1. Introduction

IJG

International Journal of Geosciences

2156-8359

Scientific Research Publishing

10.4236/ijg.2019.106035

IJG-92957

Articles

Earth&Environmental Sciences

Petrography, Geochemistry and Petrogensis of Pleistocene Basaltic Flow from Northwest Atarous Area, Central Jordan

Hassan

Al-Fugha

¹Ibrahim

Ahmad Ali Bany Yaseen

²^*

Department of Environmental and Applied Geology, Faculty of Science, University of Jordan, Amman, Jordan

Department of Earth and Environmental Sciences, Institute of Earth and Environmental Sciences, Al-al-Bayt University, Al-Mafraq, Jordan

10062019

10066136313, April 20198, June 2019 11, June 2019

2014

This work is licensed under the Creative Commons Attribution International License (CC BY). http://creativecommons.org/licenses/by/4.0/

Fifteen basaltic rock samples were collected from central Jordan at the Atarous volcanism basaltic flow area. The samples cover about 8 km ² from the Atarous Basalt flow (AB). The AB flow was introduced in the Miocene to Pleistocene periods. The samples analyze major and trace elements by using XRF. Petrography, Geochemistry and Petrogensis have investigation to carried out for the AB. The petrography analyses of the AB rocks show they are composed of plagioclase (labradorite and bytownite), pyroxene (augite), and olivine (forsterite); accessory minerals include apatite and secondary minerals magnetite, ilmenite, spinel and iddingsite. The AB is classified within alkaline to sub-alkaline and tholeiitic to Calc-Alkaline basalt. The Mg# range between 0.39 and 0.49 of basalt samples exhibits different degrees of fractionation with a low degree of melting < 15% as indicated from the varying concentration of incompatible trace elements Ba, Rb, Sr. Trace elements of primary magna show low variable abundances of compatible and incompatible elements, which reflecs a homogenous source. Geochemical parameters such as Mg# and high Ti contents indicate that the corresponding magmas are of primary origin. The tectonic setting of AB is explained by using discrimination diagrams, Ti-Zr-Sr and Nb-Zr-Y and Ti-Zr-Y, the AB plotted within the plate basalt, alkali basalt and Calk alkaline basalt field, respectively. The spider diagram shows the samples AB enrichment of the Ba, K, Nb and Ce, depletion of Nb and Y. The AB exhibited positive Nb, Ce and Ti anomalies, and negative anomalies of Ba, Sr, and P. It is attributed to the fractionation of feldspar for Ba and Sr and apatite for P depletion. The spider diagram showed a positive Nb peak, which conforms to the tertiary and to recent continental alkali basalt provinces and indicates that the AB is the product of lithosphere from upwelling asthenosphere mantle.

Petrography Geochemistry Petrogensis Pleistocene Basaltic Atarous Basalt Jordan

1. Introduction

The studied area is located within the intraplate volcanic field in the Atarous Area of central Jordan. The volcanic cone is located at the eastern side of the Dead Sea area, 1 km northwest of Atarous Village. 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 (Figure 1). These 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 [1] , 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 [2] and [3] .

The volcanism might have probably commenced during the Miocene period and continued to the Pleistocene [4] . The Cenozoic volcanism in central Jordan has a relatively long period of magmatic sequence extending from the Oligocene to the Holocene [1] and [5] . The basaltic lava poured from vertical fissures and local vents along the Jordan Rift mountain ridge in central Jordan and in northeast Jordan [6] . The Jordanian basalts are part of the Arabian plateau basalt that covers a large area in Saudi Arabia, Jordan and Syria.

In general, alkali basalts are widespread on continental plates and are usually associated with continental rifting [7] . This is also the environment of the extended young volcanic fields near the western margin of the Arabian plate, which is separated from the African plate by the Red Sea Rift. Such volcanic fields occur in Yemen, close to the triple junction with the East African Rift and the Aden Ridge, and northwards in Saudi Arabia, Jordan, Syria, Turkey and from the southern rim of the Damascus basin. It covers an area of about 11.400 km². The extensive volcanism in northeastern Jordan occurred during faulting episodes and predominantly consisted of alkali basalts, basanites and hawaiites [1] and [8] ranged from 0.2 to 18.5 Ma as determined by K-Ar dating [4] [9] [10] [11] [12] . In central Jordan volcanos, magmas transported upper mantle nodules with the composition of spinel lherzolite to the surface [13] . These xenoliths contain olivine, orthopyroxene, clinopyroxene and spinel as typical for the uppermost mantle below continental plates, analogous to worldwide occurrences [7] and [14] [15] . The objective of this study is to investigate the petrography, geochemistry, and petrogensis of the intercontinental basaltic flow at the Atarous Basalt Area (AB), which is in the east of the Dead Sea in central Jordan.

2. Geologic Setting

Jordan is part of the Arabian plate, which is drifting to the NE towards the Tauros-Zagros compressional zone due to the aforementioned opening of the Red Sea. This process is accompanied by the development of the Dead Sea transform fault, which trends north-south with a net slip along it of about 105 km [16] [17] . The volcanoes in the studied area are of stratovolcano type [18] [19] [20] . They rose above the surface of basalt flows by more than 120 m. On the slopes of the volcano, finely grained ash, angular and spherical pyroclastic of a diameter of less than 0.2 cm and basaltic bombs of different sizes with diameters ranging between 0.5 and 1.2 m are exposed. Basaltic layers of blocky lava with an average thickness of 40 cm are also present. The tectonic evolution of the Arabian plate is determined by the main regional structures of the region, including the Red Sea rift and the Dead Sea transform fault, which trends north-south and the net slip along it is about 105 km [16] [17] . The study area is affected by different structures such as Zarqa-Main fault trending E-W direction and extending from the Dead Sea to Wadi Sirhan fault. The basalt intrudes along the fault and forms a volcanic neck. The AB occurs in the direction of N-S, E-W, NW-SE, and NE-SW, which coincide within the main regional and local structural fault directions. The fracture trending N-S are parallel to Zarqa-Ma’in fault, Suwaqa fault, Hasa fault, and Salwan fault perpendicular to the Dead Sea Transform Fault and Suwaqa normal fault [5] . The trending joints NE-SW was consistent with the late Pan-African stress pattern and are parallel to Amman Hallabat fault. The trending direction NW-SE is related to the regional faults, such as Karak Fayha fault and Wadi Sirhan fault, which extends from Saudi Arabia in the south and continuing to north Jordan.

3. Sampling and Analytical Techniques

A total of 15 representative rock chip samples were collected from the outcropping Atarous Basaltic (AB) cones 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 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 the mineralogy institute at the University of Stuttgart Germany. The major and trace elements were analyzed on fused glass discs-like pellet (bead) by using X-Ray Florescence Spectrometry (XRF) at the Department of Geology, University of Stuttgart (Germany). A total of 2 gram of the powder samples were mixed with 8 gram of lithium tetraborate 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. Thin sections were prepared at the University of Jordan and petrographically investigated via a polarizing microscope with different magnifications.

4. Result4.1. Petrography and Mineralogy

The volcanic rocks of central Jordan are mainly composed of cinder cones, scoria and basaltic flows. The basaltic rocks in hand specimen are black to grey in color and fine-grained. The melanocratic rocks typically show porphyritic and trachytic texture and are characterized by olivine, augite and plagioclase phenocrysts embedded in a fine-grained groundmass that mainly consists of plagioclase, olivine, augite and glass. The average modal composition is 58 vol.% plagioclase 21 vol.% olivine, 16 vol.% clinopyroxene and 5 vol.% accessory minerals and glass.

Plagioclase occurs in tow generation as up to (>3) mm long hypidiomorphic laths and fine crystals in the groundmass. The sub-hedral plagioclase laths have compositions with 45 to 55 vol.%, indicating labradorite to bytownite composition. These were documented after [21] ternary for plagioclase diagram, all the samples sent within labradorite to bytownite field (Figure 2).

The olivine occurs as crystals are unhedral to sub-hedral, fractured, mostly unaltered and reach lengths of 2 mm and in the groundmass crystals. They are colorless to pale yellow-green. A few exceptions exhibit resorbed margins, which can be partly or completely replaced by iddingsite and chlorite. The olivine crystals are typically Magnesian in the basalt with a forsterite component.

The pyroxene (augite) crystals are colorless or pale brown to pale green, 0.5 to 4 mm in length. Perfect two set cleavage which intersected at ~90˚ in the cross-section. The pyroxene crystals had an inclined extinction between 43˚ and 48˚, indicating the presence of clinopyroxene of augite. The groundmass augite < 0.3 mm. Small amounts of this augite are affected by chloritzation where green chlorite is present along fractures and crystal rims. The classification of pyroxene after [22] diagram, the samples plotted within augite field Figure 3. Accessory minerals include apatite as minute needles and opaque phases, which were

identified as magnetite, ilmenite and spinel. These minerals generally make up about 5 vol.% of the basalt.

4.2. Geochemistry

Fifteen samples of Pleistocene alkali basalts from central Jordan have been analyzed for major, minor, and trace elements. Representative results are given in Table 1. The SiO₂ values range between 46.11 and 49.56 wt% within an average (47.86 wt%), which is within the average value reported for alkali basalt and basanite by many authors [2] and [23] and it can be classified as basalt using the Total Alkalis-Silica classification scheme [23] [25] (Figure 4(a) and Figure 4(b)). The alkalis vs. silica in the [26] diagram, shows that all the rock samples

Table 1 Chemical analyses of Atarous Basalt Rock Sample study

Sample No	AT1	AT2	AT3	AT4	AT5	AT6	AT7	AT8	AT9	AT10	AT11	AT12	AT13	AT14	AT15
Si0₂ wt%	47.51	46.5	46.42	47.49	48.17	49.21	48.81	46.8	47.95	49.56	46.11	48.92	47.62	49.31	47.55
Ti0₂	1.66	1.67	2.89	1.71	1.4	1.48	1.43	1.87	1.98	1.54	1.89	1.6	1.55	1.42	1.62
AI₂0₃	14.58	13.4	13.73	14.92	15.27	15.36	14.87	15.5	15.93	15.11	15.12	14.44	14.62	14.2	14.75
Fe₂0₃	3.16	3.17	4.39	3.71	2.9	2.98	2.93	3.37	3.48	2.87	3.72	3.08	2.92	3.11	2.97
FeO	9.12	8.82	8.41	8.09	9.01	9.05	8.54	8.79	7.67	9.65	9.08	9.25	9.66	9.17	9.31
MnO	0.21	0.19	0.21	0.25	0.2	0.19	0.26	0.22	0.2	0.21	0.22	0.23	0.21	0.22	0.21
MgO	8.75	8.35	7.92	6.95	7.16	6.96	6.08	6.95	6.24	8.94	8.08	7.95	9.15	9.72	9.27
CaO	9.49	11.9	9.86	12.24	10.1	9.89	12.47	11.6	11.47	7.48	10.5	8.78	8.83	7.48	9.56
Na₂0	3.46	3.02	3.36	2.8	2.93	2.91	2.52	2.21	2.74	1.83	2.75	3.22	2.95	3.11	2.92
K₂0	0.8	0.75	1.43	0.63	0.65	0.65	0.64	0.68	0.87	0.87	0.84	0.87	0.81	0.79	0.82
P₂0₃	0.38	0.51	0.28	0.23	0.53	0.2	0.23	0.22	0.3	0.35	0.42	0.45	0.31	0.3	0.29
Sum	99.12	98.2	98.9	99.02	98.32	98.88	98.78	98.2	98.83	98.41	98.73	98.79	98.63	98.83	99.27
LOI	0.88	1.79	1.1	0.98	1.68	1.12	1.22	1.78	1.17	1.59	1.27	1.21	1.37	1.17	0.73
Mg#	0.49	0.49	0.49	0.45	0.44	0.44	0.42	0.44	0.45	0.42	0.39	0.39	0.42	0.44	0.43
Trace Elements (ppm)
Sr	4350	5500	365	345	365	355	3750	425	375	380	375	360	365	392	325
Zr	95	115	90	60	80	80	145	80	70	85	94	105	100	75	109
Ni	160	164	143	108	115	106	106	106	73	142	155	150	162	168	157
Cr	131 .00	154	130	120	124	109	125	129	106	137	125	162	138	152	129
Pb	-	95	100	55	15	75	63	80	55	60	82	94	42	65	30
Ba	140	125	195	130	75	80	130	140	265	54	65	42	40	35	75
Rb	8	10	12	14	9	11	15	10	12	8	10	11	16	9	7
Nb	22	26	19	40	20	24	26	10	13	25	23	16	18	12	15
Y	16	22	18	26	15	19	16	15	11	17	23	16	18	12	15
Ce	45	70	66	55	46	61	66	47	25	25	31	34	22	46	35
CIPW Norms
Or	4.71	4.47	8.48	3.74	3.86	3.85	3.8	4.05	5.15	5.112	5.04	4.11	4.95	5.62	4.66
Ab	25.49	18.6	21.08	22.4	24.94	24.65	21.4	18.9	23.23	23.44	20.15	20.75	22.7	23.37	25.93
An	21.81	20.9	18.23	20.43	26.75	26.96	27.48	30.5	28.68	26.62	21.3	28.87	24.7	24.64	21.95
Ne	1.99	3.85	4.04	0.77	0	0	0	0	0	0.53	3.2	3.15	3.41	0	3.55
Wo	9.45	14.6	12.12	13.83	8.42	8.71	13.83	11	11.03	9.08	10.8	4.2	8.65	4.65	8.27
En	5.78	9.04	8.14	8.34	10.4	12.55	12.02	11.7	9.76	5.39	6.35	18.6	6.04	11.04	8.21
Fa	3.13	4.74	3.07	4.75	7.12	8.73	9.03	7.19	5.22	3.14	3.41	10.2	3.22	6.22	4.42
Fo	11.16	8.71	8.17	6.35	5.28	3.38	2.23	4.06	4.08	12.1	10.66	11.5	11.36	10.17	10.15
Fs	6.65	5.04	3.39	3.96	3.99	2.59	1.85	2.76	2.41	7.42	6.21	6.09	7.45	6.18	6.17
Mt	4.57	4.63	6.39	4.68	4.25	4.33	4.26	4.93	3.05	4.32	4.6	4.12	4.11	4.32	4.68
Il	3.14	3.2	5.51	3.27	2.67	2.81	2.73	3.58	3.77	2.65	3.11	3.08	2.66	3.11	3.12
Ap	0.9	1.22	0.67	0.55	1.26	0.47	0.55	0.33	0.71	0.75	1.05	0.81	0.75	0.72	0.52

Or: orthoclase, Ab: albite, An: anorthite, Ne: nepheline, Wo: wollastinite, En: ensitite, Fa: fayllite, Fo: forsterite, Fs: feroslite, Mt: magnetite, Il: ilmenite, Ap: apatite.

study can be plotted into the alkaline to the sub-alkaline field (Figure 5(a)). The AFM variation diagram of Figure 5(b) indicates that the compositions of the basaltic rock sample study fall into the tholeiitic to Calc-Alkaline field [26] . According to [27] , Zr/TiO₂ verses Nb/Y diagram are used for classification, with the AB rock samples plotted within alkaline basalt (Figure 5(c)).

The data for Al₂O₃, TiO₂, P₂O₅, FeO + Fe₂O₃, and CaO range between 13.4 and 16.4 wt%, 0.2 to 0.6 wt%, 11.1 to 13.0 wt%, and 7.1 to 12.5 wt%, respectively. A correlation with the determined SiO₂ content is only discernable for Al₂O_3, shows an increase of Al₂O₃ with increasing SiO₂ (Figure 6(a)). The binary plot of SiO₂ versus TiO₂, P₂O_5, FeO + Fe₂O₃ and CaO exhibits the inverse relationships between both oxides and SiO₂ (Figures 6(b)-(e)). The result is documented within Bowens Series for segregation of the minerals crystallization with basic to acidic type.

The MgO content of the AB ranged from 6.08 wt% to 9.72 wt% with an average of 7.89 wt%. The Mg number (Mg≠) is defined as the molecular proportion of Mg-values = (Mg/Mg + Fe²⁺) [28] . Mg# petrogenetic indicator is for magma fractionation and its primitive volcanic rocks [29] . The AB exhibited a high Mg≠, ranging between 0.34 and 0.49, with an average of 0.44. The Mg# of the AVB indicates evolved to moderately basalt. Mg# increases with decreasing SiO₂ (Figure 6(f)). This general trend suggests that fractional crystallization probably decreasing Mg-number as a function of increasing SiO₂ [7] .

The determined major and minor element concentrations were also used to

calculate the CIPW norm (Table 1). Normative anorthite (An) and albite (Ab) in which An is higher than Ab indicated the plagioclase calc alkali nature of these rocks. Apatite and nepheline are present in low percentage. The Ab-An-Or diagram of Figure 7(a), shows the majority of samples reflect the sodic affinity of the rocks. According to [30] , diagram Na₂O verses K₂O, all the samples were plotted within sodic series (Figure 7(b)). Normative apatite and nepheline contents are below 1.3% and 4.7%, respectively. The latter content is, however, often zero. As the FeO + Fe₂O₃ show scatter in a plot versus SiO₂ Figure 6(d), this could reflect a decreasing degree of partial melting of a relatively homogenous source.

The chemical analysis of Atarous Basalt samples was found to have a high content of Cr and Ni (Table 1). The Cr content varied between 106 and 162 ppm, with an average value of 131.73 ppm. The Ni content ranges between 73 and 168 ppm with an average of 132.71 ppm, suggesting AB fractionation by the presence of olivine and clinopyroxene [31] . The high concentration of Cr and Ni indicated that the parental magma had been derived through partial melting of peridotite mantle source [2] and [7] . The binary diagram (Figure 8) shows the Mg# versus Cr and Ni. The general trend is a decrease of Cr and Ni with increasing Mg#; this result is documented with Zarqa-Ma’in basalt, Ar-Rabba Basalt and Mudawwara-Quwayra Basaltic Dike [32] [33] [34] . These results were documented with [7] , for the crustal mixing and assimilation of magma of the country rocks and dilution of Cr and Ni.

The contents of Sr, Zr, Pb and Ba range between 325 to 5500 with an average of 1403 ppm; 60 to 145 ppm, average 93.41; 15 to 100 ppm, average 64.12; and 35 to 265 ppm with an average of 111.23, respectively.

The Rare Earth Elements (REE) concentration includes Rb, Nb, Y, Ce and Sc and have low scattering around 7 to 16 ppm with an average of 10.88; 10 to 40 ppm with an average of 21.12; 11 to 26 with an average of 17.41; 22 to 70 ppm an average of 45; and 17 to 33 ppm with an average of 24.75, respectively (Table 1). The average ratio between Zr/Nb = 4.93 Zr/Y = 5.58 and Y/Nb = 0.91. This ratio was documented by [34] [35] , reported for the intercontinental alkali basalt. On

the other hand, Ti-Zr-Sr diagram shows all the study samples (AB) were plotted within the plate field basalt (Figure 9(a)) [36] . The Nb-Zr-Y diagram shows the AB samples plotted within the alkali basalt field (Figure 9(b)) [37] . The Ti-Zr-Y diagram shows all the study samples plotted within Calk alkaline basalt field (Figure 9(c)) [38] .

The geochemical information for major and trace elements are used to explain the natural source of AB, and it can be used to explain the mantle sources of partial melting. This indicates by using trace element ratios, such as Zr/Nb (average 4.93) and K/Ba (average 0.011) ratios [39] . The high content of Zr/Y (average 5.58) and TiO₂/Y (average 1.92) ratios and low content of Y (average 17.41 ppm) indicate that to the garnet-bearing source rocks [40] . The spider diagram for Rock Primordial mantle for the studied volcanic rock samples (AB) (Figure 10) presented enrichment of the incompatible LILE such as Ba and K, depletion of Nb relatively to K, and enrichment Nb and Ce and depletion with Y. The mafic volcanic AB exhibited positive Nb, Ce and Ti anomalies. The negative anomalies of Ba, Sr, 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 [41] . The Rock Primordial mantle value of the rock (Figure 10) showed a positive Nb peak, which conforms to the tertiary to recent continental alkali basalt provinces [42] [43] [44] and indicates that the AB is the product of lithosphere from upwelling asthenosphere mantle [23] [29] .

5. Discussion

The studied basalts (AB) are alkaline to sub-alkaline with respect to silica content and often SiO₂-undersaturated. Similar rock compositions were reported by [18] [19] [20] [23] [46] [47] from NE and central Jordan. The Arabia lithospheric mantle beneath Jordan is chemically and isotopically heterogeneous. According to [48] , it is possible that the volcanic rock was sourced from lower lithosphere depth. Cenozoic interpalate volcanic fields throughout Arabia may be the product the melting of upper mantle wedge material fertilized during Pan-African subduction and incorporated into the Arabian Lithospheric mantle [48] . The primary alkali basalt 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 [49]

[50] . The alkali basalt melts can be derived in the low-velocity zonation approximate depths of 85 - 95 km, 30 kbar by about 5% partial melting and by about 10% in the Lithosphere, at 60 - 90 km and 19 - 27 kbar [51] . Basalt may be both direct products of mantle partial melting and the differentiates of more primitive picritic partial melts [7] . However, the Mg-values (Mg/Mg + Fe²⁺) ranging from 0.39 to 0.49 (Table 1) could point to little fractional crystallization and removal of olivine and pyroxene. Nickel and Cr vary between 73 - 168 ppm and 106 - 162 ppm, respectively. These concentrations also suggest some degree of olivine fractionation, which tends to increase the incompatible trace element concentration in the studied basalts. The basalt of Al-Qiranha volcano in central Jordan is indicative of a primitive upper mantle that has suffered partial melting at a temperature ranging between 1050˚C and 1210˚C and pressure 15 - 20 kbar [18] . Based on the pre-mentioned information [52] that the recent basalt of Ethiopian rift was produced as a small degree partial melting peridotite of 15 - 25 kbarm, [53] also suggested that the basalts from central France, which are similar in their mineralogy to those of central Jordan volcano, were produced by partial melting of spinel lherzolite at 16 - 20 kbar pressure. The geochemistry of alkaline basalt indicates a source for intraplate volcanism [48] . The Ti richness could be attributed to low degrees of melting of peridotite source [54] . The basalt flow from Ar-Rabba, the main Ash-Shamaliyya area of central and northwest Jordan, is produced within the intraplate to continental calc-alkaline to alkali basalt [32] [33] .

Seismic and gravity data indicate that the crust below this field is about 35 km [55] . The source of Arabian intraplate basalt, suggesting that the numerous Cenozoic intraplate volcanic fields throughout Arabia may be the product of melting upper mantle wedge material fertilized during Pan-African subduction and incorporated into the Arabian, Lithospheric mantle [48] and [56] .

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. The investigated volcano resulted from magma rich in volatile constituents lost explosively from a central vent like an eruption, and the magma reflects the presence of spinel lherzolite nodules present in the same area that did not equilibrate with the melt, indicating that the transport from the upper mantle to the surface was rapid. Thus, the consideration of trace elements and mantle xenoliths support the concept that lava from central Jordan (include Atarous Basalt) has been derived from the upper mantle with a low degree of melting < 15%.

6. Conclusions

The Atarous Basalt (AB) was introduced within Miocene to Pleistocene volcanism at central Jordan. It is produced within intraplate to continental alkali basalt to calc-alkaline. The samples study covered Atarous Volcanic Basalt flow about 8 km². The following is the conclusion of the present study:

1) The mineral composition of AB is as follows: plagioclase, pyroxene (augite), olivine, secondary minerals such as iddingsite and chlorite by alteration of olivine and pyroxene (chlorination). Accessory minerals include apatite and opaque minerals, magnetite, ilmenite and spinel. The texture observed porphyritic and trachytic texture.

2) The chemical classification of AB had Alkaline to calc-alkaline basalt and includes sodic series.

3) The tectonic setting for the discrimination diagram showed that the AB samples in the study were plotted within plate basalt, alkali basalt and Calc-alkaline basaltic field.

4) The spider diagram for Rock Primordial mantle for the studied volcanic rock samples (AB) shows enrichment of the incompatible LILE such as Ba and K, and depletion of Nb relatively to K, and enrichment Nb and Ce and depletion of Y.

5) The mafic volcanic rocks of AB exhibited positive Nb and Ce anomalies, and negative anomalies of Ba, Sr, P, and Ti may be attributed to the fractionation of feldspar for Ba and Sr depletion apatite for P depletion.

6) The Spider diagram for Rock Primordial mantle for the rock sample study showed a positive Nb peak, which conforms to recent continental alkali basalt provinces; these indicates to the AB produced of lithosphere from upwelling asthenosphere mantle.

Acknowledgements

The author is thankful to the laboratory of the University of Stuttgart, Germany, for help with analysis of major and trace elements using X-Ray Fluorescence Spectrometry (XRF) at the Department of Geology. The author is also grateful to Jordan University, geology department for help with the preparation of thin sections.

Conflicts of Interest

The authors declare no conflicts of interest regarding the publication of this paper.

Cite this paper

Al-Fugha, H. and Yaseen, I.A.A.B. (2019) Petrography, Geochemistry and Petrogensis of Pleistocene Basaltic Flow from Northwest Atarous Area, Central Jordan. International Journal of Geosciences, 10, 613-631. https://doi.org/10.4236/ijg.2019.106035

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