International Journal of Civil Engineering and Technology (IJCIET)
Volume 10, Issue 04, April 2019, pp. 1538-1547, Article ID: IJCIET_10_04_160
Available online at http://www.iaeme.com/ijciet/issues.asp?JType=IJCIET&VType=10&IType=04
ISSN Print: 0976-6308 and ISSN Online: 0976-6316
© IAEME Publication
Scopus Indexed
GEOCHEMISTRY, QUALITY APPRAISAL OF
GROUNDWATER AND HYDROGEOCHEMICAL
PROCESS IN MIDDLE OUERRHA, TAOUNATE,
RIF – MOROCCO
Ahmed El Bakouri*
Team of Waters, Wastewaters, Laboratory of Environment and Quality, Faculty of Sciences,
Ibn Tofail University, Kenitra, Morocco
Khadija El Kharrim
Team of Waters, Wastewaters, Laboratory of Environment and Quality, Faculty of Sciences,
Ibn Tofail University, Kenitra, Morocco
Mohamed Tayebi
Team of Valorisation of Georesources and Territorial Planning, Laboratory of Geosciences
and Environment, Faculty of Sciences, Ibn Tofail University, Kenitra, Morocco
Driss Belghyti
Team of Waters, Wastewaters, Laboratory of Environment and Quality, Faculty of Sciences,
Ibn Tofail University, Kenitra, Morocco
*Corresponding Author
ABSTRACT
A hydrogeochemical study was conducted in the Middle Ouerrha, Taounate,
Morocco, to identify the mechanisms responsible for the chemical compositions of the
shallow groundwater and to document water quality. Different physicochemical
parameters are determined, and correlation were used to reveal the hydrogeochemical
characteristics of the shallow groundwater, and the potential water-rock interactions.
Groundwater samples were collected from a natural source and two wells.
Unfortunately, the groundwater of Taounate district have know the problem of salinity,
which threatens their quality. In the Hammam source were characterized by high levels
of salinity. The temperature, pH, electrical conductivity, salinity, Ca, Mg, Cl, SO4, K,
NO3, Na and HCO3 were determined. The predominant mechanism controlling
groundwater chemistry proved to be the dissolution of carbonates, salt red marls and
gypsum. The purpose of this study was to identify salinity water sources and
quantitatively analyze their composition using comprehensive hydrogeochemical
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Ahmed El Bakouri, Khadija El Kharrim, Mohamed Tayebi and Driss Belghyti
determinations. This approach facilitates important decision making for water salinity
disaster control, and quickly and accurately solves the fuzzy and uncertain
characteristics of water quality. In addition, the method also can be used at various
scales for water resources development, regional water resource evaluations, and
environmental assessment.
Key words: Hydrogeochemical, Groundwater, Salinity, Taounate, Morocco.
Cite this Article: Ahmed El Bakouri, Khadija El Kharrim, Mohamed Tayebi and
Driss Belghyti, Geochemistry, Quality Appraisal of Groundwater and
Hydrogeochemical Process in Middle Ouerrha, Taounate, Rif – Morocco..
International Journal of Civil Engineering and Technology, 10(04), 2019, pp. 15381547
http://www.iaeme.com/IJCIET/issues.asp?JType=IJCIET&VType=10&IType=04
1. INTRODUCTION
Groundwater is the major source of fresh water for drinking, irrigation, and other economic
sectors [1, 2]. Day by day groundwater reserves are being depleted due to numerous natural
and anthropogenic cause. The physicochemical properties of water are influenced by the
various natural factors. They are climatic factors [3, 4], hydrological characteristics [5, 6],
topography and lithological factors [7]. The decline and degradation of its quality are not easily
perceived. Generally they come in addition to easily accessible surface waters. In addition,
drought is one of the most important phenomena resulting from climate variability and change.
Faced with this situation, it is therefore necessary to launch hydrogeochemical and
hydrogeological studies at the regional scale, integrating both the northern and southern part of
the Taouante area.
2. STUDY AREA
2.1. Geology
The study area with semi-arid climate is located in the Middle Ouerrha basin, in rifaine chain,
northernmost part of Morocco, belongs to the alpine building, betico-rifo-tellian from the
western Mediterranean. It is separated from the Cordilleras by the strait of Gibraltar.
In the Taounate area, Figure 1, the geological formations are complex; we could distinguish
several geological systems:
 Triassic: formed essentially by salt red marls and gypsum. It could be qualified the
Allochthonous Triassic. It has been the subject of various tectonic and
palaeogeographic interpretations, around the western Mediterranean, especially in
the Betic Cordillera in Andalusia [8], as polygenic gypsum matrix breccia of
sedimentary origin.
 Jurassic: the formations are largely developed under two main facies, dolomitic
limestones of the Liassic that form large massifs, and a schisto-sandstone flysch of
Callovo-Oxfordian.
 Cretaceous: Characterized by marls and marl-limestone, at the Aptian-Albian the
detrital terrigenous character of the sedimentation is accentuated and corresponds
to the flysch of Albian-Aptian.
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


Eocene: The lower and middle Eocene are presented in the form of white flint
marls, these outcrops are rare and discontinuous, since in the area of Taounate - Ain
Mediouna.
Miocene: qualified as ante-nappe in Lower Miocene by a detrital marl-sandstone
series, whose outcrops are also widely dispersed. Their sedimentation continues
until the end of the Middle Miocene [9].
Quaternary: Quaternary evolution is reflected in the course of the great wadis.
2.2. Stratigraphy
In the studied region, the upper Miocene is qualified post-nappe, it normally overcomes the
lower Miocene, or rests directly in unconformity on any subrifaine ante-Miocene series. The
Upper Miocene formations constitute thick transgressive series on the secondary lands, and fill
all the collapsed basins of the Middle Ouerrha. The detailed study of these formations at the
level of the Taounate basin makes it possible to distinguish three stratigraphic levels:
 A basic level, conglomeratic, with rounded elements (pebbles) of varied nature,
some of which belong to the underlying Upper Cretaceous, this is a conglomerate
that sometimes has a certain bedding marked by the orientation of the small
flattened pebbles, Figure 2. The cement of the elements of the conglomerate is of
sandstone-sand nature. This basic level consists of three conglomeratic and detrital
sandstone bars interspersed with marly levels, Figure 3.
 A medium level, consisting of a thick series of blue marls with shark teeth.
 Finally, at the upper level reappear sandy or sandstone detritic formations
sometimes conglomerates with however small palettes less bulky than in the basic
level. This last level appears slightly discordant could represent the second higher
Miocene.
Figure 1. Geological map of the study area, Taounate – Morocco
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Ahmed El Bakouri, Khadija El Kharrim, Mohamed Tayebi and Driss Belghyti
Figure 2. Cross-section in the upper Miocene Formation of Taounate Basin
Figure 3. Stratigraphic Log of the Upper Miocene Formation of the Taounate Basin
3. METHODS
Groundwater samples were collected from a natural source Hammam and two wells, Kara and
Twansa, of different locations in the study area during the period May, August, November
2016 and February 2017.
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Geochemistry, Quality Appraisal of Groundwater and Hydrogeochemical Process in Middle
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The analysis of the physicochemical parameters was carried out with the use of some
chemicals, materials and some apparatus as:
 The temperature was measured in situ using an alcohol thermometer.
 The pH by a pH meter Brand ADWA, model AD1030 with combined electrode.
 Conductivity (EC) and salinity were determined by an conductivity-meter brand
OHAUS, model STARTER ST3100C-F.
 Ca, Mg, Cl and HCO3 were determined by volumetry.
 SO4 and NO3 by UV spectrometer Brand SECOMAM, model UVILINE 9400.
 K and Na were measured by ICP.
4. RESULTS AND DISCUSSION
4.1. Physicochemical characterisation of groundwater
The different physicochemical parameters of groundwater are shown in table 1:
4.1.1. Temperature (T)
Important factor in all chemical reactions, temperature is an essential element to control all the
physicochemical parameters of a given system. It controls the solubility, density and viscosity
of water, as well as the speed of chemical reactions. It has a direct effect on the conductivity
and pH determination of the water.
In the study area, the temperature of the water reaches its maximum value (23 °C) at the
Hammam source during the low-water season (August 2016). The minimum value is recorded
in the Twansa well of 18.5 °C (May 2016). The temperature difference of 0.5 °C between the
Hammam source and the Kara well can be due to the geological formations, since in the
Hammam source there is dominance of the limestone rock formations, whereas in the well Kara
there are the formations hard schists at the bottom, which appear along the Oued Ouerrha. The
difference of 2.5 °C between the Hammam source and the Twansa well is due to the southern
exposure of the source and soft marly formations in the Twansa area.
4.1.2. pH
The physicochemical equilibrium of a source or a well is essentially determined by the pH. The
latter is very sensitive to environmental and geological factors such as, temperature, salinity,
lithological nature of the lands crossed, etc. Acidic pH can influence dissolution of salts from
the aquifer rocks and increase the metal and TDS load in the groundwater [10].
The spatial and temporal variation in pH shows small fluctuations with average values close
to neutrality (7.63), they vary between 7.26 and 7.77 in the Hammam source, between 7.26 and
8.5 in the Kara well and between 7.25 and 7.61 in the Twansa well. This neutral to slightly
basic character could be attributed to the sedimentary nature of the mainly carbonate secondary
lands formed by limestone, dolomite and marl, hence the buffer effect of the formations,
through all the reactions of the potential aquifer system of hydrogen (water/insoluble
carbonates/CO2 soluble bicarbonates). This variation in pH is due to the alluvial clay and sand
cover that isolates the water table, thus the amount of dissolved salt in the Hammam source
and the Kara well, which regulate the acid-base balance of the water.
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4.1.3. Electrical conductivity
The measurement of the conductivity is a good appreciation of the degree of mineralization of
a water. It is proportional to the quantity of dissolved mineralizable salts. High conductivity in
most cases reflects high salinity, which can be of natural origin [11].
The spatial and temporal evolution of the conductivity shows an increasing enrichment in
the Hammam source especially during the low-water period which varies between 22700 and
26900 μs/cm, whereas in the Kara and Twansa well it varies between 1510 and 1638 μs/cm
and between 3280 and 3700 μs/cm respectively. This high conductivity can be due to a natural
origin by leaching of carbonate lithological formations (Gypsum, red salt marl, dolomite,
limestone, etc.), hence the release of Ca, Mg, HCO3 etc., especially for the Hammam source.
4.1.4. Salinity
Salinity is the mass of salts or ionic compounds dissolved in a liter of water; it is expressed in
g/L of water. An ionic compound or crystalline ionic solid consists of positively charged
cations and negatively charged anions regularly arranged in space. An ionic crystal is
electrically neutral. The salts can be of geogenic origin from rock weathering or anthropogenic
origin like urban runoff, sewage, industrial discharge and type of material used in piping for
water supply [12].
The salinity of the water varies from one zone to another, it is between 13.68 and 16.51 g/L
in the Hammam source, 0.73 and 0.88 g/L in the Kara well and 1.46 and 1.93 g/L in the Twansa
well. The high salinity is mainly due to leaching and/or water-rock contact of the saline marl
formations of the Tortonian by aquifer waters, Figure 4, while the low mineralization is due to
dilution by aquifer waters or the absence of gypsum levels.
4.1.5. Calcium
Water is composed of many mineral and organic elements. Its richness in minerals varies
according to the composition of the soils it crosses. The calcareous grounds will give a water
rich in calcium.
Calcium is one of the parameters that contributes to the mineralization of water. It appears
that the groundwater of Taounate region, have quite remarkable levels of calcium. They range
between 677.4 and 941.2 mg/L in the Hammam source, between 76.9 and 112.2 mg/L in the
Kara well and between 108.4 and 176.3 mg/L in the Twansa well. This would be due to the
dissolution of the carbonate formations of Mio-Pliocene and alluvial gypsum formations of the
Quaternary.
4.1.6. Magnesium
Rainwater is very poor in magnesium; the latter comes mainly from the dissolution of carbonate
formations with high levels of magnesium (magnesite and dolomite). The kinetics of the
dissolution of these rocks is not fast. Since the dissolution time is greater than for calcite, the
high levels of magnesium generally indicate slow transit waters. The highest values are
observed in the Hammam source during the 2016 summer campaign (383.2 mg/L).
4.1.7. Sodium
Sodium can be generated from aquifer water interaction by cation exchange processes or from
anthropogenic sources like pollution from wastewater and septic tanks [13]. They results from
rapid dissolution and in large amounts of NaCl. Their presence is often very low, it comes from
the precipitations which constitute the principal leaching contribution of atmospheric
impurities of oceanic origin. The highest values, in the order of 5600 mg/L, are recorded in the
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Hammam source. These concentrations are influenced by the contributions due to the presence
of triassic formations (salt red marls) at the border of the source, silicate minerals, such as clays
or by evaporation, which is active in soils close to the surface which favors the reconcentration
of Na+. At the Kara and Twansa wells these concentrations are low compared to the source.
They range between 155 and 210.9 mg/L and between 440 and 670 mg/L respectively.
4.1.8. Potassium
Potassium concentrations range from 14.6 to 25 mg/L in the Hammam source, 5.2 to 6 mg/L
in the Kara well and 1.7 to 2.1 mg/L in the Twansa well. The presence of potassium in water
is linked to the alteration of potassium clays, the rapid and high dissolution of KCl. Potassium
is not very mobile in the surface environment and most anthropogenic inputs will be consumed
by biomass or through reactions involving clay minerals. It is an element that may have a
significant anthropogenic signal from agrochemicals or organic fertilisers [14].
4.1.9. Bicarbonates
Bicarbonate alkalinity seems to be the major source of alkalinity of groundwater, due to the
dissolution of CO2 and carbonates, oxidation of organic matter [15] and reaction of silicates
with carbonic acid [16].
The concentration of bicarbonates in water is a function of the temperature of the water,
the tension of dissolved CO2, the concentration of water in salts and the lithological nature of
the lands crossed. Significant concentrations occur in the Twansa zone with contents ranging
from 411.8 to 549 mg/L. In Hammam the concentrations are relatively low because the chloride
facies is the most dominant.
4.1.10. Sulphate
Sulphate concentration in groundwater usually remains low due to reducing conditions in the
aquifers, which inhibits sulphide oxidation [17]. The variability of sulphate levels observed in
groundwater is of great hydrogeological interest. Their origin is related to the precipitation,
which can contain significant quantities of SO4, or to the leaching of the evaporitic rocks
(gypsum, anhydrite, etc.). The highest value is recorded in the Hammam source of 1710 mg/L.
The lowest is 137 mg/L in the Kara well. According to WHO the limit value is 250 mg/L,
which makes the Hammam source undrinkable.
4.1.11. Chloride
Chloride concentrations are high and reach very high values, especially at the Hammam source.
They range between 8260.5 and 9005 mg/L, especially during the low-water period, whereas
in the Kara and Twansa wells these concentrations vary between 215.2 and 244.6 mg/L and
804.8 and 885.6 mg/L respectively, which is the acceptable limit for chloride is 250 mg/L
(WHO). These high values are due to the leaching of dolomitic marls and limestones on the
one hand and the leaching of Quarternary sediments covering the sector on the other hand.
The presence of alluvium and evaporitic sediments on the soil surface facilitates leaching.
During periods of low water, intense evaporation influences the levels, especially when the
piezometric level is close to the ground surface.
4.1.12. Nitrates
In natural conditions, the nitrate concentration does not exceed 10 mg/l in the water [18] so
nitrates concentration, beyond the 10 mg/L, is an indicator of anthropogenic pollution. They
represent the most oxygenated form of nitrogen and are highly soluble. The maximum level is
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Ahmed El Bakouri, Khadija El Kharrim, Mohamed Tayebi and Driss Belghyti
observed during the August 2016 outbreaks (19 mg/L in the Kara well and 25.7 mg/L in the
Twansa well). These high levels are due to the agricultural activities that control the migration
of nitrates from the soil surface to the roof of the aquifer through the unsaturated zone and its
subsequent movement in the aquifer.
a) Hammam
b) Twansa
Figure 4. The leached salts in the study area, Taounate – Morocco
Table 1. Results of water sample analysis of study area in May, August, November 2016 and
February 2017; T as °C, EC as µs/cm, Salinity as g/L, and other ions as mg/L (HS: Hammam source,
KH: Kara wells, TW: Twansa Wells)
ID
T
pH
EC
Salinity
Ca2+
HS 21 7.77 22700 13.68
KW 20.5 7.89 1510 0.73
TW 18.5 7.58 3280 1.65
677.4
76.9
160.6
HS 23 7.26 26900 16.51
KW 22.5 7.26 1631 0.88
TW 20 7.25 3510 1.83
696.8
85.3
176.3
HS 21.5 7.54 25800 15.79
KW 21 7.77 1638 0.88
TW 19 7.47 3430 1.46
941.2
102.2
108.4
HS 21 7.67 23300 13.94
KW 20.5 8.5 1598 0.78
TW 19 7.61 3700 1.93
701.4
112.2
168.3
Cations
Na+
May 2016
331.3
5600
41.9
160
44.2
670
August 2016
383.2
4900
50.9
170
38.3
440
November 2016
111.2
3950
41.7
210.9
63.6
530.9
February 2017
159.3
3760
37.5
155
61.3
610
Mg2+
+
K
HCO3
Anions
SO42− Cl−
24
5.2
1.7
284.5
365.4
443
1396 8260.5 24.4
185.9 226.9 17.3
253.3 840.2 25.3
25
6
1.8
250.1 1047.1 9005 1.9
347.7 249.8 215.2 19
411.8 285.8 804.8 25.7
15.6
5.9
1.7
14.6
5.6
2.1
−
329
402
549
NO3−
1710 8979.7 1.9
137
218 4.87
155.5 885.6 5.76
335.5 1425
344.65 216.5
437.37 314
8296 0.85
244.6 9.48
872.1 9.88
4.2. Correlation
For the correlation analysis ± 0.9 ≤ r2 ≤ 1 was considered as strong, 0.9 ≤ r2 ≥ 0.5 as moderate
and r2 ≤ ± 0.5 as poor [19]. Salinity is strongly correlated with Cl−, Na+ and SO42−, Figure 5.
However, Cl− and SO42− show stronger correlation signifying these is the most significant
parameter for salinity, regulated by hydrogeological and climatic factors as well as
anthropogenic factors in unconfined groundwater. In particular, evaporation (a climatic factor)
is very intense in the area. In addition, hydrogeological (weathering and water-rock
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Geochemistry, Quality Appraisal of Groundwater and Hydrogeochemical Process in Middle
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interactions) and anthropogenic factors (agricultural activities) contributed to increasing major
anion concentrations [20]. For K+, Ca2+ and Mg2+ showed moderate correlation with salinity,
which in this system originated mainly from the dissolution of mineral such as carbonates and
gypsum [21]. HCO3− and NO3− showed poor correlation with salinity. This signifies that
prevalence of Na-rich bicarbonates sources and less chance of halite sources [22]. Finally, it is
evident that dissolution of minerals due to aquifer water interaction plays a major role in
groundwater quality in the Taounate area.
Figure 5. Correlation
5. CONCLUSION
From the analysis and discussion of the results, it is concluded that the main reason for the
deterioration of the water quality of Taounate area, is the high salinity. In the aquifer,
groundwater may be ascribed to evaporation and soil salts dissolution, whereas high salinity in
confined groundwater is caused by water-rock interactions, controlling the groundwater
chemistry of the area by the precipitation of calcite and dolomite, dissolution of silicate
minerals, salt red marl and gypsum, and cation exchange, which increased SO4 concentrations
locally. Most of the maximum concentrations are recorded at the Hammam source, of SO4·Cl–
Na type, with cations ordered as Na+ > Ca2+ > Mg2+ > K+ and anions ordered as Cl− > SO42− >
HCO3− > CO32−. It is suggested that an appropriate mechanism be established for continuous
monitoring of the water resources for its hydrochemistry and hydrology so that a strategy and
action plan is developed for the conservation and restoration of this important resource.
ACKNOWLEDGEMENTS
I would like to acknowledge my work team of Ibn Tofail University, and I want to thank the
editor and the reviewers for their recommendation, their revision and evaluation of the
manuscript.
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