IRON ORE DEPOSITS IN EGYPT

Lecture 9:
Hassan Z. Harraz
hharraz2006@yahoo.com
2016- 2017
@ Hassan Harraz 2017

Outline of Lecture 9:
EGYPTIAN IRON ORE DEPOSITS
Iron ore deposit of sedimentary nature
 Sinai: Gabal Halal iron ore deposit
Western Desert:
 Aswan iron Ore Deposits
 Bahariya iron Ore Deposits
• The Banded Iron ore deposits (BIFs)
• Geologic Setting
• General Characteristics of the Egyptian Banded Iron Ores
• Are the Egyptian Banded Iron Ores Unique? Genesis of Egyptian Banded Iron
Formation
We will explore all of the above in Topic 9.
2

Figure 1: Distribution of iron deposits in Egypt .
This figure shows the distribution of iron ores and iron oxide traces all over Egypt. Most of the
locations are inter-related in origin to each other. The trend of the iron oxides in Western Desert points
out to a common source of the iron deposits in this area.
@ Hassan Harraz 2017 4

EGYPTIAN IRON ORE DEPOSITS
In Egypt economic iron ore deposits occur in two natures (or
forms):
i) Iron ore deposit of sedimentary nature
(Ironstone)
(Sedimentary iron ore deposit is a very limited occurrence, being
found only in the 2 localities in the Western Desert and one locality
in Sinai):-
 Sinai: Gabal Halal iron ore deposit
 Western Desert:
 Aswan iron Ore Deposits
 Bahariya iron Ore Deposits
and
ii) The Banded Iron ore deposits (BIFs)
(BIFs have being found only in the 13 localities in the central Eastern
Desert)

I) Iron ore deposit of sedimentary nature
Sedimentary iron ore deposit is a very limited occurrence, being found only in the:-
One locality in Sinai : Gabal Halal iron ore deposit
Two localities in the Western Desert
 Aswan iron Ore Deposits
 Bahariya iron Ore Deposits
Sinai: Gabal Halal iron ore deposit
 It is located ~4 km NW Sir Hadhira, Sinai (El-Far, 1965).
 This area contain oolitic iron ores of lower Cretaceous age that
extending ~8 km.
 The iron ore were found in two beds separated by 14 m sandstones:
 The lower bed (~2.65 m in thickness) is a yellowish-brown
and compact bed mainly oolitic.
 The upper bed (~5 m in thickness) is a typical oolitic iron ore.
Main ore minerals: goethite and hematite.
Gangue minerals: clay minerals, quartz, calcite-dolomite, and sulphate
minerals.

I) Iron ore deposit of sedimentary nature
Gabal Halal iron ore deposit
 It is located ~4 km NW Sir Hadhira, Sinai (El-Far, 1965).
 This area contain oolitic iron ores of lower Cretaceous age that extending ~8
km.
 The iron ore were found in two beds separated by 14 m sandstones:
 The lower bed (~2.65 m in thickness) is a yellowish-brown and
compact bed mainly oolitic.
 The upper bed (~5 m in thickness) is a typical oolitic iron ore.
Main ore minerals: goethite and hematite.
Gangue minerals: clay minerals, quartz, calcite-dolomite, and sulphate minerals.
Sinai:
Iron associated with manganese east of Abu Zenima has economic significance
as a by-product of manganese extraction, potentially accounting for the
difference between profit and loss.
Passing references occur in some reports to ferruginous horizons with oolitic
hematite in Cretaceous Nubian sandstones of the Plateau Province.
Micaceous hematite is known to occur in quartz veins in eastern Sinai, in
granite at Gebel Abu Mesud.

Iron ore deposit in Western Desert
Economic iron ore deposit of sedimentary nature, being found in the 2 localities
in the Western Desert.
Sedimentary iron ore types only occur in
 Upper Cretaceous (Senonian) sediments  East of Aswan
 Middle Eocene sediments  north of the Bahariya oases
Note:
 Senonian The final Cretaceous epoch which is dated at 88.5–
65 Ma ( Harland et al., 1989) and comprises the Coniacian,
Santonian, Campanian, and Maastrichtian Ages.
 Some authors do not include the Maastrichtian Age within the
Senonian.

Egyptian Ore Deposits
Items Bahariya Oasis mine Aswan mine
Age Middle Eocene Senonian (Upper Cretaceous)
Ore Type Hard-massive, Banded-cavernous,
Friable, and Oolitic- pisolitic
Oolitic hematite (dark red with a bluish
metallic tinge in place)
Ore Minerals • Mainly of hematite, goethite, and
hydrogoethite, with occasional
pockets of softly ochre and
lepidocordite, chamosite,
magnetite, psilomelane, and
pyrolusite.
• Pyrite and chalcopyrite occur as
rare minute single grains.
Mainly hematite with minor goethite
Gangue minerals Barite, kaolinite, glauconite, alunite,
chert, gypsum, calcite, chlorite, and
Tripoli
Quartz, gypsum, halite, glauconite and
clay minerals
Average iron content (%) 53.4 43
Average silica content (%) 6.1 18
Average phosphorous content (%) 0.21 1.1
Specific gravity (gm/cc) 3.45-4.35
Mineable Geological Reserve
(m.t.)
140
(126.7?)
El-Gedida 14
136
(142.6?)
Ghorabi
Nasser
El-Harra
Average thickness of iron bed (m) 13 0.7
Stripping ratio 0.185 2.5
Mine area (km2) 6 600
Ultimate Annual production (m.t.) 3.3 (2.5) 0.5
Distance from mine to plant at Helwan
(km)
330 850
Production cost of one ton
(Egyptian pound)
18.020
On 2004
8.865
On 1975
Number of labourers 503
on 2004
1400
On 1975
Compared between Aswan and Bahariya iron ore Deposits

Western Desert
i) Aswan iron Ore Deposits
 Economic iron has been produced from East
Aswan regions since Pharaonic times (1580 to
1380 B.C.) until 1973.
 In recent years it was the main supply of iron
ores for the Egyptian iron and steel industry till
1973 when it was replaced by Bahariya iron ore.
 The main occurrence located East of Aswan
(Kom-Ombo, Lake Naser), while small deposits
are also encountered in the variegated shales
along the Nile Valley to the south at Kalabsha,
Garf Hussein, Kurusko, and Abu Simbil.

Fig. 2. (A) Geological map of East Aswan shows the location of study samples from Wadi Abu Sobera and Wadi Abu
Agag areas. (B) Geological map of the Um Hibal area showing the locality of the iron-bearing formation. (A: after
Mucke (2000); B: after Ghazaly et al. (2015)). 12

Fig. 3. General stratigraphic column of
the late Cretaceous sedimentary cover
in Aswan area. (After El Sharkawi et
al., 1996).
13

Figure 1. Location map of the study area (up left), its main geologic topographic and iron ore localities illustrated on Landsat 8 false
color bands 7,4,2.
Salem, S.A. and E.A. El Gammal, E.A. (2015): Iron ore prospection East Aswan, Egypt, using remote sensing techniques. The
Egyptian Journal of Remote Sensing and Space Science, Volume 18, Issue 2,, 195–206. http://dx.doi.org/10.1016/j.ejrs.2015.04.003

Types of iron-ore
 tThe ore is a bedded oolitic type of Senonian age in the form of three bands
interbedded with Ferruginous sandstone and clay/Ferruginous concretion
capping Precambrian rocks.
 Three ypes of iron-ore have been distinguished in the provided areas (Salem and El
Gammal, 2015) :
(1) Ferruginous sandstone iron-ore (up to 70.46% Fe2O3 content),
(2) Oolitic iron-ore (attains 54.24% Fe2O3 content); and
(3) Ferruginous concretion iron-ore(up to 63.2% Fe2O3 content).
The Oolitic iron-ore shows P2O5 and S contents exist in relatively higher proportions
than in the ferruginous sandstone and ferruginous concretions. This is due to the
particular bioactivity in the marine environment of formation of the Oolitic ore.
Its low manganese content may be attributed to the low pH exhibited by the
leaching solutions, which dissolved the slightly basic iron with small amounts of
strongly acidic manganese.
In spite of the less contents of Fe2O3 = 54.24 and Fe = 37.94 in the Ooloitic iron ore
relative to the other ore types, it is considered as an important type due to its
dominance and distribution in the east of Aswan district, as well as the
deficiency in silica and MnO add a promise potential to the Ooloitic iron ore.

Figure 7. Ferruginous sandstone iron ore illustrations (Salem and El Gammal, 2015). (a) Ferruginous sandstone thin beds in
Wadi Timsah hill. (b) Paleosole surface rich in iron oxides in the Nubian sandstone beds, Wadi Anid. (c) Ferruginous
sandstone cracked beds hand specimen (hs). (d) Ferruginous sandstone hs. (e) Limonite rich ferruginous sandstone hs. (f)
Ferruginous sandstone with calcite and Gibbsite.
Iron ore prospection East Aswan,
1) Ferruginous sandstone occurred and
was distributed in the lower parts of Timsah
Fm which was composed of fluviatile near-
shore marine and locally eolian fine-to
medium-grained sandstone with interbedded
channel and soil deposits.
Iron ore was found as inliers and caps and
in the paleosole surfaces of the Nubian
sandstone beds, forming hematite and
goethite strata having thickness varying from
50 cm to 4 m occuring at Gabal Timsah, Wadi
Timsah and Wadi Anid (Fig. 7a and b).
The iron ore is syn-genetic bedded of
Senomanian age, formed under lacustrine
environment. The gangue minerals
associated with the iron ore deposits include
quartz, gypsum, glauconite, and clay
minerals.
The hand specimens exhibit fine bedding
and plugs in red and brown to black colors
including limonite patches in yellow color (Fig.
7c–f).

Figure 8. The Oolitic iron-ore illustrations (Salem and El Gammal, 2015). (a) General view, Gabal Abu
Hashim. (b) Spherical Oolitic grains hs. (c) Oolitic hematitic glauconitic coarse grains hs. (d) Hematitic
rich Oolites hs.
2) Oolitic iron-ore is the more
dominant, most important and
valuable iron ore type in the study
district in spite of its low content of the
Fe2O3 relative to the other types.
It is found as compact beds vary in
thicknesses from 1–3 m. distributed
and alternated through the upper parts
of the Temsah Fm in Gabal Abu
Hashim, Gabal Nugur and Gabal
Naag areas of dark-red, Oolitic
hematite (Fig. 8a).
The oolites are cemented by pure
amorphous hematitic material and
ferruginous silica; therefore the iron-
content of the matrix is less than that
of oolites.
In the hand specimens, the Oolitic
hematitic grains are easily seen by the
naked eye varying in sizes in different
specimens and even in the same
specimen (Fig. 8b–d).

Figure 9. The Ferruginous concretion iron-ore illustrations (Salem and El Gammal, 2015). (a) Ferric-duricrust surfaces of
ferruginous concretion and substratum in Wadi Quffa. (b) Hard compact masses of ferruginous concretion beds. (c) Fine
intersected beds in Ferruginous concretion in Wadi Timsah. (d) Hematite-goethite coarse grained in Ferruginous concretion hs.
(e) Blocky Ferruginous concretion hs. (f) Gebsite, and clay minerals in Ferruginous concretion hs.
3) Ferruginous concretion iron-ore
The Ferruginous concretion iron-ore form hard
compact masses of concretion beds and substratum
rich in iron-ore, found as ferric-duricrust surfaces
between isolated Nubia sandstone hills and
mountains through Wadis Timsah, Quffa, Anid,
Umm Udi and Abu Aggag (Fig. 9a,b).
The ferric-duricrust beds formed from
fragments accumulation of ferruginous sandstone,
Oolitic iron-ore and ferruginous concretions which
was already formed due to the action of surface
water on the valleys floor (in wadi fill).
The thicknesses of the glauconitic coarse grains
hs. (Fig. 9d) Hematitic rich Oolites hs. ferric-duricrust
beds vary from 10 to 60 cm, showing fantastic
outlines formed by precipitations from aqueous
solution in porous sedimentary rocks.
Due to the denudation of the sandstone
containing hematite concretions and owing to their
resistance to weathering, they were often seen
accumulating in great quantities in places on the
ground surface giving it black and red colors. In the
hand specimens, the concretions show hematite-
goethite rich grain aggregations cemented in coarse
grained matrix of black and brown color s (Fig. 9c–f).

Over hanging layer of oolitic
Iron, Wadi Abu Aggag Aswan

 The thickness of the bands varies from 20 up to 350 m.
 Iron ore deposits occur in Senonian (upper Cretaceous)
sediments ~7,000,000 tonnes were produced between 1956
and 1973.
 The estimated reserves are 121 to 135 million tonnes with 20
million tonnes proved reserves with average content of 46.8%
Fe (Attia. 1955).
Ore
 The ore is oolitic hematite, dark red with a bluish metallic tinge
in place, compact and dense (Sp.gr. 3.45-4.35 gm/cc).
 Ore minerals: are mainly hematite with minor goethite. The
hematite is occur in oolitic form range from 1-1.5 mm in
diameter and is cemented by a compact hematitic matrix.
 Gangue minerals: include quartz, gypsum, halite, glauconite
and clay minerals.
Fe
31.2 - 62.3 %
(average 46.8%)
SiO2
5 - 31%
(average 14.1%)
Mn up to 1.3%
S up to 0.3%
P 0.4 - 3.5%
 The oolites themselves contain 60% of Fe
while matrix contains 40% of the iron.

Discussion
The east of Aswan area is a suitable environment for iron ore occurrences due
to the following reasons:
(1) Presence of huge Nubia sandstone rocks which formed from the
compilations and accumulation of old rock fragments and deposits
including iron.
(2) The aquatic marine environment present in the study area is suitable for
leaching, precipitating and deposition of iron oxides from the iron rich
solutions in the sandstone terrain as hematite and limonite.
(3) Varied topography between the basement and sedimentary rocks traced
by intermountain substratum and basins are suitable for collection and
catchment of different debris, rock fragments, slags, and wadi deposits
with iron constituents. These factors motivated us to study the surface
geology of this area exploring and locating the iron ore deposits through
the exposed rocks and landforms.
The marine encroachments in the Cretaceous part of the east of Aswan area
attained N–S to SE directions forming depositional basins (Issawi, 1981). Iron
ore in the east of Aswan is considered by (Hussein, 1990) to have been formed
under lacustrine conditions, during the deposition of Senomanian sediments.
The sedimentary iron deposits are invariably confined to the middle series of
the Nubian sandstone formations which lie unconformably on the basement
rocks. The iron oxide bands are often associated to ferruginous sandstones and
clays. Transitions from ferruginous sandstone to Oolitic iron deposits are often
encountered (Adelsberger and Smith, 2009).

Gneiss
 Ore is considered to have formed under
sedimentary lacustrine to fluviomarine
conditions during the deposition of Upper
Cretaceous (Senonian) sediments of Aswan
embraces all the non-marine to marginal
and shallow marine siliciclastics exposed in
the Nubia area.
 The iron is mostly dissolved from bottom
sediments and mobilized in so-called
"carbon-dioxide zone" as ferrous
bicarbonate, then precipitated in an
oxidizing environment as ferric hydroxide.

II) Western Desert:
Bahariya iron Ore Deposits
• The Bahariya oasis is located in central plateau
of Western Desert between 27° 48/ -28° 30/ N
and 28° 55/ - 29° 10/ E.
• Its northern edge is located along the contact
between the stable and unstable shelves.

Gebel El-Maghrafa
Gebel El- Dist

Geologic map of the Bahariya area

Geologic map of the northern Bahariya area (after Said and Issawi, 1964)

The iron ore of El Harra belongs to El Harra member of El Haffuf
Formation; whereas El Gedida iron ore belongs to Naqb Formation.
The area is covered by Bahariya Formation (unfossiliferous varicolored
sandstone of Cenomanian age) followed by El Heiz Formation
(brownish limestone and sandy clay beds), and El Haffuf Formation of
sandstone, sandy clay, and ferruginous beds, which are partly taken by
the iron ore deposit, Khuman Formation (chalky limestone), and Naqb
Formation of thick limestone beds with few marl and clay associations.
The iron content in the ironstone deposits ranges from 30% to 58% Fe,
and the manganese content ranges from 0.7% to 7.66% Mn .
The stratigraphic position of Naqb Formation is partly taken by iron ore
deposits at El Gedida, El Harra, and Ghorabi; where El Gedida iron ore
member belongs to iron deposits of Lower Middle Eocene (Naqb
Formation) and the upper Eocene (Abu Maharik Formation. The ore is
localized in the crest of anticline.

Fig. 6. A. Panoramic view of the Naqb Formation showing ironstone beds and clay
intercalations (white arrows) arranged in two sequences. B. Outcrop view of the
ironstone succession exposed at the central part of El Gedida mine (X is the location of
the collected fossil sample). (after Afify et al., 2016)

A composite section (not at scale) of the main
Eocene lithostratigraphic and
chronostrigraphic units and shallow benthic
foraminiferal zones (SBZs) after Serra-Kiel et
al. (1998). The shallow benthic zones written
in red color are re-interpreted after previous
dating by Boukhary et al. (2011) and Said and
Issawi (1964). The violet shaded rectangle is
the relative timing proposed for the iron
mineralization. (For interpretation of the
references to colour in this figure legend, the
reader is referred to the web version of this
article.)

The other areas: Ghorabi, Nasser, El Heiz, and El Harra are of low
grade ores and of high manganese content. In addition, these areas
have relatively thick overburden.
These occurrences are called El Gedida, Ghorabi, Nasser and El Harra,
extending over 11.7 km2; and the ore thickness varies from 2 to 25 m
(averaging 9 m).
The deposits are under laid unconformably by the Bahariya formation
sandstones and overlaid by the Redwan formation.
The iron ore deposits are generally irregular in outline. They form a
succession of beds which are concordant with local dips (~4°).
The ore is thought to be localized in the crests of two major anticlines
trending in a NE-direction. El Gedida and El Harra ore deposits are localized
on the eastern anticline, while Ghorabi and Nasser are on the western
anticline.
The high-grade ores exist in the crests and that low-grade ores are
localized in the limbs of the anticlinal structures.
Major faults disturb the peripheries of the ore bodies, forming the major
wadis which surround the area of the iron ore deposits. Many small faults
affect the iron beds in the four areas. These structure natures of the folds
apparent to be generated by faulting affiliated with the Pelsuium mega-
shear, along which the Bahariya oasis are located (Neev et al., 1982).

1.1.1. Forms, Shapes and Textures
 Several forms characterize the constituents of the ore
deposits such as massive crystalline, crystal aggregates,
granular, botryoidal-shape, kidney-shaped, oolitic, pisolitic,
pseudoolites (spheroids), subspherulitic, and sponges.
 Therefore, several textures are recognized in the ore deposits
such as banded, disseminated, cavity filling, cavernous, and
replacing.
1.1.2. Mineralogy
 Main ore minerals: hematite, goethite, Limonite, and
hydrogoethite, with occasional pockets of softly ochre and
lepidocordite, chamosite, magnetite, psilomelane, and
pyrolusite.
Pyrite and chalcopyrite occur as rare minute single
grains.
 Gangue minerals: barite, kaolinite, glauconite, alunite,
chert, gypsum, calcite, chlorite, and Tripoli

Glauconite and Fe-rich chlorite
Rich Ore
Wadi area
(Western)
Barite Zone
Sands and Sandy clays
(Overburden)
Quartzite sandstone and
conglomerate (Radwan
Formation)
Unconformity
Intercalations
Footwall
(Bahariya Formation)
Barite patches
Saliferous Ore
High Central Area
Intercalations of clays, sand,
chert concretions and alunites
Mn rich
Wadi area
(Eastern)
East

Detrital Barite

Detrital Barite
•‫البحرية‬ ‫الواحات‬ ،‫بالجديدة‬ ‫الحديد‬ ‫بمنجم‬ ‫الهضبة‬ ‫منطقة‬ ‫فى‬ ‫المتفتت‬ ‫الباريت‬
•‫الخام‬ ‫طبقة‬ ‫أسفل‬ ‫يوجد‬‫البحرية‬ ‫لتكوين‬ ‫التابع‬ ‫الرملى‬ ‫للحجر‬ ‫العلوى‬ ‫بالجزء‬(Bahariya Formation)
•‫الخام‬ ‫لطبقة‬ ‫السفلى‬ ‫الجزء‬ ‫مع‬ ‫ومتداخال‬ ‫البحرية‬ ‫وتكوين‬ ‫الخام‬ ‫بين‬ ‫التالمس‬ ‫منطقة‬ ‫عند‬
•‫من‬ ‫السمك‬ ‫يتراوح‬5‫إلى‬ ‫سم‬50‫مترين‬ ‫إلى‬ ‫الحاالت‬ ‫بعض‬ ‫وفى‬ ‫سم‬
•‫بص‬ ‫منتشرة‬ ‫التجمعات‬ ‫وهذه‬ ،‫متصلة‬ ‫طبقات‬ ‫هيئة‬ ‫على‬ ‫وليس‬ ‫تجمعات‬ ‫او‬ ‫جيوب‬ ‫هيئة‬ ‫على‬ ‫يوجد‬‫غير‬ ‫ورة‬
‫الر‬ ‫الحجر‬ ‫من‬ ‫تكون‬ ‫الباريت‬ ‫من‬ ‫خالية‬ ‫مساحات‬ ‫ويفصلها‬ ‫واألبعاد‬ ‫السمك‬ ‫فى‬ ‫ومتفاوتة‬ ‫منتظمة‬‫ملى‬
•‫سائ‬ ‫من‬ ‫تماسكه‬ ‫درجة‬ ‫وتتفاوت‬ ‫الحديد‬ ‫خام‬ ‫من‬ ‫متفاوتة‬ ‫وبنسب‬ ‫بالرمال‬ ‫مختلط‬ ‫الباريت‬ ‫يكون‬‫إلى‬ ‫ب‬
‫الحديد‬ ‫بخام‬ ‫اختالطه‬ ‫حالة‬ ‫فى‬ ‫التماسك‬ ‫وشديد‬ ‫الرملى‬ ‫بالحجر‬ ‫اختالطه‬ ‫حالة‬ ‫في‬ ‫متماسك‬
•

Detrital Barite

1.1.3. Ore Types
Generally, four types of ore are distinguished based on texture, constituents and
chemical composition namely:
Hard-massive ore type: This type is relatively massive hard crystalline and
has a deep reddish-brown color. It consists mainly of hematite (>80%) with
minor amounts of goethite and limonite. Micro- and macro-fossils which are
replaced by hematite (and/or goethite) are common. Manganese minerals
(mainly psilomelane) are rare in this ore type.
Banded-cavernous ore type: It has a brown or yellowish color, generally
banded and cavernous. The cavities being filled with red or yellow ochre or
manganiferous powder. It consists mainly of an intergrowth of goethite and
hematite together with a little amorphous limonite and minor amounts of
manganese minerals. The pyrite and chalcopyrite are present as minute
grains within limonite or in the core of subspherulitic goethite bodies. This
banded texture is attributed to pre-existing laminations in the original
limestone.
Friable-ore type: Generally, bright yellow, soft, friable and has an earthy
luster. The ore minerals consist mainly of goethite and limonite together
with minor amounts of hematite. Glauconite is the most common gangue
mineral and result in the appreciable increase Al2O3 content of these ore
type.
Oolitic-pisolitic ore type: Low to moderate grade ore (49-45 % Fe) has a
yellow to yellowish-brown color and oolitic to pisolitic texture. It is mainly
formed of goethite, Iimonite and quartz, minor amounts of hematite,
glauconite and Fe-rich chlorite.

Reserves
• Economic iron ores confined to the lower part of the middle Eocene limestone (El Naqb
formation) in four major occurrences north of Bahariya oasis.
Today, the left minable reserves are estimated by only 63 Mt, which are just enough for about
15-20 years at the present mining rate of 3 to 3.5 Mt/y.
Bahariya iron ores have 53% Fe that is suitable for the iron high ovens in Helwan City
factories, now, iron ores excavated from El-Gedida mine with an annual rate 3.3
Million Tons then carried about 300 km away to Helwan City factories by a special
train.
It is necessary to blend the various types to obtain:
Fe 53%, SiO2 7.5%, Cl 0.7%, and MnO 1.98%,
for use in the metallurgical plants at Helwan Iron and Steel Co., Cairo.
  How Geologist do this mixture???
Area Reserves Fe SiO2 Mn S P Cl
(M.Tonnes) %
El Gedida 126.7 53.6 8.9 2.3 0.9 0.2 0.6
Ghorabi 57.0 48.0 9.0 3.0 0.7 0.9 0.8
Nasser 29.0 44.7 6.7 3.9 0.6 0.1 1.3
El Harra 56.6 44.0 12.5 2.9 1.0 0.1 0.8

They classified ore blocks according to Fe-content into three categories
as following:
 Poor ore (17-35% Fe): Low-grade iron ore, highly ferruginous
sandstones and hydrogoethite ore.
 Normal ore (35-45% Fe): Oolitic and pisolitic hydrogoethite ore,
banded hydrogoethite, and hydrohematite ore
 Rich ore (>45% Fe): Colloform hydrogoethite ore and massive
hydrogoethite-hematite ore.

Genetic Ore Types
The largest and richest of these occurrences in that of El Gedida (~127 million tonnes
proven ore). At El Gedida mine, distinguishing three genetic, types:
I) Iron ore of a massive nature and a hydrothermal-metasomatic type (Type I):
 Represented by the high central area in El Gedida mine.
 The ore is high-grade, with high Fe and NaCl contents, and low Si, and high traces of Zn
and Cu.
 The mineralized middle Eocene limestone (El Naqb formation) is brecciated and
metasomatically replaced by hydrothermal solutions ascending along NE-SW trending
fractures.
II) Iron ore is cavernous, ochreous or massive type (Type II):
 Following the emergence and faulting of the mineralized middle Eocene block, the
generated depressions received reworked rocks including high-grade ore from the high
central area.
 Fresh water lakes occupied the depressions where remobilization of Fe and Mn and
their redeposition were effected, possibly through biogenic interference.
 Tripoli earth and kaolinite were authigenetically deposited with the debris.
 Detrital barite is a common associated.
 Abrupt change in grade characterizes the iron ore of this genetic type
III) Iron ore is oolitic or pisolitic type (Type III):
 This follows type II in age and is tied to post-middle Eocene glauconitic succession
which caps the reworked iron ore of type II
 Enrichment of the marine depositional basin in Fe and K promoted the formation of
glauconitic.
 Cyclic deposition of glauconitic clays and sands was interrupted by intermittent
emergence followed by lateritic weathering of glauconite sediments
 Profound changes in the mineralogy of these sediments took place resulting in the
deposition of low-grade Fe ore characteristically poor in Mn and Ba.

1.1.4. Origin
Ambiguity arises regarding the genesis of the iron ores in the Bahariya oases
area.
Attia (1955) favored a shallow water lacustrine origin during Oligocene time.
Deposition of leached iron under lagoonal environment and subsequent
replacement of the underlying middle Eocene and Cenomanian beds. Evidence of
replacement is apparent where most of the calcareous fossils, especially the
diagnostic nummulites of the middle Eocene, are almost completely replaced by iron
oxides.
El Shazly and Hassan (1962) assumed that the Ghorabi iron ore was derived
from the chemical weathering of older rocks.
Contrary of these opinions, Tosson and Saad (1974) suggested that the ores
were formed by metasomatic replacement associated with impregnations and cavity
filling from ascending solutions affiliated with volcanic activity. The oolitic and
pisolitic iron ore outcropping in the Ghorabi area to be syngenetic, the iron being
supplied by weathering processes and the high grade ores exist in the crests and
that low-grade ores are localized in the limbs of the anticlinal structures.
On the other hand, El Aref and Lotfy (1985) suggested that the iron deposits
were formed through lateritization processes during the senile stage of post Eocene
karst event. Karst depressions and excavated unconformity acted as traps where iron
oxides are accumulated. Iron deposits together with soil products also form surfacial
crust (duricrust), capping and cementing highly subdued and altered carbonate
rocks. The evolution of megascopic and microscopic ore fabrics, the oxidation of iron
bearing minerals, and their relation to the gangue and weathering products reflect
the changes in the moisture regimes and the physicochemical conditions involved
during the pedogenesis.

Qatrani Formation At El Gedida Mine. You can see here a
burrowing of ants then filled with iron.

• In the Eastern and Western Wadi areas, the ore successions are truncated unconformably by late
Lutetian-Bartonian glauconitic sediments with lateritic ironstone interbeds of the Hamra
Formation.The iron ore and the overlying glauconitic sediments are folded and undulated. The iron
ore sequence attains its maximum thickness, up to 35 m, in the Western and Eastern Wadi areas,
reduced into 11 m in the high central area. This iron ore sequence consists of a pisolitic oolitic iron
stone unit followed by highly karstified bedded ferruginous dolostones and mudstones. Ore
conglomerates mixed with silicified limestone and chert overly the karst ore. The genesis of the ores
has been a matter of a scientific discussion for a long time.

Glauconitic green sand at Gabal El Dist
(Bahariya Formation)
Upper Eocene Hamra Formation (Glauconite
and Iron beds)

Charcoal at Gabal El Dist

ii) EGYPTIAN BANDED
IRON FORMATION
(BIFs)

ii) EGYPTIAN BANDED IRON FORMATION (BIFs)
The banded iron ore deposit is a very limited occurrence,
being found only in the 13 localities in the central Eastern Desert,
approximately between Latitude 25° 15/ - 26° 40/ N and
Longitude 33° 22/ - 34° 20/ E.
These iron ore type is concentrated in five main localities:
Abu Marawat, Wadi Kareim, Wadi El Dabbah, Wadi Um Ghamis
El Zarqa, Gabal El Hadid, and Um Nar.
The bands are variable in thickness and extension from one
locality to another and within the same occurrence.
Their extension usually vanes from some meters up to more
than 2 km along the strike, and vary in thickness from a few cms
to 18 m (normally ranging between 0.5 and 3 m).
In the most cases, the ore is present in the form of bands
and lenses of magnetite, martite and hematite with a gangue
dominantly of quartz.
The reserves for BIF ore type in Egypt amounts to 47.6 million
tonnes (Akaad and Dardir 1983) as estimated for the whole of Quseir
area.

Localities Latitude Longitude
Abu Marawat 26° 31/ N 33° 22/ E
Wadi Kareim 25o 56/ 40// N 34° 03/ E
Wadi El Dabbah 25° 48/ N 34° 09/ E
Wadi Abu Rakab 25° 48/ 30// N 34° 11/ E
Wadi El Hindusi 25° 47/ 30// N 34° 11/ E
Gabal Um Shaddad 25° 39/ 20// N 34o 20/ E
Wadi Um Ghamis El Zarqa 25° 33/ N 34° 17/ E
Wadi Sitra 25° 32/ N 34° 14/ 30// E
Wadi Siwiqat Um Lassaf 25° 21/ N 34° 08/ E
Gabal El Hadid 25° 20/ N 34° 10/ E
Um Mar 25° 18/ N 34° 15/ E
Wadi Um Hagalig 25° 15/ 30// N 34° 16/ 30// E
Map showing major iron deposits in
central Eastern Desert, Egypt.
Geographic co-ordination of the
Banded Iron Ore deposits in the
central Eastern Desert of Egypt
Fig. 1: Thematic Landsat image of
Egypt showing the location of
eleven of the most important
banded iron-ores (blue circles). Inset
is a simplified geological map of the
area outlined in the white rectangle
(from Egyptian Geological Survey,
1981) .
1) Hadrabia
2) Abu Marawat,
3) Gabal Semna
4) Diwan
5) Wadi Kareim,
6) Wadi El Dabbah,
7) Gabal Um Shaddad
8) Wadi Um Ghamis El Zarqa,
9) Gabal El Hadid,
10)El Emra
11)Um Nar
12)Wadi Hammama
13)Um Anab
Wadi Abu Rakab
Wadi El Hindusi
Wadi Sitra
Wadi Siwiqat Um Lassaf
Wadi Um Hagalig
54

Table 1: Tectonostratigraphic basement units of the Egyptian Eastern Desert
Sources: Egyptian Geological Survey (1981); El-Gaby et al. (1990); Hassan and El-Hashad (1990); Stern et al. (2006); Avigad et al. (2007); Moussa et al. (2008).
Eon/
Era
Tectonic
Stage
Age
Ma
Rock Types/ Associations Granitoid intrusion
Phanero
zoic
Post-
Orogeni
c
<570.
Younger Granites (post-tectonic, alkalic): Granite, granodiorite,
monzonite
Gattarian (570 – 475
Ma)
Neoproterozoic
PanAfrican
Accreti
on/
Collisio
n
650-
570
Dokhan metavolcanics (andesite, rhyolite, rhyodacite,
pyroclastics) intercalated with Hammamat metasediments
(breccias, conglomerates, greywackes, arenites, and siltstones)
Subduction
750-650
IslandArc
Shadhli Metavolcanics (rhyolite, dacite, tuff);
Volcaniclastic metasediments; Diamictites (Strutian: 680
– 715 Ma).
Banded Iron Ores
Meatiq (710 – 610)
Hafafit (760 – 710)
Spreadi
ng
850-
750
Ophioli
tes
Tholeiitic basalt, sheeted dykes, gabbros, serpentinites,
all weakly metamorphosed
Shaitian Granite
(850 – 800 Ma)
Archean?/
Paleoprotero
zoic
Pre-Pan-
African
<1.8Ga
Metasedimentary schists and gneisses (Hb-, Bt-, and Chl-
schists), metagreywackes, slates, phyllites, and
metaconglomerates Some BIF? Umm Nar?
Migiff – Hafafit gneiss (Hb and Bt gneiss) and migmatite

Geologic Setting
 Central Eastern Desert (CED) is a part of the Arabian Nubian
Shield (ANS) which constitute the northeastern sector of the Pan-
African (650-550 Ma., Clifford 1970) tectonic belt. The Egyptian
Banded iron formation (BIF) and the host geosynclinal
metavolcanics and/or metasediments constitute widespread and
easily recognizable sequences at 13 localities distributed in the
CED.
 The iron formations occur as sporadic deposits in layered the
volcanogenic rocks of Neoproterozoic age. The Neoproterozoic
basement complex of the CED consists largely of a crudely layered
sequence of volcanic rocks and derivative sedimentary rocks,
mainly of greenschist facies metamorphism. The terrene has many
lithologic similarities to the Archean greenstone terrenes.
 The BIF geologic sequences are considered to be genetically
related to Pan-African weakly metamorphosed island arc
assemblages ( island arc volcanics and volcanoclastics of
Neoproterozoic age) which are often associated with ophiolitic
mélange rocks

Fig. 2: Location of Wadi Kareim (K) and El Dabbagh (D) study areas.
Location of Meatiq dome (M) is also shown. Dark green area between
Kareim and Dabbagh is a Hammamat basin. From Google Earth.

Figure 23: Geologic map of Wadi Kareim area (left) and Wadi El Dabbagh
area (right; note north arrow (Stern and Dixon, unpublished)

Geological map of Wadi El Dabbah iron ore
deposit ( after Akaad and Dardir, 1983)

• Fig. 2: Geological maps of (a) Wadi Kareim area (AFTER El-Habaak and Mahmoud, 1994) and (b)
Umm Nar (after El-Aref et al., 1993). Ellipse in (a) shows location of banded iron ore. 60

General Characteristics of the Egyptian Banded Iron formation
The general characteristics of the iron formation in the central Eastern Desert are as follows:
1)The BIF occurs as sharply defined stratigraphic units within layered volcanic-volcaniclastic
sequences of calc-alkaline nature and andesitic composition.
2)Some deposits (e.g. Wadi Kareim) are reportedly associated with diamictites (e.g. Stern et al.,
2006) suggesting some relation to glaciations and possibly “Snowball Earth” conditions.
3)Individual bands range from a few centimeters to more than 10 m in thickness and are frequently
faulted and folded with steeply limbs.
4)Frequent contemporaneous folding, faulting, brecciation and slump structures are found.
5)Microbanding occurs on a scale of centimeter or less, where iron-rich bands alternate with bands
of jasper or, sometimes, of carbonates or silicates.
6)In a given area, the zone containing layers of iron-formation typically has a stratigraphic
thickness of 100 to 200 m, in which the aggregate thickness of BIF is on the order of 10 to 20 m.
7)The lateral extents and thicknesses of individual ore bodies are relatively small, typically on the
order of tens of meters (Fig. 2).
8)The entire sequence (iron ore + host rocks) is strongly deformed by a series of folds and thrusts,
and was regionally metamorphosed under at least greenschist facies conditions.
9)Deformation evident on the regional, outcrop, and hand specimen scales (Figs. 2).
10)Rhythmic banding is either streaky (Umm Ghamis) or continuous (Hadrabia) where layers of
magnetite and hematite alternate with quartz – rich layers on macro-, meso- or micro-scales.

General Characteristics of the Egyptian Banded Iron Ores
11) Hadrabia is the only deposit with oolitic and pisolitic textures. None of the other deposits
have oolites, pisolites, pellets, or granules . Other wave generated primary structures are
also lacking.
12) Oxide and silicate facies ubiquitous; carbonate facies usually represented by calcite is
common in several deposits (e.g. Wadi Kareim, Wadi Dabbah, and Hadrabia). Sulfide
facies is generally lacking.
13) Magnetite is dominant, except in a few deposits (e.g. Hadrabia) where hematite -
magnetite. Most crystals of magnetite have undergone some grain coarsening attributed
to metamorphism in several areas (e.g. Wadi Kareim).
14) Magnetite commonly altered to martite, specularite, or goethite due to post-metamorphic
oxidation.
15) Most of the iron is present as magnetite (altered in places to martite) concentrated in
steel-back bands alternating with reddish jasper or with iron-poor grey or greenish bands;
hematite is less frequent. The gangue minerals present are mainly quartz, chlorite, biotite
and clay minerals.
16) Silicate facies characterized by the minerals: chlorite, epidote, garnet, hornblende, and
stilpnomelane.
17) Some deposits are also strongly altered, often developing a porous texture
18) Many of the iron ore deposits (e.g. Gebel Semna, Gebel Hadrabia and Abu Merwat) are
characterized by high Fe and low Si contents in comparison with Algoma, Superior, or
Rapitan BIF types (Fig. 7, Table 2), whereas others (e.g. Gebel El Hadid and Wadi El
Dabbah) are characterized by Fe/Si ratios somewhat comparable to Rapitan BIF. Altered
samples with a porous texture are typically characterized by some of the highest Fe/Si
ratios (Table 2).
19) Greenschist facies metamorphism, with the development of chlorite, sericite and the iron
silicate stilpnomelane and possibly minnesotaite occur. On the contact with intrusives,
local metamorphism may reach amphibolite facies with the recrystallization of the iron
minerals and silica and development of epidote and garnet.

Table 5: Mineralogical compositions and mode of occurrence the BIF, Central Eastern Desert, Egypt
Wadi Kareim Wadi El Dabbah Umm Ghamis El Zarqa Gabal El Hadid Umm Nar
Country rocks
Metavolcaniclastics,
metavolcanics,
granodiorites, Hammamt
sediments, trachytes
tetavolcanics, serpentinites,
Older Granites, Hammamat
sediments, Younger
Granites
Metasediments, metavolcanics,
serpentinites, metagabbros,
diorites, granodiorites, granites
Metasediments,
metavocanics, serpentinites,
metagabbros, granites
Shaitian granites, metasediments,
serpentinites, metagabbros, younger
gabbros, granites
Host rocks
Metavolcanic rocks
intercalated with
volcaniclastic rocks
(andesite-dacite tuffs,
metagreywackes &
metamudstones)
Tuffaceous metasediments Calcareous metamudstones
intercalated with
metagreywackes
Metasediments-
metapyroclastics (consists of
metagreywackes,
metamudstones,
metasiltstones,
metaconglomerates,
metatuffs)
Mica-schists, amphibole schists,
marbles and quartzites.
Principal iron mineral
Magnetite, hematite Hematite and/or magnetite Magnetite with or without
hematite
Magnetite, hematite Magnetite, hematite, stilpnomelane
Subsidiary iron minerals
(rarer minerals in
parenthesis)
Goethite, siderite,
greenalite, ninnosotaite,
stilpnomelane, pyrite,
(pyrrhotite, chalcopyrite,
sphalerite)
Goethite, martite (pyrite) Martite, goethite Goethite, siderite, (pyrite,
chalcopyrite)
Martite, goethite
Gangue minerals
Quartz, jasper, calcite,
ankerite, dolosite, garnet,
epidote, chlorite, actinolite,
talc
Quartz, jasper, calcite,
garnet, epidote, chlorite,
actinolite
Quartz, jasper, chalcedony,
calcite, epidote, chlorite, garnet,
hornblende, feldspar
Quartz, jasper, chert, calcite,
dolomite. ankerite, chlorite,
epidote, muscovite, biotite,
feldspar, apatite
Quartz, calcite, plagioclase, muscovite,
biotite, hornblende, graphite, epidote,
garnet
Iron formation facies
Oxide, carbonate, silicate,
sulfide
Oxide, oxide-silicate Oxide, oxide-silicate Oxide, carbonate (rarely
sulfide)
Oxide, oxide-silicate
Ore types
Banded siliceous Massive
magnetite
Magnetite-rich (black)
Hematite-rich (red-violet)
Magnetite-jasper-(hematite) Jasper-hematite Magnetite)
Nodular chert-magnetite-
(hematite) Siderite-magnetite)
Quartz-magnetite, Hematite-
magnetite-quartz-garnet
Fe% surface
Fe% subsurface
Reserve (m.t.)
44.6
43.0
17.8
38.2
34.9
6.0
44.6
42.1
5.6
45.7
45.0
3.6
45.8
41.8
13.7
Texture
Bedding, banding,
lamination, lensoidal, slump,
pelitic, psamo-pelitic, relics
of oolitic, granular, massive
Bedding, banding,
lamination, lensoidal,
Massive
Banding, bedding, lamination,
lenses, slump, crenulation
Banded, bedded, lensoidal,
deformation, massive,
colloform, rim veins, relict
replacement
Bedding, banding, lamination, cross-
lamination, flaser structure,
granoblastic, lense, slump, lensoidal
Band thickness 0.4 to 12 m Few cm to 10 m 10 cm to 5m Few cm to 3.8 m Few cm to 3 m

BIF with japer laminations (Wadi El Kariem)
d) Meso- and (e) micro-scale banding (lamination) between alternating
jasper (red) and Fe-ore in unaltered samples from Wadi Kareim.

Fig. 4: Photomicrographs showing selected
textural relations. (a) through (e) taken
under polarized reflected light, oil
immersion; (f) - (h) under plane polarized
transmitted light. (a) Magnetite coarsened
by metamorphism, Wadi Kareim; (b) relicts
of primary? magnetite (Mgt) replaced by
hematite, Wadi Kareim; (c) coarse grained
porphyroblasts of strongly martitized
magnetite, Wadi Kareim; (d) relict
magnetite strongly martitized, and
transformed into platy specular hematite
(Hm) Wadi Kareim; (e) primary magnetite
(arrow) and quartz embedded in a matrix
of secondary goethite, Gebel Semna; (f)
oriented platy hematite, oxide facies,
strongly altered porous sample from Gebel
Semna; (g) fibrous stilpnomelane (Stp) in
silicate facies; Wadi Kareim; (h) epidote
(Ep; arrow) coexisting with magnetite,
silicate facies; Wadi Kareim; (i) chlorite
coexisting with sericite and quartz, silicate
facies; Gebel Semna; cross polarized
transmitted light.

Reserves
Abu
Marawat
Wadi
Kareim
Wadi
El Dabbah
Umm
Ghamis El
Zarqa
Gabal
El Hadid
Umm
Nar
Total (m.t.)
Reserves* (m.t.) 6.5 17.7 6.0 5.6 3.6 13.7 53.1
Fe% surface 44.4 44.6 38.2 44.6 45.7 45.8 43.7
Fe% subsurface - 43.0 34.9 42.1 45.0 41.8 -
Fe% in concentrate - 56.4 53.5 59.7 69.0 61.0 55.3
Expected
concentrates
- 10.0 3.2 3.6 2.6 7.0 27.4

Are the Egyptian Banded Iron formations Unique?
 The size and general characteristics of the Egyptian BIF led to the suggestion that they are “Algoma type” deposits (e.g.
Sims and James, 1984; Table 2). However, several points suggest that the Egyptian BIFs may be unique, namely:
 Algoma and Superior type deposits are Late Archean or Paleoproterozoic in age (e.g. Klein, 2005), whereas the Egyptian
BIF’s are Neoproterozoic (Fig. 5). Only Umm Nar is suspected to be Paleoproterozoic (El-Aref et al., 1993).
 The Neoproterozoic Rapitan/ Urucum type deposits are typically jaspilites associated with glacial deposits. Among the
Egyptian iron ores, only Hadrabia is characterized by Hm >Mgt? (Essawy et al., 1997). Diamictites have only been reported
from Wadi Kareim (Stern et al., 2006).
 Egyptian BIFs are intercalated with calcalkalic metavolcanic and metapyroclastic rocks of island arc affinity rather than the
tholeiites typical of Algoma type deposits.
 Sulfide facies is lacking, carbonates minor, usually predominated by calcite (or ankerite) rather than siderite; well
developed silicate facies with stilpnomelane, chlorite, epidote, and garnet; oxide facies predominated by magnetite.
 Garnet in many Egyptian BIFs is grossular rich (and in some cases free of almandine; Khalil, 2001; Takla et al., 1999) unlike
garnets from Algoma or Superior BIFs which are typically almandine – spessartine solid solutions (e.g. Klein and Beukes,
1993).
 Amphibole in many Egyptian BIFs is a magnesiohornblende (e.g. Takla et al., 1999; Khalil, 2001) rather than
cummingtonite – grunerite.
 Chlorite in all Egyptian BIFs is a clinochlore – ripidolite with significantly higher Mg/(Fe + Mg) ratios (0.5 – 0.7) compared
to Algoma and Superior type BIFs (Fig. 6).
 All Egyptian BIFs characterized by an unusually high Fe/Si ratio (Fig. 7), as well as higher Fe3+/Fe2+ ratios compared to
Algoma and Superior types (Fig. 8). Fe/Si is considerably higher for BIFs affected by alteration (hydrothermal or
weathering?).
 Egyptian BIFs characterized by bulk chemistries that vary considerably from one deposit to another. However, many
deposits are characterized by high Al and low Cr and Ni compared to Algoma type BIFs (Table 2).
 REE patterns for Egyptian BIFs vary from one deposit to another, and do not resemble those patterns characteristic of
Algoma, Superior, or Rapitan BIFs. “Fresh” Umm Ghamis and Umm Shaddad have prominent negative Sm and positive Nd
and Eu anomalies, and slight HREE enrichment . Hadrabia deposit (“altered”) is characterized by a positive Eu anomaly.
Strongly oxidized samples from Hadrabia show LREE enrichment relative to North American Shale Composite (NASC) .

Table 2: BIF from the Eastern Desert of Egypt compared to the main types of BIF
O = oxide, Si = silicate, C = carbonate, Sf = sulfide, Mgt = magnetite, Hm = hematite.
Algoma Superior Rapitan
Egyptian BIF
Fresh Altered
Age(Ga) >2.5 2.5 - 1.9 0.8 - 0.6 0.85? - 0.65 0.75-0.6
Size small large small small small
Thickness (m) <50 >100 75 - 270 Very thin 5 -30
Deformation Very strong Undeformed Deformed Strong Strong
Facies O, Si, SfC O, Si, C O, Si,C
Oolites rare always common none none
Ore Minerals Mt>Hm
Mt>Hm
Higher Hm
Hm Mt>Hm MtHm
Rock
Associations
Tho to CA
vol,tuffs,
wackes/shales
Carbonaceous Diamictites
CA volcanic, tuffd, shales,
wackes; Diamictites?
Chemistry
High, Cr, Mn,
Ni, Cu, As
Low Cr, Co, Ni,
Cu, Zn
High P, Fe,
Low Cr, Co,
Ni
Low Cr, Co, Ni, Cu,
Variable Al
REE/NASC
+Eu, -Ce, slight
HREE-
Enrichment
+Eu , strong
HREE-
Enrichment
Weak +Eu,
Very strong
HREE
Enrichment
-Sm, Ce?,
+Nd and Eu,
HREE- rich?
+Eu, -Yb,
LREE-rich
Fe/Si <1.36 <1.36 1.3 - 1.6 1.4 -2.75 3 -4.7
Fe2O3/FeO 1.9 2.76 46- 100 5.5 - 8 7 -57

Fig. 5: Schematic diagram showing age and abundance of
the three main types of BIF relative to Hamersley Group
as a maximum (from Klein, 2005). Note Egyptian BIF age.

Fig. 6: Compositional range for chlorites from the silicate
facies of the Egyptian BIF relative to the fields of Sheikhikhou
(1992).

Fig. 7: Bulk rock compositions of
“Fresh” and “Altered” BIFs from
Egypt relative to Algoma,
Superior, and Rapitan average
compositions from Gross &
McLeon (1980).

Fig. 8: Bulk rock major oxide components of Wadi Kareim iron
formation (solid circels) compared to overall averages for Algoma and
Superior type BIFs (shaded green) from Klein (2005). All analyses
recalculated on an anhydrous, CO2 – free basis.

Fig. 9: REE patterns normalized relative to North American Shale Composite (NASC) for (a) “fresh” BIF from Takla
et al. (1999); El-Habaak & Soliman, (1999); (b) “altered” BIF from Hadrabia (Essawy et al.,1997), and Kareim (El-
Habaak and Soliman (1999) compared to patterns typical of Algoma (c), Superior (d), and Rapitan (e). (c) – (e) from
Klein (2005).

GENESIS OF EGYPTIAN BANDED IRON FORMATION
The Egyptian banded iron formation (BIF) and the host metavolcanics or
metasediments constitute widespread and easily recognizable sequences at
13 localities distributed in the Central Eastern Desert (CED) between latitudes
25° 12/ and 26° 31/ N. These BIF sequences are considered, in the recent
literatures, to be genetically related to Pan-African weakly metamorphosed
island arc volcanic and volcaniclastic assemblages (Late Proterozoic) which
are often associated with ophiolitic mélange rocks.
However, the understanding of the environment of deposition and
geologic setting of each BIF-bearing sequence is very important to unravel
the origin of the related BIF facies as well as its genetic relationship with the
complex history of the Pan-African rock assemblages.
Two main genetic models have been postulated for the banded Egyptian BIFs:
1) a purely sedimentary origin during the accumulation of the Precambrian
geosynclinal sediments (i.e. chemical marine sediments in geosynclinal
basin; Shukari et al., 1959, and Rasmy, 1968), and
2) a volcanogenic origin related to submarine magmatism and hydrothermal
activity of Pan-African island arc assemblage (i.e., subaqueous volcanogenic
deposits in an island arc environment: (Sims and James, 1984; El-Gaby et
al., 1988).

It is generally agreed that the BIFs are chemical precipitates from water,
but there is no general agreement as to the source of the iron and silica in
them or to the physical environment in which they were deposited.
The BIF and base metal sulfides of the Egyptian Eastern Desert seem
to be occurring exclusively in the island arc assemblage which consists of
weakly metamorphosed volcanogenic sequences, where the iron oxides
represent an aerated near-shore environment to the north and the sulfides
represent deeper euxinic environment to the south.
On the other hand, the two southernmost iron occurrences at Gabal El
Hadid and Umm Nar contain pyrite, chalcopyrite and siderite beside iron
oxide minerals (Sabet et al., 1976; El-Dougdoug et al., 1985); these
occurrences may represent transitional conditions shallow or near shore
facies (i.e. iron oxide).
El Aref et al. (1993) preliminary reclassified the Egyptian BIFs into two
main genetic types of different ages;
1) Early (?) Proterozoic BIF of pre-Pan-African shelf environment,
represented by the Umm Nar occurrence., and
2) Late Proterozoic BIF of Pan-African island arc environment,
represented by Gabal El Hadid, Wadi Kareim, and Gabal El Dabbah.

Table 3: Paragenetic sequence of mineral formation of the central Eastern Desert BIFs in
relation to the metamorphic history
Sedimentation and
Diagenesis
Metamorphism Hydrothermal
process
Weathering process
Regional Contact
Mineralogical
Composition
Colloidal materials of
ferruginous/
calcareous sediments,
muds, shale, silica
gel and detritus materials ?
Magnetite
(fine euhedral
crystals)
Hematite (fine
prismatic and
flaky crystals)
Stilpnomelane
Minnosotaite
Quartz
Chlorite
Muscovite
Dolomite
Ankerite
Biotite
Epidote
Hornblende
Actinolite
Talc
Garnet
Apatite
Magnetite
(large euhedral
crystals)
Magnetite
(after chlorite)
Chlorite
Epidote
Garnet
Graphite
Magnetite (veinlets)
Goethite (veinlets)
Pyrite
Chalcopyrite
Pyrrhotite
Sphalerite
Quartz (veinlets)
Calcite (veinlets)
Hematite (martite)
Goethite
Kaolinite
Sericite
Chlorite
Textures
Banded
Massive
Colloform
Pelitic and psmao-pelitic
Relics of oolitic
Nodular
Granular
Banded
Lensoidal
Massive
Granoblastic
Vein replacemet Replacenent
Colloform
77

References:Adelsberger, K.A., Smith, J.R., 2009. Desert pavement development and landscape stability on the eastern libyan plateau. Egypt. Geomorphol. 107, 178–194.
Akaad, M. K., & Dardir, A. A. 1983. Geology of Wadi El Dabbah iron ore deposits, Eastern Desert of Egypt. Bulletin of Faculty of Earth Sciences, King Abdulaziz University, 6, 611-617.
Akaad, S. and Issawi, B. (1963). Geology and Iron Deposits of Bahayria Oasis. The Egyptian Geological Survey, No. 18, p. 300.
Attia, M.I. (1955). Topography, Geology, and Iron Ore of the District East of Aswan,” The Egyptian Geological Survey, p. 262.
Basta, E. Z. and Amer, H.(1969). El Gidida Iron Ores and Their Origin, Bahariya Oases, Egypt. Economic Geology, Vol. 64, pp. 424-444. doi:10.2113/gsecongeo.64.4.424
El Aref, M. M. and Lotfi, Z. (1985). Genetic Karst Significance of the Iron Ore Deposits of El Bahariya Oases, Western Desert. Annal of Geological Survey of Egypt, Vol. 15, pp. 1-30.
El Aref, M. M., El Doudgdoug, A., Abdel Wahed, M. & El Manawi, A. W. (1993). Diagenetic and metamorphic history of Umm Nar BIF, Eastern Desert, Egypt. Mineral. Deposita, 28, 264-278.
El Bassyony, A. A. (2000). Geological Setting and Origin of El Harra Iron Ores, Bahariya Oases, Western Desert, Egypt. Annal of Geological Survey of Egypt, Vol. 23, pp. 213-222.
El-Dougdoug et al., 1985
El Gaby, S.; List, F.K., and Tehrani, R., (1988). Geology, evolution and metallogenesis of the Pan-African Belt in Egypt. In: El Gaby, S., and Greiling, R.O. (eds.), The Pan-African Belt of Northeast Africa and Adjacent Area. Friedr Vieweg Sohn,
Braunschweig/Wiesbaden, pp. 17–68.
El Ramly, M. F.; Akaad, M. K. and Rasmy, A. H. (1963). Geology and Structure of Um Nar Iron Deposit. Special Paper, No. 28, Geological Survey of Egypt, p. 29.
El Sharkawy, M. A.; Higazi, M. A.; and Khalil, M. A. (1987). Three Probable Genetic Types of Iron Ore at El Gadida Mine, Western Desert. Egyptian Journal of Geology, Vol. 31, pp. 1-2.
El Shazly, E. M. (1962). The results of drilling in iron ore deposits of Gharabi, Bahariya Oasis, Western Desert and report on the mineralogy of the low grade iron of El Heiz area, Bahariya Oasis, Western Desert, Geol. Surv. Egypt.
El Shazly, E. M. and Hassan, A. A.(1962). The Results of Drilling in the Iron Ore Deposit of Ghorabi, Bahariya Oases, Western Desert. Geologic Survey Department of Egypt, p.41.
Essawy, M. A., Zalata, A. A., & Makroum, F. (1997). Hadrabia banded iron-formation, Eastern Desert, Egypt. Egyptian Mineralogist, 9, 147-168.
Hussein, A.A.A., (1990). Mineral deposits. In: Said, R. (Ed.), The geology of Egypt. 1990. A.A. Balkema, Rotterdam/Brookfield, pp. 511-566.
Issawi, B. (1981). Geology of the South Western Desert of Egypt. Annal of Geological Survey of Egypt, 11, 57-66.
Klein, C. 2005. Some Precambrian banded iron formations from around the world: Their age, geologic setting, mineralogy, metamorphism, geochemistry, and origin. American Mineralogist, 90, 1473-1499.
Klein, C., & Beukes, N. J. (1993). Proterozoic iron-formations. In: Condie, K.C., (ed.). Development in Precambrian Geology: Proterozoic crustal evolution. 10, 383-418.
Khalil, K. I. 2001. Banded iron-formation (BIF) of Wadi El Dabbah area, Central Eastern Desert, Egypt: A genetic concept. 5th International Conference on Geochemistry, Alexandria University, 823 333-352.
Neev, D.; Hall, K. J. and Saul, M. J. (1982). The Pelasium Megashear System across Africa and Associated Linea-ment Swarms,” Journal of Geophysical Research, Vol. 87, No. B2, pp. 1015-1030. doi:10.1029/JB087iB02p01015
• Said and Issawi, (1964)
• Sabet et al., 1976;
Salem, S.M. and El Gammal, E.A. (2015). Iron ore prospection East Aswan, Egypt, using remote sensing techniques. The Egyptian Journal of Remote Sensing and Space Sciences (Unpub)
Sims, P. K. and James, H. (1984). Banded Iron Formation of Late Proterozoic Age in the Central Eastern Desert of Egypt, Geology and Tectonic Setting. Economic Geology, Vol. 79, pp. 1777-1784. doi:10.2113/gsecongeo.79.8.1777
Takla, M. A., Hamimi, Z., Hassanein, S. M., & Kaoud, N. N. (1999). Characterization and genesis of the BIF associating arc metavolcanics, Umm Ghamis area, Central Eastern Desert Egypt. Egyptian Mineralogist, 11, 157-185.
Tosson and Saad (1974)

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