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Ministry of Higher Education and Scientific Research University of Baghdad College of Science Department of Geology
Hydrogeology and Hydrochemistry of Groundwater
in Tuz Khurmatu area
A THESIS SUBMITED TO THE COLLEGE OF SCIENCE UNIVERSITY OF BAGHDAD, IN PARTIAL FULFILMENT
OF THE REQUIREMENTS FOR THE DEGREE OF MASTER OF SCIENCE IN
GEOLOGY (HYDROGEOLOGY)
By Arjan Ali Rasheed
B. Sc. 2000
Supervised
By Prof. Dr. Qusai Yaseen Al-Kubaisi
2012 / April 1433
وزارة التعليم العالي والبحث العلمي جامعة بغداد
كلية العلوم قسم علم األرض
هيدروجيولوجية وهيدروكيميائية
المياه الجوفية في منطقة طوزخورماتو
رسالة مقدمة إلى كلية العلوم - جامعة بغداد
كجزء من متطلبات نيل درجة ماجستير/ هيدروجيولوجيفي علوم األرض
من قبل أرجان علي رشيد
2000بكالوريوس علوم
بإشراف أ.د ياسين الكبيسيقصي
1433 2012نيسان/
ولم ير ألذين كفروا أن ألسموات أ
ضآألرا ومهتقا ففتقنكانتا ر
اءالم نا ملنعجو ءيكل ش
يؤمنون حي أفال العظيم العليا صدق
30 /االنبياء
Supervisor’s Confirmation
I certify that this thesis was prepared under my supervision at the University of
Baghdad as a partial requirements for the degree of Master of Science in Geology
(Hydrogeology).
Signature:
Name: Dr. Qusai Yaseen Al-Kubaisi
Title: Professor
Address: Department of Geology
College of Science ,University of Baghdad
Date: / / 2012
In view of the available recommendations. I forward this thesis for debate by
the Examining committee.
Signature:
Name: Dr. Ahmad Sh. AL-Banna
Title: Professor
Address: Head of Geology Department
College of Science, University of Baghdad
Date: / / 2012
Confirmation of Examining Committee We the members of examining committee , certify that after reading this thesis
entitled (Hydrogeology and Hydrochemistry of Groundwater in Tuz
Khurmatu area ) and examining the student in its contents, we think in our
opinion it is adequate with standing as a thesis for degree of Master of Science in
Geology (Hydrogeology).
Approved by the council of College of Science .
Signature: Name: Dr. Moutaz A. Al-Dabbas Title: Professor Address: Department of Geology College of Science University of Baghdad Date: / / 2012 (Chairman)
Signature: Name: Dr. Ayser M. Al-Shamma'a Title: Professor Address: Department of Geology College of Science University of Baghdad Date: / / 2012 (Member)
Signature: Name: Dr. Hassan H. Salman Title: Professor Address: College of Science University of Al-Mustansiriyah Date: / / 2012 (Member)
Signature: Name: Dr. Qusai Y. Al-Kubaisi Title: Professor Address: Department of Geology College of Science University of Baghdad Date: / / 2012 (Supervisor)
Signature: Name: Dr. Saleh M. Ali Title: Professor Address: Dean of College of Science. University of Baghdad Date: / / 2012
DEDICATION
DEDICATION
To my father's remembrance
To my darling mother with my love
To my children ,my wife and my sister
To all those who love me
With my love and respect
Arjan…
ACKNOWLEDGMENT
Acknowledgment At the final stage of thesis writing . I would like to express my deepest gratitude
and thanks to my supervisor, Prof. Dr. Qusai Y. Al-Qubaisi for his guidance
, fruitful suggestions , constructive criticism and support through all stages of
work. Also, my high gratitude to all members of the Geology Department
- University of Baghdad. I would like to thank Dr. Salman Z. Khorshied for his
guidance and help.
I would like to express my sincere thanks and appreciation to the General
Commission for Groundwater represented by the general director Mr. Dhafir
Abdullah Hussein for his continuous support to simplify the difficulties .I am
grateful to the Expert, Dhia Bashoo, to support and follow-up my research , also
my thanks for all staff of the chemical laboratory .
I would like to thank my colleagues the staff of the Branch of Kirkuk for wells
drilling for helping me by providing data and apparatuses for the field work , and
my great thanks go to my friends Jawdat Abdul Jalil for helping me in computer
programs and providing me by resources and Sabah Ahmed Khorshid for his help
during the field work.
I am very grateful to my friends Hazem Karim and Arshad Wahab for their
assistance and continuous support during the study and research periods .
Finally , I would like to extend my thanks to everyone who helped me to
complete and write this thesis with my love and respect.
Arjan…
ABSTRACT
ABSTRACT The studied area is located within Salahadden governorate between latitudes
(34°50'00" - 34° 55' 00") and longitudes ( 44° 33' 00" - 44° 40' 00" ) south of
Kirkuk city by about ( 70 km) with an approximate area of (124km2). The
important geological formations in the area consist of Tertiary deposits
(Al-Fat'ha, Injana , Muqdadiya and Bai- Hassan formations) as well as recent
Quaternary deposits which cover the study area . Depending on the climatic data
recorded in Tuz Khurmatu station for the period (1991- 2010) the common
climate in the area is humid to moist. The studied area is located within
AL-Adhaim basin whose area is about (12000km2). The productive
hydrogeological unit in the studied area is Bai - Hassan Formation. The general
direction of groundwater flow is from northeast towards southwest and the
hydraulic gradient (I) average is (0.0068). By using Theis recovery (1935) and
Jacob's (1948) methods pumping test results which performed in (7) wells that
penetrate Bai - Hassan Formation partially without observation wells indicated
a transmissivity of median value of ( 176.11 m2/day) and hydraulic conductivity of
median value of ( 3.06 m/day) .
The groundwater quality is generally of low alkalinity . (EC ) and (TDS)
averages and the concentrations of Cations and Anions for the wet period are
lower than the dry period except bicarbonate ion(HCO3-) due to the dilution
process . No nitrate pollution. Depending on (TDS) values the groundwater in the
area is classified as slightly-brackish water . Hardness of water is of very hard
type. The groundwater in the study area is polluted with some heavy elements like
(Co, Ni, Cd and Pb) because their concentrations are higher than the permissible
limits according to WHO (2007) and IQS(2009).
Most wells in the study area have water type of (Na2SO4), and the other
wells range between (NaCl) ,(CaCl2),( CaSO4) and (MgSO4) water type for the
two periods. The average of hydrochemical indicators for the two periods show
that groundwater origin is from meteoric water except the wells No.(1,2,8,9,13,20)
ABSTRACT
which are of marine origin due to existence of a deep recharge . According to
Piper's classification the groundwater in the study area belongs to
(Ca2+ - Mg2+ - Cl- - SO4
2- ) and (Na+- K+ - Cl- - SO4
2-) hydrochemical facies for the
two periods . Comparing the quality of groundwater with standards for different
uses proved that it is unsuitable for human drinking purposes and industrial
purposes but it's suitable for animals watering ,building purposes and for growing
most types of crops . It's admissible as irrigation water except some samples which
are poor due to high salinity. Through the groundwater management , the annual
recharge amount for Al-Adhaim basin is (1660.56 × 106 m3/ year), while the
groundwater amount that enters the study area as renewed storativity is
(9.79 × 106 m3/ year). The amount of consumed groundwater in the area during
present study is (2.96 ×106 m3/year). So the amount of change in the groundwater
storage (ΔS ) will be (6.83 × 106 m3 / year) . This value reflects an increase in
the constant storage of the area .
LIST OF CONTENTS
Page No. Title Paragraph Chapter One
Introduction and Geology of study area 1 Introduction 1.1 1 Location of study area 1.2 2 Aims of study 1.3 2 Previous studies 1.4 5 Methods of work 1.5 5 Office work 1.5.1 5 Field work 1.5.2 6 Laboratory works 1.5.3 7 Geology of the study area 1.6 7 Stratigraphy 1.6.1 10 Tectonic and structural setting in the study area 1.6.2 10 Topography and geomorphology of the study area 1.6.3
Chapter Two Climate and Hydrogeology
12 Climate 2.1 12 Temperature 2.1.1 12 Rainfall 2.1.2 15 Evaporation from class (A) pan 2.1.3 15 Relative humidity 2.1.4 16 Wind speed 2.1.5 17 Sunshine duration 2.1.6 18 Potential Evapotranspiration (PE) 2.2 20 Water Surplus (WS) and Water Deficit (WD) 2.3 23 Classification of Climate 2.4 25 Hydrogeology of the studied area 2.5 28 Groundwater movement and recharge 2.6 30 Hydraulic aquifers properties 2.7 30 Hydraulic conductivity (K) 2.7.1 31 Transmissivity (T) 2.7.2 31 Storage coefficient (Sc) 2.7.3 31 Pumping tests analysis 2.8 32 Cooper-Jacob method 2.8.1 32 Theis recovery equation 2.8.2 33 Analysis results of pumping test 2.9 35 Specific Capacity (SC)
2.10
Page No. Title Paragraph Chapter Three
Hydrochemistry 37 Introduction 3.1 38 Accuracy 3.2 38 Physical properties 3.3 38 Temperature 3.3.1 39 pH 3.3.2 40 Total Dissolved Solids (TDS) 3.3.3 43 Electrical Conductivity (EC) 3.3.4 46 Chemical properties 3.4 46 Cations 3.4.1 46 Calcium (Ca+2) 3.4.1.1 47 Magnesium (Mg+2) 3.4.1.2 47 Sodium (Na+) 3.4.1.3 48 Potassium (K+) 3.4.1.4 48 Anions 3.4.2 48 Bicarbonate(HCO3
⁻ ) and Carbonate (CO₃⁻²) 3.4.2.1 49 Sulfate (SO4
2-) 3.4.2.2 50 Chloride (Cl-) 3.4.2.3 50 Total Hardness (TH) 3.5 52 Nitrate (NO3
-) 3.6 52 Heavy elements ( Trace elements) 3.7 53 Iron (Fe) 3.7.1 53 Cobalt (Co) 3.7.2 54 Nickel (Ni) 3.7.3 54 Copper (Cu) 3.7.4 55 Zinc (Zn) 3.7.5 55 Cadmium (Cd) 3.7.6 56 Lead (Pb) 3.7.7 57 Manganese (Mn) 3.7.8
Chapter Four Groundwater Classification and Management
59 Hydrochemical formula and water type 4.1 59 Hydrochemical Formula (Kurolov formula) 4.1.1 61 Hypothetical salts 4.1.2 63 Hydrochemical indicators 4.1.3 65 Classification of water 4.2 65 Piper Classification (1944) 4.2.1 68 Chadha classification (1999) 4.2.2 71 Groundwater suitability for different purposes 4.3
Page No. Title Paragraph 71 Groundwater suitability for human drinking purposes 4.3.1 73 Groundwater suitability for livestock purposes 4.3.2 74 Groundwater suitability for industrial purposes 4.3.3 75 Groundwater suitability for building purposes 4.3.4 75 Groundwater suitability for agriculture purpose 4.3.5 77 Groundwater suitability for irrigation purposes 4.3.6 81 Suitability of water for irrigation according to US Salinity
Laboratory classification , Richards diagram (1954) 4.4
84 Groundwater management 4.5
Chapter Five Conclusions and Recommendations
90 Conclusions 5.1 95 Recommendations 5.2 96 References
Appendices I Names and Locations of samples wells of the study area Appendix 1 II Well test data and results Appendix 2
XVI Physical properties of water samples of study area for wet and dry periods
Appendix 3
XVII Concentrations of Cations and Anions of the water samples of study area for dry period by( ppm)
Appendix 4
XVIII Concentrations of Cations and Anions of the water samples of study area for wet period by ( ppm)
Appendix 5
XIX
Concentrations of Cations and Anions by (epm) and the accuracy of the results of the water samples of study area for dry period
Appendix 6
XX
Concentrations of Cations and Anions by (epm) and the accuracy of the results of the water samples of study area for wet period
Appendix 7
XXI Trace elements concentrations in water samples of study area by ( ppm)
Appendix8
XXII Hydrochemical formula and water type for dry period water samples
Appendix 9
XXIII Hydrochemical formula and water type for wet period water samples
Appendix 10
XXIV Hypothetical salts for water samples of study area for dry and wet period
Appendix 11
XXV Hydrochemical indicators of water samples of the study area for dry and wet period
Appendix 12
LIST OF FIGURES
Page No. Title Figures 3 Location and Topographical map for the study area 1.1 9 Geological map of the study area modified from (Barwary
and Selwa,1995) 1.2
11 Tectonic map of Iraq (After AL-Kadhimi et al., 1996) 1.3 13 Average monthly temperature for the period (1991-2010)
of Tuz Khurmatu meteorological station. 2.1
14 Average monthly rainfall for the period (1991-2010) of Tuz Khurmatu meteorological station.
2.2
15 The average annual rainfall for the period (1991-2010) of Tuz Khurmatu meteorological station.
2.3
16 Average monthly evaporation for the period (1991-2010) of Tuz Khurmatu meteorological station
2.4
16 Average monthly relative humidity for the period (1991-2010) of Tuz Khurmatu meteorological station.
2.5
17 Average monthly wind speed for the period (1991-2010) of Tuz Khurmatu meteorological station.
2.6
17 Average monthly sunshine for the period (1991-2010) of Tuz Khurmatu meteorological station.
2.7
18 Relationship between different of the climatic variables 2.8 22
The relationship between monthly averages of rainfall (P)and corrected potential evapotranspiration, shows water surplus(WS), and the water deficit (WD)for the study area.
2.9
26 Main aquifers and aquifer groups of Iraq (After Alsam et al., 1990)
2.10
28 The stratigraphic correlation between the wells in the studied area
2.11
29 The flow net of the study area 2.12 34 Locations of the pumping wells in the studied area 2.13 35 Relationship between specific capacity and drawdown 2.14 39 Location of water samples wells in the study area 3.1 42 Spatial distribution of TDS in the studied area
(Dry period) 3.2A
42 Spatial distribution of TDS in the studied area (Wet period)
3.2B
45 EC - TDS relationship of ground water samples in the studied area (Dry period )
3.3
46 EC - TDS relationship of ground water samples in the studied area (Wet period)
3.4
Page No. Title Figures 62 Water quality of the study area (Dry period) 4.1A 62 Water quality of the study area (Wet period) 4.1B 66 Piper (1944) Trilinear diagram with Langguth (1966)
classification. 4.2
67 Piper diagram for water samples of study area (Dry period) 4.3A 67 Piper diagram for water samples of study area (Wet period) 4.3B 69 Chadha diagram 4.4 70 Chadha classification (1999) for water samples of study
area (Dry period) 4.5A
70 Chadha classification (1999) for water samples of study area (Wet period)
4.5B
83 Diagram for classification of irrigation water of the study area ( After US Salinity Laboratory staff ,1954)
4.6
LIST OF TABLES
Page No. Title Tables 6
Methods of analysis that are used to determine Physical and Chemical properties for Tuz Khurmatu groundwater samples
1.1
13
Monthly averages of the climate elements for the period (1991-2010) of Tuz Khurmatu meteorological station.
2.1
20
Corrected potential evapotranspiration values by Thornthwaite method for the period (1991-2010) of Tuz Khurmatu meteorological station.
2.2
22 Monthly averages of water surplus (WS) and water deficit (WD) for Tuz Khurmatu meteorological station.
2.3
23 Climate classification, according to Kettaneh and Gangopadhyaya(1974)
2.4
24
Climate classification depending on values of yearly dryness treatment (Al-Kubaisi, 2004), (A-I.1 and A-I.2)
2.5
25
Climatic classification for the period (1991- 2010) of Tuz Khurmatu meteorological station according to Kettaneh and Gangopadhyaya(1974)
2.6
36
Results of hydraulic properties values by two methods used in single well pumping test analysis for wells of the study area
2.7
39 The temperature values of water samples of the studied area
3.1
Page No. Title Tables 40 The pH values of water samples of the studied area 3.2 40 The TDS values of water samples of the studied area 3.3 41 Classification of water salinity according to (TDS) in
(ppm). 3.4
43 Percentage Test (T%) (Nordstrom,et al,1989) 3.5 44 The EC values of water samples of the studied area 3.6 44 Relationship between electrical conductivity and water
mineralization (Detay, 1997). 3.7
45 The (T %) values for TDS measured and calculated of the water in the study area
3.8
46 The Ca+² concentration of water samples of the studied area
3.9
47 The Mg+2 concentration of water samples of the studied area
3.10
48 The Na+ concentration of water samples of the studied area
3.11
48 The K+ concentration of water samples of the studied area 3.12 49 The HCO3
⁻ concentration of water samples of the studied area
3.13
49 The SO42- concentration of water samples of the studied
area 3.14
50 The Cl- concentration of water samples of the studied area
3.15
51 The TH concentration of water samples of the studied are 3.16 51 Classification of water according to total hardness. 3.17 52 The NO3
- concentration of water samples of the studied are
3.18
58 Standards specifications for trace elements in natural waters.
3.19
60 Predominant salts of water samples in the study area 4.1 61 The reaction order of the hypothetical salts 4.2 61 Average of hypothetical salts values for water samples of
study area 4.3
64 Average of hydrochemical indicators of water samples for the two periods
4.4
72 Comparison of groundwater samples (ppm) in the study area with IQS and WHO standards.
4.5
73 Water specifications for the purpose of animal consumption according to (Altoviski,1962 )
4.6
73 Water specifications for the purpose of animal consumption according to (Crist and Lowery, 1972)
4.7
Page No. Title Tables 74 Water specifications for the purpose of animal
consumption according to (Ayers and Westcot,1989). 4.8
75 Suitability of water for industrial purposes (Hem, 1985). 4.9
76 Water suitability for building purposes compared with average concentrations of samples according to (Altoviski ,1962)
4.10
76 Todd classification (2007) for the tolerance of crops by relative salt concentrations for agriculture
4.11
79 Specification standards for irrigation waters, (Ayers and Westecot, 1989).
4.12
80 Values of (SAR, Na%, RSC) for water samples in the study area
4.13
80 Classification of Don (1995) for irrigation waters 4.14 81 Classification of irrigation water based on RSC values,
according to (Turgeon, 2002) 4.15
82 Type of irrigation water according to U.S. salinity Laboratory at Hem (1989) classification
4.16
Chapter One Introduction and Geology of study area
1
Chapter One Introduction and Geology of study area
1.1 Introduction
In recent decades the groundwater became one of the most important natural
resources as a result of increasing water demand and decreasing rainfall amount
and surface water supplies . It became very necessary to find groundwater that
have high quantity , reachable ,and good quality specially when use as a drinking
water.
Tuz Khurmatu area is one of the most important areas due to its location on the
main express way linking the northern provinces with middle and southern
provinces. In addition to that ,the study area is considered an important agricultural
area and it contains several quarries of sand and gravel as well as bricks and
gypsum factories. In spite of the existence of surface water sources represented by
Tuz Chai river (Aqso river) and the main irrigation channel (Kirkuk irrigation
canal) but water problems still exist because these sources become semi seasonal
due to barriers built by farmers up stream and the general decreasing in surface
water resources. Beside surface water, Tuz Khurmatu area depends on ground
water from the wells distributed in the area ; therefore it's necessary to make
evaluation of groundwater in the area, and its suitability for different purposes
(human drinking , livestock, industrial, agriculture and irrigation purposes).
1.2 Location of study area
The studied area (Tuz Khurmatu) is located within Salahadden governorate
east of Tikrit city by about (90km) , northeast of Baghdad city . The lowest
elevation in the area reaches (200m) a.s.l., and highest elevation reaches
(245m)a.s.l. near the anticline (Fig.1.1).It lies south of Kirkuk city by about (70
km), between latitudes (34°50'00" - 34° 55' 00") and longitudes ( 44° 33' 00" - 44°
40' 00" ) with an approximate area of (124km2).
Chapter One Introduction and Geology of study area
2
1.3 Aims of Study
Evaluation of the hydrogeological conditions to determine the hydraulic
properties of groundwater aquifer in study area.
Studying the hydrochemical characteristics and evaluation of the quality of
groundwater in the area .
Study of groundwater suitability for different purposes and an attempt to
arrange a groundwater management for the area.
1.4 Previous Studies
Macfadynae (1955 ) ,studied the different water resources in Iraq (surface and
subsurface ).
Parsons Company(1955), made a hydrogeological study of Al-Adhaim basin
,including a comprehensive survey for the dug and pipe wells and springs
distributed in the area .In addition, groundwater quality has been evaluated and
its suitability for different uses are studied.
Araim and Ahmed (1980), prepared a groundwater regional study in the Al -
Adhaim basin with emphasis on the plain area, (GEOSURV Baghdad), the aim
of the study to determine the hydrogeological characteristics of aquifers in
study area.
Sogiria (1981) , made a hydrological study of Kirkuk and northern part of Al
Adhaim basin. The study aimed to determine the hydrological circumstances,
the groundwater levels and the effects of the canal on the groundwater quality.
Dijla General Company for irrigation studies(2000), prepared a hydrogeological
study of Daquq and Tuz Khurmatu areas .The study aimed to determine the
hydrogeological characteristics of aquifers and groundwater quality in study
area.
AL-Mamuri (2005), studied the optimal management of surface water and
groundwater in AL-Adhaim basin. The study showed a rise in water table result
of goods irrigation project Kirkuk has been addressed using wells pumping.
Chapter One Introduction and Geology of study area
3
Fig. 1.1 : Location and Topographical map for the study area.
Studied area
Chapter One Introduction and Geology of study area
4
The State Company of Geological Survey and Mining (2005), prepared a
hydrogeological and hydrochemical study of Samarra quadrangle sheet
(NI-38-6) ,which included the study area . The study aimed to determine
geological and hydraulic characteristics of the water bearing layers ,direction of
groundwater movement and evaluation of groundwater and its suitability for
different uses in the area .
Abdul Razak et al. (2007), made a hydrogeological study of the upper Adhaim
basin, and indicated the existence of two hydrogeological systems; confined
(Bai Hassan) and unconfined (Quaternary). The recharge is achieved by rain
and the branches of the Adhaim river. Similar movement of groundwater for
both systems trend from northeast towards the southwest and south. Water
quality with carbonate and sulphate are prevailing .
AL-Rubaii (2008), studied the hydraulic properties of groundwater aquifer in
Tuz Khurmatu area by the application of electrical resistivity . The study aimed
to determine the hydraulic properties of water bearing sediments (groundwater
aquifer) such as porosity, transmissivity, hydraulic conductivity, specific yield ,
specific retention, storage coefficient and specific capacity through the analysis
of the vertical electric sounding and the analysis of the pumping test results
with the use of the chemical analysis of some wells drilled in the area .
Al-Hamdani (2009), studied the hydrochemical effect of groundwater due to
irrigation and drainage projects in Tawuq sub-basin (south of Kirkuk ) ,which
included the study area. The purpose of the study is to know the pollutants
sources, their amounts, and their changes from one season (high water season)
to another (low water season ) by study the hydrochemical characteristics of
water wells, springs , rivers, valleys , irrigation and drainage channels and
evaluation the suitability of water for different purposes.
Chapter One Introduction and Geology of study area
5
1.5 Methods of Work
1.5.1 Office work:
Before starting field work:
Preparing the topographical map of the study area with a scale of 1:100 000
(Fig. 1.1 ).
Collecting available geological and hydrogeological information about the
studied area.
Collecting and reviewing references and previous studies about the studied area.
Preparing archival climatic data about the studied area depending on the
meteorological station in Tuz Khurmatu for the period (1991- 2010) because the
station was established in the year 1991.
Rock Ware Aq.QA software (V 1.1.5.1) 2006(Computer program):The
spreadsheet for water analyses, used to draw hydrochemical graphs.
1.5.2 Field work
A reconnaissance field trip was made to locate the water sampling points for
the wells in the study area.
The GPS (Global Positional System) was used to determine the locations
(Longitude, Latitude and height a.s.l.) for each well (appendix 1) .
The water samples were collected from (20) wells in two periods; the first
period during of September (2010) which represent the dry period, and the
second period was during March(2011) which represent the wet period ( Fig.
3.1) and (appendix 1).
Plastic bottles of one liter size were used to collect water samples after washing
for twice by samples water in order to avoid the contamination.
The acidity (pH),electrical conductivity (EC),total dissolved salt (TDS)and
temperature (C°) of the water samples were measured direct in the field by
using HANA (HI9811-5) apparatus (appendix 3) .
The static levels of wells water were measured by well sounder set.
Chapter One Introduction and Geology of study area
6
The single well pumping test was carried out for two wells within the studied
area and also water level recovery in the two pumping wells were recorded ;
these wells are represented by W1 and W2 and shown in Fig.(2.12).
1.5.3 Laboratory Works
The laboratory works include the physical and chemical analysis of water
samples .The major and minor elements analyses were made in the chemical
laboratory of the General Commission for Groundwater, while analyses of trace
elements were made in the service laboratory in the chemistry department, College
of Science, University of Baghdad. These analyses aim at determining the
concentration of cations (Ca2+, Mg2+, Na+, K+) and the anions (HCO3-, SO4
2-, Cl-),
Nitrate (NO3-) and trace elements (Fe, Co, Ni, Cu, Zn, Cd, Pb and Mn) in addition
to (pH, TDS and EC). Methods of analysis for the different parameters are shown
in the table (1.1).
Table (1.1) Methods of analysis that are used to determine
Physical and Chemical properties for Tuz Khurmatu groundwater samples.
Parameter Methods of analyses
Na+ , K+ Flame photometer (APHA,1998)
Ca2+, Mg2+ Titration with EDTA (Ethylene Diamine Tetracitic Acid)
Cl- Technicon a utoanlyzer instrument (APHA,1998)
SO42- Technicon in ultra violet spectra photometer (U.V)
HCO3-, CO3
2- Technicon in volumetric
NO3- UV-Spectrophotometric method ( λ =500 nm)
pH pH – meter EC Conductivity – meter ( Boyd,2000)
TDS Drying , in 105 C°( Boyd,2000)
Trace or heavy elements
Atomic absorption spectrometer / GBC 933 plus
Chapter One Introduction and Geology of study area
7
1.6 Geology of the Study Area
1.6.1 Stratigraphy
The important geological formations in the area consist of Tertiary deposits
(Al-Fat’ha, Injana , Muqdadiya and Bai- Hassan Formations) as well as recent
Quaternary deposits cover the study area. Al-Fat’ha Formation appears in Pulkhana
anticline and affect the groundwater salinity in the area because of the evaporates
rocks (gypsum rocks) it contains (Mohamed et al,2009) :
1- AL-Fatha Formation (L.Fars). (M. Miocene)
AL-Fatha formation is one of the most aerially widespread and economically
important formation in Iraq (Buday,1980).This formation appears in Pulkhana
anticline in the study area ( Fig. 1.2).The sediments of this formation are cyclic and
each geologic cycle is composed of anhydrite , gypsum, claystone, limestone,
sandstone and marl . The environment of deposition is semi closed coastal areas
(lagoons)( Barwary and Selwa,1995). The gypsum layers are regarded as a
separation boundary between Al-Fatha and Injana Formations (Kassab and
Jassim, 1980).
2- Injana Formation (M.&U. Fars). (U. Miocene )
The age of this formation refers to two periods , late Miocene and Pliocene .The
Injana Formation (including the middle Fars) comprises fine grained pre-molasse
sediments deposited initially in coastal areas (lagoons) and later in a fluvial
lacustrine system (Buday,1980).The formation is characterized by consecutive
beds of sandstone and claystone; few lenses of limestone and gypsum appear on
the lower part of the formation(Jassim and Goff, 2006).Most of these units
demonstrate the phenomenon of cross bedding, which indicate the environment of
deposition in shallow water (Al-Ansari,1987).The thickness of the formation is
very variable, the maximum thickness of the formation is 900m was measured near
Kirkuk (Jassim et al., 1984) .
Chapter One Introduction and Geology of study area
8
3- AL-Mukdadyia Formation(L. Bakhtiari).(L. Pliocene)
This formation is distributed mostly in the foothill zone where it is > 2000 m
thick in the Kirkuk Embayment. Mukdadyia formation was deposited in fluvial
environment in a rapidly subsiding foredeep basin (Jassim and Goff, 2006).The
formation is characterized by sedimentary cycles increasing by size from sandstone
and gravel; include mudstone and conglomerate masses ( Barwary and
Selwa,1995).The appearance of the gravel layer above Injana formation marks the
beginning of Al-Mukdadyia formation (Kassab and Jassim, 1980).
4- Bai Hassan Formation (U. Bakhtiari). (U. Pliocene)
This formation prevails in a large areas of AL-Adhaim Basin . Bai Hassan
Formation is covered by Quaternary deposits in the study area. The formation is
characterized by thick layers of conglomerates interbeded with sandstone, siltstone,
and claystone ; in general, the grain size of the clastics increases upward (Buday,
1980).The environment of deposition is continental (fluvial) resulting from the
erosion of the high mountains(Barwary and Selwa,1995 ). The appearance of the
first layer of conglomerates marks the boundary between this formation and the
underlying Mukdadyia Formation (Kassab and Jassim, 1980).
5- Quaternary Deposits
Foothill zone especially in the Kirkuk Embayment is characterized by long
anticlines with Miocene cores flanked by very broad and shallow synclines
exposing Mio-Pliocene molasse along their flank . The inner parts of the synclines
contian Quaternary deposits, referred to here as polygenetic synclinal fill. The
thickness of this Quaternary veneer is variable but is > 120 m in some water wells
(Jassim and Goff, 2006) .
The Quaternary deposits cover all parts of the study area ( Fig. 1.2 ), where
its age varies from early Pleistocene to late Holocene (Barwary and Selwa,1995 )
and include :
Slope deposits : slope sediments form along the flanks of the structures,
which covers a narrow belts along mountains. It consists of mixture of
Chapter One Introduction and Geology of study area
9
gravel , clay , aggregates of clastic and old rocks fragements they form
pediment deposits , where its thickness varies between (1 -10 m) .
Sheet runoff deposits : these sediments cover flat areas between Pulkhana and
Himreen anticlines and contain clay, silt and sand sometimes covered with
scattered gravels; it starts from pediment deposits towards the centre of the
depressions , where its thicknes ranges between ( 1 – 8 m) mostly.
Fig. 1.2 : Geological map of the study area modified from (Barwary and
Selwa,1995).
Valley fill deposits: these sediments are composed of different materials, such
as gravel, sand , clay and sometimes with pieces of rocks, and its thickness is
variable.
Flood plain deposits : these sediments form narrow strips along the valleys
and rivers ( Tuz Chai river) , It consists of mixture of clay , silt and sand
with some gravel, its thickness may reach (20 m).
Chapter One Introduction and Geology of study area
10
1.6.2 Tectonic and structural setting in the study area
The study area is situated within a physiographic zone called Foothill zone
( Makhul - Himreen subzone) in the unstable shelf ( Fig. 1.3 ) . It includes
Kirkuk block (Embayment) . This zone includes asymmetrical long anticlines
and synclines characterized by high dip value in some places associated with
joints and faults (Buday and Jassim, 1987).
Pulkhana anticline is one of the important structural elements in the study
area . It is assymmetric anticline trend ( NW- SE ) . The core of the structure
comprise the rocks of Fatha Formation surrounded by the rocks of Injana and AL-
Mukdadya ,while Bai-Hassan Formation forms the slopes of the low hills
surrounding the anticline (AL-Naqib, 1960).
1.6.3 Topography and Geomorphology of the study area
The elevation above sea level in the study area ranges between (200 – 245 m)
a.s.l., where the highest elevation lies in northeast near the anticline and decreases
towards west and southwest (Fig.1.1) .There are several factors working jointly or
individually lead to the formation different units and geomorphologic phenomena
, where the structural, climatic and lithologic factors form the geomorphologic
units (Ahmad and Al Jibouri, 2005) and include :
Units with structural origin ; Pulkhana anticline is one of the important
structural elements in the study area , which cause the occurrence of different
slopes influenced by rocky structure, various factors geodynamics such as
blocks movement and landslides can be observed in the rims of rocky and in
areas of slopes with strong dip .
Units with erosional origin ; these units form as a result of erosion process .
They include the undulating terrain (hills and slopes) and pediment deposits.
Units with river origin ; such as flood plain deposits . They occur in the form
of narrow strips along the rivers( Tuz Chai river) and valleys.
Chapter One Introduction and Geology of study area
11
Fig. 1.3 : Tectonic map of Iraq (after AL-Kadhimi et al., 1996)
Studied area
Chapter Two Climate and Hydrogeology
12
Chapter Two Climate and Hydrogeology
2.1 Climate
Climate is defined as the weather changes in a vast area and for a period of
time long enough to identify all its statistical features. Climatological change
represents the differences in the data of the average climatic readings or among
sequential climatological times(Kite, 1989) .The Climate elements have a great
role affecting water resources both surface and groundwater , and this effect is
different from one season or year to another. The climate variables relevant to
water resource are temperature, rainfall, evaporation, relative humidity, wind
speed and sunshine. The climate elements depend an determining the climate data
recorded in Tuz Khurmatu meteorological station during the period (1991-
2010), because the station was established in the year 1991. The values of the
monthly averages records for the climatic elements for the period (1991-2010)
are shown in table ( 2.1), include the following:
2.1.1 Temperature
Temperature is one of the climatic elements that have great role in the
hydrological cycle. Temperature changes are periodic within any water year, and
may affect groundwater recharge by its direct relation with evaporation and
inversely with rainfall and relative humidity (Fig. 2.8). The monthly averages of
the temperature for the period (1991–2010) is shown in table (2.1) . It is clear the
highest average of the temperature appeared in July (35.6 C°), and the lowest in
the January (9.2 C°) (Fig. 2.1 ).
2.1.2 Rainfall
Precipitation is the process by which atmospheric water vapour condenses into
liquid or solid water, which then falls under the action of gravity to the earth's
surface (Kalma and Franks 2003). Rainfall is the most effective climatic parameter
on the hydrological cycle; it is considered one of the most important climatic
elements in the hydrogeological studies and it represents the main factor in the
Chapter Two Climate and Hydrogeology
13
Table (2.1) Monthly averages of the climate elements for the period (1991-2010) of Tuz Khurmatu meteorological station.
Sunshine Wind speed Relative humidity Evaporation Temperature Rainfall Months duration ( hours)
(m/sec) ℅ (mm) (C°) (mm)
8.3 1.6 39.9 180.5 25.1 15.5 Oct. 6.5 1.4 58.3 89.5 16.4 32.7 Nov. 5.3 1.3 69.4 61 11.3 42.9 Des. 5.1 1.5 72.7 45.8 9.2 62.8 Jan. 6.3 1.8 67.2 66.7 11.3 40.5 Feb. 6.9 1.9 57.8 127.9 15.7 31.7 Mar. 7.9 2.2 50.5 175.4 21.4 36.6 Apr. 9.4 2.2 36 280.4 28.2 10.1 May. 11.2 2.2 27.5 359.3 33.4 1.0 Jun. 11.1 2.2 26.2 377.7 35.6 0.01 July. 11.1 2 26.9 352.1 35.3 0.0 Aug. 10.2 1.7 30.8 259.9 30.8 0.4 Sep.
---- ----- ----- 2376.2 ----- 274.21 Total
---- 1.83 46.93 198.01 22.8 22.85 Average
Fig. 2.1 : Average monthly temperature for the period (1991-2010) of Tuz Khurmatu meteorological station.
٠٥١٠١٥٢٠٢٥٣٠٣٥٤٠
Oct. Des. Feb. Apr. Jun. Aug.
Temperature(c°(
Chapter Two Climate and Hydrogeology
14
Fig. 2.2 : Average monthly rainfall for the period (1991-2010) of Tuz Khurmatu
meteorological station.
water balance and groundwater recharge. The monthly averages of rainfall for
the period (1991 - 2010) is shown in table (2.1).It is clear the rain is limited
between October and May and approximately disappears in the months of June,
July,August and September; the highest average of rainfall occurs in January
(62.8 mm) (Fig 2.2). The average annual rainfall of the dependable period reached
(274.21 mm). Using this average to construct the relation of the whole annual
rainfall with time (Al-Kubaisi,1996), the years of dependable period are classified
into wet and dry years as below :
The years in which the rainfall is more than the annual average are (7 years) which
represent the wet years:
7 P > —— × 100 = 35 % 20 Where:
P: rainfall
20: period interval (1991-2010)
The years in which the rainfall is less than annual average are (13 years) ,this
represents the dry years :
13 P < —— × 100 = 65 % 20
٠
١٠
٢٠
٣٠
٤٠
٥٠
٦٠
٧٠
Oct
. Nov
. Des
. Jan
. Feb
. Mar
. Apr
. May
.
Jun
. July
. Aug
. Sep
.
Rainfall (mm(
Months
Chapter Two Climate and Hydrogeology
15
The percentage of the wet years is less than the percentage of dry years
(Fig.2.3) . So this proves that the area is driven to dryness.
Fig. 2.3 : The average annual rainfall for the period (1991-2010) of Tuz Khurmatu
meteorological station.
2.1.3 Evaporation from class (A) pan
Evaporation is defined as the transfer of water from the liquid state to the
gaseous state. Evaporation is considered one of the important climatic factors in
determining the balance of water system and affect the hydrological cycle. It is one
of the water loss parameters connected with other factors and there is an direct
relationship between evaporation and temperature, sunshine duration, and area of
evaporation(Shaw,1999).It correlates by direct relation with temperature and
inverse relation with rainfall and relative humidity (Fig. 2.8 ). The monthly
averages of evaporation for the period (1991–2010) is shown in table (2.1) .The
highest average of evaporation appeared in July (377.7mm)while the lowest in
January (45.8mm) (Fig. 2.4).
2.1.4 Relative Humidity
It is the ratio between real vapor pressure of to satuaveraged vapor pressure in
air at the same temperature (Shaw, 1999). The variation in relative humidity due to
the saturation vapour pressure is determined by the change of air temperature. It
Chapter Two Climate and Hydrogeology
16
correlates positively with rainfall and negatively with temperature,evaporation and
wind speed(Fig.2.8). The monthly averages of relative humidity for the
period(1991– 2010) is shown in table(2.1).The highest average of relative humidity
appeared in January (72.7 %)while the lowest in July (26.2 %) (Fig. 2.5).
Fig. 2.4 : Average monthly evaporation for the period (1991-2010) of Tuz Khurmatu
meteorological station.
Fig. 2.5 : Average monthly relative humidity for the period (1991-2010) of Tuz
Khurmatu meteorological station.
2.1.5 Wind speed
The wind has a great role in the amount of evaporation as the rate of
evaporation increases with the excess of the wind speed. The monthly averages of
wind speed for the period (1991 – 2010) is shown in table (2.1).The highest
average of wind appeared in Apr.,May.,Jun.,and July (2.2 m/sec) , while the
lowest in December ( 1.3 m/sec) (Fig. 2.6 ) .
٠٥٠١٠٠١٥٠٢٠٠٢٥٠٣٠٠٣٥٠٤٠٠
Oct
. Nov
. Des
. Jan
. Feb
. Mar
. Apr
.
M… Ju
n. Ju
ly. A
ug. Se
p.
Evaporation(mm(
٠١٠٢٠٣٠٤٠٥٠٦٠٧٠٨٠
Oct
. Nov
. Des
. Jan
. Feb
. Mar
. Apr
. May
.
Jun
. July
. Aug
. Sep
.Relative humidity℅
Chapter Two Climate and Hydrogeology
17
2.1.6 Sunshine duration
Sunshine is considered as one of the climatic parameters which has a great
effect on the amount of the evaporated water. The increase in sunshine hours
means an increase in temperature and evaporation(Fig.2.8).The monthly averages
of sunshine duration for the period(1991- 2010) is shown in table(2.1).The highest
average recorded in June ( 11.2 hour/day) while the lowest in December (5.1
hour/day)(Fig. 2.7).
Fig. 2.6 : Average monthly wind speed for the period (1991-2010) of Tuz Khurmatu
meteorological station.
Fig. 2.7 : Average monthly sunshine for the period (1991-2010) of Tuz Khurmatu
meteorological station.
٠
٠.٥
١
١.٥
٢
٢.٥
Oct
. Nov
. Des
. Jan
. Feb
. Mar
. Apr
. May
.
Jun
. July
. Aug
. Sep
.
Wind speed (m/sec(
٠
٢
٤
٦
٨
١٠
١٢
Oct
. Nov
. Des
. Jan
. Feb
. Mar
. Apr
. May
.
Jun
. July
. Aug
. Sep
.
Sunshine (hours(
Chapter Two Climate and Hydrogeology
18
Fig. 2.8 : Relationship between different climatic variables
2.2 Potential Evapotranspiration (PE)
The potential evapotranspiration is defined as the water loss as a result of water
deficiency in soil for vegetation uses (Thornthwaite, 1948). It is an important
indicator in the water balance calculations.There are two types of
evapotraspiration ; the first is potential evapotraspiration which is defined as a
possible maximum evaporation for free water surface, the second type is actual
evapotranspiration defined as the actual amount of evapotranspiration for any
surface under climate condition (Brickle,et al, 1995).Potential evapotranspiration
(PE) can be calculated by the Lysimeter equipment and can also be calculated
theoretically (Linsley,et al, 1982).
Thornthwiate (1948) suggested an equation for potential evaporation
calculating depending on the climatic elements that affect the evaporation
processes( temperature factor) and latitude of the place and month of the year. The
equations of evapotranspiration and its variables are as follows:
PEx=16 [10tn / J]a mm/month ………………………..(2.1) 12 J = å For the 12 month ………………………………...(2.2) j =1
١
١٠
١٠٠
Oct. Nov. Des. Jan. Feb. Mar. Apr. May. Jun. July. Aug. Sep.
Rainfall (mm)
Temperature(c°)
Evaporation(mm)
Relative humidity ℅
Wind speed (m/sec)
Sunshine (hours)
Clim
atic
var
iabl
es
Chapter Two Climate and Hydrogeology
19
j = [tn / 5]1.514 …………………………………..............(2.3)
a = (675 × 10-9) J3 N (771×10-7) J2 + (179×10-4)J + 0.492
\a = 0.0 16 J+ 0.5 ……………………………………...(2.4)
The value of (a) equals (2.54)
Where:
PEx = potential evapotranspiration for each month (mm / month)
t = Mean monthly air temperature (C°)
n = Number month measurement
J = Annual heat index (C°)
j = monthly temperature parameter (C°)
a = Constant
The value of potential evapotranspiration (PEx) is a theoretical standard
monthly value based on 30 days and 12 hr sunshine per day, the values of the
corrected potential evapotranspiration (PEc) table (2.2), can be determined from
the following equation(Wilson,1971):
PEc = PEx × DT / 360 ………………………………..(2.5)
Where:
PEc : Corrected potential evapotranspiration(mm).
PEx : potential evapotranspiration(mm).
D: number of days in the month.
T: number of possible sunshine hours.
It is clear the lowest PEc value appeared in January ( 3.03 mm) while the
highest value in July ( 208.12 mm) . According to the values of evaporation the
relation between them become as follow:
(PEc < PEx < Epan)
The variation due to the difference in temperature ; sunshine time, and changes
in the rates of wind speed.
Chapter Two Climate and Hydrogeology
20
Table (2.2 ) Corrected potential evapotranspiration values by Thornthwaite method for the
period (1991-2010) of Tuz Khurmatu meteorological station.
Months Temp. (C°)
j = (tn/5)1.514 (10tn/J)a PEx (mm) DT/360
PEc
(mm/month)
Oct. 25.1 11.5 5.6 89.6 0.72 64.51
Nov. 16.4 6.04 1.91 30.56 0.54 16.5
Des. 11.3 3.44 0.74 11.84 0.46 5.45
Jan. 9.2 2.52 0.43 6.88 0.44 3.03
Feb. 11.3 3.44 0.74 11.84 0.49 5.8
Mar. 15.7 5.65 1.69 27.04 0.6 16.22
Apr. 21.4 9.04 3.73 59.68 0.66 39.38
May. 28.2 13.72 7.49 119.84 0.81 97.07
Jun. 33.4 17.73 11.55 184.8 0.93 171.86
July. 35.6 19.53 13.55 216.8 0.96 208.12
Aug. 35.3 19.28 13.3 212.8 0.96 204.28
Sep. 30.8 15.68 9.34 149.44 0.85 127.02
Total J = 127.57 1121.12 959.24
2.3 Water Surplus (WS) and Water Deficit (WD)
Water surplus is defined as the excess of rainfall over the corrected potential
evapotransipiration values during specific months of the year, while water deficit is
the excess of corrected potential evapotransipiration values over rainfall during the
remaining months of that year. According to lerner,et al.(1990) the actual
evapotranspirtion APE could be derived as follows:
APE = PEc when P ≥ PEc
APE = P when P < PEc
In the first case ( water surplus period) values of rainfall is greater than PEc, the
APE equal the PEc value; while in the second case( water deficit period ) PEc is
Chapter Two Climate and Hydrogeology
21
greater than rainfall , the APE is equal to rainfall values as expressed in the
following:
WS = P – PEc ……………………(2.6)
P > PEc , PEc = APE
WD = PEc – P …………………….(2.7)
P < PEc , P = APE
Where :
WS: Water surplus (mm)
WD: Water deficit (mm)
P : Rainfall (mm)
PEc: Corrected potential Evapotranspiration factor (mm)
APE: Actual Potential Evapotranspiration factor (mm)
The WS and WD are calculated without using the soil moisture (equal to zero).
Table (2.3) shows the monthly averages of APE , WS and WD; the water surplus
period is limited between November and March because rainfall exceeds PEc
,while the remaining months represent water deficit period where PEc exceeds the
rainfall. The WS amount is (163.6 mm) from total rainfall ( 274.21 mm), therefor
the water surplus ratio from the annual rainfall represented as:
WS % = WS / P × 100 ………………….(2.8)
WS % = 163.6 / 274.21 × 100 = 59.66 %
This percentage represents the groundwater recharge and surface runoff. While
WD amount is (848.63mm) from Corrected potential Evapotranspiration (PEc) ,
which equals to 40.34% from total rainfall as in the following equation:
WD % = 100 - WS % …………………(2.9)
WD % = 100 – 59.66 % = 40.34 %
Figure (2.9) shows the relationship between monthly averages of rainfall and
corrected potential evapotranspiration , which shows the water surplus and water
deficit periods.
Chapter Two Climate and Hydrogeology
22
Table (2.3) Monthly averages of water surplus (WS) and water deficit (WD) of Tuz Khurmatu meteorological station
Months P (mm)
PEc (mm)
APE (mm)
WS (mm)
WD (mm)
Oct. 15.5 64.51 15.5 0 49.01
Nov. 32.7 16.5 16.5 16.2 0
Des. 42.9 5.45 5.45 37.45 0
Jan. 62.8 3.03 3.03 59.77 0
Feb. 40.5 5.8 5.8 34.7 0
Mar. 31.7 16.22 16.22 15.48 0
Apr. 36.6 39.38 36.6 0 2.78
May. 10.1 97.07 10.1 0 86.97
Jun. 1 171.86 1 0 170.86
July. 0.01 208.12 0.01 0 208.11
Aug. 0 204.28 0 0 204.28
Sep. 0.4 127.02 0.4 0 126.62
Total 274.21 959.24 110.61 163.6 848.63
Fig.2.9 : The relationship between monthly averages of rainfall (P)and corrected
potential evapotranspiration, shows water surplus(WS) and the water deficit (WD)for
the study area.
٠
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١٥٠
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٢٥٠
Oct. Des. Feb. Apr. Jun. Aug.
P (mm(PEc (mm(
WDWD
Chapter Two Climate and Hydrogeology
23
2.4 Classification of Climate
There are many classifications for climate complied and proposed by many
scientists and researchers to find and determine the type of the climate. Two of
these classifications will be used to delineate type of climate in the study area as
follows:
Kettaneh and Gangopadhyaya (1974) classification , suggested a classification
depended on humidity index( HI) which represents the ratio between the rainfall
(P) to potential Evapotranspiration (PE) equation (2.10) , as shown in the table
(2.4). P H.I = ………………………….. …..(2.10) PEc
Where:
H.I: Humidity index.
P: rainfall (mm).
PEc: Corrected potential evapotranspiration (mm).
Depending on the climate information taken from Tuz Khurmatu
meteorological station for the period (1991-2010), and applying the equation of
classification (2.10). The dominated climate during the months of the year of the
study area and by comparing with the table (2.4) are shown in the table (2.6).
Table (2.4) Climate classification, according to Kettaneh and Gangopadhyaya(1974).
Humidity Index Climate type
H.I > 1 Humid
H.I < 1 < 2H.I Moist
2H.I < 1 < 10H.I Moderate to dry
10H.I < 1 Very dry
Classification suggested by Al-Kubaisi (2004) for determining the climate type by
using the annual dryness treatment depending on the amount of rainfall and
temperature, according to the following equations:
Chapter Two Climate and Hydrogeology
24
AI – 1 = (1.0 × P) / (11.525×t) …………………. ..(2.11)
AI – 2 = �P/t ……....……………………(2.12)
Where :
AI: Aridity index
P: Annual rainfall (mm)
t: Temperature (C°).
The value of (AI-1) represents the classification of the dominated climate ,
while the value of (AI-2) represents a modification of the latter classification as
shown in table (2.6 ). Applying the two equations (2.11) and (2.12) the values of
AI-1 and AI-2 becomes as follows:
AI – 1 = (1 × 274.21) / ( 11.525 × 22.8) = 1.05
AI – 2 = �274.21/22.8 = 3.47
When comparing the values of (AI-1) and ( AI-2) with the type of the climate
in table ( 2.5 ) reveals that the dominated climate in the area is humid to moist.
Table (2.5) Climate classification depending on values of annual dryness treatment (Al-
Kubaisi, 2004), (A-I.1 and A-I.2)
Type.1 Evaluation Type.1 Evaluation
AI-1>1.0 Humid to moist
AI-2>4.5 Humid
2.0<AI-2<4.0 Humid to moist
1.85<AI-2<2.5 Moist
1.5<AI-2<1.85 Moist to sub arid
AI-2<1.5 Sub arid
AI-1<1.0 Sub arid to arid AI-2>1.0 Sub arid
AI-2<1.0 Arid
Chapter Two Climate and Hydrogeology
25
Table (2.6) Climatic classification for the period (1991- 2010) of Tuz Khurmatu
meteorological station according to Kettaneh and Gangopadhyaya(1974).
Months P
(mm) PEc
(mm) H.I Kettaneh and
Gangopadhyaya,1974 Oct. 15.5 64.51 0.24 Moderate to Dry
Nov. 32.7 16.5 1.98 Humid
Des. 42.9 5.45 7.87 Humid
Jan. 62.8 3.03 20.73 Humid
Feb. 40.5 5.8 6.98 Humid
Mar. 31.7 16.22 1.95 Humid
Apr. 36.6 39.38 0.93 Moist
May. 10.1 97.07 0.104 Moderate to Dry
Jun. 1 171.86 0.0058 VeryDry
July. 0.01 208.12 0.000048 VeryDry
Aug. 0 204.28 0 VeryDry
Sep. 0.4 127.02 0.0031 VeryDry
2.5 Hydrogeology of the Studied Area
A hydrogeological unit (aquifer) is defined as a formation, part of formation or
group of geological formations which have permeability and porosity contain and
allow the movement of water with different velocities bounded from the bottom or
top or both layers or deposits of deaf impermeable to water (Walton, 1970).
Geological formations (either rock or sediment layers) in which groundwater
occurs can generally be classed as aquifers, aquitards or aquicludes (SCCG, 2006).
According to the hydrogeological division (Fig. 2.10) which shows the main
aquifers and aquifer groups of Iraq .The studied area is not considered as
independent hydrogeological basin, but it lies within big basin represented by
AL-Adhaim basin .The area of the basin is about (12000 km2 ) is located northeast
Chapter Two Climate and Hydrogeology
26
Fig. 2.10 : Main aquifers and aquifer groups of Iraq (after Alsam et al., 1990)
of Baghdad (AL-Mamuri,2005).The important water bearing formations (aquifers)
in the basin consist of Tertiary deposits ( Muqdadiya and Bai- Hassan formations)
as well as recent Quaternary deposits ( AL-Mamuri,2005) and (Abdul Razaq et al.,
2007) . Quaternary deposits cover all parts of the study area and consisting of
fluvial deposits and deposits of gravel, sand and clay, its thickness is small in the
study area and increasing towards the west . All wells in Tuz Khurmatu area are
penetrating Bai–Hassan Formation partially by different depths .Therefore this
Studied area
Chapter Two Climate and Hydrogeology
27
formation represent the upper and main hydrogeological productive aquifer in
the study area . It is considered important aquifer because of its good porosity
and permeability, and the confined location between the underlying Mukdadyia
formation and the overlying Quaternary deposit. Bai-Hassan Formation (confined
aquifer) composed of sandstone and gravel consecutive with clay and
conglomerate masses (Khudair et al.2000) and (AL-Rubaii , 2008). Al-Fat'ha
formation appears in the study area in Pulkhana anticline and affect the
groundwater salinity in the area because of the evaporates rocks (gypsum rocks) it
contains (Mohamed et al , 2009 ). The water from the Bakhtiari aquifer ( Bai-
Hassan and Muqdadiya formations ) are generally of good quality (Stevanovic and
Iurkiewicz , 2009). The hydraulic properties and groundwater quality for Bai-
Hassan Formation were measured by Ahmed and AL-Jubouri(2005) in Samarra
quadrangle, which includes the study area; the transmissivity (T) values ranged
between(4 - 829 m²/day ) , the hydraulic conductivity (K) ranged between (0.1 -
43 m/day) , the water static level ranged between ( 2 – 48 m) and production of
wells ranged between ( 20- 5862 m³ / day ) ,while groundwater quality ranged
between (Na2SO₄ and CaSO₄) to (MgSO₄, NaCl, CaCl2, Ca(HCO₃)2 and
Mg(HCO₃)2 water type , EC ranged between (334 – 11075 µS/cm) .
Stratigraphic correlation for wells of the study area was drawn by depending
on lithology of wells drilled by General Commission for Groundwater and the
available informations about the hydrogeology of the study area and shows the
main aquifer in the study area (Bai-Hassan formation ) as shown in Fig.(2.11 ).
Chapter Two Climate and Hydrogeology
28
Fig. 2.11 : The stratigraphic correlation between the wells in the studied area
2.6 Groundwater movement and recharge
Groundwater moves both vertically and laterally within the groundwater system
(Winter et al.1998).The groundwater movement depends upon the hydraulic
gradient and 'hydraulic conductivity'. The hydraulic gradient is the change in static
head per unit distance in a given direction (El-Sayed,2004).Groundwater
movement in gravels and sands is relatively rapid, whereas it is exceedingly slow
in clay or in tiny rock fractures (Harter 2003).
Recharge areas of Bai- Hassan formation (confined aquifer) are located in the
northeast where its layers are expose outside the study area and depends on rain
water (Khudair et al.2000 ) , and it is affected by water infiltration from surface
runoff (Tuz Chai river) and the water losses from irrigation canal (Kirkuk
irrigation canal ) in the study area .
Chapter Two Climate and Hydrogeology
29
Fig. 2.12 : The flow net of the study area
The general direction of groundwater movement in the area is from the recharge
areas in northeast to the discharging areas at southwest (Ahmed and Al-Jubouri,
2005) and (Mohamed et al , 2009 ). To clear up the flow direction of ground
water, a flow net map was drawn (Fig. 2.12);depending on the groundwater level
measurements in the wells of the study area (Appendix1).According to the flow net
map the direction of groundwater movement in the study area is from northeast
towards southwest as shown in Fig. (2.12 ). Groundwater moves from areas of
high hydraulic effort towards areas of low hydraulic effort, the value of the
hydraulic gradient of the study area is calculated according to the following
equation (Todd, 2007) :
I = dh/dl ………………………. (2.13)
Where:
I: hydraulic gradient
Chapter Two Climate and Hydrogeology
30
dh: Head loss between two water points.
dl: Horizontal distance between the same two water points.
The value of the hydraulic gradient in the northeast , middle and southwest of
the study area equal (0.012),(0.006),(0.0024) respectively with an average of
(0.0068) for all the study area.
2.7 Hydraulic aquifers properties
Studying and knowledge of aquifer hydraulic properties are necessary to
estimate groundwater flow velocities , flow volumes , and travel times . Common
techniques for estimating the hydraulic properties of aquifers are usually based on
solutions to groundwater flow equations simulating the response of an aquifer to
pumping stress (Victoria, 2006).
To find the hydraulic properties of the aquifer , pumping test have proved to
be the most suitable means of achieving this purpose. The important properties are
as follows:
2.7.1 Hydraulic conductivity (K)
Defined as the volume of water that will move through a porous medium in unit
time under a unit hydraulic gradient through a unit area measured at right angles to
the direction of flow. Hydraulic conductivity can have any units of (Length/ Time)
represented by the following equation (Kruseman and de Ridder, 2000):
Q K = ——— ………………………….(2.14) AI Where:
K: Hydraulic conductivity (m/day)
Q: Discharge (m3/day)
A: Area of groundwater(m2)
I: Hydraulic gradient (dimensionless unit)
The values of hydraulic conductivity for a particular unit varies from place to
another , because of the way in which geological deposits are formed (Domenico
and Schwartz, 1998).Hydraulic conductivity values commonly ranges between
Chapter Two Climate and Hydrogeology
31
0.02 and 40 m/day for unconsolidated sediment aquifers, less than 0.5 m/day for
sandstone, and below 0.0001 m/day for clays or shale (SCCG, 2006).
2.7.2 Transmissivity (T)
It is defined as the rate of flow of water under a unit hydraulic gradient through
cross-section of unit width over the whole saturated thickness of the aquifer
(Kruseman and de Ridder,2000). It equals the product of multiplying the average
hydraulic conductivity by the saturated thickness of the aquifer, expressed in
(m² /day) (David,2002):
T = K × b …………………….. (2.15)
Where:
T: Transmissivity (m² /day).
K: Hydraulic conductivity (m /day).
b: Saturated thickness of aquifer (m).
2.7.3 Storage coefficient (Sc)
The storage coefficient (Sc) of a confined aquifer is defined as the volume of
water released from storage per unit surface area of a confined aquifer per unit
declined in hydraulic head. The storage coefficient generally ranges between
0.00005 and 0.005 in confined aquifers (Kruseman and de Ridder, 2000) , it is a
dimensionless unit .
2.8 Pumping tests analysis
Pumping test process is carried out by pumping water from the aquifer with a
constant discharge for a specific period of time. The analytical methods represent
the suitable methods for the pumping test data treatment . The following methods
have been used :
2.8.1 Cooper-Jacob method
Cooper and Jacob (1946) suggested that for small values of (r) and large values
of (t) , the following method may be applied for the analysis of pumping test of a
well. Accordingly, the value of transmissivity( T ) can be obtained by noting
( t / t0 ) for one log-cycle, then log t / t0 =1 ,Where :
Chapter Two Climate and Hydrogeology
32
r: Distance from pumped well to observation well (m).
t: Time of pumping (minute).
t0: intercept point of the fitted line on the time axis.
Therefore, if ∆s is the drawdown difference per log-cycle of t, then the
equation below can be set to determine (T) value as follows(Todd, 2007) :
2.3 Q T = ———— …………………………….(2.16) 4 ∏ ∆s Where :
T: Transmissivity (m² /day)
Δs : Difference in the drawdown (m) per log-cycle of t.
Q: Discharge (m³/day).
2.8.2 Theis recovery equation
In this method the residual drawdown (s') is plotted versus (t / t') on semi
logarithmic paper and a straight line is fitted through the plotted points, where :
t : Total time of pumping plus the recovery time (minute).
t': Time since the cessation of pumping (Recovery time) (min).
The equation below is applied to determine the transmissivity (Kruseman and
De Ridder, 2000) as follows: 2.3 Q T = ———— ……………………………(2.17) 4 ∏ ∆s' Where :
Δs' : Difference in the residual drawdown, in (m) per log-cycle of (t / t'),
Terms of application in this equation is the same as in "Cooper-Jacob equation",
with the exception of using residual drawdown instead of the drawdown. This
method is more meticulous in knowing the hydraulic properties because the water
level recovery will be normal to avoid the ground water problem fluctuation during
the pumping because of the fluctuations in pumping rate which happens as result of
pump work.
Chapter Two Climate and Hydrogeology
33
2.9 Analysis results of pumping test
Single well pumping test was carried out for two wells in the studied area
with a constant discharge rate represented by :
Well ( W1). ( Mojama Tuz ) .
Well ( W2). (Esalh Tuz 1) .
And single well pumping test data are available for ( 5 ) wells drilled in the
study area that are obtained from General Commission for Groundwater
represented by:
Well ( W3). (Al Asreia )
Well ( W4). ( Al Askari )
Well ( W5). (Al Mahata )
Well ( W6). (Esalh Tuz 2 )
Well ( W7). (Nawaf Abd-Alaziz )
Observation wells are not available in the studied area , therefore these tests
have been conducted without observation wells, thus the storage coefficient is not
determined. The experimental data and graphs for the seven pumping tests wells
in the study area and their locations are listed in appendix (2) and
Fig. (2.13).Cooper-Jacob and Theis recovery methods were used in the treatment
of these data.
From graphs in the appendix ( 2) it can be observed that some forms of data
analysis of pumping tests by Jacob and Thies methods reflects the existence of
two layers; and this was evident in the stratigraphic correlation map of the study
area (Fig.2.11) which it shown and confirmed the existence of gravel layers
successive with the layers of clay within Bai-Hassan Formation ,therefore the
transmissivity and hydraulic conductivity values are calculated for each layer and
then is calculated the average .
Table (2.7) shows the hydrogeological data of wells (transmissivity , hydraulic
conductivity and specific capacity)values obtained from pumping test data analysis
by Jacob and Theis recovery methods. The average of transmissivity values range
Chapter Two Climate and Hydrogeology
34
between (95.47 - 335.72m²/day),and the average of hydraulic conductivity range
( 2.11 - 4.47 m/day ).This reflects that the hydraulic properties values of Bai-
Hassan aquifer in study area are heterogeneous and variant, as a result of
heterogeneity of Bai-Hassan aquifer due to variations in lithology and porosity of
aquifer.
Fig. 2.13 : Locations of the pumping wells in the studied area
2.10 Specific Capacity (SC)
Specific capacity is the ratio of the obtained rate of the discharge to the
drawdown, which is required to produce the obtained discharge and expressed in
cubic meter per day for each meter of drawdown (Fetter, 1994), according to the
following equation :
Q SC = —— …………………………….(2.18) s Where :
Chapter Two Climate and Hydrogeology
35
SC: Specific Capacity (m² /day).
Q: Discharge (m³/day).
s: Drawdown (m).
Fig. 2.14: Relationship between specific capacity and drawdown
The specific capacities for the pumping wells are calculated by Fetter's(1994)
equation and shown in table (2.7). From Fig.(2.14) which shows the relationship
between specific capacity and water level drawdown , it is clear that there is an
inverse relationship between specific capacity and water level drawdown
(Todd,1980).The difference in specific capacity values of wells penetrating the
same aquifer in the study area is attributed to differences in the discharging
quantity and the total depth in addition to the saturated thickness .So when the
specific capacity is high, it reflects that the productivity of the well is good and this
depends on the lithology of the aquifer, and also on depth, saturated thickness,
design and development of wells.
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Chapter Two Climate and Hydrogeology
36
Table (2.7) Results of hydraulic properties by two methods used in single well pumping test analysis for wells of the study area
Well
No.
Jacob
(Drawdown)
Theis (Recovery)
Average
Jacob and Theis
Specific
Capacity
T1
m²/d
T2
m²/d
K1
m/d
K2
m/d
T
m²/d
Average
K
m/d
Average
T1
m²/d
T2
m²/d
K1
m/d
K2
m/d
T
m²/d
Average
K
m/d
Average
T
m²/d
K
m/d
SC
m²/d
(W 1)
76.32 167.69 1.41 3.10 122 2.25 108.50 225.87 2 4.18 167.18 3.09 144.59 2.67 201.6
(W 2)
168.20 277.38 2.61 4.31 222.79 3.46 112.93 243.24 1.75 3.78 178.08 2.76 200.43 3.11 297.93
(W 3)
156.16 ----- 2.7 ----- ----- ----- 225.87 106.29 3.9 1.83 166.08 2.86 161.12 2.78 232.72
(W 4)
187.23 ----- 3.64 ----- ----- ----- 163.56 ----- 3.18 ------ ------ ------ 175.39 3.41 285.8
(W 5)
73.11 ----- 1.78 ----- ----- ----- 108.11 225.87 2.63 5.5 166.99 4.06 120.05 2.92 230.4
(W 6)
195.2 385.63 2.60 5.14 290.41 3.87 267.98 494.1 3.57 6.58 381.04 5.07 335.72 4.47 432
(W 7) 99.86 ----- 2.21 ----- ------ ----- 71.86 110.31 1.59 2.45 91.08 2.02 95.47 2.11 172.8
Chapter Three Hydrochemistry
37
Chapter Three Hydrochemistry
3.1 Introduction
Two of factors are fundamental control on water chemistry in drainage basins
, the type of geologic materials that are present and the length of time that water is
in contact with those materials. Chemical reactions that affect the biological and
geochemical characteristics of a basin include acid-base reactions, precipitation
and dissolution of minerals, sorption and ion exchange, oxidation-reduction
reactions, biodegradation and dissolution and exsolution of gases (Winter et
al.1998). The groundwater quality is nearly of equal importance to quantity.
Therefore it's necessary to make chemical, physical and bacterial analyses of
groundwater to determine its suitability for different purposes (drinking ,
livestock, industrial, agriculture and irrigation).The chemical analysis of
groundwater includes determination of the major, minor and trace metal
constituents, and also the field measurements of the electrical conductance,
hydrogen ions activity as well as the water temperature (Karanth,2008).The
chemical parameters ( EC , pH and temperature ) must be taken in the field
immediately after sampling, because water chemistry can change rapidly once a
sample is extracted from a well and exposed to light, warmth, cold, air, or other
environmental factors (Sanders, 1998).
The hydrochemical study for groundwater in study area involves the Major,
Minor and trace ionic concentrations. Besides, these ionic concentration study also
involves the salinity( total dissolved solids TDS), electrical conductivity (EC) and
acidity (pH). The water samples were collected from (20) wells in two periods,
their locations are shown in Fig.(3.1) and appendix (1), the first period during of
September (2010), this represents the dry period, and the second period was during
March(2011),and this represents the wet period.
Chapter Three Hydrochemistry
38
3.2 Accuracy
The accuracy of the results of the water samples analyses can be estimated from
the results of reaction error test (U), by calculation absolute difference between
total of cations and anions concentration on total for these concentrations in (epm)
units as percentage (Stoodly et al,1980, Gill,1997 and Appelo&Postma,2005) and
according to the following equation:
100anionsrcationsr
anionsrcationsrU ´
å+å
å-å= ………………… (3.1)
A% = 100 – U …………………………………… (3.2) Where:
U = Uncertainty (reaction error)
A = Accuracy or certainty
r: (epm) .
When (U ≤ 5%)(certain) the results could be accepted for interpretation, but if
(5% ≤ U ≤ 10%) (probable certain) the results are acceptable with risk , but if
the value ( U > 10%) (uncertain) can not depended on the results in
hydrochemical interpretation .
U values range between (0.004 – 4.1 %) for the dry period samples and
between ( 0.03 – 7.4 %) for the wet period samples (appendices 6,7). Therefore
the results of the analysis can be used in the hydrochemical interpretation for the
study area.
3.3 Physical properties:
3.3.1 Temperature.
All geochemical reactions depends on temperature (SCCG, 2006).Water
temperature is related to solar radiation and air temperature water temperature
closely follows air temperature streams، ponds and springs (Boyd,
2000).Temperature will increase with depth, about 2.9 C° for each (100 m) depth
Chapter Three Hydrochemistry
39
(Todd, 1980) .The temperature values of water samples is given in table(3.1)
and appendix (3). So it is clear there is no abnormal temperature value recorded. Table (3.1) The temperature values of water samples of the studied area
T C° Dry period Wet period
Range 21 – 24 20 - 22
Average 23.05 20.9
Fig. 3.1 : Locations of water samples wells in the study area. 3.3.2 pH
The pH of a solution is defined as the negative logarithm of its hydrogen ion
activity (Boyd, 2000):
pH= - log [H+]
The measurement of pH is an indicator of the acidity or alkalinity of water
(Langmuir, 1997). A (pH) value of 7 indicates neutrality, that is the concentration
of hydrogen ( H+) and hydroxide (OH-) ions are equal. Water with pH less than 7
Chapter Three Hydrochemistry
40
is said to be “acidic”, whereas levels above 7 are termed “alkaline”, groundwater
most commonly occurs under reducing conditions, where the limited oxygen
present is consumed by chemical and biological activity, as a result, reductions in
pH occur and values less than 7 are commonly encountered (SCCG, 2006) .The
dissolution and mobility of metals in natural water are greatly influenced by the
(pH) (Thompson et al.,2007). The pH values of water samples is given in table
(3.2) and appendix(3). Table (3.2) The pH values of water samples of the studied area
pH Dry period Wet period
Range 7.17 – 8.2 7.12 – 7.92
Average 7.71 7.40
It is clear the water samples of study area for both periods are of low alkalinity.
3.3.3 Total Dissolved Solids (TDS)
Total dissolved solids (TDS) is the total amount of solids remaining when a
water sample evaporates to dryness (Drever,1997) . Dissolved solids include both
organic and inorganic materials dissolved in a sample of water and are commonly
used as a general indicator of water salinity or quality (Bates and Jackson, 1984) .
The salinity of groundwater may be modified by the presence of salts stored within
rocks at the time of formation (connate salts), by those brought into an aquifer
through recharge, or by the products of rock weathering (SCCG, 2006).TDS
represents a total summation of ionic concentrations of cations and anions , it is
measured by the (ppm) or (mg/l) units (Boyd, 2000).The TDS values of water
samples is given in table(3.3)and appendix (3). Table (3.3) The TDS values of water samples of the studied area
TDS (ppm) Dry period Wet period
Range 339 - 2415 241 - 2287
Average 1279.85 1027.55
Chapter Three Hydrochemistry
41
It is clear that the salinity in the dry period is more than it is for the wet period
and that is due to the dilution which happens in the wet period as a result of
rainfall. Observing Fig.(3.2),which shows the spatial distribution of TDS in the
studied area through the dry and wet periods, it becomes apparent that the TDS
values are higher in wells drilled near Pulkhana anticline ( wells No.1,3,13,15) and
this is due to Al- Fat'ha formation effect, which appears in the anticline and
contain evaporates rocks (gypsum rocks) and affect the salinity of groundwater,
while wells (No. 5,14,16) are close to the anticline but the TDS values are low
this is attributed to the dilution process by the water from Tuz Chai river. The
reason why well (No.1) which is located near the anticline but the TDS value is
less than the wells (No.3,13,15) is attributed to the depth, where the depth of the
well (No.1) reaches (130 m) . It can be observed that the TDS values decrease
when moving away from the anticline towards the west and southwest which
represent the area of groundwater discharge and this is a reverse to what is
expected, especially in wells that are close to Tuz chai river .The reason for this
decrease is the dilution process of the groundwater by Tuz chai river and water
seepage from Kirkuk irrigation canal.
Comparison of TDS values for both periods (Table3.3) with three
classifications of water (Altoviski,1962; Drever,1997 and Todd,2007) (Table 3.4),
it is clear that the groundwater in the studied area is classified as slightly-brackish
water . Table (3.4) Classification of water salinity according to (TDS) in (ppm).
Todd(2007) Drever(1997) Altoviski, 1962 Water Class 10 - 1000 <1000 0 - 1000 Fresh Water
----- 1000 - 2000 1000 – 3000 Slightly Water
1000 – 10000 2000- 20000 3000 - 10000 Slightly-brackish Water
10000 - 100000 ----- 10000 - 100000 Brackish Water ----- 35000 ----- Saline Water
> 100000 > 35000 > 100000 Brine Water
Chapter Three Hydrochemistry
42
(A)
(B)
Fig. 3.2 : Spatial distribution of TDS in the studied area:
( A )Dry period (B) Wet period
Chapter Three Hydrochemistry
43
The percentage of error between the dehydration method and the ions
collecting method can be calculated as in the following equation:
TDSm – TDSc T% = –––––––––––––– × 100 …………… (Nordstrom,et al,1989) TDSm Where:
T%: Percentage of test distinctions by unit ( % ).
TDS m :Total dissolved solids of measured by dehydration method (ppm).
TDSc : Summations of concentrations (cations + Anions) in (ppm).
According to table (3.5) the values of (T %) (Table 3.8) for some water
samples of study area for both periods fall in the range of (0 ─ 5%) ,it is
considered dependent in the hydrochemical interpretations. While other samples
falling in the range of( 5 < T ≤ 10 % ), is considered dependent in the
hydrochemical interpretations with cautiously. Table (3.5) Percentage Test (T%) (Nordstrom,et al,1989)
T% Uses of interpretations
0 < T ≤ 5 % Can be used in hydrochemical interpretations
5 < T ≤ 10 % Can be used in hydrochemical interpretations cautiously T > 10 % Results are independent
3.3.4 Electrical Conductivity (EC)
Electrical Conductivity (EC) is the ability of (1cm³) of water to conduct
electrical current, at temperature of 25C°, when measured by micro Siemens per
centimeter (µS/cm).It depends on the concentration of soluble salts and the
temperature of the water (Boyd, 2000). The EC depends on water temperature
, where an increase in water temperature of one degree celsius causes an increase
in electrical conductivity by (2%) (Hem, 1985) and (Mazor,1990). Also the EC
increases with the increase of the total dissolved salts (Detay,1997). The EC values
of water samples is given in table(3.6) and appendix (3).
Chapter Three Hydrochemistry
44
Table (3.6) The EC values of water samples of the studied area
EC µS/cm Dry period Wet period
Range 546 - 3500 363 – 3402
Average 1901.4 1607.2
The (EC) value of the wet period is lower than the dry period and this due to
dilution process by rainfall.
When comparing EC values for both periods (Table 3.6) with table (3.7)
which shows the relationship between electrical conductivity and water
mineralization , it can be concluded that the type of groundwater in the studied area
is as excessively mineralized water due to the salinity.
From Fig.(3.3) and (3.4) which shows the relation between TDS and EC values
for both periods , it can be observed that the linear correlation between them for
the dry and wet periods , X-axis represent (EC) values and Y-axis represent
(TDS) values .The correlation coefficient (R²) is close to (1) refering to the strong
relation between both the TDS and the EC and for the two periods. So these
relations can be used prospectively for the estimation of TDS value, knowing Ec
values for the study area.
Table (3.7) Relationship between electrical conductivity and water
mineralization (Detay, 1997).
EC µS/cm Mineralization
<100 Very Weakly Mineralized water
100-200 Weakly Mineralized water
200-400 Slightly Mineralized water
400-600 Moderately Mineralized water
600-1000 Highly Mineralized water
>1000 Excessively Mineralized water
Chapter Three Hydrochemistry
45
Table (3.8) The (T %) values for TDS measured and calculated of the water in the study area.
Wells No.
Dry Period Wet Period
TDSm (ppm)
TDSc (ppm) T %
TDSm (ppm)
TDSc (ppm) T %
1 1857 1793 3.44 1245 1122.9 9.8 2 1686 1633.31 3.12 1380 1274.3 7.65 3 2169 2030.4 6.39 2250 2054.4 8.69 4 704 639.17 9.2 697 641.1 8.02 5 1485 1352.5 8.92 1180 1103 6.52 6 1488 1393.5 6.35 1014 929.7 8.31 7 1419 1291 9.02 1081 989.9 8.42 8 380 351.01 7.62 302 273.4 9.47 9 339 328.01 3.24 241 217.99 9.54 10 1335 1230.68 7.81 1026 965.8 5.86 11 1564 1446.5 7.51 1244 1159.57 6.78 12 533 509.3 4.44 366 353 3.55 13 2366 2193.5 7.29 2287 2187.4 4.35 14 975 877.7 9.9 966 948.4 1.82 15 2415 2272 5.92 2118 2030.5 4.13 16 1380 1314 4.78 974 885.7 9.06 17 758 731.2 3.53 373 339.5 8.98 18 756 732.1 3.16 562 542.2 3.52 19 1442 1346.6 6.61 932 877.7 5.82 20 546 497.3 8.91 313 299.66 4.26
Fig. 3.3 : EC - TDS relationship of groundwater samples in the studied area for dry
period.
TDS = 0.677Ec - 7.391R² = 0.983
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Chapter Three Hydrochemistry
46
Fig. 3.4 : EC - TDS relationship of groundwater samples in the studied area for
wet period.
3.4 Chemical properties :
3.4.1 Cations :
3.4.1.1 Calcium (Ca+2)
Calcium is an essential constituent of sedimentary rocks, and it results from the
erosion of igneous and metamorphic rocks. It is abundant almost in the all soils
(White, 2005) .Calcium is the most abundant element of the alkaline -earth metals
,and is an essential element for plant and animal . It is produced as a result of
dissolution processes of sedimentary rocks ( calcite, aragonite, limestone, dolomite
and gypsum) and from weathering of igneous rocks like ( Pyroxene, amphibole
and plagioclase feldspar (anorthite)) . Calcium also occurs in other silicate
minerals that are produced in metamorphism (Hem,1989).The source of calcium
ion in the studied area is from evaporates rocks (gypsum rocks) of Al-Fat'ha
formation, which appears in Pulkhana anticline . The calcium ion (Ca+2)
concentration of water samples is given in table (3.9), and appendices (4,5).
Table (3.9) The Ca+² concentration of water samples of the studied area
Ca+2 (ppm) Dry period Wet period
Range 33 - 253 26.01 – 234
Average 117.5 96.44
The decreases of (Ca+2) concentration in wet period due to dilution process by
rainfall.
TDS = 0.669 Ec - 48.24R² = 0.978
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Chapter Three Hydrochemistry
47
3.4.1.2 Magnesium (Mg+2)
Magnesium is an alkali-earth metal with one oxidation state in water (Mg+2).
Magnesium ions are smaller than sodium and calcium ions ,and it is one of the
necessary elements of the plants and animals (Hem, 1989). Dolomite, limestone
and clay minerals are considered as essential sources for magnesium ion.
Magnesium is found also in igneous rocks and minerals such as (Olivine ,Pyroxene
and amphibole) and metamorphic rocks such as (serpentine and talc)
(Todd, 2007). The source of magnesium ion in the studied area is from clay
minerals and fertilizers use effect. The magnesium ion (Mg+2) concentration of
water samples is given in table(3.10), and appendices (4,5). It is clear that the
(Mg+2) concentration in the wet period is slightly lower than the dry period and this
due to dilution process.
Table (3.10) The Mg+2 concentration of water samples of the studied area
Mg+2 (ppm) Dry period Wet period
Range 11 – 130 10.1 – 121
Average 53.3 47.24
3.4.1.3 Sodium (Na+)
Sodium is the most abundant member of the alkali- metal group in nature. The
source of sodium in groundwater and comes from erosion of alkalinity feldspar and
evaporation rocks and from ionic exchange of clay minerals (Appelo, 1999). Most
of salts and sodium compounds have high solubility in water , the most soluble salt
among them is sodium chloride (NaCl) while the least is sodium bicarbonate
(NaHCO₃); their solubility increases normally at high temperatures
(Hem,1985).Human activities can have a significant influence on the concentration
of sodium in surface water and ground water(Al-Manmi,2008). The sodium ion
(Na+) concentration of water samples is given in table(3.11), and appendices
(4,5).Therefore it can be observed that the sodium concentration during the wet
period is lower than the dry period and this due to dilution process.
Chapter Three Hydrochemistry
48
Table (3.11) The Na+ concentration of water samples of the studied area
Na+ (ppm) Dry period Wet period
Range 61 – 345 42 – 345
Average 185.9 131.86
3.4.1.4 Potassium (K+)
Potassium is slightly less common than sodium in igneous rocks but more
abundant in all sedimentary rocks. The main source of potassium is the products
formed by weathering of igneous minerals like(orthoclase, microcline, mica
(biotite) and the feldspathoid leucit) and sedimentary rocks . Potassium is
commonly present in clays within the structure like illite or adsorbed on other clay
minerals, evaporate rocks include sylvite and other potassium salts and organic
remains (plant) (Hem,1985). Fertilizers increases the potassium concentration in
the water (Daly,1994). Iraqi phosphate fertilizers (NPK) contains 19 % K2O
(AL-Qaraghuli, 2005). The potassium ion (K+) concentration of water samples is
given in table(3.12), and appendices (4,5).
Table (3.12) The K+ concentration of water samples of the studied area
K+ (ppm) Dry period Wet period
Range 0.3 – 5.5 0.7 – 5.4
Average 2.2 1.50
Potassium (K+) concentration in the wet period is lower than the dry period
and this due to dilution process by rainfall.
3.4.2 Anions :
3.4.2.1 Bicarbonate (HCO3⁻ ) and Carbonate (CO₃⁻²)
Bicarbonate ions are considered the source of water alkalinity (carbonate
alkalinity). Alkalinity is the ability of water for interaction with ion of hydrogen
(H+) (Faure,1998). CO2 gas in the atmosphere or in the soil dissolved in water is
the principle source of bicarbonate , in addition to solution of carbonate rocks and
oxidation of organic matter (Hem,1985).When pH < 8.2 the hydrogen ion is added
Chapter Three Hydrochemistry
49
to the carbonate and become dissolved bicarbonate, but when the pH > 8.2 the
process of (HCO3-) depletion to (CO3
-2) in solution becomes high (Davis and
Dewiest,1966). The bicarbonate concentration of water samples is given in table
(3.13), and appendices (4,5). Table (3.13) The HCO3
⁻ concentration of water samples of the studied area
HCO3⁻ (ppm) Dry period Wet period
Range 12.8 - 611 18 - 446
Average 186.6 214.71
It is clear that the concentration of the wet period is greater than the dry period
due to the recharge occurrence which coincide with the values of (pH).The
concentration of (CO₃⁻²) is zero for all water samples due to pH value less than
(8.3).This means when pH is less than (8.3) the carbonate is associate with water
converted to (HCO3⁻ ).The carbonates are usually found in water where its pH
value exceeds 10.3 (Appelo,1999).
3.4.2.2 Sulfate (SO42-)
The natural source of sulfate ions (SO42-) in groundwater is dissolution of
sulfate minerals that are found in sedimentary rocks such as gypsum and anhydrite.
Oxidation of barite minerals and the human activities (agricultural and industrial
activities)are considered another sources for sulfate (Sawyer and Mecarty 1985 ).
Iraqi fertilizers TSP, MAP, NP and NPK contains (S % ) 1.5, 0.64, 0.58 and 2.35
respectively (AL-Qaraghuli, 2005). The element is essential in the life processes
of plants and animals (Hem 1985). The sulfate concentration of water samples is
given in table(3.14),and appendices (4,5). Table (3.14) The SO4
2- concentration of water samples of the studied area So4
2- (ppm) Dry period Wet period
Range 108 - 844 43.2 - 844
Average 409.6 294.95
Chapter Three Hydrochemistry
50
The high concentration of sulfate ion in the studied area belongs to Al- Fat'ha
formation effect (gypsum rocks) which appears in Pulkhana anticline .The
concentration of sulfate ion in the dry period is more than it is for the wet period ,
this is due to dilution process by rainfall and also change of distribution of
evaporates rocks in the area .
3.4.2.3 Chloride (Cl-)
Chloride is a minor element of the earth's crust, but it is a major dissolved
constituent of most natural water. The source of chloride in groundwater is from
dissolution of sedimentary rocks particularly the evaporates like halite and sylvite
and from ancient sea water entrapped in sediments (Davis and Dewiest, 1966).
Chloride is also abundant in the minerals found in igneous rocks like apatite
, feldspathoid and sodalite . Another source of chloride is from sewage and
industrial effluents (Hem, 1985).Chloride is added during water treatment for
drinking purposes and is considered another source of chloride in groundwater
(WHO 2007). The chloride concentration of water samples is given in table (3.15)
and appendices (4,5). Table (3.15) The Cl- concentration of water samples of the studied area
Cl- (ppm) Dry period Wet period
Range 89 – 468.6 49.7 – 460
Average 242.8 173.07
The decreases of (Cl- ) concentrations in wet period due to dilution process .
3.5 Total Hardness (TH)
The hardness of groundwater predominantly results from the presence of
dissolved calcium and magnesium salts usually carbonates. Hardness is a measure
of the effect of water on the ability of soap to form suds, it can cause scaling
problems in pipework and heating systems due to the nature of the dissolved salts.
This character of groundwater is usually described in terms of “carbonate
hardness” and “non-carbonate hardness (SCCG, 2006). Total hardness mainly
Chapter Three Hydrochemistry
51
reflects water contents of Ca+2, Mg+2 ions and it is expressed by its equivalent from
calcium carbonate(Todd, 2007) according to the following equation:
TH (ppm) = 2.497 [ Ca ++ ppm] + 4.115 [ Mg ++ ppm] ……….(3.3)
There are two kinds of (TH ) (Hem, 1989) :
Temporary Hardness “carbonate hardness” – represent calcium and magnesium
concentrations, combined with the bicarbonate of water. This TH removed by
boiling the water.
Ca(HCO3)2 → CaCO3 + H2O + CO2
Permanent hardness “non-carbonate hardness – result from the combination of
calcium and magnesium concentrations with bicarbonate, chloride and nitrate. This
TH removed by adding sodium carbonate .
CaCl2 + NaCO3 → CaCO3 + 2NaCl.
The TH concentration of water samples is given in table (3.16), and appendices
(4,5). Table (3.16) The TH concentration of water samples of the studied area
TH (ppm) Dry period Wet period
Range 127.6 – 1166.6 118.85 – 1082.21
Average 512.9 435.22
TH concentration in the wet period is lower than the dry period and this due
to dilution process by rainfall. Table (3.17) Classifications of water according to total hardness .
Type of
water
Total Hardness TH (ppm)
Altoviski 1962
Boyd 2000
Todd 2007
Soft 0 - 75 0 - 50 0 – 60 Moderate Hard 75 - 175 50 - 150 60 - 120
Hard 175 - 300 150 - 300 120 – 180 Very hard > 300 > 300 > 180
TH values for both periods table (3.16) were compared with classifications of
water hardness ( Altoviski, 1962 ; Boyd,2000, and Todd, 2007)(Table 3.17) and
Chapter Three Hydrochemistry
52
as a result the groundwater in the studied area is classified as very hard water due
to the presence of dissolved calcium and magnesium salts .
3.6 Nitrate (NO3-)
The source of Nitrate ion (NO3-) in natural water is from organic sources or
from agricultural activities due to the use of fertilizers. . The chemical fertilizers
represents the main source of the ion . Animal waste, plant remains, industry and
sewage disposal are considered another sources for nitrate (Hudak,2000 and AL-
Badri & AL-Ameri, 2004).Nitrate has a significant influence on plant growth and
may present a hazard for drinking water sources if Nitrate levels are (10ppm) or
more( Landschoot, 2007 ).The (NO3-) concentration of water samples is given in
table (3.18),and appendices (4,5). Table (3.18) The NO3
- concentration of water samples of the studied area NO3
- (ppm) Dry period Wet period
Range 0.2 – 8 1.3 – 9
Average 3.25 4.83
Nitrate concentration in wet period is greater and this can be attributed to the
agricultural activities ( fertilizers use) in the recharge regions, in addition to the
agricultural activities and sewage disposal effect in the study area .
3.7 Heavy elements (Trace elements)
Heavy metals are natural components of the earth’s crust and it refers to any
metallic chemical element that has a relatively high density (more than 5 g/mL)
and is toxic at low concentrations (Berkowitz et al., 2008). Study of heavy
elements concentrations in the water is of great importance due to their direct
influence on human health and animals and plants living. The source of these
elements is from rocks weathering and human activities (agricultural and
industrial activities) (Drever,1997).The inorganic industrial materials is considered
essential source for water contaminate by heavy elements ( Manahan, 2001).
Chapter Three Hydrochemistry
53
3.7.1 Iron (Fe)
Iron is considered abundant metallic element in rocks and soil of the earth’s
crust. The element is essential in the life processes of plants and animals
(Fetter, 1980). Iron is essential for human, but it becomes toxic when the
concentration increases. The source of iron in water is from weathering of igneous
rocks such as(pyroxenes, amphiboles, biotite, magnetite, hematite and olivine),
sedimentary rocks and clay minerals (Boyd,2000). The fertilizers are considered
another source for iron . Iron concentration in Iraqi fertilizers TSP, MAP, NP and
NPK are 0.32, 0.34, 0.18, and 0.15 respectively (AL-Qaraghuli,1987). Iron
concentration of water samples of the studied area range between (0.004 - 0.409
ppm) with an average of (0.13 ppm) (appendix 8). It is clear that the wells
No.(7,10) contain higher iron ion than the permissible concentration in comparison
with table (3.19).This high concentration of iron can be attributed to the
agricultural activities (fertilizers uses) because these wells are located within
agricultural regions, in addition to weathering of clay minerals in Quaternary
deposits which cover the studied area.
3.7.2 Cobalt (Co)
The behavior of cobalt compounds is similar to that of iron compounds ,while
the ratio of cobalt in sediments and soil are less than iron and the solubility of
cobalt carbonate CoCO₃ is less than that of iron carbonate minerals (Boyd, 2000).
The source of cobalt ion(Co) in water is from weathering of minerals and rocks
which contain cobalt.(Co) is available in many minerals such as(Cobalite, Erthrite,
Glaucodot)(Emsley,1998). Fertilizers, industrial activities(metal) and waste
disposal are considered another sources for cobalt (Hem,1985).Cobalt
concentration in Iraqi fertilizers TSP, MAP, NP and NPK are 20, 16 , 10 and
10ppm respectively(AL-Qaraghuli,2005). (Co) is essential in plant and animal
nutrition, but excessive amounts will be harmful to human life (Prasad,2008).
Cobalt concentrations of water samples of the studied area range between (0.008 -
0.457 ppm) with an average of (0.17ppm) (appendix 8). It is clear that all wells of
Chapter Three Hydrochemistry
54
the study area are polluted with cobalt ion because its concentration exceed the
permissible limit in comparison with table (3.19) except the wells No.(4,16,17,18).
And this may be attributed to agricultural activities ( fertilizers uses ) in the
recharge regions, in addition to agricultural and industrial activities and waste
disposal in the study area .
3.7.3 Nickel (Ni)
(Ni) enters the environment through natural process like weathering of minerals
and from dissolution of rocks and soils ,as well as from biological cycles and
industrial processes. (Ni) present in soil in mainly sulphide and oxide forms and
its concentration may vary according to mineral composition of soil (Berkowitz et
al.,2008) . Nickel present in the sewage disposal (Alloway and Ayers, 1997). Ni
present in minerals (Carniorite, Millerite, Nicolite and Pentlandite)(Emsley,1998).
(Ni) concentration in Iraqi fertilizers TSP, MAP, NP and NPK are 88, 85, 50 and
48 ppm respectively(AL-Qaraghuli ,2005).Nickel concentration in water samples
of the studied area range between (0.012 - 0.085 ppm) with an average of ( 0.046
ppm) (appendix 8).By comparing nickel concentrations of water samples with
standard specification concentration table (3.19), it becomes apparent that all wells
of the study area are polluted with nickel ion because its concentration exceed the
permissible limit except the wells No. (4,8,16). And this may be attributed to
dissolution processes of soils and agricultural activities ( fertilizers uses ) in the
recharge areas, in addition to agricultural and industrial activities and waste
disposal in the study area.
3.7.4 Copper (Cu)
The quantity of copper compounds in nature is little or rare. (Cu) enters
groundwater and surface water from weathering of minerals and rocks which
contain (Cu). Copper is available in many minerals (Azurite, Malachite,
Brochanthite, Chalconthite and Chalcopyrite) (Emsley,1998). Fertilizers
, agricultural pesticide , the Cu which might be dissolved from water pipes and
plumbing fixtures especially by water whose pH is below 7 are considered another
Chapter Three Hydrochemistry
55
sources for (Cu) (Hem, 1985). (Cu) concentration in Iraqi fertilizers TSP, MAP,
NP and NPK are 32, 32, 17 and 14 ppm Cu respectively (AL-Qaraghuli, 2005).
(Cu ) is an essential element in plant and animal (kirk – Othmer, 1980). Cu is
considered toxic for human life if its concentration exceed the permissive limit in
drinking water (WHO,2007 ) .Copper concentration of water samples of the
studied area range between (0.006 - 0.124 ppm) with an average of ( 0.027 ppm)
( appendix 8). It is clear that the copper concentration in the area water is less than
the permissible limits in comparison with table (3.19).This reflects no copper
pollution in the groundwater of the study area.
3.7.5 Zinc (Zn)
Concentration of free zinc ion in the earth's crust is low because the minerals
which contain zinc ion have low solubility within the pH range of most natural
water (Boyd, 2000).The source of zinc in water is from weathering the minerals
and rocks which contain (Zn) . Zinc is available in many minerals such as
(Sphalerite, Smithsonite, Willemite, Biotitie, Amphibole and Hemimorphite)
(Emsley, 1998). Fertilizers, animal organic remains and the industrial activities are
considered another sources of zinc (Hem, 1985). Zn concentration in Iraqi
fertilizers TSP, MAP, NP and NPK are 594, 688, 286 and 240 ppm respectively
(AL-Qaraghuli, 2005). Zn is essential element in plant and animal but excessive
amounts will be harmful to human life (WHO,2007).Zinc concentration of water
samples of the studied area range between ( 0.005 - 0.599 ppm) with an average of
( 0.083 ppm) (appendix 8). Zinc concentration in the area water is less than the
permissible limits in comparison with table (3.19).This means no Zinc pollution in
the groundwater of the study area.
3.7.6 Cadmium (Cd)
The geochemical characters of cadmium is similar to that of zinc but (Cd ) is
much less abundant in earth's crust (Hem, 1985). It is considered relatively rare in
the geological deposits, occurring mainly in carbonate and hydroxide forms
(Boyd, 2000). Cadmium represents a highly toxic element and is unnecessary for
Chapter Three Hydrochemistry
56
the human living and animals ( Manahan, 2001). Excessive amounts (more than
10µg/L) in drinking and irrigation water will be toxic (Prasad,2008).It enters the
environment from weathering the minerals and rocks which contain (Cd).
Cadmium is available in many minerals such as(Cadmoselite, Greenockite and
Olarite) (Emsley,1998). Another sources of (Cd) are fertilizers, industrial activities
(metallurgical processes, pigments and paints), sewage and waste disposal
(Hem,1985). (Cd) concentration in Iraqi fertilizers TSP, MAP, NP and NPK are
21, 27, 11, and 8 ppm respectively(AL-Qaraghuli,2005). Cadmium concentration
of water samples of the studied area range between ( 0.002 - 0.187 ppm) with an
average of ( 0.055 ppm) (appendix 8). It is clear that all wells of the study area are
polluted with cadmium ion because its concentration exceed the permissible limit
in comparison with table (3.19) except the wells No.(2,9,14,15,16,20). This may
be attributed to agricultural activities ( fertilizers uses ) in the recharge areas, in
addition to the agricultural and industrial activities and waste disposal in the study
area.
3.7.7 Lead (Pb)
The quantity of lead ion in surface and groundwater is little because the
minerals which contain lead ion have low solubility in water and also its natural
mobility is low (Drever,1997). Weathering of minerals and rocks which contain
lead ion liberate (pb) to environment. Lead ion is available in many minerals such
as (galena (pbS), cerussite (pbCo3) and anglesite (pbSo4) (Emsley,1998) .
Fertilizers, industrial activates (batteries and paints) and human activities are
considered another sources of (pb) (Hem,1985). (Pb) concentration in Iraqi
fertilizers TSP, MAP, NP and NPK are 52, 42, 38, and 38 ppm respectively
(AL-Qaraghuli, 2005). Lead concentration of water samples of the studied area
range between (0.050 - 0.353 ppm)with an average of ( 0.192 ppm) (appendix 8).
It is clear that all wells of the study area are polluted with lead ion because its
concentration exceed the permissible limit in comparison with table (3.19) except
the well No.(9). This may be attributed to agricultural activities ( fertilizers uses )
Chapter Three Hydrochemistry
57
in the recharge areas, in addition to agricultural and industrial activities and human
activities in the study area.
3.7.8 Manganese (Mn)
The chemistry of manganese is somewhat like that of iron in that both metals
participate in redox processes in weathering environments . Many igneous and
metamorphic minerals contain divalent manganese as a minor constituent. It is a
significant constituent of basalt and many olivines and of pyroxene and
amphibole. Small amounts commonly are present in dolomite and limestone
substituting for calcium (Hem,1985). The fertilizers are considered another source
for (Mn). (Mn) concentration in Iraqi fertilizers TSP, MAP, NP and NPK are
43,36,34, and 18 ppm respectively (AL-Qaraghuli,1987). Manganese concentration
of water samples of the studied area range between ( 0.002 - 0.058 ppm) with an
average of ( 0.019 ppm) (appendix 8). Manganese concentration in the area water
is less than the permissible limit in comparison with table (3.19).This means no
Manganese pollution in the groundwater of the study area .
From the above, it can be observed that the groundwater in the study area is
polluted by elements ( Co , Ni , Cd and Pb ) because the concentrations of these
elements exceeds the permissible limits in comparison with standard specifications
[Iraqi standard (IQS, 2009) and world health organization standard (WHO 2007) ]
as a result of weathering and dissolution actions, in addition to the effect of the
Iraqi fertilizers which are used in agriculture and human activities .
Chapter Three Hydrochemistry
58
Table (3.19) Standards specifications for trace elements in natural water.
No. Elements WHO(2007) ppm
IQS(2009) ppm
Present study
average
ppm 1 Fe 0.3 0.3 0.13
2 Co ---- 0.05 0.17
3 Ni 0.02 0.02 0.046
4 Cu 1 1 0.027
5 Zn 3 3 0.083
6 Cd 0.003 0.003 0.055
7 Mn 0.1 0.1 0.019
8 Pb 0.01 0.01 0.192
Chapter Four Groundwater Classification and Management
59
Chapter Four Groundwater Classification and Management
4.1 Hydrochemical formula and water type :
4.1.1 Hydrochemical Formula (Kurolov formula)
The groundwater quality is simply the result of the geology and hydrology of
the area (Stevanovic and Iurkiewicz , 2009). The water type determining is very
important to determine its suitability for the different uses (human, agricultural and
industrial).Therefore the type of groundwater in the study area is determined
according to Kurolov formula .This formula depends on the ratio of the main ions,
(cations and anions) expressed by (Equivalent per million %) i.e (epm %) that are
arranged in descending order which have more than (15%) ratio of availability.
The cations are located at the base while the anions above. Furthermore, TDS
value is put in (mg/L) unit and (pH) value as in the following formula (Ivanov,et
al, 1968) as follows:
Anions epm% decreasing order TDS mg / L ——————————————— pH Cations epm% decreasing order
From appendices (9,10) which explain hydrochemical formula and water type
for water samples of study area , the hydrochemical Kurolov formulas for water
quality in the study area are represented by five groups determined as follows:
- Ca+2 – Mg+2 - Sodium – Cl- - HCO₃- - Sulfate _ Na2SO4
- Mg+2 - Ca+2 - Sodium - HCO₃- - SO₄-2 - Chloride _ NaCl
- Mg +2- Na+ - Calcium - HCO₃- - SO₄-2 - Chloride _ CaCl2
- Mg+2 – Na+ - Calcium - HCO₃- - Cl- - Sulfate _ CaSO4
- Ca+2 – Na+ - Magnesium – Cl- - HCO₃- - Sulfate _ MgSO4
The predominant salts in water samples are (Na2SO4) ,(NaCl),( CaCl2), (CaSO4)
and (MgSO4) for both periods.
Chapter Four Groundwater Classification and Management
60
Table (4.1) Predominant salts of water samples in the study area
Dry Period Wet Period
Hydrochemicl Formula
(water type)
Predominant
salts Frequency
Occurs Ratio (%)
Hydrochemicl Formula
(water type)
Predominant
salts Frequency
Occurs Ratio (%)
Ca+2 - Mg+2 -
Sodium - Cl- -
HCO₃- - Sulfate
Na2SO4 12 60%
Ca+2 – Mg+2 -
Sodium – Cl- - HCO₃-
- Sulfate Na2SO4 8 40%
Mg+2 – Ca+2 -
Sodium - HCO₃- -
SO₄-2 - Chloride
NaCl 5 25%
Mg+2 – Ca+2 -
Sodium - HCO₃- -
SO₄-2 - Chloride NaCl 5 25%
Mg+2 – Na+ -
Calcium - HCO₃- -
SO₄-2 - Chloride
CaCl2 2 10%
Mg+2 – Na+ -
Calcium - HCO₃- -
SO₄-2 - Chloride CaCl2 3 15%
Mg+2 – Na+ -
Calcium - HCO₃- -
Cl- - Sulfate
CaSO4 1 5%
Mg+2 – Na+ -
Calcium - HCO₃- -
Cl- - Sulfate CaSO4 2 10%
Ca+2 – Na+ -
Magnesium – Cl- -
HCO₃- - Sulfate
MgSO₄ 2 10%
Table (4.1) shows the hydrochemical formula and their prevailing salts and
their percentage ratio in the water of the study area. It is clear that the prevailing
salt in the study area is (Na2SO4) where its concentration averages reach (60%) in
dry period shown in(12) wells and (40%) in wet period shown in (8) wells. Five
wells in the dry period and five in wet period are of (NaCl) prevailed salt type
which represents the second prevailing salt in the study area with a ratio of (25%)
,where most of it is located in the groundwater discharge area especially in wet
period (Fig.4.1). This is due to dilution processes by Tuz Chai river and the water
seepage from Kirkuk irrigation canal .The remainder of wells varies between
(CaCl2),( CaSO4) and (MgSO4) water type for both periods . Generally the salts
distribution in the area is attributed to the lithology of recharge regions and the
Chapter Four Groundwater Classification and Management
61
study area as a result of weathering and dissolution actions of rocks and clay
minerals, in addition to the agricultural and human activities. The source of sulfate
ion in the area is from gypsum rocks for Al-Fat'ha Formation, which appears in
Pulkhana anticline . Fig. (4.1) shows the water quality in the study area for both
periods ,it is clear that the difference in water quality between both dry and wet
period occur as a result of recharge and dilution processes in the wet period.
4.1.2 Hypothetical salts
Hypothetical salts of water samples of the study area can be calculated by
correlation between the anions and cations according to the salts deposition
sequence as shown in table (4.2) (Collins, 1975). Table (4.2) The reaction order of the hypothetical salts Reaction
order Ions 1 2 3 Cl- SO4
-2 HCO3-
1 K+ KCl K2SO4 KHCO3 2 Na+ NaCl Na2SO4 NaHCO3 3 Mg+2 MgCl2 MgSO4 Mg(HCO3)2 4 Ca+2 CaCl2 CaSO4 Ca(HCO3)2
Appendix (11) shows the hypothetical salts for water samples of study area for
both periods .Table (4.3) shows the average of hypothetical salts values for both
periods. It is clear the prevailing salts of water samples of study area are sulfate
and bicarbonate salts represented by Magnesium Sulfate(MgSO4), Calcium Sulfate
(CaSO4) , Sodium Sulfate (Na2SO4) and Calcium Bicarbonate Ca(HCO3)2 .This
indicates a meteoric origin of water which percolate underground through the
formation outcrops and mixing with deep groundwater of marine origin.
Table (4.3) Average of hypothetical salts values for water samples of study area
Hypothetical salts
KCl NaCl MgCl2 CaCl2 K2SO4 Na2SO4 MgSO4 CaSO4 NaHCO3 Mg(HCO3)2 Ca(HCO3)2
Dry period
average
0.32 36.41 1.46 0 0 9.08 21.49 16 0 0.008 14.71
Wet period
average
0.38 33.19 2.79 0 0 6.51 23.46 9.34 0 0 24.28
Chapter Four Groundwater Classification and Management
62
(A)
(B) Fig. 4.1 : Water quality of the study area
(A) Dry period (B) Wet period
Chapter Four Groundwater Classification and Management
63
4.1.3 Hydrochemical indicators
Study of hydrochemical indicators for the water is necessary to delineate the
origin of water, in addition to comparison between ions concentration and sea
water (Fetter, 1980). Ivanov (1968) classified water into two groups, depending on
the genetic origin :
1- Meteoric water
2- Marine water
Chloride ion used to know the geochemical behaviour for main elements by
the ratio of main elements to chloride because (Cl-) is the most dissolve ion and
less influenced by physical and chemical changes in water. In addition, it is not
influenced by adsorption process and exchange of ion by the clay minerals
(Levy, 1974). If the indicators are greater than one then the water is from meteoric
origin and less than one is for water from marine origin (Ivanov, 1968).
Appendix (12) shows the hydrochemical indicators for water samples of study
area for both periods . Table (4.4 ) shows the average of hydrochemical indicators
of groundwater for the two periods. It is clear the values of hydrochemical
indicators are greater than one which means the ratio of sulfates exceeds the
chloride ratio and the origin of groundwater is meteoric, except the wells
No.(1,2,8,9,13,20) whose indicators are less than one. This reflects that the
chloride ion is the prevailing ion and the origin of groundwater is marine. This can
be attributed to the existence of a deep recharge from the deeper aquifers in these
wells. The value of (rNa/rCl) indicator in the wells No.(2,8) are close to one which
means a high and strong dilution but it dose not exceed one. The difference is due
to recharge processes and the artesian pressure of the deep wells in addition to
drawn from meteoric water.
Chapter Four Groundwater Classification and Management
64
Table (4.4) Average of hydrochemical indicators for water samples of study area for the
two periods
Well
no.
rCa /rCl
rMg/rCl
rNa/rCl
rK/rCl
rSO₄ /rCl
rNa+rK rCl
(Na+rK)-Cl rSO₄
Water Origin
1 0.965 0.76 0.8 0.00505 0.845 0.805 -0.2635 Marine
2 0.87 0.585 0.975 0.0029 0.83 0.975 -0.055 Marine
3 1.005 0.795 1.62 0.0085 1.81 1.625 0.34 Meteoric
4 0.875 0.475 1.29 0.0063 1.415 1.295 0.21 Meteoric
5 1.03 0.8 1.42 0.00755 1.64 1.43 0.165 Meteoric
6 1.04 0.655 1.58 0.0117 1.56 1.59 0.375 Meteoric
7 1.13 0.69 1.5 0.0118 1.65 1.505 0.31 Meteoric
8 0.67 0.435 0.97 0.02 0.705 0.99 -0.017 Marine
9 0.75 0.54 0.825 0.022 0.725 0.85 -0.219 Marine
10 0.87 0.66 1.46 0.00345 1.305 1.46 0.335 Meteoric
11 1.07 0.835 1.2 0.01135 1.455 1.21 0.145 Meteoric
12 0.835 0.635 1.12 0.018 1.375 1.14 0.0865 Meteoric
13 0.89 0.755 0.855 0.00435 1.16 0.86 -0.11 Marine
14 1.02 1.23 1.225 0.00305 1.455 1.23 0.155 Meteoric
15 1.005 0.805 1.3 0.0047 1.485 1.305 0.1 Meteoric
16 0.905 0.865 1.365 0.0067 1.465 1.37 0.25 Meteoric
17 0.595 0.325 1.06 0.0063 0.865 1.065 0.03 Meteoric
18 0.765 0.59 1.205 0.014 0.925 1.22 0.22 Meteoric
19 0.955 0.82 1.055 0.0027 1.215 1.06 0.02 Meteoric
20 0.69 0.645 0.87 0.0085 0.65 0.875 -0.2635 Marine
Chapter Four Groundwater Classification and Management
65
4.2 Classification of water
There are many methods for hydrochemical classification like (Piper, 1944;
Sulin,1946;Schoeller,1972;Collins,1975; and Chadha,1999). These methods are
used to determine the quality and the important properties of groundwater. All
these classifications depend on the main cations and anions concentrations by unit
equivalent weight of ion (epm) or mile equivalent per liter (mg/L). Piper (1944)
and Chadha (1999) classifications are applied in the present study as follows :
4.2.1 Piper Classification (1944)
Piper (1944) proposed a trilinear diagram that permits the classification of
water. The Piper trinlinear diagram is consists of two trilinear plots and a diamond
plot. These diagrams depend on dissolved contents in natural water which
represent cations and anions by unit equivalent per million of ion (epm) or mile
equivalent per liter (mg/L).The Rock Work software was used for plotting this
diagram to display the relative concentrations of the different ions in water samples
in the study area. Based on the main cations and anions Piper trinlinear diagram
and according to Langguth (1966) divided into seven types (Fig. 4.2) as follows :
Normal earth Alkaline water :
a- with prevailing bicarbonate
b- with prevailing bicarbonate and sulfate or chloride
c- with prevailing sulfate or chloride
Earth Alkaline water with increase portion of alkalis :
d- with prevailing bicarbonate
e- with prevailing sulfate and chloride
Alkaline water :
f- with prevailing bicarbonate
g- with prevailing sulfate and chloride
Chapter Four Groundwater Classification and Management
66
Fig. 4.2 : Piper (1944) Trilinear diagram with Langguth (1966) classification.
The results of the analyzed samples of study area for wet and dry periods by
(ppm) unit (appendices 4,5) are plotted on Piper diagrams as shown in Fig.(4.3) . It
is clear that all groundwater samples for the two periods are located in (e) and (g)
hydrochemical facies (Fig.4.2).Therefore this means the type of groundwater
samples of study area for dry and wet periods is " earth alkaline water with
increased portions of alkalis with prevailing sulfate and chloride" and " Alkaline
water with prevailing sulfate and chloride" respectively, and the major
hydrochemical facies being (Ca2+ - Mg2+ - Cl- - SO4
2- ) and (Na+- K+ - Cl- - SO4
2-)
for the two periods.
Chapter Four Groundwater Classification and Management
67
(A)
(B)
Fig. 4.3 : Piper diagram for water samples of study area
(A)Dry period (B)Wet period
Chapter Four Groundwater Classification and Management
68
4.2.2 Chadha classification (1999)
Chadha diagram is constructed by plotting the difference between alkaline earth
and alkali metals and the difference between weak acidic anions and strong acidic
anions by milliequivalent percentage (epm%) on the axises of X and Y. X- axis
represents the difference between Alkaline earth and Alkaline metallic
[(Ca+2 +Mg+2
) - (Na+ + K+ )](epm %), while Y-axis represents the difference
between weak and strong acids [(HCO₃⁻ + CO₃⁻² ) – ( Cl⁻ + SO4⁻²)] (epm %)
(Chadha,1999). Chadha classification can be used to interprets the general
properties of water for more accurate details which are not available in the Piper
classification .Chadha divided the plotting into eight parts each part represents one
type of water (Fig.4.4 ) as follows:
1- Alkaline earths exceed alkali metals.
2- Alkali metals exceed alkaline earths.
3- Weak acids anions exceed strong acids anions.
4- Strong acids anions exceed weak acids anions.
5- Alkaline earths exceed alkali metals and weak acids anions exceed strong acids
anions. This type has temporary hardness ; represented by Ca2+-Mg2+- HCO3--
type, Ca2+-Mg2+- dominant HCO3-- type, or HCO3
-dominant Ca2+-Mg2+- type
water.
6- Alkaline earths exceed alkali metals and strong acids anions exceed weak acids
anions. This type has permanent hardness and not residual sodium carbonate
Na2CO₃ in irrigation use; represented by Ca2+-Mg2+-Cl- water type, and Ca2+-
Mg2+ dominant - Cl- type, or Cl--dominant Ca2+-Mg2+ type water.
7- Alkali metals exceed alkaline earths and strong acids anions exceed weak acids
anions. This type generally creates salinity problems both in irrigation and
drinking uses ;represented by Na+-Cl--type, Na2SO4-type, Na+-dominant Cl--
type, or Cl--dominant Na+-type water.
Chapter Four Groundwater Classification and Management
69
8- Alkali metals exceed alkaline earths and weak acids exceed strong acids. This
type deposit residual sodium carbonate in irrigation and cause foaming
problems ;represented by Na+ - HCO3--type, Na+-dominant HCO3
--type, or
HCO3- -dominant Na+-type water.
Fig. 4.4 : Chadha diagram
The results of the analyzed samples of study area for wet and dry periods by
(epm%) unit (appendices 6,7) are plotted on Chadha diagrams as shown in
Fig.(4.5). It is clear that the water samples No.(1, 3, 4, 5, 7, 11 ,12, 13.14.15,19,20)
and samples No.( 2,6,8,9,10,16,17,18) in dry period are located within (part 6) and
(part 7) respectively , while in wet period all the water samples are located within
(part 6) except the sample No. (12) is located in (part7).
Therefore, this means that the type of groundwater samples for both periods for
the samples which fall in (part 6) is (alkaline earths exceed alkali metals and strong
acids anions exceed weak acids anions ) .This type is characterized by Ca2+-Mg2+
Chapter Four Groundwater Classification and Management
70
(A)
(B) Fig. 4.5 : Chadha classification (1999) for water samples of study area,
(A)Dry period (B)Wet period
Chapter Four Groundwater Classification and Management
71
-Cl- water type, and Ca2+-Mg2+ dominant - Cl- type, or Cl--dominant Ca2+-Mg2+
type water . While water type for the samples which fall in (part 7) is alkali metals
exceed alkaline earths and strong acidic anions exceed weak acidic anions
represent Na+-Cl--type, Na2SO4-type, Na+-dominant Cl--type, or Cl--dominant Na+-
type water.
4.3 Groundwater suitability for different purposes
Groundwater in the studied area is used for different purposes (drinking
, industrial and agricultural),where the area depends on the irrigation canal and
groundwater for drinking water supply(tap water)for population . Therefore it is
necessary to evaluate groundwater suitability for these purposes and especially for
human drinking .This evaluation is normally carried out by comparing its
hydrochemical parameters with some standard limits set for the different purposes
as follows :
4.3.1 Groundwater suitability for human drinking purposes.
Water for human consumption must be free from organisms and chemical
substances in concentration large enough to affect health adversely (Hamill and
Bell,1986). Groundwater suitability depends on several parameters (major and
minor elements , inorganic , organic chemicals and biological constituents) . For
the purpose of evaluating the suitability of groundwater for human drinking , Iraqi
standard (IQS, 2009) and World Health Organization standard (WHO 2007) were
used to determine its suitability as drinking water in the study area .
The average of two periods ( dry and wet) for the analyzed water samples by
(ppm) unit (appendices 4,5 ) are compared with WHO,(2007) and IQS(2009)
standards as shown in table (4.5). As a result the groundwater in study area is
unsuitable for human drinking purposes , where in the case of suitable ones
element, the another element is not suitable.
Chapter Four Groundwater Classification and Management
72
Table (4.5) Comparison of groundwater samples (ppm) in the study area with IQS and
WHO standards.
Parameters
Dry period Wet period Average of two periods
Iraqi Standard
2009
WHO Standard
2007
Exceeding limits
Range Average Range Average
pH 7.17 - 8.2 7.71 7.12- 7.92 7.40 7.55 6.5 - 8.5 6.5 - 8.5 Not exceed
TDS 339 - 2415 1279.85 241 - 2287 1027.55 1153.7 1000 1000 Exceed
EC 546 - 3500 1901.4 363 - 3402 1607.2 1754.3 1500 1530 Exceed
TH 127.6 – 1166.6 512.9 118.85 – 1082.21 435.22 474.06 500 500 Not exceed
Ca2+ 33 - 253 117.5 26.01 - 234 96.44 106.97 150 75 Not exceed
Mg2+ 11 - 130 53.3 10.1 - 121 47.24 50.27 100 125 Not exceed
Na+ 61 - 345 185.9 42 - 345 131.86 158.88 200 200 Not exceed
K+ 0.3 – 5.5 2.2 0.7 – 5.4 1.50 1.85 12 12 Not exceed
Cl- 89 – 468.6 242.8 49.7 - 460 173.07 207.93 350 250 Not exceed
SO42- 108 - 844 409.6 43.2 - 844 294.95 352.27 400 250 Not exceed
HCO₃‾ 12.8 - 611 186.6 18 - 446 214.71 200.65 200 200 Exceed
NO3- 0.2 - 8 3.25 1.3 - 9 4.83 4.04 50 50 Not exceed
Fe 0.004 – 0.409 0.13 ---- ---- 0.13 0.3 0.3 Not exceed
Co 0.008 – 0.457 0.17 ---- ---- 0.17 ---- 0.05 Exceed
Ni 0.012 – 0.085 0.046 ---- ---- 0.046 0.02 0.02 Exceed
Cu 0.006 – 0.124 0.027 ---- ---- 0.027 1 1 Not exceed
Zn 0.005 – 0.599 0.083 ---- ---- 0.083 3 3 Not exceed
Cd 0.002 – 0.187 0.055 ---- ---- 0.055 0.003 0.003 Exceed
Mn 0.002 – 0.058 0.019 ---- ---- 0.019 0.1 0.1 Not exceed
Pb 0.050 – 0.353 0.192 ---- ---- 0.192 0.01 0.01 Exceed
Chapter Four Groundwater Classification and Management
73
4.3.2 Groundwater suitability for livestock purposes
The results of the analyzed samples of the study area for both periods by (ppm)
unit (appendices 4,5 ) are evaluated for livestock and poultry purposes by using
classifications proposed by Altoviski(1962), Crist and Lowery(1972) and Ayers
and Westcot(1989) are shown in table (4.6),table (4.7 ) and table (4.8 )
respectively. It is clear that all water samples in the study area are :
Very good for animal drinking according to Altoviski (1962) classification .
Acceptable for all types of animals and poultry according to Crist and Lowery
(1972) classification.
Very satisfactory for all types of livestock and poultry, according to the
classification given by Ayers and Westcot (1989). Table (4.6) Water specifications for the purpose of animal consumption according to
Altoviski(1962 )
parameters Very good Good permissible Can be
used High limits
Average of two periods
Na+ 800 1500 2000 2500 4000 158.88 Ca2+ 350 700 800 900 1000 106.97 Mg2+ 150 350 500 600 700 50.27 Cl- 900 2000 3000 4000 6000 207.93
SO42- 1000 25000 3000 4000 6000 352.27
TDS 3000 5000 7000 10000 15000 1153.7 TH 1500 3200 4000 4700 64000 474.06
Table (4.7) Water specifications for the purpose of animal consumption according to
Crist and Lowery(1972). Salinity (ppm) quality animal
Less than 1000 good poultry \ to 2860
1000 - 3000 Acceptable
3000 - 5000 weak Horses\ to 7150
5000 - 7000 very weak
More than 7000 unacceptable Cow \ to 10000 sheep\ to 12900
Chapter Four Groundwater Classification and Management
74
Table (4.8) Water specifications for the purpose of animal consumption according to Ayers and Westcot(1989).
Notes Rating EC (µS/cm) Suitable for all classes of livestock and poultry. Excellent
< 1500
Suitable for all classes of livestock and poultry. May cause temporary diarrhoea in livestock not accustomed to such water; watery droppings in poultry.
Very Satisfactory
1500 - 5000
May cause temporary diarrhoea or be refused at first by animals not accustomed to such water.
Satisfactory for Livestock
5000 - 8000 Often causes watery faeces, increased mortality and decreased growth, especially in turkeys.
Unfit for Poultry
Suitable with reasonable safety for dairy and beef cattle, sheep, swine and horses. Avoid use for pregnant or lactating animals.
Limited Use for
Livestock
8000 - 11000
Not acceptable for poultry. Unfit for Poultry
Unfit for poultry and probably unfit for swine. Considerable risk in using for pregnant or lactating cows, horses or sheep, or for the young of these species. In general, use should be avoided although older ruminants, horses, poultry and swine may subsist on water such as
these under certain conditions.
Very Limited Use
11000 - 16000
Risk with such highly saline water is so great that it cannot be recommended for use under any conditions.
Not Recommended
>16000
4.3.3 Groundwater suitability for industrial purposes
The results of the analyzed samples of the study area for both periods by
(ppm) unit (appendices 4,5 ) are evaluated for industrial purposes by using
classification suggested by Hem (1985) is shown in table (4.9). It is clear that
all water samples are not suitable for industrial purposes, where in the case of
suitable ones element, the another element is not suitable.
Gravel and sand quarries are widespread in the study area , where they use
the groundwater for gravel and sand washing in addition to industrial processes.
Chapter Four Groundwater Classification and Management
75
Table (4.9) Suitability of water for industrial purposes (Hem, 1985) Pa
ram
eter
s
Tex
tiles
Chemical pulp
and paper
Woo
d ch
emic
als
Synt
hetic
ru
bber
Petr
oleu
m
prod
ucts
Can
ned,
dri
ed,
froz
en fr
uits
an
d ve
geta
bles
Soft-
drin
ks
bottl
ing
leat
her
tann
ing
Hyd
raul
ic
cem
ent
man
ufac
ture
U
nble
ache
d
Bl
each
ed
Ca² -- 20 20 100 80 75 -- 100 -- --
Mg+² -- 12 12 50 36 30 -- -- -- --
CL⁻ -- 200 200 500 -- 300 250 500 250 250
SO42- 0 -- -- 100 -- -- 250 500 250 250
HCO₃⁻ 0 -- -- 250 -- -- -- -- -- --
NO₃⁻ 0 -- -- 5 -- -- 10 -- -- --
Cu 0.01 -- -- -- -- -- -- 500 -- --
Zn -- -- -- -- -- -- -- -- -- --
pH 2.5 – 10.5 6 - 10 6 - 10 6.5- 8.0 6.5 – 8.3 6 - 9 6.5 – 8.5 -- 6 - 8 6.5 - 8.5
TDS 100 -- -- 1000 -- 1000 500 -- -- 600
TH 25 100 100 900 350 350 250 -- Soft --
4.3.4 Groundwater suitability for building purposes
Suitability of groundwater in the study area is evaluated for building purposes
by using classification proposed by Altoviski (1962) as shown in table(4.10) .The
average concentrations of groundwater samples by (ppm) unit (appendices 4,5 )
were compared with Altoviski (1962) standard . It is clear that all water samples in
the study area are suitable for building purposes.
4.3.5 Groundwater suitability for agriculture purpose
The productivity of agricultural crops depends on the quality of plants, its
resistance to environmental conditions, its ability to retain water ,the properties of
the soil structure , the irrigation method used and other factors . The plants
tolerance for total dissolved solids and electrical conductivity in water which uses
in irrigation are different depends on the quality of plants (Todd,1980) .
Chapter Four Groundwater Classification and Management
76
According to classification proposed by Todd (2007) as shown in table (4.11)
all water samples of the study area are suitable for growing most types of crops.
Table (4.10 ) Water suitability for building purposes compared with average
concentrations of samples according to Altoviski (1962)
Ions Permissible Limit
Average concentrations
Dry period Wet period
Na+ 1160 185.9 131.86
Ca2+ 437 117.5 96.44
Mg2+ 271 53.3 47.24
Cl- 2187 242.8 173.07
SO42-
1460 409.6 294.95
HCO3-
350 186.6 214.71
Table (4.11 ) Todd classification (2007) for the tolerance of crops by relative salt
concentrations for agriculture.
Crop Division Low Salt
Tolerance crops Ec (µS /cm)
Medium Salt Tolerance crops Ec (µS /cm)
High Salt Tolerance crops Ec (µS /cm)
Fruit Crops
0 - 3000
Limon, Strawbrry, Peach Spricot, Almond, Plum
Orange, Apple, Pear
3000 - 4000
Cantaloupe, Olive,
Figs, Pomegranate
4000 - 10,000
Date palm
Vegetable Crops
3000 - 4000
Green beans, Celery, Radish
4000 - 10,000 Cucumber, Peas, Onion Carrot, Potatoes, Sweet Corn, Lettuce, Cauliflower, Bell pepper, Cabbage, Broccoli, Tomato
10000 - 120,000
Spinach, Garden beets
Field Crops 4000 - 6000
Field beans
6000 - 10,000
Sunflower, Corn (field)
Rice, Wheat, (grain)
10,000 - 16,000
Cotton, Sugar beet Barley (grains)
Chapter Four Groundwater Classification and Management
77
4.3.6 Groundwater suitability for irrigation purposes
The (EC) and ( Na+) play a decisive role in verifying water suitability for
irrigation (Al-Manmi, 2008).The suitability of water for irrigation depends on the
kind and amount of salts present in the water and their effects on crop growth and
development. Salts are present in variable concentrations in all water and the salt
concentrations influence osmotic pressure of the soil solution. Plants can absorb
water readily when osmotic pressure is low, but absorption becomes more difficult
as the pressure increases (Glover, 1996) .There are many classifications to know
the suitability of water for irrigation purposes. They depend on several variables
including the cations , anions ,EC, TDS, pH, sodium adsorption ratio (SAR)
, soluble sodium percentage (Na%) and residual sodium carbonate (RSC) as
follows :
Sodium Adsorption Ratio (SAR)
The sodium adsorption ratio (SAR) indicates sodium concentration in water .
(SAR) is considered an important parameter for the evaluation of water suitability
for irrigation where the sodium accumulation in the soil will affect the rate of
water infiltration through the soil. (SAR) values used for estimation of infiltration
problems for soil that as a result of sodium increase with relative to the sum of
calcium and magnesium in a ratio of (1:3) , this will lead to soil crumble and
shrinking of the porosity (Ayres and Westcot, 1989).
(SAR) values are calculated according to the following equation (Todd,2007):
2
22 rMgrCa
rNaSAR
++
+
+=
…………………….. ( 4.1)
Where:
SAR: Sodium Adsorption Ratio.
rNa+, rCa+2 and rMg+2: Concentration of ions by (epm) uints.
Chapter Four Groundwater Classification and Management
78
The results of the analyzed samples of the study area for both periods by
(ppm) unit (appendices 4,5 ) are compared with Ayers and Westcot classification
(1989). It is clear that all groundwater samples are located within the permissible
limits except some wells exceeds the permissible limits are shown in table
(4.12).
Table (4-13) shows values of (SAR) for groundwater samples of the study area
for two periods. All (SAR) values lies within the permissible limits according to
Ayers and Westcot classification (1989) (Table 4.12) and Don classification (1995)
(Table 4.14).
Soluble Sodium Percentage ( Na%)
Increasing of sodium ion ratios in irrigation water will affect the soil where it
leads to decrease its porosity and permeability , thus will affect the plant growth or
stunted growth. (Na%) values were calculated according to the following equation
(Todd,2007):
rNa + rK Na% = –––––––––––––––––– ´ 100 ………………….(4.2) rCa + rMg + rNa + rK Where:
All ionic concentrations are expressed in milliequivalents per litter i.e. (epm).
Table (4-13) express values of (Na %) for groundwater samples of the study
area for two periods. ( Na%) values lies within the permissible limits according to
Don classification (1995) (Table 4.14 ).
Residual Sodium Carbonate (RSC)
The high concentration of bicarbonate in irrigation water lead to precipitation of
calcium and magnesium in the soil, Thus the sodium concentration will increase
(VanHoorn,1970) . Residual sodium carbonate (RSC) values are calculated
according to the following equation (Turgeon,2000):
RSC = ([CO32-] + [HCO3
-]) - ([Ca2+] + [Mg2+]) (epm) ……….(4.3)
Chapter Four Groundwater Classification and Management
79
Table (4.13) express values of ( RSC ) for groundwater samples of the study
area for two periods . It is clear all (RSC) values are low and negatively indicating
that sodium hazard is unlikely and lies within the permissible limits according to
Turgeon classification (2000) (Table 4.15) .
Table (4.12) Specification standards for irrigation water (Ayers and Westecot, 1989)
No. variables Unit Usual
Range Dry period Wet period
Not exceed Exceed Not exceed Exceed
1
Salinity
EC (µS/cm) 0 - 3000 All samples except No. 3,13,15
3,13,15 All samples except No. 3,13,15
3,13,15
TDS ppm 0 - 2000 All samples except No.
3,13 3,13
All samples except No. 3,13,15
3,13,15
2
Cations
Ca2+ epm 0 - 20 All samples ---- All samples -----
Mg2+
epm 0 – 5
All samples except No. 1,3,13,15,
19
1,3,13,15,19
All samples except No. 1,2,3,11,13,
14,15
1,2,3,11,13,14,1
5,
Na+ epm 0 - 40 All samples ----- All samples -----
3
Anions
Cl- epm 0 - 30 All samples ----- All samples -----
SO42- epm 0 - 20 All samples ----- All samples -----
HCO3- epm 0 - 10 All samples ----- All samples -----
CO32- epm 0 - 0.1 All samples ----- All samples -----
4
Nutrients
NO3 – N ppm 0 - 10 All samples ----- All samples ----- NH4 – N ppm 0 - 50 ----- ----- ----- ----- PO4 – P ppm 0 - 2 ----- ----- ----- -----
K+ ppm 0 - 2 2,3,4,9,10, 14,17,19,20
1,5,6,7,8,11,12,13,15,16,18
All samples except No.
3,13,18 3,13,18
5
Miscellane.
ous
B ppm 0 - 2 ----- ----- ----- -----
PH 1-14 6.0 - 8.5 All samples ----- All samples -----
SAR epm 0 - 15 All samples ----- All samples -----
Chapter Four Groundwater Classification and Management
80
Table (4.13) Values of (SAR, Na%, RSC) for water samples of the study area
Wells No.
Dry Period Wet Period SAR Na% RSC SAR Na% RSC
1 3.04 33.55 -11.91 2.16 30.76 -7.12 2 5.02 50.18 -7.34 2.28 30.22 -8.8 3 5.37 49.03 -11.04 4.77 45.56 -9.16 4 3.06 49.43 -3.87 2.96 48.3 -3.99 5 4.48 49.7 -8.01 2.47 35.25 -5.06 6 4.74 51.16 -8.22 3.31 46.1 -3.56 7 3.72 44.67 -8.87 3.37 45.67 -4.08 8 2.52 51.52 -2.56 1.63 43.03 -1.57 9 2.36 51.34 -2.34 0.92 30.75 -1.37
10 4.73 52.73 -6.26 3.35 46 -3.82 11 4.03 45 -10.08 2.43 33.85 -6.24 12 1.97 38.97 -4.45 2.47 50.84 -2.66 13 3.42 34.31 -15.45 3.42 34.28 -15.38 14 2.23 35.24 -4.63 2.37 35.48 -5.23 15 3.18 31.94 -13.31 5.37 49.05 -11.04 16 5.07 54.19 -7.07 2.25 35.16 -4.82 17 4.91 62.6 -3.5 1.72 42.61 -1.73 18 4.51 59.74 -3.86 1.94 37.48 -2.95 19 2.69 34.02 -8.68 2.52 39.95 -3.31 20 1.86 38.11 -2.38 1.64 41.64 -1.64
Table (4.14) Classification of Don (1995) for irrigation water
EC µS\cm
TDS ppm SAR Na% pH
Water
Quality 250 175 3 20 6.5 Excellent
250 -750 175 -525 3 – 5 20 -40 6.5 – 6.8 Good
750 -2000 525 -1400 5 – 10 40 – 60 6.8 – 7 Permissible
2000– 3000 1400 – 2100 10 – 15 60 – 80 7 – 8 Doubtful
> 3000 > 2100 > 15 > 80 > 8 Unsuitable
Chapter Four Groundwater Classification and Management
81
Table (4.15) Classification of irrigation water based on RSC values, according to
Turgeon (2000)
RSC Hazard
< 0 None.
0-1.25 Low, with some removal of calcium and magnesium from irrigation water.
1.25-2.50
Medium, with appreciable removal of calcium and magnesium from irrigation water.
> 2.50
High, with most calcium and magnesium removed leaving sodium to accumulate.
4.4 Suitability of water for irrigation according to US Salinity Laboratory
classification ,Richards diagram (1954)
U.S. salinity laboratory has classified groundwater to determine the suitability
of water for irrigation purposes based on electrical conductivity (EC) which is
plotted on the X - axis and sodium adsorption ration (SAR) drawn on the
Y - axis . The diagram is divided into 16 areas that are used to rate the degree to
which a particular water may give rise to salinity problems and undesirable ion-
exchange effects in soil (Hem, 1989) (Table 4.16 ). Based on this division the cases
of the use of water for irrigation purposes , salinity and sodium hazard can be
clarified as the following:
Low-salinity water (C1) can be used for irrigation on most crops in most soils with
little likelihood that soil salinity will develop.
Medium-salinity water (C2) can be used if a moderate amount of leaching occurs.
High-salinity water(C3) cannot be used on soils with restricted drainage.
Very high-salinity water (C4) is not suitable for irrigation under ordinary
conditions, but it may be used occasionally under very special circumstances.
Low-sodium water (S1) can be used for irrigation on almost all soils with little
danger of developing harmful levels of sodium.
Chapter Four Groundwater Classification and Management
82
Medium-sodium water (S2) may cause an alkalinity problem in fine textured soils
under low leaching conditions. It can be used on coarse textured soils with good
permeability.
High-sodium water (S3) may produce an alkalinity problem. This water requires
special soil management such as good drainage, heavy leaching, and possibly the
use of chemical amendments such as gypsum.
Very high sodium water (S4) is usually unsatisfactory for irrigation purposes. Table (4.16) Suitability of groundwater as irrigation water according to U.S. salinity
laboratory at Hem classification(1989)
Index water Class Dry Period Wet Period
C1S1 Excellent ----- -----
C1S2 Good ----- -----
C1S3 Admissible ----- -----
C1S4 Poor ----- -----
C2S1 Good 8 , 9 8,9,12,17,20
C2S2 Good ----- -----
C2S3 Marginal ----- -----
C2S4 Admissible ----- -----
C3S1 Admissible 4,7,12,14,16,17,18,19,20
4,5,6,7,10,11,12,14,15,16,18,19
C3S2 Marginal 10
C3S3 Marginal ----- -----
C3S4 Poor ----- -----
C4S1 Poor 1,11,13,15 13
C4S2 Poor 2,3,5,6 3,15
C4S3 V. Poor ----- -----
C4S4 V. Poor ----- ------
Chapter Four Groundwater Classification and Management
83
The results of the analyzed samples of study area for wet and dry periods are
plotted on Richards diagram(1954) ( Fig. 4.6 ). According to US Salinity
Laboratory classification. Most water samples of the area for both periods are
located in class (C3S1) and the remainder are in classes (C2S1),( C4S1) and
(C4S2) as shown in (Fig.4.9).This means that most of the water samples of the area
are good, marginal and admissible as irrigation water except some samples that are
poor due to the high salinity as shown in table (4.16).
Fig. 4.6 : Diagram for classification of irrigation water of the study area ( After US
Salinity Laboratory staff ,1954)
Chapter Four Groundwater Classification and Management
84
4.5 Groundwater management
The major goal for any groundwater management plan is to maintain a reliable
supply of groundwater for long-term uses in the area .The plan should clearly
describe how each of the adopted management objectives will help to attain that
goal. Furthermore, the plan should clearly describe how current and planned
actions help the adopted management objectives. The plan will have a greater
chance of success by developing an understanding of the relationship between
each action, management objectives, and the goal of the groundwater
management plan (Kevin,2005).
Groundwater management process is very important in organizing the
extraction of groundwater in safe and correct manner .Through this management
the water balance must be determined between the quantity of water supplied to the
aquifer and the amount leaving the aquifer. Groundwater balance in the study area
is calculated according to the equation of water balance (Domenico and
Schwartz ,1998) as follows :
ΔS = Input – Output ………………………. (4.4)
ΔS = Qin – Qout
Where:
ΔS: Changes in groundwater storage (m3/year).
Qin: Input discharge (m3/year).
Qout: Output discharge (m3/year ).
Input discharge (Qin)
To calculate the annual recharge amount of Al-Adhaim basin and the studied
area. The water Surplus (WS) for the study area was calculated in chapter two
(section 2.3) and it was equal (163.6 mm).The water Surplus (WS) represents the
Chapter Four Groundwater Classification and Management
85
total of surface runoff (SR) and groundwater recharge (GR) (Fetter, 1980) as
follows:
WS = SR+ GR ……………………….. (4.5)
Where:
WS: Water Surplus
SR: Surface Runoff
GR: Ground Recharge
The surface runoff (SR) of Al-Adhaim basin was calculated by
(AL-Mamuri,2005) it was equal (9.2%) from the annual rainfall (P).Therefore the
surface runoff (SR) is equal (25.22 mm) from the annual rainfall (274.21 mm). The
groundwater recharge can be calculated according to equation (4.5) as follows:
WS = SR + GR
163.6 = 25.22 + GR
GR = 138.38 mm
GR% = ( GR/P )× 100 = 50.46 % from rainfall
Where: P = rainfall ; P = 274.21 mm
This percentage represents the rainfall percentage that contributes in recharging
groundwater.
The area (A) of Al-Adhaim basin is about 12000 Km2 (AL-Mamuri,2005).
Therefore the annual recharge amount (Qin) for Al-Adhaim basin can be
calculated as follows:
Qin = A × GR ……………………….. (4.6 )
= 12000 × 106 × 138.38 × 10-3
= 1660.56 × 106 m3/ year
While the discharge amount which enters the study area can be calculated
according to Darcy's equation (Todd, 2007) as follows:
Q = TIL ……………………….. (4.7)
Chapter Four Groundwater Classification and Management
86
Where:
Q : Discharge (m3/day)
T : Tranmissivity (m2/day)
I : Hydraulic gradient ( dimensionless)
L: Width of the flow front of the study area (m)
The average of transmissivity for the study area is (176.11m2/day) and the
average of hydraulic gradient (I) is (0.0068) were calculated in chapter two. From
the flow net map(Fig.2.12) width of the front flow is equal (12.4Km).According to
the equation (4.7) the discharge amount (Q1) that enters the area during
(365) days is :
Q1 = 176.11× 0.0068 × 12400 × 365
= 5.42 × 106 m3/ year
While length of the flow front for the study area is equal (10Km). And
according to the equation (4.7) the discharge amount ( Q2 ) that enters along the
study area during ( 365 ) days is :
Q2 = 176.11 × 0.0068 × 10000 × 365
= 4.37 × 106 m3/ year
Therefore the total discharge amount (Qin .Total) that enters the study area is :
Qin . Total = Q1 + Q2
= 9.79 × 106 m3/ year
Output discharge (Qout)
The output discharge (Qout) represents the total of groundwater consumption in
the studied area. The amount of consumed groundwater for different purposes can
be calculated as follows :
1- Groundwater consumption for agriculture purposes
The groundwater is considered important factor for agriculture in the study
area. According to Tuz Khurmatu Agriculture Directorate ,the lands which invest
Chapter Four Groundwater Classification and Management
87
in agriculture and livestock breeding in addition to fish aquariums within the study
area depend on Kirkuk irrigation canal and also on groundwater during the water
shortage in the canal. During the field tours through the agricultural lands and
encountered the some peasants , it was clear that (14) wells were drilled and
distributed in these lands . These wells work during the irrigation canal water
shortage with an average of ( 8 ) days per month about (4 ) hours/day . It means
that the average working days for each well is (16) days a year with an average
discharge of 10 L/sec i.e. (864 m3/day).Therefore the average of groundwater
consumed for agricultural purposes in the study area can be calculated as follows:
GWCA = W.no ×Q ×T
Where:
GWCA : Groundwater Consumption in Agriculture (m3 / year)
W.no : number of wells
Q : Discharge of wells (m3 / day)
T : Time (day)
GWCA = 14 × 864 × 16
= 193536 m3 / year
2- Groundwater Consumption for Industrial Purposes
Industrial importance of the study area associate with the geological nature of
the region by containing Quaternary and Tertiary deposits exposed on the surface.
Therefore the area contains several quarries of sand and gravel as well as bricks
and gypsum factories. All those quarries and factories depend on groundwater for
their works . According to Tuz Khurmatu Municipality Directorate , there are
about (25) quarries and factories distributed within the study area. It was clear
during the field tours in the quarries and factories , the wells work with an average
of ( 5 ) hours/day . It means that the average working days for each well is
( 76.04 ) days a year with an average discharge of 10 L/sec i.e. (864 m3/day) .
Chapter Four Groundwater Classification and Management
88
Average of groundwater consumed for industrial purposes can be calculated as
follows:
GWCI = F.no ×Q ×T
Where:
GWCI: Groundwater Consumption for Industries (m3 / year)
F.no: Number of factories
Q: Discharge of wells (m3 / day)
T: Time (day)
GWCI = 25 × 864 × 76.04
= 1642464 m3 / year
3- Groundwater consumption for domestic uses
Tuz Khurmatu area depends on Kirkuk irrigation canal in tap water supply for
population and also on groundwater during water shortage in the canal ,where the
population of area uses the groundwater for drinking although it is not suitable for
drinking as mentioned in section (4.3.1) . According to Tuz Khurmatu Water
Center, there are (29) wells were drilled and distributed within the study area for
tap water supply during the water shortage in the irrigation canal , these wells work
with an average of (15) days per month about (6) hours/day .It means that the
average working days for each well is (45) days a year with an average discharge
of 10 L/sec i.e. (864 m3/day). Average of groundwater consumed for domestic
purposes can be calculated as follows:
GWCD = W.no ×Q ×T
Where:
GWCd : Groundwater Consumption for domestic purposes(m3 / year)
W.no: Number of wells
Q: Discharge of wells (m3 / day)
T: Time (day)
Chapter Four Groundwater Classification and Management
89
GWCD = 29 × 864 × 45
= 1127520 m3 / year
Therefore approximately all the consumed groundwater in the study area during
present study is :
Total groundwater consumption = GWCA + GWCI + GWCD ( Al-Azawi,2009)
= 2963520 m3 / year
The difference between the amount of input discharge (Qin .Total) into the study
area and the amount of consumed groundwater of it (Qout) can be calculated
according to the equation (4.4) as follow:
ΔS = Qin .Total – Qout
= (9.79 – 2.96) × 106
= 6.83 × 106 m3 / year
This value represents the change in groundwater storage, and indicate to an
increase in the constant storage of the area. So we can conclude that the total
groundwater consumption in the area has a little influence on the groundwater
amount that enter the study area as renewed storativity and has no effect on the
constant storage of the area.
It is clear that the study area depends on surface water (Kirkuk irrigation canal )
bigly especially in agriculture and domestic uses (tap water supply).
Iraq is facing shortages in surface water sources (Lorenz,2008).This will lead to
depending on groundwater mainly in future. So it is necessary to protect
groundwater quantity in the area by good management to keep groundwater
sustained. Through this management the control on the random drilling of wells in
the study area especially by the farmers and gravel quarries and monitoring
groundwater levels in the area by drilling wells for monitoring. Groundwater
quality must be also protected by minimizing the contamination from human
activities .
Chapter Five Conclusions and Recommendations
90
Chapter Five Conclusions and Recommendations
5.1 Conclusions
The following conclusions are derived from the present study :
1- Climate :
Depending on the climatic informations recorded in Tuz Khurmatu station for
the period (1991- 2010) , the values of climate variables for the area are as follows:
· The annual average temperature is (22.8C°), while the monthly averages are
expressed in three periods :
Hot period, which extends from June (33.4C°) to September (30.8C°) with the
highest average appears in July (35.6C°) .
Temperate period , which represented by the months of October, April and
May.
Cold period, which extends from November (16.4C°) to March(15.7C°),with
the lowest average appears in January (9C°).
· Average annual rainfall is ( 274.12 mm) and using this average, the water years
from 1991-2010 are classified into dry years which have rainfall less than the
average represented by (13) years , and wet years which have rainfall higher than
the average, represented by (7) years. The rain is limited between October and
May and approximately disappears in the months June, July, August and
September ,where the highest average of rainfall occurs in January(62mm).
· The annual average for relative humidity is (46.93 % ), while the monthly averages
are expressed in three periods :
Dry period, which extends from June(27.5%) to September(30.8%), ,where the
lowest average is in July (26.2 %) .
Humid period, which extends from November (58.3%) to April (50.5%), where
the highest average is in January(72.7 %).
Transitional period that falls between the humid and dry periods represented
by October (39.9%) and May (36%).
Chapter Five Conclusions and Recommendations
91
· The total amount of evaporation is (2376.2mm ) are expressed in three periods :
First period, which extends from May (280.4mm) to September ( 259.9mm)
where the highest average of monthly evaporation is in July(377.7mm)
Second period, which extends from November (89.5mm), to March (127.9mm)
, where the lowest average of monthly evaporation is in January(45.8 mm).
Third period, is a transitional one represented by October (180.5mm) and April
(175.4mm).
· The highest average of wind speed is in Apr. , May. , Jun. and July (2.2 m/sec)
,while the lowest is in December ( 1.3 m/sec) .
· Corrected potential Evapotranspirtion (PEc) is determined according to
Thornthwait (1948), where its total amount is (959.24 mm), while the total amount
of (PE) is (1121.12 mm). According to the values of evaporation the relation is
recognized: (PEc < PEx < Epan) .
· Water surplus ratio from the total rainfall (annual rainfall )is calculated as
(59.66 %) ,this percentage represents the groundwater recharge and surface runoff
, while the water deficit is (40.34 %).
· According to Kettaneh and Gangopadhyaya classification (1973) ,the months from
Nov. to Mar. have humid climate, while the months from Jun. to Sep. have very
dry climate. The months Oct. and May. have moderate to dry climate . April
monthes have moist climate.
· According to Al-Kubaisi classification (2004), the dominated climate in the area is
humid to moist .
2- Hydrogeology
The studied area is not considered as independent hydrogeological basin, but
it lies within big basin represented by AL-Adhaim basin. The productive
hydrogeological unit in the studied area is Bai - Hassan Formation (confined
aquifer) and composed of sandstone and gravel consecutive with clay and
conglomerate masses .All wells in the area penetrating this formation partially
, the recharge sources are located in the northeast area outside the study area where
Chapter Five Conclusions and Recommendations
92
its layers are exposed. The general direction of groundwater flow in the study area
is from northeast towards southwest and the hydraulic gradient (I) average is
(0.0068). Al-Fat'ha formation appears in Pulkhana anticline and affect
groundwater salinity in the area because of its content of evaporates rocks
(gypsum rocks).
Results of single pumping test performed on seven wells distributed in the
study area are analyzed to measure transmissivity (T) and hydraulic conductivity
(K) values for wells. Jacob and Theis recovery methods are used in the treatment
of these results. (T) values range between(95.47- 335.72 m²/day) and (K) values
between ( 2.11 - 4.47 m/day ) . This reflect that the hydraulic properties values of
Bai- Hassan aquifer in study area are heterogeneous and variant, as a result of
heterogeneity of Bai-Hassan aquifer due to variations in lithology and porosity.
Specific capacity for these wells is measured and found varying between
(172.8 - 432 m²/d). It shows an inverse relationship between the specific capacity
and drawdown in the wells.
3- Hydrochemical
The results of chemical analysis of groundwater samples show that the reaction
error test for all water samples range between (0.004-4.1%) for the dry period and
between( 0.03 - 7.4 %) for the wet period, which indicates that they are less than
(10%). Thus, these results can be used in hydrochemical interpretations. The
results are as follows:
The groundwater in the study area is generally of low alkalinity with ( pH )
average ranging between (7.71) for dry period and ( 7.40 ) for the wet period.
(EC) and (TDS) averages in wet period are lower than dry period due to dilution
process. The water of the area is excessively mineralized due to the salinity. TDS
values are higher in the wells close to Pulkhana anticline as a result of Al- Fat'ha
Formation effect which appears in the anticline and decrease towards the west and
southwest due to the dilution by Tuz chai river and the seepage from Kirkuk
irrigation canal . Depending on (TDS) values for both periods the groundwater in
Chapter Five Conclusions and Recommendations
93
the area is classified as slightly-brackish water. The relationship between (EC)
and (TDS) in the groundwater of the study area is strong and the value of
correlation coefficient (R2) is close to one.
The results of the analysis of major elements (cations and anions) and nitrate in the
groundwater of the study area showed that the predominant ion in the cations is
(Na+) ion and anions is (SO42-) ion as a result for dissolution processes of
evaporations rocks (gypsum rocks) and from ionic exchange of clay minerals.
Concentrations of cations and anions in wet period are lower than dry period due
to the dilution process except bicarbonate ion(HCO3⁻) which is greater in the wet
period due to the recharge process, where the carbonate is associated with water
converted to (HCO3⁻). No nitrate pollution in the groundwater of the study area,
nitrate concentration in wet period is greater due to agricultural
activities(fertilizers) and sewage effect. According to Total Hardness (TH) the
groundwater in the study area is classified as a very hard water due to the presence
of dissolved calcium and magnesium salts and its concentration in the wet period
is lower due to dilution process.
The results of the analysis of heavy elements in the groundwater of the study
area confirm that groundwater is polluted with some elements like (Co, Ni, Cd and
Pb) because their concentrations are higher than the permissible limits according to
WHO (2007) and IQS(2009) as a result of weathering and solution action, in
addition to the effect of the Iraqi fertilizers and human activities.
4- Groundwater Classification and Management
The results of hydrochemical classification, quality , origin and suitability of
groundwater are as follows:
The results of hydrochemical formula show that most wells of study area have
water type of (Na2SO4), and the other wells range between NaCl ,CaCl2,CaSO4 and
MgSO4water type for the two periods. Generally the salts distribution in area water
is attributed to the lithology of recharge areas and the study area as a result of
weathering and solution action of rocks and clay minerals in addition to the
Chapter Five Conclusions and Recommendations
94
agricultural and human activities. The spatial distribution of water quality in the
study area for both dry and wet periods shows difference in water quality between
both periods as a result of recharge and dilution processes in the wet period.
The average of hydrochemical indicators for wells in the study area for the two
periods are greater than one ,which indicates that the ratio of sulfates exceeds the
chloride ratio and the origin of groundwater is meteoric , except the wells
No.(1,2,8,9,13,20) which are less than one. This means that the chloride ion is the
prevailing ion and the origin of groundwater is marine due to the existence of a
deep recharge from the deeper aquifers in these wells.
Piper Classification showed that the type of groundwater in the study area for both
periods is "earth alkaline water with increased portions of alkalis with prevailing
sulfate and chloride" belongs to hydrochemical facies (Ca2+ - Mg2+ - Cl- - SO4
2- )
and (Na+- K+ - Cl- - SO42-) for the two periods .
The groundwater in the study area is unsuitable for human drinking purposes
according to WHO (2007) and IQS (2009 ) standards, but its suitable for all kinds
of animals both domestic and livestock animals.
The groundwater in the study area is not suitable for industrial purposes , but its
suitable for building purposes .
The groundwater in the study area is suitable for growing most types of crops
, and its admissible as irrigation water except some samples which are poor due to
the high salinity.
Through the groundwater management, the annual recharge amount for Al-Adhaim
basin is (1660.56 × 106 m3/ year), while the groundwater amount that enters the
study area as renewed storativity is (9.79 × 106 m3/ year). The amount of
consumed groundwater in the area during present study is (2.96 ×106 m3/year).
Therefore the amount of change in the groundwater storage (ΔS ) will be
(6.83 × 106 m3 / year) .This value represents an increase in the constant storage of
the area .So we can conclude that the total groundwater consumption has
Chapter Five Conclusions and Recommendations
95
a little influence on groundwater amount that enters the study area as renewed
storativity and has no effect on the constant storage of the area.
5.2 Recommendations
1- Conducting biological study for groundwater in the area to determine the
organic and bacteriologic pollution.
2- The groundwater of study area is unsuitable for human drinking purposes
, therefore it must be treated before use as drinking water.
3- Conducting analysis of the heavy elements that have not been studied, such
as aluminum, barium, arsenic, chromium, silver .etc, to make sure water is
not contaminated with these elements.
4- Sewage disposal and septic tank systems are considered one of the sources
of groundwater pollution in the area, and therefore a drainage system for
sewage must be constructed to drain away from urban areas.
5- Establish a monitoring stations program of groundwater levels in study area
to measure the water level fluctuation in order to evaluate the conditions for
different purposes , and to control the random drilling of wells by farmers
and gravel quarries to protect the groundwater reserve .
6- Launch education campaigns for the farmers and industrialists for the best
usage and reduce waste of groundwater. and especially in the gravel and
sand quarries.
Appendix 1
I
Appendix 1
Names and Locations of samples wells of the study area
Water head
on S.L (m)
S.W.L m)(
Depth m)(
Elev. m)(
Location Well Name
Well No.
Longitude Latitude
215 30 130 245 44° 38' 14.9'' 34° 53' 51.7'' Al malab
1
188 25 112 213 44° 35' 53.7'' 34° 53' 56.2'' Karanaz
2
183 35 90 218 44 °37' 01.7'' 34° 53' 42.2'' Shenaw (mardan)
3
187 32 75 219 44° 35' 59.8'' 34° 53' 30.1'' Ali okla
4
184.1 34.90 110 219 44° 38' 10.2'' 34° 52' 46.2'' Erfan
5
186 23 91 209 44° 35' 51.4'' 34° 52' 54.2'' Abbas allwo
6
179.83 17.25 110 205 44° 35' 26.8'' 34° 53' 37.7'' Saleh marof
7
175.23 28.77 80 204 44° 36' 10.0'' 34° 51'40.3'' Mamal bablan
8
177.82 18.30 80 208 44° 35' 38.4'' 34° 52' 00.3'' Alsalam
9
188.9 38.10 90 227 44° 37' 45.1'' 34° 52' 45.1'' Rassol
10
183.56 34.44 84 218 44° 37' 19.2'' 34° 52' 49.0'' Emam ahmad
11
177 33 80 210 44° 36' 02.9'' 34° 52' 03.6'' Mamal Hassan
12
185 36 90 221 44° 37' 40.9'' 34° 53' 17.2'' Alzerah
13
188.75 35.25 100 224 44° 38' 16.7'' 34° 52' 18.8'' Mamal azadi
14
182 30 84 212 44° 36' 54.5'' 34° 54' 11.9'' Mojama Tuz
15
178 38 95 216 44° 37' 59.3'' 34° 52' 06.2'' Mamal talal
16
177 28 74 205 44° 36' 11.4'' 34° 51' 01.1'' Mamal al saeed
17
181.88 12.35 70 217 44° 37' 37.8'' 34° 52' 14.2'' Mamal saeed
Qasem
18
180 37 70 217 44° 37' 23.2'' 34° 53' 02.8'' Al etfah
19
174 26 82 200 44° 35' 44.8'' 34° 50' 58.3'' Mamal Diary
20
Appendix 2
II
Appendix ( 2 )
Well test data and results
Data of drawdown and recovery water level for well (W 1)
(Mojama Tuz )
Well ( W- 1)
d (m) S.W.L (m) b (m) Q (m³/d) Location Elev. (m) Latitude Longitude
84 30 54 604.8 34° 54' 11.9'' 44° 36' 54.5'' 212 Well Data
Drawdown water level
Recovery water
level
t (min)
Drawdown (m)
s (m)
t' (min)
Residual Drawdown s' (m)
t /t' (min)
1 31.72 1.72 1 1.05 361
2 31.85 1.85 2 0.95 181
3 31.98 1.98 3 0.88 121
4 32.15 2.15 4 0.72 91
5 32.35 2.35 5 0.60 73
10 32.49 2.49 10 0.45 37
15 32.60 2.60 15 0.35 25
20 32.74 2.74 20 0.28 19
25 32.82 2.82 25 0.22 15.4
30 32.88 2.88 30 0.13 13
45 32.95 2.95 45 0.05 9
60 32.98 2.98 60 0.0 7
90 33 3 90 0.0 5
120 33 3 120 0.0 4
180 33 3 180 0.0 3
240 33 3 240 0.0 2.5
300 33 3 300 0.0 2.2
360 33 3 360 0.0 2
Appendix 2
III
Graphs of drawdown and recovery water level with time for well ( W 1 ) by using Jacob (Drawdown) and Theis (Recovery) methods
Appendix 2
IV
Data of drawdown and recovery water level for well ( W 2 ) (Esalh Tuz 1)
Well ( W- 2)
d (m) S.W.L (m) b (m) Q (m³/d) Location Elev. (m) Latitude Longitude
96 31.74 64.26 864 34°52'7.57'' 44°36'35.04'' 211
Well Data Drawdown water
level
Recovery water
level
t
(min)
Drawdown
(m)
s
(m)
t'
(min)
Residual Drawdown
s' (m)
t /t'
(min)
1 33.55 1.81 1 1.18 361
2 33.72 1.98 2 1.05 181
3 33.88 2.14 3 0.92 121
4 33.96 2.22 4 0.80 91
5 34.08 2.34 5 0.66 73
10 34.21 2.47 10 0.49 37
15 34.32 2.58 15 0.30 25
20 34.40 2.66 20 0.16 19
25 34.47 2.73 25 0.11 15.4
30 34.53 2.79 30 0.07 13
45 34.58 2.84 45 0.0 9
60 34.64 2.9 60 0.0 7
90 34.64 2.9 90 0.0 5
120 34.64 2.9 120 0.0 4
180 34.64 2.9 180 0.0 3
240 34.64 2.9 240 0.0 2.5
300 34.64 2.9 300 0.0 2.2
360 34.64 2.9 360 0.0 2
Appendix 2
V
Graphs of drawdown and water level recovery with
time for well ( W 2 ) by using Jacob (Drawdown) and Theis (Recovery) methods
Appendix 2
VI
Data of drawdown and recovery water level for well (W 3 )
(Al Asreia )
Well ( W- 3)
d (m) S.W.L (m) b (m) Q (m³/d) Location Elev. (m) Latitude Longitude
84 26.18 57.82 691.2 34°54'18.80'' 44°36'32.25'' 209
Well Data Drawdown water
level
Recovery water
level
t
(min)
Drawdown
(m)
s
(m)
t'
(min)
Residual Drawdown
s' (m)
t /t'
(min)
1 27.86 1.68 1 1.35 361
2 27.95 1.77 2 1.19 181
3 28.09 1.91 3 1.1 121
4 28.17 1.99 4 1.02 91
5 28.25 2.07 5 0.91 73
10 28.45 2.27 10 0.78 37
15 28.60 2.42 15 0.65 25
20 28.76 2.58 20 0.54 19
25 28.85 2.67 25 0.42 15.4
30 28.95 2.77 30 0.3 13
45 29.04 2.86 45 0.12 9
60 29.12 2.94 60 0 7
90 29.15 2.97 90 0 5
120 29.15 2.97 120 0 4
180 29.15 2.97 180 0 3
240 29.15 2.97 240 0 2.5
300 29.15 2.97 300 0 2.2
360 29.15 2.97 360 0 2
Appendix 2
VII
Graphs of drawdown and water level recovery with time for well ( W 3 ) by using Jacob (Drawdown) and Theis (Recovery) methods
Appendix 2
VIII
Data of drawdown and recovery water level for well (W 4)
( Al Askari )
Well ( W- 4) d (m) S.W.L (m) b (m) Q (m³/d) Location Elev.
(m) Latitude Longitude 84 32.62 51.38 777.6 34°52'42.30'' 44°36'49.56" 215
Well Data Drawdown water
level
Recovery water
level
t
(min)
Drawdown
(m)
s
(m)
t'
(min)
Residual Drawdown
s' (m)
t /t'
(min)
1 34.34 1.72 1 1.26 361
2 34.40 1.78 2 1.15 181
3 34.48 1.86 3 1.05 121
4 34.55 1.93 4 0.96 91
5 34.64 2.02 5 0.87 73
10 34.79 2.17 10 0.7 37
15 34.92 2.3 15 0.54 25
20 35.08 2.46 20 0.4 19
25 35.17 2.55 25 0.28 15.4
30 35.22 2.6 30 0.2 13
45 35.26 2.64 45 0.1 9
60 35.30 2.68 60 0.05 7
90 35.34 2.72 90 0 5
120 35.34 2.72 120 0 4
180 35.34 2.72 180 0 3
240 35.34 2.72 240 0 2.5
300 35.34 2.72 300 0 2.2
360 35.34 2.72 360 0 2
Appendix 2
IX
Graphs of drawdown and water level recovery with time for well ( W 4 ) by using Jacob (Drawdown) and Theis (Recovery) methods
Appendix 2
X
Data of drawdown and recovery water level for well (W 5 )
(Al Mahata )
Well ( W- 5)
d (m) S.W.L (m) b (m) Q (m³/d) Location Elev. (m) Latitude Longitude
78 37 41 691.2 34°52'46.83" 44°37'39.37" 221
Well Data Drawdown water
level
Recovery water
level
t
(min)
Drawdown
(m)
s
(m)
t'
(min)
Residual Drawdown
s' (m)
t /t'
(min)
1 38 1 1 1.5 361
2 38.15 1.15 2 1.1 181
3 38.30 1.3 3 0.9 121
4 38.50 1.5 4 0.7 91
5 38.70 1.7 5 0.5 73
10 39.10 2.1 10 0.3 37
15 39.50 2.5 15 0.2 25
20 39.80 2.8 20 0.15 19
25 39.90 2.9 25 0.1 15.4
30 39.95 2.95 30 0.05 13
45 39.98 2.98 45 0 9
60 39.99 2.99 60 0 7
90 40 3 90 0 5
120 40 3 120 0 4
180 40 3 180 0 3
240 40 3 240 0 2.5
300 40 3 300 0 2.2
360 40 3 360 0 2
Appendix 2
XI
Graphs of drawdown and water level recovery with time for well ( W 5 ) by using Jacob (Drawdown) and Theis (Recovery) methods
Appendix 2
XII
Data of drawdown and recovery water level for well (W 6)
(Esalh Tuz 2 )
Well ( W- 6)
d (m) S.W.L (m) b (m) Q (m³/d) Location Elev. (m) Latitude Longitude
106 31 75 864 34°52'15.34" 44°36'37.53" 214
Well Data Drawdown water
level
Recovery water
level
t
(min)
Drawdown
(m)
s
(m)
t'
(min)
Residual Drawdown
s' (m)
t /t'
(min)
1 32.10 1.1 1 0.95 361
2 32.15 1.15 2 0.75 181
3 32.22 1.22 3 0.65 121
4 32.30 1.3 4 0.6 91
5 32.40 1.4 5 0.47 73
10 32.75 1.75 10 0.25 37
15 32.84 1.84 15 0.2 25
20 32.90 1.9 20 0.16 19
25 32.94 1.94 25 0.13 15.4
30 32.97 1.97 30 0.09 13
45 32.99 1.99 45 0.04 9
60 33 2 60 0 7
90 33 2 90 0 5
120 33 2 120 0 4
180 33 2 180 0 3
240 33 2 240 0 2.5
300 33 2 300 0 2.2
360 33 2 360 0 2
Appendix 2
XIII
Graphs of drawdown and water level recovery with
time for well ( W 6 ) by using Jacob (Drawdown) and Theis (Recovery) methods
Appendix 2
XIV
Data of drawdown and recovery water level for well (W 7 )
(Nawaf Abd Al aziz )
Well ( W- 7 )
d (m) S.W.L (m) b (m) Q (m³/d) Location Elev. (m) Latitude Longitude
80 35 45 518.4 34°52'31.15" 44°37'54.64" 222
Well Data Drawdown water
level
Recovery water
level
t
(min)
Drawdown
(m)
s
(m)
t'
(min)
Residual Drawdown
s' (m)
t /t'
(min)
1 36.40 1.4 1 1.75 361
2 36.75 1.75 2 1.55 181
3 36.90 1.9 3 1.33 121
4 37.08 2.1 4 1.1 91
5 37.22 2.26 5 0.85 73
10 37.30 2.39 10 0.5 37
15 37.54 2.5 15 0.34 25
20 37.71 2.71 20 0.25 19
25 37.80 2.8 25 0.18 15.4
30 37.88 2.88 30 0.1 13
45 37.95 2.95 45 0.05 9
60 37.99 2.99 60 0 7
90 38 3 90 0 5
120 38 3 120 0 4
180 38 3 180 0 3
240 38 3 240 0 2.5
300 38 3 300 0 2.2
360 38 3 360 0 2
Appendix 2
XV
Graphs of drawdown and water level recovery with
time for well ( W 7 ) by using Jacob (Drawdown) and Theis (Recovery) methods
Appendix 3
XVI
Appendix 3
Physical properties of water samples of study area for wet and dry periods
Dry period Wet period
Well
no.
TDS
(ppm)
EC
µS/cm T C° pH
TDS
(ppm)
EC
µS/cm T C° pH
1857 2910 24 8 1245 1847 22 7.3 1
1686 2330 23 7.33 1380 1990 22 7.4 2
2169 3210 24 7.44 2250 3176 21 7.2 3
704 1042 24 7.62 697 1049 22 7.62 4
1485 2415 23 7.17 1180 1967 21 7.71 5
1488 2250 22 8.01 1014 1736 20 7.25 6
1419 1995 24 8.03 1081 1794 21 7.35 7
380 582 24 8.2 302 419 22 7.12 8
339 546 23 7.91 241 363 20 7.27 9
1335 2190 24 7.22 1026 1775 21 7.2 10
1564 2360 24 7.61 1244 1988 22 7.92 11
533 883 23 7.71 366 690 20 7.48 12
2366 3420 22 8.01 2287 3402 20 7.81 13
975 1465 24 8.04 966 1420 21 7.32 14
2415 3500 23 8.07 2118 3237 20 7.44 15
1380 1874 21 7.81 974 1682 20 7.35 16
758 994 22 7.62 373 586 22 7.49 17
756 956 22 7.21 562 808 20 7.29 18
1442 2120 21 7.33 932 1770 20 7.3 19
546 986 24 8.03 313 445 21 7.22 20
Appendix 4
XVII
Appendix 4
Concentrations of Cations and Anions of the water samples of study area for dry period by ( ppm)
well no. Cations Anions
NO3‾ TH
Ca+2
Mg+2 Na+ K+ CO3
2- HCO3‾ SO42- Cl‾
1
194 106 212 2.9 0 396.5 413 468.6 3.1 920.6
2
159 55 288 1.11 0 312 456.2 362 1.15 623.3
3
178 82 345 1.4 0 280 844 300 1.5 781.8
4
64 21 110 1.17 0 64 249 130 4.9 246.2
5
113 58 235 2.5 0 146 609 189 8 520.8
6
140 43 250 5.5 0 140 560 255 2 526.5
7
148 43 200 5 0 125 540 230 2 546.5
8
38 12 69 2.01 0 19 108 103 1.9 144.2
9
33 11 61 1.21 0 12.8 110 99 2.18 127.6
10
100 48.6 230 1.08 0 166 408 277 8 449.6
11
166 50 230 5.5 0 141 570 284 1.1 620.2
12
52.2 28 71 2.1 0 28 239 89 1.4 245.5
13
235 121 259 2.5 0 380 730 466 4 1084.7
14
78 56 106 0.7 0 236 266 135 7.11 425.2
15
253 130 250 3 0 611 565 460 3 1166.6
16
112 45 251 3 0 135 513 255 7 464.8
17
50 22 165 1.2 0 49 257 187 3.1 215.3
18
53 25 159 2.1 0 51 261 181 2.1 235.2
19
138.2 82.5 162 0.7 0 305 374.2 284 0.2 684.5
20
46 28 65 0.3 0 135 121 102 1.3 230
Appendix 5
XVIII
Appendix 5
Concentrations of Cations and Anions of the water samples of study area for wet period by ( ppm)
well
no.
Cations Anions
NO3‾ TH Ca+2 Mg+2 Na+ K+ CO3
2- HCO3‾ SO42- Cl‾
1 140.2 61.2 122.3 1.2 0 299 293 206 8 601.91
2 160.3 73 138.4 1.6 0 317 293 291 3.1 700.66
3 180 91 314 5.4 0 446 690 328 8.1 823.92
4 65 22 108 1.1 0 65 250 130 5.2 252.83
5 122 52 129 1 0 323 264 212 9 518.61
6 86 39 147 0.7 0 240 280 137 7.11 375.22
7 93 42 156 0.9 0 245 308 145 2.2 405.05
8 28 13.2 42 1.8 0 55 62.4 71 1.8 124.23
9 26.01 13.1 23.08 1.9 0 61 43.2 49.7 1.8 118.85
10 90 40 152 0.8 0 242 298 143 4.3 389.33
11 112.2 71 134 1.17 0 317.2 346 178 8.7 572.32
12 38 13 69 2 0 18 109 104 2 148.38
13 234 121 258 2.4 0 381 731 460 4.5 1082.21
14 84.1 62.4 117.7 0.7 0 250 288 145.5 8.6 466.77
15 178 82 345 1.5 0 280 844 300 1.3 781.89
16 80 57 108 0.7 0 236 268 136 7.11 434.31
17 38 10.1 46.1 0.8 0 61 91.2 92.3 1.8 136.44
18 62.1 28.8 73.8 2.3 0 153 115.2 107 2.4 273.57
19 82 38 110 0.7 0 238 272 137 7.11 361.12
20 30.06 15 44 1.5 0 67.1 53 89 2.5 136.78
Appendix 6
XIX
Appendix 6 Concentrations of Cations and Anions by (epm) and the accuracy of the results of the water samples of study area for dry period
Cations
∑C
atio
ns Anions
∑A
nion
s
U
A% well no.
Ca+2 Mg+2 Na+ K+ CO₃⁻² HCO₃⁻ SO₄⁻² Cl‾
epm
epm% epm
epm% epm
epm% epm
epm%
epm
epm% epm
epm% epm
epm% epm
epm%
1 9.68 34.9 8.72 31.4 9.22 33.2 0.07 0.25 27.69 0 0 6.49 22.94 8.59 30.36 13.21 46.69 28.29 1.07 98.93
2 7.93 31.7 4.52 18 12.52 50.1 0.02 0.08 24.99 0 0 5.11 20.59 9.49 38.25 10.21 41.15 24.81 0.36 99.64
3 8.88 28.9 6.74 21.9 15 48.9 0.03 0.09 30.65 0 0 4.58 14.96 17.57 57.39 8.46 27.63 30.61 0.06 99.94
4 3.19 32.8 1.72 17.7 4.78 49.2 0.02 0.2 9.71 0 0 1.04 10.52 5.18 52.42 3.66 37.04 9.88 0.86 99.14
5 5.63 27.2 4.77 23 10.22 49.4 0.06 0.29 20.68 0 0 2.39 11.72 12.67 62.13 5.33 36.14 20.39 0.7 99.3
6 6.98 32.4 3.53 16.4 10.87 50.5 0.14 0.65 21.52 0 0 2.29 10.83 11.65 55.13 7.19 34.02 21.13 0.91 99.09
7 7.38 37.4 3.53 17.9 8.69 44 0.12 0.6 19.72 0 0 2.04 10.32 11.24 56.88 6.48 32.79 19.76 0.1 99.9
8 1.89 31.9 0.98 16.5 3 50.6 0.05 0.84 5.95 0 0 0.31 5.68 2.24 41.1 2.9 53.21 5.45 4.38 95.62
9 1.64 31.4 0.9 17.2 2.65 50.7 0.03 0.57 5.22 0 0 0.2 3.78 2.29 43.37 2.79 52.84 5.28 0.57 99.43
10 4.99 26.2 3.99 21 10 52.6 0.02 0.1 19 0 0 2.72 14.3 8.49 44.63 7.81 41.06 19.02 0.05 99.95
11 8.28 36.7 4.11 18.2 10 44.3 0.14 0.62 22.53 0 0 2.31 10.41 11.86 53.49 8 36.08 22.17 0.8 99.2
12 2.6 32.3 2.3 28.6 3.08 38.3 0.05 0.62 8.03 0 0 0.45 5.67 4.97 62.67 2.51 31.65 7.93 0.62 99.38
13 11.72 35.5 9.95 30.1 11.26 34.1 0.06 0.18 32.99 0 0 6.22 18 15.19 43.96 13.14 38.08 34.55 2.3 97.7
14 3.89 29.6 4.6 35 4.61 35.1 0.01 0.07 13.11 0 0 3.86 29.26 5.53 41.92 3.8 28.8 13.19 0.3 99.7
15 12.62 36.8 10.69 31.2 10.87 31.7 0.07 0.2 34.25 0 0 10 28.79 11.76 33.86 12.97 37.34 34.73 0.69 99.31
16 5.58 27.5 3.7 18.2 10.91 53.8 0.07 0.34 20.26 0 0 2.21 11 10.68 53.18 7.19 35.8 20.08 0.44 99.56
17 2.49 21.6 1.81 15.7 7.17 62.3 0.03 0.26 11.5 0 0 0.8 7 5.35 46.84 5.27 46.14 11.42 0.34 99.66
18 2.64 22.6 2.05 17.5 6.91 59.3 0.05 0.42 11.65 0 0 0.83 7.3 5.43 47.79 5.1 44.89 11.36 1.26 98.74
19 6.89 33.2 6.78 32.7 7.04 33.9 0.01 0.04 20.72 0 0 4.99 24.01 7.79 37.48 8 38.49 20.78 0.14 99.86
20 2.29 30.8 2.3 31 2.82 38 0.007 0.09 7.41 0 0 2.21 29.11 2.51 33.06 2.87 37.81 7.59 1.2 98.8
Appendix 7
XX
Appendix 7
Concentrations of Cations and Anions by (epm) and the accuracy of the results of the water samples of study area for wet period
A%
U
ΣAnions
Anions
Σcations
Cations well no.
Cl⁻
SO₄⁻² HCO₃⁻ CO₃⁻² K+ Na+ Mg+2 Ca+2
epm %
epm
epm %
epm
epm %
epm
epm %
epm
epm % epm
epm % epm
epm % epm
epm % epm
98.4 1.6 16.81 34.56 5.81 36.28 6.1 29.14 4.9 0 0 17.36 0.17 0.03 30.58 5.31 28.97 5.03 40.26 6.99 1 98.59 1.41 19.49 42.07 8.2 31.29 6.1 26.62 5.19 0 0 20.05 0.19 0.04 30.02 6.02 29.92 6 39.85 7.99 2 98.91 1.09 30.91 29.92 9.25 46.45 14.36 23.61 7.3 0 0 30.24 0.42 0.13 45.13 13.65 24.73 7.48 29.69 8.98 3 99.19 0.81 9.92 36.89 3.66 52.41 5.2 10.68 1.06 0 0 9.76 0.28 0.028 48.01 4.69 18.52 1.81 33.16 3.24 4 97.65 2.35 16.75 35.64 5.97 32.77 5.49 31.58 5.29 0 0 15.98 0.15 0.025 35.09 5.61 26.71 4.27 38.03 6.08 5 98.99 1.01 13.61 28.36 3.86 42.76 5.82 28.87 3.93 0 0 13.89 0.12 0.017 45.98 6.39 23.02 3.2 30.86 4.29 6 98.68 1.32 14.5 28.13 4.08 44.2 6.41 27.65 4.01 0 0 14.89 0.15 0.023 45.52 6.78 23.16 3.45 31.15 4.64 7 98.36 1.64 4.19 47.73 2 30.78 1.29 21.47 0.9 0 0 4.33 1.06 0.046 41.97 1.82 24.9 1.08 32.05 1.39 8 98.21 1.79 3.28 42.68 1.4 27.13 0.89 30.18 0.99 0 0 3.4 1.4 0.048 29.34 1 31.39 1.07 37.85 1.29 9 99.24 0.76 14.19 28.4 4.03 43.69 6.2 27.9 3.96 0 0 14.41 0.13 0.02 45.87 6.61 22.83 3.29 31.15 4.49 10 99.6 0.4 17.41 28.83 5.02 41.35 7.2 29.81 5.19 0 0 17.27 0.16 0.029 33.68 5.82 33.79 5.84 32.35 5.59 11
95.48 4.52 5.48 53.46 2.93 41.24 2.26 5.29 0.29 0 0 6 0.84 0.051 49.99 3 17.66 1.06 31.49 1.89 12 97.75 2.25 34.42 37.68 12.97 44.18 15.21 18.12 6.24 0 0 32.9 0.18 0.061 34.1 11.22 30.24 9.95 35.47 11.67 13 99.1 0.9 14.18 28.91 4.1 42.24 5.99 28.84 4.09 0 0 14.44 0.11 0.017 35.37 5.11 35.5 5.13 29 4.19 14
99.94 0.06 30.61 27.63 8.46 57.39 17.57 14.96 4.58 0 0 30.65 0.12 0.038 48.92 15 21.98 6.74 28.96 8.88 15 99.55 0.45 13.26 28.88 3.83 42 5.57 29.11 3.86 0 0 13.38 0.12 0.017 35.03 4.69 35.03 4.69 29.8 3.99 16 92.76 7.24 5.48 47.44 2.6 34.48 1.89 18.06 0.99 0 0 4.74 0.42 0.02 42.19 2 17.51 0.83 39.87 1.89 17 95.13 4.87 7.9 38.1 3.01 30.25 2.39 31.64 2.5 0 0 8.71 0.66 0.058 36.82 3.21 27.07 2.36 35.44 3.09 18 94.42 5.58 13.42 28.76 3.86 42.17 5.66 29.06 3.9 0 0 12 0.14 0.017 39.81 4.78 25.98 3.12 34.06 4.09 19 99.68 0.32 4.7 53.4 2.51 23.4 1.1 23.19 1.09 0 0 4.67 0.81 0.038 40.82 1.91 26.29 1.23 32.06 1.5 20
Appendix 8
XXI
Appendix 8
Trace elements concentrations in water samples of study area by ( ppm)
Well No.
Trace elements Fe Co Ni Cu Zn Cd Pb Mn
1 0.009 0.134 0.068 0.053 0.194 0.046 0.251 0.039
2 0.004 0.280 0.045 0.009 0.014 0.002 0.289 0.053
3 0.191 0.457 0.081 bdl 0.011 0.005 0.203 0.058
4 0.100 bdl bdl bdl 0.019 0.122 0.149 0.051
5 0.256 0.195 0.045 0.027 0.049 0.030 0.174 bdl
6 0.194 0.268 0.027 0.014 0.024 0.050 0.219 bdl
7 0.409 0.073 0.068 bdl 0.014 0.099 0.090 0.002
8 bdl 0.341 0.012 0.023 0.005 0.109 0.232 bdl
9 0.092 0.103 0.063 bdl 0.055 bdl bdl 0.007
10 0.343 0.059 0.048 bdl 0.006 0.059 0.237 0.009
11 0.124 0.136 0.059 0.031 0.186 0.012 0.204 0.056
12 0.096 0.163 0.047 bdl bdl 0.187 0.050 0.005
13 0.136 0.064 0.026 0.124 0.012 0.134 0.261 bdl
14 0.096 0.367 0.068 0.006 0.051 bdl 0.140 0.024
15 0.041 0.072 0.026 bdl 0.599 bdl 0.244 bdl
16 0.075 0.008 bdl 0.096 0.027 bdl 0.253 0.005
17 0.055 bdl 0.037 0.082 0.023 0.006 0.353 bdl
18 bdl bdl 0.074 0.028 0.049 0.172 0.075 0.015
19 0.256 0.455 0.085 0.022 0.336 0.068 0.288 0.017
20 0.155 0.227 0.050 0.039 bdl bdl 0.129 0.037 v bdl : below detection limit
Appendix 9
XXII
Appendix 9 Hydrochemical formula and water type for dry period water samples
Water
type Hydrochemical formula
W.
no. Water
type Hydrochemical formula
W.
no.
Na2SO4
SO₄-2
(53.49) Cl- ( 36.08 ) TDS(1564) ——————————————— PH (7.61)
Na+ ( 44.3) Ca+2 ( 36.7 ) Mg+2 ( 18.2) ( Mg+2 – Ca+2 - Sodium – Cl- - Sulfate)
11
CaCl2
Cl- ( 46.69) SO₄-2
(30.36) HCO₃- (22.94) TDS( 1857) ————————––––––––––––––––—— PH (8)
Ca+2(34.9) Na+
( 33.2) Mg+2(31.4)
( Mg+2 - Na+ - Calcium - HCO₃- - SO₄-2- Chloride)
1
Na2SO4
SO₄-2
(62.67) Cl- ( 31.65)
TDS( 533) ——————————————— PH (7.71) Na+
( 38.3 ) Ca+2(32.3) Mg+2
( 28.6) ( Mg+2 – Ca+2 - Sodium – Cl- - Sulfate)
12
NaCl
Cl-
( 41.15) SO₄-2(38.25) HCO₃-
(20.59) TDS( 1686) ————————————————— PH(7.33) Na+
(50.1 ) Ca+2 ( 31.7 ) Mg+2
( 18 ) ( Mg+2- Ca+2 - Sodium -HCO₃- - SO₄-2 -Chloride)
2
CaSO4
SO₄-2
(43.96) Cl-(38.08) HCO₃-
(18) TDS(2366) ——————————————— PH (8.01)
Ca+2 (35.5) Na+ ( 34.1) Mg+2 ( 30.1)
( Mg+2 – Na+ - Calcium - HCO₃- - Cl- - Sulfate)
13 Na2SO4
SO₄-2
(57.39) Cl- ( 27.63)
TDS( 2169) —————————————— PH (7.44) Na+
(48.9) Ca+2( 28.9) Mg+2
( 21.9) ( Mg+2 – Ca+2 - Sodium – Cl- - Sulfate)
3
Na2SO4
SO₄-2
(41.92) HCO₃-(29.26) Cl- (28.8)
TDS( 975) ——————————————— PH (8.04) Na+
( 35.1) Mg+2 ( 35) Ca+2 (29.6)
(Ca+2 – Mg+2 - Sodium – Cl- - HCO₃- - Sulfate)
14
Na2SO4
SO₄-2
( 52.42) Cl- ( 37.04)
TDS( 704) ——————————————— PH (7.62) Na+
(49.2) Ca+2( 32.8) Mg+2
(17.7 ) ( Mg+2 – Ca+2 - Sodium – Cl- - Sulfate)
4
CaCl2
Cl- (37.34) SO₄-2(33.86) HCO₃-
(28.79) TDS( 2415) ———————————————PH (8.07)
Ca+2(36.8) Na+
( 31.7 ) Mg+2( 31.2)
(Mg+2 -Na+ - Calcium - HCO₃- - SO₄-2 - Chloride)
15
Na2SO4
SO₄-2 (62.13) Cl- ( 36.14 )
TDS(1485) ——————————————— PH (7.17) Na+ ( 49.4) Ca+2 ( 27.2) Mg+2 ( 23 )
( Mg+2 – Ca+2 - Sodium – Cl- - Sulfate)
5
Na2SO4
SO₄-2 (53.18) Cl- ( 35.8)
TDS(1380) ——————————————— PH (7.81) Na+ ( 53.8 ) Ca+2
(27.5 ) Mg+2( 18.2 )
( Mg+2 – Ca+2 - Sodium – Cl- - Sulfate)
16
Na2SO4
SO₄-2 (55.13) Cl - ( 34.02)
TDS( 1488)——————————————— PH (8.01) Na+ ( 50.5) Ca+2 ( 32.4) Mg+2 ( 16.4)
( Mg+2 – Ca+2 - Sodium – Cl- - Sulfate)
6
Na2SO4
SO₄-2 (46.84) Cl- ( 46.14)
TDS (758) ——————————————— PH (7.62) Na+ ( 62.3 ) Ca+2 (21.6) Mg+2
( 15.7)
( Mg+2 – Ca+2 - Sodium – Cl- - Sulfate)
17
Na2SO4
SO₄-2 (56.88) Cl- ( 32.79)
TDS(1419 )——————————————— PH (8.03) Na+
(44) Ca+2 ( 37.4) Mg+2 (17.9 )
( Mg+2 – Ca+2 - Sodium – Cl- - Sulfate)
7
Na2SO4
SO₄-2 (47.79 ) Cl- ( 44.89)
TDS( 756) ——————————————— PH (7.21) Na+ ( 59.3 ) Ca+2
(22.6 ) Mg+2 ( 17.5)
( Mg+2 – Ca+2 - Sodium – Cl- - Sulfate)
18
NaCl
Cl- (53.21) SO₄-2 (41.1)
TDS(380) ——————————————— PH (8.2) Na+ (50.6) Ca+2
(31.9) Mg+2(16.5)
( Mg+2 – Ca+2 - Sodium - SO₄-2 - Chloride)
8
NaCl
Cl- ( 38.49) SO₄-2
(37.48 ) HCO₃- (24.01)
TDS(1442) ——————————————— PH (7.33) Na+ (33.9 ) Ca+2
(33.2) Mg+2 ( 32.7)
( Mg+2-Ca+2 - Sodium - HCO₃- - SO₄-2 - Chloride)
19
NaCl
Cl- (52.84) SO₄-2 (43.37)
TDS(339) ——————————————— PH (7.91) Na+ ( 50.7 ) Ca+2 (31.4 ) Mg+2 (17.2)
( Mg+2 – Ca+2 - Sodium - SO₄-2 - Chloride)
9
NaCl
Cl- (37.81) SO₄-2 (33.06) HCO₃- (29.11)
TDS(546) ——————————————— PH (8.03) Na+ (38) Mg+2 (31 ) Ca+2 (30.8 )
( Ca+2 -Mg+2 -Sodium - HCO₃- - SO₄-2 - Chloride)
20
Na2SO4
SO₄-2 ( 44.63 ) Cl- ( 41.06 )
TDS(1335) ——————————————— PH (7.22) Na+ ( 52.6 ) Ca+2 ( 26.2) Mg+2 (21)
( Mg+2 - Ca+2 - Sodium – Cl- - Sulfate)
10
Appendix 10
XXIII
Appendix 10 Hydrochemical formula and water type for wet period water samples
Water
type Hydrochemical formula
W.
no. Water
type Hydrochemical formula
W.
no.
MgSO4
SO₄-2
(41.35) HCO₃-(29.81) Cl-
(28.83 ) TDS(1244) ——————————————— PH (7.92)
Mg+2(33.79) Na+
(33.68) Ca+2(32.35 )
(Ca+2 – Na+ - Magnesium – Cl- - HCO₃- - Sulfate)
11
CaSO4
SO₄-2
(36.28) Cl- (34.56) HCO₃- (29.14) TDS( 1245) ——————————————— PH (7.3)
Ca+2(40.26) Na+
(30.58) Mg+2(28.97)
( Mg+2 – Na+ - Calcium - HCO₃- - Cl- - Sulfate)
1
NaCl
Cl- (53.46) SO₄-2 (41.24)
TDS(366) ——————————————— PH (7.48) Na+
(49.99 ) Ca+2(31.49) Mg+2
(17.66) ( Mg+2 – Ca+2 - Sodium - SO₄-2 - Chloride)
12
CaCl2
Cl-
(42.07) SO₄-2(31.29) HCO₃-
(26.62) TDS( 1380) ———————————————— PH (7.4)
Ca+2(39.85) Na+
(30.02 ) Mg+2(29.92 )
( Mg+2 – Na+ - Calcium - HCO₃- - SO₄-2 - Chloride)
2
CaSO4
SO₄-2
(44.18) Cl-(37.68) HCO₃-
(18.12) TDS(2287) ———————————————PH (7.81)
Ca+2 (35.47) Na+ (34.1) Mg+2(30.24)
( Mg+2 – Na+ - Calcium - HCO₃- - Cl- - Sulfate)
13 Na2SO4
SO₄-2 (46.45) Cl-
(29.92) HCO₃-(23.61)
TDS( 2250) —————————————— PH (7.2) Na+
(45.13) Ca+2( 29.69) Mg+2
(24.73) ( Mg+2 – Ca+2 - Sodium - HCO₃- - Cl- - Sulfate)
3
MgSO4
SO₄-2
(42.24) Cl-(28.91) HCO₃-
(28.84) TDS(966)——————————————— PH (7.32)
Mg+2( 35.5) Na+
( 35.37) Ca+2(29)
(Ca+2 – Na+ - Magnesium - HCO₃- - Cl- - Sulfate)
14
Na2SO4
SO₄-2 (52.41) Cl- (36.89)
TDS(697) ——————————————— PH (7.62) Na+
(48.01) Ca+2(33.16) Mg+2
(18.52 ) ( Mg+2 – Ca+2 - Sodium – Cl- - Sulfate)
4
Na2SO4
SO₄-2 (57.39) Cl-
(27.63) TDS(2118) ——————————————— PH (7.44)
Na+(48.92 ) Ca+2
(28.96) Mg+2(21.98)
( Mg+2 - Ca -+2 Sodium – Cl- - Sulfate)
15
CaCl2
Cl-(35.64) SO₄-2
(32.77) HCO₃-(31.58)
TDS(1180) ——————————————— PH (7.71) Ca+2
(38.03) Na+(35.09) Mg+2
(26.71 ) ( Mg+2 – Na+ - Calcium - HCO₃- - SO₄-2 - Chloride)
5
Na2SO4
SO₄-2
(42) HCO₃-(29.11) Cl-
(28.88) TDS(974) ——————————————— PH (7.35)
Na+( 35.03) Mg+2
(35.03 ) Ca+2(29.8 )
(Ca+2 – Mg+2 - Sodium – Cl- - HCO₃- - Sulfate)
16
Na2SO4
SO₄-2
(42.76) HCO₃-(28.87) Cl-(28.36) TDS(1014)——————————————— PH (7.25)
Na+(45.98) Ca+2
(30.86) Mg+2(23.02)
( Mg+2 – Ca+2 - Sodium – Cl- - HCO₃- - Sulfate)
6
NaCl
Cl-
(47.44) SO₄-2(34.48) HCO₃-
(18.06) TDS (373)——————————————— PH (7.49)
Na+( 42.19) Ca+2
(39.87) Mg+2( 17.51)
( Mg+2 - Ca+2 -Sodium - HCO₃- - SO₄-2 - Chloride)
17
Na2SO4
SO₄-2 (44.20) Cl- (28.13) HCO₃-
(27.65) TDS(1081)——————————————— PH (7.35)
Na+(45.52) Ca+2
(31.15) Mg+2(23.16 )
( Mg+2 – Ca+2 - Sodium - HCO₃- - Cl- - Sulfate)
7
NaCl
Cl-
( 38.1) HCO₃-(31.64) SO₄-2
(30.25 ) TDS( 562) ——————————————— PH (7.29)
Na+ (36.82 ) Ca+2 (35.44 ) Mg+2 (27.07) ( Mg+2 – Ca+2 - Sodium - SO₄-2 - HCO₃- - Chloride)
18
NaCl
Cl-
(47.73) SO₄-2(30.78) HCO₃-
(21.47) TDS(302) ——————————————— PH (7.12)
Na+(42.97) Ca+2
(32.05) Mg+2(24.9)
( Mg+2 – Ca+2- Sodium -HCO₃- - SO₄-2 - Chloride)
8
Na2SO4
SO₄-2 (42.17 ) HCO₃- (29.06) Cl- (28.76)
TDS(932) ——————————————— PH (7.3) Na+
(39.81) Ca+2(34.06) Mg+2 (25.98)
( Mg+2 – Ca+2 - Sodium – Cl- - HCO₃- - Sulfate)
19
CaCl2
Cl- (42.68) SO₄-2 (27.13)
TDS(241) ——————————————— PH (7.27) Ca+2
(37.85 ) Mg+2(31.39) Na+
(29.34 ) ( Na+ - Mg+2 - Calcium - SO₄-2 - Chloride)
9
NaCl
Cl- (53.4) SO₄-2 (23.4) HCO₃- (23.19)
TDS(313) ——————————————— PH (7.22) Na+ (40.82) Ca+2 (32.06 ) Mg+2 (26.29 )
( Mg+2 - Ca+2 - Sodium - HCO₃- - SO₄-2 - Chloride)
20
Na2SO4
SO₄-2 (43.69 ) Cl- (28.4 ) HCO₃- (27.9)
TDS(1026) ——————————————— PH (7.2) Na+ (45.87 ) Ca+2 ( 31.15) Mg+2 (22.83)
( Mg+2 – Ca+2 - Sodium - HCO₃- - Cl- - Sulfate)
10
XXIV
Appendix 11 Hypothetical salts for water samples of study area for dry and wet periods
Well No. Hypothetic -al salts
20 19 18 17 16 15 14 13 12 11 10 9 8 7 6 5 4 3 2 1
0.09 0.04 0.42 0.26 0.34 0.2 0.07 0.18 0.62 0.62 0.1 0.57 0.84 0.6 0.65 0.29 0.2 0.09 0.08 0.25 KCl
Dry
per
iod
37.61 33.9 44.28 45.64 35.26 31.7 28.43 34.1 30.88 35.38 40.7 50.07 50.6 32.1 33.25 25.61 36.5 27.51 41.02 33.2 NaCl
0 4.46 0 0 0 5.4 0 3.62 0 0 0 1.13 1.46 0 0 0 0 0 0 13.15 MgCl2
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 CaCl2
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 K2SO4
0.39 0 15.02 16.66 18.54 0 6.67 0 7.42 8.92 11.9 0 0 11.9 17.25 23.79 12.7 21.39 9.08 0 Na2SO4
31 28.24 17.5 15.7 18.2 25.8 34.83 26.48 28.6 18.2 21 16.07 15.04 17.9 16.4 23 17.7 21.9 18 18.25 MgSO4
1.51 9.16 15.08 14.24 16.06 8 0 17.32 26.48
26.28 11.4 26.93 25.76 26.9 21.35 14.91 21.6 14.01 11.12 12.05 CaSO4
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 NaHCO3
0 0 0 0 0 0 0.17 0 0 0 0 0 0 0 0 0 0 0 0 0 Mg(HCO3)2
29 24 7.2 6.9 10.9 28.7 28.83 17.9 5.6 10.4 14.2 3.7 5.6 10.3 10.8 11.6 10.4 14.89 20.5 22.85 Ca(HCO3)2
0.81 0.14 0.66 0.42 0.12 0.12 0.11 0.18 0.84 0.16 0.13 1.4 1.06 0.15 0.12 0.15 0.28 0.42 0.19 0.17 KCl
Wet
per
iod
40.82 28.62 36.82 42.19 28.76 27.51 28.8 34.1 49.99 28.67 28.27 29.34 41.97 27.98 28.24 35.09 36.61 29.5 30.02 30.58 NaCl
11.77 0 0.62 4.83 0 0 0 3.4 2.63 0 0 11.94 4.7 0 0 0.4 0 0 11.86 3.81 MgCl2
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 CaCl2
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 K2SO4
0 11.19 0 0 6.27 21.41 6.57 0 0 5.01 17.6 0 0 17.54 17.74 0 11.4 15.63 0 0 Na2SO4
14.52 25.98 26.45 12.68 35.03 21.98 35.5 26.84 15.03 33.79 22.83 19.45 20.2 23.16 23.02 26.31 18.52 24.73 18.06 25.16 MgSO4
8.88 5 3.8 21.8 0.7 14 0.17 17.34 26.21 2.55 3.26 7.68 10.58 3.5 2 6.46 22.49 6.09 13.23 11.12 CaSO4
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 NaHCO3
0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 Mg(HCO3)2
23.18 29.06 31.64 18.06 29.1 14.96 28.83 18.12 5.28 29.8 27.89 30.17 21.47 27.65 28.86 31.57 10.67 23.6 26.62 29.14 Ca(HCO3)2
XXV
XXV
Appendix 12
Wet period Dry period
Well no. (Na+rK)-Cl
rSO₄ rNa+rK
rCl rSO₄ /rCl rK/rCl rNa/rCl rMg/rCl rCa /rCl (Na+rK)-Cl
rSO₄ rNa+rK
rCl rSO₄ /rCl rK/rCl rNa/rCl rMg/rCl rCa /rCl
-0.077 0.91 1.04 0.0051 0.91 0.86 1.2 -0.45 0.7 0.65 0.005 0.69 0.66 0.73 1 -0.35 0.73 0.74 0.0048 0.73 0.73 0.97 0.24 1.22 0.92 0.001 1.22 0.44 0.77 2 0.31 1.48 1.55 0.014 1.47 0.8 0.97 0.37 1.77 2.07 0.003 1.77 0.79 1.04 3 0.2 1.28 1.42 0.0076 1.28 0.49 0.88 0.22 1.31 1.41 0.005 1.3 0.46 0.87 4
-0.06 0.94 0.91 0.0041 0.93 0.71 1.01 0.39 1.92 2.37 0.011 1.91 0.89 1.05 5 0.43 1.65 1.5 0.0044 1.65 0.82 1.11 0.32 1.53 1.62 0.019 1.51 0.49 0.97 6 0.42 1.66 1.57 0.0056 1.66 0.84 1.13 0.2 1.35 1.73 0.018 1.34 0.54 1.13 7 -0.1 0.93 0.64 0.023 0.91 0.54 0.69 0.066 1.05 0.77 0.017 1.03 0.33 0.65 8
-0.39 0.74 0.63 0.034 0.71 0.76 0.92 -0.048 0.96 0.82 0.01 0.94 0.32 0.58 9 0.41 1.64 1.53 0.0049 1.64 0.81 1.11 0.26 1.28 1.08 0.002 1.28 0.51 0.63 10 0.11 1.16 1.43 0.0057 1.15 1.16 1.11 0.18 1.26 1.48 0.017 1.25 0.51 1.03 11
0.053 1.04 0.77 0.017 1.02 0.36 0.64 0.12 1.24 1.98 0.019 1.22 0.91 1.03 12 -0.11 0.86 1.17 0.0047 0.86 0.76 0.89 -0.11 0.86 1.15 0.004 0.85 0.75 0.89 13 0.17 1.25 1.46 0.0041 1.24 1.25 1.02 0.14 1.21 1.45 0.002 1.21 1.21 1.02 14 0.37 1.77 2.07 0.0044 1.77 0.79 1.04 -0.17 0.84 0.9 0.005 0.83 0.82 0.97 15 0.15 1.22 1.45 0.0044 1.22 1.22 1.04 0.35 1.52 1.48 0.009 1.51 0.51 0.77 16 -0.3 0.77 0.72 0.0076 0.76 0.31 0.72 0.36 1.36 1.01 0.005 1.36 0.34 0.47 17 0.1 1.08 0.79 0.019 1.06 0.78 1.02 0.34 1.36 1.06 0.009 1.35 0.4 0.51 18 0.16 1.24 1.46 0.0044 1.23 0.8 1.05 -0.12 0.88 0.97 0.001 0.88 0.84 0.86 19 -0.51 0.77 0.43 0.015 0.76 0.49 0.59 -0.017 0.98 0.87 0.002 0.98 0.8 0.79 20
XXVI
Hydrochemical indicators of water samples of the study area for dry and wet periods
ABSTRACT
المستخلص ("00 '55 °34 - "00'50°34) بين خطي عرضصالح الدين محافظة ضمنالدراسة منطقة تقع
وبمساحة تقدر ) Km 70 (كركوك بحوالي مدينة جنوب ( "00 '40 °44 - "00 '33 °44)وخطي طول
تكوينات (تشمل ترسبات العصر الثالثي المنطقة في الجيولوجية اهم التكوينات .)Km2 124 (بحوالي
الدراسة. منطقة تغطي التي باالضافة الى ترسبات العصر الرباعي) وباي حسنالمقدادية ، انجانة،فتحةال
) 2010- 1991( للفترة طوزخورماتو االرصادية محطة في المسجلة المناخية البيانات على باالعتماد
حوض العظيم والتي تبلغ مساحتها بحدود ضمن تقع منطقة الدراسة مناخ المنطقة شبه رطبة الى رطبة.
) Km212000.( هي تكوين باي حسن (العصر الثالثي) المنطقة في المنتجة الوحدة الهيدروجيولوجية .
الجنوب الغربي ومعدل الميل نحو من الشمال الشرقي الجوفية في المنطقة المياه لجريان العام اإلتجاه
نتائج الضخ االختباري لعودة المنسوب ثايسوطريقة جاكوب ). بإستعمال طريقة 0.0068الهيدروليكي (
معدل الناقلية جزئيا وبدون ابار مراقبة كانت حسن تكوين باي تخترق ابار) 7 (في التي اجريت
) m2 / day176.11 (الهيدروليكي ومعدل التوصيل) m / day 3.06.(
) EC معدالت التوصيلة الكهربائية(.منخفضة قاعدية المنطقة عموما هي في الجوفية المياه نوعية
من أوطأ كانت الرطبة والسالبة للفترة الموجبة اآليونات وتراكيز TDS)ومجموع االمالح الذائبة الكلية (
HCO3 (البيكاربونات آيون ماعدا الجافة الفترة تلوث بايون بسبب عمليات التخفيف باالمطار.التوجد)-
المياه الجوفية في المنطقة تصنف كمياه مالحة قليال. TDS)اعتمادا على قيم ال(.المنطقة في النترات
العناصر ببعض ملوثة الدراسة منطقة في الجوفية المياه عسرة المياه في المنطقة من النوع العسر جدا.
طبقا للمواصفات القياسية المسموحة الحدود من أعلى كانت تراكيزهم ألن ,Pb (Co, Ni, Cdالثقيلة (
.)2007 ومنظمة الصحة العالمية ()2009 (العراقية
بقية االبار كانت تتفاوت بين ،بينما(Na2SO4)كانت الدراسة آبار منطقة نوع الماء في اغلب
(CaCl2) (NaCl) ,(CaSO4), (MgSO4)معدل الدوال الهيدروكيميائية . وللفترتين الجافة والرطبة
)1,2,8,9,13,20(المياه الجوية، ماعدا االبار من المنطقة في الجوفية المياه أصل وللفترتين اظهرت ان
المياه الجوفية في Piper حسب تصنيف حيث يحدث فيها تغذية عميقة. فان اصلها من المياه البحرية
Na+- K+ - Cl- - SO4) منطقة الدراسة تعود الى السحنات الهيدروكيميائية +Ca2+ - Mg2و ((-2
-
Cl- - SO4 ) وللفترتين.-2
اظهرت المختلفة لالستعماالت مع مواصفات قياسية الجوفية في منطقة الدراسة المياه نوعية مقارنة
الحيوانات والغراض البناء مناسبة لشرب ولكنها لشرب االنسان ولالغراض الصناعية مناسبة غير بأنها
خالل .العالية الملوحة بسبب سيئة العينات بعض ماعدا ري كماء ومقبوله ولزراعة اكثر انواع المحاصيل ،
) بينما كمية المياه m3/ year 106 × 1660.56ادارة المياه الجوفية، كمية التغذية السنوية لحوض العظيم (
ABSTRACT
كمية المياه الجوفية ) .m3/ year 106 × 9.79الجوفية التي تدخل منطقة الدراسة كخزين متجدد سنويا (
لذا ستكون قيمة التغيير . ) m3 / year 106 × 2.96 (تساويالمستهلكة في المنطقة اثناء الدراسة الحالية
وهذه القيمة تعكس مقدار زيادة )ΔS) ( 6.83 × 106 m3 / yearفي خزين المياه الجوفية في المنطقة (
في الخزين الثابت للمنطقة .
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