Introduction

Water is an important natural resource, which forms the core of ecological system (Selvam et al. 2013). The demand of groundwater increases with some factors like increasing population and pollution of surface water bodies by agriculture and industrialization. The study area, Rangpur, lies in north western part of Bangladesh. The area lacks industries and is dominated by agricultural activities. The water is mainly used here for drinking, domestic, irrigation and industrial purposes. Hydrochemical study is a useful tool to identify the suitability of groundwater. Both the physical and chemical parameters are taken into considerations. The chemical parameters taken into consideration are hydrogen ion concentration (pH), specific electrical conductance (EC), total dissolved solids (TDS) and all major cations and anions. Several researchers had carried out extensive studies on water quality of the Tista floodplain. Islam et al. (2017) studied the trace element contents of Rangpur district and concluded that the trace element quality of groundwater is mainly related to natural/geogenic sources followed by anthropogenic sources. Salinity with increasing depth has been reported in lower Tista floodplain which is an indicative of mixing of fresh and saline bodies due to marine transgression during Holocene period in the Bengal delta (Afroza et al. 2009). The present research work shows that the quality of the groundwater is mainly controlled by geogenic processes to a lesser extent by anthropogenic activities.

Groundwater is the principal source of water supply for irrigation, drinking and domestic purpose. Higher concentrations of chemical constituents negatively affect the environment and public health (Anderson 2014). Examples of groundwater pollution sources include salt water intrusion, leakage of fertilizer, natural erosions and other anthropogenic activities. The present study is conducted to assess the groundwater quality for understanding its suitability for various purposes. The study will also reveal the sources of chemical constituents of groundwater.

The main objective of this research work is to assess the groundwater quality for drinking, domestic and irrigation purposes and to characterize the hydrogeochemical processes which are dominant in the study area.

Study area

The Tista River originated from the Pauhunri (Teesta Kangse) glacier above 7068 m and flows southwards through gorges and rapids in the Sikkim Himalaya (Meetei et al. 2007; Wiejaczka et al. 2014). Overall drainage pattern of the Tista River is anastomosing and braided type (Bhattacharyya and Mukherjee 2009). The presence of numerous abandoned channels with various degrees of aggradations indicates large-scale migrations of the rivers. The Tista is a Trans-Himalayan River that flows through the granites and volcanic rocks of Neogene and Paleogene age (i.e., about 2.6 to 65 million years old). The aquifers of the Tista fan, both active fan and inactive, that lie in Rangpur and Dinajpur districts are composed of coarser sediments and have the highest transmissivity in Bangladesh varying from 1000 to 7000 m2/day (UNDP 1982; Hussain and Abdullah 2001). The aquifers mainly composed the piedmont deposits of old Tista floodplain containing fine, medium and coarse sands with a higher proportion of silt and clay with mean thickness of 2 m. In some places, clay lenses are found in the sands. The thickness of the aquifer varies from 5 to 50 m with average thickness of 20 m (Hussain and Abdullah 2001). The aquifer of the study area is mainly extensive unconfined and locally semi-confined in Kurigram district. The temperature of Rangpur varies from 32 to 11 °C, and the annual average rainfall is 2931 mm (Fig. 1).

Fig. 1
figure 1

Map of the study area

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Methodology

Nineteen groundwater samples were collected from tubewell of shallow aquifers in July 2014 in order to study physicochemical characters of the study water. The pH and electrical conductance (EC) of groundwater samples were measured in the field using pH meter (HANNA) and EC meter (HANNA), respectively. The temperature of the groundwater was measured and recorded in situ. Sampling was carried out using pre-cleaned polythene bottles, after pumping continuously 10–15 min until the temperature, electrical conductivity (EC) and pH reading had stabilized. To analyze the water chemistry, 100 mL polythene two sample bottles were filled at each tubewell. The sampled water was filtered through 0.45 µm filters at the time of sampling in order to remove colloidal and suspended materials. Ten drops of ultrapure nitric acid (HNO3) was added in one of the bottles to preserve the groundwater for the analysis of cations. Collected samples were preserved at 4 °C and taken into the laboratory for chemical analyses. Ca and Mg were determined by Atomic Absorption Spectrometer, model Shimadzu AA 7000 at 422.7 and 285.2 nm wavelength. A flame photometer was used to determine the concentration of Na and K at 589 and 765.5 nm (Afroza et al. 2009). Chloride (Cl−) was determined by argentometric method using standard AgNO3 solution as titrate and potassium chromate as indicator (APHA 1995). Carbonate (CO32−) and bicarbonate (HCO3−) were determined with titration with HCl. SO4 was determined by UV–visible spectrophotometer, model Shimadzu UV-1800 at a wavelength of 535 nm. Based on the results of the physicochemical analyses, irrigation quality parameters like total hardness (TH), sodium absorption ratio (SAR), residual sodium carbonate (RSC), permeability index (PI), soluble sodium percentage (SSP) and magnesium hazard were calculated.

Total hardness (TH) of the water samples was calculated by using the formula as given by Raghunath (1987) and Sawyer et al. (2003):

$${\text{TH in mg/L}} = \left( {{\text{Ca}}^{ + } + {\text{Mg}}^{ + } } \right) \times 50$$

where all the concentrations are in meq/L.

Residual sodium carbonate (RSC) of the water was estimated by the formula (Eaton 1950; Raghunath 1987):

$${\text{RSC = }}\left( {{\text{CO}}_{3}^{{{\mathbf{2}} - }} + {\text{HCO}}_{3}^{ - } } \right) - \left( {{\text{Ca}}^{ + } + {\text{Mg}}^{ + } } \right)$$

where all the concentrations are in meq/L.

Permeability index (PI) was computed using equation developed Doneen (1964) and Raghunath (1987):

$${\text{PI = }}\frac{{{\text{Na}} + \sqrt {{\text{HCO}}_{ 3} } }}{{{\text{Ca}} + {\text{Mg}} + {\text{Na}}}} \times 100$$

where all the concentrations are in meq/L.

The sodium adsorption ratio was estimated by using the formula formulated by Richards (1954):

$${\text{SAR}} = \frac{\text{Na}}{{\sqrt {{\text{Ca}} + {\text{Mg}}} /2}}$$

where all the concentrations are in meq/L.

Soluble sodium percentage (SSP) of water was computed using the equation given by Todd (1980):

$${\text{SSP}} = \frac{{\left( {{\text{Na}} + {\text{K}}} \right) \times 100}}{{\left( {{\text{Ca}} + {\text{Na}} + {\text{Mg}} + {\text{K}}} \right)}}$$

where all the concentrations are expressed in meq/L.

Magnesium hazard (MH) was calculated by following the equation developed by Szabolcs and Darab (1964) for irrigation use of water:

$${\text{MH = }}\frac{{{\text{Mg}} \times 100}}{{{\text{Mg}} + {\text{Ca}}}}$$

where all the concentrations are expressed in meq/L.

Results and discussion

On-site field measurements

pH The pH values of the studied samples are shown in Table 1, where minimum is 6.20, maximum is 7.40, which is almost permissible ranging 6.5–8.5 of WHO (1997) and median value is 6.50. The pH values of the groundwater varying from 6.20 to 7.40 are an indicative that the groundwater aquifer conditions vary from slightly acidic to slightly alkaline. Low pH (pH > 7) groundwaters are resulted from the absence of calcite or nearly so, and the main host rock is granitic origin (Robins 2002). The pH of natural water is an important factor which is influenced by the chemical and biological parameters of the water as well as toxicity of many compounds (Haque 2009).

Table 1 Results of physicochemical analysis of the groundwater samples of the study area
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Temperature The temperature of the investigated groundwater was uniform, which varied with a range from 25 to 28 °C and the median value is 26 °C as shown in Table 1.

EC The EC values of groundwater samples range from 110 to 1190 μS/cm. Based on the EC, the groundwater of the study area is fresh in nature (< 1000 μS/cm) and only one sample is slightly saline (> 1000 μS/cm).

Hydrogeochemistry

Major cations and anions

The mean abundance of major cations is Na+ > Ca+2 > Mg+2 > K+, whereas the major anions is HCO3− > Cl− > SO−24. Among the cations, Na+ is the dominant and K+ is the lowest constituents, whereas HCO3− is most abundant and SO−24 is the minor constituents in anions.

Sodium (Na+) Sodium (Na+) is the most abundant member of the alkali metal group of studied groundwater. Sodium concentration of groundwater of the Tista River Basin varies from 11.5 to 80.5 mg/L. The maximum concentration of sodium is 80.5 mg/L, reported in Kaunia Upazila of Rangpur and Sundarganj of Gaibandha. None of the samples exceeds the maximum permissible limits of sodium of recommended standards of WHO (1997) and EQS (1989).

Tista floodplain sediments contain feldspar at different locations (Mazumder et al. 1994). The results suggest that sodium in groundwater was derived from the weathering of halite and silicate minerals like feldspar in this area (Khan et al. 2014; Mostafa et al. 2017). The agricultural by-products might be the other sources of sodium content of the groundwater in the study area (Hem 1989; Sultana 2009).

Potassium (K+) Potassium (K+) is the second abundant alkali metal reported in the groundwater samples of the investigated area. The concentrations of potassium (K+) are lower than that of sodium because of slower weathering rate of potassium bearing rocks than those of sodium bearing rocks. Potassium is resulted from the chemical decomposition of the sylvite (KCl) and silicates especially clay minerals. Potassium can be added to groundwater through fertilizer use and breakdown of animal or waste products.

The average concentration of potassium (K+) in the study is 6.51 mg/L, whereas maximum content of K+ is 23.4 mg/L at Tista, Lalmonirhat and minimum concentration is 0.78 mg/L at Stadium Para, Lalmonirhat. Three groundwater samples exceed the maximum permissible limit of potassium of recommended standards of WHO (1997 )and EQS (1989).

Calcium (Ca2+) The maximum concentration of calcium (Ca2+) is 36 mg/L, minimum calcium content is 4 mg/L, and the median value for concentration of calcium is 8 mg/L. Calcium is the most abundant alkaline earth in the groundwater of the aquifer of the Tista River Basin. All of the groundwater samples were within the permissible limit for WHO (1997) and EQS (1989).

The normal concentration of calcium in groundwater ranges from 10 to 100 mg/L (Nag 2009). The basic sources of calcium are carbonate rocks, i.e., limestones and dolomites, which are dissolved by carbonic acid in groundwater. The chemical breakdown of calcic-plagioclase feldspars and pyroxenes may be responsible for calcium in the groundwater (Ganyaglo et al. 2010). Calcium can also originate as lime in agricultural fertilizers.

Magnesium (Mg2+) Magnesium in groundwater derived from the decomposition of dolomite, ferromagnesian minerals like olivine, pyroxene, amphiboles and dark colored micas. In the metamorphic rocks, magnesium occurs in the structure of chlorite, montmorillonite and serpentine (Nag 2009). The reaction involving solution of magnesium is influenced by the amount of CO2 in the groundwater in dissolved condition.

The maximum amount of magnesium is found in the groundwater of Tista, Lalmonirhat 17.01 mg/L, and the minimum concentration is reported in the groundwater of three wells of Rangpur whose values are 2.43 mg/L. The median value of magnesium is 7.29 mg/L. The magnesium content of the all groundwater sample is below the maximum permissible limit of WHO 1997 and EQS 1989.

Chloride (Cl−) The chloride (Cl−) concentration of groundwater may be attributed to the presence of chlorides from rocks, evaporates, seawater intrusion, connate and juvenile water, or contamination by industrial waste or domestic sewage. Normally, the concentration of chloride in groundwater is less than 30 mg/L, but concentration of 1000 mg/L or more is common in arid regions (Nag 2009).

The mean concentration of chloride in the groundwater of present study is 78.64 mg/L. The chloride contents of groundwater of the aquifer of the Tista floodplain range from 3.40 to 207.60 mg/L. The low value of chloride ions is an indication of low salinity of the groundwater of the study area. The chloride content of the all groundwater sample is below the maximum permissible limit of WHO (1997) and EQS (1989). The high concentration of chloride is found in the wells of Nilphamari, Lalmonirhat and Rangpur districts that could be resulted from the mixing of fresh water with seawater. Positive correlation of chloride with sodium and potassium indicates that the principal source of chloride is from halite and sylvite (Figs. 2 and 3).

Fig. 2
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Correlation of Na versus Cl

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Fig. 3
figure 3

Correlation of K versus Cl

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Sulfate (SO2−4) The occurrence of sulfate in groundwater resulted from the oxidation of sulfur of the igneous rocks, the dissolution of the other sulfur bearing minerals. Sedimentary rocks, such as organic shale, may play a key role in this connection by the oxidation of marcasite and pyrite (Matthess 1982; Rahman et al. 2013a, b). The sulfate (SO42−) of the groundwater from the aquifers of the active Tista floodplain varies from 0.22 to 28.22 mg/L. The sulfate content of the all groundwater sample is below the maximum permissible limit of WHO (1997) and EQS (1989). The median value of sulfate (SO42−) content of the groundwater of the study area is 4.38 mg/L. The low concentrations of sulfate suggest that bacterial sulfate reduction has occurred (Kirk et al. 2004). The lower sulfate content of groundwater indicates that the study area lacks industries as the high sulfate contents indicate anthropogenic sources and industrial process (Mostafa et al. 2017).

Bicarbonate (HCO−3) The possible sources of bicarbonate include the presence of organic matter in the aquifer that is oxidized to produce carbon dioxide, which promotes dissolution of minerals (Khashogji and El Maghraby 2013). The fossil carbon of the calcite and dolomite in the aquifer would contribute half of the bicarbonate ions. This weathering enriches the groundwater in calcium, magnesium and bicarbonate ions. Bicarbonate ions may be resulted from the weathering of silicate minerals (Gastmans et al. 2010).

The concentrations of bicarbonate in the groundwater samples range from 39.6 to 183 mg/L. The concentration of bicarbonate ions is higher in the northern and central portions of the study area, while the bicarbonate content of groundwater decreases with increase in longitude.

Assessment of water quality for drinking

To evaluate the quality for drinking water and public health quality, the physical and chemical parameters of the groundwater were compared with the prescribed pattern recommended by the World Health Organization (WHO 1997) and Environmental Quality Standard for Bangladesh Table 2. From this correlation Table 2, it can be summarized that pH, TDS, Na+, Ca2+, Mg2+, Cl−, SO42−, HCO3− and CO32− values of water from the study area belong to standard limit which can be used for drinking purpose and public health without any risk. Three of the groundwater samples show high K+ concentrations. As much as 16% of the groundwater samples exceed the maximum allowable limit of the allowable limit for drinking purpose and public health (WHO 1997; EQS 1989).

Table 2 Correlation between the groundwater samples of the study area with the standard limits prescribed by WHO (1997) and EQS (1989) for drinking water purposes
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Correlation coefficient matrix (r) The coefficient correlation matrix (r) is one of the important tests that shows the connections between two independent parameters of the water. The most familiar measure of dependence between two parameters of water is the Pearson product moment correlation coefficient matrix. It is a measure to demonstrate how well one variable predicts the other (Bahar and Reza 2010; Howlader et al. 2014). The correlation coefficient, r, ranges from − 1 to + 1. When the value of r is close to − 1, the relationship is demarcated as anti-correlated or has a negative slope. The association is considered to be correlated or have a positive slope, while the value of r is close to + 1. If the value of r tends to be zero, the points are considered to become less correlated and eventually are uncorrelated (Srivastava and Ramanathan 2008; Howlader et al. 2014).

The correlation matrices for physicochemical parameters of the groundwater of the Tista floodplain aquifer are calculated and shown in Table 3. From Table 3, it can be concluded that pH shows positive correlation only with Ca2+, whereas with other parameters like Na+, K+, Ca2+, Mg2+, FeTotal, Cl−, HCO3−, SO42− it show negative correlation with pH. Here, the EC reflects the positive correlation with Na+, K+, Mg2+, FeTotal, Cl−, HCO3−, SO42−. Moreover, Na–K, Na–Ca, Na–Mg show the remarkable positive correlation pairs in the analysis. The Cl−, HCO3− and SO42− show positive correlations with the cations like Na+, K+, Ca2+, Mg2+, FeTotal.

Table 3 Correlation coefficient matrix of groundwater quality parameters (n = 19)
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Hydrochemical facies in water of the Tista river active floodplain

Piper trilinear diagram analysis The Piper trilinear diagram is one of the important tools that is used to interpret the hydrogeochemical facies (Piper 1944). The diagram shows the similarities and differences among water samples as those with similar qualities will have a tendency to fall in the same group (Todd 1980; Ramesh et al. 2014). Major cations (Ca2+, Mg2+, Na+ and K+) and anions (HCO3−, CO32−,Cl− and SO42−) are plotted in the two basal triangles of the diagram, where all of the major cations and anions are expressed as percent of meq/L. The central portion of the diagram which is diamond shaped describes the classification of water. Among the major cations, Na+ and K+ are treated as alkalis and Ca2+ and Mg2+ are considered as alkaline earth. HCO3− and CO32− anions are designated as weak acid, while Cl− and SO42− ions are defined as strong acids. The hydrochemical facies of groundwater show that sodium, sodium–magnesium, sodium–calcium, sodium–magnesium–calcium and sodium–calcium–magnesium are cation facies and chloride–bicarbonate, bicarbonate–chloride and bicarbonate are anion facies (Fig. 4).

Fig. 4
figure 4

Piper trilinear diagram of groundwater of the study area

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Potassium feldspar is resistant to chemical weathering, whereas sodic-feldspars and calcic-feldspars are susceptible to chemical changes. These minerals yield the metal cation and silica solution and commonly form clay minerals with aluminum and part of the original silica (Hem 1989). Sodium may be presented as unaltered mineral grains in sediments that are resistant to weathering, as an impurity in cementing material, or as crystals of readily soluble sodium salts deposited within the sediments left in the sediments by saline seawater. Sodium ions are the most important cation in stream and spring water (Feth et al. 1964). High sodium concentration in water may be resulted from the mixing of freshwater with saline water bodies due to marine transgression during Holocene epoch in the Bengal Basin (Afroza et al. 2009).

Sources major ions in groundwater The Tista fan has developed by the sediments carried by the rivers, originating from the Himalayas, and draining through the Siwalik group of sediments (Rahman et al. 2013a, b). The chemistry of these sediments might have influence on the groundwater quality of the investigated area. Groundwater chemistry in the study area is regulated by different processes and mechanisms. The subtropical climatic conditions, rock-water interactions, precipitation and evaporation might have the significant role in groundwater chemistry. The Gibbs mechanisms (Gibbs 1970) were employed in the study, suggesting that groundwater chemistry in the investigated area has been influenced by the chemical weathering of rock-forming minerals existing in igneous rock, and ion exchange processes are the dominant solute acquisition mechanisms controlling the concentration of chemical constituents in groundwater and the anthropogenic sources also influence the groundwater composition (Apodaca et al. 2002; Martinez and Bocanegra 2002; Singh and Hasnain 2002; Jeelani and Shah 2006; Bhardwaj et al. 2010; Li et al. 2010; Jeelani et al. 2014).

From the observations, it is worthy to note that most of the major ions were high at shallow depth of the groundwater. The sources of the major ions in shallow groundwater may be resulted from the lithogenic and anthropogenic activities, mainly from agricultural activities. The lower concentration of major ions in greater depth of groundwater indicates that the sources of major ions are lithogenic in deeper aquifers and are naturally preserved from contamination by anthropogenic activities. The relative proportion of various dissolved ions in the groundwater depends on their abundance in the host rock/aquifer and their solubility (Sarin et al. 1989). The present research work has been carried out in the active portion of the floodplain deposits of the Tista River of Holocene age. The ion exchange between the groundwater and its host environment during the residence or during in movement process can be best illustrated by chlorine alkaline indices which are also known as Schoeller index (Schoeller 1977). It is expressed as: CAI = Cl−–(Na++K+)/Cl−. A majority of the water samples from the groundwater (58%) showed positive CAI indicating exchange of Na and K from the groundwater with Mg and Ca of the rocks, whereas 42% of the samples showed negative CAI indicating exchange of Mg and Ca of the water with Na and K of the rocks (Nagaraju et al. 2006). The Cl−/HCO3− values range from 0.068 to 3.911. Values of this hydrogeochemical index given for inland waters are between 0.1 and 5 (Nwankwoala and Udom 2011). The calculated values of the ratio of Mg2+/(Ca2++Mg2+) of 84% of the groundwater samples are less than 0.5 indicating dolomite dissolution where the value of 16% of the groundwater samples is more than 0.5 indicating limestone–dolomite weathering.

Evaluation of water quality for irrigation Most natural waters are between pH 5 and 8. The generally accepted pH for irrigation water is in between 5.5 and 7.5.

Total hardness (TH) The total hardness (TH) is an important parameter of water for the utility of water in various purposes, for example domestic, industrial or agricultural purposes. The total hardness of water results from the excess concentration of Ca, Mg and Fe salts in water. The average value of total hardness is 62.63 mg/L which reveals that 23% water samples (Table 4) are soft in nature (Sawyer and McCarty 1967). The total hardness value of the water samples of the investigated area ranges from 20 to 160 mg/L which is less than the WHO recommended values (500 mg/L) for drinking water purposes (Islam et al. 2016).

Sodium adsorption ratio (SAR) The US Salinity Laboratory showed that the sodium adsorption ratio (SAR) reasonably estimates the degree to which irrigation water tends to enter into cation-exchange reaction in soil. High magnitudes of SAR imply a hazard of sodium replacing absorbed calcium and magnesium, and lead to a condition that ultimately damages the soil structure (Khan and Abbasi 2013).

The median value of SAR is 2.12 which denotes that the studied water samples are excellent in quality for irrigation. The SAR value of the water samples of the investigated area ranges from 0.79 to 5.53 as shown in Table 4. The SAR value of all this samples indicates the excellent quality for irrigation water.

Table 4 Showing the values of irrigation parameters of groundwater of the study area
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Residual sodium carbonate (RSC) The concentration of bicarbonate and carbonate controls the suitability of water for irrigation (Reddy 2013). One of the empirical approaches was made based on the assumption of the precipitation of calcium and magnesium carbonates considering the hypothesis Eaton, 1950 proposed by the concept of residual sodium carbonate (RSC) for the measurement of high carbonate waters. Residual sodium carbonate (RSC) determines the hazardous effects of carbonate and bicarbonate on the quality of water for agricultural purpose.

The average value of residual sodium carbonate is 0.31 meq/L. According to US Salinity Laboratory 1954, the magnitude of all the water samples was less than 1.25 meq/L, which is an indicative of safe water quality for irrigation.

Permeability index (PI) The permeability of soil is influenced by the continuous use of irrigation water. By the amounts of sodium, calcium, magnesium and bicarbonate ions, the soil is increased by the utility of irrigation water (Chandu et al. 1995). The permeability index (PI) is a measure suitability of water for irrigation purpose. The permeability index (PI) is categorized as class I (> 75%), class II (25–75%) and class III (< 25%). The waters under class I and class II are designated as good for irrigation that have PI 25% and above, while class III waters have PI values less than 25% and unsuitable for irrigation (Doneen 1964; WHO 1989). The permeability index of the groundwater of the investigated wells is 72% and above, whereas they fall in class I and class II, which are suitable for irrigation purposes.

Soluble sodium percent (SSP) The soluble sodium percent is a measure of the tendency for a water to enter into cation-exchange reactions (Khan and Abbasi 2013). It is the percent of total cations made up by Na ions. The divalent cations normally occupy the exchangeable positions on clay minerals, the extensive displacement of calcium and magnesium ions by Na ions unless the SSP is considerably higher than 50% of the total concentration of the solutes is large (Hem 1989). Soluble sodium percent (SSP) is an important factor for the classification of irrigation water. A certain ratio of air water in the pore spaces of the soil is essential for the proper nutrition and growth of the plants. The water-containing sodium reacts with the soil, accumulates in the void spaces the soil and reduces the permeability of the soil. The sodium concentration is expressed in terms of soluble sodium percent. The maximum permissible limit of SSP is 60% for irrigation water. Sixty-eight percent of the studied water samples have the SSP value less than 60%.

Magnesium hazard (MH) Magnesium and calcium ions are essential for plant growth although these ions may be added with the soil aggregation and cause friability of soil. High concentration of calcium and magnesium of irrigation water can increase the pH of soil that may cause loss of phosphorus. Magnesium ions are also important for the productivity of soil. The water is safe and suitable for irrigation if the numerical value of magnesium hazard (MH) is less than 50% (Szabolcs and Darab 1964). The value of 58% of the water samples of the study area less than 50% is safe and suitable for irrigation purposes.

Assessment of water quality for livestock

Water is essential for all forms of life. The availability of adequate quantity and quality of water has the largest impact of types of life and number of individuals that an environment can sustain and may be a limiting factor for livestock production systems. Water is an essential second only to oxygen in importance to sustain life and optimum growth, lactation and reproduction of dairy cattle (Breede 2006). Water is a medium for transportation of nutrients, waste products, hormones and other electrolytes, and aids in the movement of food through the gastrointestinal tract (Lardner et al. 2005). For the livestock, high-quality water should be provided in order to prevent them from different diseases, salt imbalance and poisoning from toxic components (Bhardwaj and Singh 2011). Most of the water quality variables for livestock are same as for human drinking water, although the total permissible levels of total suspended solids and salinity may be higher (Bhardwaj and Singh 2011). The total dissolved solids (TDS) are the main parameter usually used to assess the suitability of any water for livestock farming. Based on the Australian and UNESCO standards, the TDS value between 0 and 2900 mg/L is suitable for all the animals (Hamill and Bell 1986; Jeelani et al. 2014). In this case, the groundwater is good for livestock purposes as the TDS in groundwater ranged from 73.7 to 797.3 mg/L (Table 5).

Table 5 Upper limit of TDS for livestock consumption
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Conclusion

The study reveals that the environment sensitive index parameters like pH, EC and the temperature values of the groundwater samples in the study area are within the permissible limit. The mean concentration of major cations in the groundwater samples is Na+ > Ca+2 > Mg+2 > K+, whereas the major anions is HCO3− > Cl− > SO−24. Among the cations, Na+ is the dominant and K+ is the lowest constituents, whereas HCO3− is most abundant and SO−24 is the minor constituents in anions. Concentrations of calcium, magnesium and sodium of all the samples are within the permissible limit. Correlating with WHO (1997) and EQS (1989) guideline values for drinking water and public health, it may be concluded that the groundwater of the study area is suitable for all drinking and domestic purposes, where only three samples exceed the maximum allowable limit of potassium. The allowable concentrations of all chemical parameters suggest that the quality of the groundwater is mainly controlled by geogenic processes. The excess concentration of potassium in three groundwater samples might be resulted from anthropogenic activities like use of fertilizer. Based on total hardness, SAR, RSC, PI, SSP and MH values, it can be summarized that the groundwater of the investigated area has excellent quality for irrigation purpose. On the basis of Australian and UNESCO standard, the groundwater of the study area is also suitable for livestock purposes. Further research works can be taken to show the seasonal variation of the geochemical parameters of the groundwater in the investigated area.