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Mineralogical and Geochemical Study of Sediments of Lower Mesopotamia,
Southern Iraq
Khaleel J. Alsudani1,*, Badir N. Albadran2, Liviu Giosan3
1. Department of Geology, College of Science, University of Basrah, Basra, Iraq.
2. Almaaqal University, Basra, Iraq
3. Woods Hole Oceanographic Institution, Boston , Ma, USA
*Corresponding author E-mail: khaleel.mola@uobasrah.edu.iq
Doi:10.29072/basjs.20220115
Received 7 Mar 2022; Received in revised form 11 Mar 2022; Accepted 22 Apr 2022, Published 30
Apr 20
ARTICLE INFO
ABSTRACT
Keywords
Clay minerals, Grain
size analysis,
Chemical analysis
and Lower
Mesopotamia.
This study is based on forty eight samples that were collected from
selected sites in Lower Mesopotamia. Sampling depth varies between 1
and 9 m in the South Hammar Marsh, Southern. Grain size distribution
indicates that the deposits are mainly composed of silt with a small
amount of clay and sand, silt texture is dominate in the sediments,
followed by sandy silt, mud, and muddy sand. The dominate nonclay
minerals are calcite, quartz, dolomite, feldspar and gypsum, while the
clay minerals are composed of; kaolinite, illite, montmorillonite,
chlorite, Palygorskite, mixed layers montmorillonite - chlorite and
palygorskite - illite. Chemical analysis showed that all samples have
high concentration in SiO2 and CaO in comparison with Al2O3, Fe2O3,
MgO, SO3, K2O and Na2O. These results are generally related to the
clay minerals composition. The depositional environment of these
minerals may be characterized by an arid to semi-arid climate in the
source area.
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1. Introduction
The Mesopotamian plain in the lower is a broad, flat deltaic complex with shallow freshwater
marshes such as Baghdad and Zechri, and brackish water like Shafi and Hammar marshes which
though to be formed as young as 640-552 BP [1] with around <3 m depth surrounded by
extensively vegetated marshes, locally called the Ahwar. Quaternary deposits (1.65 M.Y) are
considered widespread constitutes, more than one third of the surface sediments of Iraq. The
Mesopotamian plain is mostly covered by sediments of the Quaternary period [2], where these
sediments consist largely of silt and clay with a little amount of sand fraction. Unfortunately,
very few systematic clay mineralogical studies have been done on the lower Mesopotamian
plain; studied the heavy mineral composition of the sand fraction of Tigris and Shatt Al-Arab
Rivers and identified the dominate mineral in the sediments of Tigris, Euphrates and Shatt Al-
Arab Rivers. The study of the distribution of the main elements in sediments is an important
means of detecting the quality of source rocks and the geological and climatic conditions
prevailing during weathering processes, as well as knowing the nature of subsequent sedimentary
and diagenesis processes. The aim of this study is to clarify the weathering condition and ancient
climate of the area.
2. Materials and Methods
Forty-eight sediment samples were collected from four boreholes were in study
area (Fig. 1). The depth of coring was about 2m in site one, 4m at site two, and in sites
three and four were 9 meters in the sites one, two, three, and four by using two inches
diameter tubes with one meter length connected by sockets and used for coring, using a
hammer machine to push the tubes down the ground. Visual description and sampling
were done in the tunnel with depth (Fig. 2) which was drawn by Sedlog 3.0 program.
Grain size analysis is carried out to separate sand from silt and clay, using a sieve 0.063
mm by wet sieving. Forty- four samples were analyzed by X- Ray diffraction technique to
identify both oriented clay samples and non- clay minerals of total sediments. The
instrument used is Bruker D2 Phaser in the Iraqi German Laboratory / University of
Baghdad/ College of Science/ Department of Geology. Target: Cu, Wave: 1.54060,
Voltage: 40 KV, Current: 30 mA. Twenty two samples were analyzed for their major
oxides (CaO, SiO2, Al2O3, Fe2O3, MgO, Na2O, SO3, K2O, TiO3 and Loss on ignition).
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Major oxides elements were analyzed by using XRF techniques (XRF: Ed-XRF
Instrument Spectro-Xepos of Ametek Company, in the Iraqi German Laboratory in the
University of Baghdad/ College of Science / Department of Geology).
Figure 1: Map of study area
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Figure 2: Lithology of sites 1, 2, 3, and 4
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3. Results and Discussion
3.1 Grain size analysis
The results of the grain size analysis are given in Tables 1, 2, 3, and 4 for forty eight samples,
which show the percentages of sand, silt, and clay. Clay was low percent in selected samples (1-
26) % with an average of 5.35%, while the silt portion is high percent in all samples, it ranged
between (36- 98) % with an average of 86.45%, While the extent of sand in the sediments of the
study area was (1- 62) % with an average of 8.2%. The color of sediments is light olive to grey
indicating anaerobic and quiet environment conditions.
Table 1: Grain size Percentage and statistical parameters of south Hammar marsh in site one.
Table 2: Grain size Percentage and statistical parameters of south Hammar marsh in site two.
Sample
Depth
Sand%
Silt%
Clay%
Lithology
Mean
median
Sorting
Kurtosis
Skewness
HB1
0-0.5
14
82
4
Sandy
silt
6.3
6.2
1.6
0.85
0.04
HB2
0.5-1
16
81
3
Sandy
silt
6.2
6.3
1.5
0.85
0.04
HB3
1-1.5
7
90
3
Silt
6.5
6.4
1.6
0.89
0.04
HB4
1.5-2
7
89
4
Silt
6.3
6.7
1.23
0.83
-0.15
HB5
2-2.5
2
76
26
Mud
6.3
6.6
1.57
0.84
-0.03
HB6
2.5-3
3
71
22
Mud
6.4
6.8
1.58
0.85
-0.01
HB7
3-3.5
3
79
18
Mud
6.2
6.3
1.5
0.85
0.04
HB8
3.5-4
3
81
16
Mud
6.5
6.4
1.6
0.89
0.0r4
Sample
Depth
Sand%
Silt%
Clay%
Lithology
Mean
median
Sorting
Kurtosis
Skewness
HA1
0-0.5
6
90
4
Silt
6.5
6.4
1.6
0.89
0.04
HA2
0.5-1
6
78
19
Mud
6.4
6.8
1.58
0.85
-0.01
HA3
1-1.5
4
82
14
Mud
6.4
6.5
1.45
0.75
-0.03
HA4
1.5-2
3
83
14
Mud
6.4
6.7
0.73
0.75
-0.01
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Table 3: Grain size Percentage and statistical parameters of south Hammar marsh in site three.
Sample
Depth
Sand%
Silt%
Clay%
Lithology
Mean
median
Sorting
Kurtosis
Skewness
HC1
0-0.5
7
92
2
Silt
6.3
6.7
1.35
1.13.
0.04
HC2
0.5-1
8
90
2
Silt
6.4
6.4
1.25
0.81
-0.20
HC3
1-1.5
6
93
1
Silt
6.3
6.7
1.23
0.83
-0.15
HC4
1.5-2
7
91
2
Silt
6.3
6.6
1.57
0.84
-0.03
HC5
2-2.5
6
89
5
Silt
6.4
6.8
1.58
0.85
-0.01
HC6
2.5-3
2
95
3
Silt
6.4
6.4
1.62
0/87
-0.04
HC7
3-3.5
1
98
1
Silt
6.5
6.5
1.59
0.72
-0.02
HC8
3.5-4
1
95
4
Silt
6.3
6.3
1.63
0.73
-0.01
HC9
4-4.5
1
96
3
Silt
6.4
6.5
1.45
0.75
-0.03
HC10
4.5-5
1
97
2
Silt
6.4
6.7
0.73
0.75
-0.01
HC11
5-5.5
1
98
1
Silt
6.3
6.7
1.35
1.13.
0.04
HC12
5.5-6
1
95
4
Silt
6.4
6.4
1.25
0.81
-0.20
HC13
6-6.5
1
96
3
Silt
6.3
6.7
1.23
0.83
-0.15
HC14
6.5-7
1
94
5
Silt
6.3
6.6
1.57
0.84
-0.03
HC15
7-7.5
2
93
5
Silt
6.4
6.8
1.58
0.85
-0.01
HC16
7.5-8
1
96
3
Silt
6.4
6.4
1.62
0/87
-0.04
HC17
8-8.5
1
96
3
Silt
6.5
6.5
1.59
0.72
-0.02
HC18
8.5-9
1
98
1
Silt
6.3
6.3
1.63
0.73
-0.01
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Table 4: Grain size Percentage and statistical parameters of south Hammar marsh in site four
3.2 Mineralogical analysis
The percentages of minerals were calculated by semi-quantitative method.
3.2.1 Non-clay minerals
Sample
Depth
Sand%
Silt%
Clay%
Lithology
Mean
median
Sorting
Kurtosis
Skewness
HD1
0-0.5
22
75
3
Sandy silt
6.4
6.4
1.85
1.14
-0.18
HD2
0.5-1
18
77
5
Sandy silt
7.1
6.3
1.93
1.91
-0.21
HD3
1-1.5
20
76
4
Sandy silt
6.3
6.6
1.27
1.82
0.12
HD4
1.5-2
19
75
6
Sandy silt
7.2
6.5
1.26
1.92
0.13
HD5
2-2.5
7
90
3
Silt
6.3
6.7
1.35
1.13.
0.04
HD6
2.5-3
4
92
4
Silt
6.4
6.4
1.25
0.81
-0.20
HD7
3-3.5
1
95
4
Silt
6.3
6.7
1.23
0.83
-0.15
HD8
3.5-4
1
97
2
Silt
6.3
6.6
1.57
0.84
-0.03
HD9
4-4.5
2
97
1
Silt
6.4
6.8
1.58
0.85
-0.01
HD10
4.5-5
1
98
1
Silt
6.4
6.4
1.62
0/87
-0.04
HD11
5-5.5
2
97
1
Silt
6.5
6.5
1.59
0.72
-0.02
HD12
5.5-6
1
96
3
Silt
6.3
6.3
1.63
0.73
-0.01
HD13
6-6.5
1
97
2
Silt
6.4
6.5
1.45
0.75
-0.03
HD14
6.5-7
2
96
2
Silt
6.4
6.7
0.73
0.75
-0.01
HD15
7-7.5
60
38
2
Muddy
sand
3.4
2.9
1.38
1.75
0.60
HD16
7.5-8
62
36
2
Muddy
sand
3.9
3.4
1.35
1.66
0.58
HD17
8-8.5
25
70
5
Sandy silt
6.1
6.5
1.46
0.77
-0.02
HD18
8.5-9
23
73
4
Sandy silt
6.2
6.4
1.59
0.76
-0.04
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Twenty- two samples were attended of both sites 1, 2, 3, and 4 and measured by (XRD) an
angle of (2-60)2θ. Calcite, quartz, dolomite, feldspar and gypsum are most of minerals in the
sediments of the studied area (Fig. 3 and Table5).
Figure 3: XRD diffractogram of Non-clay minerals.
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Table 5: Percentage of non-clay minerals in south Hammar marsh sites
3.2.2 Clay minerals
Clay is a natural material of very fine texture less than (0.002 mm). Twenty- two samples
were attended of both sites 1, 2, 3, and 4 and measured an angle of (2-20)2θ. Kaolinite, illite,
montmorillonite, chlorite, palygorskite, mixed layers of montmorillonite-chlorite and illite-
palygorskite were most of the clay minerals identified in the sediments of the study area (Fig.4),
(Table 6). To understand the genesis of clay minerals by knowledge in-depth geological of a
specified environment [3].
Site No. Lithology Depth (m) Calcite% Quartz%
Dolomite
%
Feldspar
%
Gypsum
%
Silt 0-0.5 50 36 563
Mud 0.5-1 44 37 973
Mud 1-1.5 44 37 11 4 4
Mud 1.5-2 52 33 636
(44- 52) (33-37) (5-11) (3-7) (3-6)
47.5 35.75 7.75 5 4
0-0.5 48 34 865
0.5-1 46 36 10 4 4
2.5-3 40 31 15 7 7
3.5-4 44 35 885
(40-48) (31-36) (8-15) (4-8) (4-7)
44.5 34 10.25 6.25 5.25
HC1 0-0.5 50 33 764
HC5 2-2.5 45 39 844
HC7 3-3.5 50 29 975
HC11 5-5.5 48 33 577
HC13 6-6.5 50 33 485
HC15 7-7.5 40 40 974
HC18 8.5-9 48 34 495
(40-50) (29-40) (4-9) (4-9) (4-7)
47.28 34.42 6.57 6.85 4.85
0-0.5 49 30 10 5 6
2-2.5 42 33 12 6 7
3-3.5 44 31 13 5 7
7-7.5 44 34 958
7.5-8 40 39 012 9
8-8.5 36 43 13 4 4
8.5-9 38 50 066
(36-49) (30-50) (0-13) (4-12) (4-9)
41.85 37.14 8.14 6.14 6.71
HD18
Sandy silt
Range
Average
HD15
Muddy sand
HD16
Muddy sand
HD17
Sandy silt
Silt
Range
Average
Site Four
HD1
Sandy silt
HD5
Silt
HD7
Silt
Mud
Range
Average
Site Three
Silt
Silt
Silt
Silt
Silt
Silt
Range
Average
Site Two
HB1
Sandy silt
HB2
Sandy silt
HB3
Silt
HB8
Sample
Site One
HA1
HA2
HA3
HA4
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Figure 4: XRD diffractogram of clay minerals.
Table 6: Percentage of clay mineral in south Hammar marsh sites.
K= Kaolinite, P= Palygorskite, I= Illite, M- Ch= Montmorillonite- Chlorite mixed layers, M= ontmorillonite
P- I= Palygorskite- Illite mixed layers, Ch= Chlorite
Site No. Sample Lithology Depth (m) K% I% M% Ch% P% M-Ch% P-I%
HA1 Silt 0-0.5 23 17 24 10 12 10 4
HA2 Mud 0.5-1 25 23 15 12 9 6 10
HA3 Mud 1-1.5 23 24 19 13 876
HA4 Mud 1.5-2 17 19 23 15 13 8 5
22 20.75 20.25 12.5 10.5 7.75 6.25
HB1 Sandy silt 0-0.5 22 13 30 20 654
HB2 Sandy silt 0.5-1 30 18 13 35 4 - -
HB3 Silt 1-1.5 27 18 10 30 7 8 -
HB8 Mud 3.5-4 31 16 828 576
27.25 16.25 15.2 28.2 5.5 6.6 5
HC1 Silt 0-0.5 25 20 14 16 613 6
HC5 Silt 2.5-5 23 16 17 20 4 9 11
HC7 Silt 3-3.5 35 24 11 13 - 8 9
HC11 Silt 5-5.5 25 12 13 18 712 13
HC13 Silt 6-6.5 27 19 10 14 9 9 12
HC15 Silt 7-7.5 20 16 916 12 11 16
HC18 Silt 8.5-9 33 20 12 17 576
26.85 18.14 12.28 16.28 7.16 9.85 10.42
HD1 Sandy silt 0-0.5 25 16 12 18 612 11
HD5 Silt 2-2.5 32 21 15 13 -10 9
HD7 Silt 3-3.5 26 20 18 20 8 9 -
HD11 Silt 5-5.5 25 22 14 14 997
HD16 Muddy sand 7.5-8 26 20 12 12 10 812
HD17 Sandy silt 8-8.5 22 19 10 18 10 714
HD18 Sandy silt 8.5-9 17 15 18 14 22 11 8
24.71 19 14.14 15.57 10.83 9.42 10.16
Site Four
Average
Site One
Average
Site Two
Average
Site Three
Average
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The results obtained for clay minerals diagnosed kaolinite, illite, montmorillonite,
chlorite, palygorskite, and the mixed layers montmorillonite - chlorite and palygorskite -
illite (Fig. 4 andTable 6). The average of kaolinite mineral varies in sites 1, 2, 3 and 4
between 22%, 27.25%, 26.85%, and 24.71% respectively. The amount of kaolinite is
relatively stable along the studied sites, and it increases in small amount with depth in
study area, may be due to an increase in the proportion of movable kaolinite. Kaolinite
mineral in the sediments had detrital origin because the appropriate conditions to form this
mineral in situ are not available in the sediments of study area. The percentage of Illite
increases with depth (Table 6); this may be attributed to the leaching of the sediments by
the irrigation process or degradation phenomenon in the presence of organic matter. There
is a noticeable increase in the percentage of chlorite mineral with depth, especially in sites
one and two, chlorite minerals may be formed during weathering of Ferro magnesium
rocks that are rich in magnesium, iron.
The mixed-layered minerals present in the studied sites are montmorillionite-chlorite,
palygorskite-illite, and noting an increase with depth, especially in sites three and four.
This difference may back to the diagenetic processes by illitization and chloritization. By
studying the groups of clay minerals in the samples, we can conclude that these groups are
derived from many sources and from different locations, and they are minerals in origin
and transported by rivers, even by the wind, as a result of the weathering of different
rocks, except for the palygorskite mineral, which is likely to be authigenic. The
predominant mineral in these sediments is kaolinite, where we notice from Table 6. Illite
mineral was in the second place in the study area, while chlorite mineral was in the third
place and reflects its composition in an environment characterized by a dry climateWhere
[4] showed that Illite is formed in warm climatic conditions and the dominance of physical
weathering. As for the minerals montmorillonite and chlorite, they are produced from the
weathering of volcanic rocks [5], and their environment is characterized by a dry to semi-
arid climate.
Palygorskite mineral is found in a percentage ranging from little to medium in Table 6,
where its percentage increases in samples are HA1(12%), HC15(12%), HD18(22%) which
were characterized by dry arid climatic conditions. This gives evidence that the prevalent
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sedimentary environmental conditions in the study area were drier. It is possible that there
has been transgression in study area. Palygorskite crystallizes in shallow lakes under
oxidizing environment [6]. Palygorskite created in the sabkha sediments of central and
southern Iraq, resulting from the process of transition of montmorillonite to palygorskite,
in the presence of additional amounts of magnesium. Where the sabkha areas in central
and southern Iraq are suitable environments characterized by a dry-semi-arid climate with
an increase in the amount of evaporation.
The results that were reached in the current study were similar to a certain extent to the
results reached by [2]. In their study of the clay minerals in the alluvial sediments, the
Hammar marsh sediments, and the mud sediments along the Tigris, Euphrates and Shatt
al-Arab basin, and successively, where they found that kaolinite and Illite are the main
minerals in these sediments in addition to chlorite and montmorillonite, but the
palygorskite was recorded in the current study and in all samples. Can be formed after
deposition during the diagenesis process.Twenty- two samples were analyzed for their
major oxides (CaO, SiO2, Al2O3, Fe2O3, MgO, Na2O, SO3, K2O, TiO3 and Loss on
ignition) (Table 7).
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Table 7: Concentrations of major oxides in south Hammar marsh sites.
The high content of CaO is due to the presence of a high percentage of calcite, which may be
related to the presence of shells, especially in the sample HD18 in the fourth position. The high
content of CaO, most probable related to deposits of limestone [7]. The presence of silica in the
sediments of the study area is in the form of quartz mineral, which has been proven in mineral
studies and with the help of X-ray diagrams in addition to the presence of silica within the crystal
structure of clay minerals [8]. As [9] suggest that clay minerals are mainly composed of alumina
and silica in major amounts and other different mineral matters in low amounts. Alumina is
concentrated in sediments of the study area mainly within the structure of clay minerals with the
possibility of its adsorption on the surfaces of these minerals as Al(OH)2 aluminum hydroxide,
which may exist between plates of montmorillonite and kaolinite minerals. Where the presence
Site No. Sample Lithology Depth(m) CaO% SiO2%Al2O3%Fe2O3% MgO% Na2O% SO3% K2O% TiO3% L.O.i%
HA1 Silt 0-0.5 26.71 42.81 8.95 5.87 4.79 1.55 1.86 2.04 1.66 15.76
HA2 Mud 0.5-1 27.71 41.91 11.22 6.91 7.1 2.56 1.98 1.89 1.38 18.23
HA3 Mud 1-1.5 24.22 43.22 10.42 8.44 5.29 2.04 0.89 1.78 1.38 19.27
HA4 Mud 1.5-2 21.45 45.62 6.76 4.95 3.99 2.03 0.78 1.49 1.22 21.25
Range
21.45-
27.71
41.91-
45.62
6.76-
11.22 4.95-8.44 3.99-7.10 1.55-2.56 0.78-1.98 1.49-2.04 1.22-1.66
15.76-
21.25
25.02 43.39 9.33 6.54 5.29 2.04 1.37 1.8 1.41 18.62
HB1 Sandy silt 0-0.5 30.05 40.62 10.55 5.95 4.98 1.45 1.45 1.79 2.01 9.76
HB2 Sandy silt 0.5-1 26.53 40.33 9.66 7.66 5.93 2.02 1.95 2.05 1.87 10.43
HB3 Silt 2.5-3 22.76 40.65 9.77 8.55 5.66 2.45 1.5 1.98 1.94 13.56
HB7 Mud 3-3.5 17.19 40.43 10.57 6.77 3.89 1.85 1.65 0.65 0.94 19.65
Range
17.19-
30.05
40.33-
40.65
9.66-
10.57 5.95-8.55 3.89-5.93 1.45-2.45 1.45-1.95 0.65-2.05 0.94-2.01 9.76-
19.65
24.13 40.5 10.13 7.23 5.11 1.94 1.63 1.61 1.69 13.35
HC1 Silt 0-0.5 21.55 45.7 9.78 6.56 5.86 1.99 1.33 1.92 1.1 12.45
HC5 Silt 2-2.5 18.76 44.43 11.01 7.81 4.76 2.45 0.77 1.5 1.05 13.56
HC7 Silt 3-3.5 14.92 38.9 11.33 6.17 5.88 1.45 0.78 1.89 0.79 14.77
HC11 Silt 5-5.5 25.91 42.81 9.77 8.17 5.59 2.02 0.91 2.11 0.96 12.67
HC13 Silt 6-6.5 28.54 40.54 10.22 6.81 2.55 0.95 1.77 2.07 0.91 19.53
HC15 Silt 7-7.5 26.71 43.66 8.12 7.14 6.78 2.7 0.75 1.84 0.9 14.77
HC18 Silt 8.5-9 30.63 37.67 4.55 5.48 4.66 1.88 0.91 0.61 0.38 13.24
Range
14.92-
30.63
37.67-
45.70
4.55-
11.33 5.48-8.17 2.55-6.78 0.95-2.70 0.75-1.77 0.61-2.11 0.38-1.10
12.45-
19.53
23.38 41.95 9.25 6.87 5.15 1.92 1.03 1.71 0.87 14.42
HD1 Sandy silt 0-0.5 39.46 30.67 11.26 7.81 6.63 2.23 1.19 1.92 1.1 12.45
HD5 Silt 2-2.5 22.84 46.1 9.56 6.42 5.96 1.78 0.56 1.5 1.05 13.56
HD7 Silt 3-3.5 17.67 41.24 10.25 6.61 5.36 1.73 0.56 1.89 0.79 14.77
HD11 Silt 5-5.5 28.64 46.92 10.81 7.7 6.51 1.86 0.92 2.11 0.96 12.67
HD13
Muddy
sand
6-6.5 30.36 44.65 10.23 7.17 6.37 1.9 0.9 2.07 0.91 19.53
HD15 Sandy silt 7-7.5 49.53 17.43 9.31 6.84 5.92 2.16 0.92 1.84 0.9 14.77
HD18 Sandy silt 8.5-9 54.2 12.59 2.87 2.9 3 1.96 2.07 0.61 0.38 13.24
Range
17.67-
54.20
12.59-
46.92
2.87-
11.26 2.90-7.81 3-6.63 1.73-2.23 0.56-2.07 0.61-2.11 0.38-1.10
12.45-
19.53
34.67 34.22 9.18 6.49 5.67 1.94 1.01 1.71 0.87 14.42
Site Four
Average
Site One
Average
Site Two
Average
Site
Three
Average
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of Al2O3, SiO2, and MgO, is related to the abundance of clay minerals [10]. The iron content in the
sediments of the sites1, 2, 3, and4 were between 4.95-8.44%, 5.95-8.55%, 5.48-8.17%, and 2.90-7.81%
with an average 6.54%,7.23%, 6.87%, and6.49% of sites 1,2,3, and 4 respectively (Table 7), this
reflects the oxidation conditions in the sediments of the study area. Magnesium is mainly present
in the sediments of the study area within the crystal lattice of the clay minerals. Magnesium is
included in the octa hedral position of some clay minerals such as palygorskite and chlorite. As
for the montmorillonite mineral, it is done by total replacement of aluminum in these sites and as
indicated by [12].
Study area sediments show a remarkable increase in sodium concentrations, reaching between
1.55-2.56%, 1.45-2.45%, 0.95-2.70%, and1.73-2.23 of sites 1,2,3,and 4 respectively (Table 7).
Sodium is present in region sediments as a major phase within the structural of clay minerals or
as adsorbed to them. Sodium is one of the basic elements included in the crystal network of
montmorillonite minerals, may be the possibility of fixing sodium in clay minerals by means of
ionic substitution with potassium. The range of SO3 in study area is between 0.78-1.98%, 1.45-
1.95%, 0.75-1.77%, and 0.56-2.07% of sites 1, 2, 3, and 4 respectively (Table 7). The presence
of sulfates in the study area is associated with the presence of sulfate minerals such as gypsum,
which was proven to be present in the mineral study. Where the proportion of gypsum mineral in
the samples HB3, HC11, HD5, HD7, HD15, and HD16 was high and this gives evidence that the
environment was drier. The concentration of K2O reached between1.49-2.04%, 0.65-2.05%,
0.61-2.11%, and 0.61-2.11% (Table 7) of sites 1, 2, 3, and 4 respectively (Table 7). The
presence of potassium is associated with clay minerals, especially in the mineral illite, whose
presence was proven during the mineral study, where potassium enters as an essential element
between the Illite sheets and works to link these plates among themselves.
The concentration of titanium in the samples ranged between 1.22-1.66%, 0.94-2.01%, 0.38-
1.10%, and 0.38-1.10% of sites 1, 2, 3, and 4 respectively (Table 7). TiO2 is abundant in clay
minerals especially in montmorillonite and kaolinite minerals, where Ti is absorbed on kaolinite.
Titanium is concentrated in fine particles, as its concentration increases as the size of the
particles decreases due to the increase in the surface area. The oxides; Silica, calcium oxide,
aluminum, magnesium and iron were considered basic components, while the oxides - alkali
potassium, sodium, titanium oxide and sulfate were secondary components in lower
572-241Bas J Sci 40(1) (2022) K. J Alsudani et al.
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Mesopotamia. Loss on ignition includes all the losses by ignition of CaCO3, organic matter and
evaporates (F, Cl), in addition, part of the losses by ignition are due to the water present in its
various forms (H2O-, H2O+) in the clay minerals. The amount of unburned carbon in the
sediment represents Loss on ignition [8].Loss on ignition content in site one ranged between
15.76-21.25%with an average 18.62%, while site two is from 9.76-19.65% with an average
13.35% , site three 12.45-19.53% with an average 14.42% and for site four is from 12.45-
19.53% with an average 14.42% (Table 7).
4. Conclusions
The grain size analysis showed the predominance of silt in the study area. Study area
sediments were classified as soft sediments mainly represented by Silt, Sandy silt, Mud, and
Muddy sand. The environment affecting the sediments of study area is the calm environment.
The sediments were derived, was characterized by the predominance of mechanical weathering
processes and that the climate of the region was dry to semi-arid. The diversity of the source
rocks in the sediments of study area due to the great variation in clay and non- clay minerals.
The presence of Palygorskite mineral in a high percentage in different depths of the study area
gives evidence that the prevailing sedimentary environment conditions were drier. The increase
in the concentration of magnesium (MgO) in the sediments is related to the abundance of the
mineral Palygorskite. Most of the main elements in the sediments of study area, represented by
(SiO2, Al2O3, Fe2O3, MgO, Na2O, and K2O) were found in a main phase within the crystal lattice
of clay minerals.
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572-241Bas J Sci 40(1) (2022) K. J Alsudani et al.
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1
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PalygorskiteMontmorilloniteChloritePalygorskite - Illite
2
SiOCaO
3
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2
Al
3
O
2
eFMgO
3
SOO
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