Wadi Al Arab is located at the northwestern part of Irbid Governorate, about 81 km from the capital city of Amman-Jordan (Figure 1), it is situated at the transition between the mountainous highland in the southeast, the high plateaus and hilly areas in the central part, the rift escarpment, and the Jordan Valley along the western part.

Wadi Al Arab well field was commenced in 1982 with five wells. Currently the well field is composed of 18 operational wells used for the water supply in Irbid. Initially the early drilled five wells were artesian flowing wells and the discharge was ranging between 640 m³/h and more than 1500 m³/h [13] [14]. The annual abstraction from these wells was 26 Million Cubic Meters (MCM). This high abstraction amount caused the water level to decline significantly and consequently leading all wells to become non-artesian flowing wells. Due to this; the abstraction rate from these wells reduced to approximately 16 - 18 MCM/Year [15]. Since 1982, the measured decline in the water level is 118.64 m/35year. The average annual decline rate of groundwater level is estimated as 3.39 m/year [16].

The change in groundwater level leads to a dynamic groundwater system characterized by changing aquifer conditions, accompanied by changes in water quality [17] [18] [19]. As a result, the quality of produced water in the study area shows increased concentrations of heavy metals, in particular Molybdenum, Nickel, and Arsenic, which is in many wells proves a rising trend of contamination.

The geological succession in the study area is hydrogeologicaly subdivided into lithostratigraphic units, which form systems of aquifers and aquitards. The aquifer systems in the study area include two major (Kurnub, and Amman Wadi As Sir Aquifer System), and three minor (Na‘ur (A l-2); Hummer (A4); and Rijam (A4)) [20] [21].

Amman-Wadi As Sir Aquifer (Silicified Limestone and Phosphatic Limestone) (A7/B2) is the main aquifer in the study area. The Muwaqqar Formation (B3) conformably overlies the Amman Formation (B2) in the study area. The B3 is a regional aquitard, which confines the underlying A7/B2 Aquifer system [22] [23] [24].

The water quality field and analytical parameters of the major ions composition of Wadi Al Arab groundwater samples for 1986 and 2017 are shown in Table 1 and Table 2.

Most of the water samples anions are dominated by HCO 3 − with relative abundance of HCO 3 − > SO 4 2 − > Cl⁻ > NO₃, whereas; the main cation is Ca²⁺, with relative abundance of Ca²⁺ > Mg²⁺ > Na⁺ > K⁺. The trace element content of As, Mo, and Ni exhibits increase concentration in the groundwater of Wadi Al Arab, which is beyond the concentration threshold of the Jordan Institution for Standards and Metrology (JISM), and the World Health Organization (WHO) guidelines.

Scatter plots of the cations (Na⁺, K⁺, Ca²⁺, and Mg²⁺) and anions ( HCO 3 − ,Cl⁻

and SO 4 2 − , NO 3 − ) were shown in Piper’s diagram [25],classifying the hydrochemical characteristics. One main water type has been identified; all water samples were concentrated on the field of Ca-HCO₃, The reason is groundwater passing through carbonate rock, for cation concentration Calcium type and for anion concentration; HCO₃-Type of water Predominated (Figure 2). Total hardness of the sample is classified as very hard water, which exceeds 300 mg/L.

The Schöeller diagram (Figure 3) further demonstrates the uniformity and similarity of composition among the groundwater samples by the cluster of the lines of concentration from cations to anions.

The relationship between dependent and independent variables is known as Correlation Matrix, and is statistically measured. It assists in predicting the mutual relationship between two variables. The correlation between the parameters differentiates between strong (the range is +0.8 to 1.0 and −0.8 to −1.0), and weak (the range is +0.0 to 0.5 and −0.0 to −0.5). The correlation values obtained in the present study in Wadi Al Arab are presented respectively in (Table 3 and Table 4). As per the findings of the correlation matrix, it can be inferred that the correlation matrix between parameters is changed during the period between 2017 and 1986, which marks the change of the geochemical processes.

Groundwater composition is controlled by three main hydrogeochemical processes; including water rock interaction, evaporation and precipitation. Gibbs diagram [26] is used to give an indication of the main process affecting the water quality. The distribution of the sampling points in the Gibbs diagram showed that the majority of samples are plotted within the field of rock weathering (Figure 4), which indicates that the main factor controlling dissolved hydrochemical components of the water samples is the dissolution of the rock-forming minerals.

Hydrogeochemical data for groundwater in the study area suggested the occurrence of Ca 2+ -HCO 3 − water type as a result of the dissolution of the carbonate minerals, as shown in the following Equation (1) and Equation (2).

CaCO 3 ( calcite ) + H 2 CO 3 → Ca 2 + + 2 HCO 3 − (1)

CaMg ( CO 3 ) 2 ( dolomite ) + 2 H 2 CO 3 → Ca 2 + + Mg 2 + + 4 HCO 3 − (2)

To further know the functional relationship of the dissolved ions and their contribution to the groundwater the data are plotted in the scatter diagram in Figure 5; Based on the Equations (1) and (2) above the dissolution of calcite and dolomite would produce the Ca 2+ / HCO 3 − and ( Ca 2+ + Mg 2 + ) / HCO 3 − with a molar ratio of (0.5). In this study; the Ca 2+ / HCO 3 − ratios of most samples are above (1) as a result of the dissolution of calcite, while ( Ca 2+ + Mg 2 + ) / HCO 3 − ratios are below (1).

Additionally when the Ca²⁺/Mg²⁺ molar ratio below (1) the groundwater is undersaturated with respect to Mg²⁺ which triggers the dissolution of dolomite, most of the plotted samples had the Ca²⁺/Mg²⁺ molar ratios largely less than (1) which indicate the dissolution of the aquifer matrix dolomites. Moreover, if the Ca²⁺/Mg²⁺ molar ratio greater than (2) can be the result of the dissolution of silicate minerals (silicified limestone and chert).

The relation of Na⁺/Cl⁻ molar ratio indicates whether the Na⁺ was derived from the dissolution of halite. The Na⁺/Cl⁻ molar ratio of most water samples is less than 1 in the analyzed samples collected during 2017. While the 1986 ratio is equal or more than 1. This is attributed to the weathering action of silicate minerals.

The Ca²⁺ and SO 4 2 − concentrations of groundwater are controlled by gypsum dissolution and precipitation processes (Equation (3)), the ratio between Ca²⁺ and SO 4 2 − showed enriched Ca²⁺ anddeficient SO 4 2 − concentration.

CaSO 4 ⋅ 2 H 2 O ⇄ Ca 2 + + SO 4 2 − + 2 H 2 O (3)

The relation between (Ca²⁺ + Mg²⁺) versus ( HCO 3 − + SO 4 2 − ) identifies whether ion exchange or reverse ion exchange is the dominant process based on Equations (4) and (5).

Ionexchange:   2 Na + -Clay + Ca 2 + → 2 Na + + Ca 2 + -Clay 2 (4)

ReverseIonexchange:   Ca 2 + -Clay 2 + 2 Na + → Ca 2 + + 2 Na + -Clay (5)

The result of the scatter plot showed that most of the samples falling along the equiline of ( HCO 3 − + SO 4 2 − ) / ( Ca 2+ + Mg 2 + ) ratio. Can assume that the Ca²⁺ and Mg²⁺ are in equilibrium and signify the result of carbonate weathering.

The equilibrium state of the water with respect to a mineral phase can be determined by calculating a saturation index (SI) which gives insight of minerals reactivity and can reflect the thermodynamic process of natural water systems, SI values (Equation (6)) of water samples were calculated using Phreeqc Interactive Software.

SI = log (IAP)/K (6)

The calculated results for groundwater samples are shown in (Table 5) Most of the water samples yielded SI calculated results as follows: calcite is supersaturated, dolomite is approximately saturated to supersaturated; which released from the dissolution of carbonate rock (A7/B2) aquifer of Wadi Al Arab. All of the groundwater samples were under-saturated to gypsum and Halite because the major lithological units of the Wadi Al Arab area are insufficient in respect to these minerals.

In order to consider the groundwater safe and portable, its contents must concurrently meet the set standards. Some of these constituents occur in significant amounts with the main ions and others are present as trace elements. The water in the study area shows enrichment of trace elements largely with Mo followed by less concentration amounts of Ni, As, and U. Those categorized as critical parameter relevant from a health prospective based on the JSMO standard (2015) and WHO (2017) and can be harmful to the human health.

The increased concentration of Molybdenum in Wadi Al Arab wells starting from 2008 exceeding the threshold in standards with time (Figure 6), which clearly present the spatial heterogeneity of Mo Groundwater concentration in Wadi Al Arab Aquifer.

The incremental increase of molybdenum concentration in the groundwater

with maximum concentration of 1.62 mg/L in well 11a. A correlation of the heavy metal Mo, As, Ni, and U are conducted. In the scattered plot of the Mo with other critical heavy metals (Figure 7), it clearly shows a different trend line. Such concentrations suggest that the Mo was originated and contributed to the groundwater from two different sources which could be the oil shale and the phosphate host rocks.

The wells are divided into two groups based on the correlation behavior of the heavy metal;

· Group 1: includes well name WA11a, WA15, WA5, WA14 which are located in the southern part of the catchment area, at the unconfined aquifer (Figure 7) and have the same behavior.

· Group 2: includes well name WA02, WA3, WA3a, WA13a, which are located in the northern part of the catchment area, at the confined aquifer (Figure 7) and have the same behavior too.

Reduction/oxidation (Redox) processes affect the chemical quality of the groundwater in the aquifer system [27]. The redox conditions of groundwater reflect those of their reservoir rocks, even though chemical equilibrium is not usually reached between all minerals present and the groundwater.

The effects of pH and redox potential on Mo mobility in water are reviewed using the paurbaix diagram (Figure 8). As the Mo is highly soluble in water, it is usually present in the form of an oxyanion, and relatively weak in terms of sorption onto geological media with a low organic content [28].

The paurbaix diagram present (electro-potential/pH (pE/pH) diagram) for Mo. Oxidizing and reducing conditions are described by the y-axis of the diagram (higher positive electrode potential = more oxidizing environment). The acidic and alkaline conditions of the environment are described by x-axis (pH conditions).

The common redox states of Mo in the environment ranges from +4 to +6 (Mo (IV) to Mo (VI)). Under the oxic or nitrate reducing condition the most oxidizing Mo species molybdate ( MoO 4 2 − ) and hydrogen molybdate ( HMoO 4 − )

are expected to be the dominant species under neutral pH condition (pH = 6 - 8). Both MoO 4 2 − and HMoO 4 − are very mobile.

Under iron reducing conditions, Mo(VI) species can be reduced to Mo(V) species ( MoO 2 + ). Under anaerobic highly sulfidic conditions, Mo can be further reduced to a solid form as Mo disulfide (or Molybdenite, MoS₂), which is considered immobile in the aquifer [29].

The Mo species in the twelve sampled wells are confined to the field of MoO 4 ( 2 − ) ; Anoxic/non sulfidic condition (Fe reduction) which is located in the unconfined part of the aquifer, and MoS 2 ( s ) which is Sulfidic condition (low and high) in the confined aquifer.

The MoS₂ is not soluble in water; oxidation of this mineral will result in the production of molybdate oxyanion, which is very mobile in water. The stoichiometry of the reaction can be expressed as in Equation (7).

2 MoS 2 + 9 O 2 + 6 H 2 O → 2 MoO 4 2 − + 12 H + (7)

Similarly, oxidation of other Mo-Bearing sulfides, such us Pyrite, may also result in production of molybdate. Iron or Sulfide oxidizing bacteria have the potential to facilitate metal leaching but in anoxic or anaerobic condition bioleaching reaction is expected to be very slow [30] [31].