تقييم الموارد المائية في حوض التون كوبري / شمال شرق كركوك
رسالة متاحة للتحميل :
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تقييم الموارد المائية في حوض التون كوبري / شمال شرق كركوك
لـ : مازن عبد العظيم أحمد العبادي
دكتوراه في الموارد المائية
جامعة بغداد - كلية العلوم 2013
::
@ شكرا للدكتور مازن على اهداء رسالته للموقع لنشرها
WATER RESOURCES EVALUATION OF ALTUN KOPRI BASIN, NE KIRKUK
A THESIS
SUBMITTED TO THE COUNCIL OF COLLEGE OF SCIENCE OF
UNIVERSITY OF BAGHDAD
IN PARTIAL
FULFILLMENT OF THE REQUIRMENTS FOR THE DEGREE
OF PHILOSOPHY OF DOCTORATE OF SCIENCE
IN WATER RESOURCES (GEOLOGY)
BY
MAZIN A. A. AL-ABADI
M.Sc. 2002
SUBMITTED TO THE COUNCIL OF COLLEGE OF SCIENCE OF
UNIVERSITY OF BAGHDAD
IN PARTIAL
FULFILLMENT OF THE REQUIRMENTS FOR THE DEGREE
OF PHILOSOPHY OF DOCTORATE OF SCIENCE
IN WATER RESOURCES (GEOLOGY)
BY
MAZIN A. A. AL-ABADI
M.Sc. 2002
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ABSTRACT
:
Left side of Altun Kpori basin is located in the northeast of Iraq, Kirkuk. It lies between
latitudes N 35° 30′ 00″ - 35° 50′ 00″ and longitudes E 44° 07′ 00″ - 44° 37′ 00″, with an area
of 1175 km2. There are Khalkhalan Dagh mountains (750 m above sea level) which occur
eastward and northeast, while Kani Domlan (400 m above sea level) which extends to Baba
dome (Kirkuk mountains group) lie in the west and southwest. Two aquifers systems are
taken in consideration, they form within Holocene - Pleistocene (Quaternary) deposits and
Pleistocene - Pliocene Bai-Hassan Formations as well as Pliocene - Al-Mukdadya. Mostly,
the lithological facies are clastic sediments including conglomerate, gravel, sand,
interbedded by clay and a little silt or/and evaporates.
The soil of study area composes from gravel, sand, silt and clay with various ratios
spatially. The soil moisture is about 6.7%. Sand forms 50%, silt 23%, clay 16% and gravel
about 11% of the soil textures. Land use and land cover map has been suggested depending
on the soil analysis and areal image. It is noticed that there is an increase in industry instead
of the agricultural activities. The lands of rainfed crop reach to 50% of the total area. Annual
amount of precipitation reach 342.7 mm. Then, gross volume of rainwaters over the basin
area is 403,025,000 m3. The evapotranspiration is much more than precipitation amounts.
The annual total average is 1662.9 mm. Wind erosion is insignificant as a result to low speed
of wind. Comparing yearly precipitation and evaporation, it is seen that the local climate
changes in loops of semiarid to arid and vice versa. Semiarid climate forms 75% and 25% is
arid. The daily indices of climate change have been applied using available daily data that
explain the irregularity of rainfall indices during four years.
Hydraulic head of whole aquifers system is interpolated which has average 355 m.
Most wells penetrated the upper aquifer are located in the basin center while lower aquifer
wells are found in the basin limbs. Groundwater level decreases toward west and northwest.
Hydraulic conductivity of upper aquifer has range from 58 m/day to 327 m/day and
approximately 30 m/day as average of lower aquifer. Average of specific storage of the upper
aquifer is 0.053 while the lower aquifer has range extended from 1.8×10-3 to 4.2×10-3.
Hydraulic gradient equals to 0.005 to 0.035. The annual recharge averages of groundwater
of whole basin are more 178 × 106 or/and 252 × 106 based on chloride mass balance
method. The daily average of consumed groundwater through pumping wells is 204 m3. Six
piezometers of groundwater monitoring infer that there is an increasing of groundwater
demand within the last years in the central zone of study area.
There are not distinct seasonal fluctuations of water level of Lesser Zab river since
2005 to 2011 in Altun Kopri town station. Watershed delineation is sketched showing the
most important potential points of rainfall harvesting and overland flow. The spatial and
latitudes N 35° 30′ 00″ - 35° 50′ 00″ and longitudes E 44° 07′ 00″ - 44° 37′ 00″, with an area
of 1175 km2. There are Khalkhalan Dagh mountains (750 m above sea level) which occur
eastward and northeast, while Kani Domlan (400 m above sea level) which extends to Baba
dome (Kirkuk mountains group) lie in the west and southwest. Two aquifers systems are
taken in consideration, they form within Holocene - Pleistocene (Quaternary) deposits and
Pleistocene - Pliocene Bai-Hassan Formations as well as Pliocene - Al-Mukdadya. Mostly,
the lithological facies are clastic sediments including conglomerate, gravel, sand,
interbedded by clay and a little silt or/and evaporates.
The soil of study area composes from gravel, sand, silt and clay with various ratios
spatially. The soil moisture is about 6.7%. Sand forms 50%, silt 23%, clay 16% and gravel
about 11% of the soil textures. Land use and land cover map has been suggested depending
on the soil analysis and areal image. It is noticed that there is an increase in industry instead
of the agricultural activities. The lands of rainfed crop reach to 50% of the total area. Annual
amount of precipitation reach 342.7 mm. Then, gross volume of rainwaters over the basin
area is 403,025,000 m3. The evapotranspiration is much more than precipitation amounts.
The annual total average is 1662.9 mm. Wind erosion is insignificant as a result to low speed
of wind. Comparing yearly precipitation and evaporation, it is seen that the local climate
changes in loops of semiarid to arid and vice versa. Semiarid climate forms 75% and 25% is
arid. The daily indices of climate change have been applied using available daily data that
explain the irregularity of rainfall indices during four years.
Hydraulic head of whole aquifers system is interpolated which has average 355 m.
Most wells penetrated the upper aquifer are located in the basin center while lower aquifer
wells are found in the basin limbs. Groundwater level decreases toward west and northwest.
Hydraulic conductivity of upper aquifer has range from 58 m/day to 327 m/day and
approximately 30 m/day as average of lower aquifer. Average of specific storage of the upper
aquifer is 0.053 while the lower aquifer has range extended from 1.8×10-3 to 4.2×10-3.
Hydraulic gradient equals to 0.005 to 0.035. The annual recharge averages of groundwater
of whole basin are more 178 × 106 or/and 252 × 106 based on chloride mass balance
method. The daily average of consumed groundwater through pumping wells is 204 m3. Six
piezometers of groundwater monitoring infer that there is an increasing of groundwater
demand within the last years in the central zone of study area.
There are not distinct seasonal fluctuations of water level of Lesser Zab river since
2005 to 2011 in Altun Kopri town station. Watershed delineation is sketched showing the
most important potential points of rainfall harvesting and overland flow. The spatial and
temporal variations of physiochemical parameters of groundwater and surface water show
retreating during wet period due to dilution through recharge. Human made activities are
clear in the western and middle of the basin which leads to higher concentration of
specifically trace elements and cations. Piper, Durov and hydrochemical formula are adopted
to classify the water type, where predominant groundwater facies are Ca2+-SO4
2- and Ca2+- HCO3
1-. For Lesser Zab river samples, HCO3
1- and Ca2+ are significant in both periods; hence
the water type is Ca2+-HCO3
1-. On the contrary, the samples of runoff have SO42- plus Ca2+
only, and then the water type is Ca2+-SO4
2-. Generally, the water resources are suitable for all
purposes except a slight rise in total hardness.
Environmental stable isotopes (18O and 2H) are used to investigate the origin of
groundwater. The local meteorological water line is concluded. Surface water (Lesser Zab river and overland flow) is analysed isotopically. Mostly, similar ranges of isotope contents in
groundwater are noticed during dry and wet periods, except some samples which have
distinct differences of δ2H. Even the groundwater source is unique; the δ2H and δ18O can
change by fractionation processes throughout their traveling from atmosphere. Two
groundwater groups can be estimated; the first lies between EMWL and GMWL, and the
second lies below GMWL. The wells have highest values of isotopic ratios are d-excesses,
which mean their water suffered much more evaporation during travelling stages beginning
from atmosphere until percolation or/and within flow paths of groundwater. Dry and wet
periods have convergent averages of d-excess of 11.53 ‰ and 10.18 ‰ consecutively. Even
the d-excess values closer to 10‰, the source of wells water may be LMWL. Groundwater
dating using 3H suggest probably submodern, in which there is potential mixing between the
two aquifers.
Hydrogeochemical modeling by NETPATH, shows the saturation indices of most
carbonate phases of groundwater are oversaturated during the dry period. On the other hand, mostly there is oversaturation of carbonate minerals in the wet period, except some wells that have undersaturation indices of dolomite. Anhydrite and gypsum are
undersaturated in groundwater within dry and wet periods. Through multivariate statistical,
there is slightly variation of most parameters in the lower aquifer comparison with the
upper aquifer wells. The interaction between the rocks and groundwater increase the physiochemical contents in the (semi)-confined aquifer. At the same time, the mutual upward and downward leakages may be the cause of convergence. The water samples have been classified using hierarchical cluster into three clusters for groundwater and two clusters for the surface water samples
retreating during wet period due to dilution through recharge. Human made activities are
clear in the western and middle of the basin which leads to higher concentration of
specifically trace elements and cations. Piper, Durov and hydrochemical formula are adopted
to classify the water type, where predominant groundwater facies are Ca2+-SO4
2- and Ca2+- HCO3
1-. For Lesser Zab river samples, HCO3
1- and Ca2+ are significant in both periods; hence
the water type is Ca2+-HCO3
1-. On the contrary, the samples of runoff have SO42- plus Ca2+
only, and then the water type is Ca2+-SO4
2-. Generally, the water resources are suitable for all
purposes except a slight rise in total hardness.
Environmental stable isotopes (18O and 2H) are used to investigate the origin of
groundwater. The local meteorological water line is concluded. Surface water (Lesser Zab river and overland flow) is analysed isotopically. Mostly, similar ranges of isotope contents in
groundwater are noticed during dry and wet periods, except some samples which have
distinct differences of δ2H. Even the groundwater source is unique; the δ2H and δ18O can
change by fractionation processes throughout their traveling from atmosphere. Two
groundwater groups can be estimated; the first lies between EMWL and GMWL, and the
second lies below GMWL. The wells have highest values of isotopic ratios are d-excesses,
which mean their water suffered much more evaporation during travelling stages beginning
from atmosphere until percolation or/and within flow paths of groundwater. Dry and wet
periods have convergent averages of d-excess of 11.53 ‰ and 10.18 ‰ consecutively. Even
the d-excess values closer to 10‰, the source of wells water may be LMWL. Groundwater
dating using 3H suggest probably submodern, in which there is potential mixing between the
two aquifers.
Hydrogeochemical modeling by NETPATH, shows the saturation indices of most
carbonate phases of groundwater are oversaturated during the dry period. On the other hand, mostly there is oversaturation of carbonate minerals in the wet period, except some wells that have undersaturation indices of dolomite. Anhydrite and gypsum are
undersaturated in groundwater within dry and wet periods. Through multivariate statistical,
there is slightly variation of most parameters in the lower aquifer comparison with the
upper aquifer wells. The interaction between the rocks and groundwater increase the physiochemical contents in the (semi)-confined aquifer. At the same time, the mutual upward and downward leakages may be the cause of convergence. The water samples have been classified using hierarchical cluster into three clusters for groundwater and two clusters for the surface water samples
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