




































Asian Review of Environmental 

and Earth Sciences 
ISSN: 2313-8173 
Vol. 2, No. 1, 9-22, 2015 

http://www.asianonlinejournals.com/index.php/AREES 

 
 

 

* Corresponding Author 

 

 

9 

 

Groundwater Vulnerability Assessment Using Different 

Overlay and Index Methods for Quaternary Aquifer of 

Wadi El-Tumilat, East Delta, Egypt  
 

GAD, M. I.
1*

 --- El-Kammar, M. M.
2
 --- Ismail, H. M. G.

3
 

 
1,3

Hydrology Division, Desert Research Center, El-Mataryah, Cairo, Egypt 
2 
Geology Department, Faculty of Science, Cairo University, Cairo, Egypt 

 

Abstract 
 

 

 

 

 

 

 

 

 

 

 

 

 
 

 

 

 

 

 
 
 

 
This work is licensed under a Creative Commons Attribution 3.0 License 

Asian Online Journal Publishing Group 

 

Contents 
1. Introduction ............................................................................................................................................................................... 10 

2. Materials and Methods ............................................................................................................................................................. 12 

3. Results and Discussion .............................................................................................................................................................. 16 

4. Conclusion and Recommendations .......................................................................................................................................... 21 

References ...................................................................................................................................................................................... 21 

 
 

 

 

 

 

 

 

 

 

 

 

 

Contamination from rapid urban development, industrialization and agricultural sources increasingly 

threatens the groundwater resource in the shallow phreatic Quaternary Aquifer of the Wadi El-Tumilat 

(QAWT), East Delta, Egypt. In this paper, fourteen environmental sensitive heavy metals and two 

minor elements (PO4
--
 and NO3

-
) were checked by the chemical analysis of both 25 surface and 

groundwater samples at 2006. An assessment of the QAWT intrinsic vulnerability was carried out in 

this paper based on GOD, PRAST and DRASTIC methods. The calculated vulnerability indexes 

resulted from the three methods showed great differences due to the different criterions used. 

Moreover, a weight modification was assumed to adequate the arid zone. The obtained QAWT 

vulnerability maps showed the high extension of medium vulnerability zones. The high vulnerability 

zones occupied about 35% and 31% from applying PRAST and DRASTIC methods respectively. The 

high vulnerability in these areas was mainly related to the low values of depth to water (less than 10 

m), the high permeability of the soils (9 m/day) and the high permeability of the vadose zone materials 

(more than 11 m/day). The most suitable areas for new reclamation activity were located in the 

southern boundary of Wadi El Tumilat especially the strip south El Mahsama drain by 5 km. These 

resulted maps may provide planners with tools for a preliminary selection of priority areas for different 

forms of sustainable development. 
 

Keywords: Hydrogeology, Vulnerability assessment, Wadi El-Tumilat, GOD, PRAST, DRASTIC methods. 

http://creativecommons.org/licenses/by/3.0/


Asian Review of Environmental and Earth Sciences, 2015, 2(1): 9-22 

 

 

 

 

10 

 

1. Introduction 
The term “vulnerability of groundwater to contamination” was first used by Margat [1]. Vowinkel, et al. [2] 

defined vulnerability as sensitivity plus intensity, where intensity is a measure of the source of contamination. 

Intrinsic vulnerability is controlled exclusively by geological structure and hydrogeological conditions, while 

specific vulnerability includes, besides the former parameters, consideration of the type of a contaminant and the 

character of a contamination source [3].  

In this paper, due to the groundwater contamination in some plots of the Quaternary Aquifer of Wadi El Tumilat 

(QAWT), a trial to assess the intrinsic groundwater vulnerability was carried out applying three different methods to 

delineate the less vulnerable areas suitable for new reclamation activities. 
 

1.1. Location of the Studied Area 
      The QAWT lies between latitudes 30

0
25

\
 and 30

0
35

\ 
N and longitude 31

0
45

\
 and 32

0
20

\ 
E. It is bounded on the 

NW by Bahr El Baqar  Drain, on the west by Wadi El Watan, on the east by Suez Canal and its attached lakes and on 

the south by Cairo-Shubrawit Ridges with total area of magnitude 1500 km
2
 (Figu5r4e 1). It is characterized by 

desert climate, with arid, hot and rainless summer, and mild winter with low precipitation (22-40 mm/year). The 

evaporation rate is very high (6-12 mm/day).  

 

 
Figure-1. Location map of the infiltration tests, pumping tests and monitored wells in the QAWT 

 

1.2. Geomorphological Aspects 
In the literatures [4-7], Wadi El Tumilat represents a part of the eastern gravelly slopes fringing the Nile Delta 

and bears the structural affinity to the Syrian arc system. The northern limit is defined by the well known buried Nile 

branch "Pelusaic" which extends in NE-SW direction and is represented by a semi flat plain called El Salhia plain 

(Figure 2). El Timsah and Bitter lakes represent the remnants of an old structural and topographic low land area 

called Isthmus Stretch along the eastern boundaries. The southern boundary of Wadi El-Tumilat is represented by 

Umm Gidam gravelly sand sheets in the form of low lying slopes. The southern boundary is determined by a series 

of structural ridges extend in an E-W trend. The foreland slopes of the southern structural ridges are dissected by few 

morphotectonic main drainage lines, mostly of NW-SE trend with numerous dendritic tributaries (Figure 2).  

 

1.3. Geological Aspects 
The study area is built up of sedimentary rocks belonging to both Tertiary and Quaternary ages (Figure 2) with 

thickness more than 1500 m (Table 1) [5, 7-13]. Tertiary rocks are exposed south of the study area and represented 

by Eocene, Oligocene, Miocene and Pliocene units (Figure 2). Middle and Upper Eocene rocks are formed of 

shallow marine fossiliferous chalky, dolomitic sandy and marlylimestones. Oligocene rocks are exposed in the area 

between Cairo and Suez at Gebel Umm El Ragm and Gebel Umm Qamar. They are formed of continental sands and 

gravels as well as volcanic basalts with variable thickness ranging from 45m at Gebel Iwiebid to 100m at Gebel El 

Nassuri area. Miocene rocks are composed of sandy limestone and sandy marls of shallow marine origin and are 

represented by El Shatt Formation and El Hommath Formation. Pliocene rocks are exposed in the area northwest of 

Cairo along the margins of the Heliopolis basin. Quaternary deposits have a wide distribution represented by old 

deltaic deposits which are composed of fluviatile coarse quartz sand, cherty flinty pebbles and igneous fragments 

with few occasional fossil wood remains and young Aeolian deposits. The subsurface sedimentary succession is also 

built of Tertiary and Quaternary rocks, Tertiary rocks include Miocene sandy limestone water bearing Formation and 

Pliocene impermeable shale and clay beds. The regional structure of the study area is homoclinal having a low 

northward dip. This dip controls the thickness of some aquifers. It forms the foreland side of the ancient 

Mediterranean geosyncline. Normal faults are the most conspicuous structural elements affecting the landscape in 

this area, and are dominantly represented by NE-SW trend with downthrown side toward SE and NW and NW-SE 

trend with downthrown side toward NE direction. The vertical displacement along these faults ranges from few 

meters to hundred meters which led to an increase of the thickness of the Quaternary water bearing Formation by due 

3 m/km towards northeast direction [13].  

 



Asian Review of Environmental and Earth Sciences, 2015, 2(1): 9-22 

 

 

 

 

11 

 

1.4. Hydrogeological Conditions 
The water bearing formations in the Wadi El-Tumilat area comprise the QAWT, occupies the shallow zone and 

the Miocene aquifer dominating the deeper part [14]. The QAWT represents the main aquifer in the region and 

composed of fluviatile and fluviomarine graded sand and gravel with clay intercalations of limited extension (Figure 

3). The basal portion of this aquifer is formed of dark plastic clay. The Quaternary deposits rest directly with 

unconformity surface on the Miocene hard limestone as recognized in the north and south of Wadi El-Tumilat. Its 

total thickness increases generally from south to north. It is mainly recharged by Nile water from the river branches 

and canals. The Miocene aquifer is dominated by clasticfacies in the southern part of the study area and overlain by 

about 200 m of Quaternary deposits [15]. In Belbies-El Tell El Kabier-El Salhiyafluviatile plain, the Miocene 

sediments are composed of alternating sandy limestone and clay lenses, loose quartz sand and marl. The aquifer is 

more clayey towards east. The cross-section along the QAWT monitoring well line (Figure 3) shows the general 

characteristics of the mode of groundwater occurrences. It is clear that, the clay intercalations are generally existed 

towards south and north. In the narrow strip adjacent to the Ismailia canal, the depth to the groundwater is highly 

affected by the surface water running in the canal.  

 

Port   Said

Mediterranean    Sea

El-Ismailia
Q Q

Q Q Q

Cairo
Tv

Tv

Tv

Te
Te

Te

To
To

To

To

To

To

Te

Tn
Tn

Tn

TnTn

TnTo

To

Tn

0              20           40             60 km

Scale

31   00 32   00

31
30

31
00

30
30

30
00

Quaternary

Surfacial deposits
Sand dunes
Sabkhas

Tertiary
Eocene
Undifferentiated Neogene
Extrusive rocks
Oligocene
Undifferentiated Cretaceous

Q Te
Tn

To
Tv

K

K

To

Legend

El Manzala  

    Lake
Port   Said

Mediterranean    Sea

BitterLake

El-Ismailia

Cairo

0              20           40             60 km

Scale

31   00 32   00

31
30

31
00

30
30

30
00

Legend

El Ankabia-Iweibid structural plain
Bitter lakes and Isthmus plain
Belbies-El Tell El Kabier-El Salhiya plains
              (Old deltaic plains)
Wadi El Tumilat depression
Desert dry drainage lines

Suez
Gulf 

Suez
Gulf 

 
Figure-2. Geomorphologic map (left map) and the compiled geological map after geological map of Egypt, 1971(right map) of the East Delta 

 
Table-1. Sedimentary succession in the study area 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 
 

Figure-3. The cross-section along the QAWT monitoring well line in NE-SW direction showing different water bearing formations (after Gad 

[13])  

 

The QAWT and the Miocene aquifers are hydraulically connected but in some places, they are separated by a 

semi-permeable layer which is highly controlled by deep-seated faults. These faults cause the saline groundwater of 

Miocene aquifer to move upward along the fault planes and mixed with the groundwater of the QAWT [13]. The 

groundwater in the QAWT ranges from unconfined in the western part to semi-confined in the eastern part due to the 

presence of capped and underlying clay beds.  

The groundwater flow in the QAWT is directed mainly from south to north in the southern part (Miocene 

aquifer) with very low hydraulic gradient (≈ 2x10
-4

). An opposite direction is recorded from north to south in the area 

lying south of Ismailia canal (hydraulic gradient ≈ 4x 10
-4

). Along the main flood plain and down stream of Wadi El 

Age Lithology Approximate Thickness (m) 

Eocene  Chalky limestone, sand and clay 432 
Oligocene Sand, gravel and basalt 264 
Miocene  Sandy limestone and clay  224 
Pliocene  Marine clay 192 
Pleistocene Fine sand and gravelly calcareous sand 352 
Recent Aoelian sand and silt 40 

W.21
W.22

W.766 E.5
W.28

W.25

W.33

W.34 W.36

Miocene aquifer

Quaternary aquifer

El
 M

an
ai

ef
 c

an
al

El
 M

ah
sa

m
a 

dr
ai

n

Is
m

ai
lia

 c
an

al

W.24

-200

-160
-140

-120
-100

-80
-60
-40

100

80

60
40

0
20

-20

m

Sea 
level

A A

NESW

Fig. (3.10): Hydrogeological cross section A-A` extending in NE-SW direction (Modified after Gad, 1995).

Water
Table

EL Karnak Lake

Sarabium Lake

Ismailia   Canal

El Mahsama Drain El Mahsama Lake

EL Temsah Lake

0 5 10 km

Scale

30
27

30
30

30
33

31  45 32  00 32  15

A

A

Sand

Sand and gravel

Clay

Legend

Sea level

Water Table



Asian Review of Environmental and Earth Sciences, 2015, 2(1): 9-22 

 

 

 

 

12 

 

El Ismailia Canal

El Mahsama drain

El Mahsama Lake

0 5 10 km

Scale

30
30

30
27

30
33

32  00 32  7.5 32  15

Unexposed area.

Area of aquifer depletion
   (negative values area)

Area of neutral quifer
    (zero value area)

Area of aquifer accretion 
     (positive values area)

Legend

Fig. (3.23): Resultant water table map at the study area (December 1992 - December 2005).

 

Tumilat, an opposite direction is recorded from north to south (local flow) in the area lying south of Ismailia canal 

(the hydraulic gradient is about 8 x 10
-4

). The main groundwater recharging source is the Ismailia canal while Suez 

and El-Manaief fresh water canals are additional sources. In the Western and eastern parts of the QAWT, a general 

trend of discharge in W-E direction is observed due to the intensive pumping of groundwater for reclamation projects 

at Wadi El-Mullak, El-Manaief and Sarabium occupying the central part (Figure 4, Ismail [16]). 

 

 

 

 

 

 

 

 

 

 

 

 

 
Figure-4. Water table map at Dec. 2005 (left map) and water table fluctuation map during 1992-2005 (right map, Ismail [16]) of the QAWT 

 

The constructed water table fluctuation map over the period Dec. 1992- Dec. 2005 reflects the wide change in the 

water table values during this interval (Figure 4). This reflects the need for intrinsic rather than specific vulnerability 

assessment. On the contrary, the uncultivated flat areas in the central flood plain of the QAWT reveal no changes in 

the groundwater storage. The most deteriorated areas are those lying in the northern lowlands of the QAWT while 

the least deteriorated areas are located in the southeastern part of it. The main irrigation canals network (Suez fresh 

water canal and El Manaief canal), the main drainage network (El Mahsama drain, El Mahsamalake, El Karnak lake, 

El Manaief lake and Sarabium lake) play a significant role in the groundwater pollution in the QAWT based on its 

vulnerability.   

 

2. Materials and Methods 
The materials used in this paper are collected through carrying out four field trips in QAWT area during the 

period 2005-08 with the team work of the Desert Research Center. These materials include collection of archival 

well data (discharge, distribution, operating systems,…etc.) beside carrying out both pumping and infiltration tests 

representing the different soils in the QAWT. The four infiltration test are performed using the double ring method, 

as described by Black [17] and the field data are analyzed according to Philip [18] beside archival data of six tests 

carried out by Gad [13] and two tests by Afify [19] . Complete chemical analyses of both 26 surface water and 28 

selected groundwater samples are performed in the Central Lab of the Desert Research Center during the year 2005-

07 according to the methods adopted by the U.S Geological Survey, Rainwater and Thatcher [20]. In addition, the 

environmental sensitive heavy metals and minor elements including Al, B, Cd, Co, Cr, Cu, Fe, Mn, Mo, Ni, Pb, Sr, 

V, Zn, PO4 and NO3 are evaluated to clarify the industrial and agricultural pollution. Moreover, the following maps 

are prepared: 

 

2.1. Depth to Water Map  
      Depth to water parameter represents the depth of the water table from the topographic surface and gives an idea 

of the minimum distance that a pollutant has to travel to reach the saturated zone. Depth to water was computed 

based on the field data during 2005. The recorded depth to water in the selected wells was used in constructing the 

depth to water map. 

 

2.2. Net Recharge Map 
      The weighted net recharge depends mainly on the constructed isohyetal map of the QAWT based on the 

meteorological data of the period 1936-993. The computed net recharge values in the selected points are equal to the 

difference between precipitation plus return flow after irrigation minus the evapotranspiration. Applying the number 

of points for each value (Table 2), the weighted net recharge map is constructed.  

 
Table-2. Assessment of net recharge [21] 

Net recharge (mm/year) No. of points 

0 – 50 1 

50 – 100 3 

100 – 180 6 

180 – 250 8 

>250 9 

 

2.3. Aquifer Media Map 
      Aquifer media information is depicted from the three major maps (the diffusivity, lithology cover and aquifer 

thickness maps). The diffusivity values were resulted from dividing the transmissivity T and the storativity S (or 

specific yield Sy in case of unconfined aquifer). The Transmissivity T and the storativity S is estimated from the 

El Ismailia Canal

El Mahsama drain

El Mahsama Lake

0 5 10 km

Scale

30
30

30
27

30
33

32  00 32  7.5 32  15

Fig. (10): Water table contour map of the selected groundwater samples (December, 2005).



Asian Review of Environmental and Earth Sciences, 2015, 2(1): 9-22 

 

 

 

 

13 

 

carried out five pumping tests and four recovery tests in addition to other eight tests from previous work. Theis [22] 

type curve method, Cooper and Jacob [23] straight line method  and Theis recovery method are used in the analysis 

of these data. The weighted diffusivity map has been prepared by multiplying the diffusivity value (T/S) for every 

borehole by its aquifer saturated thickness and the output data were organized in GIS format through which the 

successive weighed diffusivity at each well can be determined. Repeating the same steps for the other two 

parameters, the weighted aquifer media map is obtained.  

 

2.4. Soil Media Map 
The soil media map is very important because it determines the overall protective effectiveness of the soil and 

rock covers above the shallow aquifers. It reflects the main properties of the soil zone as effective field capacity 

(eFC), cation exchange capacity (CEC) and electric conductivity of the soil (EC). The eFC, CEC and EC analyses 

resulted from the deep soil profile of the QAWT sited in Shata [24] (Table 3) is used in developing the soil media 

map. 

 
Table-3. The available data of soil parameters of the different soil profiles in the study area (after Shata [24]) 

Soil profile N. Soil depth (m) eFC CEC EC Soil texture 

1 0 – 0.2 8 6.36 820 Sand 

0.2 – 0.5 22 43.46 95 Loam 

0.5 – 1 22 56.51 32 Loam 

2 0 – 0.1 8 1.34 1.5 Sand 

0.1– 0.35 8 6.85 4.5 Sand 

0.35 – 0.7 8 6.47 6 Sand 

0.7 – 1.5 8 1.63 5.5 Sand 

3 0 – 0.25 8 3.69 2.5 Sand 

0.25 – 0.35 8 4.29 16 Sand 

0.35 – 1 8 6.36 24.5 Sand 

4 0 – 0.15 8 7.66 7 Loamy sand 

0.15 – 0.45 8 4.89 8 Sand 

0.45 – 0.75 8 4.29 0.75 Sand 

0.75 – 2 8 3.69 0.45 Sand 

5 0 – 0.15 8 5.11 11 Sand 

0.15 – 0.6 8 4.89 16.5 Sand 

0.6 – 0.75 8 7.28 17.5 Sand 

0.75 – 1.5 8 4.24 18 Sand 

6 0 –0.72 8 2.07 0.95 Sand 

0.72  – 1.05 8 2.17 0.8 Sand 

1.05 – 1.2 8 43.48 0.6 Loamy sand 

 

eFC is effective field capacity, CEC is cation exchange capacity and EC is electric conductivity of the soil  

 

2.5. Topography Map 
It is represented by steepness percent. Areas with steep slopes are less vulnerable to groundwater contamination. 

The Digital Elevation Model map (90 m x 90 m DEM-map) obtained from Shuttle Radar Topography Mission 

(SRTM) is used in extracting the topographic feature of the QAWT. Accordingly, the DEM-map is modeled on GIS 

platform using GIS Software to define the slope of each cell.   

 

2.6. Impact of Vadose Zone Map 
The impact of vadose zone involves two main parameters of the unsaturated zone, the thickness of clay lenses 

and the soil infiltration rate. The clay content is an important parameter for adsorption processes, and to a slightly 

lesser extent for cation exchange and biodegradation processes. The weighted clay lenses' thickness is developed as 

described by Bodenkunde [25], (Table 4).   

 
Table-4. Assessment of unconsolidated rocks (number of points = Ru), by Bodenkunde [25] 

Type of unconsolidated rock 

 

Ru = No. of points per meter bed thickness 

Clay 500 
Loamy clay, slightly silty clay 400 

Slightly sandy clay 350 

Silty clay, clayey silty loam 320 

Clayey loam 300 

Very silty clay, sandy clay 270 

Very loamy silt 250 

Slightly clayey loam, clayey, silty loam 240 

Very clayey silt, silt loam 220 

Very sandy clay, sandy silty, loam, slightly sandy loam, loamy silt  200 

Sandy loam, slightly loamy silt 180 
Slightly loam, silt, sandy loamy silt,silt, slightly sandy loam. 160 

 Continue 



Asian Review of Environmental and Earth Sciences, 2015, 2(1): 9-22 

 

 

 

 

14 

 

        

 In the other side, the methodological approach used in this paper is based on the vulnerability modeling 

techniques using a range of different methods [3, 21, 26-36]. Unfortunately, no unified methodology of vulnerability 

assessment has been accepted in the QAWT although the problem has been presented in several works [16, 37-40]. 

This may attribute to the complexity and variability of recharge and groundwater flow conditions in the 

hydrogeological medium. For this reason, when developing the current concept for the intrinsic groundwater 

vulnerability map of QAWT, the authors based it not only on the use of concepts published abroad but also on their 

own experience.  

 

2.7. Intrinsic Vulnerability Methodology 
Intrinsic vulnerability is assessed by the GOD, PRAST and DRASTIC overlay and index methods. The first 

GOD method [27, 41]  considers the susceptibility of the aquifer to the entry of contaminants from the topographic 

surface. The following variables are analyzed: groundwater occurrence (G), overall lithology of aquifer or aquitard 

(O) and depth to groundwater table (D). The D factor depends on aquifer recharge. The marked irrigation system 

irregularity, both flooding and drip irrigation, that is typical in QAWT, requires defining a specific period when 

evaluating the vulnerability of the QAWT to contamination. Vulnerability should be analyzed for the situation of 

greatest risk of groundwater contamination, that is, one corresponding to a period of high levels of irrigation, 

favoring aquifer recharge and the transport of contaminant materials, Goldscheider and Popescu [42]. QAWT 

recharge from return flow after irrigation and seepage from the surface water bodies produce a rise in the piezometric 

level and thus increased vulnerability, due to the reduced transit time between the entry of potential sources of 

contamination and their contact with the groundwater. According to Vrba and Zaporozec [3] and Civita [43], the 

GOD method comprises a mapping overlay based on a factor-scoring system. The variables G, O and D are obtained 

from the field measurements and the different constructed maps. The super-position of these three information layers 

is performed within a Geographic Information System (GIS), which is used to calculate the index and classes of 

vulnerability where the GOD Index reads: 

GOD vulnerability index = Rating for Groundwater occurrence x Rating for Overlaying lithology (only in case of 

unconfined aquifers) x Rating for Depth to water            ……………………………………………..………….1 

 
Figure-8. GOD overlay and index system of aquifer vulnerability assessment (after Foster and Hirata [41]) 

Very clayey sand, clayey sand, loamy silty sand 140 

Sandy silty, very loamy sand 120 

Loamy sand, very silty sand 90 

Slightly clayey sand, silty sand, sandy clayey gravel 75 

Slightly loamy sand, sandy silty gravel 60 

Slightly silty send, slightly silty sand with gravel 50 

Sand 25 

sand with gravel, sandy gravel 10 

gravel, gravel and breccia 5 

unconsolidated volcanic material 200 

Peat 400 

Sapropel 

 

 

300 



Asian Review of Environmental and Earth Sciences, 2015, 2(1): 9-22 

 

 

 

 

15 

 

 

In addition, the second PRAST rating system  [43] is another method for quick assessment of vulnerability using 

five parameters: Protective effectiveness, Net Recharge, Aquifer media, Soil media and Topography. The overall 

"Pollution Potential" or PRAST Index PI is established by applying the following formula:              

PI = PrxPw + RrxRw + ArxAw + Sr xSw + TrxTw…………………................................………..2 

Where r is the rating value and w is the weight associated to each parameter. The ratings in PRAST model were 

assigned values between 1 and 10, while the weight of every factor had a fixed value which is listed in Table 5.  

Table-5. Assigned weights for PRAST parameters. 
 

 

 

 

One of the most widely used groundwater vulnerability methods is the third chosen method; i.e., DRASTIC [26]  

and developed by the United States Environmental Protection Agency (US EPA) [44] as a method for assessing 

groundwater pollution potential. In the DRASTIC method specific criteria are assigned different degrees of 

importance on a scale 1 to 5 (Table 6). These criteria including: depth to water level, effective infiltration, aquifer 

media, type of soil, topography, impact of vadose zone, and the hydraulic conductivity of aquifer. Vulnerability 

DRASTIC index DI is the sum of the multiplication of variable rank and weight of individual criterion. For each 

mapping unit, it is calculated using the most important seven different hydrogeological parameters that affect the 

potential for groundwater pollution. It is computed as [45-51]:  

DI = DrxDw + RrxRw + ArxAr + SrxSw + TrxTw + IrxIw + CrxCw …………..3 

Where D is the Depth to water, R is the net Recharge, A is the Aquifer media, S is the Soil media, T is the 

Topography, I is the Impact of the vadose zone, C is the hydraulic Conductivity, r is the rating value and w is the 

weight associated to each parameter. Each parameter is assigned the same weight all over the QAWT but different 

ratings, according to the hydrological, geological and hydrogeological conditions. The weight of three criterions 

(Soil media S, vadose zone media I and topography T) is modified to adapt the physical conditions of the QAWT. 

Worth mention, the soil media (S) and the impact of the vadose zone media (I) of the QAWT can be considered as 

one continuous layer of equal importance, and can thus be assigned an equal weight (5). Also, the DRASTIC 

criterion relative to the slope of topography is governed mainly by the prevailing irrigation practice in humid areas 

including mountainous, rugged and flat surfaces which is different in arid area like the QAWT with flat lands or 

lands with gentile slope. It modified from weight of 1 to 2.   

 
Table-6. Rating and weight of criterion for DRASTIC criterions with assigned weights (after Aller, et al. [26]- modified for the QAWT)  

No 

 

Criterion Classes of criterion Weight of criterion Rank 

 1 Depth to groundwater table >5 m 5 7 

3.1- 5 m 8 

1.1 – 3 m 9 

<1 m 10 

2 Net Recharge (mm/year) 50-75 4 2 

76-100 3 

101-125 4 

126-150 5 

>150 6 

3 Lithology of Aquifer Sandy clay, loam, loam and sand 3 2 

Sandy loam, sands 3 

Sands, sandy loam 4 

Sands 6 

Sands, gravel 8 

4 Soil media Loam 5 5 

Sandy loam 6 

Shrinking clay 7 

Peat 8 

Thin anthropogenic 9 

Absent 10 

5 Topography (slope) (%) 2.9-3.9 2 7.5 

2.5-2.9 8 

2.0-2.5 8.5 

1.6-2.0 9 

1.0-1.6 9.5 

1.0-0.0 10 

6 Impact of vadose zone Clay 5 2 
Silty loam 3 

 Continue 

Parameter Weight 

Protective effectiveness 8 

Net Recharge 4 
Aquifer Media 3 

Soil Media 2 
Topography 1 



Asian Review of Environmental and Earth Sciences, 2015, 2(1): 9-22 

 

 

 

 

16 

 

Loam 4 

Sands 6 

Sands, gravel 8 

7 Hydraulic Conductivity of 

aquifer (m/day) 

< 9 3 1 

9-11 2 

12-28 4 

29-40 6 

41-80 8 

 

3. Results and Discussion 
The results of the chemical analysis of the chosen groundwater samples of the QAWT show that the salinity 

distribution map (Figure 5) is well conformable with the water table map (Figure 4), where salinity increases 

gradually with the hydraulic gradient and vice versa. Also, the hypothetical salt assemblages change from north to 

south according to metasomatic processes. The effect of the evaporites in the eastern parts is more pronounced in the 

high salinity of their groundwater. Chloride water type is the dominant and exists by 86%, while the bicarbonate 

water type represents 14% only. The gradual increase of salinity and the change of water type in the QAWT reveal 

that, the groundwater has been subjected to physiochemical mixing processes during the beginning of the Holocene 

periods, cation exchange and the mixing of Nile water with locally infiltrated fossil water.  

 

 
Figure-5. Salinity distribution map in mg/l (left) and the hypothetical salt assemblages (right map, Fatouh, et al. [52]) of the groundwater of 

the QAWT 

 

The groundwater pollution is observed from the results of the chemical analysis of the 14 environmental 

sensitive heavy metals and two minor elements (Table 7). Both surface and groundwater are mostly polluted with B, 

Sr, V, PO4
--
 and NO3

-
 according to the World Health Organization Standards for Drinking Water (WHO) [53] and 

Egyptian Health Committee for drinking Water standards (EHCW) [54] standards (Table 7). The concentration of 

these pollutants exists in risky levels. The concentration of PO4
-- 

in the groundwater ranges from 0.097 to 53.23 mg/l 

while NO3
-
 concentration ranges from 5.17 to 83.65 mg/l (Table 7 & Figure 6). Figure 6 shows that the northeastern 

part is more polluted than the southern part of the QAWT. This may attribute to the shallow depth to water, flood 

irrigation system, over use of the fertilizers and bad drainage system characterizing to the northeastern cultivated 

lands.   

 
Table-7.Results of chemical analysis of the minor and trace elements in the surface and groundwater of the QAWT (values in mg/l). 

   BDL is Below Detection Limit, and the sign * represents the median concentration [21]. 

 

Element Concentration 

range in surface 

water (mg/l) 

Concentration 

range in ground 

water (mg/l) 

World Health 

Organization Standards 

for Drinking Water 

(WHO) [53]   (Acceptable) 

Egyptian Health Committee 

for drinking Water 

standards (EHCW) [54]  

(Permissible) 

Al 0.1 - 0.4744 (BDL) 0.05 - 0.2 0.2 

B 0.006 - 9.245 0.0607 - 3.369 1 No index 
Cd (BDL) (BDL) - - 

Co (BDL) (BDL) - - 

Cr 0.004 - 0.0257 0.004 - 0.0308 0.01 - 0.1
*
 - 

Cu 0.02 - 0.0915 0.02 - 0.2293 1 1.5 

Fe 0.003 - 0.2524 0.003 - 0.509 0.3 1 

Mn 0.0149 - 0.0151 0.0062 - 0.2087 0.1 0.5 

Mo 0.01 - 0.1584 0.01 - 0.0646 0.05 - 0.5
*
 - 

Ni 0.006 - 0.0114 0.006 - 0.0114 0.01 - 0.04
*
 - 

Pb (BDL) (BDL) - - 
Sr 0.4252 - 22.425 0.4136 - 7.925 0.11

*
 - 

V 0.007 - 2.681 0.0438 - 0.4084 0.01 - 0.1 - 

Zn 0.001 - 0.2257 0.012 - 0.1551 5 15 

Phosphate 0.037 - 2.9 0.097 - 53.23 1 1 

Nitrate 0.115 - 58.222 5.17 - 83.65 10 10 



Asian Review of Environmental and Earth Sciences, 2015, 2(1): 9-22 

 

 

 

 

17 

 

 
Figure-6. Iso-PO4 concentration map (left) and Iso-NO3 concentration map in mg/l (right) in the groundwater of the QAWT at 2005 

 

In addition, the calculated GOD vulnerability index ranges from 0.2 (low vulnerable) to 0.5 (moderate 

vulnerable) (Table 8) while it ranges from 36 (low vulnerable) to 97 (very high) for PRAST index (Table 9). The 

calculated DRASTIC vulnerability index shows a range from 80 to 142 (Table 10). As a general, these indexes do 

not provide absolute answers; they only differentiate highly vulnerable areas from less vulnerable areas. The nature 

of these models are additive. Every parameter in the model has a fixed weight indicating the relative influence of the 

parameter in transporting contaminants to groundwater. The parameter rates are variable, which allows the user to 

calibrate the model to suit a given region. The vulnerability classes are defined according to the range of the obtained 

vulnerability index, taking into account a classification made by Navulur and Engel [55], but even the classification 

proposed by Lobo Ferreira and Oliveira [56] will show the same vulnerability in the QAWT. 
 

Table-8. The estimated GOD index (GI) required for intrinsic vulnerability mapping of the QAWT 

 
 

Table-9. The estimated PRAST index (PI) required for intrinsic vulnerability mapping of the QAWT 

W.N P R A S T PI W.N P R A S T PI W.N P R A S T PI 

9 4 1 6 25 0 36 51 16 1 9 25 0 51 59 10 1 18 30 15 74 
10 4 1 9 25 0 39 52 16 1 6 25 0 48 68 10 1 9 30 15 65 
17 22 1 6 25 0 54 53 16 1 9 25 0 51 69 10 1 24 30 15 80 
19 26 1 9 25 0 61 54 18 1 12 25 0 56 70 16 1 9 25 15 66 
21 24 1 6 25 16 56 55 18 1 6 25 0 50 71 24 1 9 25 15 74 
25 4 1 9 25 16 55 56 16 1 9 25 0 51 72 10 1 9 25 15 60 
32 24 1 24 25 16 90 57 16 1 12 25 17 54 73 10 1 12 30 15 68 
47 14 1 12 25 16 68 60 4 1 18 25 17 65 74 10 1 18 30 15 74 
48 14 1 6 25 15 62 61 4 1 12 25 16 59 75 10 1 9 30 15 65 
28 30 1 9 25 15 80 62 6 1 9 25 16 57 76 32 1 6 30 15 84 
46 14 1 12 25 15 67 63 8 1 6 35 16 66 77 10 1 9 35 15 70 
11 16 1 18 25 15 75 64 36 1 9 35 16 97 78 14 1 6 35 15 71 
12 8 1 18 25 15 67 65 6 1 12 35 16 70 79 14 1 9 35 16 74 
13 8 1 9 25 15 58 66 8 1 18 35 16 78 80 12 1 12 35 16 76 
49 6 1 12 25 15 59 67 8 1 9 30 16 64 81 8 1 18 35 16 78 
50 16 1 18 25 0 75 58 10 1 12 25 15 64 82 10 1 24 35 16 86 

 
Table-10. The estimated DRASTIC Index (DI) required for intrinsic vulnerability mapping of the QAWT 

W. N D R A S T I C DI W. N D R A S T I C DI 
9 35 1 6 25 0 15 3 85 61 35 1 12 25 16 10 3 102 

10 35 1 9 25 0 15 3 88 62 35 1 9 25 16 10 3 99 

17 40 1 6 25 0 15 3 90 63 35 1 6 35 16 10 3 106 

19 40 1 9 25 0 15 6 96 64 40 1 9 35 16 15 3 119 

21 40 1 6 25 16 10 6 104 65 35 1 12 35 16 15 3 117 

25 35 1 9 25 16 10 6 102 66 40 1 18 35 16 15 3 128 

32 35 1 24 25 16 10 12 123 67 45 1 9 30 16 15 3 119 

47 35 1 12 25 16 10 6 105 58 40 1 12 25 15 10 3 106 

48 35 1 6 25 15 10 12 104 59 40 1 18 30 15 10 3 117 

28 40 1 9 25 15 30 6 126 68 35 1 9 30 15 10 3 103 

46 40 1 12 25 15 30 12 135 69 35 1 24 30 15 10 6 121 
11 35 1 18 25 15 15 6 115 70 40 1 9 25 15 10 6 106 

12 35 1 18 25 15 15 6 115 71 35 1 9 25 15 10 6 101 

13 35 1 9 25 15 15 6 106 72 40 1 9 25 15 10 6 106 

49 35 1 12 25 15 15 3 106 73 35 1 12 30 15 10 6 109 

50 35 1 18 25 0 15 3 97 74 45 1 18 30 15 10 6 125 

51 35 1 9 25 0 15 3 88 75 40 1 9 30 15 10 6 111 

                 Continue 



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18 

 

52 35 1 6 25 0 15 3 85 76 35 1 6 30 15 10 6 103 

53 35 1 9 25 0 10 3 83 77 40 1 9 35 15 10 6 116 

54 35 1 12 25 0 10 3 86 78 40 1 6 35 15 10 6 113 

55 35 1 6 25 0 10 3 80 79 45 1 9 35 16 10 6 122 

56 35 1 9 25 0 10 3 83 80 45 1 12 35 16 10 6 125 

57 35 1 12 25 17 10 3 103 81 45 1 18 35 16 10 6 131 

60 35 1 18 25 17 10 3 109 82 50 1 24 35 16 10 6 142 
W.N is well number, D is the Depth to water, R is the net Recharge, A is the Aquifer media, S is the Soil media, T is the Topography, I is the Impact 

of the vadose zone, C is the hydraulic Conductivity and DI is the vulnerability DRASTIC index. 

 

The effect of the hydrogeological conditions on the vulnerability assessment of the QAWT is clear through the 

small differences between the produced intrinsic vulnerability maps applying the PRAST and DRASTIC methods of 

overlay and index. The final intrinsic vulnerability maps obtained in this study show three classes of vulnerability in 

the QAWT: low, medium and high (Figure 7, 8 and 9). The resulted intrinsic vulnerability map of QAWT applying 

GOD method (Figure 7) indicates higher vulnerability in the area around El-Mahsama lake and El-Mahsama drain 

and clearly indicates the bad drainage system of this locality. The same results of high vulnerable areas of the QAWT 

are obtained applying both PRAST and DRASTIC models (Figure 8 & 9). These two vulnerability maps reflect 

simplicity of aquifer vulnerability spatial distribution which is practically more or less not true. This may attribute to 

the selection of the ratings and weights that has to be assigned to the five or seven base maps which represent the five 

or seven parameters in case of PRAST or DRASTIC model. Such a selection can strongly affect the result of the 

final vulnerability map. Given the fact that it is not possible to avoid subjectivity, the way to deal with it is by 

performing a sensitivity analysis which is out of scope of this study. 

 

 
Figure-7. Intrinsic vulnerability map according to GOD method 

 

 
Figure-8. Intrinsic vulnerability map according to PRAST method 

 



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19 

 

 
Figure-9. Intrinsic vulnerability map according to DRASTIC method 

 

The obtained vulnerability maps by different methods show, in general terms, some sort of homogeneity in 

respect to overall zonation. In other words, the maps show two distinct zones, the northern zone which tends to attain 

comparatively high index values, and the southern zone which is characterized generally by the lowest index values. 

This is particular due mainly to the extreme difference between the northern and the southern zones in respect to 

depth to water, net rate of recharge, topography and presence or absence of agricultural lands where pesticides 

weights has to be taken into account. The northern zone is featured by lands of relatively low levels and accordingly 

the proximity of groundwater to the surface, in addition to intensive irrigation. The southern zone is characterized by 

higher topographic levels accompanied accordingly by deeper groundwater in addition to limited irrigation practice. 

Therefore, it can be stated that the southern zone is less vulnerable than the northern zone. 

As a general, the obtained results related to the vulnerability show the high extension of the zones with medium 

vulnerability (21%, 65% and 61% for applying GOD, PRAST and DRASTIC methods respectively) comparing to 

the other zones of the groundwater. The zones with high vulnerability occupy about 35% and 31% from applying 

PRAST and DRASTIC methods respectively while the GOD method do not show any ratio for this class. The zones 

with low vulnerability occupy about 79%, 13% and 8% of the total surface of the groundwater in case of applying 

GOD, PRAST and DRASTIC methods respectively. The zones with high vulnerability are located mainly in spots 

between El-Qassasin and El-Mahsama lake in the west and El-Manaif village in the east. Also, they cover great parts 

of Abu Sweir city (Al-Amal and Al-Mostaqbal new towns). The high vulnerability in these zones is mainly related to 

the low values of depth to water (less than 10 m), the high permeability of the soils (9 m/day) and the high 

permeability of the vadose zone materials (more than 11 m/day), which are mainly constituted by sandstone or by 

intercalations of sand and sandstone. The moderate vulnerability areas are locating in a vast zone located in the 

south, west and north of the Ismailia town. Other occurrence is related to the area of the village of Nefisha, at the 

crossroads of the Cairo-Ismailia and Suez-Ismailia highways, and in the zone of Sarabium. Finally, the areas with 

low vulnerability are locating in the extreme south of the Wadi El-Tumilat, and in some restricted zones NE the 10
th
 

of Ramadan city and in the region of the El-Wadi drain. However, these newly developed maps are found to be more 

or less in conformity with the salinity distribution map of the groundwater in the study area (Figure 5), which shows 

high values of TDS in the north and that the salinity decreases towards the south direction. Also, the developed maps 

shows the presence of two infected centers with pollution (in the north and the south) which is comparable with the 

PO4
--
& NO3

-
 concentration contour maps (Figure 6). Finally, it is noticed that in general, in the QAWT, the areas 

located adjacent to the Ismailia canal and local drains crossing high vulnerable zones are characterized by a 

permeable vadose zone, and that can increase the risk of the pesticides' pollution and other pollutants in these areas. 

In the other point, if the newly developed DRASTIC map is compared with the previous DRASTIC maps 

prepared by RIGW/IWACO [37] (Figure 10) and by Saad [39] (Figure 11) and by the vulnerability map of Dahab, et 

al. [40] (based on the classification scheme of Zekster [57] (Figure 12), some distinct variations are observed. 

Whereas, the newly developed DRASTIC map identifies spots of the northern portion of the QAWT as highly 

vulnerable, and the southern portion attains low vulnerability, the other previous maps reveal opposite conclusions. 

This is, however, due mainly to the fact that the latter vulnerability mapping do not take into consideration some 

important factors (depth to water, net recharge and hydraulic conductivity). RIGW/IWACO [37] DRASTIC map 

neglects the soil media and hydraulic conductivity parameters while [37] DRASTIC map divides the DRASTIC 

parameters into static (five parameters) and dynamic (two parameters). Dahab, et al. [40] vulnerability map neglects 

the depth to groundwater and the net recharge parameters. Also, the RIGW/IWACO [37] map has not given 

differentiation between the weights of the various factors involved in the aquifer vulnerability, and accordingly, all 

factors are given the same degree of importance. It can thus be concluded that the RIGW/IWACO [37] map 

represents, to a great extent, the static features, of the aquifer vulnerability. Accordingly, if the dynamic parameters 

are integrated to the RIGW/IWACO [37] map the final aquifer vulnerability will approach the final DRASTIC map 

presented in this paper. Finally, these previous maps are considered as operative maps in the classification of Civita 

[43].  

 



Asian Review of Environmental and Earth Sciences, 2015, 2(1): 9-22 

 

 

 

 

20 

 

 

Figure-10. Intrinsic vulnerability map according to DRASTIC method (after RIGW/IWACO [37] ) 
 

 
Figure-11. Intrinsic vulnerability map according to DRASTIC method (after Saad [39]) 

 

 
Figure-12. Intrinsic vulnerability map according to DRASTIC method (after Dahab, et al. [40]) 

 



Asian Review of Environmental and Earth Sciences, 2015, 2(1): 9-22 

 

 

 

 

21 

 

4. Conclusion and Recommendations 
In this paper, the groundwater pollution of the QAWT is detected from the results of the chemical analysis of 

both surface and groundwater samples collected at 2005. Both surface and groundwater resources are mostly polluted 

with B, Sr, V, PO4
--
 and NO3

-
 with risky levels. The concentration of PO4

-- 
and NO3

- 
in the groundwater ranges from 

0.097 to 53.23 and 5.17 to 83.65 ppm respectively. The northeastern part is more polluted than the southern part of 

the QAWT due to shallow depth to water, flood irrigation system, over use of the fertilizers and bad drainage system.   

Three different overlay and index methods (GOD, PRAST and DRASTIC) have been used based on the 

hydrogeological conditions for vulnerability assessment. The calculated vulnerability indexes resulted from these 

three methods show greet differences due to the different criteria used. The calculated GOD vulnerability index 

ranges from 0.2 (low vulnerable) to 0.5 (moderate vulnerable) while it ranges from 36 (low vulnerable) to 97 (very 

high vulnerable) for PRAST index, and from 80 (low vulnerable) to 142 (very high vulnerable) for DRASTIC index. 

These indexes only differentiated highly vulnerable areas from less vulnerable areas. Also, a modification from 

weight of 1 to 2 for the DRASTIC criterion relative to the slope of topography is assumed to adequate the 

hydrogeological conditions of arid zones like the QAWT. 

The obtained results related to the vulnerability maps show the high extension of the zones with medium 

vulnerability (21%, 65% and 61% for applying GOD, PRAST and DRASTIC method respectively) comparing to the 

other zones of the groundwater. The zones with high vulnerability occupy about 35% for the PRAST overlay method 

and 31% for the DRASTIC overlay method while the GOD method do not show any ratio for this class. The zones 

with low vulnerability occupy about 79% for the GOD overlay method, 13% and 8% of the total surface of the 

groundwater in case of applying PRAST and DRASTIC overlay methods. The zones with high vulnerability are 

located mainly in spots between El-Qassasin and El-Mahsama lake in the west and El-Manaif village in the east. 

Also, they cover great parts of El-Manaif village in the east and Abu Sweir city (Al-Amal and Al-Mostaqbal new 

towns). The high vulnerability in these zones is mainly related to the low values of depth to water (less than 10 m), 

the high soil permeability (9 m/day) and the high permeability of the vadose zone materials (more than 11 m/day). 

The developed intrinsic vulnerability maps show the presence of two infected centers with pollution (in the north and 

the south) which are comparable with the PO4
--
& NO3

-
 concentration contour maps. The newly developed DRASTIC 

map is more or less comparable with the previous DRASTIC maps cited in RIGW/IWACO [37] and Saad [39] and 

the vulnerability map in Dahab, et al. [40]. Some distinct variations are observed due mainly to both the fact that the 

latter vulnerability mapping do not use some important factors like depth to water, net recharge and hydraulic 

conductivity, and equalization between the weights of the various factors involved in preparing these aquifer 

vulnerability maps.  

Based on the results of this paper, it is recommended that the most suitable areas for new reclamation activity 

locate in the southern boundary of Wadi El Tumilat especially the strip south El Mahsama drain by 5 km. It is also 

highly recommended to make public awareness about the threats of pollution on groundwater resources especially in 

the vulnerable areas. Sealing the drainage system to minimize the pollution by heavy and trace elements in the 

northern and eastern lowlands is highly recommended.  Improving the irrigation system and preventing the 

continuous drainage of sewage and waste water to Ismailia canal and the drainage system is also recommended. The 

continuous use of the huge garbage dumps, especially near Sarabium area and the Ismailia-Suez desert road 

characterized by shallow groundwater must be transported to other suitable places.  

 

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