JAKU: Earth Sci., Vol. 22, No. 2, pp: 185-201 (2011 A.D. / 1432 A.H.)
DOI: 10.4197 / Ear. 22-2.8
Hydrochemistry of the Groundwater Aquifer in As Suqah
Area, Makkah District, Western Arabian Shield, Saudi
Arabia.
Mohammed Amin M. Sharaf
Faculty of Earth Sciences, King Abdulaziz University
P.O. BOX 80206, Jeddah, 21589, Saudi Arabia
E-mail: [email protected]
Received: 29/06/2010
Accepted: 30/10/2010
Abstract. This study dealt with the hydrochemistry of As Suqah area,
NE of Jeddah, Saudi Arabia. The study is based on the analyses of the
major and trace elements of 16 water samples. The groundwater
shows relatively high concentrations in their overall mineral contents
and a high EC, TDS, and total hardness as CaCO3.
Two groundwater types were identified in the As Suqah area:
Na-Mg-Ca-Cl-SO4 and Na-Ca-Mg-Cl water types. Sodium adsorption
ratio has a mean value of 14.39. The exchangeable sodium ratio has a
mean value of 0.456 and a maximum value of 1.706. The average
magnesium hazard was found to be about 49.97. The groundwater in
As Suqah area was slightly supersaturated with respect to calcite and
supersaturated with respect to dolomite. The mean saturation indices
for these species are 1.21 and 2.60 respectively. The main
hydrochemical processes responsible for the above discussed variation
in water quality are recharge, ion-exchange and mineral dissolution.
The water quality within the sedimentary succession was found to be
of relatively higher salinity. Its use is restricted for domestic use only
if adequately treated.
Keywords. Makkah district, Usfan groundwater, Wadi As Suqah area,
Western Saudi Arabia.
Introduction
As Suqah area lies about 70km N to NE of Jeddah city within a typical
arid region, the average rainfall amounts to around 100mm. per year, the
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Mohamed Amin M. Sharaf
average evaporation rates exceed 2000 mm. per year. Rainfall usually
occurs during the months of December and January. Spring rainfall
events may occasionally occur during the months of April and May.
From the geologic point of view, the study area comprises
Precambrian-Cambrian basement rocks, Cretaceous-Tertiary sedimentary
succession, the Tertiary- Quaternary basaltic lava flows, and the
Quaternary-Recent alluvial deposits. Wadi As Suqah is a NW-SE low
lands surrounded from the west by Precambrian rocks overlain by black
basaltic lava flows (Harrat, Fig. 1, 2).
The Precambrian rock units in the study area have been studied by
different workers of the Directorate General of Mineral Resources (e.g.
Al-Shanti, 1966). According to Moore and Al- Reheili (1989), the
basement rocks in the study area consist of Late-Proterozoic basaltic to
rhyolitic volcanic and volcanoclastic and epiclastics of primitive islandarc type, that have been repeatedly deformed and metamorphosed and
injected by intrusive bodies of different ages and compositions. These
rock units are divided into Zibarah, Samran, and Fatimah groups
(sedimentary rocks). Plutonic rock units are gabbro, diorite, tonalite and
granodiorite to monzonite of probably early Cambrian ages.
Fig. 1. General geologic map showing the location of wadi As Suqah.
Hydrochemistry of the Groundwater Aquifer in As Suqah Area, Makkah District…
187
Fig. 2. Detailed geologic map showing the locations of the studied boreholes of As Suqah
area.
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Mohamed Amin M. Sharaf
The Cenozoic sedimentary rocks are exposed beneath a cover of
flat-lying lavas and Quaternary deposits in the study area. Brown and
others (1963) assigned the terms of Shumaysi and Usfan formations to
these sedimentary sequences after Karpoff (1958). Spincer and Vincent
(1984) subdivided the sedimentary rock group into the Haddat Ash Sham,
Shumaysi, Khulays, and Buraykah Formations.
Basalt lava flows form discontinuous caps overlying the upper
levels of both the basement complex and the sedimentary rocks; the lavas
either rest on peneplain or infilled ancient wadis. They are preserved in
three north-northwest trending, asymmetric depositional troughs which
are the Sham, Suqah and Shumaysi troughs. These troughs are bounded
in the north by faults downthrown to the west and in the west by an
unconformity at the base of the easterly dipping strata.
Quaternary deposits cover large parts of the study area. They
principally occur in the large drainage basins of Haddat Ash Sham. The
principle units of the Quaternary rocks are the terrace gravel, alluvial fan
deposits, tallus deposits, alluvial sands and gravels of wadi beds and
some eolian edifices. The thickness of these deposits varies widely from
one place to another.
Three main sets of faults: NW, NE and N. The NW faults are the
oldest and seem to have controlled the depositional troughs in the study
area, mainly those of Haddat Ash Sham and As Suqah. They are mostly
normal faults dipping steeply to the southwest. The NE faults displace
the NW set and seem to be second component in block faulting. The N
trending faults are shear faults with lateral displacement for the above
mentioned NW and NE sets.
Groundwater Occurrences
Several hydrogeological research activities have taken place in
Jeddah area and its hinterland since the early seventies of this century.
Italconsult (1967) drilled three boreholes in the study area to determine
the thickness of the alluvial deposits and the depth to the basement
complex. Kotb et al. (1988) gave a general overall view of the
hydrochemical characteristics of groundwater in the Usfan Basin and
they indicated that, the groundwater therein is of Cl-Na type and the
general trend of salinity variation in the groundwater of the Usfan Basin
Hydrochemistry of the Groundwater Aquifer in As Suqah Area, Makkah District…
189
was found changing from secondary to primary type. Sharaf (2009 a and
b) carried out a geophysical and hydrochemical study on Haddat Ash
Sham and Ash Shamiyah areas and concluded that, the groundwater is
mainly present in the Quaternary alluvial deposits and the Tertiary
sandstones and conglomerates of Haddat Ash Sham and Ash Shumaysi
Formations.
In As Suqah (the study area), Sharaf (2010) carried out a detailed
study on the geological and geophysical exploration for groundwater
based on two drilled test wells and integrated electro-resistivity (VES),
seismic and magnetic geophysical tools and he reached for the following
conclusions: 1) Groundwater occurs mainly in two water-bearing
horizons, the alluvial deposits and within the clastic sedimentary rocks of
Haddat Ash Sham and Ash Shumaysi formations. The shallow zone is
characterized with a saturated thickness of 3- 20 m and water is found
under confined to semi-confined conditions, 2) Water levels were
encountered at depths varying from 3-16m in the alluvial wadi deposits,
and from 18-62 m in the sedimentary succession, 3) Groundwater
movement is towards the west and northwest, following in general the
surface drainage system, and 4) Hydraulic gradient varies greatly from
one point to another depending on the pumping rates and cross-sectional
area of the aquifer in addition to its transmissivity.
Hydrochemical Study
The pump-tested wells, the large and small diameter wells as well
as the test well of the study area are shown in Fig. 2. In the present study,
16 water samples have been collected from wells scattered all over the
study area (Fig. 2), all samples have been fully analyzed for major,
secondary and trace constituents. The Major constituents are: Ca+2, Mg+2,
Na+, K+, HCO-3, CO-23, SO-24 and Cl-. Beside the determination of pH,
E.C., T.D.S and total hardness (Table 1). The secondary and trace
constituents are: NO3, Fe, Mn, Pb, Si, Al and B, the results are shown in
Table (2).
Classification of Water Types
Durov diagrams
The expanded Durov diagram is used to classify the water facies of
the study area. In As Suqah area, the most important facies is No. 9 and
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Mohamed Amin M. Sharaf
followed by facies No. 8 (Fig. 3). In facies No. 9 Cl- and Na+ ions are
dominant. This frequently indicates end- point waters for simple
dissolution or mixing (Old brackish water). Facies No. 8 may be related
to reverse ion exchange of Na+- Cl- waters (Fig. 3). It is worth
mentioning that all the samples of the study area do not belong to facies
No.1 or facies No. 2. This shows that there is no indication of adequate
recharge water. Partial ion exchange process is absent. In short, the main
hydrochemical processes from the upstream to the downstream of the
study area are simple dissolution, reverse ion exchange, ion-exchange
and mixing.
Fig. 3. Durov representation of major ions hydrochemistry of As Suqah area.
Trilinear Diagram
Major cations and anions such as Ca, Mg, Na, K, HCO3 and Cl in
meq/l were plotted in Piper’s trilinear diagram of Piper (1944) to evaluate
the hydrochemistry of surface water of As Suqah area (Fig. 4). The
following water types are indicated: Two groundwater types were
identified in the As Suqah sub-area: Na-Mg-Ca- Cl-SO4 and Na-Ca-MgCl water types. Sodium adsorption ratio has a mean value of 14.39. The
Hydrochemistry of the Groundwater Aquifer in As Suqah Area, Makkah District…
191
exchangeable sodium ratio has a mean value of 0.456 and a maximum
value of 1.706. The average magnesium hazard was found to be about
49.97. The groundwater in As Suqah area was slightly supersaturated
with respect to calcite and supersaturated with respect to dolomite. The
mean saturation indices for these species are 1.21 and 2.60 respectively.
Fig. 4. Distribution of water samples according to Piper diagram.
Areal Variations of Elements
Hydrochemical variation of elements included well location,
electrical conductivity, TDS, calcium, pH, potassium, magnesium,
sodium, chloride, bicarbonates, carbonates, sulphates, nitrates,
manganese, iron, silicates, fluoride, boron, aluminum, lead, total hardness
as CaCO3 and water level are illustrated in the data of Table 1, 2 and Fig.
5, 6, 7, 8 and 9.
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Mohamed Amin M. Sharaf
Table 1. Data of chemical analyses for major constituents of As Suqah water wells.
Well
No.
Absolute pH
Major Cations (ppm)
Major Anions (ppm)
Total
E.C. T.D.S
depth to at
Depth
ms/cm (ppm)
-2
-2
+2
+2
+
+
Water 25C
Ca
Mg
Na
K HCO3 CO3 SO4
Cl
1
S-1
39.54 21.71042
7.6
20.1
16190 1190 663.9 2780
2
S-4
39.53 21.74361
8.1
8.67
6872
468.9 389.1 1115 4.9 213.8 24.74 1572 2370.44 2767.74
3
S-5
39.53 21.74642
8.1
9.62
7968
589.2 462.1 1105 4.8 188.6 24.74 2016 2474.25 3367.48
4
S-6
39.52 21.73906
8.1
4.63
3438
168.3 132.5
5
S-8
39.51 21.74497
8
9.31
7416
6
S-9
39.51 21.74997
8.1
10.62
8548
613.2 381.8 1545 4.9 179.8 24.74 2045 2933.33 3098.51
7
S -14
39.51 21.74372
8.3
7.34
5928
428.9 250.5 1155 3.8 227.6 12.37 1842 1782.15 2099.2
8
S -15
39.51 21.74522
8.1
12.17
10002 841.7 445.1 1665 5.6 201.2 24.74 2286 3547.01 3928.95
9
S -16
39.47 21.76317
8
21.4
17274 1463 595.8 3290 7.1 188.6 24.74 2376 7491.97 6100.24
10
S -17
39.5
8
21.9
17954 1403 778.2 3146 6.2 207.5 37.11 2495 7613.09 6697.78
11
S -18
39.51 21.76347
7.9
19.29
13900 961.9 705.3 2590 3.8 197.1 31.31 2055 5982.39 5296.45
12
S -19
39.5
21.76817
7.7
27
20178 1471 890.1 3725 3.8 148.1 31.31 2595 8978.58 7326.8
13
S -21
39.49 21.76503
7.7
34.3
25342 1924 858.5 5302 1.8 164.1 14.45 2330 12193.5 8329.45
14
S -22
39.49 21.77681
7.7
34.3
25778 2124 729.6 5295
15
S -24
39.51 21.76753
8
7.5
5258
311.4
16
S -25
39.49 21.77217
8
12.41
8924
663.2 432.9 1450 3.8 220.4 14.45 1663 3290.31 3433.19
No.
21.76397
481
757
9
3
294.3
0
T.Hard
Ca CO3
1897 6747.96 5698.1
282.9 12.37 892.4 1029.5
964.26
413.4 1186 3.9 198.7 37.11 1699 2474.25 2897.5
214
4
123.7 31.31 2219 12263.9 8301.96
1050 2.4 197.1 31.31 1359 1609.97 1656.03
Table 2. Data of chemical analyses for minor constituents of As Suqah water wells.
Serial
No.
Well No.
1
2
3
4
5
6
7
8
9
10
11
12
13
14
15
16
S-1
S-4
S-5
S-6
S-8
S-9
S -14
S -15
S -16
S -17
S -18
S -19
S -21
S -22
S -24
S -25
Trace Elements (ppm)
NO3
Fe
Mn
Pb
Si
Al
B
F
577.66
456.14
453.75
84.59
487.54
358.8
387.9
228.38
224.35
370.05
343.33
376.55
305.67
203.78
182.74
265.8
1.263
0.731
0.603
0.224
2.513
4.827
3.038
0.128
0.026
2.032
0.47
0.626
0.42
0.375
0.033
0.056
0.011
0.003
0.016
0.003
0.006
0.01
0.016
0.025
0.015
0.019
0.052
0.267
0.403
0.407
0.01
0.025
0.225
0.138
0.15
0.02
0.145
0.138
0.076
0.161
0.237
0.216
0.136
0.179
0.193
0.191
0.187
0.051
0.407
0.351
0.357
0.431
0.163
0.158
0.386
0.349
0.468
0.48
4.25
3.27
2.88
2.95
3.32
3.31
0.138
0.055
0.27
0.147
0.008
0.157
0.549
0.259
0.288
0.238
0.052
0.096
0.055
0.039
0.052
0.072
2.34
0.71
0.68
0.67
0.94
0.94
0.73
1.1
2.15
2
0.725
0.92
0.88
0.891
0.691
0.571
0.68
0.7
0.74
0.68
0.7
0.8
0.75
0.78
0.81
0.78
1.4
1
1.43
1.23
1.4
1.2
Hydrochemistry of the Groundwater Aquifer in As Suqah Area, Makkah District…
193
Fig. 5. X-Y relationships between HCO3 vs Ca; SO4 vs, Ca; HCO3 vs. Ca + Mg and Cl vs,
Na in As Suqah water.
Fig. 6. Variations in Electric Conductivity (E.C.), T.D.S., HCO3 and Cl variation in As
Suqah area.
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Mohamed Amin M. Sharaf
Fig. 7. Ca, Mg, Na and K variation in As Suqah area.
SE
700
NW
A
SE
6
NW
NO3/ppm
600
Fe/ppm
500
400
300
200
100
4
3
2
1
0
0
1
2
3
4
5
6
7
8
0
9 10 11 12 13 14 15 16 17
0
1
2
3
4
5
6
0.45
SE
0.4
7
8
9 10 11 12 13 14 15 16 17
Well No.
Well No.
NW
C
SE
0.25
NW
D
0.2
0.35
Pb/ppm
Mn/ppm
B
5
0.3
0.25
0.2
0.15
0.15
0.1
0.05
0.1
0.05
0
0
0
1
2
3
4
5
6
7
8
Well No.
9 10 11 12 13 14 15 16 17
0
1
2
3
4
5
6
7
8
9 10 11 12 13 14 15 16 17
Well No.
Fig. 8. Variation of NO3, Fe, Mn and Pb in As Suqah water wells.
Hydrochemistry of the Groundwater Aquifer in As Suqah Area, Makkah District…
195
Fig. 9. Variation of Si, Al, B and F in As Suqah water wells.
Groundwater Level Variation
The groundwater in the study area occurs within two main waterbearing units: the alluvium of the Wadi system under unconfined
conditions and within the clastic layers of the Cretaceous sedimentary
succession. The general groundwater flow in the aquifer system follows
the surface drainage towards the northwest to Usfan city; it takes place
from areas of high potential to areas of low potential (Fig. 2). Both the
elevation and pressure heads define the direction of groundwater flow
towards northwest. The values of the depth to water in Table 1 represent
the absolute depth to the water while the values of the contour lines
showing the flow direction in Fig. 2 represents the water depth above sea
level (a. s. l.).
E. C. Variation
Electro conductivity, or specific conductance, is a measure of the
ionic content of a water sample and is commonly recorded
potentiometrically by means of two platinized electrodes and a
Wheatstone bridge. Freshly-distilled water has a conductivity of 0.5-2 uS
196
Mohamed Amin M. Sharaf
cm-1. Most natural waters fall in the range of 50-500 uS cm-l range
whereas highly mineralized waters have conductivity values in excess of
1000 uS cm-l (Pagenkopf 1978). An empirical relationship exists
between specific conductance and total dissolved solids. Multiplying the
conductivity value by a factor of 0.5 to 1.3 can provide a reasonable
estimate of the TDS content (Pagenkopf 1978). However, due to ion
pairing in solutions of high ionic strength, the relationship may not be
applicable in saline waters.
The electrical conductivity of the water samples collected from the
wells of As Suqah area varies from 7.5 to 34.3 ms/cm (Table 1). The
wells of the southeastern part of the study area (Fig. 2) are generally of
low E.C. values (4-12) while those of the central parts are generally of
moderate E.C. values (average 12-21). The wells of the extreme
northwestern part are of high E. C. values (12-34). This indicates the
variation in the water salinities from the southeastern, central and
northwestern wells of the study area (Fig. 6A).
Total Hardness
The total hardness of the groundwater samples collected from the
study area varies from 964.26 to 8329.5 mg/l (Table 1). It is observed
that, there is a strong correlation between the total hardness and the
electro conductivity (E.C./ms/sc). The SO4 varies from 892.35 (in well
No. S- 6) to up to 2594.7 ppm (in well No. S-19).
The total dissolved salts (TDS) vary from 3438 ppm (in well no. S6, Table 1) to up to 25778 (well No. S-22, Table 1). Figure 6B shows a
characteristic low TDS values in the bore holes of the southeastern part
of the study area and high values in the northwestern part of the study
area (TDS values of Table 1).
There is a negative relation between HCO3 and Ca which indicates
the slow dissolution of calcite (Fig. 5A). On the other hand, there is a
positive relation between SO4 and Ca which indicates the dissolution of
gypsum (Fig. 5B). Similar negative relation is present between HCO3 and
Ca + Mg which is the negligible contamination (addition) of these
elements by dolomite dissolution (Fig. 5C). There is a strong positive
relation between Na and Cl (Fig. 5D) which indicates dissolution of
halite within the ground water-bearing horizons The chlorine content
varies between 1029.5 (well No. S-6, Table 1) to up to 12264 (well No.
Hydrochemistry of the Groundwater Aquifer in As Suqah Area, Makkah District…
197
5-22, Table 1). It is also observed that, there is an increase in the Cl and
Na content from the bore holes of the southeastern part to these of the
northwestern part of the study area (Fig. 6D). The electroconductivity
shows a general increase towards the northwestern part of the study area
(Fig. 6A). The bore holes of the southeastern parts are of low E.C. values
in contrast to those in the north-western part. The same relation and
variation trend is observed within the values of T.D.S. (Fig. 6B).
pH and Alkalinity
The pH of water is a master variable (Stumm and Morgan 1981)
influencing virtually all physical, chemical and biological processes. It is
the primary driving variable for weathering and therefore controls the
concentration of most major ions in natural waters. The pH of water also
affects transformation reactions and the availability of nutrients and
metals. Hydrogen ion concentration is controlled by various buffer
systems. Although carbonates provide the primary buffering system in
water, other species including naturally occurring organic anions,
hydroxides, sulphides, silicates and phosphates may be important in
regulating pH if they are present in significant concentrations.
The pH values of As Suqah groundwater ranges from 7.6 to 8.3.
The groundwater in the study area is slightly alkaline to alkaline. The
HCO3 shows a characteristic northwestern decreases in its values where
the bore holes of the southeastern part of the study area are of high HCO3
values while those of the northwestern parts are of low HCO3 values (Fig.
6C).
Major Ions Variations
The variation of the major cations and anions in the study area
varies spatially from place to place (Table 2, Fig. 6C, D, 7A, B, C, D).
The Cl content shows a reverse relation when compared with the HCO3
where the bore holes of the southeastern part are of low Cl values while
those of the northwestern parts are of high values (Fig. 6D).
Ca shows an upward increase towards the northwest direction (Fig.
7A). The bore holes of the southeastern parts of the study area are of low
Ca content when compared with those of the northwestern part (Fig. 7A).
Mg nearly shows the same trends of Ca values where the bore holes
of the southeastern parts are of low Mg values when compared with those
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Mohamed Amin M. Sharaf
of the northwestern parts (Fig. 7B). Na also the same trend of Ca and Mg
where the bore holes of the southeastern part of the study area are of low
Na content when compared with those of the northwestern part of the
study area (Fig. 7C). K shows a reverse trend where the bore holes of the
southeastern part are of high K values when compared with those of the
northwestern part of the study area (Fig. 7D).
Trace Elements Variations
The trace elements chemical analyses of NO3, Fe, Mn, Pb, Si, Al, B
and F (Fig. 8 and 9). NO3 and Fe show a northwest decreases where the
bore holes of the southeastern parts of the study area are of high values
when compared with those of the northwestern parts (Fig. 8 A and B).
Mn analyses (Fig. 8C) shows fluctuations but generally, the bore
holes of the southeastern part of the study area are of low Mn content
while bore holes No. S-19, 5-21, 5-22 are of high Mn content. Pb shows
a fluctuation of its values but bore holes no. 5-1, 5-16 and 5-17 are of
high Pb values. Si concentration shows two main domains where the
boreholes of southeastern part are of low Si content while those of the
northwestern part are of high Si content (Fig. 9A).
The Al content shows somehow fluctuation but borehole no. 5-14 is
of high Al content (Fig. 9B). Boron shows some sort of fluctuation but
the boreholes no. 5-1, 5-15 and 5-16 are of high boron content (Fig. 9C).
Fluorine shows an increase from the southeast to the northwest (Fig. 9D).
Discussion and Conclusions
During the groundwater exploration in the area north and northeast
of Jeddah, Italconsult (1967) drilled three boreholes in the study area and
found the bed rocks at depth of 36m. Al Khatib (1977) argued that the
main aquifer in the area consists of the alluvial deposits while the
Shumaysi sandstone was considered an aquifuge. Kotb et al. (1988) gave
a general overall view of the hydrochemical characteristics of
groundwater in the Usfan Basin and they indicated that the groundwater
therein is of Cl - Na type. Hussein and Bazuhair (1992) studied the
groundwater condition in the Haddat Ash Sham-Al Bayada area and
concluded that, the groundwater within the Cretaceous-Tertiary members
moves under a hydraulic gradient of 6.4x10-4 an average transmissivity
of 180m2 /day and a maximum coefficient of storage of l.lxl0-3.
Hydrochemistry of the Groundwater Aquifer in As Suqah Area, Makkah District…
199
In As suqah area the groundwater shows relatively high
concentrations in their overall mineral contents. This applies as well to
the EC, TDS, and total hardness as CaCO3 and to the ions. Calcium
shows relatively higher values. Magnesium and sodium concentrations
are high as well. Bicarbonate and chloride concentrations are
exceptionally high.
Two groundwater types were identified in the As Suqah area: Na –
Mg – Ca – Cl - SO4 and Na – Ca – Mg - Cl water types. Sodium
adsorption ratio has a mean value of 14.39. The exchangeable sodium
ratio has a mean value of 0.456 and a maximum value of 1.706. The
average magnesium hazard was found to be about 49.97. The
groundwater in As Suqah area was slightly supersaturated with respect to
calcite and supersaturated with respect to dolomite. The mean saturation
indices for these species are 1.21 and 2.60 respectively.
Under the assumptions that present abstraction rates continues as it
is now, and in the absence of flood waters, the alluvial deposits are liable
to be dewatered in the coming five years and wells are possibly to
become dry in future years. The sedimentary layers may continue to
supply water with continuous lowering in their overall head. Under such
conditions and due to the prevailing aridity environment in the study area,
it is necessary to monitor the groundwater levels in the aquifer system.
This monitoring program includes implementation of groundwater level
recording instruments at the inlets and outlets of each of the investigated
sub areas.
According to the hydrochemical model set up for the study area,
the main hyrdochemical processes controlling the groundwater quality
are recharge, ion-exchange and mineral dissolution. Recharge and
evaporation are synonymous under the prevailing arid conditions. The
water quality of the sedimentary succession is generally characterized by
relatively high salinities and may be used for domestic purposes if
adequately treated.
Acknowledgement
The author would like to thank the staff members of the project no.
AT-16-20 funded by the King Abdulaziz City for Science and
Technology (KACST). The author also gives deep thanks for Prof.
Abdullah Sabtan for reading and revising the manuscript.
200
Mohamed Amin M. Sharaf
References
Al-Khatib, E. (1977): Hydrogeology of Usfan district, Saudi Arabia. M.Sc. Thesis, I.A.G., King
Abdulaziz University, Jeddah.
Al-Shanti, A.M.S. (1966): “Oolotic iron ore deposits in Wadi Fatima between Jeddah and
Mecca, Saudi Arabia.” Saudi Arabian directorate General of Mineral
Resources,
Bulletin 2, 51p.
Brown, G. F., Jackson, R.O., Bogue, R.G., and MacLean, W.H. (1963): Geology of the
Southern Hijaz quadrangle, Kingdom of Saudi Arabia: Saudi Arabian Directorate
General of Mineral Resources, Miscellaneous Geologic Investigations MAP I – 210 A,
1 : 500,000 scale.
Hussien, M. T., A. S. Bazuhair and M. S. Al-Yamani (1993) Ground water availability in the
Khulais Plain, Western Saudi Arabia. “ ,Hydro – Sci Jour., 38 ( 3 ): 203 - 213.
Italconsult, (1967) Water Supply Surveys for Jeddah-Mecca-Taif Area. First interim report,
Ministry of Agriculture and Water, Riyadh.
Karpoff, R. (1958) Esquisse geologiques de I,Arabie Saoudite : Bulletin Societe Geologique de
France, 6 ser. VIIm, p. 653 – 696.
Kotb, H., S. M. Saidi and Hakim (1988) Hydrochemical characteristics of groundwater In the
Usfan basin, Saudi Arabia. Jour. King Abdulaziz Univ. : Earth Sci., 1: 113 – 132.
Moore, T. A., and Al-Rehaili, M. H. (1989) Geologic map of the Makkah quaderangle, Sheet
21D, Kingdom of Saudi Arabia. “, Saudi Arabian Deputy for Mineral
Resources,
Geologic map GM-107 C, scale 1: 250,000 with text 62 p., Jeddah, Saudi Arabia.
Pagenkopf, G. K. (1978) Introduction to Natural Water Chemistry. Marcel Dekker, New York.
272pp.
Piper, A. M. (1944): A graphic procedure in the geochemical interpretation of water analyses.
Sharaf, M. A. M. (2009b) Geophysical and Hydrochemical Studies on the Groundwater Aquifer
in Ash Shamiyah Area, Makkah District, Western Saudi Arabia. Journal of Environmental
Hydrology, paper 13, 18: 2010.
Sharaf, M. A. M. (2010) Geological and Geophysical Exploration of the Groundwater Aquifers
of As Suqah Area, Makkah District, Western Arabian Shield (submitted to the Arabian
Journal of Geosciences).
Sharaf, M. A. M. (2009a) Hydrogeology of Haddat Ash Sham area: Geophysical and
hydrochemical Constrains. In press in the proceeding of the 5th international Conference
of the Geology of the Tethys, Cairo Univ.
Spincer, C.H., and Vincent, P. L. (1984) Bentonite resource potential and geology of the
Cenozoic sediments, Jeddah region: Saudi Arabian Deputy Ministry for Mineral
Resources, Open-File Report BRGM-O-F-02-34, 34 p.
Stumm, W. and Morgan, J.J. (1981) Aquatic Chemistry, 2nd edition. John Wiley & Sons, New
York, 780 pp.
Hydrochemistry of the Groundwater Aquifer in As Suqah Area, Makkah District…
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