GEOLOGICAL, STRUCTURAL AND PETROTECTONICAL ASPECTABLE FEATURES OF NEOPROTEROZOIC ROCKS, GABAL EL DOB AREA, NORTH EASTERN DESERT, EGYPT

International Journal of Scientific Engineering and Applied Science (IJSEAS) - Volume-1, Issue-8, November 2015 ISSN: 2395-3470 www.ijseas.com

GEOLOGICAL, STRUCTURAL AND PETROTECTONICAL ASPECTABLE FEATURES OF NEOPROTEROZOIC ROCKS, GABAL EL DOB AREA, NORTH EASTERN DESERT, EGYPT Ibrahim Abu El-Leil1, Mahmoud H. Bekhit1, Abdellah S. Tolba1, Ashraf F. Moharem2 and Taher M. Shahin1 1) Geology Department, Faculty of Science, Al-Azhar University, PO Box 11884, Nasr City, Cairo, Egypt. 2) Nuclear Materials Authority, P.O. Box 530, El-Maadi, Cairo, Egypt.

ABSTRACT Gabal El Dob area is covered by oceanic terrain related rocks, synextensional and late to post magmatic rocks. The oceanic terrain related rocks are represented by metavolcanoclastic and metavolcanic rocks. The synextensional magmatism is represented by tonalite-granodiorite rocks. The late to post magmatism is represented by gabbro, monzogranite, alkali feldspar granite and rhyolite porphyry in addition to different dikes. Structurally the area had been affected by compressional and extensional deformations. The compressional deformation is represented by folding, thrusting and schistosity. The extensional deformation is represented by normal and strike-slip faults, joints, dikes and drainage patterns. Geochemical affinity and petrotectonic features suggest calc-alkaline and tholeiitic island-arc series of the metavolcanoclastic and metavolcanic rocks. The gabbro has calc-alkaline and tholeiitic affinity of arc-volcanic origin. The granitic rocks are varying from calcalkaline (tonalite, granodiorite and monzogranite) to alkaline affinity (alkali feldspar granite). They are either related to I-type granite (tonalite, granodiorite and monzogranite) or within plate granite (alkali feldspar granite). The rhyolite porphyry is subalkaline rock, emplaced as within plate magma. Keywords: granites, structural, Neoproterozoic, Gabal El Dob, Eastern Desert, Egypt.

1. INTRODUCTION The area under study is situated in the northern part of the Eastern Desert of Egypt. It covers about 745 km2 of the crystalline basement rocks, between longitudes 33° 12ˋ and 33° 30ˋ and latitudes 26° 35ˋ and 26° 47ˋ (Fig. 1). The area is characterized by low to relatively high topography reliefs varying from 500 to 989 m above sea level. It forms a part of Neoproterozoic evolution of the North Arabian–Nubian Shield (NANS) as results of accretion plateaus in the course of consolidation of the Gondwana (Gass, 1982; Stern, 1994; Kröner et al., 1994; Abdelsalam and Stern.1996). A generalized picture shows that the final configuration of greater Gondwana, resulted from the collision and amalgamation of the Arabian–Nubian Shield (ANS) arc terrains with the Sahara and Congo–Tanzania Cratons to the west and Azania and Afif terrains to the east, constituting one of more continented blocks between the Indian Shield and Congo–Tanzania–Bangwenla Craton (Collines and Pisarrisky, 2005). The area under investigation had been subjected to different studies since Hume (1935); Schürman (1966) and Sabet et al., (1972). Moreover, El Gaby (1983) proposed the presence of an oblique NE thrust with dextral component along NED/CED margin that cased the uplifting of NED in relation to CED. Abu El Ela (1996) considered Abu Zawal gabbroic intrusion to represent three stages of fraction crystallization from an island arc high alumina basaltic magma, derived from mantle source. Moreover, Abd El-wahed (2009) interpreted Wadi Fatira Shear Zone as a hot ductile transpressional shear zone, developed as result of oblique collision. On other 332

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hand, Khalaf (2010) believed that the Neoproterozoic volcanic and siliciclastic strata of Fatira area prove an example of subareial and submarine system. To fulfill the study, a new geological map at scale 1:40000 had been established, to show the relationship of different exposed rock units and structure pattern of the area under study (Fig. 2). More than 60 rock samples were collected and subjected to chemical analyses for major, trace and rare earth elements in Nuclear Materials Authority (NMA) of Egypt (Table 1 & 2).

Fig. 1: Location map of the study area. 2. GEOLOGICAL SETTING The exposed various rocks of Gabal El Dob area belong to the Northern part of Arabian–Nubian Shield (ANS) that began at ~ 870 Ma and established at ~ 620 Ma ago, when convergence between east and west Gondwana fragments closed Mozambique ocean along East African – Antarctic Orogen (EAAO), (Stern, 1994; Jacobs and Thomas, 2004). Gabal El Dob area represents a part of the northern Arabian–Nubian Shield, formed during second growth phase of EAO between ~ 760 and ~ 730 Ma, when Midyan – Eastern terrains were formed. The terrains subsequently collided and amalgamated with the earlier terrains along Yanbu – Onib – Sol 333

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Hamed – Gerf – Allaqi – Heaini sutures (Johnson et al., 2011). The resulting geologic entity is commonly referred to as the western arc or oceanic terrains of ANS (Stoester and Forst, 2006; Ali et al., 2009; Johnson et al., 2011). The western arc or oceanic terrain collided and amalgamated between 680 and 640 Ma with Afif and Tathlith terrains creating a neocontinental crustal block referred to as the proto – Arabian–Nubian Shield (pANS), (Johnson et al., 2011). Field observations show that the area under study is mainly covered by metamorphic and unmetamorphic rocks. The metamorphic rocks are represented by the metavolcanoclastic and metavolcanic rocs, while the unmetamorphic rocks comprise tonalite – granodiorite, gabbro, monzogranite, alkali feldspar granite and rhyolite porphyry in addition to various dikes of different composition. The examined metamorphic rocks (metavolcanoclastics and metavolcanics) represent a part of the older upper crust thrusted over the younger lower crust of high-grade metamorphic rocks (gneisses and migmatites). The juxtaposition of low grade metamorphic rocks of ophiolite and island arc sequence against the high grade gneiss along extensional shear suggests crustal – scale thinning by NW – SE extension accompanied by intense late to post magmatic activity (Blasband et al., 2000; Fowler and El Kalioubi, 2004; Fowler and Osman, 2009; Andresen et al., 2010). The investigated metavolcanoclastic and metavolcanics are thus related to the oceanic terrains of northwestern Arabian–Nubian Shield that had been colliged and amalgamed with ophiolite (arc – arc accretion), followed by the synextensional, late and post magmatism. The following is a full description of the study rocks according to above mentioned geologic phenomena. 2.1- OCEANIC TERRAIN RELATED ROCKS (ISLAND-ARC ASSEMBLAGE) The metavolcanoclastic and metavolcanic rocks are related to western arc of oceanic terrains (island arc assemblages) of ANS that collided and amalgamated between 680 and 640 Ma, creating neocontinental crustal block referred to as the proto – Arabian–Nubian Shield (pANS), (Johnson et al., 2011). These rocks were metamorphosed up to greenschist facies and folded forming up of major recumbent anticline, as well as they had been affected by thrust movements, which the older metavolcanoclastics thrusted over the younger metavolcanics, (Fig. 2) during the collision stage (amalgamation).

Fig. 2: Geologic map of Gabal El Dob area.

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The metavolcanoclastics are situated at the western part of the mapped area, between Wadi Fatira El Beida and Wadi Abu Zawal, forming up two successive members of metarhyolite and metaandesite tuffs. The metarhyolite tuff is shown as alternated white and dark thin layers of ribbon shape to suggest marine environment (Fig. 3). This member becomes more vertical and steep due to Abu Zawal fault action. On other hand the metaandesite tuff is represented by highly schistose rocks, structurally overlaying by the metarhyolite tuff member. Generally the schistosity has often NE and NW trend (Fig. 4). The metavolcanoclastics (particular the metarhyolite tuff) are often associated with some banded iron formation (BIF), coinciding generally with the main trend of schistosity. The metavolcanic formation covers relatively wide area at the western part of the mapped area extending from Gabal Hadrabiya at the south to Wadi Fatira El Beida at the north, forming up the two limbs of the recumbent plunging anticline (Fig. 2).Generally, the metavolcanics are represented by NE and NW sheeted rocks of composition varying from metaandesite to metadacite. 2.2- SYNEXTENSIONAL TONALITE-GRANODIORITE The synextensional magmatism is represented by tonalite – granodiorite association. These rocks cover most all the eastern part of the mapped area. Generally, the two rock units are mixed with each other however, the content of the granodiorite increases toward the west and the tonalite to the east. However, the tonalite extend farther to the east to represent the western part of Barud tonalite (Barud Gneisses of Hume, 1935) that forms a huge batholithic mass extending across the entire with NED, west of Safaga (Fowler et al., 2006). The batholith margins are clearly discordant to the foliation trend of the Abu Furad amphibolites and cut across the contacts between the amphibolites, the metagabbro – diorite complex and Abu Marawat metavolcanics (Abu ElLeil et al., 2003; Folwer et al., 2006). The features of this batholith are consistent with it being an entirely intrusive igneous body and not as an autochthonous granitoids detected from the remobilized Pre- Pan-African basement as proposed by Akaad et al., (1973), El Gaby and Habib (1980, 1982); Habib (1987, a, b); El Gaby et al., (1988), El Gaby (1994) and El- Shazly and El-Sayed (2000). Generally, the tonalite-granodiorite had been formed by insitu melting at the present crustal level of the NED and intruded along its pre-existing NE trending shear zone (Abd El-Wahed and Abu Anbar, 2009) at depth about ~ 9km (Helmy et al., 2004). The tonalite-granodiorite rocks are medium to coarse - grained, with predominant xenoliths and alignment of mafic minerals forming gneissose texture. They are highly jointed and cross – cut by the monzogranite and the alkali feldspar granite of Gabal El Urf - Abu Shihat pluton (Fig. 5), as well as, they are invaded by some dikes and gold bearing quartz veins (Abu Zawal Gold Mine). On the other hand, they intrude directly the metavolcanic sequence of Gabal Hadrabiya (Fig. 6). 2.3- LATE TO POST MAGMATISM The late to post magmatic stage comprises igneous activity emplaced during the late Cryogenian – Ediacaran evolution of the ANS included both intrusive and extrusive events (Johnson et al., 2011). The particular feature of the ANS is an abundant of A-type granite, with addition to sills, dikes and stocks. The general features of plutons indicate typically discordant with respect to already deformed and metamorphosed country rocks, these rocks had been emplaced at late – to post amalgmation stage (arc – arc accretion) either as plutonic rocks represented by gabbro, monzogranite and alkali feldspar granite, or as terrestrial post amalgamed volcanic basins represented by rhyolite porphyry. The late Cryogenian – Ediacaran gabbro in the ANS comprises the layered and unlayered gabbro with age ranging from ~ 640 Ma to 540 Ma (Augland et al., 2011).The gabbro under study is represented by three small masses at the west of Gabal El Urf (Fig. 2), with relatively low–moderate relief of NE and NS trend. The gabbro is unlayered medium to coarse-grained, dark greyish to dark greenish color and composition varying from leucogabbro to pyroxene hornblende gabbro. It is directly cross-cut by the monzogranite and the alkali feldspar granite.

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Fig.3: Photograph showing the metavolcanoclastics with alternated white and black thin layers at Wadi Abu Zawal.

Fig. 4: Photograph showing well-developed schistosity of the metavolcanoclastics at Wadi Abu Zawal.

AG

M G G

Fig. 5: Photograph showing the sharp contact between the granodiorite (G) and alkali feldspar granite (AG) of Gabal Abu Shihat.

Fig. 6: Photograph showing the sharp contact between the metavolcanics (M) and granodiorite (G) at Gabal Hadrabiya.

B

V

G M

Fig. 7: Photograph showing the exfoliation and onion like shape in the monzogranite at Wadi Abu Zawal.

Fig. 8: Photograph showing the curved basalt dike (B) cut through the monzogranite (G) at Wadi Abu Zawal.

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The monzogranite was mapped as intrusive adamellite (Sabet et al., 1972). Field study and mineral composition suggest monzogranite composition. It intrudes directly the tonalite – granodiorite, gabbro and metavolcanics. It covers a relatively vast area, forming low to moderate reliefs traversed by abundant NE dikes and faults. Along Wadi Abu Zawal and El Dob, it is affected by E-W left lateral strike – slip movement. It is jointed and weathered; exfoliation and onion like shape are common (Fig. 7). Alkali feldspar granite constitutes an elongated NE belt extending from Wadi El Dob in the north (Gabal El Urf) to Wadi Um Taghir at the south. It is characterized by relatively high topographic relief up to ~ 989 m above sea level and represents the latter puls of the granitic magma. Evidence of this: (1) It invades directly the tonalite – granodiorite, the gabbro and the monzogranite (2) It has NE trend coinciding with the main structure features (3) It is nearly devoid of dikes. (4) It is only affected by the younger E-W strike – slip sinisteral movement that displaced the northern part of Gabal El Urf ~ 1.5 km to the west (Fig. 2). The rhyolite porphyry emplaced the area as post amalgamation volcanic basins activity referred to as Dokhan volcanic in the Eastern Desert. The volcanic rocks of this event as other parts of the northwestern part of the ANS are terrestrial volcanic, suggesting a location more elevated and/or farther for from the sea, (marine basin in the east of ANS). They are of Ediacaran age erupted between ~ 630 and ~ 592 Ma (Stern, 1979; AbdelRahman and Doig, 1987; Stern and Hudge, 1985, Wilde and Youssef, 2000). Generally, they show affinity of calc-alkaline subduction-related rocks. However, their undeformed character, their temporal and spatial association with post-tectonic A-type granite suggest emplacement following the cessation of subduction in an extensional within plate setting (Mohamed et al., 2000). The investigated rhyolite porphyry was considered as anorogenic volcanic rock, quite comparable with the Feirani volcanics in southern Sinai (Abu El-Leil and El Gamal, 1991; Abu El-Leil et al., 1991; Khalaf, 2010). The rhyolite porphyry is situated at the western side of the mapped area, exhibiting the same general characteristic features of the anorogenic Ediacaran extrusion (~ 630 and ~ 592 Ma) in ANS. It forms an elongated NE discordant belt with surrounding metavolcanoclastic and tonalite – granodiorite rocks, as well as it is devoid of dikes, coinciding well with the main characteristic features of the anorogenic alkali feldspar granite. Most of the study rock unites are traversed by NE basic, intermediate and acidic dikes. The less have NW trend, and occur as tilted dikes due to E-W left lateral action affected the anorogenic alkali feldspar granite (Fig. 8) 3- STRUCTURE PATTERNS The structure features due action of compressional and extensional forces such as; folding, thrusting, faulting, jointing, trending of dikes, schistosity and drainage pattern are discussed. 3.1- COMPRESSIONAL FEATURES The compressional action of the arc – arc accretion phase had been affected throughout the Arabian – Nubian Shield at 750 – 650 Ma. Folding, thrusting and schistosity are the main accretion phase in the study area. Folding is recorded as a major recumbent anticline, formed by highly schistose metavolcanoclastics and metavolcanics at the western side of the area. The western closure is plunging to NW and NE at an average angle of 50° and 40° respectively, and E – W axial plane to indicate N – S compressional action (arc – arc accretion) subjected the area. Thrusting had been affected the western sides of the area after action of folding, due to NE – SW compressional action, where the older metavolcanoclastics thrusted over the younger metavolcanics. Along the thrust zone, the rocks are highly deformed and associated with cataclastic fragments. The schistosity (S1) is a common feature in the metavolcanoclastic and the metavolcanic rocks, essentially NE and NW trends. Primary layering and sheeting (S0) are less common, particular in the metavolcanoclastic rocks (Fig. 2).

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Fig. 9: Shaded relief image created by combining shaded relief images sun angles of 0°, 45°, 90°, 135°, 180°, 225°, 270° and 315°.

Fig. 10: Automatic lineament map of combining shaded relief images sun angles of 0°, 45°, 90°, 135°, 180°, 225°, 270° and 315°.

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3.2- EXTENSIONAL FEATURES The extensional features comprise all the lineamental elements, such as faults, joints, dikes and drainage patterns. The lineamental identification has been interpreted either in the field or using Digital Elevation Modal (DEM), of which eight-shaded reliefs of image are generated (Lattman and Nickelsen, 1958; Clark and Wilson, 1994; Hung, 2005). The combination of eight shaded relief images are computed using GIS overlay technique, to produce one image with multi – illumination direction (0°, 45°, 90°, 135°, 180°, 225°, 270° ad 315°) (Fig. 9). This image has been used for automatic extraction lineaments over the study area, by using algorithms and computer software (e.g., Costa and Sturkey, 2001; Kim et al., 2004; Hung el al., 2005; Abdullah et al., 2009; Abdullah et al., 2010 and Zohier and Emam, 2013). In this study, PIC Geomatica software is used. The recorded lineamental analysis show one common NE trend affected throughout the area (Fig. 10), coinciding well with Qena – Safaga shear zone trend, of about 50 km wide and more dipping steeply northward (El Gaby, 1983). Two types of faults have are recorded; the normal faults and strike slip faults. The normal faults are abundant in NE trend and less common in NW. They are accompanied by linear displacement of dikes, shearing and alignment of the drainage patterns. On other hand, the left lateral strike – slip movement, affected throughout the northeastern part of the area, where the northern part of Gabal El Urf alkali feldspar granite pluton, displaced laterally by about 1.5 km to west (Fig. 2). Many features are shown as tilting of dikes, stretching of the mafic minerals and xenoliths, as well as shearing of the granites, to prove that E – W left lateral had been done after NE extensional movements ( normal faults). Due to tensional and shearing stresses acting on the rock masses many joints are developed. Generally, they are well recorded in the granitic rocks particular in NE, NNW, NW, SW and N-S trends. Dikes are widely distributed in NE trend, the less are in NNE and N-S trends, coinciding often with the main trend of structure elements. The drainage patterns are often structurally controlled. Most of them have NE trend as Wadi Fatira El Beida, Abu Zawal and El Dob (Fig. 2). 4- GEOCHEMICAL AFFINITY AND PETROTECTONIC BEHAVIOR The geochemical affinity and petrotectonic behavior are shown, based on 60 representative samples collected from different rock units and chemically analyzed in Egyptian Nuclear Materials Authority (Table 1 & 2). The results are discussed through many diagrams used for this purpose. The metavolcanoclastic and metavolcanic rocks have subalkaline nature according to SiO2-Na2O+K2O diagram (Irvine and Baragar, 1991) (Fig. 11). However they are varying from calc-alkaline to tholeiitic according to Zr-P2O5 diagram (Winchester and Floyed, 1976) (Fig. 12), and medium-K content on K2O-SiO2 diagram (Le Maitre, 1989) (Fig. 13). Following the proposed diagrams of Mullen (1983) and Floyed (1991). They are varying from island arc tholeiitic series to island arc calc-alkaline series (Figs. 14 & 15). The origin of island arc is improved also from the normalized N-MORB diagram of both metavolcanoclastics and metavolcanics displaying an enrichment of Rb to Y, with strong depletion of K and slight smooth decreasing from Nd to Y (Figs. 16 & 17). The chondrite normalized diagrams of rare earth elements (REE) exhibit as island arc pattern. They are enriched in (LREE) light rare earth elements (La-Sm), with relatively flatted pattern for (HREE) heavy rare earth elements (Th-Lu) with slightly positive Eu anomalies. The investigated gabbro is varying from calc-alkaline to tholeiitic affinity on AFM diagram (Irvin and Barragr, 1971) (Fig. 18) and Zr-P2O5 diagram (Winchester and Floyed, 1976) (Fig. 19). The normalized N-MORB diagram of the investigated gabbro has a spiked pattern closer match with volcanic-arc origin, which shows strong negative K anomaly and positive Sr anomaly (Fig. 20). On other hand, the chondrite-normalized REE diagram (Boynton, 1984) shows enrichment in La and moderate content of Ce to Sm, with clear strong depletion in Eu, followed by increasing of Gd to Lu (Fig. 21) The investigated granites are sub-alkaline according to TAS diagram (Fig. 22) of Irvin and Baragar (1971). However, they are varying from calc-alkaline (tonalite-granodiorite and monzogranite) to alkaline (alkali feldspar granite) according to alkalinity ration- SiO2 diagram (Fig. 23) of Whight (1969), as well as they 339

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are varying from metaluminous (tonalite- granodiorite and monzogranite) to peraluminous nature (Fig. 24) according to Maniar and Piccoli (1989). The plots of the investigated granitic rocks on R1-R2 diagram (Batchelor and Bowded, 1995) give more than tectonic setting of them. Both tonalite and granodiorite are related to post collision granite, the monzogranite is related to late orogenic granite and the alkali feldspar granite is related to anorogenic granite (Fig. 25). Moreover, on Rb - Y+Nb and Nb-Y diagrams, (Pearce et al., 1984), both tonalite and granodiorite are volcanic arc granite (VAG) and the monzogranite and alkali feldspar granite are within plate granite (WPG) (Fig. 26). However, they are varying from I-type granite (tonalite, granodiorite and monzogranite) to within plate granite (alkali feldspar granite) according to Chappell and White (1974) diagram (Fig. 27). The N-MDRB normalized diagram (Sund and Mc Donough, 1989) locks like as the pattern of the magmatic rocks formed on an active continental margin for the tonalite, granodiorite and monzogranite, (Fig. 28). However, the alkali feldspar granite behaves as within plate granite, which shows clear negative Sr anomaly (Maniar and Picoli, 1989; Eby, 1990; Abu El-Leil et al., 1995 & 2003). The normalized REE diagram (Boynton, 1984) shows two individual patterns, one for tonalite, granodiorite and monzogranite and other for alkali feldspar granite (Fig. 29) suggesting I-type origin for former and A-type origin for the latter. The investigated rhyolite porphyry has sub-alkaline affinity according to TAS diagram (Fig. 30) It was developed either at/or nearby destructive plate margin basalts (Fig. 31) (Wood, 1980). However, it was emplaced as within plate magma according to Pearce et al., (1984) diagram.

20

1.4

18

14 12

P2O5

Na2O+K2O

16

10 Alkaline

8

0.7

6 4 Subalkaline

2 0 35

0.0

40

45

50

55

60

65

70

75

80

85

0

200

400

600

Zr

SiO2

Fig. 11: TAS diagram for the investigated metavolcanoclastics and metavolcanics (Irvine and Baragar, 1971).

Fig. 12: P2O2-Zr diagram for the investigated metavolcanoclastics and metavolcanics (Winchester and Floyd, 1976).

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Table 1: Major oxides (wt %), trace elements (ppm) and rare earth elements (ppm) of the metavolcanoclastics, metavolcanics, gabbro and rhyolite porphyry. Metavolcanoclastics

Metavolcanics

Rock unite

Gabbro Metaandesite tuff

Sample

Metarhyolite tuff

Metaandesite

SiO2 TiO2 Al2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O P2O3 L.O.I. Total

9A 55.57 0.82 14.42 4.55 2.71 0.15 7.88 7.25 4 0.89 0.13 1.56 99.93

10A 56.62 0.71 13.97 4.49 2.67 0.17 7.51 7.20 4.09 0.82 0.11 1.60 99.96

12A 56 0.79 13.99 4 2.66 0.15 8 7.23 4 0.85 0.17 2.01 99.90

33A 71.38 0.09 13.81 0.93 2.51 0.07 0.83 1.85 4.22 3.07 0.10 1.04 99.90

34A 71.68 0.14 12.95 0.88 2.28 0.07 0.73 1.97 4.45 3.82 0.17 0.72 99.86

35A 71.26 0.17 14.02 1.07 2.09 0.06 0.64 2.01 4.32 3.17 0.18 0.19 99.90

50A 71.30 0.11 13.78 1.15 2.17 0.05 0.92 2 4.36 3.31 0.12 0.62 99.89

50B 72.42 0.09 13.12 1.04 2.25 0.06 0.68 1.79 4.29 2.98 0.10 1.11 99.93

4B 58.60 0.85 14.45 3.43 2.02 0.12 6.51 7 4.42 1.08 0.28 1.17 99.93

5B 58.76 0.89 14.31 3.26 2.04 0.14 6.43 6.99 4.58 1.15 0.21 0.99 99.75

Sr Rb Ba Ni Cr Y Zr Ta Nb Hf Co V Zn Cu Ga Pb U Th

251 32 223 36 146 21 117 4 5 32 178 43 17 3 12 -

244 28 210 41 159 20 126 4 7 35 170 45 20 3 16 -

300 41 199 52 139 16 117 4 5 40 178 43 21 3 18 1.5 4

142 98 398 19 238 3 52 25 41 77 20 35 8 16

136 102 445 18 217 3 55 20 50 18 18 33 8 16

141 110 453 47 230 3 62 19 24 42 36 17 9 17

152 115 452 40 244 8 63 18 30 39 14 17 10 17 152 115

118 113 441 36 205 3 60 21 41 35 18 20 9 16 118 113

205 36 223 33 144 27 121 3 5 24 168 45 19 8 20 -

211 40 230 29 136 22 119 3 4 21 174 39 15 9 28 -

La Ce Nd Sm Eu Gd Tb Er Yb Lu ∑REE

12 18 8 2 0.8 3.2 1 2.6 1.8 0.7 50.1

9 20 9 2.4 1 3.6 0.8 3 2 0.5 51.3

15 16 9 2.2 1.1 4 1.5 3 2.6 0.8 55.2

12 22 10 2 1 3.5 2 2 2.5 1 58

29 71 15 3 1.2 3.5 0.5 7 6 1.7 137.9

26 68 13 2.2 1 4 1 6.4 6 2 129.6

27 70 14 2 1.3 4 0.7 3 6 1.4 129.4

28 72 13 2 1 3 0.6 5 7 1.5 133.1

10 24 14 2 0.8 3 0.6 2 2 0.3 58.7

10 24 15 2 0.8 4 0.7 3 3 0.4 62.9

Rhyolite porphyry

Metadacite

7A 43 44B 56.50 55.08 66.90 0.73 0.74 0.23 13.84 15.66 14.57 4.49 4.49 1.29 2.77 2.97 1.71 0.17 0.17 0.15 7.86 6 1.23 7.17 7.32 5.54 4.08 3.08 4.05 0.80 0.72 2.78 0.12 0.11 0.12 1.42 2.47 1.31 99.95 99.82 99.88 Trace elements (ppm) 233 437 223 31 13 124 216 150 652 39 124 151 177 23 12 8 119 59 48 4 3 2 6 2 9 15 30 47 184 163 41 78 41 18 27 40 2 7 14 14 12 26 1 1.3 3 5 Rare earth elements (ppm) 10 10 26 26 25 62 10 8 26 2 1 7 0.8 0.7 2.5 3 2 12 0.7 0.6 2 2 1.7 4 2 2.6 3 0.2 0.5 1 56.7 52.1 144.5

341

44B 66.90 0.23 14.57 1.29 1.71 0.15 1.23 5.54 4.05 2.78 0.12 1.31 99.88

15B 50.37 1 16.04 4.68 3.01 0.17 8.52 9.51 4.23 0.52 0.10 1.67 99.82

16B 49.16 1 18.68 3.04 4.58 0.12 7.92 9.23 3.42 0.62 0.11 2.02 99.90

16D 48.15 1.18 17.54 3.11 4.86 0.15 8.30 10.08 3.13 0.84 0.18 2.45 99.97

17A 48.63 0.52 18.34 2.92 5.54 0.12 8.41 10.91 2.12 0.69 0.08 2.23 99.88

20A 49.20 0.15 17.31 2.55 5.09 0.13 9.68 10.34 2.75 0.54 0.05 2.18 99.97

21A 50.32 0.48 17.85 8.21 4.56 0.25 6.11 5.63 2.01 0.64 0.13 3.57 99.76

25B 50.35 0.65 16.96 7.74 5.12 0.22 6.50 6.12 2.15 0.81 0.07 3.28 99.97

10B 74.48 0.15 12.45 0.52 1.41 0.07 0.57 1.08 4.09 4.28 0.06 0.64 99.8

11B 74 0.1 12.49 0.79 1.38 0.06 0.6 1.05 4.08 4.32 0.12 0.86 99.85

12B 73.84 0.12 12.41 1.07 1.19 0.05 1.06 1.08 3.86 4.1 0.09 0.94 99.81

48 72 0.29 14 1.61 0.46 0.05 0.62 1.53 3.85 4.27 0.15 1.0 99.83

223 124 652 8 48 2 9 15 41 40 14 26 1.3 5

485 12 99 88 180 35 80 1 8

535 17 93 59 195 16 45 3 11

42 147 83 77 2 9 1 4

46 163 83 50 3 7 3 6

719 16 80 63 208 14 42 2 7 26 149 72 42 3 8 3 5 719

645 13 128 57 122 18 39 2 8 22 152 60 75 6 6 3 6

502 14 132 61 106 17 32 1 9 30 155 65 69 4 7 3 6

501 18 110 95 182 35 80 1 8 42 10 110 83 2 17 2 5

532 16 115 65 147 27 72 1 6 13 103 62 97 3 32 3 6

45 251 187 30 185 3 52 10 18 14 17 30 7 14

44 271 175 27 192 3 50 4 28 13 17 43 6 19

40 263 188 30 185 2 51 5 17 15 17 44 6 14

12. 79 427 28 255 3 49 20 35 71 20 42 14 19

27 61 28 7 3 10 2 5 3 1 147

7 8 8 1 0.4 2 0.4 2 2 0.3 31.1

6 8 8 2 0.4 2 0.4 2 2 0.5 31.3

8 9 7 2 0.4 3 0.4 2 3 0.6 35.4

7 8 7 2 0.5 3.2 0.5 3 3 0.7 34.9

7 8 8 2 0.6 3 0.6 3 3 0.6 35.8

7 7 7 3 0.5 3 0.5 3 3 0.5 34.5

7 8 7 2 0.6 3 0.6 2 3 0.4 33.6

46 63 14 4 4 21 4 2 2 2 162

42 55 15 3 4 30 7 2 2 3 163

51 52 18 4 4 24 6 2 2 2 165

46 49 11 4 3 33 7 3 3 2 161

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Table 2: Major oxides (wt %), trace elements (ppm) and rare earth elements (ppm) of the tonalite, granodiorite, monzogranite and alkali feldspar granite.

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TiO2 /10 TiO2

K2O

5

4

CAB =Calc-Alkaline Basalts IAT =Island Arc Tholeiites MOR=Mid-Ocean Ridge

3

Basalts OIA =Ocean

Island OIT OIT

2 MORB MORB IAT IAT

1

OIA OIA CAB CAB

0 40

50

60

70

80

MnO*10 MnO*10

SiO2

Fig. 14: MnO*10-P2O5*10-TiO2/10 diagram for the investigated metavolcanoclastics and metavolcanics (Mullen, 1983). S a m p le /N -T y p e M O R B

Fig. 13: SiO2-K2O diagram for the investigated metavolcanoclastics and metavolcanics (Le Maitre, 1989).

P2O5*10 P2O5*10

300 100 10 1 0.1 0.01 0.001 Rb Ba

Fig. 15: Zr vs. Ba diagram for the investigated metavolcanoclastics and metavolcanics (Floyed, 1991).

Nb La

Ce

Sr Nd Zr

Ti

Y

Fig. 16: Normalized spider diagram for the study metavolcanoclastics and metavolcanics to N-MORB (Sun and McDonough 1989). FeOt

60 40

S a m p le /C h o n d r ite

K

Tholeiitic

10 10

Calc-Alkali ne

86 La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu

Na2O+K2O

Fig. 17: Chondrite-normalized REE diagram for investigated metavolcanoclastics and metavolcanics rocks (Boynton, 1984).

343

MgO

Fig. 18: AFM diagram for the investigated gabbro (Irvine and Baragar, 1971).

S a m p le /N -T y p e M O R B

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Alka TH+

40 10

1

0.1

0.01

0.001 Rb Ba

Fig. 19: P2O2-Zr diagram for the investigated gabbro (Winchester and Floyd, 1976).

Nb La

Ce

Sr

Nd Zr

Ti

Y

Fig. 20: Normalized spider diagram for the investigated gabbro to N-MORB (Sun and McDonough 1989). 20

30

18 16

Na2O+K2O

S a m p le /C h o n d r ite

K

10

14 12 10 Alkaline

8 6 4

Subalkaline

2 0 35

40

45

50

55

60

65

70

75

80

85

4

SiO2

La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu

Fig. 23: Chondrite-normalized REE diagram for the investigated gabbro (Boynton, 1984).

Fig. 22: TAS diagram for the investigated granites (Irvine and Baragar, 1971).

Fig. 24: SiO2 versus alkalinity ratio (A.R.) diagram for the investigated granites (Wright, 1969).

Fig. 25: Maniar and Piccoli (1989) diagram for the investigated granites. A=Al2O3, C=CaO, N=Na2O and K=K2O.

Tonalite

Granodiorite

Monzogranite

Alkali feldspar granite 344

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2000 1000

Syn-C OLG

WP G

Rb

100

10

VAG

ORG

1 1

10

100

1000 2000

Y+Nb

Fig. 27: Rb vs. Y+Nb diagram for the investigated granites (Pearce et al., 1984). S a m p le /N -T y p e M O R B

Fig. 26: R1 – R2 binary diagram for the investigated granites (Batchelor and Bowden, 1985).

600 100 10 1 0.1 0.01 0.001 Rb Ba

Fig. 28: K2O-Na2O diagram for the investigated (Chappell and White, 1974). A-type field is after Liew et al., (1989).

Ti

Y

Fig. 29: Normalized spider diagram for the investigated granites to N-MORB (Sun and McDonough 1989). 20

80

18 16

Na2O+K2O

S a m p le /C h o n d r ite

K Nb La Ce Sr Nd Zr

14 12 10 Alkaline

8 6

10

4 Subalkaline

2 0

5 La

Pr Ce

Eu Nd

Sm

Tb Gd

Ho Dy

Tm Er

35

Lu

40

45

50

55

60

65

70

75

80

85

SiO2

Yb

Fig. 30: Chondrite-normalized REE diagram for the investigated granites (Boynton, 1984).

Fig. 25: TAS diagram for the study rhyolite porphyry (Irvine and Baragar, 1971).

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Hf/3

2000 1000

Syn-COLG

WPG

100 R b

A

B

10

D C

VAG

ORG

1 1

Th

Ta

10

100

1000 2000

Y+Nb

Fig. 26: Th-Ta-Hf/3 diagram for the study rhyolite porphyry (Wood 1980).

Fig. 27: Rb vs. Y+Nb diagram for the study rhyolite porphyry (Pearce et al., 1984).

CONCLUSIONS The study area forms a part of Neoproterozoic evolution of the North Arabian-Nubian Shield (NANS) formed during second growth phase of East Africa Orogen (EAO) between ~760 and 730 Ma and related to the western arc or oceanic terrains of ANS. The exposed rocks of Gabal Dob area are related to oceanic terrain, extensional and late to post magmatism of the northwestern part of Arabian Nubian Shield. The oceanic terrains are represented by the metavolcanoclastic and metavolcanic rocks. The synextensional magmatism comprises tonalite and granodiorite. The late to post magmatism comprises gabbro, monzogranite and alkali granite. The metavolcanoclastics comprise two successive members of metarhyolite and metaandesite tuffs. The metarhyolite tuff is shown as alternated white and dark thin layers of ribbon shape suggest marine environment, often associated with banded iron formation (BIF). The metavolcanics are represented by metaandesite and metadacite rocks forming the two limbs of the recumbent plunging anticline. The synextensional tonalite and granodiorite represent the western part of Barud batholitic mass of features consistent with it being as entirely intrusive igneous body. The late post magmatic stage comprises igneous activity emplaced during late Cryogenian-Ediacaran evolution of ANS of both intrusive and extrusive events. The intrusive rocks are represented by gabbro, monzogranite and alkali feldspar granite, while the extrusive rocks are represented by terrestrial post amalgamed rhyolite porphyry. Structurally, the study area had been affected by compressional and extensional deformations. The compressional action (arc-arc accretion) phase at about 750-650 Ma affected throughout ANS and tracked the area, whereas such features as folding, thrusting and schistosity are recorded. Folding is recorded as major recumbent anticline plunging to NW and NE and E-W axial plane due to N-S arc-arc compressional accretion. Thrusting had been done after folding due to NE compressional action, whereas the older metavolcanoclastics thrusted over the younger metavolcanics. NE and NW trends of schistosity (S1) are common in the metavolcanoclastics while the primary layering and sheeting (S0) are less common. The extensional features comprise all the lineamental elements such as faults, joints, dikes and drainage patters. Automatic lineamental identification analyses shows one common NE trend affected throughout the 346

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area. Two types of faults are recorded; the normal and strike slip faults. The normal faults are abundant in NE trend. The E-W left strike-slip movement affected the area after the emplacement of the alkali granite and dikes. Due to tensional and shearing stresses acting on rock masses many joints are developed in NE, NNW, NW, and NS directions. Dikes preferred also NE trend coinciding with the main structure trend as well as the drainage patterns have the same NE trend. Chemical affinity and petrotectonic behavior of the metavolcanoclastics and metavolcanics are varying from island arc tholeiitic series to island arc calc-alkaline series. The investigated gabbro is varying from calcalkaline to tholeiitic affinity closer match with volcanic arc origin. The granitic rocks are varying from calcalkaline (tonalite, granodiorite and monzogranite) to alkaline (alkali feldspar granite). However, they are related to I-type granite (tonalite, granodiorite and monzogranite) and within plate granites (alkali feldspar granite). The rhyolite porphyry has sub-alkaline affinity, emplaced as within plate magma.

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