Structural and Tectonic Framework of Neoproterozoic Basement of Egypt: From Gneiss Domes to Transpression Belts

Fowler, Abdel-Rahman; Hamimi, Zakaria

doi:10.1007/978-3-030-15265-9_3

Cited by 24 publications

(24 citation statements)

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“…They were derived from an old sedimentary succession intercalated by basic igneous sills (ortho-amphibolites), marls (paraamphibolites) and quartzite layers. The sedimentary sequence was accumulated along a passive continental margin and then subjected to high-T and low-P regional metamorphism up to the upper amphibolite facies (Abd El -Wahed et al, 2016Hamimi et al, 2019;Fowler and Hamimi, 2020;Hamimi and Abd El-Wahed, 2020;Stern and Ali, 2020;El-Bialy, 2020). The gneisses and migmatites occur as antiforms and domed structures in the ENS (e.g.…”

Section: High-grade Gneisses and Migmatitesmentioning

confidence: 99%

“…The ENS is characterized by five main lithological components: (i) arc assemblage, (ii) dismembered ophiolites, (iii) gneiss terranes with core complexes (iv) Dokhan Volcanics and molasse sediments and (v) granitoid intrusions (Fritz et al, 1996(Fritz et al, , 2002Abd El-Naby et al, 2000;Abd El-Wahed, 2008Ali et al, 2015;Hamimi et al, 2019). These lithotectonic units were tectonically amalgamated through several phases of thrusting as well as sinistral shearing along NW-striking shear zones of the Najd Fault System and other shear zones, mainly in the central part of the ENS Hamimi et al, 2019;Fowler and Hamimi, 2020;Hamimi and Abd El-Wahed, 2020). The highly deformed granitoid gneisses in the ENS occur in antiformal 'domed' structures (e.g.…”

Section: Introductionmentioning

confidence: 99%

“…However, other studies indicated that these gneiss complexes were formed along one or more magmatic arcs in intra-oceanic or continental arc settings along the western margin of the Mozambique Ocean prior to amalgamation of East and West Gondwana at ~630 Ma (e.g. El-Ramly et al, 1984Greiling et al, 1984Greiling et al, , 1988Stern, 1994;Abd El-Wahed, 2008Andresen et al, 2009Andresen et al, , 2010Abd El-Wahed and Kamh, 2010;Augland et al, 2012, Lundmark et al, 2012Ali et al, , 2010aAli et al, , b, 2012Ali et al, , 2015Abd El-Wahed et al, 2016Hamimi et al, 2019;Fowler and Hamimi, 2020;Hamimi and Abd El-Wahed, 2020;El-Bialy, 2020).…”

Section: Introductionmentioning

confidence: 99%

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Neoproterozoic Tectonic Events of Egypt

El‐Wahed

Hamimi

2021

Acta Geologica Sinica (Eng)

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The Egyptian Nubian Shield (ENS) represents the northwestern part of the Arabian‐Nubian Shield and the northern extension of the East African Orogen. The ENS is regarded as being formed due to northward‐directed escape tectonics. It is characterized by mild accretion and suture zones dominated by major strike‐slip zones with a commonly sinistral sense of movement; some shear zones display a dextral sense of shear. It is dominated by gneisses and migmatites in the south, arc volcaniclastic metasediments and highly dismembered ophiolites in the central parts, whereas its northern part is dominated by late‐ to post‐tectonic granitoids. In southern Sinai, the Neoproterozoic rocks are grouped into four complexes, namely Feiran–Solaf, Sa'al–Zaghra, Kid and Taba. The ENS ophiolites were formed between 730–750 Ma, mainly in a supra‐subduction zone setting. The ENS has undergone a Neoproterozoic deformation history involving three successive phases: (1) Early N–S shortening phase (D1), (2) Syn‐accretionary phase (D2) and (3) Post‐accretionary phase (D3). The initial island‐arc stage (780–730 Ma) is a N–S shortening phase initiated by collision between the Eastern Desert tectonic terrane to the north with both the Gebeit and Gabgaba terranes to the south (830–720 Ma). During the arc‐splitting and back‐arc spreading stage (730–620), voluminous syn‐tectonic granitoids intruded into the ENS (750–610 Ma). The E–W‐directed compressional/transpressional phase (620–450 Ma) led to the overall uplift of the central part of the ENS and consequently the development and exhumation of the core complexes in oblique convergent zones. The E–W intense shortening deformation resulted also in the formation of NW‐ and NE‐striking sinistral and dextral strike‐slip shear zones, respectively. The latest periods of the E–W‐directed compressional/transpressional regime were characterized by deposition of the molasse‐type Hammamat Sediments unconformably over the Dokhan Volcanics, or interbedded with them. The combined thrusting, folding and sinistral‐reverse shearing structures have been interpreted to resulted from the E–W‐directed compressional/transpressional phase in response to the oblique shortening of the Arabian‐Nubian Shield between East and West Gondwana.

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Section: High-grade Gneisses and Migmatitesmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

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Neoproterozoic Tectonic Events of Egypt

El‐Wahed

Hamimi

2021

Acta Geologica Sinica (Eng)

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“…Orogenic gold deposits in the Eastern Desert were formed in two successive epochs (Botros, 2021) Lundmark et al, 2012) and the two episodes at 715-700 Ma and 685-665 Ma of Stern and Hedge (1985). The granitoids of this stage are trondhjemites, tonalites and granodiorites (Fowler and Hamimi, 2020). Arc-arc collision zones in the ANS are represented by ophiolite-decorated sutures from southern Egypt and Sudan into the western arc terranes of Saudi Arabia (Fowler and Hamimi, 2020).…”

Section: Tectonic Settings Of Gold Deposits In Egyptmentioning

confidence: 99%

“…The granitoids of this stage are trondhjemites, tonalites and granodiorites (Fowler and Hamimi, 2020). Arc-arc collision zones in the ANS are represented by ophiolite-decorated sutures from southern Egypt and Sudan into the western arc terranes of Saudi Arabia (Fowler and Hamimi, 2020). Collision between the south Eastern Desert-Midyan and Gabgaba-Gebeit-Hijaz terranes along the ophiolite-bearing Yanbu-Onib-Sol Hamed-Gerf-Allaqi-Heiani suture zone occurred at ~700 Ma (Ali et al, 2010;Johnson et al, 2011).…”

Section: Tectonic Settings Of Gold Deposits In Egyptmentioning

confidence: 99%

Intrusion‐related Gold Deposits in Egypt

Botros

2021

Acta Geologica Sinica (Eng)

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Intrusion‐related gold deposits (IRGDs) occur in the Eastern Desert (ED) of Egypt within magmatic districts that are exploited for tungsten and tin mineralization. IRGDs and intrusion‐related rare metal deposits (IRRMDs) are almost invariably linked with the late to post collisional Younger Granites (YGs) that have three successive phases (I, II and III). At ∼635–630 Ma, the ED underwent a transition in deformation style from compressional to extensional and a switch from subduction with crustal thickening to delamination with crustal thinning. This transition was concurrent with the emplacement of a short magmatic pulse (∼635–630 Ma) that represents a transition between orogenic gold deposits and IRGDs. K‐rich calc alkaline granites (phase I and II of the YGs) hosting IRGDs like the Hangalia deposit were emplaced during the time span 630–610 Ma. Alkaline magmatism began at 610 Ma, coexisting with the K‐rich calc‐alkaline magmatism over the 610–590 Ma time span, where the Fawakhir (598 ± 3 Ma) and Um Had (596 ± 2 Ma) granites that host the IRGDs were emplaced. In time, the alkaline magmatism became more alkaline giving rise to phase III of the YGs that hosts IRRMDs. A distinct metallogenic epoch comprising both IRGDs and IRRMDs, was undergoing extreme growth at ∼600 Ma.

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The Egyptian Nubian Shield Within the Frame of the Arabian–Nubian Shield

El‐Wahed

Hamimi

2020

Regional Geology Reviews

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Structural and Tectonic Framework of Neoproterozoic Basement of Egypt: From Gneiss Domes to Transpression Belts

Cited by 24 publications

References 275 publications

Neoproterozoic Tectonic Events of Egypt

Neoproterozoic Tectonic Events of Egypt

Intrusion‐related Gold Deposits in Egypt

The Egyptian Nubian Shield Within the Frame of the Arabian–Nubian Shield

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