Environmental threats of on-Site Sewage disposal on

Transcription

Eighteenth International Water Technology Conference, IWTC18
Sharm ElSheikh, 12-14 March 2015
ENVIRONMENTAL THREATS OF AN ON-SITE SEWAGE DISPOSAL ON
GROUNDWATER AT MINIA-ALQAMH, SHARKIA GOVERNORATE,
EGYPT
Abdel Fattah Morsi Atwa1, Abdelazim Negm2, Asaad M. Armanuos3
1
National Organization for Potable Water & Sanitation Co., General Manager in Sharkia
Dep.
2
Chairperson of Environmental Engineering Dept., Egypt-Japan University of Science and
Technology E-JUST, New Borg El-Arab, Alexandria, Egypt, E-mail: [email protected], (seconded
from Zagazig Uniersity, [email protected])
3
Ph.D. Student, Environmental Engineering Dept, School of Energy and Environment and
Chemical & Petrochemical Engineering, Egypt-Japan University of Science and Technology, E-JUST,
Alexandria, Email:[email protected]
ABSTRACT
All over the world, the urban growth increases the demand of fresh water supply. In some regions
the groundwater (GW) is main the sources of fresh water especially when the surface water in not
sufficiently available or scarce. This is the case of some places in East of the Nile Delta. In some
cases, the GW is polluted be the sewage water causes serious human health problems. Recently, the
quality and quantity of the GW has been identified in response to the increased human activities and
the deficient in fresh surface water. It was found that the greatest danger of GW pollution is from
surface sources such as: sewer, polluted drains, sewage ponds, septic tanks and refuse disposal sites
and human sources.
The main objectives of this study are to assess the GW in some selected areas in Minia-Alqamh
district and to locate the potential sources for GW pollution, based on the available land use data. The
study area lies to the eastern part of Nile Delta. The ultimate objective is to improve wastewater
treatment in the study area to protect the GW as a fresh water source from being polluted. In order to
achieve the goals of this study, the geoelectric resistivity survey were carried out and interpreted in the
form of apparent and true resistivity maps, geoelectric cross sections and integrated models. The final
models are based on the results of integration of resistivity measurements and data of both hydrogeological and chemical analysis.
The extensive analysis of geoelectric resistivity indicated that the quaternary aquifer consists of four
layers. The GW level subdivides the second layer into two resistivity facies, the upper facies
represented by low values sandy facie and the lower facies represented by silty to sandy facies. The
geochemical analysis indicated that a potential pollution from the surface pollution sources are
possible and the salinity levels are very high and risky. Therefore, it is recommended that the primary
treatment and biological treatment should be included in the water treatment plants to remove BOD
and the total suspended solids in addition to The tertiary treatment also to remove impurities from
sewage, producing an effluent of almost drinking-water quality.
Keywords: Groundwater contamination, Geoelectric resistivity, pollution, treatment, wastewater,
landfill waste, Sharika Governorate.
1 INTRODUCTION
Urban growth has increased the demands on GW supplies in the area east of the Nile Delta. The
problem of GW quality and quantity has been identified during the few years in response to the
increased human activities. In this regards, Abdel-Lah and Shamrukh (2001) stated that the Sewage is
the main source of pathogenic microbial contamination of ground water as it is in surface water.
127
Bacteria travel through soil matrix and diverse the microbes within this group. Also, many diseases
caused by bacteria such as diarr hoeal, dysentery, cholera, and typhoid fever. The unsafe method of
sewage system construction and the shallow depth of water table made the situation of sewage
contamination is worsening. In rural areas of Upper Egypt the wastewater is disposed and collected
into an underground sewage room and it contact direct with ground water. The results showed that
water samples from many hand pumps and deep well s in a Nile Valley village contaminated with
pathogenic bacteria. They recommended to prevent the leaching from sewage rooms in Upper Egypt
part of Nile Valley aquifer and the depth of hand pumps and wells must be deeper and far away from
the sewage tank. Also, Taha et al. (2004) assessed the state of groundwater pollution in the new
communities, Southeast Nile Delta, Egypt. Industrial, agricultural and domestic activities were the
sources of pollution and cause deterioration of groundwater quality due to the misuse of fertilizers and
pesticides. They evaluated the suitability of different water resources in new communities and stated
its impacts on human health and plant hazard. Moreover, Gemail et al. (2011) integrated 1D resistivity
sounding and 2D resistivity imaging surveys with geological and hydrochemical data to assess the
vulnerability and the seawater intrusion in El-Gharbyia main drain, north of Nile Delta, Egypt. Twenty
Schlumberger soundings and six 2D dipole–dipole profiles were executed in the western side of the
main drain. They assessed the protection of the groundwater aquifer and the potential risk of
groundwater pollution depending on results from the results from the resistivity and hydrochemical
data. They estimated the integrated electrical conductivity (IEC) by using the inverted resistivity and
thicknesses of the layers above the aquifer layer and used if after that for quantification of aquifer
vulnerability. The aquifer vulnerability maps indicated that underlying sand aquifer is high
vulnerability zone with slightly fresh to brackish groundwater and the subsoil structure around the
main drain that is highly affected by waste water.
In addition to the above, the resistivity method used in a wide range in geological studies especially
in groundwater Nile Delta aquifer. Abdel-Raouf and Abdel-Galil (2013) used electrical resistivity
soundings method to investigate groundwater of Wadi El Natrun, Eagypt northwest of the Nile Delta.
Also, they studied the stratigraphic sequence of the different aquifers and delineating the factors
affecting groundwater potentialities and movements. The results of electrical soundings delineated that
there are different water bearing zones with varying thicknesses. The hydrogeological data of the
study area related to existence of four main aquifers distributed in the study area. The main aquifer of
the study area has been contaminated due to the effect of surface water irrigation.
Recently, Armanuos et al. (2015) investigated the factor controlling the groundwater quality
western Nile Delta aquifer by using multivariate statistical technique. The results showed that there
were four factors account for 77 % of the total variance of hydrochemistry data. The first and second
factors related to mineralization, mining and salinity due to saltwater intrusion. The other factors
assigned to industrial wastes, domestic wastes and agriculture activities. They recommended that the
authorities should take necessary actions to control the different sources of groundwater pollution.
Also, Armanuos et al. (2015) assessed the groundwater of western Nile Delta, Egypt for drinking
purposes by using water quality index. They used the WHO and Egypt standards (ES) as a reference to
determine the suitability of groundwater for drinking purpose. The results showed that about 45.37%
and 66.66 % of groundwater wells falls in good drinking water zone according to WHO and Egypt
standards. Also, t 37.03 % and 15.07 % fall in the poor drinking water zone according to WHO and ES
respectively and 9.25 % and 11.2 % falls in unfit for DW category according to WHO and ES. They
concluded that human activities, agriculture activities and other industrial pollutants contribute in the
degradation of groundwater quality Nile Delta aquifer.
This research presents the results of geohydrochemical - geoelectric resistivity of fresh water
aquifer in Minia Alqamh, Sharikia Governorate to answer the question “is the fresh groundwater in the
area subject to contamination from the sources of waste water?. To achieve the goals of this study, the
geoelectric resistivity survey are carried out and interpreted in the form of apparent and true resistivity
maps, geoelectric cross sections and integrated models. The final models are based on the results of
integration of resistivity measurements and data of both hydro geological and chemical analysis.
128
2 CHARACTERISTICS OF THE STUDY AREA
The study area lies to the eastern part of Nile Delta figure (1), where the Quaternary unconsolidated
aquifer is separated from the underlying Miocene aquifer by a Pliocene thin clay bed.
31°
15'
31° 30'
31° 15'
32° 00
31° 45'
32° 15' PORT
SAID 31°
15'
Manzala
Lake
31°
00
31°
00
DAKAHLIYA
Diarb
Nigm
30°
45'
Abu
Kabir
30°
45'
Faqus
Hihya
30°
15'
30°
30'
A
lq
a
mh
El Salhiya
Mi
na
30°
30
Ismailiya Canal
30°
15'
Mashtul El
Soak
Tenth of
Ramadan
30°
00
10
31° 15'
31° 30'
31° 45'
Studied area
0
32° 00
10 Km
32° 15'
30°
00
City Location
Fig. (1): Location map of the study area
2.1 General Geology
Generally, the eastern part of the Nile Delta was investigated by different geological studies, e.g.
Bayoumy (1971), Zaghloul et al., (1977), Shata et al., (1979), Said (1981), Korany et al., (1997), Abd
El Gawad (1997) Ibrahim et al., (2005), and El Sharkawi (2008).
2.2 Topography
The study area ranges between 3m (above sea level) at the northern, to about 15 m at the south of
area, with a general slope towards the north (Fig. 2). It is dissected by a complex irrigation system,
which has a direct influence on both the GW recharge and movement of the Quaternary aquifer (Shata
et al., 1979).
2.3 Surface Geology
The surface geology of the study area was studied by several geological studies eg., El Said (1981)
and Zaghloul et al., (1990). CONOCO, (1987), According to GPC & the rock units exposed in the
area can be mainly classified into Quaternary deposits as follows:
2.3.1 Quaternary deposits
Quaternary deposits cover the studied area. It represented by Nile silt, wadi deposits, alluvial fans
and sand dunes. According to mode of formation, Quaternary deposits are classified, from bottom to
top, into Pleistocene and Recent (Holocene) (Fig. 3).
Fig. (2): Topographic map of the studied area
(Compiled after Shata et al., 1979).
Fig. (3): Geological map of the study area (Compiled
after GPC, CONOCO, 1987).
129
2.3.2 The Pleistocene sediments;
The Pleistocene sediments are considered as the main GW aquifer in the study area. It includes
three types of deposits, namely, the old Aeolian deposits or (Mit Ghamr Formation, the old
fluviomarine deposits and the old deltaic deposits.
2.3.3 The Holocene deposits
They are widespread and divided into the following types:
1) The young deltaic deposits Neonile (Bilqas Formation); which are composed of Nile silt, fine
sand and clay. They show gradual increase in thickness (10 m) to the north (Fig.3).
2) The young Aeolian deposits; which are represented by loose fine to coarse sand with variable
thickness (Fig. 3).
2.4 Subsurface Geology
The subsurface Tertiary rocks in the study area have been subdivided by Shlumberger (1984) from
bottom to top into three formations belonging to Miocene and three formations belonging to Pliocene
rocks (Fig. 4).
2.4.1 A-Miocene rocks:
The Miocene rocks are divided into three formations from bottom to top as follows: Sidi Salem
Formation (Middle Miocene, Qawasim Formation Upper Miocene and Rosetta Formation.
2.4.2 B-Pliocene rocks:
The Pliocene rocks are divided into three formations from bottom to top as follows Abu Madi
Formation (Lower Pliocene , Kafr El Sheikh Formation (Middle Pliocene) and Wastani Formation
(Upper Pliocene). The Quaternary subsurface in the studied area are classified into two rock units;
Pleistocene rocks (at the bottom) and recent rocks. (Fig. 4).
THICNESS(ft)
TIME ROCK UNITS
980
DELTAIC
FLUVIATILE
FLUVIATILE
SHALLOW
MARINE
4900
SHALLOW
MARINE
TO
KAFR
EL-SHEIKH
OPEN
MARINE
ABU MADI
980
HOLOCENE
UPPER
MIDDLE
LOWER
EL-WASTANI
ROSETTA
160
NEAR
SHORE
LAGOONAL
QAWASIM
2950
UPPER
SHALLOW
MARINE
FLUVIATILE
DELTAIC
SIDI
SALEM
2300
MIDDLE
MIOCENE PLIOCENE
TERTIOARY
CENOZOIC
MIT
GHAMR
2300
BILQAS
RECENT
SHALLOW
MARINE
LOWER
MOGHRA
Fig. (4): Generalization Litho-stratigraphic column of the studied area (after Schlumberger,
1984).
2.5 Structural setting
The structural setting of the study area has been discussed by several researchers, among them are
El-Fayoumy (1968), El Diasty (1969), El Shazely et al., (1975), El Dairy (1980), El Ahwani (1982), El
130
Gamili. (1982), Sallouma (1983) and Khabar (1992).No structures of the study area have been
detected.
2.6 Hydrogeology
The present section deals with the studying of the GW formation, hydrogeological sitting and the
hydrogeological relationship between surface water and GW flow at the study area.
2.6.1 Groundwater Formation:
In the study area, the sediments are of hydrogeological importance as it belongs to the Quaternary.
The Quaternary aquifer represents the main source of GW in the studied area. It is underlined by the
Pliocene plastic clay that acts as an aquiclude, especially in the area of flood plain around Zagazig,
Rizzini et al., (1978), El Hefny (1980), Said (1981) and Serag El Din (1989).
2.6.2 Quaternary Aquifer (Nile Delta aquifer)
The Quaternary aquifer is the principal reservoir of the GW. It is underlined by the Pliocene plastic
clay that acts as an aquiclude, especially in the area of flood plain around Zagazig city. The lateral
and vertical variations in the facies of the Quaternary sediments, lead to their classification into a
number of distinguishable horizons. Each of these horizons has its own characters such as porosity,
hydraulic conductivity, ability for retaining and yielding water, and mode of water occurrence rather
than water quality. These horizons are:
a) Nile silt, sandy clay and clayey sand (Holocene).
b) Fine and medium sands with related sediments (Late Pleistocene).
c) Coarse sands and gravels (Early Pliocene).
2.7 Hydrogeological sitting of the study area
For studying the lateral and vertical lithological variation and structure elements affecting on the
different aquifers in the study area, three hydrogeological cross sections were constructed, covering
the whole area Fig. (5), Atwa (2010). Two of them are marked as L2-L2’and V1-V1’.
Fig.(5): Hydrological cross section, Atwa (2010)
2.7.1 The hydrogeological cross section (L2-L2’)
Figure 6 presents the north-south cross section which shows that the Quaternary aquifer forms the
extension of the eastern flood plain of the Nile Delta (Serag El Din, 1983). It is present under semiconfined conditions toward the north of Ismailia Canal, while, it becomes unconfined and in hydraulic
contact with the canal at the south. The Quaternary aquifer is underlined directly by the deep aquifer.
The Quaternary aquifer is considered as the main source of GW in the study area.
2.7.2 The hydrogeological cross section (V1-V1’) (Fig. 7)
131
Figure 7 presents the cross section V1-V1’ where it passes the SW-NE direction through wells
Abu Hammad and E5 and shows a normal fault structure elements and the presence of two waterbearing formations (Pleistocene and Miocene). The thickness of Pleistocene aquifer in two wells is
less variables approximately.
L2
RAS EL BAR 1
___ ___
0
200
ABU MADI A
___ ___
___ ___
___ ___
E
V3
4/11
L2'
BILQAS
FORMATION.
___ ___
___ ___
S.W BILQAS1
___ ___
MIT GHAMR 1
7/10
1/11
1/7
5/10
8/7
1/8
17/1
W
V3'
2/1
NE
Sw
E4
Abu Hammad
V1 P2
19/1
V1'
10
Water Table
Water
table
___ ___
0
Pleistocene
-1 0
-400
-2 0
-600
-800
Quaternary aquifer
-3 0
MIT GHAMR FORMATION.
Miocene
?
-1000
-4 0
Pliocene
-5 0
20
0
20km
6
-6 0
EL WASTANY FORMATION.
-7 0
CONGLOMERATE
COARSE SAND
FINE SAND
___ ___
CLAY ___ ___ SILT
5
0
0
6 Km
5km
-8 0
Sand & gravel
Muddy Layer
Fine Sand
Bentonite
Coarce Sand With Gravels
Medium Sand
YellowCoarse Sand
Green Coarce Sand
Sands
Clays
Water table
Fault plane
Silty clay
Fig. (7): Hydrogeologic cross section along profile (V1-V1’)
(Compiled after Ibrahem et al. 2005).
Fig. (6): Hydrogeologic cross-section in Quaternary aquifer
along profile (L2-L2’) Compiled after Serag El Din, 1983).
2.7.3 Recharge and discharge of the aquifer and relationship between surface water and GW:
The main GW aquifer (Quaternary aquifer) in the study is considered as free aquifer relating to
Pleistocene age and composed of loose quartz sand with pebbles and granules with intercalated thin
clayey beds. The aquifer is recharged mainly by three sources, the seepage from the Nile Delta
aquifer, seepage from fresh water of Ismailia canal, surface irrigation canals and drains and seepage
from agricultural water uses and its fertilizers and Rainfall from desert wadis and from surface run off
falling on shed area to the south. The occurrence of GW is highly controlled by the surface water. The
relationship between GW and surface water is strongly influenced by the following factors, canal or
lake depth, height of the water table relative to the surface and surface water levels, type of sediments
forming the bottom and banks of surface water courses, rate of horizontal and vertical hydraulic
boundary conditions of the GW system and Hydraulic conductivity of the aquifer.
2.8 Hydrogeochemical Studies
2.8.1 General outlines
The hydrogeochemistry at the study area, has been studied by many workers among them Shata &
El Fayoumy (1968), El-Shazly et al., (1975), El Hefny (1980), Sallouma (1983), Geriesh (1989), Gad
(1995), El Sharkawi (2008) and Atwa (2010).
Many ecological changes that occur in water result from human activities includes agricultural,
industrial and municipal wastes (Katz et al., 1969). The liquid wastes and sewage are sometimes
discharged into the River Nile and other water resources. Generally pollution expected from these
sources: seepage from surface polluted irrigation canals , Fig. (8), seepage from agricultural water uses
and its fertilizers refuses disposal sites, Fig. (9), sewer, polluted drains Fig. (10), sewage ponds, septic
tanks (landfill and open dumpsites) and human sources and rainfall on the area of study from rock
wadis and from surface run off falling on shed area to the south.
The study of the hydrogeochemical characteristics of GW aims to recognize the water
characteristics of the aquifer in the study area, reveal the effect of the geologic setting and the running
132
surface water on the GW quality and check the water stability for use for drinking, domestic and
irrigation purposes.
Fig. (8): Public disposal in Canal.
Fig. (9): Public disposal in Drain
Fig. (10): Qalubi Drain gaining wastewater
2.8.1 The hydrochemical Pollution
Pollution is defined as any change in the physical, chemical, or biological conditions of the
environment, which may harmfully affect the quality of human life including effects upon animals and
plants. Environmental pollution represents a major problem in both developed and/ or under developed
countries. Egypt is one of these countries which suffer from high biosphere pollution (air, soil and
water).The water is to be polluted if it contains any chemical constituents in concentration over the
maximum permissible level of the Guideline values average daily intake (ADl) of certain pesticides
(Table 1).
Table (1): The W.H.O. (1983) Guideline values average daily intake (ADl) of certain pesticides.
Compound
DDT
Aldin & Dieldrin
Chordane
Hexachlorobenzene
Lindane
2,4- D
2,4-Dichlorophenoxy acetic acid
Guideline value
1.0
0.03
0.3
0.01
3.0
30.0
100.0
ADI – body weight mg/kg
0.005
0.0001
0.001
-0.01
0.1
0.3
2.8.2 Hydrogeochemical Characters of GW
It will deals with hydrogeochemical studies at the study area as depth and quality of GW for
drinking and domestic uses, quality of GW for livestock and poultry and the hydrochemical pollution.
The W.H.O. (1971) and (1983) guidelines values, international and upper limit values for the drinking
water quality standards are shown in Table (2). Depth to water table ranges between 3.43 m at WDB30 and 6.3 m at W33, while elevation of water table ranges between 2.6 m at WDB-30 and 7.7 at W
33 (Table 3). The water table in the southern portion of the old deltaic plain, i.e. at Zagazig, occurs at
great depth, while it becomes shallower in the northern direction towards the north and east (Sallouma,
1983).
Table (2): The W.H.O. (1971) and (1983) guidelines: for the drinking water quality standards.
Characteristic constituents
PH
Chloride (Cl)
Magnesium (Mg)
Sodium (Na)
Sulphate (So4)
Calcium (Ca)
Total dissolved solids.(TDS)
W.H.O.(1983)
guide line value
6.5- 8.5
250
----------------400
--------1000
W.H.O.(1971)
international standard
7.5- 8.5
200
----------------200
75
500
133
Upper limit of
concentration
6.5- 9.2
600
150
200
--------200
1500
Table (3): The results of depth to water table and elevation for selected boreholes located in figure (5).
Well No.
MES-6
W9
W10
BB-14
MZ-14
Depth to
water(m)
Elevation of water
Table(m)
2.1
4.51
5.08
4.3
3.5
7.9
4.49
2.8
8
7
Well No.
W61
W8
WMES-7
W61
W8
Depth to
water (m)
4.5
5.26
4.18
4.62
5.26
Elevation Of water
Table(m)
4.5
3.
10.8
3.4
3
The direction of GW salinity increasing is from the south (El Nakhas 1070 ppm) towards the south
(El Zawamel 400ppm) with gentle gradient. The water salinity with depth reflects that; the seepage is
from the lower salt aquifer through a good pervious layer of Pleistocene old deltaic deposits (Table 4).
Table (4): Salinity and electric conductivity in aquifer encountered in wells MA-7, MA-61, Mes-6 and Mit
Gaber.
Depth (m)
10
36
60
80
100
MA-7
T.D.S.
E.C.
526
0.85
(ppm) (m.mho)
460
0.82
480
0.82
620
1.05
860
1.38
MA-61
T.D.S.
E.C.
810
1.25
(ppm)
(m.mho)
400
0.85
470
0.75
540
0.86
680
1.088
Mes-6
T.D.S.
E.C.
1005
1.26
(m.mho)
500
0.85
540
0.86
620
1.05
Mit Gaber
T.D.S.
E.C.
1100
1.76
(ppm)
(m.mho)
520
0.85
670
0.8
870
1.6
Groundwater hydrochemistry of the study area is based on the chemical analyses of water samples
collected from 14 bore holes distributed through and around the area. The chemical analysis includes
the measurement of pH (alkalinity), TDS (total dissolved salts), EC (electrical conductivity), total
major cations (Na+, Mg++ and Ca++) and total major anions (Cl-, HCO3- and SO4--). These
measurements are carried out at SHAPWASCO, Table (5), Atwa (2010).
7.6
8
0.9
9
MA-7
Mes-6
BB-14
Location
1.66
SO 4 -- .ppm.
6
HCO3-. ppm.
9
78
Cl-. ppm.
400
Ca++ .ppm.
7.5
Mg+ .ppm.
TDS. ppm.
0.85
Na+ .ppm.
PH
3
S.No.
61
W.n.
EC.m mho
Table (5): Results of Chemical analysis of water samples at the studied area analyzed by The
SHAPWASCO laboratory, Atwa (2010).
24
52
130
230
38.4
Shembara
1070 168
31.2
84
240
340
176
El Nakhas
7.4
584
84
19.2
24
140
140
105.1
Zagazig
1.05
7.5
620
108
4.8
120
180
360
111.6
Bany H|elal
10
0.82
7.5
460
96
33.6
64
160
300
73.6
El Talein
11
0.9
7.5
480
72
14.4
104
120
320
80.4
Minia Alkamh
15
0.65
7.5
490
102
28.8
80
170
400
48
Mashtul Masaken
16
0.95
7.5
500
78
50.4
76
130
300
48
El Sehafa
17
0.65
7.5
360
30
33.6
64
50
300
34
Anshas
134
14
18
0.8
8.5
512
73
12
66
114
244
49
El Zankaloun
23
0.85
7.5
520
45.6
9.6
40
76
140
85
Shobra El nakhla
24
1.6
7.5
870
180
24
72
300
280
29.6
Mit Gaber
25
0.85
7.4
400
120
19.2
40
200
180
38
El Zawamel
26
1.1
7.5
680
216
31.2
56
360
270
111.8
Awlad Seif
2.8.3 Graphical representation of the chemical analysis and hydrochemical salt combinations:
PH Values:
The pH values ranges between 7.4 (El Zawamel) and 8.5 (El Zankaloun). Its distribution map figure
(10) shows that, the alkalinity increases toward southern and eastern parts with gentile gradient. The
water PH lines around canals and drain are irregular and concave in shape which reflect that; the
seepage is from canal to the surrounding lands through a good pervious layer of Pleistocene old deltaic
deposits of the surrounding region (deltaic deposits), where the GW is more deep and fresh water.
The results of chemical analyses show that leaching of salts may cause a change in pH values.
2.8.4 Distribution of Total Dissolved Solids:
Total dissolved solids (T.D.S.) comprise dissociated and undissociated substances in water (Korany
et al. 1997). The T.D.S. contour map (Fig.11) illustrates that low salinity samples occupied the central
and western parts, while the high salinity are concentrated in the northern and the eastern parts. Total
dissolved solids (T.D.S.) ranges between 1070 ppm (El Nakhas with freshwater old deltaic deposits)
and 400 ppm (El Zawamel). The salinity shows gradual increase with depth and reaching about 1070
ppm at depth 80 shown in table (4).
The lines around Ismailia Canal, Moweis canal and Bahr El Bakar drain are irregular and concave
in shape which reflect the seepage from the canals and drain to the surrounding lands through a good
pervious layer of Pleistocene old deltaic deposits. The used evaluation methods show that the water is
generally suitable for drinking, irrigation and industrial usage whereas some samples have
concentrations more than the permission by oxidation (weathering) precipitation and infiltration before
usage.
31° 15'
31° 15'
32° 15'
31° 45'
32° 15'
31° 45'
Manzala
Lake
Manzala
Lake
16
31°
31°
00
31°
00
00
14
31°
00
El Huseiniya
12
Diarb
Nigm IbrahimiaAbu
Kabir
Hihya
a
mh
10
8
Faqus
Abu
Hammad
El Salhiya
A
lq
30°
30
30°
30'
30°
30
Ismailiya Canal
Faqus
Abu
Hammad
El Salhiya
30°
30'
Ismailiya Canal
Mi
na
6
El Huseiniya
Diarb
Nigm IbrahimiaAbu
Kabir
Hihya
4
Mashtul El
Soak
Tenth of
Ramadan
2
30°
0
00
0
31° 15'
2
4
6
31° 45'
8
10
10
Mashtul El
Soak
10 Km
0
12
32° 15'
14
Tenth of
Ramadan
16
30°
00
30°
00
C.I; 0.2
31° 15'
10
31° 45'
0
10 Km
32° 15'
30°
00
C.I; 1000 ppm
Fig. (11): PH Value contour map of the
aquifer of the studied area.
Fig. (12: Iso Salinity (T.D.S.) contour map of the
2.8.5 Electrical conductivity
Electrical conductivity (E.C) is the ability of substances to conduct an electric current. Specific
electrical conductance can be defined as the conductance of a cubic centimeter of water at standard
temperature of 25 oC. The ability of the solution to conduct the current is a function of the
concentration and change of the ions, and the ability of each dissolved ions. Figure 13 shows the pH
values contour map of the aquifer.
135
Specific conductance, is measured in mmhos/cm, and gives results that are convenient as a general
induction of T.D.S. (Todd, 1980). The maximum E.C. (1.66 mmhos / cm) is attained in W-9, while
the minimum is obtained in sample (Enshas: 0.65 mmhos /cm). These values reflect the relation
between the E.C. and T.D.S., where as the electric conductivity of water increase. Figure Fig. 14
presents the contour map for sodium Na+ of the aquifer in the study area.
31° 15'
32° 15'
31° 45'
31° 15'
Manzala
Lake
32° 15'
31° 45'
Manzala
Lake
16
14
31°
00
31°
00
31°
00
El Huseiniya
Diarb
Nigm IbrahimiaAbu
Kabir
Hihya
30°
30
Faqus
Abu
Hammad
31°
00
El Huseiniya
12
Diarb
Nigm IbrahimiaAbu
Kabir
Hihya
10
Faqus
8
El Salhiya
30°
30
30°
30'
El Salhiya
Abu
Hammad
Ismailiya Canal
30°
30'
Ismailiya Canal
6
Mashtul El
Soak
4
Tenth of
Ramadan
30°
00
31° 15'
10
0
Mashtul El
Soak
10 Km
Tenth of
Ramadan
10
0
10 Km
2
31° 45'
32° 15'
30°
00
31° 15'
4
30°
00
C.I; 0.5 mmhos / cm
Fig. (13): PH Value contour map of the
6
8
31° 45'
10
12
14
32° 15'
16
30°
00
C.I; 50 ppm.
Fig. (14): Iso- Sodium (Na+) contour map of the aquifer
of the studied area.
3 FIELD SURVEYING AND INTERPRETATION OF THE MEASURED DATA
3.1 A-Field Surveying And Data Acquisition
Geophysical tools are useful in locating and delineating subsurface aquifers. The electrical
geophysical techniques including 1-D resistivity sounding and 2-D imaging represent the main tools
for mapping subsurface lithofacies and hydrogeochemical conditions and features of the GW aquifer.
Description of the field measurements for each method is given in details. The resistivity
measurements were carried out using SAS 300C system manufactured by ABEM Co., Fig. (18). The
measuring current is selected manually with a maximum of 20 mA.
Fig. (18):SAS-300C resistivity meter during sounding
3.2 Measuring of Resistivity Data: measurements.
3.2.1 Measuring of I-D resistivity data:
During the last two decades, the curve matching technique become obsolete because of the
availability of more computerized techniques (1-D inversion), which are the fastest and more accurate.
However, the curve matchingmeathod might still be used in the absence of computation facilities
during the tie of survey or derive an approximate model that is required as starting model for one of
the iterative modeling techniques. The parameters of a layered sequence can be obtained from the
resistivity transform of the field data using linear filtering theory (Koefoed, 1979), or directly from the
field observations without using its resistivity transform (Zohdy, 1989).
136
3.2.2 Measuring of 2-D resistivity data:
Loke and Barker (1995 and 1996) developed the smoothness-constrained least-squares inversion
(deGroot-Hedlin and Constable, 1990) and produced a fast computer program (Res2dinv) for
inversion of 2-D resistivity and IP data. The procedures of this technique are based on inversion by
quasi- Newton method. The inversion technique of Loke and Braker (1996) is used to invert the
measured 2-D pseudo sections in the present work and can be summarized as follows.
3.2.2.1 1-D Sounding Survey:
A total number of 30 points of 1-D resistivity sounding were executed all over the area. The
measurements are carried out along some selected drains, canals and other pollution sources at some
selected sites. These sounding are carried out to reflect a regional picture about the subsurface
geologic succession and to have an idea about the water bearing formations in the area. The location
of the measured points is marked using GPs positioning. The distributions of these sounding points are
shown in Fig. (19). The electrical sounding is carried out using Schlumberger configurations with
maximum current electrode (AB) spacing of 400 m to explore shallow subsurface conditions.
3.2.2.2 2-D Resistivity Survey:
The 2-D resistivity inversion aims to construct an image of the obtained true subsurface resistivity
distribution and to map the saltwater intrusion within the area of study. The measured resistivity
pseudo sections are 3 profiles at 3 sites located as indicated in Fig. (19). It is inverted using RES2INV
inversion software, version 3.4. The inversion procedures used by this program are based on the
smoothness-constrained least-squares inversion algorithm. The Sequence of measurements is used to
build up a pseudo section in the field (Loke and Barker, 1995); Fig. (20).
31° 30 '
32° 00
37
41
Manzala Lake
42
31
Aw
31°
00
lad
46
qr
Sa
34
68
67
Ka
fr
Sa
54
61
IB-5
25
AK-1
Abu Kabir
53
72
el
et
ny
Mi mh
Qa
64
Hihya
81
52
Bah
r
B
El
aq
ar
Dra
in
45
43
40
66
65
74
75
18
76
51
23
3
14
9
Faqus
58
57
HI-1
26 HI-8
24
22
azig17
Zag
16
30°
30
55
56
IHI-8
20
15
19
62
63
27
91
28
96
6
44
El Huseiniya
59
Ibrahimiya
35
48
36
Z4
50
qr
60
13
31°
00
47
69
33
30
12
11
Diarb
Nigm29
39
49
73
38
7
5
78
El Salhiya
77
Z26"
30°
30 '
Abu Hammad
82
11
10
8
Mashtul el
Soak
Ismailiya Canal
70
83
10
71
BB-1
Studied area
VES Location
79
88
4
80
89
2
87
90
2-D imaging location
96
Z20"
86
10
85
0
10 Km
84
97
Tenth of Ramadan
30°
00
31° 30 '
E7
32° 00
30°
00
Fig. (20): Sequence of measurements used to build up a
pseudo section in the field (after Loke and Barker,
1995).
Fig. (19): 1-D sounding points ( V.E.S.es) and 2-D locations
3.3 B-Interpretation of The Measured Data
3.3.1 Interpretation of 1-D Resistivity Sounding:
The resistivity sounding data, in the form of apparent resistivity and electrode spacing (AB/2), are
interpreted both qualitatively and quantitatively. The results of interpretation have been inspected to
determine the litho-stratigraphic boundaries of subsurface layers and to define the possible waterbearing layers in the area as well as to evaluate the depth to save GW for drinking.
Quantitative interpretation of the field data is carried out to obtain the true resistivity and
thicknesses of subsurface layers using two different techniques, as follows, automatic interpretation
technique of Zohdy (1989), the obtained multi-layer model from Zohdy technique is used as
preliminary 1-D model for IPI2win software, version2.0 (Bobachev et al., 2001).
The obtained results of 1-D modeling are illustrated in columns with the same scales, as geoelectric
horizons and correlated with obtained data from drilled boreholes as exemplified in, Figs. (22 and 23).
137
To derive a resistivity spectrum of the different subsurface formation and reaching a reliable and
acceptable interpretation, the following brief description of the obtained calibration is done:
Sounding No. 95 was conducted beside well number 54 (Fig. 23). The inspection of the V.E.S.
results corresponding to borehole horizon shows that, the first geoelectrical layer has a specific
m and a thickness of 4.2 m. This resistivity is attributed to the near surface clay.
The second geoelectrical layer has specific resistivities of 2.61 mand thickness of 5.67 m, this
resistivity of 3.6
resistivity may be attributed to clay with seepage water. The third
geoelectrical layer has specific
mand thickness of 25 m, this resistivity may be attributed to sandy faces. The
geoelectrical layer of 56.24 m is correlated with the saturated with freshwater gravelly sand in the
resistivities of 23.3
borehole.
Therefore, there is a large discrepancy in the V.E.S. results and the lithological log of the borehole,
which may be attributed to the fact that this area is subjected to compaction to construct zone of
surface water. The increases of compaction and water seepage with depth give low values of
resistivities. On the other hand, the deeper layers show good agreement with the borehole data, Atwa
(2010).
ATO PROGRAM
Appar. Resistivity [Ohmm]
RMS: 2.5 %
Sounding No. 6
RESIST PROGRAM
Current Electrode Distance (AB/2) [m]
Appar. Resistivity [Ohmm]
RMS: 6 %
Fig (22): Geoelectrical horizon
Sounding No. 6
IPI PROGRAM
1-D modeling sounding results
In addition, the interpreted layer parameters of the subsurface layers are listed in Table (6).
Current Electrode Distance (AB/2) [m]
Table (6): Results of computation of layer electric Resistivities and layer thicknesses for the field
measurements. (ρ in ohm.m) (H in meters).
V.E.S.
NO.
1
3
5
6
9
14
19
72
82
83
88
Type
(True Resistivities valuse m)
K-A
H-A
K-A
H-A
H-A
H-A
H-A
K
A-Q
A-Q
A-K
1
4.96
16.6
13.4
3.52
2.93
7.7
4.429
6.33
3
9.8
9.61
2
9.62
11.6
48.2
2.076
2.07
5.41
2.071
7.42
2.26
3.78
3.63
3
12.6
44.7
41.4
17.02
2.82
11.7
20.82
12
5.09
11
10.8
4
46.4
49.2
56.2
47.4
9.62
383
80.72
120
23
53
111
Thickness of layers (m)
5
6
7
58.4
63.1
22.4
56.2
83.6
72.8
94.2 3.03
2.1
2.1
138
H1
4
0.2
1.26
3.37
0.55
1.82
2.73
2.624
4
6
5.9
H2
11
0.9
4
9.63
4
1.8
1.57
2.284
23
11.9
12
H3
6
3.5
7.9
20.9
3.62
3.24
1.18
17.7
10
20
18
H4 H5
31.5
13.7
2.63 61.8
10.4
20
3.3.2 Hydro geophysical Investigation:
In hydro geophysical investigation, many geophysical tools are useful in locating and delineating
subsurface aquifers. The interpreted layer parameters in the form of resistivity spectrum and lithology
of the obtained layers are listed in Table (7).
Table (7) Resistivity spectrum and lithology of the obtained layers in the study area.
Formation
Interpreted Lithology and hydrogeologic
conditions
Resistivity
(Ώm)
Thickness (m)
Belqas Formation Holocene
Surface layer (Agricultural layer)
3- 16.6
1.26-6
deposits
Clayey facies
2.26-48.2
0.9-11.9
Clayey to Sandy facies (Cape rock)
5.09-44.7
1.18-20.9
Sand with gravel
31.4- 383
Mit
Ghamr
Pleistocene deposits
Formation
3.3.2.1 Inversion of 2-D Resistivity Data:
The 2-D resistivity inversion aims to construct an image of the obtained true subsurface resistivity
distribution and to map the saltwater intrusion within the area of study. The measured resistivity
pseudo sections (4 profiles at 4 sites) are inverted using RES2INV inversion software, version 3.4. The
inversion procedures used by this program are based on the smoothness-constrained least-squares
inversion algorithm, which was previously described. The 2-D model used in this program divides the
subsurface into a number of rectangular blocks and the resistivity of the blocks are adjusted in an
iterative manner to reduce the difference between the measured pseudo section and calculated model,
Fig. (24). The resistivities of calculated model are obtained using either the finite-element or finite
difference method.
Fig. (24): The apparent resistivity pseudo section, calculated
model, and 2-D inversion for a Wennar array at
Teheimer site.
4 RESULTS AND DISCUSSION
From the previous calibration of the resistivities with the corresponding lithofacies and
hydrogeochemical conditions, as well as the different geoenvironmental sites in the area of study, it is
observed that the resistivity differs for different lithologies according to the their hydrogeochemicl
conditions. The study area is characterized by shallow freshwater aquifer trough the following
investigations:
1-Hydroresistivity application: 30 sounding points were executed all over the area Fig. (25). The
deduced layer parameters were used to construct 10 geoelectric cross- sections correlated with 8
boreholes at different locations as indicated in Fig. (26).
2-Resistivity application; where different geophysical surveys were applied.
139
Geoelectric resistivity 1-D using vertical sounding (V.E.S.’es) and Schlumberger
configurations with maximum current electrode (AB) spacing of 400m has been carried out to explore
shallow subsurface condition sand zone of pollution.
The interpreted layer parameters in the form of resistivity spectrum and lithology of the obtained
layers correlated with boreholes all over the area of study. Hydrogeochemical and geoenvironmental
application are listed in (Table 11).
3-True resistivity contour maps are prepared by contouring the values of interpreted true resistivities
for different geoelectrical layers, in order to study the lateral and vertical variations of the
resistivities with depth. From the tabulated resistivity values Table, (1), three geoelectrical layers
are mapped in figures 27, 28, 29, 30, 31 and 32).
4-Three 2-D inverted sections are selected along drains, canals and other pollution sources at some
selected sites all over the area of study. (Teheimer, El Nakhas and El Zankaloun) using Wenner
array, Fig. (25).
The constructed sections are useful in defining the subsurface layer distribution, exploring shallow
subsurface conditions and zone of pollution and outlining the extension of the expected aquifer layers.
31° 30 '
32° 00
31° 30 '
32° 00
31°
15 '
37
31°
15 '
41
Z30"
41
37 Z33
Z31
Manzala Lake
42
31
Sector 2
Z34
46
31°
00
34
31°
00
39
49
47
34
Z23
68
67
50
44
45
El Huseiniya
61
DB-30
13
Ibrahimiya
IB-5
35
ZM-17
48
36
91
72
MA-15
MA-7
16
38
El Salhiya
77
Abu Hammad
Z26"
72
30°
30 '
T57
Z11
Z1
Z8
Z9'
79
10
DB-14
E3
BB-1
Studied area
VES Location
Water Smple location
Bore Hole location
4
E2
2
P3
90
89
87
Z20"
86
T7
MES-10
MES-7
MES-5 MES-6
88
30°
15 '
79
85
84
0
Z5
7
AH-6
10
Z14"
BB-1
E2
87
Z20"
T7
T56
Z11"
E7
32° 00
Fig. (25):2-D, V.E.S.es and borehole location
E5
VES Location
Bore Hole location
Resistivity Cross-section
30°
15 '
T56
Z12 97
Ramadan
Z29"
31° 30 '
T57
Ismailiya Canal
89
85
Tenth of
Tenth of Ramadan
E6
Z26"
Z12"
Z21"
Z35"
Sector 396
84
97
30°
00
77
Z15"
T25
4
P3
T56
El Salhiya
78
Z24"
2
Z14
E4
38
Z13
86
74
75
Abu Hammad
71
90
30°
45 '
Sector 1
Z27"
Z10
7
Z19"
E3
Z22"
66 Z18"
76
51
Z28"
80
Z19
10 Km
55
Z28
Z23" Z24
70
DB-14
8
Mashtul el
Soak
E1
10
Z9
Z4'
10
96
Sector 3
Z29
3 Z6'
Z7'
73
5
BB-12
8
FA-1
Z27" 64
65
Z17" Z15
52
11
Z20
Faqus
58
57
AH-3
17
Z3
14
Z2
Z22
MA-27
DB-7
71
80
E1
9
82
83
E5
10
8
ZM-4
MA-15
MA-7
Ismailiya Canal
70
BB-12
8
MES-10
MES-7
MES-5 MES-6
Mashtul el
Soak
78
AH-6
7
Z4'
11
88
T56
E4
3
73
DB-7
83
FA-4
Z33"
Z25"
AK-1
Abu Kabir
53
Z30
Z26
AK-7
56
40
62
Z29"
23
Z34
Z32
45
44
El Huseiniya
63
18
22
17
19
MA-13
Sector 2
50
54
43
HI-5
Z6
6
47
69
68
Z27
61
ZC-9
76
51
AH-3
5
MA-27
74
75
Sector 1
23
Z3
14
9
82
52
18
22
17
ZM-4
30°
30
66
HI-5
Z4
19
30°
45 '
55
65
39 Z18
49
Z25
67
60
Ibrahimiya
Z29 13
IB-5
25
Z16"
35
ZM-19
Z8' ZM-17
IHI-8
27
Z1"91
ZM-2 Z5'
48
Z2'
20
15
HI-1
Z3'
Hihya
Z10' Z7
ZC-18 26 HI-8
81
24
36
28
FA-1
64
81
24
96
MA-13
Faqus
58
57
Hihya
ZC-18 26 HI-8
28
FA-4
AK-1
Abu Kabir
53
HI-1
Z21
11
DB-30
DB-32
AK-7
56
27
20
ZC-9
6
25
Diarb
Nigm29
62
63
IHI-8
ZM-2
15
40
Z34"
59
30
Z31"
Z16
12
43
60
33
Z17
59
54
DB-32
Sector 2
46
69
33
30
12
11
Diarb
Nigm29
Manzala Lake
42
31
Z35
10
0
10 Km
E6
30°
00
31° 30 '
E7
32° 00
Fig. (26): cross-sections, V.E.S.es and borehole location
4.1 The Geoelectric Cross-Section (shallow freshwater aquifer):
The shallow fresh water aquifer includes the geoelectric cross-sections of Markaz El Zagazig and its
surrounding. The aquifer represented by Mit Ghamr Formation. The correlation between 1-D models
30 V. E. S.es, chemical analysis of water samples and 8 boreholes shows resistivity spectrum of the
subsurface litho- hydrogeological units in the studied area and characterized by fresh water aquifer
area table. Positions of different cross sections are shown in table (8). GW level subdivided the second
layer into two resistivity facies, the upper facies represented by low values sandy facie and the lower
facies represented by silty to sandy facies. The resistivity ranges for the upper and lower facies are
shown in Table (9).
Table (8) Positions of different cross sections and corresponding sounding point
Number of Cross
Position
Sounding point included
Section
6, 28, 15 and 35 across the borehole
Z1-Z1
El Talein, El Nakhas, Frsis and El Setohia).
No.9
(Mit Rabiaa, El Zankloun, Gamal Abd El Naser,
9, 19, 21, 95 and 17 across the
Z2-Z2
Maokaf El Mansoura and Manzel Haian).
borehole No. 33
(Mit Habib, Mit Abu Ali, El Aslogy, El Shobak, El
1, 14, 16, 17, 22 and 24 across the
Z3-Z3
Salamoun).
borehole No.10
Z4-Z4
(El Talein, El Znkloun, Mit Abu Ali, Bourdein).
No 14
Z8-Z8
(El Talein, Shembara, Deweida and Setohia).
No.61
(El Sanagra Bourdein, Mit Hbib, Mit Rabiaa and
7, 5, 1, 9 and 6 across the borehole
Z9-Z9
El Talein).
No.8
140
Table (9) The resistivity ranges in the second layer for the upper and lower facies
Number of
Cross
Section
Z1-Z1
Z2-Z2
Z3-Z3
Z4-Z4
GW level subdivided the second layer into two resistivity facies
The upper facies represented by low
The lower facies represented by silty to
values sandy facie and resistivity ranged
sandy facies and resistivity ranged
between
between
2.076ohm.m at V.E.S.6 and 7.36ohm.m
13.1ohm.m at V.E.S. 15 and 17.02ohm.m
at V.E.S.15,
at V.E.S.6.
2.07ohm.m at V.E.S. 9 and 3.85ohm.m
9.62ohm.m at V.E.S.9 to 20.82ohm.m at
at V.E.S.85,
V.E.S.19.
1.69ohm.m at V.E.S.24 and 42ohm.m at
4.64hm.m at V.E.S.16 to 11.7ohm.m at
V.E.S V.E.S.16
V.E.S.14.
2.07ohm.m at V.E.S.14 and 48.2 ohm.m
11.7 ohm.m at V.E.S.14 and 41.4 ohm.m at
at V.E.S.5,
V.E.S.5.
There was variety of resistivity values in the four layers for each cross section. Table (10) shows the
depths of the four layers and the range of resistivity values in each cross section. The deduced layer
parameters are used to construct 10 geoelectric cross- sections at different locations and directions as
indicated in Fig. (26) to Fig (32).Correlation between salinity distribution in the layer and the variation
of salinity are shown in Table (11).
141
Table (10) specific resistivity and layers thickness for different cross section
Number of
cross section
Range in
Thickness
Z1Z1
Specific
Resistivity
Range in
Thickness
Z2Z2
Specific
Resistivity
Range in
Thickness
Z3Z3
Specific
Resistivity
Range in
Thickness
Z4Z4
Specific
Resistivity
Range in
Thickness
Z8Z8
Specific
Resistivity
Range in
Thickness
Z9Z9
Specific
Resistivity
Layer 1
Holocene
riverine dry clay
to clayey silt and
sand range
0.298 m at
V.E.S. 35 and
2.51 m at V.E.S.
28
3.526 ohm.m at
V.E.S.6 and 9.26
ohm.m at
V.E.S.15.
0.595 m at
V.E.S. 21 and
2.73 m at V.E.S.
2.49ohm.m at
V.E.S.9 and
86.1ohm.m at
V.E.S.21
1.8 m at
V.E.S. 16 and 5.5
m at V.E.S. 1.
2.01ohm.m at
V.E.S. 24 and
42ohm.m at
V.E.S.16.
1.26 m at
V.E.S.5 and
2.442 m at V.E.S.
19.
3.526ohm.m at
V.E.S.6 and
13.4 ohm.m at
V. E. S.5.
0.298 m. at
V.E.S. 35 and
2.89 m. at V.E.S.
48.
3.52 ohm.m
at V.E.S. 6 and
7.66 ohm.m. at
V.E.S. 48.
0.554 m at
V.E.S. 9 and 5.5
m at V.E.S. 1.
2.93 ohm.m
at V.E.S. 9 and
13.4 ohm.m. at
V.E.S. 5.
Layer 2
Holocene Riverine
(Nile ) clay, silty
clay and silt
2 m. at V.E.S.28
and 4.05 m at
V.E.S.35.
2.076 ohm.m at
V.E.S.6 to 7.36
ohm.m at V.E.S.15.
1.57 m at V.E.S. 19
to 3.37 m at V.E.S.
85 1.57 ohm.m at
V.E.S.19 to 6.24
ohm.m at V.E.S.21.
-------------------------
4.64 ohm.m at
V.E.S.16 and 9.62
ohm.m at V.E.S.1.
Layer 3
Pleistocene
sands
Layer 4
Pleistocene
gravely and
coarse sand
--------------
-------------------
ohm.m at
V.E.S.6.
13.1ohm.m and
17.4 ohm.m
-----------------
47.4 ohm.m at
V.E.S. 6 and 197
ohm.m at
V.E.S.28.
----------------
7.08 ohm.m at
V.E.S. 27 to
20.82 ohm.m at
V.E.S.19.
8.91 ohm.m at
V.E.S.16 and
35.4ohm.m at
V.E.S.24.
8.91 ohm.m to
9.3 ohm.m
46.4 ohm.m at
V.E.S. 27 to 94.8
ohm.m at V.E.S.
21.
------------------
2.435 m at V.E.S.19
and 2.8 m at V.E.S.
14
----------------
31.6ohm.m at
V.E.S.16 and 383
ohm.m at
V.E.S.14
--------------------
2.07 ohm.m at
V.E.S.19 and
5.41ohm.m at
V.E.S.14.
1.69 m. at V.E.S. 36
and 3.14 m. at
V.E.S. 35.
11.9 ohm.m
atV.E.S.5 to
22.9 ohm.m at
V.E.S.6,
-----------------
47.4ohm.m at
V.E.S.6 and 383
ohm.m at V.E.S.
14.
---------------------
2 ohm.m at V.E.S.
16 and 6.81 ohm.m
at V.E.S. 35.
13.6 at V.E.S.
35 and 35.6
ohm.m at V.E.S.
6.
2.63m at V.E.S.
9 and 22.99m at
V.E.S. 6.
50.1 ohm.m at
V.E.S. 35 and 147
ohm.m at V.E.S.
48.
-------------------
12.6 ohm.m at
V.E.S. 1 and
48.2 ohm.m at
V.E.S.
32.5 ohm.m
at V.E.S. 7 and
63.1 ohm.m at
V.E.S. 9.
1.64 m. at
V.E.S. 7 and
25.541 m at V.E.S.
6.
2.82 ohm.m at
V.E.S. 9 and 48.2
ohm.m at V.E.S. 5.
142
Fig. ( 30): The Geoelectric Cross-Section Z4-Z4".
1
Fig. ( 32): The Geoelectric Cross-Section Z9-Z9"
Table (11) correlation between specific resistivity and salinity distribution in different cross section
No. of Section
Z2-Z2
Z3-Z3
Z4-Z4
Correlation between resistivity and TDS confirmed that
the Pleistocene sands represents the upper aquifer of underground water and the static water level measured at depth of 3.9 m.
the expected connection between drain water zone and clay zone.
the Pleistocene sands represents the upper aquifer of underground water and the static water level measured at depth of 4.62 m.
2
Z8-Z8
a connection between seabage water and underground water (increasing resistivity from 2.56 ohm.m for upper facies to 6.81 ohm.m .
3
4.2 True Resistivity Contour Maps
True resistivity maps are prepared by contouring the values of interpreted true resistivities
for different geoelectrical layers, in order to study the lateral and vertical variations of the
resistivities with depth. From the tabulated resistivity values Table, (1), four geoelectrical
layers are mapped in figures 33, 34, 35 and 36). Consideration of these maps shows that;
1-The north and eastern parts Zagazig , of the studied area is graded from low resistivity
values of clays and sandy clays to medium values of moisture to partially saturated sands,
while some localities of dry surface layers due to presence of drains is represented by high
resistivity values as El Aslogy. The developed low resistivity anomaly may be due to
decreasing in the percent of gravels in this local part.
2-The southern part is occupied by high resistivity values at layer 1 of dry sand, which is
shifted toward the west at layer 2. This anomaly is graded to medium values at layer 4 of
saturated gravelly sands.
3- Depth 1m. is represented by high resistivity values at layer 1 of dry sand and presence of
drains , which is shifted toward the west. This anomaly is decreased at depth 5m Fig. (33)
as the effect of seepage water and fertilizers. This anomaly is graded to medium values at
10m Fig. (34) of saturated gravelly sands. The developed low resistivity anomaly may be
due to decreasing in the percent of gravels in this local part of buried channels.
4- Groundwater resistivity is characterized by depths 36m and 46m which low grade variation
in values Figs. (35 and 36). The anomaly graded to medium values towards north and east
is in well agreement with T.D.S. contour map Fig. (12).
31° 15'
31° 15'
32° 15'
31° 45'
32° 15'
31° 45'
Manzala
Lake
Manzala
Lake
16
14
31°
00
31°
00
31°
00
12
31°
00
El Huseiniya
El Huseiniya
Diarb
Nigm IbrahimiaAbu
Kabir
Hihya
10
Diarb
Nigm IbrahimiaAbu
Kabir
Hihya
Faqus
Faqus
8
30°
30
6
Abu
Hammad
El Salhiya
30°
30'
30°
30
Ismailiya Canal
Abu
Hammad
El Salhiya
30°
30'
Ismailiya Canal
4
Mashtul El
Soak
2
Tenth of
Ramadan
30°
0
00
31° 15'
0
2
4
6
10
31° 45'
8
10
Mashtul El
Soak
10 Km
0
32° 15'
12
14
Tenth of
Ramadan
16
30°
00
30°
00
31° 15'
C.I; 10 Ohm.m
0
10 Km
32° 15'
31° 45'
Fig. (34): True resistivity Contour Map at Depth 10 m.
31° 15'
32° 15'
31° 45'
32° 15'
31° 45'
Manzala
Lake
Manzala
Lake
31°
00
31°
00
31°
00
31°
00
El Huseiniya
El Huseiniya
Diarb
Nigm IbrahimiaAbu
Kabir
Hihya
30°
30
Diarb
Nigm IbrahimiaAbu
Kabir
Hihya
Faqus
Abu
Hammad
El Salhiya
30°
30
30°
30'
Faqus
Abu
Hammad
El Salhiya
Mashtul El
Soak
Mashtul El
Soak
Tenth of
Ramadan
31° 15'
30°
30'
Ismailiya Canal
Ismailiya Canal
30°
00
30°
00
C.I; 10 Ohm.m
Fig. (33 ): True resistivity Contour Map at Depth 5 m.
31° 15'
10
10
0
31° 45'
Tenth of
Ramadan
10 Km
32° 15'
30°
00
30°
00
31° 15'
31° 45'
10
0
10 Km
32° 15'
30°
00
C.I; 20 Ohm.m
C.I; 20 Ohm.m
Fig. (35):True resistivity Contour Map at Depth 36 m.
Fig. (36):True resistivity Contour Map at Depth 46 m.
4.3 2-D resistivity imaging:
Four 2-D inverted sections are obtained along the selected locations using Wenner array.
1
Site 1 is located eastern side of El Qaliubia drain at Teheimer village sector 1 Fig. (37). Along
the profile, a well defined low resistivity zone of 0.865 to1.91 ohm.m is observed at a depth of 6.38 m
and corresponds to the fresh and brackish water as indicated by the drilled borehole. The lower aquifer
boundary defined by a layer continuing less saline water. The depth to fresh water and saline water
boundary is increased in the western part (drain direction passing with) to reach maximum value of
12.4 m at spacing 25 m to reflect more thickness of polluted water at that place. It should be noticed
that the dry zone near drain of increasing resistivity is in well agreement with 1-D sounding 16.
Fig. (37 ): 2-D Wenner inverted image eastern side of El Qaliubi Drain at Teheimer
village.
Site 2 is located in El Nakhas village sector 1, Fig. (38). Along the profile, a well defined low
resistivity zone of 0.958 to15 ohm.m is noticed at a depth of 6.38 m and corresponds to the fresh and
brackish water as indicated by the drilled borehole. The lower aquifer boundary is defined by a layer
continuing less saline water. The depth to fresh water and saline water boundary is increased with
depth to reach maximum of 12.4 m at spacing 25 m and 120 to reflect more thickness of polluted
water at that places. It should be noticed that the lower fresh water aquifer zone of increasing
resistivity is in well agreement with 1-D sounding 28.
Fig. (38): 2-DWenner inverted section inside of El Nakhas village area
Site 3 is located in El Zankaloun village sector 1, Fig. (39). Along the profile, a well defined low
resistivity zone of 0.958 to59.6 ohm.m can be noticed that depth of 6.38 m and corresponds to the
fresh and brackish water as indicated by the drilled boreholes. The lower aquifer boundary is defined
by a layer containing less saline water. The depth to fresh water and saline water boundary is increased
with depth to reach maximum value of 12.4 m at spacing 25 m and 120 m to reflect more thickness of
polluted water at that places. It is observed that the lower fresh water aquifer zone of increasing
resistivity is in well agreement with 1-D sounding 19.
Fig. (27): 2-DWenner inverted section inside of El Znkaloun village.
2
Fig. (39): 2-DWenner inverted section inside of El Nakhas village area
4.5 PROPOSED TREATMENT METHODS
The results of the resistivity maps in the one and two dimensions indicated that the salinity values is
very high so the primary treatment should be taken into account to reduce the BOD of the incoming
wastewater. The experience of the first author with this treatment method proved that the use of the
primary treatment method reduces the BOD by 20-30% and the reduces the total suspended solids by
some 50-60% . The use of the secondary (biological) treatment is important to remove the suspended
solids. It is removal efficiency is about 85% of the suspended solids. The BOD can be also removed
by a well running plant with secondary treatment. Also, the tertiary treatment can remove more than
99 percent of all the impurities from sewage, producing an effluent of almost drinking-water quality as
shown in Table (12). The additional costs due to use of Tertiary treatment for different types of station
are tabulated in Table (13).
Table (12). Chemical analysis of effluents and permitted to freshwater.
Type Analysis
TDS
T. S. S.
C.O.D.
H2S
B.O.D
T.C.F/100ml
Raw water Analysis
1092
440
640
10
410
20000
Primary
Effluent
987
105
280
3
183
12000
Secondary Effluent
797
18
24
0.4
16
4200
Tertiary
Effluent
677
2
0
0
0
1000
Table (13). Original cost of some treated stations and suggesting adding values for tertiary treating at
Minia Alqamh, Sharkia Governorate, Egypt.
Treated water station
Shalshalamoun
Algodeida
Shembara
Atallein
Original Cost
pounds
710000000
67000000
71000000
26000000
Designal Productive quantity
m3/day
Suggesting adding value
for tertiary treating
20000
15000
15000
5000
2000000
1800000
1800000
1000000
5 SUMMARY AND CONCLOSION
The study area of the present paper lies to the eastern part of Nile Delta. The present study assesses
the GW in some selected areas in Minia-Alqamh district and locates the potential sources for GW
pollution, based on the available land use data and by using, the geoelectric resistivity survey. The
geoelectric resistivity are carried out and interpreted in the form of apparent and true resistivity maps,
geoelectric cross sections and integrated models. The final models are based on the results of
integration of resistivity measurements and data of both hydro-geological and chemical analysis.
The results of the six geological cross sections showed that the quaternary aquifer consists of four
layers. The first layer presented by Holocene riverine dry clay to clayey silt and sand range (3- 16.6
Ώm), the second layer presented by Holocene Riverine (Nile) clay, silty clay and silt(2.26-48Ώm).
The third layer presented by Pleistocene sands (5.09-44.7Ώm) while the fourth layer presented by
Pleistocene gravely and coarse sand (31.4- 383Ώm). The GW level subdivides the second layer into
two resistivity facies, the upper facies is represented by low values sandy facie (Belqas Formation
Holocene deposits ) and the lower facies is represented by silty to sandy facies. (Mit Ghamr
Formation). The results of the present research indicate that;
-
Very high conductive anomalies in the top 4-12 m of the subsurface.
3
-
-
The groundwater in the study area is subject to a potential pollution from the surface waste
from surface pollution sources such as: sewer, polluted drains, sewage ponds, septic tanks and
refuse disposal sites and human sources.
The values of the BOD and the total suspended solids are very high and exceeding the
allowable values, so the primary treatment and biological treatment should be included in the
water treatment plants to reduce their concentration in the wasted water before it finds its way
to the drain and after that to the groundwater.
6 RECOMMENDATIONS
-
-
Improper land waste disposal within the drains has negative impacts on the quality of
the groundwater at the studied area. Therefore, landfill sites should have secured lines
so that the groundwater resources left in a potable condition.
The tertiary treatment is highly recommended to remove impurities from sewage,
producing an effluent of almost drinking GW quality.
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6

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