Egypt
History - Pan-African plate tectonic geology of the Arabian Nubian Shield
Extracted from: W.R. Church, 1988. Ophiolites, sutures, and micro-plates of the Arabian-Nubian Shield: a critical comment, p. 289-316 in El-Gaby, S., and Greiling, R.O., eds., The Pan-African belt of Northeast Africa and adjacent areas; Tectonic evolution and economic aspects of a Late Proterozoic orogen, Friedr. Vieweg & Sohn, Braunschweig/Wiesbaden (Jabal Zebara viewed from the North; Zebara is located on the eastern flank of the Hafafit extensional dome)
Google Earth -
Arabian-Nubian (Sudan) Shield
(290) INTRODUCTION
It is now commonplace to represent
the Arabian-Nubian Shield (Fig 1) as a cratonized
assemblage of oceanic and continental margin arcs located between the Nile
craton to the west and some other presently ill-defined craton to the east of
the Ar Rayn terrane, the most easterly volcanic terrane within the exposed part
of the Arabian Shield (Roobol et al., 1983). Most models of the Shield assume
that the accretionary process involved face-on collision of a succession of
arcs, and that consequently the collision zone would be marked by a trail of the
remnants of the subducted ocean crust. Definition of the five arc terranes (microplates)
currently recognised in the Arabian-Nubian Shield (Stoeser and Camp, 1985; Vail,
1985) (Fig. Ib) is based on this assumption, and depends particularly on the
supposed presence of ophiolite-decorated suture zones in the Sudan (Embleton et
al. 1982), and the long distance correlation of the ophiolites of Bir Umq and
Jabal Thurwah (Delfour, 1982), and of Jabal Al Wask and Sol Hamed (Duyverman,
1984; Nassief et al. , 1984). The microplate scheme envisioned by Vail (1985) is
similar to that of Stoeser and Camp (1985) but includes the definition of two
additional arc terranes; one in the Sinai region, the other the result of the
division of the Asir terrane of Stoeser and Camp into two independent
microplates. Vail has also raised the status of Camp and Stoeser's microplate
distribution map to that of a palinspastic map, implying that the present
position of the microplates is essentially that which they occupied at the time
of their amalgamation. Although in substantial agreement over the location of
suture zones. Vail, and Camp and Stoeser nevertheless disagree concerning the
polarity of subduction; Vail, along with Kroner (1985), preferring a subduction
direction to the west, and Camp and Stoeser a subduction direction to the east.
Irrespective of the difficulty of
determining subduction polarity, defining plate boundaries in terms of ophiolite
trails, while a simple elegant, and apparently rational (291) procedure, may
however not be legitimate. Firstly, as is illustrated in Fig 1, defining plate
boundaries by joining ophiolite occurrences appears to be an arbitrary
procedure; secondly, it is assumed that ophiolites represent intra-arc oceanic
crust, which may not be true; and thirdly, available geological data suggests
that the evolution of the Saudi-Nubian Shield was more complicated than current
microplate models suggest. In the subsequent parts of this paper, following a
brief review of the 'ophiolite problem', the status of some of the currently
favoured suture zone sites will be examined from the latter two points of view.
THE OPHIOLITE PROBLEM
It is clear that many ophiolites
formed at spreading centers analogous to those of mid ocean ridges.
Nevertheless, the origin of many ophiolites as examples of MOR-type oceanic
crust has long been questioned, and it has been suggested that they variously
represent the roots of primitive island arcs, back- arc marginal basins, and,
more recently (Pearce et al. 1984), spreading centres formed above subduction
zones at the inception of arc development - and therefore located within the
fore-arc parts of the subsequently evolved arc. Basaltic rocks formed at
mid-ocean ridges are usually plagioclase-phyric, exhibit Ti02 (wt.) values
numerically equivalent to the FeOt/MgO ratio of the rocks, are LREE and LIL
depleted, have Ti/Zr ratios of about 100, and only rarely (Bouvet Fracture zone
of the Southwest Indian Ridge, Le Roex et al. 1984) exhibit negative Nb-Ta
chondrite-factorized anomalies. Cumulates in ophiolites with these
characteristics (e.g. Macquarie Island, Vale, 1972; Bay of Islands, Church and
Riccio, 1977; the 'Alps', Serri, 1981) characteristically include troctolites,
and the crystallisation sequence at low pressures is olivine-plagioclase-clinopyroxene-orthopyroxene.
It should be noted however that anomalous low TiO2 basaltic rocks have been
found in the vicinity of transform fault zones (0.5 wt.; Bryan, 1979, ARP74
stations 31 and 33), as well as (292) at one site in the Somali Basin (Frey et
al. 1980; site 236). Basalts taken from back-arc basins such as the Scotia Sea
include MOR, LIL-enriched ocean island, and arc types, as well as mixed MOR/arc
rocks exhibiting LREE enrichment and Nb depletion relative to La and Ba-Rb-K
(Saunders and Tarney, 1984). In contrast, fore-arc basement rocks (e.g.
Marianas, Crawford, 1981) include arc tholeiites and rocks of the
boninite series. Cumulate rocks formed in
this environment, such as - according to Pearce et al. (1984) - those of the
Troodos ophiolite (Desmet, 1977; Robinson et al., 1983; Murton, 1986),
crystallise in the sequence olivine (chromite; high Cr)-
clinopyroxene-orthopyroxene-plagioclase, whereas boninitic volcanic rocks with
extremely low TiO2 values (0.2 wt. percent) and concave upwards REE patterns
crystallized in the sequence olivine-orthopyroxene-clinopyroxene-plagioclase.
The associa tion of such rocks with a ductile fault zone in the Troodos
ophiolite (Arakapas zone; Murton, 1986) and with a spreading centre in the case
of the Belts Cove ophiolite of Newfoundland (Coish and Church, 1979; Coish et
al., 1982; Church, 1987) might suggest that ophiolites with these
characteristics owe their preservation in part to their origin as strike-slip
fault slivers detached from the frontal part of arcs as a result of oblique
subduction. If such ophiolitic slivers are transported by strike slip movement
prior to obduction and arc assembly, they may be less useful in the delineation
of arc boundaries than has tended to be assumed, although of course they do
indicate the one-time existence of active subduction.
In the Arabian-Nubian Shield
petrographic descriptions and limited chemical data are available for the Al
Wask (Bakor et al. 1976), Jebel Ess (Shanti, 1984), Jebel Thurwah (Nasseef et
-al. 1984), and Al Amar Idsas (Nawab, 1979; Church, 1980) ophiolites in Saudi
Arabia, the Sol Hamed (Hussein, 1981; Fitches et al. 1983) and Wadi Onib
(Hussein et al. 1984) ophiolites in the Sudan, and the Fawkhir (Stern, 1979;
Dixon, 1979), Wadi Ghadir (El Bayoumi, 1980) and Sabahiya (Basta, 1983)
ophiolites in Egypt. Although plagio-phyric lavas occur in the high-Ti (>3 wt
percent.) 'within-plate' Wadi Ghadir ophiolite, (293) in no case have troctolitic cumulates been recorded, and for this reason alone the
interpretation of any of the above ophiolites as major ocean or back-arc oceanic
crust is presently uncertain.
THE SUTURE PROBLEM
Historical Perspective
The earliest mention of ophiolitic
rocks in the Arabian-Nubian Shield and their interpretation as fractionated
products of deep-sea mafic magmatism can be attributed to Rittman (1958), but
the first references to the Arabian-Nubian ophiolites in the context of plate
tectonic theory are contained in papers by Garson andShalaby (1974; 1976), Bakor,
Gass and Neary (1976), Neary, Gass, and Cavanagh (1976) (Fig.
la), and Al Shanti and Mitchell (1976). Garson and Shalaby considered the
ophiolites to mark oceanic sutures separating a series of continental margin
arcs that developed episodically above a long-lived - since the Archean -
westward dipping subduction zone. Bakor et al. and Neary et al., however,
following the suggestion of Greenwood et al. (1975) that the Arabian Shield
could be considered a cratonized island-arc developed above an easterly dipping
subduction zone, proposed that the ophiolites represent oceanic remnants of as
many as seven northwest-trending back-arc marginal basins, five of which could
be recognized within the Nubian Shield of the Eastern Desert of Egypt. This idea
was also taken up by Frisch and Al-Shanti (1977), who described the development
of the Arabian Shield in terms of a complex of arcs and back-arc basins which
were sequentially closed along slip planes dipping generally to the east, and
further developed by Gass (1977) in his proposal that the whole of continental
North Africa east of the West African Craton was formed of cratonized oceanic
island arcs of Late Proterozoic age.
In contrast Kazmin et al. (1978)
explained the development of the Arabian-Nubian Shield in terms of the opening
and closing (294) of an intracontinental Proto-Red Sea basin with dimensions
approximately defined by the present distribution of greenstones in the
Arabian-Nubian Shield, whereas Shackleton (1979), in linking the Egyptian and
Saudi Arabian suture zones of Bakor et al. to ophiolite occurrences in southern
Sudan, Ethiopia, and Kenya (Fig. la), suggested that oceanic crust was
periodically extended by the southward propagation of spreading ridges of
oceanic crust in the north into continental crust in the south; there was
therefore a transition from crust formed by arc accretion in the north to crust
characterised by Himalayan-type collision in the south. Some support for these
views was provided by Dixon’s discovery of Archean-age zircons in quartzite
clasts in a conglomerate located within the ophiolite zone of the southern
Eastern Desert of Egypt (Dixon, 1979).
In the Eastern Desert of Egypt
mention of ultramafic rocks as obducted slabs of mantle and oceanic material was
made by Abdel-KhaIek (1979), and the back-arc hypothesis was reinforced by the
discovery of typical ophiolite sequences at Wadi Ghadir (El-Sharkawy and El-Bayoumi,
1979) and Bir Fawkhir. The representation of the Eastern Desert ophiolites as
marking a series of intra-arc suture zones was however questioned by Church
(1979; 1980; 1983), who argued that the ophiolitic material of the Eastern
Desert occurred in association with exogeosynclinal deposits, and its primary
distribution was therefore lithostratigraphically controlled; that is, the
ophiolitic material represents olistostromal debris derived from an 'internal'oceanic
source undergoing east towards west obduction in a manner similar to that
invoked in the case of the emplacement of the early Ordovician flysch and
associated ophiolite sheets of the western margin of the Appalachian system. On
this basis Church concluded that the ophiolitic zones of the Eastern Desert did
not mark the location of in situ marginal basin oceanic crust, but rather, that
the present distribution of the ophiolitic 'geosynclinal sequence' was
controlled by secondary deformation structures. In terms of modern plate systems
analogy was drawn with the Pacific region (295) between Australia and New
Zealand. Stern (1979) also proposed that the Arabian-Nubian orogen originated as
an intra- continental rift, and Engel et al. (1980) drew attention to
similarities between the Arabian-Nubian Shield and the development of Archean
systems.
The nature of the ophiolite-bearing
melange of the Eastern Desert was described by El Sharkawi and El Bayoumi (1979)
and by Shackleton et al. (1980), and petrographic details of the ophiolite at
Fawkhir were given by Nasseef et al. (1980). El Bayoumi (1980) interpreteted the
melange as having originated in a trench environment, and the tectonic history
of the Eastern Desert in terms of a rift ocean basin which was closed by
consumption of oceanic crust along a westerly dipping subduction zone. In the
Arabian shield, arc development as a result of westerly subuction was also
favoured by Nawab (1979), Schmidt et al. (1979), and Hadley and Schmidt (1980),
whereas Gass (1979) considered the Shield to have developed above one or more
easterly-inclined subduction zones. An exogeosynclinal arc-obduction model for
the development of the ophiolite- bearing terrane of the Eastern Desert was
espoused by Ries et al. (1983), who, however, suggested that ophiolitic melange
material was deposited on both continental and oceanic crust close to the
interface between an arc and a continental margin about to enter into collision
with one another. The melange received debris from the arc, by westward sliding
of oceanic material into a trench from thrusts in the fore-arc prism, as well as
from the continent, and was tectonically imbricated with slabs of serpentinite
during a thrusting event - coeval with the extrusion of the Dokhan volcanics -
that brought the melange' terrane over shelf sediments of the subducting
continental margin.
Following abandonment of the view
that the ultramafic rocks of the Eastern Desert delineated in situ zones of
back-arc ocean collision, Embleton et al. (1984) defined a new set of northeast
trending suture zones in the Sudan, whereas in Saudi Arabia Delfour (1982)
depicted the Jabal Thurwah ophiolite as (298) lying in the same northeast
trending zone as the Bir Umq ophiolite. The northeast trending sets of sutures
on either side of the Red Sea were then correlated by Duyverman (1984) (Fig.
1e)
and Nassief et al. (1984) (Fig. 1d); that is, the original northeast trend
suggested for the ophiolite-decorated zones was abandoned in favour of a
northwest trend. Following extensive mapping in Sinai, Shimron (1984)
interpreted the geology of the Wadi Kid area in terms of northwards (westwards)
subduction of oceanic crust beneath Proterozoic continental crust and the
resulting development of accretionary prisms marginal to an Andean type margin
-although the existence of ophiolites in the Wadi Kid and surrounding areas of
the northern Eastern Desert was denied by Stern et al. (1985). El Bayoumi and
Greiling (1984) and El Ramly et al. (1984) also considered the Nubian Shield to
have formed above a west dipping subduction zone following the development of an
island arc and a marginal basin arranged such that the latter separated the arc
from the Nile craton. Following closure of various oceanic systems to the east,
rocks of the marginal basin and the arc were thrust over the continental margin.
In this model the ophiolitic material of the melange unit(s) forms the basal
units of a series of imbricate slices and are therefore considered to have been
tectonically incorporated into the melange rather than formed as olistostromal
units. Stacey and Hedge (1984) confirmed the presence of continental crust
beneath the eastern part of the Arabian-Nubian Shield - proving that 'accretion'
and 'intracratonic' are not mutually exclusive concepts - and, adopting the
suture distribution of Nasseef et al. (1984), Stoeser and Camp (1985) have
attempted to describe the development of the Arabian Shield in terms of the
amalgamation of three ensimatic island arc terranes and two microplates with
continental affinities. Vail (1985) has now extended this concept into the Red
Sea Hills region of the Sudan. Stoeser and Camp also revert to the view of
Greenwood et al. (1976) in considering closure of the main ocean basin to (300)
the northwest to have involved subduction towards the southeast. Kroner (1985)
and Vail (1985) on the other hand invoke a pattern of subduction closure
opposite to that adopted by Stoeser and Camp.
The Eastern Desert
The ‘ultramafic rocks as sutures'
point of view has previously been debated (Church, 1979, 1981; Nassief and Gass,
1977) with respect to the serpentinites of the Eastern Desert of Egypt, and it
is now generally conceded that in the latter instance, other than Sinai (Vail,
1985), the ultramafic rocks are indeed allochthonous. Work since that time in
the Marsa Alam - Gebel Zabara - Hafafit and Meatiq regions of the Eastern Desert
(El Bayoumi, 1980, 1984; Basta, 1983; Sturchio et al. 1984; Habib et al. 1985)
has also shown that the ophiolite/arc debris-bearing terranes (including low-Ti
high MgO 'boninitic' units) constitute a set
of east-facing thrust sheets, down through wich there appears to be an
incremental increase in strain, style of deformation, and degree of metamorphism
(Church, 1983). The geology of the higher sheets is further complicated by the
structural imbrication of apparently younger volcanic and volcano-sedimentary
units. In the southern part of the Egyptian Desert, continental margin
sediments, autochthonous or parallochthonous relative to Nubian basement rocks,
are possibly represented by marbles beneath the schists and overlying ultramafic
sheets and associated olistostromal mudstones of the Abu Swayel region (e.g. at
Um Krush in the Abu Swayel region; AS, Fig. 3). In
this respect it is conceivable that the whole of the Eastern Desert is a
composite allochthonous sheet, the leading edge of which is located along the
line of the Nile, with the Nuba Mountains (El Ageed and El Rabaa, 1981) and
Ingessana (Kabesh, 1961) ophiolites of the Sudan to the south occupying an
external position analogous to that of the Bay of Islands ophiolite of the
Appalachian system.
(302) The isotope studies of Harris
et al. (1984) and Ries et al. (1985) indicate that metasediments (Rahaba Group)
of the Bayuda Desert and southern Eastern Desert of Egypt (Wadi Haimur in the
Abu Swayel region), while intruded by mantle derived igneous rocks and
metamorphosed at c. 900 Ma., include the erosion products of older early-middle
Proterozoic continental crust. Furthermore, in the northern part of the Eastern
Desert of Egypt Abdal Rhaman (1986) has determined an age of 881 ± 44 for a
tonalite suite at Ras Gharib. The high Ri value of these rocks suggests the
existence of older crust at depth beneath this part of the Eastern Desert. On
the other hand, the very low R- values of some rocks (e.g. Abu Swayel, Stern,
1979; Bayda and Jizi, Kemp et al. 1982; Um Aud diorite, unpublished data) and
the Nd/Nd data of Bokhari and Kramers (1981), Claesson et al. (1984) and Harris
et al. (1984) indicate that the mantle beneath at least parts of the
Arabian-Nubian Shield is anomalously LIL depleted, and in this respect the
problem of the presence or absence of thinned old continental crust beneath the
Eastern Desert of Egypt and the Red Sea Hills of the Sudan is therefore not
entirely resolved. It is also puzzling that the Abu Hamed Quartz ite unit of the
Bayuda Desert, although dominated by seemingly shallow water carbonates and
quartzites and therefore similar to the Wadi Haimur sediments of the Abu Swayel
region, does not have a strong older crustal isotopic signature comparable to
the Wadi Haimur and Rahaba rocks. Nevertheless, the available isotopic data are
compatible with the view that the Eastern Desert is in part composed of
continental margin slope and rise deposits, including thick marbles at Abu
Swayel, and pelitic and quartzitic rocks, intercalated with ophiolitic melange
units, at Hafafit, Wadi Miya (chiastolite and calc-siliceous rocks), and Meatiq;
intrusive arc (?) rocks emplaced at about 900 Ma; and a thrust cover of
ophiolitic rocks unconformably overlain by arc volcanics (Abu Swayel 768 ± 30,
Neferdeib 712 ± 60, El Koro 800 ± 80, Kadaweib 723 ± 6; Figs.
2 and 3) with an
age uncertainty range of 700-800 Ma (Fig. 2), all intruded by tonalite at 711 ±
6 Ma (Dixon, 1979). Other than in the northern Eastern Desert, the isotopic data
indicate that 'old' (303) basement rocks if present are of considerably reduced
thickness beneath the Eastern Desert. According to Sturchio et al. (1984)
thrusting continued until at least 614 Ma. It is uncertain therefore whether the
Abu Swayel-Naferdeib volcanics were thrust with the ophiolitic rocks or were
formed after ophiolite emplacement. The ophiolites were however emplaced prior
to 680 Ma, the age of diorite (Sturchio et al. 1984) intrusive into deformed
ophiolitic material of the Hafafit area, and probably prior, to 711 Ma (Dixon,
1981).
A further problem concerning the
source of material in the melange sheet relates to the origin of pebbles of
older Precambrian gneiss and granitoid material, and of quartzites and arkoses
containing Archean age detrital zircons (Dixon, 1979). Since the melange is
almost certainly derived from the east the presence of this material implies
either that foundered continental crust, now considerably thinned and basified,
and its cover of slope and rise sediments extended well to the west of the
present Red Sea, or that a continental microplate was at one time interspersed
with the arcs of the Arabian Shield, or that at one time the Afif zone was much
closer to the Eastern Desert of Egypt. Clearly, further field and isotopic
studies are required to resolve these problems. The Yanbu Suture The Yanbu
suture is defined by Camp (1984) in terms of the Karig model of accretionary
prism development, with the Farri Group representing the accretionary prism and
the Al Ays Group the overlying fore-arc basin. Camp also suggests that the Yanbu
suture zone was the site of origin of the ophiolitic melange of the Eastern
Desert of Egypt, thereby implying that formation of the melange post-dates the
initial phase of development of the Al Ays fore-arc basin, and is therefore
likely older than 725 ± 12 Ma, the age of the Jabal Salajah tonalite. However,
while the geology of the Al Ays area is indeed complex, it is (304) not certain
that available descriptions and age relationships are compatible with the accretionary prism model.
The Farri Group: an accretionarv prism
Whereas Camp (1984) refers to the Farri Group as being formed of highly deformed ophiolite-bearing accretionary prism deposits, Kemp et al. (1982) describe the group as being composed of thick, welded keratophyric tuff (locally peralkalic) with an age of 742 ± 6 Ma (Calvez, 1983, oral communication quoted by Claesson et al., 1984), mixed sedimentary and volcanic rocks, andesites and epiclastic breccias, turbiditic sediments, and pillowed basalt. Furthermore, the presence of two-pyroxene gabbros, volcanics with low TiO2 relative to P2O5, and absence of a sheeted diabase unit in the Jabal Al Wask ophiolite (Bakor et al., 1976) suggests that the Al Wask complex may represent part of an arc rather than ocean crust separating adjacent arcs.
The Al Wask ophiolite occurs in association with the upper basalt unit of the Farri Group and has a radiometric age (Sm/Nd, 743 ± 24 Ma, Claesson et al., 1984), identical to that of the underlying felsic volcanic rocks of the Farri Group. The age of the ophiolite and Farri Group would therefore appear to be well constrained at c. 730-750. However, zircons from the Haja plagiogranite supposedly associated with the ophiolite have an age of 780 ± 20 Ma (Calvez, 1983, oral communication quoted by Claesson et al., 1984). Therefore, either the Haja granophyre and Al Wask ophiolite have an 'overlap' age of 760-770 Ma (Fig. 2) and are older than the Farri Group, or the granophyre represents remobilized material of the 796 ± 23 Ma old Jar tonalite suite melted by the intrusion of Al Wask mafic liquids. In either case, rocks mapped by Kemp et al. (1982) as Farri but cut by the 796 ± 23 Ma old Jar tonalite (Kemp et al. 1982) likely belong to a volcanic unit older than the Farri Group. These rocks, along with the gneissic Al Hinu Formation and the gneissic rocks of the domes to the north of Al Wask could be equivalents of the lower thrust units exposed in the (305) Hafafit (El Ramly et al., 1984) and Urn Samuiki (Shukri and Mansour, 1980) domes of the Eastern Desert (Fig. 3).
Since the Farri-Al Wask rocks are unconformably overlain by Al Ays sediments (which are cut by the 725 Ma old Salajah tonalite), they could well represent the older (750-725 Ma) part of a southeasterly migrating arc (Al Ays Group) presently located between pre-800 Ma rocks to the northwest (older Farri) and 805 Ma (Hedge pers. comm. to Stoeser and Camp, 1984) and 945 ± 45 Ma (Al Shanti et al. 1984) intrusive-volcanic complexes (Birak and Rabigh rocks) to the southeast.
The root zone of the Eastern Desert and Jabal Ess ophiolites
The well preserved Jabal Ess ophiolite described by Shanti and Roobol (1979) and Shanti (1984) is characterised by the enigmatic presence of both low-Ti, 'normal' Ti (TiO2 FeOt/MgO), and 'within-plate' basaltic liquids. It therefore represents an example of an ophiolite complex in which interlayered basaltic and dike sequences exhibit both oceanic and arc characteristics. In terms of its low degree of metamorphism and deformation and its association with melange, turbidites, and arc volcanics, the Jebel Ess ophiolite is comparable to the adjacent (after closure of the Red Sea) uppermost ophiolite - melange unit of the Wadi Ghadir - Marsa Alam - Hafafit nappe pile of the Eastern Desert of Egypt. In as much as it is the most easterly ophiolite in this zone, it may therefore represent the highest structural unit of the nappe. In the southern part of the Eastern Desert relatively undeformed volcanic rocks (Abu Swayel volcanics, 768 ± 31; Stern, 1979) overlie intensely deformed allochthonous sheets of ultramafic rock and associated distal mudstones and minor olistostromal units that have been thrust over garnet-amphibolite grade layered metasedimentary and metavolcanic schists and gneisses. The age of the Abu Swayel volcanics relative to the Jebel Ess ophiolite and Jar tonalite is not certain due to the large ± values associated with the isotopic ages of these rocks (Fig. 2), but an age of 782 or older for the Jabal Ess ophiolite (Claesson et al. 1984) is compatible (306) with an emplacement age for the Eastern Desert ophiolites of 760 to 780 Ma, slightly later than the intrusion of the Jar tonalite suite in the Al Wask area, and the Birak und Dhukhr tonalite suites to the southeast. Arc plutonic and volcanic rocks equivalent in age to the Jar tonalite could therefore be the source of the abundant felsic plutonic and volcanic debris in the Eastern Desert melange; which would imply that the surface outcrop of the boundary separating the melange from its arc source lies east of the Jabal Ess ophiolite and west of the Iqwaq granodiorite (821 ± 40 Ma). However, if the gneiss domes of the Al Wask region are analogous to those of Hafafit and Um Samuiki of the Eastern Desert, it is conceivable that the Jar tonalite suite, if not also the Farri and Al Ays groups, has been thrust to the west of the location of the root zone of the suture. Locating the suture may therefore be an intractable problem.
The extension of the Yanbu suture into the Sudan
Nasseef et al. (1984; Fig. 1d) and later Vail (1985; Fig. 1b) extended the Yanbu suture into the northern Red Sea Hills of Sudan to link up with the supposed Sol Hamed - Wadi Onib suture. However, as discussed above, the Al Wask complex may not represent oceanic crust. Furthermore, given the clearly allochthonous nature of the ophiolites in southern Egypt (e.g. Urn Krush in the Abu Swayel area. Fig. 3) it is more likely that the Sol Hamid ophiolite belt constitutes the leading edge of a major northwesterly directed thrust than the actual zone of closure of an oceanic basin. Embleton et al. (1984) have proposed that a second more southerly suture be recognised to include the Nakasib belt of the Sudan and the Jabal Thurwah ophiolite of Saudi Arabia. It should be noted however that serpentinites occur southwest of Muhammed Qol in the area between the Sol Hamid and Nakasir belts - and others may remain to be discovered. It is therefore not inconceivable that ultramafic material underlies more area between Sol Hamid and the region to the south than just the supposed suture zones. Furthermore, the presence of wehrlite and Iherzolite cumulates in the Sol Hamed ophiolite (Fitches et al., 1983) as (307) well as perhaps also the Wadi Onib ophiolite, and the absence of troctolitic cumulates in any of these ophiolites, suggests that rather than representing intra-arc oceanic crust they may well be strike-slip fault slices of primitive suprasubduction zone fore-arc crust.
The Bir Umq - Jabal Thurwah Suture
The Jebel Thurwah ophiolite (Nasseef et al., 1984) is petrologically (presence of orthopyroxene-bearing cumulates) and chemically (low Ti) unlike 'normal' oceanic crust. Rather, as suggested by Nasseef et al. (1984), it is more similar to oceanic crust developed within the fore-arc segment of a primitive arc (Troodos, Cyprus; Betts Cove, Appalachians). The ophiolite can be interpreted as an allochthonous sheet emplaced onto the Samran Formation from either the northwest or southeast from beyond the present outcrop of the Samran, or from beneath the Samran. Nor is it proven that it is in continuity with either the Bir Umq ophiolite or with the widely spaced and poorly developed ultramafic rocks in the vicinity of Port Sudan in the Sudan. Even in terms of Camp's attempt (Camp, 1984) to model the At Taif metamorphics, Baish volcanics, and An Nimas plutonics in terms of a frontal arc, back arc basin, and remnant arc system, it is apparent that the trend of the marginal basin and remnant arc is north-south, the purported northeast trend of the suture being evident only in terms of a supposedly primary elongation of the much younger Fatimah volcanic basin, the northeast trend of faults cutting sediments and volcanics of the supposed arc - trench gap, and the supposed recognition of an upper slope discontinuity. The status of the Jebel Thurwah ophiolite as marking a suture zone is therefore highly uncertain. It is of interest to note that the boundary that does separate zones containing rocks with an -age greater than 900 Ma from terranes of less than 900 Ma within the Asir terrane is not marked in Saudi Arabia by a suture. (308)
The Nabitah suture - Nabitah mobile belt
Interpretation of the ultramafic-mafic complexes of the Nabitah zone as ophiolites is not universally accepted (Caby, 1984; Agar, 1985). Although a plate boundary may well therefore lie somewhere within the Nabitah zone, it is not necessarily demarcated by an 'ophiolite'-decorated fault zone. According to Stacey and Agar (1985) the suture is occupied by the syntectonic Subay igneous suite, in which case strike-slip juxtaposition of the adjacent arc terranes remains a possibility. It might also be noted in this respect that Caby (1984) concluded that continental accretion of the Arabian Shield was essentially vertical and suggested that the absence of evidence for large scale horizontal movements precluded involvement of the Shield in any major collisional event. Furthermore, Stoeser et al. (1984) state that the synorogenic emplacement of 650 to 690 Ma old granodiorite plutons in areas marginal to the supposed Nabitah suture zone reflects major westward-directed compressional orogeny related to a continental collisional event possibly located somewhere to the east of the exposed southeastern Arabian Shield.
The Al Amar suture
A reasonable case can be made for situating the Al Amar ophiolitic rocks (Al Shanti and Mitchell, 1976; Nawab, 1979; Jackson et al. 1980) in proximity to a suture. However, irrespective of the number of geologic problems concerning correlation and age (Al Shanti et al., 1984; Calvez et al. 1985) that require clarification, there is considerable uncertainty about the oceanic nature of the ophiolites (Le Metour et al. 1982), which, as in the case of the Thurwah ophiolite, do not appear to represent 'normal' oceanic crust (Church, 1980a). Since the Al Amar ophiolites are likely allochthonous, perhaps emplaced in association with the deposition of flysch representing the products of the erosion of the overthrusting plate (Church, 1980b), their present location does not determine the suture zone nor the nature of movement on the suture. The metallogenic zonation - copper to the east, silver-lead-zinc to the west, might imply subduction (309) from east to west leading to the development of a Sea of Japan type back-arc basin as suggested by Nawab (1979), but since copper and gold zones also occur to the west of the polymetallic zone, subduction could equally well have been towards the east.
CONCLUSIONS
Although some ultramafic-mafic complexes of the Arabian-Nubian shield likely formed in a spreading centre environment, whether fore-arc, back arc or continental margin rift (Tasman-sea- type), their present locations do not delineate with certainty the original sites of the ocean basins. The practice of linking widely separated ultramafic-mafic complexes to define suture zones cannot therefore be accepted without question. Furthermore, given that the width of the Arabian-Nubian shield from the Nile to the Nabitah boundary zone is of the same order of distance as that across the strike-slip amalgamated collage of the Canadian Cordillera, the possibility must be allowed not only that the microplates of the Nubian Arabian shield have been laterally rafted into position, but that the plate boundaries may have been considerably modified as a result of collision. Any assessment of crustal growth rates in the Arabian-Nubian shield should take this point into account.
Notwithstanding the considerable uncertainty concerning the arc amalgamation process in the Shield, geochronological data obtained by Stacey and Hedge (1985) and Stacey and Agar (1985) now indicate that the Arabian Shield - as might be guessed from the distribution of zinc-lead mineral showings - is bordered to the east by older continental crust. The isotopic studies ofHarris et al. (1984), Ries et al. (1985), and Abdel Rahman (1986) suggest that the western margin of the Nubian Shield is formed of an about 900 Ma continental margin volcanic arc over which the Egyptian-Sudanese ophiolite terrain has been thrust from the east. The results of recent studies in southern East Africa (Maboko et al., 1985) also suggest that the granulite (310) belts of western Tanzania were formed 715 Ma ago and may have been thrust (Sacchi et al., 1984), along with 'ophiolite'-type rocks, to the southwest over a basement of 1100 Ma continental margin arc rocks (Ri .7027) and its cover of 900-1000 Ma continental-derived sediments (Ri .7091-.713). If the Hijaz ocean was continuous along the length of east Africa during the late Proterozoic, it would appear therefore that either considerable overthrusting has caused the loss from view of the southern arc equivalents of the Arabian-Nubian Shield or the southerly arc elements have migrated laterally northwards and '\ presently form part of the Arabian-Nubian amalgamated terrane. In this context, a more comprehensive examination of the potential role of strike-slip movements in the assembly of the Arabian-Nubian arcs may prove to be more profitable than is perhaps currently thought.
REFERENCES
Abdel-KhaIek, M.L., 1979. Tectonic evolution of the basement rocks in the southern and central Eastern Desert. Bull.Inst. Appl. Geol. Jeddah, v. 3, (1), p. 53-62.
Abdel-Rahman, A-F., 1986. Plutonism and tectonic evolution of the Ras Gharib segment of the northern Nubian Shield. Ph.D. thesis. McGill University.
Agar, R.A. 1985. Stratigraphy and palaeogeography of the Siham group: direct evidence for a late Proterozoic continental microplate and active continental, margin in the Saudi Arabian Shield. J. Geol. Soc. London, 142, p. 1205-1220.
Al Shanti, A.M.S., A.A. Abdel-Monem and F.H. Marzouki, 1984a.Geochemistry, petrology, and Rb-Sr dating of trondjemite and granophyre associated with the Jabal Tays ophiolite, Idsas area, Saudi Arabia. Precambrian Res., 24, p. 321-334.
Al Shanti, A.M.S., A.A. Abdel-Monem and A.A. Radain, 1984b. Rb-Sr dating and petrochemistry of Urn Gerig granitic rocks (Rabigh Area), western Saudi Arabia. Faculty of Earth Sciences King Abdulaziz University Bulletin 6, p. 233-248.
Al Shanti, A.M.S. and A.H.G. Mitchell, 1976. Late Precambrian subduction and collision in the Al Amar-Idsas region, Arabian Shield, Kingdom of Saudi Arabia. Tectonophysics, v. 30, p. T41-T47.
Bakor, A.R. , I.G. Gass and C.R. Neary, 1976. Jabal al Wask, northwest Saudi Arabia: an Eocambrian back-arc ophiolite. Earth Planet. Sci. Lett., v. 30, p. 1-9.
Basta, F.F., 1983. Geology and geochemistry of the ophiolitic melange and other rock units in the area around and west of Gebel Ghadir, Eastern Desert, Egypt. Ph.D. thesis, Cairo University, 137p.
Bokhari, F.Y. and J.D. Kramers, 1981. Island arc character and late Precambrian age of volcanics at Wadi Shwas, Hijaz, Saudi Arabia: geochemical and Sr and Nd isotopic evidence. Earth Planet. Sci. Lett., v. 54, p. 409-422.
Bryan, W.B., 1978. Regional variation and petrogenesis of basalt glasses from the FAMOUS area, Mid-Atlantic ridge. J. Petrol., v. 20, p. 293-325. Caby, R., 1984. Pan-African evolution of the Tuareg Shield (Central Sahara) and the Arabian Shield: a comparison. Faculty of Earth Sciences King Abdulaziz University Bulletin 6, p. 23-25.
Calvez, J.Y., C. Alsac, J. Delfour, J. Kemp and C. Pellaton, 1984. Geological evolution of the western, central and eastern parts of the Northern Precambrian Shield, Kingdom of Saudi Arabia. Faculty of Earth Sciences, King Abdulaziz University, Bulletin 6, p. 23-48.
Calvez, J. Y., J. Delfour and J.L. Feyhesse, 1985. 2000 million-yr old inherited zircons in plutonic rocks from the Al Amar region: New evidence for an early Proterozoic basement in the Eastern Arabian Shield; Saudi Arabian Deputy Ministry for Min. Res. Rep. BRGM-OF-05-11,27p. , .
Camp, V.E., 1984. Island arcs and their role in the evolution of the western Arabian Shield. Geol. Soc. America Bull., v. 95, p. 913-921.
Church, W.R., 1979. Granitic and metamorphic rocks of the Taif area, western Saudi Arabia; discussion. Geol. Soc. America Bull., v. 90, p. 893-896.
Church, W.R., 1980a. Late Proterozoic Ophiolites. Orogenic Mafic and Ultramafic Association, Colloques Internationaux du Centre National de la Recherche Scientifique No. 272, p. 105-118.
Church, W.R. 1980b. Geology of the Jabal Idsas-Jabal Tays-Jabal Zriba areas in the Eastern Arabian Shield. Newsletter - "Pan-African Crustal Evolution in the Arabian-Nubian Shield", v. 3, p. 53-57.
Church, W.R., 1983. Late Precambrian evolution of Afro-Arabian crust from ocean arc to craton; discussion. Geol. Soc. America Bull., v. 94, p. 679-681.
Church, W.R., 1987. Discussion of 1.0. Oshin and J.H. Crocket, 1985. The geochemistry and petrogenesis of ophiolitic volcanic rocks from Lac de 1'Est, Thetford Mines Complex, Quebec, Canada. Canadian J. Earth Sci., v. 23, p. 202-213 (in press)
Church, W.R. and L. Riccio, 1977. Fractionation trends in the Bay of Islands ophiolite of Newfoundland: polycyclic cumulate sequences in ophiolites and their classification. Can. J. Earth Sci., v. 14, p. 1156-1165.
Claesson, S., J.S. Pallister and M. Tatsumoto, 1984. Samanum- neodymium data on two late Proterozoic ophiolites of Saudi Arabia and implications for crustal and mantle evolution. Contrib. Mineral. Petrol., v. 85, p. 244-252.
Coish, R.A. and W.R. Church, 1979. Igneous geochemistry of mafic rocks in the Betts cove ophiolite, Newfoundland. Contrib. Mineral. Petrol., v. 70, p. 29-39.
Coish, R.A., R. Hickey and F.A. Frey, 1982. Rare element geochemistry of the Betts Cove ophiolite, Newfoundland:complexities in ophiolite formation. Geochim. Cosmochim. Acta, v. 46, p. 2117-2134.
Crawford, A.J., L. Beccaluva and G. Serri, 1981. Tectono- magmatic evolution of the West Philippine region and the origin of boninites. Earth Planetary Sci. Letters, v. 54, p. 346-356.
Delfour, J., 1982. Geologic, tectonic and metallogenic evolutions of the northern part of the Precambrian Arabian Shield (Kingdom of Saudi Arabia). Bull. BRGM (deuxieme serie) 2, p. 1-19.
Desmet, A., 1977. Contribution a 1'etude de la croute oceanique mesozoique de Mediterranee orientale: Les Pillow-lavas du Troodos (Cypre). D.SST thesis, 1'Universite de Nancy, 221p.
Dixon, T.H., 1979. The evolution of continental crust in the Late Precambrian Egyptian Shield. Ph.D. thesis. University of California, San Diego, 230p.
Dixon, T.H., 1981. Age and chemical characteristics of some pre-Pan-African rocks in the Egyptian Shield. Precambrian Res., v. 14, p. 119-133.
Duyverman, H.J., 1984. Late Precambrian granitic and volcanic rocks and their relation to the cratonisation of the Arabian Shield. Faculty of Earth Sciences King Abdulaziz University Bulletin 6., p. 50-69.
El Ageed, A.I. and S.M. El Rabaa, 1981. The geology and structural evolution of the northeastern Nuba Mountains, southern Kordofan Province, Sudan. Bull. Geol. Miner. Res. Dept. Sudan, p. 1-50.
El Bayoumi, R.M., 1980. Ophiolites and associated rocks of Wadi Ghadir, east of Gebel Zabara, Eastern Desert, Egypt. Ph.D. thesis, Cairo University, 227p.
El Bayoumi, R.M., 1984. Ophiolites and melange complex of Wadi Ghadir area. Eastern Desert of Egypt. Faculty of Earth Sciences King Abdulaziz University Bulletin 6, p. 329-342.
El Bayoumi, R.M.A. and R. Greiling, 1984. Tectonic evolution of a Pan-African plate margin in southeastern Egypt - a suture zone overprinted by low angle thrusting. In: J. Klerkx and J. Mi.chot (eds). Geologie africaine - African Geology, p. 47-56.
El Ramly, M.F., R. Greiling, A. Kroner and A.A.A. Rashwan, 1984. On the tectonic evolution of the Hafafit area and environs. Eastern Desert of Egypt. Faculty of Earth Sciences King Abdulaziz University Bulletin 6, p. 113-126.
El Sharkawi, M.A. and R.M. El Bayoumi, 1979. The Ophiolites of Wadi Ghadir area. Eastern Desert, Egypt. Annals Geol. Surv. Egypt, v. 9, p. 125-135.
Embleton, J.C.B., D.J. Hughes, P.M. Klemenic, S. Poole and J.R. Vail, 1984. A new approach to the stratigraphy and tectonic evolution of the Red Sea Hills, Sudan. Faculty of Earth Sciences King Abdulaziz University Bulletin 6, p. 101-112.
Engel, A.E.J., T.H. Dixon and R.J. Stern, 1980. Late Precambrian evolution of Afro-Arabian crust from ocean arc to craton. Geol. Soc. America Bull., v. 91, p. 699-706.
Fitches, W.R., R.H. Graham, I.M. Hussein, A.C. Ries, R.M. Shackleton and R.C. Price, 1983. The late Proterozoic ophiolite of Sol Hamed, NE Sudan. Precambrian Res., v. 19, p. 385-411.
Frey, F.A., J.S. Dickey Jr. , G. Thompson, W.B. Bryan and H.L. Davies, 1980. Evidence for heterogeneous primary MORB and mantle sources, NW Indian Ocean. Contr. Mineral. Petrol., v. 74, p. 387-402.
Frisch, W. and A.M.S. Al-Shanti, 1977. Ophiolite belts and the collision of island arcs in the Arabian Shield. Tectonophysics, v. 43, p. 293-306.
Garson, M.S. and I.M Shalaby, 1976. Precambrian-Lower Palaeozoic plate tectonics and metallogenesis in the Red Sea region. Special Paper Geological Association of Canada, v. 14, p. 573-96.
Gass, I.G., 1977. The evolution of the Pan-African crystalline basement in NE Africa and Arabia. J. Geol. Soc. London, v. 134, p. 129-38. Gass, I.G., 1979. Evolutionary model for the Pan-African crystalline basement. Bull. Inst. Appl. Geol. Jeddah, v. 3, (1), p. 11-20.
Greenwood, W.R., D.G. Hadley, R.E. Anderson, R.J. Fleck and D.L. Schmidt, 1975. Late Proterozoic cratonization in southwestern Saudi Arabia. U.S. Geol. Survey Saudi Arabian Project Rept. 196, 23p.
Greenwood, W.R., D.G. Hadley, R.E. Anderson, R.J. Fleck and D.L. Schmidt, 1976. Late Proterozoic cratonization in southwestern Saudi Arabia. Phil. Transact. R. Soc., Ser. A, v. 280, p. 517-527.
Habib, M.E., A.A. Ahmed and O.M. El Nady, 1985. Two orogenies in the Meatiq area of the Central Eastern Desert, Egypt. Precambrian Res., v. 30, p. 83-111.
Hadley, D.G. and D.L. Schmidt, 1980. Proterozoic sedimentary rocks and basins of the Arabian Shield and their evolution. Bull. Inst. Appl. Geol. Jeddah, v. 3, (4), p. 26-50.
Harper, G.D., 1984. The Josephine ophiolite, northwestern California. Geol. Soc. America. Bull., v. 95, p. 1009-1026.
Harris, N.B.W., C.J. Hawkesworth and A.C. Ries, 1984. Crustal evolution in North-East and East Africa from model Nd ages. Nature, v. 309, p. 773-776. Hussein, I.M., 1981. An outline of the geology and structure of the Sol Hamed ophiolite of the Halaib area, northern Red Sea Hills, Sudan. Newsletter - "Pan-African Crustal Evolution in the Arabian-Nubian Shield", v. 4, p. 19-25.
Hussein, I.M., A. Kroner and St. Diirr, 1984. Wadi Onib - a dismembered Pan African ophiolite in the Red Sea Hills of the Sudan. Faculty of Earth Sciences King Abdulaziz University Bulletin 6, p. 319-328.
Jackson, N. , A. Kroner, W.R. Church and A. Hashad, 1980. Notes on some stratigraphic relationships in the J.I. area. Newsletter. Pan-African Crustal Evolution in the Arabian- Nubian Shield, No. 3, p. 16-17.
Kabesh, M.L., 1961. The geology and economic minerals and rocks of the Ingessana Hills. Bull. Geol. Surv. Sudan, v. 11, p. 1-61.
Kazmin, V., A. Shifferaw and T. Balcha, 1978. The Ethiopian Basement: stratigraphy and possible manner of evolution. Geol. Rundschau, v. 67 (2), p. 531-546.
Kemp, J., C. Pellaton and J.-Y. Calvez, 1982. Cycles in the chelogenic evolution of the Precambrian shield in part of north western Saudi Arabia. Prof. Paper Saudi Arabian Dir. Gen. Mineral. Res., v. 1, p. 27-41.
Klemenic, P.M., 1985. New geochronological data on volcanicrocks from Northeast Sudan and their implication for crustal evolution. Precambrian Res., v. 30, p. 263-276.
Kroner, A., 1985. Ophiolites and the evolution of tectonicboundaries in the Late Proterozoic Arabian-Nubian Shieldof northeast Africa and Arabia. Precambrian Res., v. 27, p. 277-300.
Kroner, A., M. Halpern and A. Basahel, 1984. Age and significance of metavolcanic sequences and granitoid gneisses from the Al-Lith area, southwestern Arabian Shield. Faculty of Earth Sciences King Abdulaziz University Bulletin 6, p. 380-388.
Le Metour, J., V. Johan and M. Tegyey, 1982. Relationships between ultrabasic to basic complexes and volcanicsedimentary series in the Precambrian of the Arabian Shield. Saudi Arabian Deputy Ministry for Miner. Res. Open-File Report BRGM-OF-02-21, 42p.
Maboko, M.A.H., N.A.I.M. Boelrijk, H.N.A. Priem and E.A.Th. Verdurmen, 1985. Zircon U-Pb and biotite Rb-Sr dating of the Wami River granulites, eastern granulites, Tanzania: evidence for approximately 715 Ma old granulite-facies metamorphism and final Pan-African cooling approximately 475 Ma ago. Precambrian Res., v. 30, p. 361-378.
Murton, B.J., 1986. Anomalous oceanic lithosphere formed in a leaky transform fault: evidence from the western Limassol Forest complex, Cyprus. J. Geol. Soc. London, v. 143, p. 845-854.
Nasseef, A.O. and I.G. Gass, 1977. Granitic and metamorphic rocks of the Taif area. Western Saudi Arabia. Geol. Soc. America Bull., v. 88, p. 1721-1730.
Nassief, M.O., R. MacDonald and I.G. Gass, 1984. The Jebel Thurwah Upper Proterozoic Ophiolite complex, western SaudiArabia. J. Geol. Soc. London, v. 141, p. 537-546.
Nawab, Z.A., 1979. Geology of the Al-Amar-Idsas region of the Arabian Shield. Bulletin Institute of Applied Geology, Jeddah, v. 3, (4), p. 29-40.
Neary, C.R., I.G. Gass and B.J. Cavanagh, 1976. Granitic association of northeastern Sudan. Geol. Soc. America Bull., v. 87, p. 1501-12.
Pearce, J.A., S.J. Lippard and S. Roberts, 1984. Characteristics and tectonic significance of supra-subduction zone (ssz) ophiolites. In: B.P. Kokelaar, and M.F. Howells (eds). Special Publication of the Geological Society, v. 16, p. 77-94.
Ries, A.C., R.M. Shackleton, R.H. Graham and W.R. Fitches, 1983. Pan-African structures, ophiolites and melange in the Eastern Desert of Egypt: a traverse at 26 N. J. Geol. Soc. London, v. 140, p. 75-95.
Ries, A.C., R.M. Shackleton and A.S. Dawoud, 1985. Geochronology, geochemistry and tectonics of the NE Bayuda Desert, N. Sudan: implications for the Western Margin of the Late Proterozoic fold belt of NE Africa. Precambrian Res., v. 30, p. 43-62.
Rittmann, A., 1958. Geosynclinal volcanism, ophiolite and Barramiya rocks. Egyptian Journal of Geology, v. II, p. 61-65.
Robinson, P.T., W.G. Melson, T. O'Hearn and H.-U. Schmincke, 1983. Volcanic glass compositions of the Troodos ophiolite, Cyprus. Geology, v. 11, p. 400-404.
Le Roex, A.P., H.J.B. Dick, A.J. Eriank, A.M. Reid, F.A. Frey and S.R. Hart, 1984. Geochemistry, mineralogy, and petrogenesis of lavas erupted along the Southwest Indian ridge between the Bouvet Triple Junction and 11 degrees east. Journal Petrology, v. 24, p. 267-318.
Roobol, M.J., C.R. Ramsay, N.J. Jackson and D.P.F. Darbyshire, 1983. Late Proterozoic lavas of the Central Arabian Shield - evolution of an ancient volcanic system. J. Geol. Soc. London, v. 140, p. 185-202.
Sacchi, R., J. Marques, M. Costa and C. Casati, 1984. Kibaran events in the southernmost Mozambique belt. Precambrian Res., v. 25, p. 141-159.
Saunders, A.D. and J. Tarney, 1984. Geochemical characteristics of basaltic volcanism within back-arc basins. In: B.P. Kokelaar and M.F. Howells (eds). Special Publication of the Geological Society, v. 16, p. 59-76.
Schmidt, D.L., D.G. Hadley and D.B. Stoeser, 1979. Late Proterozoic crustal history of the Arabian Shield, southern Najd Province, Kingdom of Saudi Arabia. Bull. Inst. Appl. Geol. Jeddah, v. 3, (2), p. 41-58.
Serri, G., 1981. The petrochemistry of ophiolite gabbroic complexes: a key for the classification of ophiolites into low-Ti and high-Ti types. Earth Planetary Science Letters, v. 52, p. 203-212.
Shackleton, R.M., 1979. Precambrian tectonics of North-East Africa. Bull. Inst. Appl. Geol. Jeddah, v. 3, (2), p. 1-7.
Shackleton, R.M., A.C. Ries, R.H. Graham and W.R. Fitches, 1980. Late Precambrian ophiolitic melange in the eastern desert of Egypt. Nature, v. 285, p. 472-474.
Shanti, M., 1984. The Jabel Ess ophiolite. Faculty of Earth Sciences King Abdulaziz University Bulletin 6, p. 289-318.
Shanti, M. and M.J. Roobol, 1979. A late Proterozoic ophiolite complex at Jabal Ess in northern Saudi Arabia. Nature, v. 279, p. 488-91.
Shimron, A.E., 1984. Evolution of the Kid Group, southeast Sinai Peninsula: thrusts, melanges, and implications for accretionary tectonics during the late Proterozoic of the Arabian-Nubian Shield. Geology, v. 12, p. 242-247.
Shukri, N.M and M.S. Mansour, 1980. Lithostratigraphy of Urn Samuiki district. Eastern Desert, Egypt. Bull. Inst. Appl. Geol. Jeddah, v. 3, (4), p. 83-94.
Stacey, J.B. and A. Agar, 1985. U-Pb isotopic evidence for the accretion of a continental microplate in the Zaim region of the Saudi Arabian Shield. J. Geol. Soc. London, v. 142, p. 1189-1204.
Stacey, J.S. and C.E. Hedge, 1984. Geochronologic and isotopic evidence for early Proterozoic crust in the eastern Arabian Shield. Geology, v. 12, p. 310-313.
Stern, R.J., 1979. Late Precambrian ensimatic volcanism in the Central Eastern Desert of Egypt. Ph.D. thesis. University of California, San Diego, 210p.
Stern, R.J., D. Gottfried and C.E. Hedge, 1985. Discussion of A.E. Shimron, 1984. Evolution of the Kid Group, southeast Sinai Peninsula: thrusts, melanges, and implications for accretionary tectonics during the late Proterozoic of the Arabian-Nubian Shield. Geology, v. 13, p. 155.
Stern, R.J. and C.E. Hedge, 1985. Geochronologic and isotopic constraints on late Precambrian crustal evolution in the Eastern Desert of Egypt. American J. Sci., v. 285, p. 97-127.
Stoeser, D.B. and V.E. Camp, 1985. Pan-African microplate accretion of the Arabian Shield. Geol. Soc. America Bull., v. 96, p. 817-826.
Stoeser, D.B., R.J. Fleck and J.S. Stacey, 1984. Geochronology and origin of an early Tonalite Gneiss of the Wadi Tarib Batholith and the formation of syntectonic gneiss complexes in the Sotheastern Arabian Shield, Kingdom of Saudi Arabia. Faculty of Earth Sciences King Abdulaziz University Bulletin 6, p. 351-364.
Sturchio, N. , M. Sultan, P. Sylvester, R. Batiza, C. Hedge, E.M. El Shazly and A. Abdel-Meguid, 1984. Geology, age, and origin of the Meatiq dome: implications for the Precambrian stratigraphy and tectonic evolution of the Eastern Desert of Egypt. Faculty of Earth Sciences King Abdulaziz University Bulletin 6, p. 127-144.
Vail, J.R., 1985. Pan-African (late Precambrian) tectonic terrains and the reconstruction of the Arabian-Nubian shield. Geology, v. 13, p. 839-842.
Varne, R. and M.J. Rubenach, 1972. Geology of Macquarie island and its relationship to oceanic crust. In: D.E. Hayes (ed). Antarctic Oceanology II: The Australian-New Zealand sector. Antarctic Research Series, v. 19, p. 251-266.