Na–HCO3
M8207.682.6949742736949.31034 16.577.444.3Na–Cl
M9138.251.3489545.445.0nd257 2.10 7.395.43Na–HCO3
M102207.9821.59368193207012.25857 32.2206 44.7Na–Cl
M11507.892.44135135480nd522 19.2101 47.9Na–SO4
M12156.960.956791111654.35213 15.220.4 6.45Na–HCO3
M13127.291.367221401072.10382 9.10 1.40 0.54Na–HCO3
M14127.931.4965412983.114.4 806 10.0 2.30 0.52Na–HCO3
M15127.612.37769512412107 531 17.218.9 12.8Na–Cl
M16357.510.6919889.21362.30 200 6.87 28.5 7.54Na–HCO3
M17156.844.48760144743120.1 825 23.2 14.9 46.4Na–Cl
M1886.913.36448166118214.51161 12.1 122 56.9Na–Cl
M19126.781.75302408335200 132 12.9 6.46 2.18Na–Cl
M20137.784.41751142542120.3 775 18.4 22.7 59.8Na–Cl
M21158.288.561017908348527.31814 19.4 63.4 78.7Na–SO4
M22177.360.8825114049.224.5 216 18.412.5 0.92Na–Cl
M23107.241.5998028.011313.4 309 16.3 9.37 3.50Na–HCO3
M2487.161.0680610435.019.3 661 19.032.420.3Na–HCO3
M25147.3123.38355536148619.53158 22.4109152Na–Cl
M26127.951.33356112117nd 877 21.271.632.6Na–HCO3
M27507.254.18651571190nd 836 23.350.122.3Na–HCO3
M28147.889.763211142804nd1969 69.8432147Na–Cl
M29157.065.35405109970745.21065 57.7319120Na–Cl
M30107.641.4186411016412.2 320 15.233.222.1Na–HCO3
M31507.763.059642445196.50 563 7.59 4.57 2.24Na–HCO3
M32127.298.051868130043.210.1 489 3.12 35592.2Na–HCO3
M33107.265.296797625822.30 747 19.512388.4Na–Cl
M34127.531.1550085.191.221.3 268 9.71 19.111.3Na–HCO3
M3588.172.98165216511625.4 549 6.16 3.74 3.90Na–HCO3
M36107.1711.8186874215062.252100 2.71 90.4150Na–SO4
M3787.551.7492073.210813.5 823 8.54 15.6 9.30Na–HCO3
M38208.946.3321410121350nd 994 10.8 18.355.8Na–Cl
M39157.2610.04632634125872.11029 67.8498202Na–Cl
M40527.0019.47644636152023.4 200 54.2183182Mg–Cl
M41658.5124.98175121153739.42100 67.967.0144Na–Cl
M42128.921.4366826.035.521.2 244 11.5 8.06 3.37Na–HCO3
M438 7.281.8161823474.24.50 765 32.457.616.3Na–HCO3
M4411 7.072.5072345090.156.1 223 30.313264.6Ca–Cl
M4512 6.8114.4298567426.342.4 459 28.61100400Ca–Cl

Nd: non detected. All concentrations are expressed as mg L−1.

Major ion compositions of the analyzed groundwater samples and the major water types are shown in Table 1. High nitrate concentrations (max = 200 mg L−1) are present locally in some wells, probably due to anthropogenic influences, and a significant amount of is thought to be from evaporation. However, since the correlation between and Cl is weak ( ), evaporation is unlikely to be the most important cause of the high concentrations.

Considerable spatial variation is observed for the distributions of major cations with dominance of Na+ (132 to 5857 mg L−1); K+ (2.10 to 110 mg L−1); Ca2+ (1.40 to 1100 mg L−1), and Mg2+ (0.54 to 400 mg L−1). The same variation is observed for distribution of major anions, with dominance of (median value 679 mg L−1), Cl (median value 269 mg L−1), and (median value 209 mg L−1). Statistical parameters are shown in Table 2.


ParameterMean MedianRange10th percentil90th percentilStandard deviation

Depth (m)22.013.05.00–2208.0050.033.1
pH7.547.516.50–8.946.908.220.55
EC (mS/cm)5.272.500.69–24.90.9913.46.28
(mg L−1)699679135–1868299974376
Cl (mg L−1)108226914.4–819350.138351832
(mg L−1)57020918.0–348543.91514789
(mg L−1)29.714bdl–2000.0353.436.1
F (mg L−1)1.291.000.10–4.200.303.081.10
Na+ (mg L−1)875644132–58572141907989
K+ (mg L−1)23.618.42.10–1106.9656.321.5
Ca2+ (mg L−1)10128.51.40–11005.33274191
Mg2+ (mg L−1)53.720.30.52–4002.2014976.2
S (mg L−1)49.30.570.006–7240.06125130
P (mg L−1)2.700.80.17–22.90.308.264.41
As (µg L−1)2131007–199017.0500347
Al (µg L−1)56199.060.0–1738060.02572601
Ba (µg L−1)12214.0bdl–14002.00135211
B (µg L−1)40201970156–2191028378965599
Cd (µg L−1)2.002.00bdl–7.01.004.001.40
Cu (µg L−1)23.06.00bdl–2800.1065.848.7
Co (µg L−1)27.23.00bdl–2801.4082.66.20
Fe ( µg L−1)27681.0bdl–20000.10716396
Mn (µg L−1)1525.00bdl–37400.10327574
Mo (µg L−1)23.921.0bdl–1603.0042.030.8
Si (µg L−1)1057150bdl–165700.4024152803
Sr (µg L−1)449862.00–487115.0873873
Se (µg L−1)1.91.00bdl–10.00.16.602.70
Sb (µg L−1)5.41.00bdl–1110.109.001.7
Ni (µg L−1)0.90.10bdl–10.00.103.001.90
V (µg L−1)20476.0bdl–264611.4416431
Zn (µg L−1)83.83.00bdl–28130.1067.0487

Major ion compositions plotted on a Piper diagram (Figure 2) indicate that bicarbonate and chloride were the dominant anions followed by sulfate, and that sodium was the prevalent cation. The major water types in the samples are presented in Table 1.

EC values vary from 0.69 and 24.9 mS cm−1 with a median value of 2.50 mS cm−1 and mean value of 5.27 mS cm−1. This may be due to contribution of Na+, , Cl, and . In saline groundwater, chloride and sulfate are also important. The most saline groundwater samples are of Na–Cl type (maximum Cl concentration 8193 mg L−1; Tables 1 and 2) although Na– types are also important (maximum concentration 3485 mg L−1). The most significant correlations are those of chloride versus EC and sodium ( ; ) and sulfate versus EC and sodium ( ; ), which is related to the predominance of sodium chloride types in groundwater with higher salinity. Sodium bicarbonate waters are related generally with low salinity samples; in analyzed groundwater samples the EC shows poor correlation with ( ).

Results of chemical analysis show large variations in chemical composition and also indicate the high salinity of many of the groundwater samples. According to Larroza and Fariña [19], the salinity of groundwater in the basin of the Chaco region is due to the previous existence of a shallow sea of restricted environment, which has left its salts; this geographical feature, called Paranaense Sea, has originated during the Middle and Upper Miocene. The extremely heterogeneous values of EC from groundwater could be explained by the local variation in sedimentary and hydrogeological characteristics [13]. Moreover, the evaporation in arid and semiarid zones favors the increase of salinity and alkalinity [15, 22].

3.2. Total Arsenic and Fluoride

Arsenic is classified as a human carcinogen (Type A) based on sufficient epidemiologic evidence linking increased mortality from liver, kidney, bladder, and lung cancers to drinking As-contaminated water [23]. The provisional guideline value recommended by the WHO [5] for this carcinogenic contaminant in drinking water is 10 μg L−1 and in Argentina this would be enforced in 2017 [24]. On the basis of this criterion, only 9% (4/45) of groundwater source is within levels recommended for consumption; whereas about 73% (33/45) of all analyzed samples showed As values above 50 μg L−1 (CAA) [25]. Mean concentration of total arsenic in groundwater was 213 μg L−1 and maximum was 1990 μg L−1 (Table 2). The highest As concentration was found in groundwater collected in sample M36. The presence of arsenic in the groundwater samples collected from this region of Argentina is natural; the local geology and rainfall have been shown to have major impact on the variations of As concentration in groundwater.

Different positive correlation were observed in groundwater between As versus and Na+ ( ; ), and a negative correlation was found between As and Ca2+ ( ). It could be assumed that As is associated with Na– system, related to feldspar dissolution [26]. Based on values of pH found in groundwater of this region of Chaco, including data reported from other sites of the region [1, 13, 27], it can be presumed that pH controls As mobility.

The study made by Smedley et al. [28] reveals that highly As(V)-contaminated groundwater in oxidizing environments throughout the world are characterized by high concentration of (>500 mg L−1) and (>250 mg L−1) and pH > 7.50. Similar geochemical conditions occur in the Chaco-Pampean plain, like in the arid regions of Santiago del Estero, Córdoba y La Pampa [13, 14, 27]. High As concentrations are common and dominated by As(V), and the groundwater have correspondingly high F concentrations. These general characteristic are consistent with the analyzed groundwater. However, arsenic speciation is not performed in the present study.

On the other hand, smaller quantities of fluoride ion in the order of 1 mg L−1 in ingested water are usually considered to have a beneficial effect by lowering the rate of occurrence of dental caries. Excessive intake (>1.5 mg L−1) would results in pathological changes in teeth and bones, such as mottling of teeth or dental fluorosis, along with metabolic changes reported on soft tissues such as thyroid, reproductive organs, brain, liver, and kidneys [29].

The WHO guideline value for F concentration in drinking water is 1.5 mg L−1 [5], whereas the Código Alimentario Argentino (CCA) [25] establishes a limit that varies according to the average temperature of the place (1 mg L−1 for an average temperature of 21.5°C in the area under study). The distribution of F concentrations is heterogeneous and similar to As. A positive correlation was observed between As and F with . The analyzed groundwater, 31% (14/45) of the samples exceeded the WHO guideline value of 1.5 mg L−1 [5]. About 47% of all analyzed samples showed F values above 1 mg L−1 recommended by CAA (Table 4). Similar correlations between As and F were also observed in groundwater from neighboring Santiago del Estero [13], Santa Fe [14], and Salta Provinces [30].

In the same way as arsenic, the F rich water is characterized by high concentration of Na+ and low concentration of Ca2+ and Mg2+ ( ; 0.09 and 0.16; resp.). Fluoride is a highly reactive element that combines with other elements in covalent and ionic bonds. It is mainly found in alkaline rocks and alkaline soils, fluorite being the principal component. Gomez et al. [27] explain that the processes that could control the low relationship between F and Ca2+ and the positive relationship between F and bicarbonate ( ) would be the balance equation relating calcite and fluorite when both are in contact with water.

As and other trace elements such as V, Mo, U, and minor elements such as B and F are presumed to have their original source in volcanic ashes originated from the volcanism in the Andes (5–25% in the loess-type sediments of the Chaco-Pampean plain) [9]. The main components of these sediments are feldspars, quartz, volcanic glass shards, and minor amounts of muscovite and calcite. The composition of volcanic glass is typically rhyolitic, containing a high concentration of F, As, V, and B among other trace elements [28].

3.3. Other Trace Elements

A series of various trace elements, including Ag, Al, B, Ba, Be, Cd, Co, Cr, Cu, Fe, Mn, Mo, Ni, P, Pb, S, Sb, Se, Si, Sr, Ti, V, and Zn were also determined in the studied groundwater. The concentrations of target elements are summarized in Table 3. Among all 23 target analytes, concentrations exceeding the WHO recommended drinking water limits (in parentheses) were found for B (2400 μg L−1), Ba (700 μg L−1), Cd (3 μg L−1), and Sb (20 μg L−1). Table 4 shows the percentage of groundwater samples exceeding these WHO and CAA elemental concentration guidelines. On the other hand, concentrations of Sn, Co, Cu, Ni, S, Se, Sr, V, and Zn were very low. Silver, beryllium, chrome, selenium, lead and titanium are not includ in Tables 2 and 3 because these elements were never found above respective quantification limits.


Sample IDAs(tot)FAlFeMnBBaMoSiVCdSrCoNiZnCuSP(tot)Sb

QL5.000.1010.010.05.0020.010.010.050.010.03.0025.010.010.010.010.00.0250.102.50

M1 5001.90 11060.0 5.001598bql126 bql83.05.0073.0bqlbqlbqlbql11.00.80bql
M2 25.00.50 12040.1bql310156bql 30945.0 bql420bqlbqlbqlbql2.000.30bql
M3 1001.80 90.01603.00875bqlbql bql10.0 bql 691bqlbql30.0bql1072.90bql
M4 15.00.30 100bql bql206bqlbql bql22.0 bql 290bqlbqlbqlbql7.000.30bql
M5 1270.74 220bql9.0081179.142.0 227119 bql 594bqlbql41.0bql0.200.90bql
M658.00.80 110bqlbql29710.0bql bql44.0 bql 498bqlbqlbqlbql7.000.50bql
M724.00.40 100bqlbql27548.212.0 bql43.0 bql 230bqlbqlbqlbql8.000.30bql
M81201.00 100bql6.00265479.0bql209990.03.002012bqlbqlbqlbql11.00.80bql
M91781.98 1305507.00155010.199.0 5491637.00 81.1bqlbqlbql63.07.000.809.00
M105002.60 80.022087015070bql1601657039.04.004871bqlbqlbqlbql7251.90bql
M11 2502.24 100bql6.001387bql14.048023.0 bql641bqlbqlbqlbql1320.50bql
M1211.00.44 100bql19.450062.0bql11453.0 bql334bql10.0bqlbql13.00.60bql
M1395.21.10 110bql5.0050026.942.0bql76.04.00 68.3bqlbqlbqlbql10.00.303.00
M14 1161.50 110bql5.00665bql43.1bql65.05.0054.0bqlbqlbqlbql7.000.70bql
M1531.00.50 10250.05.00244940.230.368057.0 bql521bqlbqlbqlbql49.00.60bql
M1629.00.40 1301505.0025551.8bql49011.0 bql362bqlbqlbqlbql26.00.30bql
M1783.01.20 100bqlbql178240.3bql394094.03.00 1427bqlbqlbqlbql1130.203.00
M1862.00.80 70.0bql18.2734bqlbql255028.0 bql2510bqlbqlbqlbql2810.60bql
M1910.00.20 110bql5.0029814.4bqlbql30.0 bql157bqlbqlbqlbql8.000.50bql
M20 1121.45 100bqlbql231622.010.947501123.001390bqlbqlbqlbdl1470.40bql
M21 7001.90 100bql25.42470bql11.235328.0 bql1361bqlbqlbqlbql4158.90bql
M2210.00.20 100bql29.215616.9bqlbqlbql bql 86.0bqlbqlbqlbql6.001.50bql
M2336.00.30 110bqlbql630109bqlbql30.0 bql225bqlbqlbqlbql5.000.709.00
M2486.00.751738031029621560111bql138012.03.0032.4bqlbql321bql0.100.80bql
M2577.01.20 2980bql5216308bqlbql164722.0 Bqlbql.bql10.0 283132.00.102.504.00
M261003.4060.0110bql180015021.01501983.0015.0bqlbqlbqlbql0.061.80bql
M272144.2060.0855bql6890bql21.31505603.00213280bql67.02800.061.10bql
M281003.4060.0428bql8450bql21.41502193.0015.0 22.0bqlbql22.00.066.70bql
M291000.6060.0660bql6850bql20.81501003.0015.0bqlbql67.0bql0.067.70bql
M302440.9060.081.033.0305018521.01505473.0015.0bqlbql24.0bql0.061.3025.0
M317703.40280101323.07290bql21.015026463.0032.2bqlbqlbqlbql0.300.30bql
M327.000.102102863740508063.220.9150bql3.0016464.0bql 11064.00.202.303.00
M331741.7060.073432.1279069.021.075402663.0015.0bqlbql27.0bqlBql2.20bql
M343170.3036057524.0197011.821.41504363.0015.0bqlbqlbqlbql0.400.60bql
M3510730.3060.0194bql634030.120.5150 12493.0015.0120bql49.01200.060.3030.0
M3619904.2560.0510135580bql21.01502513.0028824.0bql13.0bql0.065.303.00
M372000.3057060613129011321.01503873.0020.324010.016.067.00.600.50bql
M381501.9060.02000bql3710bql21.015038.03.0020.095.0bqlbqlbql0.060.303.00
M3920.00.5060.0300bql483014.021.01501043.0020.0bqlbqlbql67.00.069.9014.0
M4020.00.5060.0689bql21910bql21.01501243.0020.0bqlbqlbql24.00.061.303.00
M41 1501.5060.0988bql21580bql21.01501763.0030.2bqlbqlbqlbql0.061.103.00
M421300.8060.0426bql1970bql21.01503453.00369180bql27.01110.060.203.00
M431501.4060.070.0431103010721.0150bql3.00bql55.0bql22.027.00.060.80bql
M441001.2060.080.0bql260028921.01501913.00bqlbqlbqlbqlbql0.064.80bql
M452001.6060.0262331240140021.015035.03.00bqlbqlbql 11049.00.062.30bql

QL: quantifiction limit; bql: bellow quantification limit; all concentrations are expressed as µg L−1 excepted for F, S, and P expressed as mg L−1.

Element Risk-based drinking water criteria Percentage of groundwater samples exceeding these criteria
WHO*CAA**WHOCAA

As (µg L−1)10***509173
Al (µg L−1)not established200NA16
B (µg L−1)24005007878
Ba (µg L−1)700None2NA
Cd (µg L−1)35132
Cr (µg L−1)50***50 00
Cu (µg L−1)2000100000
Fe total (µg L−1)not established300NA31
F (mg L−1)1.501.003147
Mn (µg L−1)not established100NA16
Ni (µg L−1)702000
Pb (µg L−1)10***5000
Sb (µg L−1)20204.54.5
Se (µg L−1)10***1000
Zn (µg L−1)not established5000NA0

NA: not applicable.
*WHO: World Health Organization, have not established risk-based drinking water criteria for Al, Ag, Be, Bi, Co, Fe, Mn, Mo, Si, Sr, Ti, V, and Zn.
**CAA: Código Alimentario Argentino.
***Provisional guideline value.

From the samples investigated, only one (M45) showed elevated value of barium (1400 μg L−1) than in the WHO drinking water guideline (700 μg L−1) with an average value of 122 μg L−1 (Table 2).

In small quantities, B is essential for healthy bones, joint function, and the metabolism of steroidal hormones. Boron deficiency seems to affect calcium and magnesium metabolism and affects the composition, structure, and strength of bone [31]. The concentrations of boron (B) ranged from 1560 to 21910 μg L−1 with an average of 4020 μg L−1 (Table 2). Boron concentration in the 44% (20/45) of the samples exceeds the WHO and 78% (35/45) of the samples exceeds the CAA standard limits for drinking water (Table 4). The highest concentration of boron was observed in sample M40 which is associated with the largest value of EC (19371 μS cm−1). In general, the presence of boron in groundwater depends on its salinity (represented as EC), such that it increases with increasing salinity [32]. In this study, a positive correlation between EC and boron ( ) suggests that boron might be associated with the salinity of these samples. Hence, the salinity mainly reflects the variation of Cl concentration, with a strong linear correlation ( ) between EC and Cl, suggesting that the increase of Cl concentration contributes to increase in EC value. The hydraulic conductivity, salinity, type of clay sediments, pH and temperature are the crucial factors that determine boron mobility in the groundwater system [32]. Boron was strongly correlated with Na+, K+, Mg2+, Cl, , , and As, probably due to their common origin. The correlation between B and As is often observed in groundwater [1, 13].

Our results indicate that approximately 31% of the groundwater samples tested exceeded the CAA criteria of 300 μg L−1 for total Fe in drinking water. The highest total Fe concentration (2000 μg L−1) appeared in sample M38. In general, Fe concentration was low in the studied groundwater samples; only fourteen samples had higher Fe with a mean value of 276 μg L−1 and median value of 81 μg L−1. On the other hand, weaker correlation is observed between Fe and As in groundwater ( ). Moreover, almost all groundwater with high Fe concentration (>300 μg L−1) contained total As concentration over 10 μg L−1 (Table 3).

The concentration of dissolved Al varied between 60.0 to 17380 μg L−1 with a mean value of 561 μg L−1 (Table 2). A 16% (7/45) exceeded the 200 μg L−1 CAA drinking water guideline. However, the mean concentration of Al decreases significantly down to 178 μg L−1 (median 98.5 μg L−1), if the anomalous of sample M24 is excluded. Also Aluminum shows no correlation with As ( ).

Manganese exceeded the 100 μg L−1 CAA drinking water guideline value in 13% (6/45) of the samples (Tables 3 and 4). The highest Mn concentration (3740 μg L−1) was found in sample M32. However, the mean concentration of Mn decreases significantly from 152 to 70.0 μg L−1 (median 5.00 μg L−1), if the anomalous value of this sample is excluded. Manganese shows no correlation with As ( ). Mn is known as an essential element for human survival, serves as a catalyst and cofactor in many enzymatic processes involved in the synthesis of fatty acids and cholesterol. The chronic ingestion of Mn in drinking water is associated with neurologic damage [33]. Moreover, manganese is a known mutagen [34].

Many samples have Fe, Al, and Mn concentrations below detection limits and most have below CAA guideline value. However, concentrations are higher in a few samples (Table 2). Smedley et al. [1] suggest that at the pH of the groundwater, the high concentrations for these elements trace are most likely due to presence of colloidal particles. As the groundwater are oxidizing, solubility of Fe, Al, and Mn oxides is low and concentrations of dissolved Fe, Al, and Mn are, therefore, mostly low.

The processes of dissolution and release from oxides and oxyhydroxides, mainly Al, Mn, and Fe, control the presence and mobility of As and F in groundwater [1]. Kim et al. [35] suggested that the cocontamination of As and F observed in oxidizing aquifers in many countries is associated with the desorption from the Fe-(hydr) oxides by the pH increases. The correlations between As and F are generally very high in those aquifers because the As released from Fe-(hydr) oxides does not readily precipitate again in the oxidizing alkaline condition. This is consistent with our observations, as many of the samples show high pH values and moderate coefficient correlation value between As and F ( ). Also, solubility of Al minerals may be enhanced by the complex of dissolved Al with F that is also released from volcanic glasses.

Vanadium in groundwater ranged between <10.0 (QL) and 2646 μg L−1. The highest V concentration was found in sample M31 (Table 2). Vanadium shows a moderated positive correlation with As ( ) and is likely to be derived from similar mineral sources (secondary Fe and Mn oxides) under the high pH conditions [1]. Our results also indicate that Mo in general appears in low concentrations (Table 3). Molybdenum is weakly correlated with As ( ).

Gomez et al. [27] suggest that V, U, B, and Mo are enriched in volcanic materials and are mobilized as vanadate, molybdate, borate, and so forth, under oxidizing conditions. Alternatively, they are mobilized in alkaline solutions under conditions of high pH and high , controlled by carbonate reactions, (e.g., the F may be forming anionic complexes with B, Fe, and Al).

Antimony (Sb) is ubiquity a Group V of the periodic table and is similar to As in aspects as chemical behavior and toxicity to animals [5]. The Sb concentrations in studied samples exceeded 20 μg L−1, WHO and CAA drinking water guideline values in 4.5% (2/45) of the analyzed samples (Tables 3 and 4).

Cadmium reaches a maximum of 7.0 μg L−1 with most samples being less than 3.0 μg L−1. As this element forms cationic species in solution, its mobilization is not favored under the alkaline conditions of the groundwater [1].

The presence of arsenic and heavy metals in the samples collected from this region of Chaco in Argentina may be due to local geochemical conditions that facilitate the transfer of naturally occurring arsenic from soil and sediment to the water. The people in the Comandante Fernández Department may be overexposed not only to As, but also to B, Cd, Mn, and F. Adverse health effects may appear in coming years. This problem is a serious concern for the local population.

4. Conclusions

The results of the current study indicate that approximately 91% of the groundwater samples used for consumption by human and livestock, from the Comandante Fernández Department (Chaco province, Argentina), exceed the WHO provisional guideline value of 10 μg L−1 As, recommended as a maximum allowable level in potable water.

Evaporation, potentiated in arid, and semiarid zone, favors the increase of salinity and alkalinity, the results is a low quality of the resource but is not conditioning the concentration of As and F. Hence, factors other than evaporation, such as desorption from metal oxides and possibly silicate reaction, could be likely controlling As and F mobilization. Furthermore arsenic, associated trace elements may be absorbed on the surface of iron and aluminum oxides and oxyhydroxides (hematite, goethite, Fe(OH)3, and gibbsite), limiting the mobility of trace elements. Groundwater with high pH values and high concentration of bicarbonate would facilitate the dissolution of volcanic glass; thus, trace elements may enter groundwater cycles, forming anionic complexes in alkaline solutions and acquiring great mobility.

The hydrochemical trace in the region is characterized by high salinity and high As and F concentrations, which is related to volcanism and hydrothermal activity from the Andes. This association is often linked to presence of B, Cd, Mo, Mn, and V, indicating their common origin in the volcanic glasses.

Due to high As concentrations found in groundwater, serious health risk must be considered. The population in the area may be exposed to the chronic toxicological effects of hydro arsenicism and fluorosis, increasing the risks of contracting other diseases derived from them. Since the groundwater studied here constitutes the principal source of drinking water in the zone, mitigation efforts should not be limited to As health risks from other toxic elements present in drinking water must also be addressed in this region.

Conflict of Interest

The authors declare that there is no conflict of interests regarding the publication of this paper. Its publication is approved by all authors and tacitly or explicitly by the responsible authorities where the work was carried out, and that, if accepted, it will not be published elsewhere in the same form, in English or in any other language, including electronically without the written consent of the copyright-holder.

Acknowledgments

This work was supported with funds from PI 36/00005 Universidad Nacional del Chaco Austral (UNCAus). Patricia S. Blanes thanks the National Academy of Exact, Physic and Natural Sciences for granting a Ph.D. fellowship.

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