The dominant basaltic petrographic rock types in the GPVF are basanites, alkali basalts and alkali olivine basalts (Table 1). They are composed mainly of olivine, plagioclase, and augite phenocrysts set within a fine-grained to slightly medium-grained matrix containing intergranular growth. Most samples are glomeroporphyritic with glass in the groundmass.

Plagioclase is the most abundant mineral (7% to 24% by volume; Table 2). It occurs as euhedral to subhedral grains or as small microliths within the matrix. It is mostly optically un-zoned, but some grains show rare oscillatory zoning and sericite alteration. Olivine is the second most dominant mineral phase, forming between 6% and 20% of the rock volume (Table 2). It occurs as subhedral phenocrysts, commonly surrounded by iddingsite rims. In most samples, olivine contains inclusions of idiomorphic spinel.

Clinopyroxene (6% to 12% by volume) forms subhedral phenocrysts showing the characteristic near-orthogonal simple and sector zoning. It occurs within the microcrystalline matrix or in association with olivine and plagioclase clusters. In some samples, the pyroxene crystals are engulfed by rims of fine-grained magnetite, which occasionally occurs as small inclusions along the margins. A brownish-green hornblende is generally found in the sodium-rich samples and is

frequently inter-grown with the clinopyroxene. Accessory minerals include magnetite, ilmenite and apatite. Glass constitutes about 4% to 8% in some of the groundmass in the GPVF basaltic rocks. (Figure 3)

Ultramafic xenoliths are classified in this study according to the scheme of [14]. Xenoliths associated with the Ghab basaltic magmas are mostly chromium spine-peridotite type, including lherzolite and harzburgite.

It consists of three primary minerals: forsterite, enstatite and chromium diopside. Petrographically, the GPVF ultramafic xenoliths have a medium-grained equigranular texture. In these rocks, the mineral grain boundaries meet at interfacial angles of 120˚ that sometimes encloses anhedral phlogopite along the grain boundaries. Olivine is subhedral and optically homogeneous. It is mostly fresh with minimal alteration. Pyroxene is subhedral, but some grains are anhedral and display the characteristic ~90˚ cleavage.

Some xenoliths contain dark melt pockets of different sizes, and some of the pyroxene grain are spongy with tiny droplets of glass. Spinel is present as anhedral crystals in all samples of the Ghab xenoliths. Contacts between olivine and

pyroxene occasionally show reaction corona textures in which amphibole replaces pyroxene, and spinel and magnetite replace olivine. Some of the xenolith samples show signs of variable metasomatism, like thin veins of fine-grained phlogopite.

Chemical compositions of the GPVF basalts show high alkalinity values for Na₂O + K₂O, permitting them to be classified as mainly alkali basalt and basanite on the basis of the TAS classification scheme of [16] (Figure 4).

Figure 5(a) shows the major elements chemistry. SiO₂ contents vary in a narrow range between 44.33 wt% and 46.63 wt%. MgO shows variations from 4.01 wt% to 8.28 wt%. The K₂O content varies from 0.67 wt% to 1.91 wt%, while the Na₂O content changes from 1.5 wt% to 3.73 wt%. The Al₂O₃ content of the Ghab

volcanic samples varies from 12.48 wt% to 15.21 wt%, averaging 14.25 wt%. The FeO content is mostly uniform in these basalts and the total iron is generally similar in most samples. It ranges from 13.6 wt% to 18.07 wt%. The TiO₂ content varies between 0.98 wt% and 3.1 wt%. The differentiation index (D.I.) calculated for the GPVF basalts spans a range of 18% to 35%, with an average value of about 28%.

As shown by Figure 5(b) the rocks are characterized by high concentration of Co (42 to 56 ppm), Ni (113 to 193 ppm), Cr (247 to 331 ppm), and V (160 to 197 ppm). The average Ni content of 185 ppm is higher than the value of 145 ppm reported for Ni in alkali basalt by [17].

Strontium and barium contents vary from 1123 to 1405 ppm and from 583 to 805 ppm, respectively, with Sr averaging 1300 ppm and Ba averaging 719 ppm. These averages are higher than the values of 1069 ppm and 546 ppm reported for these two elements by [18] for basaltic rocks from northern Syria. The Zr content in the investigated samples ranges from 185 to 261 ppm, whereas the Nb content ranges from 78 to 124 ppm. The Y content varies in a narrow range between 20 and 30 ppm.

The two most abundant oxides in the ultramafic xenoliths of the GPVF, SiO₂ and MgO, vary in extremely narrow compositional ranges. They change from 42.73 wt% to 43.67 wt% in the case of SiO₂ and from 41.34 wt% to 43.81 wt% in the case of the MgO, for spinel lherzolite and spinel harzburgite. In addition, the xenoliths show variations in the Al₂O₃ and CaO contents, and exhibit higher contents of both elements in the spinel lherzolite (Figure 6).

Figure 6 shows chemical variations of the major elements (Al₂O₃, CaO and TiO₂), and the minor element Cr₂O₃ versus MgO (wt%) for the GPVF ultramafic xenoliths. The plots for the first three elements are compared with variations of these elements in ultramafic xenoliths elsewhere [19] [20] [21].

Bulk compositions of these spinel peridotite xenoliths in the Ghab region display a low content in Al₂O₃, CaO and TiO₂ when plotted against MgO (Figure 6).

Generally, the differentiation index for the GPVF rocks is relatively low, indicating possibly a limited differentiation in the magma chamber supplying magmas to the surface of the Ghab region. The relatively high normative olivine reflects the high content of magnesium and iron oxides in the rocks. The magnesium number (Mg#) is exceptionally high and is almost unity (89.63 - 90.91).

Overall variations in the content of major element oxides and minor elements in the GPVF basaltic rocks show limited concentration ranges. Such uniformity in the chemical composition reflects possibly the operation of several competing petrological processes during the genesis of these rocks, although this interpretation is derived only from a small investigation field area.

These petrological processes involve partial melting of the mantle source, crystallization of basaltic liquids during their ascent to the surface, and crystallization at shallow depths and on the surface.

Several geochemical features of the GPVF basalts show that the compositional variations cover only restricted concentration ranges.

The most critical feature suggesting homogeneity of the magmas is the relatively small ranges of the differentiations index (D.I.) (averaging 27.6) and the Mg# which ranges from 44 to 87 and averages around 64 (Table 3(a) and Table 3(b)).

For some elements in the GPVF basalts like SiO₂, TiO₂, Sr, V, and Co, the variations display minimal changes (Figure 5(a) and Figure 5(b)). In some instances, the contents of these elements remain nearly constant.

The diagram for Y – Nb variations (Figure 7) does not display a clear correlation

between these two elements, due to the near constant Y values of 22 to 28 ppm. This behavior contrasts with diagrams showing positive correlations. The behavior of these two elements in the GPVF rocks is attributed to the strong chemical homogeneity displayed by the magmas crystallizing these rocs.

The plots showing the relationships between Ni and MgO and Co and MgO (Figure 8(a)) display a similar behavior as that of the major chemistry (Figure 5(a)), and thus supports a similar reasoning. These two plots show the Ghab basalts as clusters lacking evidence for systematic variations. This situation is different from the Ni and Co cases showing clear crystal fractionation and positive relationships (e.g. [23] ), and attests to the homogeneity of the investigated Ghab rocks. This strong uniformity in the major element composition thus indicate a coherent chemical character for the magmas of the GPVF, leading to the conclusion of minimal modifications of their composition from the time of generation by partial melting until extrusion.

Fractionation and differentiation have played a very limited role in the evolution

of the GPVF basaltic magmas. The relatively narrow range of MgO, in addition to the clustering in the three plots in Figure 8(a) (Ni, Co and CaO/Al₂O₃ vs. MgO), is evidence for an insignificant or lack of fractionation and differentiation [24]. This is attributed to a rapid rise of the magmas through the upper mantle and the crust, precluding the possibility of differentiation. This, in turn, suggests the magmas did not reside intermittently along its path through the continental lithosphere, circumventing the possibility for mineral separation and fractionation. Furthermore, this reasoning, along with the magma homogeneity suggested above, implies the GPVF magmas are close to their initial pristine composition at the site of the partial melting, and the lack of any subsequent significant differentiation and fractionation.

The geochemical behavior of Cr in the GPVF volcanic rocks (Figure 5(b)) supports the contention expressed above for the negligible role of fractionation. Chromite and chrome-spinel, the main repository of Cr in basaltic rocks, crystallize at an early stage of solidification of primary magmas. High concentration of Cr in the earliest crystallization product from primary mafic magmas is explained adequately by fractionation of chromite, reinforced by an early coupled separation of chrome-spinel (or Cr in solid solution in magnetite) and clinopyroxene, as suggested by [25]. Such a scenario is applicable to the situation in the GPVF basalts, where both of these phases form constituents in the analyzed samples.

The slight negative correlation between Cr and silica in the GPVF (Figure 5(b)) is attributed to the fractionation of clinopyroxene and minor quantities of Cr-spinel from the initial magma, an interpretation similar to that of [26]. Yet, another observed feature of Cr in the Ghab basalts is the relatively high content of Cr (299 ppm) that is much higher than twice the value of 142 ppm tabulated by [27] for primary basaltic magmas. This relatively high Cr content in the basalts is inconsistent with the Ghab magmas having undergone any significant differentiation or crystal accumulation.

In view of the similarity in chemical affinity between Ni and Cr, a similar reasoning is advanced as an explanation for the pattern of Ni variations in the Ghab volcanic rocks, but the controlling crystallizing phase for Ni is fundamentally olivine. The decrease in the Ni content with silica in the Ghab rocks (Figure 5(b)) may be ascribed to a fractionation mechanism solely involving the extraction of olivine [26]. Thus, relatively high abundances of Cr and Ni in the GPVF basalts testify to a very small change in the magma composition since its inception. [28] reached a similar explanation for the Harrat Al Fahda basaltic rocks in Jordan.

Another illustration pertaining to this lack of differentiation-fractionation is the relationship between each of the ratios of Ni/FeO and Co/FeO and the Al₂O₃/MgO ratio (Figure 8(b)). The plot of Ni/FeO in the figure shows this ratio in the lavas to vary between 17 and 23, while the Co/FeO ratio ranges from 2 to 6. [22] Used similar plots to assess the degree of fractionation and concluded that only clearly unambiguous relationships in them can be utilized as evidence for fractionation. An application of this logic to the Ghab volcanic rocks shows that changes in these ratios display a lack of relationship in the first plot in (Figure 8(b)) and a negative relationship in the second plot in. The covariation in the Ni case displays a very insignificant relationship, while the covariation in the Co case shows a negative trend (Figure 8(b)). The Co plot displays a clear and slightly steeper slope than in the Ni plot.

The Pearson correlation coefficient (r) was calculated for the Ni and Co magnitude of linearity. The (r) values were (−0.43) for the Ni case and (0.01) for the Co case. These values are very low and support the conclusion for lack of differentiation. Even when the outlier sample (GS03) was excluded from the regression, the resultant (r) values were (−0.09) for Ni and (0.25) for Co. The overall explanation for the low and nearly flat covariations is the absence of any sign of differentiation and fractionation in the Ghab Pliocene volcanic rocks and their parent magmas.

Ba and Sr readily substitute for K in K-feldspar (anorthoclase in the GPV basalts) and Ca-plagioclase, respectively. Variations in the content of these two elements in the GPVF basalts thereby reflect the fractionation of these two phases. The constant level of content of both elements argues against much fractionation of these minerals. Nonetheless, the slight decrease of Ba at the highest level of silica values in these rocks may reflect a selective, but limited and late, fractionation of anorthoclase.

The most likely cause for the magnitude of the differentiation index (D.I.) and the magnesium number (Mg#), as well as the invariability in the content of most major and minor elements, is an attainment of a long-lived, continuous melt extraction and homogenization, stipulated at the site of the partial melting supplying magmas to the surface of the Ghab region. This is augmented by a very limited fractionation and differentiation during the magma ascent to the surface

The extent of magma mixing has a direct influence on chemical variations of magmas. It requires the coexistence of magmas with contrasting chemical compositions.

When relevant, magma-mixing processes are represented by mixing lines in plots like that relating Zr and Nb abundances in the Zr - Nb variation space. These two elements generally produce a linear trend of variation, similar to that in Figure 9(a). This plot of the Zr - Nb co-variations for the GPVF rocks illustrates that their concomitant co-variation falls far from the mixing line (dashed line). This divergence signifies the improbability of magma mixing as a viable mechanism during the genesis of the GPVF basalts.

In addition, the noticeable lack of crustal felsic xenoliths in the GPVF xenolith assemblage that was entrained by the Ghab Pliocene basaltic magmas argues against a substantial involvement of crustal lithologies and contamination of the

magmas. This interpretation is similar to that reached by ( [18] [33] ), who stipulated for basalts from other areas in Syria only a limited upper crustal contribution from an ancient Proterozoic basement.

The three curves in Figure 9(a) peridotite-1, peridotite-2 and peridotite-3 correspond each to a model d peridotite composition with the following olivine-orthopyroxene-clinopyroxene-garnet ratios: (0.50:0.25:0.20:0.05), (0.58:0.27:0.13:0.02) and (0.65:0.28:0.05:0.02).

The partial melting process responsible for the generation of basaltic melts is analyzed with the aid of this Zr - Nb plot [29]. The plot shows a summary of partial melting of three different pyrolite models, each containing peridotite assemblages with contrasting contents of olivine, clinopyroxene, orthopyroxene and garnet [29]. The Zr - Nb plot shows the three-pyrolite models capable of production of basaltic liquids. Each of these models shows as a unique and discrete curve that predicts the behavior of these two elements during melting.

Figure 9(a) illustrates the application of this plot to the GPVF case. The Z - Nb variations adhere very closely, and are in a good agreement, with the curve displaying partial melting of model peridotite 1. Most likely, this interpretation points to a mantle source region whose composition approximates a peridotite of mineral constitution similar to this peridotite model in the plot.

Ultramafic xenoliths generally constitute a common component in basaltic rocks, and their origins link them to the upper mantle. They are also associated with mafic alkaline rocks. Compared with other Cenozoic peridotite xenoliths trapped in basalts in settings belonging to oceanic extensional environments (Oman) ( [19] [20] [21] ), the Ghab xenoliths record chemical variations which resemble more variations in xenoliths from continental extensional rifting settings than those from other environments.

The GPVF xenoliths display generally negative correlations between the contents of Al₂O₃, CaO, and TiO₂, and the MgO content (Figure 6). The variations are against 8% spread in the MgO content. This geochemical spread in the MgO values is wider than reported in xenoliths from the three regions.

Figure 6 also shows the relationship between Cr₂O₃ and MgO in the Ghab xenoliths. The absence of a clear relationship between the two elements is ascribed to the refractory geochemical behavior of Cr in Cr-diopside and Cr-spinel in the mantle undergoing partial melting. [34] Consider chromite as a congruently melting mineral during partial melting of peridotite in the upper mantle. The degree of this partial melting is probably small and at high pressure, as suggested by the high iron content (13.60 - 19.94 wt%) of the GPVF basalts. This iron content is high when compared with its content from other parts of the region, like the northwestern part of the Harrat Ash Sham volcanic field [35].

The xenoliths from the GPVF are invariably separated from their host basalts by thin basalt films (less than 1 mm wide). This feature characterizes many of the xenoliths; it is true for xenoliths contained in the lava flows, as well as those xenoliths enclosed in the pyroclastic bombs. [35] Interpreted this texture to suggest that the basaltic magmas quenched against the xenoliths, because of the rapid transit and fast cooling of the magmas during their ascent. This minimizes the possibility of modification and alteration of the xenoliths. The spongy texture of the clinopyroxene in the xenoliths suggests the melting of this mineral during decompression while ascending through the transpression forces of the Dead Sea graben [36].

An exceptionally large abundance of xenoliths in volcanic fields indicates a mechanism of transport to the surface that involves fast transit through the lithosphere [29]. Consequently, such xenoliths are subjected to insignificant corrosion and contamination. This mode of transport is a reasonable mechanism contributing to the preservation and abundance of ultramafic xenoliths in the GPVF.

Analogous to their host basaltic lavas described earlier, the peridotite xenoliths of the GPVF display a limited variation in their chemistry (Table 4). For example, the Mg# is almost constant (89.63 - 90.91). This very narrow compositional range can potentially lead to some ideas regarding the genesis of the xenoliths. The meager number of xenolith samples analyzed does not, however, hamper the arrival at basic conclusions in this regards.

Figure 9(b) shows the MgO - Al₂O₃ plot for basaltic and ultramafic xenoliths [37]. It is a plot of the relationship between Al₂O₃ and MgO for both the GPVF basalts and their enclosed xenoliths. Visual inspection of the trend vector shows that the projection of the linear variations in the xenolith compositions passes through the cluster of compositions of the basaltic samples. Such a linear array joining the two compositional end-members implies that a genetic relationship exists between the GPVF basalts and their companion xenoliths. The significance of the linearity in the xenolith Al₂O₃ - MgO compositional covariation, nonetheless, is reduced by the limited spread due to the small number of xenoliths (6 samples).

The simplest interpretation in the GPVF case is the derivation of these basaltic melts from the parent lithology of the enclosed xenoliths at the site of partial melting in the mantle in the Pliocene. [37] Have used this Al₂O₃ - MgO relationship to enforce the interpretation above.

[32] Presented a plot of ultramafic xenoliths collected from many regions, which shows a negative correlation between the Mg/Si and Al/Si ratios for the xenoliths in the plot of Figure 10(a). A line through the data points depicts the trend of crystal fractionation in such rocks [32]. This crystal fractionation trend provides a relationship that sheds light on the evolution of ultramafic xenoliths.

Figure 10(a) is such a diagram containing a plot for the GPVF xenoliths. They display a negative trend of Mg/Si ratio against Al/Si ratio that resembles the plot produced by [32]. This trend is viewed as indicating partial melting of a primitive

mantle source to produce lherzolite. [38] Arrived at a similar conclusion for ultramafic xenoliths from the Golan Heights in southwestern Syria. This resultant lherzolite upper mantle eventually underwent partial melting beneath the Ghab region and generated the Ghab basaltic magmas during the Pliocene.

Additionally, the GPVF xenoliths record a positive correlation between Al₂O₃ and CaO (Figure 10(b)), which, similar to the Mg/Si - Al/Si plot, depicts the continuous evolution from the harzburgite field to the lherzolite field, a feature that was explained by [37] to reflect the evolution stipulated above.