Mineral Resources in Sinai

MINERAL RESOURCES
IN
SINAI - EGYPT
Hassan Z. Harraz
hharraz2006@yahoo.com
2017- 2018

Geology
• The geology of South Sinai is characterized by the presence
of thick Precambrian granites, weakly deformed granitoids
and alkali feldspar granites present in the core of the South
Sinai Peninsula triangle.
• The Precambrian rocks are associated with Paleozoic-
carboniferous dolomitic limestone deposits.
• Bordering the peninsula triangle are thick quaternary
sediments in the limestone plateaux, raised coral reefs and
gravel terraces along the Gulf of Suez and Aqabah, Ras
Mohamed and Sharm co-exist in these raised terraces. As
for Dahab, the city is surrounded by Precambrian granites.
• Patches of Mesozoic cretaceous carbonates are found in the
western middle part of South Sinai.

7
Facies analysis and
stratigraphic
sequence of S. Sinai

9
Shalaby and Shawky / Journal of African Earth Sciences 100 (2014) 289–302

MINERAL DEPOSITS
Mineral deposits in Sinai could be classified into:
➢Metallic Ores
➢Nonmetallic Deposits
➢Building Materials; and
➢Ornamental Stones.

Locations of Deposits
• Most of the metallic and non-metallic deposits are found in the
Middle Western portion of South Sinai, close to the Gulf of Suez.
• These deposits are scattered in evaporites and chemical organic
sediments.
• Most of the deposits, contrary to the metallic and non-metallic,
are found in the Mesozoic cretaceous carbonates and siliciclastics,
in lower Eocene limestone with shales and in lower and middle
Miocene biogenic carbonates with shales and marls. The eastern
part of South Sinai is characterized by deposits found in igneous
intrusive granites and syenites.
• It is apparent from the two tables that the building materials and
ornamental stones exceed the metallic and non-metallic deposits.
Also both are predominantly found in the western part of South
Sinai in sedimentary rocks.
• Figure (1) shows the metallic and nonmetallic deposits in South
Sinai.

Mineral
Potential
Map of
Sinai
12

Types of Deposits
Mineral deposits of potential economic significance in
Sinai:
Construction aggregate and sand
Limestone and dolomite (for cement production)
White Sand (High silica sand for glass production)
Coal
Gypsum
Kaolin
Manganese- Iron
Iron
Turquoise (semi-precious stones)
Copper
Uranium
Phosphate
Heavy mineral-bearing beach sands (monazite, ilmenite, zircon)
Sulfur

Location
No.*
Name of Locality Deposit Ore Comments
Non-Metallic Occurrences
1 Port Said Common Salt
Under Exploition, Major
Saline sources
10 Farsh el Ghozlan Kaolinitic clay Exploited until 1967
12 Musabba Salama Kaolinitic clay Exploited until 1967
13 Abu Zenima Limestone
14 Budra Kaolinitic clay Exploited until 1967
15 Abu Natash Kaolinitic clay Exploited until 1967
16 El Deheissa Kaolinitic clay
17 Gini Kaolinitic clay
19 Sarabit el Khadim Turquoise
Under exploitation since
ancient Egyptian times
20 Sulfur
*Refer to map in Figure 3-1.
14
10
12
13 14 15
1716
19
20
2
5

Location
No.*
Name of Locality Deposit Ore Comments
Metallic
Occurrences
1 Wadi el Arish Black sands
2 Umm Bugma Manganese
Largest manganese
reserves in Egypt,
discovered 1898
production began in
1908, production from
1911 to 1967 totalled 5.5
million tonnes, reserves 4
million tonnes.
3 Wadi Nassib Manganese
4 Wadi el Noaman Manganese
5 Wadi Shallal Manganese
6 Gebel Abu Qafas Manganese
7 Wadi el Husseni Manganese
8 Gebel el Adidiya Manganese
9 Sarabit el Khadim Copper Ancient workings
10 Abu Suweira Copper
11 Abu Rudeib Copper
12 Rashidia Copper
13 Abu Zagatan Copper
14 Tawlleh Copper
15 Abu el Nimran Copper
16 Tarfa Copper
17 Tarr Copper
18 Feiran Copper
19 East of El Agma Copper Ancient mine
20 Regeita Copper
Ancient mine 0.21 to
8.85% Cu
21 Rahaba Copper
22 Samra Copper Ancient mine
23 Sharm el Sheikh Manganese Small reserves
*Refer to map in Figure 3-2. 16

Tab. 1: Chemical and Physical Properties of Local ores from Sinai
Ore Type
Chemical
Composition
Physical Properties
Specific
Gravity
Moisture %
Oil Absorp.
at 100gm
pH
Matter
Soluble
Hardness Brightness
L.S & Chalk 92-96 CaCO3 2.633- 2.693 0.33-0.70 26-40 8.0 0.10- 0.375 2.5- 3.0 96-97
Kaolin 49 SiO2 2.647 0.53 35 7.86 0.23 2.5 79.0
Glass Sand 99% SiO2 2.62 0.16 29 9.14 0.025 7.0 86.6
Gypsum 43% SO3 2.325 5.00 29 7.65 0.65 2.0 98.0

1) Construction Aggregate and Sand
 Materials suitable for the production of mortar and
cement sand, cement gravel, and base rock occur
widely as pediment cover and wadi fill throughout
Sinai.
 Materials readily available for economic use in the
northern third of the region consist of poorly sorted
clastic limestone, dolomite, and chert, with a
moderate-to-high soluble salt content.
 Quarrying of cretaceous limestone exposed in Gebel
Libni or Gebel Asagil would yield excellent
construction aggregate, but at costs far above that
of screened alluvium.
 Regional exploration and testing may locate
presently unknown major sources of quality alluvial
construction aggregate. High quality sources of
construction aggregate occur in nearly every wadi
throughout south Sinai. In this region, production
sites can be conveniently located near each
construction project for minimum transport
expense.
 As for building materials and ornamental stones
there are numerous deposits in the lower, middle
and middle upper part of South Sinai, again
concentrated along the Gulf of Suez. Very scattered
deposits are found on the eastern side

2) Natural Calcium Carbonate (Limestone & Chalk)
• Limestone and dolomite suitable for cement manufacturing occur
throughout the Platform and Suez Rift Provinces. However, use of this
resource in Sinai is more contingent on other siting and resource
criteria (i.e., energy availability, infrastructure, transport distances)
than on limestone availability.
Fig. 2: Limestone of (A) Wadi Nukhl, South of Sinai; and (B) Limestone of Gabal
Egma, South of Sinai
Chalk of Wadi Matulla: Chalk is composed of rounded oolitic forms of calcite cemented by
fine grains of calcite and little organic matter. The colorless or cloudy, fine to coarse
aggregates and organic structure„ oolitic or spherulitic ‟ are characterize the chalk of Wadi
Matulla .
Chalk of Wadi Nukhul is composed mainly of calcite, and fossiliferous skeleton, organic
matter and clay matrix.

Natural Calcium Carbonate
 The carbonate materials are abundant in West Central Sinai; they occur as thick beds of large extension.
Therefore, limestone reserves in Sinai are considered unlimited. Important sites for limestone, from north to
south are Gabal Libna, Um Mafroth, El Hegam, Reasan Eneiza, El Mostan, El Maghara, El Halal, Ekma,
Wadi Nukhul (Fig. 2 & 3), Wadi Ferain, and Wadi Matullah.
➢ Limestone deposits are characterized by having large parts of it with no overburden.
➢ The limestone differs in their hardness as a result of differences in their degree of crystallization.
➢ All limestone could be considered hard to very hard, CaO: 40 to 55.6 % and MgO: up to 7 %.
➢ The wide availability and the low cost of CaCO3 make it the most widely used as extender pigments
today.
➢ They are used in all kinds of decorative and protective coating.
 The carbonate ore deposits are abundant in South Sinai, Abu Zenima and Egma.
❖ Abu Zenima carbonates were formed at the Miocene age (Fig. 2& 3). The CaO content 51.0% to 53.0%.
They possess the following physical properties; high brightness (96 % to 97 %), specific gravity (2.633 to
2.693), low oil consumption (26 to 40), pH (8), low moisture content (0.33% to 0.70%), low matter soluble
in water (0.10% to 0.375%) and viscosity (90 to 112.5 cp.).
❖ Wadi Nukhul carbonate rocks are classified as biomicrite limestone, these limestone are silty and
fossiliferous, they contain abundant iron oxides and have low porosity. Wadi Nukhul limestone is finely
crystalline calcite containing few grains of quartz. The matrix composed of clay transformed to
Glauconite. Most of ore samples are composed of Foraminefral limestone contains organic matter. The
limestone composed of fine aggregates. Dolomite and magnesite are associated with limestone.

3) Coal
 Prospecting for coal carried out in 1958-1962 resulted in the discovery of the coal deposits of Maghara,
Ayun Musa, and Wadi Thora in Sinai.
 Coal deposits have been explored to varying degrees at Gebel Maghara; Ayun Musa, 14 kilometers
southeast of Suez; and wadi Thora, roughly 25 kilometers east of Abu Zenima.
 Exposed coal deposits are known in two areas of Sinai, the Maghara district and Um Bogma district.
 Thin coal seams have also been recorded in oil and gas exploration boring logs elsewhere in Sinai, but
none suggest sufficient depth and seam thickness to justify further exploration.
❖ At present, the only deposit considered economic is that of Maghara in north Sinai (Hussein,
1990).
❖ Coal Reserves:~167 million tons
 Coal seams appear in middle Jurassic Bathonian sediments on the northwest limb of the Maghara
Anticline. The estimated reserves are about 51.8 million tons in a 30 km2 area. The sequence contains
up to 10 coal seams, of which two are of commercial thickness. The entire sequence dips northwestward
at angles of 5 to 10 degrees. It is divided into numerous blocks by small faults of the same trend.
 The principal seams at Maghara-named Upper and Lower-range from a minimum thickness of 20 cm to a
maximum thickness of 190 cm, with few partings, and are separated by 8 to 10 m of limestone
sandstone, clay, and shale. The coal is black, half dull, hard, resinous, and subbituminous A in rank. It is
low ash, high sulfur, and based on tests to date-has limited coking potential.
 Drill holes at Ayun Musa penetrated up to 11 seams of coal in a 70 to 100 m sequence of lower
Cretaceous rocks, at depths ranging from 400 to 600 m below surface. Ten coal seams occupied the
upper 30 m of the section, with a maximum seam thickness of 120 cm. The lower part of the sequence
contained a single seam, ranging in thickness from 18 to 120 cm. The seams are lenticular and
nonpersistent, with no apparent workable thickness; because of these characteristics, and great depths
and complicated geologic structures, the deposits at Ayun Musa are considered noncommercial. Future
exploration potential in the region is also believed to be limited.
 Twenty drill holes and several pits and adits have served to test a coal horizon that occurs in
Carboniferous sediments at Wadi Oeda and Wadi Thora, roughly 14 km apart, east of Abu Zenima. The
single seam was found to range between 10 and 80 cm in thickness and to be of low quality. It has
limited potential beyond local heating use.

Landsat TM image of the northern
Sinai inversion folds
23
Simplified structural form-line
map of northern Sinai after Khalil
and Moustafa (1994)showing the
Syrian Arc folds in northern Sinai
and the nearby area of the Naqb
Desert

‫المغاره‬ ‫فحم‬
‫بسيناء‬

4) Manganese -Iron Deposits
Manganese- iron deposits occur as lens-shaped, concordant bodies and
fissure fillings in the Carboniferous Um Bogma Formation east of Abu Zenima
and Abu Rudeis.
The ore lenses average 2 m in thickness, but locally achieve a thickness of 4
m.
The host rock consists of red and yellow crystalline dolomite, variegated
shale, and sandy clay.
The mineralization consists of manganese oxides mixed with iron oxides;
earthy oxides and pyrolusite are associated with goethite, hematite and other
minerals such as calcite.
Traces of uranium and copper accompany the manganese.
An average lens might contain 10,000 tonnes of ore above a cut-off of 20 %
manganese.
Ore specimens with up to 60 % manganese occur in the deposits; historically
mined, hand-sorted, high-grade material from the Umm Bogma district
averages up to 40 % manganese. Remaining explored deposits of significant
tonnage average between 20 and 30 % manganese.
Around 30,000 tons of Ferro- manganese alloys are exported to Japan,
Europe, and Arab countries most of it by sea from the Abu Zenima terminal
and some by truck to El Aqaba in Jordon.
25

Fig.2 : Distribution map of the Lower Carboniferous in the Um Bogma area, west-central Sinai,
Egypt (after Kora and Jux, 1986).
26

Abu Thora Formation
Um Bogma Formation
Sarabit El Khadim-Adedia formations
Precambrian Basement
27

Um Bogma District
 Um Bogma region West Central Sinai are considered to be the most important area in Egypt for
manganese deposits.
 Extensive workable manganese deposits contributed significantly to the Egyptian economy up to 1967,
when the mines were abandoned.
 Reopening the best mines is being considered and evolution of newly discovered occurrence.
 Manganese- iron deposits occur as lens-shaped, concordant bodies and fissure fillings in the
Carboniferous Um Bogma Formation east of Abu Zenima and Abu Rudeis.
 Manganese ore deposits occur wide spread at eight localities of the manganese deposits from the Um
Bogma region, west central Sinai. These localities are:
1) Abu Hamata left,
2) Abu Hamata right,
3) Abu Thor,
4) Abu Zarab,
5) Rass EI-Homara ,
6) Area 10,
7) Area 9, and
8) Area 8.
 Manganese ore deposits occur in Paleozoic sediments of Lower Carboniferous age.
Traces of uranium and copper accompany the manganese.
28

Table 2. Chemical composition of Um Bogma manganese ores.
Low Mn Ore
wt%
Medium Mn Ore
wt%
High Mn Ore
wt%
Fe2O3 30.37 17.94 14.96
MnO 35.30 43.00 48.59
Mn/Fe 1.46 3.32 4.54
29
The reserve of these ores in Um Bogma is ~5 million tonnes of Fe-Mn.
An average lens might contain 10,000 tonnes of ore above a cut-off of 20 %
manganese.
Ore specimens with up to 60 % manganese occur in the deposits; historically
mined, hand-sorted, high-grade material from the Umm Bogma district
averages up to 40 % manganese. Remaining explored deposits of significant
tonnage average between 20 and 30 % manganese.
It is also Producing Ferromanganese Alloys at the plant installed at nearby
Abu Zeneima, a port on the Gulf of Suez.
Around 30,000 tons of Ferro- manganese alloys are exported to Japan,
Europe, and Arab countries most of it by sea from the Abu Zenima terminal and
some by truck to El Aqaba in Jordon.

Egyptian Ore Deposits 30
Shallow
Open
Marine
Pink colour, Sandy Dolostone -
Marl Dolostone
Mn-Fe ore
Igneous and Metamorphic Rocks
i) Middle Carbonate Unit (Um Bogma
Formation, 0 – 41 m, Lower
Carboniferous):
▪ This is represented by dolomite and
limestone rocks and are covered
conformably the lower sandstone unit.
▪ Four members are differentiated from
base to top:
➢Dolomite Member.
➢Marly dolomite and Silt member,
➢Silt-Shale member,
➢ Dolomite and Manganese-
bearing member,
Lower Sandstone
Unit (Cambo-
Ordovician to
Devonian)
ii) Upper Sandstone Unit (Abu
Thora Formation, 30 – 200 m;
Visean)
➢ represented by medium to coarse
grained sandstone.
➢ Some beds are almost Snow-white,.
Friable Sands With Three Kaolinitic
Claystone Layers (~80 Million Tons)Kaolinitic Claystone Layers
Medium to Coarse Grained
Sandstone
Glass Sand Member
Um
Bogma
Abu
Thora
Carboniferous
Fluviatile
,
Swampy
To
Coastal
Marine
Adedia

Figure: (a) The lower sandstone series capped with Um Bogma Formation (A Sarabit El-Khadim Formation, B Abu
Hamata Formation, and C Adedia Formation).
(b) Layer of manganese ore interbedded with dolomites of Um Bogma Formation.
( c ) Manganese lens in the dolomite of Um Bogma Formation.
(d) Green copper staining in the fine-grained sandstone of Sarabit El-Khadim Formation
32

▪ The Manganese Ore is a stratiform
type occupying more or less the same
stratigraphic horizon in the dolomitic
limestone member of the Um Bogma
formation which caps the clastic
Adedia Formation.
▪ Ore deposits always tend to occupy a
particular stratigraphic horizon (i.e.
Dolomite and manganese-bearing
member), representing the base of the
middle carbonate (dolomitic limestone)
unit, which belong to Lower
Carboniferous.
▪ The manganese bodies are usually
surrounded by a zone of calcareous
shale, siltstone or sandstone that
form the transition with the
surrounding dolomite.
▪ The ore bodies usually show abrupt
contacts with the dolomite and are
frequently found to fill depressions in
the underlying Adedia formation.
▪ The ore bodies are irregular
in shape, tending to be
lenses or lenticular beds
(The thickness varies from 10
cm to 8 m and the extent of the
beds may reach 100 m).
▪ In some occurrences, the ore
bodies are present as veins
cutting the calcareous shale
that forms a transition with the
dolomite.
▪ Several forms characterize the
constituents of the ore
deposits such as Massive
Crystalline, Granular,
Nodular, Botryoidal,
Reniform, Fibrous,
Radiating, Need-like
Crystals, Earthy Soft And
Ochreous varieties.
33
FormsOre deposits

Mineralogy
The ore body:
➢varies in composition from Pure Manganese ore to Pure Iron ore; but
➢it generally represents a mixture of the two ore in variable
concentrations.
❖Small lenses are richer in Mn than the lenticular beds, where Mn
occurs admixed with Fe.
❖Multistage formation of the Mn minerals is noticed especially in the
regeneration and recrystallization of pyrolusite.
❖The transition between the ore bodies and the surrounding dolomite
is abrupt distinguished by enrichment (up to 73%) of quartz and
grains.
Ore Minerals:
➢Main Minerals: Pyrolusite, Psilomelane, Hematite, and
Goethite.
➢Minor Minerals +/- subordinate amounts: Polianite,
Manganite, Cryptomelane, Hausmannite, and Ramsdellite.
➢Rare Minerals: Chalcophanite Turquoise, Malachite, Alunite
and Pyrochroite.
Gangue minerals include Quartz, Dolomite, Calcite, Barite, Gypsum, and
some Clay minerals.
34

Mineralogy
Um Bogma manganese ore deposits divided into three
mineralogical zones:
i) The inner manqaniferous zone:
➢ essentially composed of Psilomelane and Pyrolusite with
rare Manganite, Hausmannite, Polianite and Pyrochroite.
➢ Hematite and Clay minerals usually <25%.
➢ The structure is massive, but concretions of Pyrolusite may
be present.
ii) The intermediate ferruginous-manganese zone:
➢ consists of Psilomelane, Pyrolusite and Hematite
➢ Goethite, Quartz, Barite, and Clay minerals up to 15%.
➢ The ore is massive and constitutes the main ore reserves of
Um Bogma.
iii) The outer ferruginous zone:
➢ composed mainly of Hematite and Goethite with minor
Psilomelane.
➢ Detrital quartz is common and spherulitic concentrations are
frequent.
35

5) Gypsum
• Gypsum and anhydrite in Sinai are associated with marl and
sandstone in the Miocene Ras Malaab and Ras Gemsa Formations
along the Suez Rift Border Province.
• Ras Malaab gypsum occurs on the Eastern shore of the Gulf of Suez
at lat. 29º-10' N & long. 32º-50º E, 110 km south of Suez.
• Gypsum at Ras Malaab, varies from 5 to 30 m in thickness. It has
been segmented by normal faults with throws ranging up to 10 m,
and is overlain by 1 to 3 m of alluvium and leached weathered cap-
rock. Gypsum and anhydrite appear in thick inter-lensing zones
surrounded laterally by sandy shale and clay.
• The high grade gypsum deposits of Ras Malaab, possesses calcium
sulphate content ranging from (93% to 98%), pH (7.65), matter
soluble (0.65), high brightness (98 %).
• Gypsum of Ras Malaab has a colorless and fibrous structure. Fibrous
grain shape gives a good reinforcement for the paint film after
application on substrate. Gypsum occurs associated with calcite,
dolomite and halite .
36

6) Kaolin Deposits
West Central
Sinai at Abu
Zenima District
Lower
Carboniferous
Sandstone (Glass sand
member) and kaolinitic
claystone rocks of the
Abu Thora Formation
North Abu Zeneima
area: Gabal Hasbar
and Khaboba, Nukhl
South of Abu Zeneima
area: Wadi Abu
Natash, Farsh El
Ghoazlan, Wadi Budra,
El Dehesa, El Shellal,
and Mukattab.
Lower
Cretaceous
Sandstones belong to
the Malha Formation
Mosabaa, Esela, Kheel,
Sakar, Hanash and Teeh
 Abu Zenima area : Kaolin Reserves in Abu Zeneima district are estimated to be
about 1,453,000 tons
 Kaolin deposits are ranging from are ranging from Lower Cretaceous and Lower
Carboniferous age.

The Carboniferous sedimentary kaolin deposits
i) in North and East of the Abu Zenima area, west central Sinai, occur in the Khaboba
and Hasbar areas between latitudes 29o03/00// and 29o13/30//north and longitudes
33o10/00// and 33o16/33// east and belong to the Abu Thora Formation.
❖ Kaolin deposits in these two areas occur as moderately hard, gray to dark
gray, massive or rarely fine laminated kaolin.
❖ They exist in the form of lenses that may attain a maximum thickness of
about 2.5 m.
❖ The clay fractions of the Carboniferous deposits at the Khaboba and Hasbar
areas are composed of kaolinite, anatase, illite and traces of chlorite and were
sourced from a mixture of low grade, granitic and/or alkaline rocks.
ii) Southeast of the Abu Zenima area, the Carboniferous kaolin deposits cover the floor of
wadis Abu Natash, El Shellal, and Mukattab.
❖ The kaolin deposit of Abu Natash area looks different in lithology compared
to those of the Kaboba and Hasbar areas.
❖ It occurs as whitish gray to earthy gray, massive, moderately hard beds that
range in thickness from few centimeters up to 7 m and are bounded by
sandstones.
❖ On the other hand, the clay fraction of the Carboniferous deposit at Abu
Natash deposit is composed of kaolinite and anatase and was derived from
mafic rocks.

• Known occurrences of kaolin appear in the Carboniferous Abu Zarab Formation
and a clayey and sandy horizon in the Cretaceous Nubian Formation. All reported
deposits are located in the Suez Rift Border Province, east of Abu Zenima and Abu
Rudeis. The best known of these, where some development and production have
occurred, is at Budra near the Um Bogma manganese mine.
• At the Budra site four kaolinite beds with an aggregate thickness of 36 m occur in a
95 m thick sequence of Nubian sandstone. The Kaolin horizons are lensoidal-
pinching and swelling with variations in quality. The beds dip to the southwest at
angles between 20 and 40 degrees and are offset by faults with throws of up to
100 m. The kaolin horizons are pure or slightly silty and sandy and range in color
from light grey through violet to dark grey. The clay is chemically pure or slightly
ferruginous and consists principally of kaolinite with small admixtures of dickite
and hydromica. Its quality is suitable for the production of fine ceramics.
• The kaolin composition of Farsh El Ghozlan and Wadi Budra at southern Sinai is
mainly composed of kaolinite and montmorillonite of Senonian age. The chemical
analyses show that, the ore contains (37.23%) Al2O3, (46.40%) SiO2., and L.O.I
about 14%. Many authors (Boulis and Attia, 1994; Abdel Razek, 1994) explain the
origin of kaolin deposits, it is suggested that, these deposits were derived from the
weathering mantle of the underlined feldspathic rocks of the basement complex.

The lower Cretaceous sedimentary kaolin deposits
• in west central Sinai belong to the Malha Formation and occur mainly in
the north and northeast of Abu Zenima covering an area of 200 km2
between latitudes 29o03/00// and 29o13/30// north and longitudes
33o10/00// and 33o16/33// east where the Mosabaa, Esela, Hanash and
Teeh deposits are located.
• Kaolin deposit in the Mosaba area occurs in the form of lenticular beds in
three kaolin horizons (20 cm to 2 m thick) that are separated by
sandstones, while at the Esela area, kaolin deposit attains approximately 7
m thick of intercalations of black, gray, yellowish, brownish, massive, and
moderately hard kaolin.
• In the Teeh Plateau, kaolin deposit occurs as separated beds range in
thickness from 10 cm to 1.5 m that are intercalated, underlain and
overlain by yellowish to reddish sandstones.
• The clay fractions of the lower Cretaceous deposits in Sinai are composed
of kaolinite and anatase and were derived from a mixture of medium to
high grade metamorphic, granitic and/or alkaline rocks.

7) High Silica Sand (or White Sands)
 White sand occurs at several localities in Sinai namely Gabal Dalal, Wadi Maktab, Wadi Mussaba,
Khabouba, Abu Kafas, Abu Natash at Abu Zeneima area and the area of El Gunna plateau in south Sinai.
 The ores of both north and south of Sinai belong to lower the Cretaceous and occurs in the form off
lenticular beds that range in thickness from centimeters to 15m or so, with alternating beds of
ferrugineous sandstone, shale or kaolin.
 The deposit has little or no overburden, and is exposed in extensive areas.
 Quartzitic sand, which is optimum for the production of clear glass should be uniformly distributed in size
between 200 and 600 micrometers, have SiO2 content is 99.54% ; an iron content of less than 0.07% and
have minimum contaminating sodium, calcium and potassium.
 The ore reserves are huge, and exceed billions of tons but not yet evaluated and the SiO2 content is
99.54% (Attia and Ghaalib, 1960) and (Geological Survey report on glass sand, 1994).
 The best source of glass sand in Egypt occurs in a quartz sandstone horizon of Carboniferous sedimentary
rocks east of Abu Zenima and Abu Rudeis.
 White Sand of Abu Zenima
➢ white sand horizons outcrops in west central Sinai.
➢ The quartz sand horizon at the best known location near Wadi el Khabouba northeast of Abu Zenima
is approximately 30 m thick. The Abu Zenima white sand is related to the Cretaceous age.
➢ Further south near Wadi Budra where the same quartz sand horizon was approximately 15 m thick.
➢ This physically and chemically persistent horizon represents an unlimited source of high quality silica
for glass manufacturing, which may have export potential. Its development for economic production
and marketing will require some exploration and testing.
➢ It is chemically inert and contains (99 %) SiO2, with an ideal physical and rheological property for
utilization as pigment for paints. The moisture content is (0.16 %), oil absorption (29g/100g), matter
soluble in water (0.025), hardness (7.0), good brightness (86.6 %). It can be used in producing epoxy
paint (Sigma cap EP primer)
 White Sand of Um Bogma has a clear appearance, lack of cleavage. The quartz grains are predominant
and ranges from sub-rounded to round. Clay matrix and carbonate cement the quartz grains.
 Two million tons of Silica sand deposits are sent to El Arish Port for export.

Cross-bedding and scour in a fine sandstone, Sinai

8) Cupriferous Sandstone
 Precambrian crystalline rocks at a number of locations in south
Sinai bear thin quartz veins of short length which contain
copper carbonate, probably an oxidation product of sparse
chalcopyrite.
 Historically, copper has been produced from copper oxide-
bearing sandstones of the Cambrian Serabit el Khadim
Formation or from overlying lower Carboniferous strata.
 Extensive beds of cupriferous sandstone in these units are
reported to have been mined in ancient times near Wadi
Maghara in west central Sinai. Ores are described as
containing up to 18% copper in carbonates and silicates.
 Several occurrences of copper were recorded in Phanerozoic
sediments in the Center and West Sinai (e.g., Wadi El-
Maghara, Wadi Samra and Serabit el-Khadim) as secondary
malachite and in some places mixed with Manganese.
 The deposits are sometimes associated with sandstone-
bearing uranium and silver.

Ancient copper mine
Copper deposit at Wadi Samra, Sinai
47

7) Turquoise
 Chemically, a hydrated phosphate of copper and aluminum
{CuAl6(PO4)4(OH)8*5H2O}, turquoise is formed by the percolation of
meteoric or groundwater through aluminous rock in the presence
of copper. For this reason, it is often associated with copper
deposits as a secondary mineral, most often in copper deposits in
arid, semiarid, or desert environments.
 Turquoise mining is known to have been carried
on at Serabit el Khadim, near Um Bogma, for an
extended period.
 Hume (1906) also reported turquoise
occurrences at Gebel Maghara.
 Turquoise mining is typically a small, labor-
intensive industry.
 Deposits generally occur as thin seams along
fractures or small pockets of pebbly stone in a
sandstone matrix.

To mine the turquoise and copper, the Egyptians would hollow out
large galleries in the mountains, carving at the entrance to each a
representation of the reigning pharaoh who was the symbol of the
authority of the Egyptian state over the mines. A huge quantity of
turquoise over that period was mined, carried down the Wadi
Matalla to a Garrisoned port located at el-Markha (south of Abu
Zenima), and loaded aboard ships bound for Egypt.
The turquoise was then used both for jewelry and to make color
pigments for painting. Stone tool assemblages made up of flint
scrapers, hand axes, and pounders comprise the largest corpus of
mining tools found at the Serabit el-Khadim turquoise and copper
mines (Elizabeth, 2010).
Copper staining, Eastern Desert, Egypt
49

The Sinai malachite (sehmet) and turquoise (mafaket)
deposits have attracted miners since the sixth
millenium BCE. Near Serabit el-Khadim, a few
kilometres inland from the western cost of the Sinai
peninsula, turquoise deposits were discovered by the
middle of the fourth millenium BCE and taken over by
the Egyptians a few centuries later. Following the
turquoise veins they excavated large galleries in the
sandstone, supported the roof with pillars and carved
at the entrance reliefs of the Pharaoh into the rock. In
winter water was conducted into the mine in order to
e x t r a c t t h e s t o n e s.
TURQUOISE DEPOSITS OF EGYPT
http://www.terraflex.co.il/ad/egypt/timelines/topics/mining.htm

Maps Bible Archeology Timna
Serabit el-Khadim, Egyptian
mining copper-turquoise
51

By about 3000 BC the Egyptians had become masters of the Sinai mines, and at
Serabit el-Khadem they set up a large and systematic operation. For the next two
thousand years, great quantities of turquoise were carved from Serabit el-Khadem
For the Egyptians, the brilliant blue-green stone served myriad purposes: scarabs
were carved from it, and the bright mineral enamels of powdered turquoise were
used to color everything from fine statuettes to bricks.
http://www.geographia.com/egypt/sinai/serabit.htm

Egyptian Turquoise
Egypt was a country rich in gold and precious stones.
2600 years BC, there were turquoise mines at Wadi Maghara in the Sinai.
53

Heavy Mineral Bearing Sands
 The beach sediments at El-Arish and surrounding on both eastern and western sides along the
northern Sinai coast are characterized by the presence of extensive black sand placer deposits.
 The area between Port Said to east of Bir El-Kharoba on the northern Sinai coast is
characterized by beach sediments containing a huge amount of black sands. The distribution
patterns of non-opaque heavy mineral assemblages and heavy mineral indices in the study area
were studied in details. The non-opaque heavy minerals in the investigated coastal sands
include, amphiboles, pyroxenes, epidotes, zircon, rutile, tourmaline and garnet (not necessarily
in this order of abundance), they constitute together more than 85% of the total assemblages.
Other minerals such as staurolite, biotite and monazite occur as minor components.
 The maximum, minimum and averages of the relative frequency percentage of the identified non-
opaque heavy minerals lead to establish three well defined non-opaque heavy mineral
provinces:
❖ The area between Port Said and east of El-Tinah bay, Rommana. The beach sands of this
area are characterized by the predominance of pyroxenes, amphiboles, epidotes, zircon and
reduced amounts of rutile, tourmaline and garnet. The great similarity between the distribution
of pyroxenes, amphiboles and epidotes in this mineralogical assemblage and those of the
main Nile sediments indicates their derivation from the Nile sediments contributed at El-Tinah
bay by the old extinct Pelusaic Nile branch which poured its sediments at Tel El-Farma, to be
drifted eastward by the Mediterranean long shore currents.
❖ The area between Port Said to east of Bir El-Kharoba on the northern Sinai coast is
characterized by beach sediments containing a huge amount of black sands.
❖ The area from Rommana to El-Arish. The beach sands in this area were characterized by the
high frequency of the ultra stable minerals (zircon, rutile and tourmaline) with considerable
amounts of amphiboles, garnet and epidotes and obvious lower values of pyroxenes. The
sands in this province are most probably derived from the neighboring sand dune by the
northwesterly winds prevailing in the area.
54

 The area between El-Arish and east of Bir El-Kharoba. The beach sands present in this area are
characterized by the enrichment of amphiboles, epidotes, garnet, staurolite with considerable
amounts of zircon, rutile and tourmaline. The reduced amounts of pyroxenes are also a distinctive
feature of this assemblage. The main source of these sands is Wadi El-Arish which drains big
quantities of fluvial sediments from both northern and central Sinai.
 At El-Arish and the area around it from both eastern and western sides the beach sediments are
characterized by containing a huge amount of black sand deposits, which in turn contains a number
of heavy economic minerals (Osman et al, 2008).
 These areas extend from 2 km West of Al Arish to the East of Sabkhat El Bardaweel over an area
of 18 km2.
 The total reserves in this area, to a depth of 1 m, are about 88 million tonnes with 1.1 million tonnes
as proved ore.
 The proved reserves to a depth of 10m are estimated by 3 million tonnes of ore. The concentration
and extension of the black sands to the East of Al Arish are negligible.
55

Sulfur
Elemental sulfur has been reported at Abu Durba, 40
km south of Abu Rudeis along the Gulf of Suez coast,
and in the Platform Province near Gebel Bedabaa and
the Agama Mound.
Near Abu Durba, sulfur is rumored to occur in fractures
in shale and sandstone of the Upper Ras Malaab
Formation. At these locations, sulfur is directly and
genetically related to gypsum-anhydrite deposits.
Comparable deposits have no practical potential as
sources of raw elemental sulfur.
Economically, the production of sulfur by acid
processing of gypsum-anhydrite holds greater
opportunities.
56

Figure 1: South Sinai map for metallic and
non-metallic deposit
Source: Metalogenic Map, EGSMA, 1998
A Abu Zunaymah Copper Western lower S. Sinai
H Wadi Nassib Copper Western upper S. Sinai
N Ra's Qillah Copper Eastern lower S. Sinai
B Umm Bujmah Carbonaceous Shale Western lower S. Sinai
D Wadi Thura Carbonaceous Shale Western upper S. Sinai
C Wadi as Shaww Uranium Western lower S. Sinai
E Wadi 'Alluqah Uranium Western upper S. Sinai
F Umm Bujmah Manganese Western upper S. Sinai
O Sharm ash Shaykh Manganese Eastern lower S. Sinai
G Sarabit al Khadim Turquoise Western upper S. Sinai
I Jabal Abu Thura Turquoise Western upper S. Sinai
J Umm Zurayq Fluorite Eastern lower S. Sinai
L Wadi at Tarr Soda Feldspar (Albite) Eastern lower S. Sinai
K Wadi Kid Pyrite Eastern lower S. Sinai
M Wadi Firani Pyrite Eastern lower S. Sinai
South Sinai Governorate
South Sinai is characterized manly by Turquoise, Uranium,
Copper, and Soda Feldspar in the metallic and non-metallic
category and by Limestone, Kaolin, Egyptian Alabaster,
and White Sand in the building materials and ornamental
stones category.
The governorate has 170 quarries by:
➢ 72 Stone Quarries
➢ 14 Natural Stone Quarries and Building Sand
➢ 37 Gypsum Quarries
➢ 33 Glass Sandstone Quarries
➢ 2 Shale Quarries
➢ One Dolomite Quarry

Reserves in South Sinai
Source: South Sinai Governorate, 2002
Material Reserve Reserve Geological Locations
Soda Feldspar (Albite) 26,000,000 tons 1,500,000,000 ton
40 km north Sharm El Sheikh, Sharm Dahab road & 20 km
east in Wadi El Tour
Potassium Feldspar 15,000,000 tons N/A Dahab & Newbie
Red Granite 477,000 m
3
1,431,000 m
3 Al 'Ayn al Akhdar, Wadi Firani, Wadi Shakik Al'Agouz, Wadi as
Sidd, Wadi Maktab, Wadi Mndira, Jabal al Looz
Pink Granite 21,118,800 m3
6,356,400 m3
Wadi Lathi, Wadi Zaghra, Wadi Umm as Sidd, Wadi al Osh,
Wadi Kassab, Wadi al Akhdar, Wadi Al Torfa, Wadi Soal, Wadi
Umm Adawi, Wadi al Giebi, Wadi Umm Looz, Wadi Umm Erk,
Wadi Sohieb, Wadi as Seida, Wadi Umm Amer, Wadi Nakhil,
Wadi al Megarra, Wadi Meknas, Wadi Abu Hasib, Wadi Torfat
al Kadreen, Bear Eliance, Wdai al A't, Wadi Maitora, Wadi
Mander, Wadi Umm Oror, Wadi al Hammam, Jabal al Manader,
etc..
Gray Granite 1,801,000 m
3
5,403,000 m
3
Wadi Raiha, Wadi al Rasasa, Jabal al Manader, Wadi Zagra,
Jabal al Mokhtar, Wadi Agir Ariha, Wadi Sahab, Wadi So Laf,
Wadi Miar, Wadi Seada, Wadi al Malha, Wadi Nakhil, Wadi
Mandiri, Wadi Nassib, Jabal ash Sheikh al Frenga, Wadi
Yahmed, Ayn al Akhdar, Wadi Mekhizna, Wadi Abu Hassib,
Jabal Khotar, Miah Dakik, Wadi Mander, Wadi Mokbela, Wadi
ak Keid, Wadi Madsos & Wadi Mozeimer
Rose & Pink Granite 995,000 m3
2,985,000 m3 Wadi Mander, Wadi Mokbla, Wadi an Nafkh, Wadi Umm Adawi,
Jabal ash Shallal, Wadi Zograh & Wadi al Mahash as Sofly
Black Granite 297,170 m
3
895,100 m
3 Wadi al Mahash al A'lla, Wadi Saal, Wadi an Nasb, Wadi
Zagrah, Wadi Firan, Wadi Mokbela & Wadi al Keid
Green Marble 160,000 m
3
480,000 m
3
Wadi Dehisa Abu Taleb & Wadi So Laf
Dark Brown Marble 120,000 m
3
360,000 m
3
Wadi Dehisa Abu Taleb & Wadi So Laf
Light Marble 30,000 m3
90,000 m3
Wadi Umm Grifat
Volcanic ashes 70,000 m3
210,000 m3
Wadi Okir & Wadi Khashib
Volcanic rocks 146,000 m
3
438,000 m
3
Wadi Umm Shoky, Wadi ash Shallal
Volcanic
Conglomerates
5,000 m3
N/A Wadi Zagrah
Yellow Limestone 225,750 m
3
N/A
Wadi Wata, Wadi as Seih, Wadi Kasseb, Wadi ash Shalah,
Jabal al Keih Wadi Umm al Baroud & Wadi Firan
Limestone 127,000 m
3
381,000 m
3 Wadi an Nazazat, Wadi Firan, Wadi Umm Mahagier, Wadi
al Karifi & Wadi al Kabbash
Black Limestone 205,000 m
3
N/A Jabal al Matalla
Gray Limestone 84,000 m
3
N/A Jabal al Bazary & Wadi as Sieh
White Sands N/A N/A
Abu Natsh, Abu Kafas, Farsh al Ghezlan, Aldehisah, Umm
Tamim, Nakb Bodra & Jabal al Gannah
Kaolin 9,610,000,000 tons N/A Masbaa Salamah, Wadi Natash, Wadi Bodra,
Gypsum 20,000,000 tons 216,000,000 tons Ras Mala'ab & Wadi El Rayainah
Coal 15,000,000 tons 60,000,000 tons
Bituminous Sand N/A 200,000,000 m3
Abu Darb

Figure 2:
South Sinai
map for
building
materials
and
ornamental
stones
Source: Metalogenic Map, EGSMA, 1998

REFERENCES
Attia, MI, & Ghalib, SE (1960). Ore minerals in Sinai. Sinai Manganese Co.: Arabic Internal Report.
Abdel Aziz A.H.(1990). Mineral deposits. Geological Survey of Egypt., Mineral deposits section 2.5 &
2.6, 557-558.
Abdel Razek, M.M.(1994). Geology and processing trials on kaolin - bearing sandstone from the
Gulf of Aqaba and Abu Zeneima areas, southern Sinai , Egypt . Geological Survey of Egypt, 1st
International symposium on industrial application of clays, 78-88.
British Geological Survey (1994). Mineral Resource Development in the Third World.
Boulis, S.N. & Attia, A.K.M.(1994). Mineralogical and chemical composition of carboniferous and
Cretaceous kaolin‟s from a number of localities in Egypt. 1st International symposium on
industrial application of clays, 99-127.
Egyptian Geological Survey and Mining Authority report on Glass sand of Sinai (1994).
El Sawy, S.M.(1994). Egyptian Kaolin as a filler and extender pigment for anticorrosive paints. Corro.
Prev. & Control, 41, 31 – 35.
Soliman, M. S.(1998). Limestone‟s appraisal of classifications and environmental modeling‟s.
Sedimentologic Lecture Season, 6, 196 – 198.
63

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