Characterization of Mineralogy, Petrography, Geochemistry and Petrogensis of Basaltic Outcrops in Jurf Ed Darawish Area, Central Jordan ()
1. Introduction
The basalt in Jordan occurs as sporadic volcanic centers along the eastern side of the Dead Sea [1] . The basaltic rocks cover about 18% of Jordan area [2] . The basalt is associated with continental rifting and in caption of the Dead Sea boundary, and it is found between magmatism and tectonic activities that have produced melted generation into fissure system [3] . The volcanism occurs at the western margin of the Arabian plate and has been tectonically controlled by the Arabian plate movement, which moved northwards along the Dead Sea transform fault. The volcanoes are clearly associated with continental rifting and inception of the Dead Sea plate boundary. The relationship between the magmatism and tectonics of the intraplate volcanism has been reported by [4] , indicating that alkaline volcanism in Jordan is similar to the Arabian intraplate volcanic fields, which erupt through two main fissure systems along the eastern margin of the Dead Sea rift in the east-west direction [3] [5] . The volcanism has probably commenced during the Miocene period and continued to the Pleistocene [6] ). The eruptions of basaltic flows in Jordan are classified and distributed into four groups; first: Central Jordan Basalt (basalt volcanoes within the rift); second: South Jordan Basalt (the eastern margin basalt) and third: Northeast Jordan basalt, Harrat Al-Sham (plateau basalt) [1] , and fourth group is the Northeast basalt (Harrat Irbid) [7] . The volcanic basalts flowing broadly at central and north west Jordan have been found to occur in eight places, namely, Tafila, Wadi Dana, Jabal Shiihan, El-Lajjoun, Jurf Ed Darawish, Ghor Al-Katar, Wadi Zarqa-Main and Ash-Shuna Ash-Shamaliyya in the form of plateau basalts. The flows have been composed of wadi fills or individual volcanic bodies (cones, plugs, and dikes) [8] [9] .
The studied area (JDB) is located within the intraplate volcanic field in central Jordan at Jurf Ed Darawish Area. The rock samples study of JDB flows covered the basalt flows into Tell El Qirana area, being 4 km west of Jurf Ed Darawish village. The main objectives of this study were to evaluate the properties of Jurf Ed Darawish basalt (JDB), as well as to investigate the Mineralogy, Petrology, Geochemistry and Petrogensis of the rock basalt outcrop in the study area.
2. Geological Setting
The Jurf Ed Darawish Basalt (JDB) are located about 20 km Southwest of Al Hisa City, and about 4 km west of Jurf Ed Darawish Village at 35˚45'380"E to 35˚45'394"E and 30˚30'398"N to 30˚30'404"N (Figure 1). The JDB covers an area of about 20 Km2, with width of about 0.5 to 2 km which include Tell El Qirana area. The JDB is represented by the volcanoes of central Jordan, within the continental plateau. The basaltic study erupted onto the middle Pleistocene age, second stage of the opining of the Red Sea at last 5 Ma [1] [9] . The JDB is covered with Amman Silicified limestone and Al Hisa Phosphorite within Belqa Group of Campanian age, and covered by fluviatile gravels, cobbles and boulders of basalt and alluvium and wadi sediments [10] .
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Figure 1. (a) Simplified Geological map of Jordan shows the Study Area (Jurf Ed Darawish Basalt), (b) Study area Jurf Ed Darawish Basalt (JDB), modified after [10] .
The study area is affected by Jurf Ed Darawish faults trending NE-SW, and many faults trending NW-SE are distributed in the study area and subparallel to the Al Karak Al Fayha fault system, these fault trending the E-W direction [11] .
3. Sampling and Analytical Techniques
A total of 16 representative rock chip samples were collected from the outcropping of Jurf Ed Darawish Basalt (JDB) in central Jordan (Figure 1). The samples are crushed and powdered using a stainless steel Jaw Crusher and an Agate Ball Mill machine to obtain a grain size (less than −80 μ). The samples were quartered to get a statistically representative (splitter) fraction and powdered using two geochemical techniques at the labs of Al al-Bayt University. The major elements were analyzed on fused glass discs-like pellet (bead) using a Phillips X-Ray Florescence Spectrometry (XRF) MAGIX PRO PW 2440 Model at the Al al-Bayt University (Water Environment and Arid Region Research Center Labs). A total of 2 g of the powder samples were mixed with 8 g of lithium tetra borate and fused in platinum crucibles over gas burners (1000˚C) for 1 h. The melts were poured into a mold to create glass disks. The Loss on Ignition (LOI) was determined by the weight lost after melting at 1000˚C. Thereafter trace elements of Sr, Cr, Co, Ni, Pb and Ba analyses by using Atomic Absorption Spectrometry (AAS), and the elements of Zr, Rb, Nb, Y and Ce analysis by using Inductively Coupled Plasma (ICP) at Al al-Bayt University, Water Environment and Arid Regions Research Center. Digestion 0.2 gm powder samples for Aquaregia solution (2.5 ml HCl + 2.5 ml HNO3 + 5 ml HF) and added 50 ml of H3BO3 to produce original solution samples, at Institute of Earth and Environmental Sciences labs, Al al-Bayt University. Thin sections were prepared at Institute of Earth and Environmental Sciences labs, Al al-Bayt University and petrographically investigated via a polarizing microscope type Lico proccer with different magnifications. The geochemical data were processed and pictorially represented using the softwares programs. Igpet 32 and GCDkit have been used to visualize, elaborate and model the geochemical data for igneous petrography purposes. CIPW-Norm calculations were carried out using the Excel sheet [12] .
4. Results
4.1. Petrography and Mineralogy
The Jurf Ed Darawish Basaltic rock samples study were holocrystalline, hypidiomorphic fine to medium grained and exhibited aphanitic to porphyritic texture, with elongated and oval-shaped vesicles. The JDB basaltic rocks in hand specimen are black to grey in color and fine-grained. The melanocratic rocks typically showed porphyritic and trachytic texture and are characterized by olivine, diopside and plagioclase phenocrysts embedded in a fine-grained groundmass that mainly consists of plagioclase, olivine, diopside and opaque minerals. The average modal composition is 45 vol.% plagioclase, 25 vol.% clinopyroxene, (diopside), 20 vol.% olivine, 10 vol.% opaque minerals (iron oxide). The secondary minerals included calcite and iddingsite. The common textures of the JDBrock samples were aphanitic, porphyritic, trachytic, glomeroporphyritic, sub ophitic, vesicular, corona and amygdaloidal.
4.1.1. Plagioclase
Plagioclase occurs in tow generation, being 3 to 6 mm long hypidiomorphiclaths and fine crystals in the groundmass. The sub-hedral plagioclase laths have compositions with 33 to 45 vol.% for modal of the rock, indicating labradorite to bytownite composition. The crystals showed simple twining. The extinction angles on plagioclase phenocrysts ranged from 28˚ to 33˚. The ternary diagram for plagioclase after [13] shows all the samples presented in labradorite and bytownite field (Figure 2(a)). The plagioclase crystals exhibited orientation within olivine and pyroxene crystals, presenting a trachytic texture (Figure 3(c)). The glomerophyritic texture (plagioclase, pyroxene, and olivine) are enclosed in ground mass and it
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Figure 2. (a) Ab-An-Or ternary for plagioclase of Jurf Ed Darawish basaltic rock samples, modified after [13] . (b) Classification of pyroxene from Jurf Ed Darawish Basaltic rocks after [14] , all the sample study plotted within diopside and Augite field.
is divided into clusters of four crystals (Figure 3(e)). Sub ophitic texture are formed for plagioclase crystal partially enclosed by pyroxene crystals. The oscillatory zoning of plagioclase (Figure 3(a) and Figure 3(f)) is present in rock samples study, as a result of the mineral chemistry which continuously oscillates between high and low-temperature compositions going from the core to the rim during crystal growth.
4.1.2. Pyroxene
The clinopyroxene (diopside) crystals are colorless or pale brown, 0.5 to 3.5 mm in length, with subhedral to unhedral crystals, have about 4 to 25 vol.% for modal. Two set cleavage intersected at ~90˚ in the cross-section (Figure 3(b)). The pyroxene crystals have an inclined extinction between 41˚ to 47˚, indicating the
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Figure 3. Photomicrographs of the JDB rock samples study (a) Simple twining and zoning of plagioclase, with Intergranular texture minerals (XPL, magnification 4×); (b) Clinopyroxene crystal with second order interference color, and plagioclase crystal (XPL, magnification 4×); (c) Euhedral to Subhedral olivine crystals, rounded by iron oxide in the rim iddingsite minerals and form to corona texture (XPL, magnification 4×); (d) The vesicles were filled with secondary minerals calcite form to amygdaloidal texture (XPL, magnification 4×); (e) Glomeroporphyritic texture, plagioclase and olivine crystals has bunched in aggregate, opaque minerals are present (PPL, magnification 4×); (f) Euhedral Plagioclase crystal, vesicles filling with silicate minerals (XPL, magnification 4×); (Ol: olivine; cpx: clinopyroxene; Pl: plagioclase; magnification 4× = 0.05 mm).
presence of clinopyroxene of diopside to augite mineral. The classification of pyroxene after [14] diagram, the rock samples of JDB is plotted within diopside and augite field (Figure 2(b)), these result documented within [15] . The clinopyroxene intersected with plagioclase crystals to form sub ophitic texture.
4.1.3. Olivine
The phenocrysts olivine crystals occuras eubhedral to subhedral crystals, ranging between 2 mm to 5 mm in diameter in the groundmass and forming 10 vol.% to 20 vol.% for modal. The olivine phenocrysts showed high relief with prismatic crystals, cracks and fracture, it is a light to colorless crystal in PPL and parallel extension. The olivine crystals exhibiting high degree of alteration to iddingsite have brownish to red color. The aggregate crystals exhibit glomeroporphyritic texture. The Glomeroporphyritic texture has bunched plagioclase and olivine crystals in aggregate. Iddingsite is common, particularly the edge (rim) of the crystal which produces corona texture (Figure 3(c)). Trachyte texture is formed by the olivine crystal surrounded by plagioclase laths.
4.1.4. Opaque and Accessory Minerals
The opaque minerals are found in JDB, forming about 5 vol.% to 10 vol.% model of the rocks, and ranging from 0.2 to 2 mm in size. They mostly occur as iron oxide magnetite and illuminate phenocrysts. The iron oxide is black in color with PPL and XPL optics. The CIPW norm calculation for the iron oxide mineral range between 4.88 to 5.92 wt% and 1.96 to 2.34 wt% norm of magnetite (Fe3O4) and ilmenite (FeTiO3), respectively. Apatite being the accessory minerals is found in JDB rock sample study with a low percentage.
4.1.5. Vesicles
The JDB rock samples show an irregular, rounded to elongated vesicles, weighing from 4 mm to 6 mm. The vesicles were filled with secondary minerals such as calcite and silicate minerals to produce amygdaloidal texture (Figure 3(d) and Figure 3(f)).
4.1.6. Groundmass
The groundmass of rock sample study consists of plagioclase (labradorite and bytownite), pyroxene (diopside, augite), olivine and opaque minerals (mainly iron oxide), with secondary minerals such as iddingsite, calcite, and silicate.
4.2. Geochemistry
4.2.1. Major Oxides
The results analysis of sixteen JDB rock samples study for major, minor, and trace elements is listed in Table 1. The JDB rocks exhibit a narrow range of silica (SiO2) saturation (between 46.11 to 49.69 wt%), with an average of 48.14 wt%, which is within the average value reported by several authors for alkali basalt and basanite [2] [3] [16] [17] , and it can be classified as basalt to Trachy basalt and basalt picrite using the Total Alkalis Vs. Silica classification scheme [18] and [19] (Figure 4(a) and Figure 4(b)). The Zr/TiO2 verses Nb/Y diagram after [20] , shows all the rock samples study classified by JDB, and plotted within the alkaline basalt (Figure 4(c)). The Al2O3 contents in the JDB samples vary from 14.11 to 16.74 wt%, within average 15.28 wt%, meanwhile, the concentration of CaO varies between 7.43 and 9.98 wt% within an average of 8.94 wt% (Table 1). The MgO content of the JDB rock sample ranged from 3.47 wt% to 8.65 wt% with an average of 6.68 wt%. The Mg number (Mg≠), defined as the molecular proportion
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Table 1. Chemical analyses of the Rock samples from JDB, major oxides (wt%), trace elements (ppm) and CIPW wt% norm.
Or: Orthoclase, Ab: Albite, An: Anorthite, Pl: Plagioclase, Di: Diopside, Hy: Hypersthene, Ap: Apatite, He: Hematite, IL Ilmenite, Ol: Olivine, Ne: Nepheline.
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Figure 4. (a) SiO2 vs. (Na2O + K2O) (TAS) diagram after [29] , the JDB rock samples plotted within basalt to Trachy basalt Field]; (b) SiO2 vs. (Na2O + K2O) diagram after [19] , the JDB rock samples plotted within basalt picrite filed; (c): Zr/TiO2 vs. Nb/Y diagram after [20] , the JDB rock samples plotted within Alk-Basalt field,
of (Mg+2/(Mg+2 + Total Fe) [21] . Mg# was used as a petrogenetic indicator for magma fractionation and its primitive volcanic rocks [22] . The JDB exhibited a high Mg≠ ranging between 30 to 53, with an average of 46. The Mg# of the indicated JDB evolved within moderately basalt. The relationship between Mg# and SiO2 shows a decrease in Mg# with increasing concentration SiO2 (Figure 5(a)). These relationship tend to be that fractional crystallization probably plays a role in decreasing Mg-number as a function of increasing SiO2 [23] . The magnesium value was considered for Fe content in the rocks. [24] reported that the values of Mg≠ > 70 can be considered as a threshold that characterizes primitive magmas. The total FeO and Fe2O3 content of the JDB ranged between 11.79 wt% to 16.23 wt%, with an average of 14.16 wt%, indicating that the rocks were enriched in Fe. According to [3] , the SiO2 under saturated magma had a high FeO and MgO content more than11 wt% and 7 wt%, respectively. The content of Na2O and K2O for the JDB sample study ranged between 1.10 wt% to 2.36 wt%, and 2.35 wt% to 3.29 wt%, respectively. The total alkali (Na2O + K2O) ranged between 3.45 wt% to 5.65 wt%, with an average of 4.74 wt%. The SiO2 Vs. Alkalis shows the rock samples study for JDB plotting in the alkaline field, these result indicates that JDB has alkaline rocks (Figure 5(b)). These results have been documented by many authors such as [17] [25] [26] [27] [28] . The major elements
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Figure 5. (a) SiO2 vs Mg# data, (b) SiO2 Vs. Alkalis After [18] , the basalt rock samples (JDB) plotted within Alkaline basalt field.
concentrations were used to calculate the CIPW norm (Table 1). The Normative anorthite has higher concentrations than albite, which indicates the plagioclase calc alkali nature of these rocks. Apatite and nepheline are present at low percentage with an average of 0.52 and 0.54, respectively, in the rock samples study (JDB). The high Normative diopside and Hypersthene fall within average of 15.22 and 5.88 respectively, these mean and indicate the clinopyroxene nature of the JDB. The normative of magnetite and ilmenite are present in the JDB, these reflected in the high percentage of the opaque minerals (Figure 3(e)).
4.2.2. Trace Elements
The JDB basaltic rock samples have a high content of Cr, Co and Ni. The content of Crrange between 23 to 221 ppm with an average of 132 ppm, Co range between 11.20 to 18.50 with an average of 15.48 ppm, and Ni ranged between 13.9 to 51.3 ppm within average 20.13 ppm (Table 1). The high content of Cr, Ni and Co indicated by the parental magma had been derived through partial melting of peridotite mantle source, which suggests the presence of olivine and clinopyroxene fractions in the JDB [3] [17] [24] [30] . The binary diagram in Figure 6, shows the Mg# versus Cr, Co and Ni. The general trend of Crdecrease with increasing Mg# (Figure 6(a)), this result is documented with Zarqa-Ma’in basalt, Ar-Rabba Basalt, Mudawwara-Quwayra Basaltic Dike and Atarous Basalt [17] [25] [26] [31] . Inverstrend falls between Mg# versus Co and Ni (Figure 6(b) and Figure 6(c)), These results arethe most probable from magma mixing and assimilation within the country rock and this resulted to dilution of Cr, Co and Ni, where Cr is related to clinopyroxene [32] .
The concentration of Sr, Zr, Pb and Ba in the JDB rock sample study had relatively high contents. The Sr ranging between 365 to 630 ppm with average of 425 ppm, Zr content 74 to 136 ppm with average of 91 ppm, Pb range between 2.9 to 27 with average of 8 ppm and Ba range between 45 to 214 within average 114 ppm, respectively (Table 1). The Sr+2 is substitute for Ca in plagioclase minerals (Anorthite CaAl2Si2O8) and lesser extent was found in K-feldspar. Zr is found in accessory minerals such as Zirconium (ZrSiO4), Pb substitute for K in K-feldspar and Ba+2 appears in biotite and potash feldspar, because of its higher charge Ba+2 should be captured by potassium compounds. Pb tends to be captured by potassium minerals [33] [34] .
The Rare Earth Elements (REE) includes Nb, Y, Ce content ranging between 16 to 42 ppm for Nb, 15 to 25 ppm for Y and 28 to 67 ppm for Ce, respectively (Table 1). The REE were replacement of Ca+2 in accessory minerals such as Apatite (Ca5(PO4) (OH, F, Cl) and Titanite (CaTiSiO5). Niobium (Nb5+) does not substitute for major elements because of its high charge, but it may substitute for titanium due to their similar ionic radii and valence state [34] ). Ce evidently remains in the liquid at late stage of crystallization, it is concentrated in micas and potash feldspar to produce pollucite minerals (CeAlSi2O6) [35] . The average ratio between Zr/Nb, Y/Nb and Zr/Y are 4.40, 0.89 and 4.98, respectively. These ratios were documented and reported by [26] [36] ) for the intercontinental alkali basalt.
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Figure 6. (a) Mg# vs. Cr data for JDB rock samples study; (b) Mg# vs. Co data for JDB; (c) Mg# Vs. Ni data for JDB.
5. Petrogensis
The chemical analysis of major and trace elements for JDB rock samples study are used to construct discriminatory diagrams, which help in the classification, nomenclature and interpretation of the tectonic setting of the JDB. The Classification for [37] include all the JDB samples plotted in the alkaline to sub alkaline rock field (Figure 5(b)). The AFM diagram shows the JDBrock samples plotted within the calcalkaline series (Figure 7(a)). The ternary diagrams for Ti-Zr-Sr and Ti-Zr-Y diagrams (Figure 7(b) and Figure 7(c)) after [32] , shows all the JDB Rock samples plotted within the calcalkaline basalt field. The MgO-FeO(tot)-Al2O3 diagram after [38] , shows the JDB rock samples were plotted within continental basaltic field (Figure 7(d)).
The low content of SiO2 (46.11 to 49.69 wt%) and high content of MgO (3.47 to 8.65 wt%) and total FeO + Fe2O3 (11.79 - 16.23 wt%) indicated the natural fractionation of the JDB [17] ). The high concentration of Crranging between 23 to 221 ppm within average 132 ppm is consistent with findings reported for primary magma [3] [21] [31] [39] . The high Mg# (average 46) for JDB is similar to that reported for rock affected by fractionation or accumulation of clinopyroxene, orthopyroxene, as well as olivine and plagioclase [40] .
The high content of Zr/Y (average 4.98) and TiO2/Y (average 0.06) ratios and low content of Y (average 18.81 ppm) indicate the garnet-bearing source rocks [41] . The spider diagrams for Rock Primordial mantle are used to study basaltic rock samples (JDB) (Figure 8). They presented enrichment of the incompatible
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Figure 7. (a) AFM diagram after [37] ), shows the basalt rock samples study (JDB) were located within Calc-Alkaline basalt field; (b) Ti-Zr-Sr discrimination diagram after [38] , shows the JDB rock samples study were plotted within Calc-alkali basalt field; (c) Ti-Zr-Y discrimination diagram after [32] ); shows the basalt rock samples study located within Calc-alkali basalt and Within-Plate basalt field; (d) Discrimination diagram MgO-FeO(tot)-Al2O3 after [38] , shows the JDB rock samples plotted within Continental basaltic field.
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Figure 8. Spider diagram of incompatibility elements from the JDB rock samples study; Rock/Primordial mantle for trace element abundance patterns of the basaltic rocks after [57] .
LILE such as Ba and K, depletion of Ce relative to K, and enrichment of Nb and Pb with depletion of Y. The mafic volcanic rocks for JDB exhibited positive Nb, Zr and Ti anomalies. The negative anomalies of Ba, Sr, Ti and P may be attributed to the fractionation of feldspar for Ba and Sr depletion apatite for P depletion, and (Fe-Ti) oxides for Ti depletion [42] . The Rock Primordial mantle value of the basaltic rock samples study (JDB), shows a positive Nb peak, which conforms to the tertiary to recent continental alkali basalt provinces [16] [17] [43] [44] , and indicate the JDB product for the lithosphere from upwelling of the asthenosphere mantle [22] [45] [46] .
6. Discussion
The basalt samples study (JDB) characterized are alkaline to sub-alkaline with respect to silica content and under saturated SiO2. Similar rock compositions were reported by [25] [26] [27] [39] [45] [47] [48] , from central, Northwest and Northeast Jordan. The lithosphere mantle in Arabia within Jordan is chemically heterogeneous [17] . According to [49] , there is a possibility that the volcanic rock was sourced from the lower lithosphere depth and from asthenosphere. The Cenozoic interpalate volcanic fields which form Arabia may be the product for the melting of upper mantle wedge material, fertilized during Pan-African subduction and incorporated into the Arabian Lithospheric mantle [3] [46] [49] .
According to [50] the primary alkali basalt rocks can be formed by low degree of melting at a pressure as low as 13 kbar and can fractionate to tholeiitic liquids between 4 and 12 kbar. [51] explained that the alkali basalt melts can be derived for the low-velocity zonation, 5% partial melting approximate depths, 85 - 95 km within 30 kbar and 10% partial melting in the Lithosphere, at 60 - 90 km within 19 - 27 kbar. The geochemistry of alkaline basalt indicates a source for intraplate volcanism [49] . The basalt flows may be both direct products of mantle partial melting and the differentiates of more primitive picritic partial melts [24] ; However, the basalt samples study was plotted within basaltic picrite field (Figure 4(d)).
The Mg# values (Mg+2/(Mg+2 + Total Fe) ranging from 30 to 53 (Table 1), could bea pointer to the little fractional crystallization and removal of olivine and pyroxene. The concentration of Cr and Ni vary between 23 to 221 ppm and 14 to 51 ppm, respectively. These concentrations contribute to some degree of olivine fractionation, and tends to increase the incompatible trace element concentration in the studied basalts (JDB) [17] . [48] studied the basalt of Al-Qiranha volcano in central Jordan, and it was concluded that the basalt flows is indicative of a primitive upper mantle that has suffered partial melting at a temperature ranging between 1050˚C and 1210˚C and pressure between 15 - 20 kbar. Based on the study and information for [52] , produced by the recent basaltic flows in Ethiopian rift as a small degree partial melting peridotite of 15 - 25 kbar. Also [53] suggested that the basaltic flows from central France are similar in their mineralogy of central Jordan volcano, and were produced by partial melting of spinel lherzolite at 16 - 20 kbar pressure. The basalt flow from El-Lajjoun, Ar-Rabba, Zarqa-Ma’in Atarous and Ash-Shun Ash-Shamaliyya areas of central and northwest Jordan, is produced within the intraplate to continental calc-alkaline to alkali basalt [17] [25] [26] [27] [45] , these results documented to the JDB is from the same sources product.
The primary alkali basalts can be formed by low degree of melting, as they are similar in their mineralogy to those of central Jordan volcano produced by partial melting of spinel lherzolite at 16 - 20 kbar pressure [17] [54] [55] . The geophysical methods for seismic and gravity data are indications that the crust thickness below this field is about 35 km [56] . After all the information obtained for the JDB study, I suggested that the source of the JDB is the contribution within Arabian intraplate basalt produced by numerous Cenozoic intraplate volcanic fields, throughout the melting upper mantle wedge material fertilized during Pan-African subduction and incorporated into the Arabian, Lithospheric mantle [57] . According to [58] , had reported to that seem to be originated Arabian lithosphere in the region from depths of ~85 km.
7. Conclusions
The Jurf Ed Darawish basalt (JDB) was introduced within intraplate to alkali basalt in Miocene to Pleistocene volcanism field at central Jordan. The study area covered the western part of Jurf Ed Darawish village, about 20 Km2, including the Tell El Qirana area. The following is the conclusion of the present study:
1) The mineral composition of basaltic rock samples study (JDB) is as follows: plagioclase, pyroxene (diopside-Augite) and olivine. Secondary minerals such as iddingsite are produced by alteration of olivine crystal and calcite. The accessory minerals include apatite and opaque minerals, magnetite. The texture observed was aphanitic, porphyritic, trachytic, glomeroporphyritic, sub ophitic, vesicular, and amygdaloidal texture.
2) The chemical classification of JDB as basalt, Trachy basalt to basalt picrite, had Alkaline to sub-alkaline with respect silica content under saturated silica (SiO2). The discrimination diagram showed that the JDB rock samples studied were plotted within the calcalkaline basalt field and continental basaltic field. The alkali basalt rocks can be formed by low degree of melting at a pressure as low as 13 kbar and can fractionate to tholeiitic liquids between 4 and 12 kbar.
3) The Cenozoic interpalate volcanic fields throughout form Arabia may be the product for the melting of upper mantle wedge material, fertilized during Pan-African subduction and incorporated into the Arabian Lithospheric mantle. The alkali basalt melts can be derived for 5% partial melting approximate depths 85 - 95 km within 30 kbar and 10% partial melting in the Lithosphere, at 60 - 90 km within 19 - 27 kbar, and the recent study, concluded that to originated Arabian lithosphere from depths of ~85 km.
4) The Mg# values (Mg+2/(Mg+2 + Total Fe) ranging from 30 to 53, it could be pointed to the little fractional crystallization and removal of olivine and pyroxene. The concentration of Cr and Ni varies between 23 to 221 ppm and 14 to 51 ppm, respectively. These concentrations contribute to some degree of olivine fractionation, and tend to increase the incompatible trace element concentration in the studied basalts (JDB).
5) The spider diagram for Primordial mantle shows the rock samples study (JDB) enrichment of the incompatible LILE such as Ba and K, depletion of Ce relatively to K, and enrichment Nb and Pb with depletion of Y and positive Nb, Zr and Ti anomalies. Negative anomalies of Ba, Sr, Ti and P may be attributed to the fractionation of feldspar for Ba and Sr depletion apatite for P depletion.
6) The source of the JDB is the contribution within Arabian intraplate basalt produced by numerous Cenozoic intraplate volcanic fields, throughout of melting upper mantle wedge material fertilized during Pan-African subduction and incorporated into the Arabian, Lithospheric mantle. The positive Nb peak conforms to the tertiary to recent continental alkali basalt provinces, which conforms to recent continental alkali basalt provinces; these indicate the JDB produced of lithosphere from upwelling asthenosphere mantle.
Acknowledgements
The author is thankful to the laboratory of the University of Al al-Bayt University, Institute of Earth and Environmental Sciences for the geochemical and thin section preparation samples. Thanks to the Water Environment and Arid Region Research Center Labs at Al al-Bayt University for analysis of major elements using X-Ray Florescence Spectrometry (XRF) and trace elements using Atomic Absorption Spectrophotometer (AAS) and Ion Conductive Plasma (ICP). The author is very grateful to Mr. Adnan Mashaqbeh for assisting in the preparation of thin sections, at the Institute of Earth and Environmental Sciences labs, Al al-Bayt University.