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Eighteenth International Water Technology Conference, IWTC18 Sharm ElSheikh, 12-14 March 2015

158

HYDROCHEMISTRY AND EVALUATION OF GROUNDWATER

SUITABILIRY FOR IRRIGATION AND DRINKING PURPOSES IN WEST

EL- MINIA DISTRICT, NORTH UPPER EGYPT

Esam Ismail, Rafat Zaki, Ali Kamel

Geology Department, Faculty of Science, Minia University, Egypt

[email protected]

ABSTRACT

Since the quantity and quality of water available for irrigation in Egypt is variable from

place to place. Groundwater quality in west El-Minia district, north Upper Egypt was evaluated for

its suitability for drinking and irrigation purposes by collecting 88 groundwater samples. Pleistocene

aquifer represents the main aquifer in the study area and it is composed of sands and gravels of

different sizes, with some clay intercalations. The quality assessment was made by estimating pH,

electrical conductivity, total dissolved solids, and hardness, besides major cations (Ca2+

, Mg2+

, Na+,

and K+) and anions (HCO

3-, Cl

-, and SO4

2-). As well as, irrigation quality parameters were calculated,

i.e., sodium absorption ratio, Na %, residual sodium carbonate, concentration of boron, total

hardness, and permeability index. The groundwater samples were categorized as Ca(HCO3)2 water

type, and the hydrochemical classification shows that, most of the studied water samples are

meteoric origin. The results indicate that most of the collected water samples are suitable for

drinking and irrigation purposes.

Keywords: Pleistocene aquifer, Hydrogeochemistry, major ions, El-Minia district. Irrigation uses.

1 INTRODUCTION

In arid region like Egypt, groundwater is the important source of water. The availability and

quality of groundwater resources have been affected by activities and projects associated with rapid

development. Groundwater preservation and protection measures have been generally overlooked in

the majority of the practices (Shaibani 2008).

Since groundwater is intensively used for irrigation and drinking purposes, an effort is made

in the current paper to discern the hydrogeochemistry of groundwater and to classify the water in

order to evaluate its suitability for municipal and irrigational/ agricultural use. The quality of

groundwater for different uses was studied by, C. Delgado et al. (2010), S. Lecina et al. (2011), and

P. Ravikumar and R. K. Somashekar (2011), Fakhre Alam (2014), Moneer S. Khashogji and Magdy

M. S. El Maghraby (2013), M. K. Fattah (2012) and Mohamed Saber et al. (2014).

The area under investigation is located between latitudes 27° 30É and 28° 65Ń and

longitudes 30° 30É and 31° 10Ń, ~ 260-150 km south of Cairo, west El Minia district, northern

Upper Egypt (Fig.1). The area reaches about 32.279 km2 width and about 135 km length.

The study area is characterized by an arid climate with evaporation rate of 4897.91 mm/year

(Korany et al. 2008). Mean annual rainfall for the last 15 years ranged from 23.05 to 33.15 mm/year.

The average temperatures in winter ranges from 5° to 20°c with the maximum one about 42°c in

summer. The mean monthly relative humidity during daytime ranged from 62% in May to 29% in

December (Korany 1984).


159

Fig. (1): Location map of the study area

MATERIALS AND METHODS

A total of 88 groundwater samples were collected during 2013 in the study area (Fig. 1). The

water samples were collected from well pumps after a pumping period of at least one hour and

transferred into pre-cleaned polyethylene bottles. Electrical conductivity, pH, temperature, and total

dissolved solids (TDS) for the collected water samples were measured in the field immediately after

sampling. Complete chemical water analyses were carried out during winter season at the Central

Health Laboratories, Abdein, Cairo, Egypt.

Based on the physico-chemical analyses, irrigation quality parameters, i.e., boron, sodium absorption

ratio (SAR), %Na, residual sodium carbonate (RSC), noncarbonated hardness, and permeability

index were calculated. The correlation of the analytical data has been attempted by plotting different

graphical representation such as those of Eaton (1950), Richards (1954), Todd (1959), Gibbs (1970),

Piper (1994), and Wilcox (1995), to determine the classification of groundwater and suitability for

different purposes by ascertaining various factors on which the chemical characteristics of water

depend. The suitability of the groundwater sources for drinking, domestic, and irrigation purposes

was evaluated by comparing the values of different water quality parameters with water quality

guidelines for human drinking and domestic uses (Egyptian Higher Committee for water, 2007) and

those of the World Health Organization (2004).

GEOLOGY AND HYDROGEOLOGY


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Locally, the stratigraphic sequence of the study area is built up from base to top (Zaki et al.

2001) as; Middle Eocene limestone intercalated with shale; Pliocene undifferentiated sands, clays,

and conglomerates; Plio-Pleistocene sand and gravel with clay and shale intercalations; Pleistocene

sand and gravel with clay intercalations; and Holocene silt and clay.

The Nile valley displays three geomorphologic units are: the young alluvial plain, which is

composed of modern Nile silt and clay sediments; old alluvial plain underlain by mixed sands,

gravels, and rock fragments; and the structural limestone plateau.

The Quaternary aquifer represents the main aquifer in the study area and composed of massive

cross-bedded fluvial sand with gravel and clay sediments and rests directly on the Pliocene clay

and the fissured Eocene limestone. Generally, the thickness of this aquifer decreases gradually

towards the Eocene plateau and hydraulically connected with the underlined Eocene aquifer

through many faults (Sanad, 2010). This aquifer is recharge mainly from the surface water,

particularly through the irrigations canals, which play a main role in the configuration of the water

table. The discharge of this aquifer takes place during the evaporation process. The depth to the

groundwater (water table) of Pleistocene aquifer varies from one locality to another and ranges

from 0.9 m to 8 m. The water level of the Pleistocene aquifer ranges between 29.4 m at the

northern part and 43 m at the southern ones.

RESULTS AND DISCUSSION

Physico-chemical parameters of the studied groundwater samples are presented in Tables (1 & 2)

and indicated that the values of pH varies from 7.4 to 8.2 of a slightly acidic nature and all the

samples within the permissible limit of 6.5–8.5 (BIS, 1998).

Table (1): Analytical results of groundwater samples in the study area

Sample

ID

Temp.

(°C) pH

TD

S

pp

m

EC

µs/cm

Major cations Major anions TH

pp

m

Total

alkalinity

ppm Ca

2

+

Mg2+

Na

+

K+ HCO3

- SO4

2- Cl

- NO3 PO4

1 27.5 7.8 450 675 38 19 20 2.6 217 8 26 0.06 0.02 260 275

2 30.5

7.6 660 990 73 25 28 8 350 1

6 40 0.05 0.08 360 370

3 27.8

7.9 530 795 80 35 45 8 450 2

0 46 0.07 0.04 320 350

4 29.3

7.9 580 870 76 26 25 4 380 1

6 40 0.03 0.09 340 400

5 30.6

7.9 670 100

5 68 26 48 8 360

1

6 56 0.12 0.02 380 430

6 27.4 7.6 630 945 44 22 20 2.6 250 8 26 0.04 0.03 320 420

7 27.8

7.6 600 900 70 26 25 4 390 1

6 40 0.05 0.02 290 350

8 30.2

7.8 100

0

150

0 105 60 82 10 360

1

6 56 0.03 0.04 570 430

9 30.2 7.6 220 330 22 12 20 2.3 150 5 15 0.05 0.07 145 130

10 28.9

7.9 460 690 40 20 27 2.6 240 1

0 26 0.14 0.01 250 230

11 28.4

7.8 695 104

3 53.4 25 25 4.3 210

1

6 36 0.1 0.13 400 320


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Table (2): Continuous

12 27.8

8.1 630 945 66 26 34 3.6 340 1

4

42 0.02 0.01 350 290

13 29.8 7.8 382 573 30 18 28 2.6 210 8 26 0.05 0.01 190 180

14 30.0 7.6 272 408 28.6 12.4 19 2 173 4 17.5 0.29 0.11 160 140

15 27.4

7.6 402 605 56 20 32 3.2 289 1

2

36 0.05 0.05 280 200

16 27.4

8.1 600 902 84 28 35 9 420 1

5

40 0.15 0.18 340 290

17 27.4

8.0 660 992 95 40 50 8

520 2

0

55 0.22 0.22 350 450

18 27.9

7.9 600 903 76 26 25 4 380 1

6

40 0.32 0.032 370 420

19 28.4

7.7 405 608 57 21 32 3.2 290 1

2

36 0.04 0.01 290 270

20 27.9

7.4 460 692 62 24 34 3.6 318 1

4

42 0.262 0.12 310 260

21 30.3

8.1 640 960 88 30 34 8 440 1

5

42 0.392 0.03 410 320

22 29.2

8.0 620 932 52 25 36 8 300 1

7

42 0.214 0.23 420 310

23 24.9

7.9 492 740 58 30 42 8 350 2

2

46 0.042 0.12 280 260

24 28.0

8.1 630 946 45 22 40 4 308 1

0

30 0.05 0.02 360 300

25 27.9 7.7 222 335 21.6 11.8 20 2.3 148 5 15 0.162 0.032 150 145

26 27.4 7.8 420 632 60 23 32 3.2 310 14 38 0.05 0.13 210 185

27 27.6 8.0 497 746 59 30 43 8 350 22 46 0.04 0.04 250 330

28 26.8 7.8 416 625 30 18 20 2.6 195 8 26 0.06 0.11 230 200

29 28.8 7.8 371 557 36 20 27 2.8 222 8 30 1.55 0.18 200 195

30 27.6 7.9 477 716 42 20 34 3.6 245 14 36 0.08 0.12 250 390

31 28.1 7.9 410 616 70 24 32 3.2 340 12 40 0.03 0.19 220 205

32 28.4 7.9 409 615 66 20 30 3.2 310 12 40 0.34 0.13 260 230

33 28.8 7.8 400 602 76 26 36 3.4 375 12 42 0.45 0.12 250 210

Sample

ID

Temp.

(°C) pH

TDS

ppm

EC

µs/cm

Major cations Major anions TH

ppm

Total

alkalinity

ppm Ca2+

Mg2+

Na+ K

+ HCO3

- SO4

2- Cl

- NO3 PO4

45 28.5 7.9 346 520 40 18 26 2.6 230 8 24 0.16 0.08 230 195

46 29.5 7.8 300 450 36 16 26 2.6 215 8 23 0.08 0.07 210 185

47 27.8 8.1 420 630 67 21 30 3.2 320 12 36 0.18 0.06 300 280

48 28.3 8.1 550 826 54 22 28 3.4 290 12 30 2.78 0.09 400 350

49 29.3 7.9 320 480 37 18 26 2.6 225 8 23 0.07 0.07 210 185

50 28.4 7.6 580 870 58 24 28 3.6 310 12 33 0.67 0.03 410 460

51 28.8 8.0 493 740 40 20 26 2.6 246 8 24 0.26 0.04 340 430

52 30.5 7.8 350 526 40 22 26 2.6 255 8 25 0.06 0.06 230 210

53 28.2 7.7 280 422 22.8 9 20 2.1 138 6 15 0.67 0.08 160 145

54 28.9 8.1 650 975 46.5 23.4 32 3.2 285 10 36 0.23 0.09 405 420

55 27.4 8.1 505 758 48 23 20 3 270 7 25 0.16 0.07 330 280

56 28.8 7.9 376 565 37 21 22 2.6 230 8 26 0.25 0.09 200 185

57 27.8 8.2 708 1063 44 24 33 3.8 294 10 32 0.47 0.09 406 340

58 29.0 7.8 400 600 47 28 28 3 298 12 28 0.34 0.19 230 200


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The electrical conductivity (EC), varies widely and ranges from 316 and 2193 µs/cm and lies within

the permitted limit (BIS, 1998). TDS of groundwater samples are ranging between 210 and 1460

ppm, with an average of 835 ppm (Tables 1 & 2) and 98% of these samples have TDS less than 1000

ppm, reflect the fresh water type and the rest are slightly saline (above 1000 ppm).

Water hardness is caused primarily by the presence of cations such as calcium and magnesium and

anions such as carbonate, bicarbonate, chloride, and sulfate in water. Total hardness of the collected

samples is ranging from very hard (90%) and hard water (10%). The high levels of total hardness

reflect the high dissolution of limestone.

The Ca ion is the cation composition of the groundwater, while the anion is HCO3 dominated. This

chemistry resulted from the rock water interaction and anthropogenic impact. The main water types

are Ca (HCO3)2.

The relation between the different major ions could be studied through the determination of the ion

ratios. The expression of the ionic relationship in terms of mathematical ratio is quite helpful for

establishing the chemical similarities among water, representing a single geologic terrain or single

aquifer (rNa+ /rCl). The collected samples have ratio ranging from 1 to 2.42, with an average 1.71,

and the increasing is due to the impact of marine salts on the groundwater composition, dissolution,

ion exchange process and also may attributed to the addition of sodium salts of terrestrial origin to

the water. Furthermore, the rNa / rCl ratio is always above unity and indicate that, Na+ has been

enriched and the origin of this groundwater is meteoric. (rSO4--/rCl

-) are ranging from 0.13 to 0.67,

with an average 0.4, this indicate that the groundwater is less than unity and reflected the abundance

of halite (NaCl) in the aquifer deposits (Sulin, 1946 and Hounslow, 1995). (r Ca++

/ rMg++

) are

ranging from 0.99 to1.98 with an average 1.49, and the higher values are due to presence of gypsum,

59 28.4 7.9 580 872 58 30 30 3.6 345 10 35 0.54 0.12 360 300

60 28.9 8.0 530 796 46 27 27 3 290 11 27 0.07 0.11 340 420

61 27.6 7.6 215 323 32 19 22 2.8 210 7 21 0.12 0.09 170 160

62 27.0 7.7 280 422 28 12 24 2.8 168 8 22 1.67 0.19 210 190

63 28.4 7.8 340 512 32 18 22 3 200 7 24 0.42 0.17 190 180

64 28.9 7.8 419 630 38 18 30 3.2 244 8 26 0.45 0.10 260 280

65 29.3 7.7 320 482 27 14 26 3 180 8 22 0.77 0.09 200 190

66 28.2 8.1 620 932 62 36 34 4 390 11 38 2.34 0.24 380 360

67 26.9 8.0 530 796 46 27 27 3 290 9 28.5 0.55 0.09 340 300

68 29.0 7.9 470 706 52 26 21 2.6 282 12 32 2.35 0.54 320 280

69 28.9 8.2 730 1096 72 36 35 4.8 410 14 45 0.46 0.47 470 380

70 28.4 7.9 600 902 56 26 28 3.6 315 8.5 34 0.68 0.78 420 480

71 26.6 7.9 450 676 68 30 28 3.2 380 8 27 0.02 0.02 230 195

72 26.8 7.8 460 692 64 32 32 3.2 310 10 35 0.35 0.03 250 220

73 29.8 7.8 580 872 42 24 20 2.6 265 8 20 0.54 0.07 320 350

74 28.6 7.9 500 752 70 32 32 3.2 395 9 36 0.47 0.09 340 300

75 27.1 8.0 230 346 28 14 20 2.2 180 4 18 0.58 0.08 170 160

76 27.4 8.1 790 1186 46 28 28 3.2 286 12 34 0.46 0.56 480 410

77 29.8 7.9 460 692 40 22 28 2.8 250 8 28 0.47 0.09 260 210

78 29.9 8.1 820 1230 80 40 38 5 470 12.5 42 0.69 0.87 520 450

79 28.1 8.2 1460 2193 150 74 52 12 850 19 70 0.96 0.08 780 650

80 29.0 8.0 610 916 28 12 19 2.3 160 7.5 20 0.26 0.63 380 360

81 28.5 7.9 750 1126 76 38 35 4.8 450 10 34 0.69 0.14 400 320

82 28.5 7.6 230 346 32 18 20 2.8 210 6..5 19 0.86 0.03 190 180

83 27.7 8.2 1060 1592 100 52 46 8 585 19 52 3.68 0.01 680 430

84 27.8 7.9 250 376 30 16 20 2.2 190 5 18 3.46 0.03 220 200

85 28.7 8.1 610 916 28 12 19 2.3 160 6.5 20 0.55 0.09 320 280

86 27.6 8.1 600 902 45 26 22 2.8 284 8 20 0.44 0.08 330 380

87 30.3 7.9 480 722 72 36 28 4 410 6.5 36 0.68 0.07 280 240

88 29.6 8.0 750 1128 76 38 35 4.8 450 13 35 0.87 0.1 400 360


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anhydrite and calcite dissolution. This also referred to the dissolution of calcium carbonate that

originated from the limestone.

Piper's diagram (Fig. 2) shows that all the studied samples are located inside the sub-area (1), reflects

the water type is Ca (HCO3)2, as well as meteoric origin

Fig. (2): Piper trilinear diagram

EVALUATION OF WATER QUALITY FOR DRINKING

Generally, drinking water has to be free from colour, specific taste, turbidity, and excessive amounts

of dissolved salts. The groundwater samples in the context of international standards for human

drinking water and the Egyptian Committee for Water (2007). It is clear that the majority of the

collected samples (98%) are suitable for drinking due to their low levels of salinity (<1200 ppm) and

also the major ions within the permissible limits. The remaining samples (2%) are unsuitable due to

their high salinity (1200 ppm to 1460 ppm).

Evaluation of water quality domestic and industrial purposes

In determining the suitability of groundwater for domestic and industrial purposes, hardness is an

important criterion, as it is involved in making the water hard. Water hardness has no known adverse

effects; however, it causes more consumption of detergents at the time of cleaning, and some

evidence indicates its role in heart disease (Schroeder, 1960). The total hardness (TH) in ppm (after


164

Todd, 1980; Hem, 1985 and Ragunath, 1987) was determined by following Eq. TH = 2.497 Ca2+

+

4.115 Mg2+

According to Hem (1985), the studied samples (Table 3), shows that 90% of samples are very hard

and 10 % are hard water.

Table (3): Hardness water classification according to Hem (1985).

Water type classification Groundwater%

Soft 0-60 mg/l as CaCO3 --------------

Moderately 61-120.mg/l as CaCO3 --------------

Hard 121-180mg/1asCaCO3 9 samples10%

Very hard >180 mg/1 as CaCO3 79 samples 90%

GROUND WATER QUALITY FOR IRRIGATION

Water quality, soil types and cropping practices play an important role for a suitable irrigation

practice. Excessive amounts of dissolved ions in irrigation water affect plants and agricultural soil

physically and chemically, thus reducing productivity. The physical effects of these ions are to lower

the osmotic pressure in the plant structural cells, thus preventing water from reaching the branches

and leaves. The chemical effects disrupt plant metabolism. Water quality problems in irrigation

include indices for salinity, sodicity (Mills, 2003) and alkalinity. The important chemical

constituents that affect the suitability of groundwater for irrigation can be utilized to verify the

suitability, are as follows:

• Salinity index or salinity hazard or total concentration of soluble/dissolved salt as computed by

measured EC values.

• Sodicity index or sodium hazard or relative proportion of sodium to other principal cations as

expressed by SAR.

• Sodium hazard expressed as a percent of sodium as a total cations (%Na).

• Bicarbonate hazard or bicarbonate (HCO3) concentration as related to the concentration of calcium

plus magnesium such as RSC and RSBC.

• Boron hazard (concentration of boron or other elements) that may be toxic.

• Permeability index (PI)

SALINITY INDEX

The groundwater samples have been classified according to Bauder et al. (2007), Table (4). The

samples are categorized under good quality to permissible quality. About 51% of the samples belong

to good quality category and 49% one is permissible quality.

Table (4): Classification of water samples based on E.C

EC (μS/cm) Water salinity range Collected

samples%

< 250 excellent quality --------


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The salinity index of the groundwater samples was computed using the measured electrical

conductivity value. The studied samples exhibit low to moderate salinity (classes 1 and 2), which are

not considered very harmful to soils or crops, whereas those exhibiting high salinity (class 3) are

suitable for irrigation, which are medium and high salt-tolerant crops. High salinity water (class 4) is

suitable for irrigating high salt-tolerant crops; however water of salinity class 5 or above is generally

unsuitable for irrigation. All the collected groundwater samples are categorized in classes 1–3, which

are suitable for irrigation (Fig. 3).

Fig. (3): Salinity index of groundwater samples

SAR OR SODICITY INDEX

Another important factor for water quality is the sodium concentration to express the reactions with

the soil and know the reduction in its permeability. High sodium-deposits waters are generally not

suitable for irrigate the soils and higher sodium may deteriorate the soil characteristics.

SAR values according to Bauder et.al. (2007) show that, the samples lie below excellent water

values and <10 % are classified as excellent for irrigation (i.e., S1 category). The sodicity index was

calculated using the SAR; with water up to class 2 are generally considered to be suitable for

irrigation and used for the classification of the groundwater samples. Based on the sodicity index, all

the samples belong to class 0 (Fig. 4).

251–750 good quality 51%

750 –2000 permissible quality 49%

2001–3000 Doubtful --------

>3000 Unsuitable --------


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Fig. (4): Sodicity index for the studied samples

SALINITY HAZARD

The total concentration of soluble salts (salinity hazard) in irrigation water can be expressed in terms

of specific conductance. The salinity hazard shows that the majority of the studied samples are

located in classes C2 and C3. A more detailed analysis for the suitability of water for irrigation can

be made by plotting the sodium absorption ratio and electrical conductivity data on the US Salinity

Laboratory (USSL) diagram (Richards 1954), Fig. (5). According to this classification the

groundwater samples of the Pleistocene aquifer is excellent for irrigation purpose.


167

Fig. (5): Wilcox diagram of the studied samples

PERCENT SODIUM

Wilcox (1995) and Richards (1954) methods are used to classify and understand the basic character of

the chemical composition of groundwater, since the suitability of the groundwater for irrigation

depends on the mineralization in water and its effect on plants and soil. Percent sodium can be

determined using the following formula:

Na% = (Na + K) * 100 (epm)

(Ca+ Mg+ Na+ K)

When the concentration of sodium is high in irrigation water, the sodium ions tend to be absorbed by

clay particles, displacing Mg2+

and Ca2+

ions. This exchange process of Na+ in water for Ca

2+ and

Mg2+

in soil reduces the permeability and eventually results in soil with poor internal drainage.

Hence, air and water circulation is restricted during wet conditions, and such soils become usually

hard when dry (Saleh et al., 1999).

Wilcox (1948) classified the groundwater for irrigation purposes by correlating the percent of

sodium (i.e., sodium in irrigation waters) and the electrical conductivity. The samples in figure 6

show that the 51 % are good quality and 49% are permissible quality.


168

Fig. (6): Percent sodium vs. EC plot (after Wilcox, 1995)

RESIDUAL SODIUM CARBONATE

In addition to the SAR and Na %, the excess amount of carbonate and bicarbonate in groundwater, as

well as the amount of calcium and magnesium are influence the suitability of groundwater for

irrigation. RSC is calculated followings (Eaton, 1950 and Ragunath, 1987);

RSC = (CO3 + HCO3) – (Ca + Mg) (epm)

The groundwater having RSC > 2.50 epm is not suitable for irrigation purposes. The samples have

RSC less than 2.5 indicate suitability for irrigation.

THE CONCENTRATIONS OF BORON (B)

Boron is essential in plant nutrition and sometimes added to fertilizer in small amounts because some

soils in humid region are deficient in boron. If boron is excess with small amount over the needed

amount is toxic to some types of plants. Some plants are most sensitive in agriculture, so, an excess

of boron in irrigation water is harmful, however, some fruits such as lemon or orange trees, citrus

and walnut trees are toxic concentration, where concentration is low of 1.0 mg/l. The majority of the

samples of the Pleistocene aquifer are suitable for irrigation of all crops.

PERMEABILITY INDEX (PI)


169

The PI values also indicate suitability of groundwater for irrigation, as the soil permeability is

affected by long-term use of irrigation water, influenced by the Na+, Ca

2+, Mg

2+, and HCO

−3 contents

of the soil. Doneen (1964) and Ragunath (1987) evolved a criterion for assessing the suitability of

water for irrigation based on PI, and groundwater can be classified as classes 1, 2, and 3. The

concentrations are reported in mille equivalents per liter.

The PI calculated as follows:

PI =Na ± HCO3 ∗ 100

Ca + Mg + Na + K

According to the permeability index values of Doneen’s chart ( Domenico and Schwartz, 1990; Fig.

7), all the samples fall under class 1 and reflect suitability for irrigation purposes.

Fig. (7): Doneen (1964) classification for irrigation water based on the permeability index

MECHANISMS CONTROLLING GROUND WATER CHEMISTRY

Lastly, to know the groundwater chemistry and the relationship of the chemical components of the

groundwater to their respective aquifers, such as the chemistry of the rock types, the chemistry of

precipitated water, and the rate of evaporation, Gibbs (1970) has suggested a diagram in which the

ratio of dominant anions and cations are plotted against the value of TDS. The chemical data of the

collected groundwater samples are plotted in the Gibbs diagram (Fig. 8), and show that the majority

of the samples suggested that the chemical weathering of rock-forming minerals are influencing the

groundwater quality through the dissolution of the host rock.


170

Fig. (8): Gibbs diagram of groundwater samples

CONCLUSIONS

The Quaternary aquifer represents the main aquifer in the study area, the thickness of this aquifer

decrease gradually towards the Eocene plateau and hydraulically connected with the underlined

Eocene aquifer through the faults. This aquifer is mainly recharged from the surface water, and the

discharge takes place during the evaporation process. TDS of the collected water samples reflect the

fresh water type. Total hardness is range from very hard to hard water. The main water type are Ca

(HCO3)2. The majority of the collected samples are suitable for drinking due to their low levels of

salinity and the major ions within the permissible limits.

The suitability of groundwater for irrigation was evaluated based on the irrigation quality

parameters, i.e., boron, SAR, Na %, RSC, and permeability index. Among these parameters, SAR is

excellent for irrigation. Na% shows that half of samples are good quality and the other one is

permissible quality for irrigation uses. According to boron concentration and permeability index all

the collected samples are suitable for irrigation. Based on Gibbs diagram, the majority of the samples

suggested that the chemical weathering of rock-forming minerals are influenced the groundwater quality

through the dissolution of the host rock.

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Agricultural Water Management 97 (2010) 1423–1433

Domenico, P. A. and Schwartz, F. W. (1990): Physical and chemical hydrogeology. New York:

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171

410–420

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