GEOCIENCIAS-VOL 14-1 2010.vp


EARTH SCIENCES

RESEARCH JOURNAL

Earth Sci. Res. J. Vol. 14, No. 1 (June 2010): 44-62

GEOPHYSICAL CONTRIBUTION TO EVALUATE THE

HYDROTHERMAL POTENTIALITY IN EGYPT:

CASE STUDY: HAMMAM FARAUN AND ABU SWIERA, SINAI, EGYPT

Magdy A. Atya1, Olga A. Khachay2, Aiman Abdel Latif1,

Oleg Y. Khachay2, Gad M. El-Qady1 and Ayman I. Taha1

1 National Research Institute of Astronomy and Geophysics, Helwan, Cairo, Egypt.
2 Institute of geophysics UD RAS, Ural’s state University, Russia.

ABSTRACT

The geothermal potentiality in Egypt has a minor significance in the aspects of the Egyptians life, while the hydraulic and hy-

drocarbon resources are more convenient. However, some other applications for the geothermal activity such as direct warm-

ing, pools, and physiotherapy make the research for geothermal as requested. In the present work, two locations with rather

good geothermal potentiality will be studied; these are Hammam Faraun and Abu Swiera (water temperature is about 70 °C; at

Sinai Peninsula).

The contribution of the geophysical techniques to evaluate such potentiality could be considered, as its capability to identify

the reservoir characteristics and its implementation is acceptable. Therefore, a geophysical survey program has been con-

ducted in terms of seventeen vertical electrical soundings (VES) and two wide profiles of Control Source Electromagnetic

(CSEM) forward step at Hammam Faraun and two wide profiles of CSEM at Abu Swiera. The geophysical techniques yield in-

formation on the spatial distribution of electrical conductivity, which is the most sensitive parameter to fluids in the rocks.

The analysis of the geophysical data, together with the field and geochemical studies lead to the conclusion that, the thermal

water in the subsurface formations might be considered as the preferred cause of the high conductivity in the subsurface

on/close to the boarder of tectonically active regions, particularly, where the anomalous conductivity is correlated with high

heat flow and other geophysical and geological parameters.

Key words: Hammam Faraun, Abu Swiera, vertical electrical soundings, control source electromagnetic, conductivity of

subsurface.

RESUMEN

La potencialidad de la energía geotérmica en Egipto tiene una importancia menor en los aspectos de la vida de los Egipcios,

comparado con los recursos hidráulicos y de hidrocarburos. Sin embargo, algunas aplicaciones de la actividad geotérmica,

como el calentamiento directo, las piscinas y la fisioterapia, hacen de la investigación de la energía geotérmica necesario. En el

presente trabajo, dos localidades con potencialidad geotérmica bastante buena serán estudiados; éstos son Faraun y Abu

Hammam Swiera (la temperatura del agua es de aproximadamente 70 °C, en la península del Sinaí).

44

Manuscript received: 03/02/2010

Accepted for publication: 14/04/2010



Debe considerarse la contribución de las técnicas geofísicas para evaluar el potencial así como la capacidad para identificar las

características del reservorio, y su aplicación. Un programa de prospección geofísica se realizó por medio de diecisiete

Sondeos Eléctricos Verticales (SEV) y dos de gran perfil con fuente Electromagnética controlada (CSEM) en Hammam Faraun

y dos grandes perfiles CSEM en Abu Swiera. Las técnicas geofísicas muestran información sobre la distribución espacial de la

conductividad eléctrica, que es el parámetro más sensible a los fluidos en las rocas.

El análisis de los datos geofísicos, junto con el campo y los estudios geo-químicos llevan a la conclusión de que, el agua termal

en las formaciones del subsuelo podría ser considerada como la causa de la alta conductividad en el subsuelo o cerca del borde

de la regiones tectónicamente activas, en particular, donde la conductividad anómala se correlaciona con el alto flujo de calor y

otros parámetros geofísicos y geológicos.

Palabras clave: Hammam Faraun, Abu Swiera, sondeos eléctricos verticales, control de código fuente electromagnética,

conductividad de superficie.

1. Introduction

Two sites have been selected to study the geothermal occur-

rences in the central part of Sinai Peninsula; Hamam Faraun

and Abu Swiera close to the Gulf of Suez (Figure 1). As

shown, the studied areas are located on the eastern side of

the Gulf of Suez region which represents one of the most

prolific and prospective oil provinces in Egypt. The area in-

cludes a number of oil fields such as Assel oil field. Hamam

Faraun lies at 29° 11´ 55.18``N and 32° 57´ 18.64´E and the

elevation is about 9 m above sea level, while Abu Swiera

area lies 29° 32´ 47.44``N and 32° 48´ 38.60´E and the ele-

vation is about 44 m above sea level. To spot more light on

Hamam Faraun and Abu Swiera Hot Springs, we carried out

Vertical Soundings (VES) and an approach to utilize

planshet Control Source Electromagnetic (CSEM) wide-pro-

files crossing the geothermal active fields. The main aim of

this study is to analyze the geophysical, geochemical, and

also the geological feed back in order to define the signifi-

cant tectonic patterns, which are responsible for the struc-

tural development of the geological units at the area of study.

The study resulted in understanding of the hydro-geother-

mal regime at Hammam Faraun and Abu Swiera through the

evaluation of the subsurface imaging and the capability for

investment projects.

2. Geology and tectonics

of Central Sinai Peninsula

The central part of Sinai province represents a tectonic spe-

cific belt put it as one of the most prolific and prospective oil

provinces in Egypt. In the early tertiary period (Oligocene -

Miocene), where the opening of the Red sea rift, some volca-

nic activity took place. In western and central Sinai, there are

a number of basaltic bodies mostly of doleritic dikes, sills

and plugs; flows are known near to Abu Zenima and

Hammam Faraun (Meneisy, 1990). The major geological

structural feature of the study area is a well-defined fault

block oriented NNW-SSE, which tilts strongly eastward on

its western side. Also there is a fault escarpment overlook-

ing directly the Gulf of Suez and rising about 300 m above

the Gulf (El-Shinnawi, and Sultan, 1973).

Hamam Faraun area is one of more vigorous topogra-

phy because of the presence of several local mountain ar-

eas (Gebel Hammam Faraun and Gebel Tall) of altitudes

varies from 50 to 480 m above sea level. The shallow geo-

logical succession in Hamam Faraun area (Fig. 2) could

be, mainly, distinguished into the following formation

(Said, 1962):

1. Post-Pliocene composed of sand and conglomerate

of about 50 m thickness.

2. Pliocene rocks, differentiated into sand, sandy lime-

stone, and lagoonal gypsum deposits of thickness

about 50 m.

3. Miocene and Oligocene rocks which composed of

gypsum, sandy marl and conglomerate with total

thickness of about 70 m.

4. Eocene rocks of total thickness 100m, which can

be differentiated into, upper Eocene of limestone

and sandstone, Middle Eocene of shale and lime-

stone, and Lower Eocene of chalk and flinty lime-

stone.

5. Upper Cretaceous rocks which are composed of

shale with minor limestone.

As for Abu Swiera hot spring, from the geological point

of view, the area is a triangular excavation represents the

synclinal trough to the southwest of El-halal anticline massif.

45

GEOPHYSICAL CONTRIBUTION TO EVALUATE THE HYDROTHERMAL POTENTIALITY IN EGYPT:

CASE STUDY: HAMMAM FARAUN AND ABU SWIERA, SINAI, EGYPT



The head of this triangle is directed northward while its base

measures a length of about 25 km facing Gebel Kharim in the

south. The length of this plain attains about 50 km. Its ground

elevation decreases northward from 300m at its base to about

190 m at its apex. The surface of these plains is dotted by nu-

merous mesas and buttes, which formed of early Eocene lime-

stone with cherty bands. This surface is dominated by

washed, dark angular to sub-angular cherty and limestone

fragments. Locally, these plains are covered by active sand

dunes, which form several lines of isolated branches. The area

is controlled by three different tectonic provinces related to

northern part of the African plate (Said, 1962). These are the

northern Egypt fold belt, NE-SW (Syrian arc system) and the

Suez rift which is younger than north Egypt fold belt, is domi-

nated by NW to NNW oriented normal faults.

3. Hydrothermal regime at the study sites

At Hammam Faraun, the spring issues thermal water at the

foot of the Gebel from fractured karstifed dolomitic

Eocene limestone Formation. The spring seepages were

estimated to 880 m3/d (El- Ramly, 1966), 3000 m3/d

(Himida and Diab, 1976). These seepages are drained

through minor channels mixed with the gulf water. The

thermal seepages are tested from Hammam Faraun cave.

H2S gas is present with its characteristic odor. The ther-

mal water seepage and flow toward the gulf water. Issar et

al. (1971) proposed a thermal flow mechanism in which a

sequence of aquifers is interconnected by means of a sys-

tem of faults and fractures zones, resulting in the occur-

rence of springs at the surface. The contribution of

various aquifers to the total outflow of spring is regulated

46

MAGDY A. ATYA, OLGA A. KHACHAY, AIMAN ABDEL LATIF, OLEG Y. KHACHAY, GAD M. EL-QADY AND AYMAN I. TAHA

MEDITERENEAN SEA

BAHARIYA

OASIS

OASIS

OASIS

OASIS

DAKHLA

KHARGA

G
U

L
F

O
F

S
U

Z
E

RED SEA

Eastern Desert

Western Desert

FARAFRA

CAIRO

29 00 ` 00 `31 33 00 ` 3500 `27 00 `25 00 `

31

00

29

00

27

00

25

00

QATTARA DEPRESSSION Ayun Musa

Ain Sukhna

12

9
6

13
10

11

8

15

167

5
4

3

1

2

14

Scale :-

0 40 80 100 Km.

Legend:-

Hot wells

Hot springs

32° 42’ 17” 32° 58’ 09.78”

29° 39’ 27.57”
Ras Sidr

Abou Swira

29° 11’ 29.40”

Gulf of Suez

Scale Hammam Faraun

0
13.5

27 km

32° 58’ 09.78”

N

W E

S

Figure 1: Location map of the studied area.



47

GEOPHYSICAL CONTRIBUTION TO EVALUATE THE HYDROTHERMAL POTENTIALITY IN EGYPT:

CASE STUDY: HAMMAM FARAUN AND ABU SWIERA, SINAI, EGYPT

Ras Sudr

Ras Matarmah

Legend

Gulf of Suez

Ras Malab

Abu Aggag Fm.

Duwi Fm.

Esna Fm.

G. El-Ahmar Fm.

Gharandal Group

Matulla Fm.

Ras Malaab Group

Sabkha deposits

Sudr Fm.

Tertiany Alkali Olivine Basalt

Thebes Group/Egma Fm.

Wadi Deposits

Alluvial Deposits
Scale

0 7,000 14,000 28,000
Meters

Figure 2: Geologic map of the studied area.



by their relative and absolute potentials. All the pressure

in these formation caves depleted with time, an Eocene

aquifer located at higher level began to flow and contin-

ues to do so to the present day.

ElRefeai (1992) and El-Kiki et al. (1992) carried out a

cluster analysis of the hydrochemical variables for wells

and springs tapping the deep aquifers in the Gulf of Suez

region. The produced dendrogram differentiate the

Eocene aquifer from the underlying (Nubia aquifers) and

the overlying Miocene one. In this dendrogram the

Hammam Faraun spring was designated as a member in

the cluster of Eocene aquifer in the region.The underlying

Esna shale is considered as the aquiclude, which separates

the Eocene beds from the underlying aquifer (Nubia).

However, the interconnection through the faults and frac-

ture zone should not be completely disregarded. Issar et

al. (1971) conceived an evaluation history of the forma-

tion waters in the Gulf of Suez region which the Eocene

aquifer is a product of mixing, through fracture system,

between ancient seawater and Pleistocene meteoric water.

Unfortunately, no more work related to Abu Swiera hot

spring.

4. Approach to use the Control Source

Electromagnetic (CSEM)

Concept of CSEM

The demand to the enhanced geophysical technique and de-

vice, in addition to the precise analytical interpretation of the

geophysical data, is the resolution of the geophysical com-

plex research, especially by the absence of priory informa-

tion about the researched place. The device for use the

planshet method of electromagnetic induction (Hachay O.

A., 1997a, Hachay O. A. and Bodin, 1997b, Hachay O. A. et

al., 1999, and 2000, Hachay O. A., 2002 ) in the frequency

domain was developed by Chelovechkov A.I. The method

was adapted to map and monitor the high complicated geo-

logical mediums, to determine the structural factors and cri-

teria of stability of the rock massif in the mine subsurface.

The field observation and the way of interpretation make the

new technology differ from other known earlier methods of

field raying or tomography (Hachay O. A. and Novgorodova

E. N., 1997c, Hachay O. A. et al., 1999, and 2000, and Lau

K.H., and Cheng P. 1977).

The concept to research the 3D geoelectric medium is

based on interpreting the alternating electromagnetic field in

the frame of a block-layered isotropic medium with inclu-

sions over three stages (Hachay 1997a, and 2002); in the

first stage, the geoelectric parameters of the horizontal

block-layered medium, which includes the block

heterogeneities, are defined, in the second stage, a geometri-

cal model of the different local heterogeneities or groups in-

side the block-layered medium is constructed based on the

data of local geoelectrical heterogeneities, while in the third

stage, the surfaces of the searched heterogeneities could be

calculated in account of the physical parameters of the

anomalous objects.

Obtainable field data

For practical realization of that conception, the system of ob-

servation for alternating electromagnetic field with use of

vertical magnetic dipole was elaborated. Such local source

of excitation and regular net of observations allows realizing

overlapping by different angles of observation directions.

As incoming data for interpretation, modules of three com-

ponents of magnetic field are used. For the case on surface

observations the data are measured on the Earth’s surface at

the set of distances between the source and receiver as a

function of frequencies. The measurements of the module of

three components of the magnetic field (vertical ��z� and

two horizontal: one directed to the source �Hr� and second

perpendicular to that direction �Hö�) are provided in the

frame of planshet for the fixed net with fixed step and fixed

length of the planshet’s side. In the frame of profile observa-

tions the planshet become to a band or a line and the length

of the band or the line is a base of observations or an array.

For the variant of the wide profile (band) the source of exci-

tation is located at the beginning of the array on the profile,

which is parallel to the measured profile. We shall call that a

wide array. It moves systematically with a fixed step of me-

ters. For the variant of a usual profile the source is located on

the measuring profile and the moving of the oscillator is sim-

ilar. For the variant of a planshet survey the source is located

into the center of the planshet using the fixed net of observa-

tion. Then the planshet array moves systematically with

overlapping usually on the half of the planshet.

Processing and interpretation of CSEM data

For each array and fixed frequency ù two interpretation pa-

rameters are defined:

ñeff (r)=ùr2(�Hz�/�Hr�)/ð ä(r) =(�Hö�/�Hr�)100%.

Where ñeff (r) is the apparent resistivity, r is the distance

between the source and the point of observation, ù is the fre-

quency f multiplied by 2ð, �Hz� is the module of the vertical

48

MAGDY A. ATYA, OLGA A. KHACHAY, AIMAN ABDEL LATIF, OLEG Y. KHACHAY, GAD M. EL-QADY AND AYMAN I. TAHA



magnetic component, �Hr� is the horizontal component of

magnetic field oriented to the source, ð = 3.14, ä(r) is the pa-

rameter of geoelectrical heterogeneity, and �Hö� is the sec-

ond horizontal component of magnetic field perpendicular

to the direction of the source.

That data are the information base for the further inter-

pretation. On the first stage we define the geoelectrical pa-

rameters of the 1-D section for each array and each

frequency after the preliminary filtration of the data:

ñeff (r): ä(r)<A

where A is a level of data filtration to the area of inverse

problem operator for one-dimensional medium (Hachay O.

A., 1997a).

The interpretation is made in a frame of n-layered model

for each array and planshet location. After that each point of

the planshet is associated with one and only column of layers

thicknesses and corresponding fixed column with resistance

of the medium in that layers. Gathering information of all

planshets together we obtain a many-valued function of each

point – distribution of thicknesses and resistances of the me-

dium layers. Then we calculate the average value for these

distributions for each point of the observation set. Thus we

obtain the unique distribution of thicknesses of horizontal

layers and resistances, which corresponds to the medium

model as a cylinder with vertical axis and with a rectangle at

the bottom and with a point of observation located in its cen-

ter. Thus we change over layered model to a block-layered

model. Then, gathering the values of thicknesses and

resistances for all points of observation, located on one and

the same profile we obtain the file of an average cross-sec-

tion along the profile.

The next step is combining the neighboring blocks with

close-range values of resistance to one block. That operation

is made according to the fixed scale of resistance.

The second stage of interpretation is used to define the

geometrical characteristics of conductive inclusions and

their equivalent moments, which are proportional to the ratio

of the conductivity difference in the host rock and in the in-

clusion to the conductivity in the host rock. Here the approx-

imation principle is used for alternating electromagnetic

fields. The initial model of the inclusion is a current line of

fixed length. That approximation construction is used for fit-

ting of the average parameter of geoelectrical heterogeneity,

which is calculated as an average value of ä in each point of

the profile, located in each point of the profile (Hachay O.

A., 2002).

5. Hammam Faraun Site

Hamam Faraun area is characterized by several hot

springs lying at the foot of Gebel H. Faraun along, a more

or less, straight line extending about one km along the

Gulf of Suez coast. The fault forms a steep cliff bordering

the Gulf of Suez. Two groups of thermal springs are

found. The northern group (70 �C) issues on land while

the southern group emerges beneath the surface of the

Gulf’s water. The cliff above the spring is composed of

dolomite. A geological examination of the area (Moon

and Sadek, 1923) indicates a gradual progressive change

from dolomite through dolomitic limestone to limestone

as one proceeds from the cliff inland. The heat source for

these springs is probably derived from high heat flow and

deep circulation controlled by faults associated with the

opening of the Red Sea and Gulf of Suez rifts. It is sup-

posed that the spring’s water is presumably a mixture of

brine and water of Pleistocene contained in the Nubian

sandstone aquifer which infiltrated the outcrops on the

highland of Sinai and emerged along the fault lines bor-

dering Sinai Peninsula (Magaritz & Issar, 1973).

6.1 Geophysical measurements

6.1.1 Vertical Electrical Soundings (VES);

At the area around Hammam Faraun, Seventeen Vertical

Electrical Sounding (VES) have been surveyed to AB/2 up to

1000 m in successive steps. The VES locations have been

chosen on the basis of the accessibility and applicability of

the Schlumberger method (Figure 3).

The apparent resistivity curves have been inverted into one

dimension model using the least square method to give a

multi layered resistivity model whose response fits the mea-

sured sounding curve. Zohdy’s method has been applied to

the observed data. The output of Zohdy’s method has been

used as a starting model in the Marquardt’s method to get the

best fit for the observed data. Figure (4) shows the resistivity

distribution in the study area. A general outlook to the inter-

pretation of the VESes curves reveals that, the number of the

interpreted layers is varying from five to seven layers

through the study area. The true resistivity of these layers is

varying from 0.2 to over 3000 ohm-m, while the thickness

varies from 0.9 to 291 m.

El-Qady et al, (2000) had conducted the 2D inversion for the

same data set using an algorithm based on the ABIC (Akaike

Bayesian Information Criterion, Akaike, 1980) algorithm to

obtain convergence to a solution with the optimum smooth-

49

GEOPHYSICAL CONTRIBUTION TO EVALUATE THE HYDROTHERMAL POTENTIALITY IN EGYPT:

CASE STUDY: HAMMAM FARAUN AND ABU SWIERA, SINAI, EGYPT



ness using a Finite Element calculation mesh. The integrated

2-D geoelectric cross section is illustrated in Figure 5. The

analytical reread of the site via resistivity distribution shows

the relation between the hot springs place and the

extensional cave inside Gebel Faraun, while this place de-

scribes a resistive strata setting forming the massive base

and extending inward the mountain, where the cave shows

higher temperature as man goes more inside. Then it is sup-

posed that the hot water comes through the fractures con-

nected to this base.

5.1.2. CSEM data

The observation system at Hammam Faraun includes

the measurements along two wide profiles (Fig.3); a longitu-

dinal profile on the road band between the mountain and the

shoreline of the Red Sea, and a traversal profile. The longitu-

dinal wide profile is of 400 m length and the band width of

the profile is 20 m, the distance between the observations

points is 25 m, and between the source locations is also 25 m.

The outlet of thermal hot waters is located on the profile be-

tween the 4th and 5th pickets of the observation points. The

traversal wide profile begins at the sea shoreline traversing

the road band and climbing the mountain margins, its length

is 95 m and the band width of the profile is 10 to 15 m, the

observations are carried out on 5 m separated points, while

the distance between the sources of excitation is 15 m. The

transversal profile crosses the longitudinal wide profile at

the pickets 17th and 18th.

The distribution of the average parameter of the

geoelectrical heterogeneity at referenced frequencies for

both the longitudinal and traversal wide profiles is shown in

figure (6a and b) respectively. On figure (6a), for the fre-

quency 5.08 kHz and starting from the 7th picket of observa-

tion, local anomalies and raising of the background

component of the parameters could be clearly noticed, the

largest values of the average parameter of geoelectrical het-

erogeneity are recognized for the frequency 2.54 kHz on the

pickets 13 and 15. The values of the traversal wide profile

(Fig.6b) are significantly lower in comparison with the lon-

gitudinal wide profile, which testifies the more homoge-

neous structure of the massif in the transversal direction.

Approximately to the middle of the profile (picket 11) there

are anomalies in the distribution of the parameter on the fre-

quency 0.635 kHz, for the second part we see the increasing

of its values for higher frequencies, what can testify the more

homogeneous structure for that places on the deeper depths.

50

MAGDY A. ATYA, OLGA A. KHACHAY, AIMAN ABDEL LATIF, OLEG Y. KHACHAY, GAD M. EL-QADY AND AYMAN I. TAHA

Gulf of Suez

Topography (100 m)

Hot spring

Water well

Sinai Mang. Company

VES’s Location & number
CSEM profile

Figure 3: Location Map for the Geophysical Survey at Hammam Faraun area



Figure (7) shows the geoelectrical cross sections with

blocked structure and distribution of crack zones in the mas-

sif at the three controlled excitation frequencies. On the sec-

tions, the contact of the block structure on the pickets 3 and

17 could be sharply seen. The visual inspection and the geo-

logical survey show that zones are looking from the surface

as faulted and cracked zones. The geoelectrical structure of

the block from picket 3 to 17, beginning from the depth 92 m

practically does not change its characteristics. It testifies that

for increasing the resolution for deeper areas we must in-

crease the base of observation and use lower frequencies

with the same step of observation.

Approximately up to 72 m on the blocked sections, the

thermal outlet is situated together with cracked and very

conductive rocks, around the 11th picket of observation,

the cracked zones reach about 40 m depth. On the section

representing the frequency 2.54 kHz (Fig. 7b) and at the

pickets 2–6, the block of rocks with low resistance, which

are linked with the zones of outlet and location of high hot

thermal water is well mapped. On the same section we see

a near surface structure (up to 12 m), which is linked with

the outlet of the vertical fault zone, which is linked with

the contact. The results of observation on the frequency

0.635 kHz testify and increase that conclusion. Thus the

provided electromagnetic induction observations on the

three frequencies give the information about the geometry

of the thermal reservoir and also about the degree of rocks

faulting, of which consists the block. The last information

51

GEOPHYSICAL CONTRIBUTION TO EVALUATE THE HYDROTHERMAL POTENTIALITY IN EGYPT:

CASE STUDY: HAMMAM FARAUN AND ABU SWIERA, SINAI, EGYPT

Gulf of Suez

Gulf of Suez

Gulf of Suez

Gulf of Suez

Figure 4. Resistivity contour maps at different values of AB/2 at H. Faraun Area.



52

MAGDY A. ATYA, OLGA A. KHACHAY, AIMAN ABDEL LATIF, OLEG Y. KHACHAY, GAD M. EL-QADY AND AYMAN I. TAHA

Figure 5: Integrated 2-D geoelectric cross section at Hamam Faraun hot spring area (El-Qady et al., 2000).

1000
950
900
850
800
750
700
650
600
550
500
450
400
350
300
250
200
150
100

50
0

�, %

2 4 6 8 10 12 14 16

5.08 kHz
2.54 kHz
.635 kHz

(a)
The longitudinal

wide profile

N

Figure 6: Distribution of the average parameter of geoelectrical heterogeneities along the longitudinal and the traversal (a) and (b) respec-

tively wide profiles (Fig. 3).

�, %
100

90

80

70

60

50

40

30

20

10

0
0 2 4 6 8 10 12 14 16 18 20

5.08 kHz
2.54 kHz
.635 kHz

(b)
The traversal
wide profile

N



53

GEOPHYSICAL CONTRIBUTION TO EVALUATE THE HYDROTHERMAL POTENTIALITY IN EGYPT:

CASE STUDY: HAMMAM FARAUN AND ABU SWIERA, SINAI, EGYPT

1 3 5 7 9 11 13 15 17

-152

-132

-112

-92

-72

-52

-32

-12

0 50 100 150 200 250 300 350 400

Pk

m

m

0 20 50 90 150 200 300 400 500 1000 5000 or more (Om"m)

Mo~

less .1

.1 - .2

.2 - .5

.5 - .7

.7 - 1

1 - 2

2 - 4

4 - 6

6 - 10

10 or more

-152

-132

-112

-92

-72

-52

-32

-12

0 50 100 150 200 250 300 350 400

1 3 5 7 9 11 13 15 17Pk

m

m

0 20 50 90 150 200 300 400 500 1000 5000 or more (Om"m)

Mo~

less .1

.1 - .2

.2 - .5

.5 - .7

.7 - 1

1 - 2

2 - 4

4 - 6

6 - 10

10 or more

1 3 5 7 9 11 13 15 17

-152

-132

-112

-92

-72

-52

-32

-12

0 50 100 150 200 250 300 350 400

Pk

m

m

0 20 50 90 150 200 300 400 500 1000 5000 or more (Om"m)

Mo~

less .1

.1 - .2

.2 - .5

.5 - .7

.7 - 1

1 - 2

2 - 4

4 - 6

6 - 10

10 or more
(c)

0.635kHz.

(b)

2.54 kHz.

(a)

5.08 kHz.

Figure 7. Geoelectrical cross-sections along the longitudinal wide profile in Hammam Faraun.



54

MAGDY A. ATYA, OLGA A. KHACHAY, AIMAN ABDEL LATIF, OLEG Y. KHACHAY, GAD M. EL-QADY AND AYMAN I. TAHA

0 2 4 6 8 10 12 14 16 18 20

-152

-132

-112

-92

-72

-52

-32

-12

0 10 20 30 40 50 60 70 80 90 100

Pk

m

m

0 20 50 90 150 200 300 400 500 1000 5000 or more (Om"m)

Mo~

less .1

.1 - .2

.2 - .5

.5 - .7

.7 - 1

1 - 2

2 - 4

4 - 6

6 - 10

10 or more

0 2 4 6 8 10 12 14 16 18 20

-152

-132

-112

-92

-72

-52

-32

-12

0 10 20 30 40 50 60 70 80 90 100

Pk

m

m

0 20 50 90 150 200 300 400 500 1000 5000 or more (Om"m)

Mo~

less .1

.1 - .2

.2 - .5

.5 - .7

.7 - 1

1 - 2

2 - 4

4 - 6

6 - 10

10 or more

0 2 4 6 8 10 12 14 16 18 20

-152

-132

-112

-92

-72

-52

-32

-12

0 10 20 30 40 50 60 70 80 90 100

Pk

m

m

0 20 50 90 150 200 300 400 500 1000 5000 or more (Om"m)

Mo~

less .1

.1 - .2

.2 - .5

.5 - .7

.7 - 1

1 - 2

2 - 4

4 - 6

6 - 10

10 or more(c)
0.635 kHz

(b)
2.54 kHz

(a)
5.08 kHz

Figure 8. Geoelectrical cross-sections along the traversal wide profile in Hammam Faraun.



will be more significant if we shall provide additional cy-

cles of observation for identification of the stability state

of the reservoir.

Figure (8) represents the detailed geoelectrical cross-sec-

tions, which had been constructed for the data of the tra-

versal wide profile for the three frequencies. That section

reflects the geoelectrical characteristics in the vicinity of

the contact with the block of the first wide profile. From

the depth 52 m the cross sections for all frequencies show

the same block structure: on the 9th picket, on the depth

92–112 m we see a contact in the high resistance bottom

of the section. The conductive rocks are situated aver-

agely up to the depth 30 m, and the crack zones of weak in-

tensity up to the depth 12 m.

6. Abu Swiera Site

At this site we carried out CSEM survey only. The electro-

magnetic observations measured around the thermal sources

outlet has been provided using the method of area planshet

survey: in which, the sources of excitation has been located

on a middle profile between two receiving profiles (observa-

tion lines) forming an area planshet. The distance between

the excitation source profile and the observation profiles is

15 m, while the points of observation have been situated

with a step 5 m. The length of the observation profiles

reached 100 m using two controlled source frequencies are

5.08 kHz and 0.635 kHz (Fig. 9). The distribution of the av-

erage parameter of the geoelectrical heterogeneities along

55

GEOPHYSICAL CONTRIBUTION TO EVALUATE THE HYDROTHERMAL POTENTIALITY IN EGYPT:

CASE STUDY: HAMMAM FARAUN AND ABU SWIERA, SINAI, EGYPT

Figure 9. Location map of the area planshet wide profiles around the thermal water source at Abu Swiera, Sinai Peninsula, Egypt.



Line 1 and Line 2 within the area planshet wide profiles is

shown in figure (10).

The geoelectrical cross-sections are shown in figure (11)

as (a) and (b) are for Line 1 and (c) and (d) are for Line 2.

The results testify that the search of the source of the hy-

drothermal system and the inlet channels to their outlet on

the surface is a very complicated structural, manly ranged

problem and demands methods with high resolution and

high comprehensiveness. So for the band 30 m for the ob-

56

MAGDY A. ATYA, OLGA A. KHACHAY, AIMAN ABDEL LATIF, OLEG Y. KHACHAY, GAD M. EL-QADY AND AYMAN I. TAHA

100

90

80

70

60

50

40

30

20

10

0

�, %

5.08 kHz
2.54 kHz
.635 kHz

2 4 6 8 10 12 14 16 18 20

Line 1

�, %
350

300

250

200

150

100

50

0
2 4 6 8 10 12 14 16 18 20

5.08 kHz
2.54 kHz
.635 kHz

Line 2

Figure 10. Distribution of the average parameter of the geoelectrical heterogeneities along Line 1 and Line 2 in the area planshet wide pro-

files around Abu Swiera hot spring, Sinai Peninsula, Egypt.

1 3 5 7 9 11 13 15 17 19 21

-152

-132

-112

-92

-72

-52

-32

-12

0 10 20 30 40 50 60 70 80 90 100

Pk

m

0 20 50 90 150 200 300 400 50010005000 or more (Om"m)

Mo~

less .1
.1 - .2
.2 - .5
.5 - .7
.7 - 1
1 - 2
2 - 4
4 - 6
6 - 10

10 or more

1 3 5 7 9 11 13 15 17 19 21

-152

-132

-112

-92

-72

-52

-32

-12

0 10 20 30 40 50 60

70

80 90 100

Pk

m

m

0 20 50 90 150 200 300 400 50010005000 or more (Om"m)

Mo~

less .1
.1 - .2
.2 - .5
.5 - .7
.7 - 1
1 - 2
2 - 4
4 - 6
6 - 10

10 or more

1 3 5 7 9 11 13 15 17 19 21

-152

-132

-112

-92

-72

-52

-32

-12

0 10 20 30 40 50 60 70 80 90 100

Pk

m

m

0 20 50 90 150 200 300 400 5001000 5000or more (Om"m)

Mo~

less .1
.1 - .2
.2 - .5
.5 - .7
.7 - 1
1 - 2
2 - 4
4 - 6
6 - 10

10 or more

1 3 5 7 9 11 13 15 17 19 21

-152

-132

-112

-92

-72

-52

-32

-12

0 10 20 30 40 50 60 70 80 90 100

Pk

m

m

0 20 50 90 150 200 300 400 500 10005000or more (Om"m)

Mo~

less .1
.1 - .2
.2 - .5
.5 - .7
.7 - 1
1 - 2
2 - 4
4 - 6
6 - 10

10 or more

(b)

Line 1
0.635 kHz

(a)

Line 1
5.08 kHz

(a)

Line 2
5.08 kHz

(b)

Line 2
0.635 kHz

Figure 11. Geoelectrical cross-sections; (a) and (b) represent Line 1, while (c) and (d) represent Line 2 in the area planshet observation sys-

tem at Abu Swiera, Sinai Peninsula, Egypt.



tained geoelectrical cross sections we see the difference in

the blocked structure, beginning from the depth 52 m.

Similar differences are in the upper levels of the sections

and in the crack zones location. If we take into account,

that the place of the outlet location of the source of the hot

water was known, the picket 2 on the source profile, so we

can formulate recommendations for using that method to-

gether with other geophysical and geochemical methods

for solution of the problem for searching the state of the

geothermal system.

7. Geochemical analysis

This study has been done to estimate the variation of the

chemical composition of the geothermal waters and to deter-

mine the subsurface temperature of the water reservoirs in

these regions. Chemical geothermometers are applied to the

hydrochemical data. Also, the hydro-geochemical charac-

teristics of the collected thermal water from hot springs are

taken in consideration.

7.1. Material and methods

Two groups of geothermal water samples have been col-

lected from Hammam Faraun and Abu Swiera hot springs.

Their locations are illustrated in Fig. (1). It is found that the

total dissolved salts content range from 6053.49 to 12687.1

ppm. The samples of thermal water were stored in polyethyl-

ene bottles. The electrical conductivity (EC), temperature

and pH values of the geothermal water samples were mea-

sured after taken from the field directly. The chemical anal-

57

GEOPHYSICAL CONTRIBUTION TO EVALUATE THE HYDROTHERMAL POTENTIALITY IN EGYPT:

CASE STUDY: HAMMAM FARAUN AND ABU SWIERA, SINAI, EGYPT

Figure 12. Piper diagram for the major cations and anions for Abu

Swiera and Hammam Faraun in Egypt.

Io
n

E
xc

ha
ng

e

M
ixi

ng
lin

e

R
ev

er
se

io
n

E
xc

ha
ng

e

Figure 13. Durov diagram for the major cations and anions for the

Abu Swiera and Hammam Faraun in Egypt.

N
a

+
K

Cl + SO

HCO + CO3 3

4

Groundwater

0
0

Ocean

50

40

30

20

10

0
0 10 20 30 40 50

1 2

Seaw
water-groundwater mixing-line In

te
ra

ct
io

n
w

ith
C

O
2

C
a

+
M

g

50

Figure 14. Langelier –Ludwig diagram for the Abu Swiera and

Hammam Faraun in Egypt.

Sea water

Rain water

1

2

Concentration (meq/l)

1000.

100.

10.

1.
Mg Ca Na+K Cl So HCO4 3

Figure 15. Schoellar diagram for the major cations and anions for

the Abu Swiera and Hammam Faraun in Egypt.



ysis of underground water samples were carried out in

laboratory of the Ministry of Agricultural in Cairo, to calcu-

late the values of Na, K, Mg, Ca, Cl, SO4 and HCO3 ( mg/l),

results are listed in Table(1). The results have been evalu-

ated by applying the Aquachem (Calmbach, 1997) and

Wateq (Truesdell and Jones 1974) programs.

7.2 Classification of water chemistry data

Graphical and statistical methods were used to classify the

water sample into groups. Piper, Durov, Schoeller and

Langelier- Ludwing, and Q- mode cluster analysis were ap-

plied as follows; Piper diagram (1944) that modified by

Langguh (1966) shows that samples numbers 1 and 2 are al-

kaline water with prevailing sulfate chloride (Fig.12), Durov

digram (Llyod and Heathcoat, 1985): Figure (13) shows the

sample numbers 1 and 2 have Cl and Na dominant fre-

quently indicate the end point of water, Langelier –Ludwing

diagram (Fytikas et al, 1989): shows that the samples are

Na-SO4 water types(Fig.14), and Schoellar diagram (1962)

applied on the collected samples and shows that the samples

numbers 1 and 2 are similar to each other reflect the same

aquifer characters (Fig.15). When correlation with Gulf of

Suez and rain water , we fiend that sample numbers 1 and 2

related to rain water and affected by Gulf of Suez water with

different ranges.

7.3 Cluster analysis

The cluster analysis has been applied using the statistical

package (SPSS 13).The Euclidean distance as similarity

measurement together with Word `s method for linkage has

been used to produce grouping. A dendrogram of Q-mode

cluster analysis (Fig.16) shows two groups, the first contain

the sample number 1 and rain water have similarity at dis-

tance cluster 1 and sample number 2 at distance cluster

2.5.The second group contain Gulf of Suez water. This coin-

cidence the affect of rain water is more than the Gulf of Suez

water.

7.4 Principal component analysis (PCA)

The principal component analysis (PCA) has been exten-

sively applied to different the samples to be compared and

give finer prints to identifying the origin of the chemical

origin (Fig. 17). PCA results declare the contribution de-

gree of variation in the data of the study area. 60.201 % 1st

PC 35.186% for 2nd PC and 4.613 %for 3rd PC of data set.

The 1st PC is strong positive distribution of the loading

values for TDS, Cl, SO4 and HCO3 and moderate positive

loading on pH, Mg and Ca but negative with K. These ions

have dominant contribution to the explanation of the PC1.

The strong positive terms are due to dissolution of salts of

the geological components. The factor 2 is Ca enrichment

factor. The presence of dissolved carbonate might en-

hance or suppress adsorption and forming precipitates.

Factor 3 has strong positive loading with Ca, Mg and SO4,

moderate with TDS, Na and small with Cl. The negative

loading with K and HCO3, suggesting that two have the

same source of fresh water resulting from dissolution by

the rain water.

58

MAGDY A. ATYA, OLGA A. KHACHAY, AIMAN ABDEL LATIF, OLEG Y. KHACHAY, GAD M. EL-QADY AND AYMAN I. TAHA

Dendrogram using Ward Method

Rescaled Distance Cluster Combine

Case 0 5 10 15 20 25

Label Num +– – – –+– – – –+– – – –+– – – –+– – – –+

1

Rainwater 3 =

2
Sea water

4

Figure 16. Q-mode analysis of groundwater samples.

Table 1: Fresh water and sea water percentages in water from study area calculated by means of Aquachem (Calmbach,

1997).

Sample No. Water sample name Fresh water % Sea water %

1 Abuo Sira 90 10

2 Hammam Pharoun 80 20

3 Rain water 100 0

4 Gulf of Suez 0 100



59

GEOPHYSICAL CONTRIBUTION TO EVALUATE THE HYDROTHERMAL POTENTIALITY IN EGYPT:

CASE STUDY: HAMMAM FARAUN AND ABU SWIERA, SINAI, EGYPT

Table 2. Subsurface temperature values in hot springs by geochemical thermometers.

Sample
No.

Calculated the groundwater temperature by using different geothermometers methods in degree °C

K/Mg
Giggenbach
et al 1983

Na/K
Fournier &
Truesdell

1973

Na/K
Truesdell

1976

Na/K
Fournier &

Porter
1979

Na/K
Fournier

1979

Na-K-Ca
Fournier

1979

Chalcedony
Fournier

1977

Quartz
Fournier

1977

Quartz
Fournier

1977

NA/Li
Kharaka

1989

1 41 214 216 262 239 206 62 93 95 79

2 48 110 119 175 160 163 62 93 95 60

1.6 E9

1.4 E9

1.2 E9

1.0 E9

8.0 E8

6.0 E8

4.0 E8

2.0 E8

0.0 E0

E
ig

en
va

lu
e

1 2 3 4 5 6 7 8 9 10 11
Component number

Scree Plot

Component Plot in Rotated Space

Component 1

C
om

po
ne

nt
2

Component 3

0

0.5

1.0

1.5

2.0

1.2

1

0.8

0.6

0.4

0.2

0

-0.2

-0.4

-0.6

1.2

1

0.8

0.6

0.4

0.2

0

-0.2

-0.4

0.4

0.3

0.2

0.1

0

-0.1

-0.2

-0.3

pH Tw
a

C
on

d

TD
S N
a K M
g

C
a C
l

S
O 4

H
C

O 3

Tw
a

C
on

d

TD
S N
a K M
g

C
a C
l

S
O 4

H
C

O 3

1

1
Series 2

Tw
a

C
on

d

TD
S N
a K M
g

C
a C
l

S
O 4

H
C

O 3

Series 3

Figure 17. Factor analysis of the groundwater chemistry analysis.



Table 1 shows the percentage of Gulf of Suez and rain

water calculated by means of Aquachem (Calmbach, 1997)

by optimizing Cl and TDS mass balances.

The water samples numbers 1 and 2 having 90 % and

80% from rain water respectively. These indicate that sam-

ple no.2 is affected by Gulf of Suez water than sample no.1.

Then, the salinity of Hammam Faraun is higher than that of

Abu Swiera spring. The acquired salinity of Hammam

Faraun is probably, resulted from their mixing between the

Eocene aquifer (similar to the Abu Swiera water) and the

presented seawater due to its location at the seashore or to

the product of rock-water interaction.

Cl-SO4-HCO3 Ternary diagram (Fig.18); according

to Giggenbach, 1988, and Giggenbach and Goguel, 1989)

shows that sample no.1 mature waters while sample 2 lie on

the line between chloride water and volcanic water.

Na-K-Mg diagram (Giggenbach, 1988) (Fig.19) is

used to differentiat between immature, partially equilibrated

and full equilibrated water. It predicts the temperature of res-

ervoir and the relationship of equilibrium of the water and

host rock. The sample no.2 lies on the line between imma-

ture water and partially equilibrated water. It lies between

temperature lines 160 and 180 °C as sample no.1 lies be-

tween lines 240-260 °C.

In this study, temperature of the hydrothermal aquifer

has been evaluated by using geothermometers methods

through Aquachem Program (Calmbach, 1997) and tabu-

lated in Table (2).

8. Discusión and conclusión

Two sites have been selected to study the geothermal oc-

currences in central part of Sinai Peninsula; Hamam Faraun

and Abu Swiera close to the Gulf of Suez. The geophysical

measurements on both sites showed that the uppermost 40

meters are cracked low resistive medium connected to a

massive resistive base rock. This base rock could be the

container of thermal water or at least adjacent to the source

of heating. Practically, this can be evidenced by the

extensional cave in Gebel Faraun heart, where the more in-

side in lateral and downward directions results the raise in

temperature, which might be interpreted as being closer to

the heat source.

Now it becames an objective need of developing a com-

plex direction of research, which must ensure the theoretical

base of exploration and operation of geothermal deposits.

That direction must include all key problems, which are

linked with their developing such as:

1. Developing of geological models of geothermal de-

posits on the base of detailed geological mapping of

volcanic magmatic complexes, which are sources of

heat feeding of hydrothermal systems and revealing

of the hydrothermal reservoirs structure.

2. Providing and interpretation of the geophysical data

on the base of models, which are adequate to the ge-

ometry of the geothermal reservoirs in the volume,

research of the headrace, along what moves the heat

60

MAGDY A. ATYA, OLGA A. KHACHAY, AIMAN ABDEL LATIF, OLEG Y. KHACHAY, GAD M. EL-QADY AND AYMAN I. TAHA

Steam heated water

Chloride waters

Sulphate waters Bicarbonate waters

Na
- CI M

ature
lW

ater

Peripheral water

Vo
lc

an
ic

w
at

er

Figure 18. Relative Cl,SO4 and HCO3 contents of Abu Swiera and

Hammam Faraun in Egypt.

20

40

60

80

100

20 40 60 80 100

Fully Equilibrated

Waters

Na 001+

Immature Waters

Partially Equilibrated Waters

K*.01
SQR(Mg)

Figure 19. Graphical evaluation of the water –rock equilibration

temperature after Giggen- bach, 1988; Giggenbach and Coralles,

1992 using relative Na, K and Mg concentrations (mg/Kg) of Abu

Swiera and Hammam Faraun in Egyp



flow. In that case, a very informative method (Con-

trol Source Electromagnetic induction frequency –

geometrical research) which is introduced in this

paper shows the capability to provide the adequate

resolution to analyze and probably solve the geo-

thermal problems.

3. The development models of geophysical and geo-

chemical character, which are used for revealing of

the flow picture and estimation of the dynamical

characteristics of the heat flow on the base of the

geophysical monitoring data.

The geochemical analysis to the two samples groups

showed that the TDS is ranging from 6053.49 to 12687.1 ppm,

the water chemistry was classified as alkaline water with pre-

vailing sulfate chloride (Piper diagram), the existence of Cl

and Na as dominant frequently indicates the end point of wa-

ter (Durov diagram) and a relation to rain water affected with

the gulf water was concluded. The interpretation of the factor

analysis model is matching well with all results of Sholler

analysis and Aquachem program as the thermal water were a

mixing with meteoric water explain the hydrochemical varia-

tion of the thermal water within the Eocene aquifer.

The present study concludes that the two sites are excellent

places for investment in thermal water utilization just for

aqua thermal pools, thermotherapy, and thermal basins.

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62

MAGDY A. ATYA, OLGA A. KHACHAY, AIMAN ABDEL LATIF, OLEG Y. KHACHAY, GAD M. EL-QADY AND AYMAN I. TAHA