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

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GEOLOGICAL, STRUCTURAL AND PETROTECTONICAL

ASPECTABLE FEATURES OF NEOPROTEROZOIC

ROCKS, GABAL EL DOB AREA, NORTH EASTERN

DESERT, EGYPT

Ibrahim Abu El-Leil1, Mahmoud H. Bekhit

1, Abdellah S. Tolba

1, Ashraf F. Moharem

2 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 calc-

alkaline (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

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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



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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 El-

Leil 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.

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.

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.

M

V

G

AG

G

M

B

G



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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; Abdel-

Rahman 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



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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.

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).

0 200 400 6000.0

0.7

1.4

Zr

P2

O5

35 40 45 50 55 60 65 70 75 80 850

2

4

6

8

10

12

14

16

18

20

Alkaline

Subalkaline

SiO2

Na2O

+K

2O

35 40 45 50 55 60 65 70 75 80 850

2

4

6

8

10

12

14

16

18

20

Alkaline

Subalkaline

SiO2

Na2O

+K

2O



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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.

Rock unite Metavolcanoclastics Metavolcanics

Gabbro Rhyolite porphyry Metaandesite tuff Metarhyolite tuff Metaandesite Metadacite

Sample 9A 10A 12A 33A 34A 35A 50A 50B 4B 5B 7A 43 44B 44B 15B 16B 16D 17A 20A 21A 25B 10B 11B 12B 48

SiO2 55.57 56.62 56 71.38 71.68 71.26 71.30 72.42 58.60 58.76 56.50 55.08 66.90 66.90 50.37 49.16 48.15 48.63 49.20 50.32 50.35 74.48 74 73.84 72

TiO2 0.82 0.71 0.79 0.09 0.14 0.17 0.11 0.09 0.85 0.89 0.73 0.74 0.23 0.23 1 1 1.18 0.52 0.15 0.48 0.65 0.15 0.1 0.12 0.29

Al2O3 14.42 13.97 13.99 13.81 12.95 14.02 13.78 13.12 14.45 14.31 13.84 15.66 14.57 14.57 16.04 18.68 17.54 18.34 17.31 17.85 16.96 12.45 12.49 12.41 14

Fe2O3 4.55 4.49 4 0.93 0.88 1.07 1.15 1.04 3.43 3.26 4.49 4.49 1.29 1.29 4.68 3.04 3.11 2.92 2.55 8.21 7.74 0.52 0.79 1.07 1.61

FeO 2.71 2.67 2.66 2.51 2.28 2.09 2.17 2.25 2.02 2.04 2.77 2.97 1.71 1.71 3.01 4.58 4.86 5.54 5.09 4.56 5.12 1.41 1.38 1.19 0.46

MnO 0.15 0.17 0.15 0.07 0.07 0.06 0.05 0.06 0.12 0.14 0.17 0.17 0.15 0.15 0.17 0.12 0.15 0.12 0.13 0.25 0.22 0.07 0.06 0.05 0.05

MgO 7.88 7.51 8 0.83 0.73 0.64 0.92 0.68 6.51 6.43 7.86 6 1.23 1.23 8.52 7.92 8.30 8.41 9.68 6.11 6.50 0.57 0.6 1.06 0.62

CaO 7.25 7.20 7.23 1.85 1.97 2.01 2 1.79 7 6.99 7.17 7.32 5.54 5.54 9.51 9.23 10.08 10.91 10.34 5.63 6.12 1.08 1.05 1.08 1.53

Na2O 4 4.09 4 4.22 4.45 4.32 4.36 4.29 4.42 4.58 4.08 3.08 4.05 4.05 4.23 3.42 3.13 2.12 2.75 2.01 2.15 4.09 4.08 3.86 3.85

K2O 0.89 0.82 0.85 3.07 3.82 3.17 3.31 2.98 1.08 1.15 0.80 0.72 2.78 2.78 0.52 0.62 0.84 0.69 0.54 0.64 0.81 4.28 4.32 4.1 4.27

P2O3 0.13 0.11 0.17 0.10 0.17 0.18 0.12 0.10 0.28 0.21 0.12 0.11 0.12 0.12 0.10 0.11 0.18 0.08 0.05 0.13 0.07 0.06 0.12 0.09 0.15

L.O.I. 1.56 1.60 2.01 1.04 0.72 0.19 0.62 1.11 1.17 0.99 1.42 2.47 1.31 1.31 1.67 2.02 2.45 2.23 2.18 3.57 3.28 0.64 0.86 0.94 1.0

Total 99.93 99.96 99.90 99.90 99.86 99.90 99.89 99.93 99.93 99.75 99.95 99.82 99.88 99.88 99.82 99.90 99.97 99.88 99.97 99.76 99.97 99.8 99.85 99.81 99.83

Trace elements (ppm)

Sr 251 244 300 142 136 141 152 118 205 211 233 437 223 223 485 535 719 645 502 501 532 45 44 40 12.

Rb 32 28 41 98 102 110 115 113 36 40 31 13 124 124 12 17 16 13 14 18 16 251 271 263 79

Ba 223 210 199 398 445 453 452 441 223 230 216 150 652 652 99 93 80 128 132 110 115 187 175 188 427

Ni 36 41 52 19 18 47 40 36 33 29 39 124 - - 88 59 63 57 61 95 65 - - - -

Cr 146 159 139 - - - - - 144 136 151 177 - - 180 195 208 122 106 182 147 - - - -

Y 21 20 16 - - - - - 27 22 23 12 8 8 35 16 14 18 17 35 27 30 27 30 28

Zr 117 126 117 238 217 230 244 205 121 119 119 59 48 48 80 45 42 39 32 80 72 185 192 185 255

Ta 4 4 4 3 3 3 8 3 3 3 4 3 2 2 1 3 2 2 1 1 1 3 3 2 3

Nb 5 7 5 52 55 62 63 60 5 4 6 2 9 9 8 11 7 8 9 8 6 52 50 51 49

Hf - - - 25 20 19 18 21 - - - - 15 15 26 - - - - 10 4 5 20

Co 32 35 40 - - - 30 41 24 21 30 47 - - 42 46 149 22 30 42 13 - - - -

V 178 170 178 - - - 39 35 168 174 184 163 - - 147 163 72 152 155 10 103 - - - -

Zn 43 45 43 41 50 24 14 18 45 39 41 78 41 41 83 83 42 60 65 110 62 18 28 17 35

Cu 17 20 21 77 18 42 17 20 19 15 18 27 40 40 77 50 3 75 69 83 97 14 13 15 71

Ga 3 3 3 20 18 36 10 9 8 9 2 7 14 14 2 3 8 6 4 2 3 17 17 17 20

Pb 12 16 18 35 33 17 17 16 20 28 14 12 26 26 9 7 3 6 7 17 32 30 43 44 42

U - - 1.5 8 8 9 152 118 - - - 1 1.3 1.3 1 3 5 3 3 2 3 7 6 6 14

Th - - 4 16 16 17 115 113 - - - 3 5 5 4 6 719 6 6 5 6 14 19 14 19

Rare earth elements (ppm)

La 12 9 15 12 29 26 27 28 10 10 10 10 26 27 7 6 8 7 7 7 7 46 42 51 46

Ce 18 20 16 22 71 68 70 72 24 24 26 25 62 61 8 8 9 8 8 7 8 63 55 52 49

Nd 8 9 9 10 15 13 14 13 14 15 10 8 26 28 8 8 7 7 8 7 7 14 15 18 11

Sm 2 2.4 2.2 2 3 2.2 2 2 2 2 2 1 7 7 1 2 2 2 2 3 2 4 3 4 4

Eu 0.8 1 1.1 1 1.2 1 1.3 1 0.8 0.8 0.8 0.7 2.5 3 0.4 0.4 0.4 0.5 0.6 0.5 0.6 4 4 4 3

Gd 3.2 3.6 4 3.5 3.5 4 4 3 3 4 3 2 12 10 2 2 3 3.2 3 3 3 21 30 24 33

Tb 1 0.8 1.5 2 0.5 1 0.7 0.6 0.6 0.7 0.7 0.6 2 2 0.4 0.4 0.4 0.5 0.6 0.5 0.6 4 7 6 7

Er 2.6 3 3 2 7 6.4 3 5 2 3 2 1.7 4 5 2 2 2 3 3 3 2 2 2 2 3

Yb 1.8 2 2.6 2.5 6 6 6 7 2 3 2 2.6 3 3 2 2 3 3 3 3 3 2 2 2 3

Lu 0.7 0.5 0.8 1 1.7 2 1.4 1.5 0.3 0.4 0.2 0.5 1 1 0.3 0.5 0.6 0.7 0.6 0.5 0.4 2 3 2 2

∑REE 50.1 51.3 55.2 58 137.9 129.6 129.4 133.1 58.7 62.9 56.7 52.1 144.5 147 31.1 31.3 35.4 34.9 35.8 34.5 33.6 162 163 165 161



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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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Fig. 13: SiO2-K2O diagram for the investigated

metavolcanoclastics and metavolcanics (Le Maitre,

1989).

Fig. 14: MnO*10-P2O5*10-TiO2/10 diagram for

the investigated metavolcanoclastics and

metavolcanics (Mullen, 1983).

Fig. 15: Zr vs. Ba diagram for the investigated

metavolcanoclastics and metavolcanics (Floyed,

1991).

Fig. 16: Normalized spider diagram for the

study metavolcanoclastics and metavolcanics

to N-MORB (Sun and McDonough 1989).

Fig. 17: Chondrite-normalized REE diagram for

investigated metavolcanoclastics and metavolcanics

rocks (Boynton, 1984).

Fig. 18: AFM diagram for the investigated

gabbro (Irvine and Baragar, 1971).

6

10

60

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

Sa

mp

le/C

ho

nd

rit

e

8

10

40


Sa

mp

le/C

ho

nd

rit

e

Tholeiitic

Calc-Alkali ne

Na2O+K2O MgO

FeOt

0.001

0.01

0.1

1

10

100

300

Rb Ba K Nb La Ce Sr Nd Zr Ti Y

Sa

mp

le

/N

-T

yp

e M

OR

B

0.001

0.01

0.1

1

10

100

300


Sa

mp

le

/N

-T

yp

e M

OR

B

40 50 60 70 800

1

2

3

4

5

SiO2

K2

O

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

CAB

IAT

MORB

OIT

OIA

MnO*10 P2O5*10

TiO2

CAB

IAT

MORB

OIT

OIA

MnO*10 P2O5*10

TiO2 /10



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Fig. 19: P2O2-Zr diagram for the investigated

gabbro (Winchester and Floyd, 1976).


investigated gabbro to N-MORB (Sun and

McDonough 1989).


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.

Alka

TH+

0.001

0.01

0.1

1

10

40


Sa

mp

le

/N

-T

yp

e M

OR

B

4

10

30


Sa

mp

le

/C

ho

nd

rite

35 40 45 50 55 60 65 70 75 80 850

2

4

6

8

10

12

14

16

18

20

Alkaline

Subalkaline

SiO2

Na2O

+K

2O

Tonalite Granodiorite

Monzogranite Alkali feldspar granite



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Fig. 26: R1 – R2 binary diagram for the

investigated granites (Batchelor and Bowden,

1985).

Fig. 27: Rb vs. Y+Nb diagram for the

investigated granites (Pearce et al., 1984).

Fig. 28: K2O-Na2O diagram for the investigated

(Chappell and White, 1974). A-type field is after

Liew et al., (1989).


investigated granites to N-MORB (Sun and

McDonough 1989).


the investigated granites (Boynton, 1984).

Fig. 25: TAS diagram for the study rhyolite

porphyry (Irvine and Baragar, 1971).

5

10

80

La

Ce

Pr

Nd Sm

Eu

Gd

Tb

Dy

Ho

Er

Tm

Yb

Lu

Sa

mp

le

/C

ho

nd

rite

35 40 45 50 55 60 65 70 75 80 850

2

4

6

8

10

12

14

16

18

20

Alkaline

Subalkaline

SiO2

Na2O

+K

2O

1 10 100 1000 20001

10

100

1000

2000

Syn-C OLG WP G

ORGVAG

Y+Nb

Rb

0.001

0.01

0.1

1

10

100

600


Sa

mp

le

/N

-T

yp

e M

OR

B



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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

1 10 100 1000 20001

10

100

1000

2000

Syn-C OLG WP G

ORGVAG

Y+Nb

Rb

A

B

C

D

Th Ta

Hf/3



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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 calc-

alkaline to tholeiitic affinity closer match with volcanic arc origin. The granitic rocks are varying from calc-

alkaline (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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