Introduction
Since early times, clay has been considered as a noble material due to its abundance, low-cost, efficiency, and eco-friendliness compared to other commercial materials (Mkaouar et al. Reference Mkaouara, Maherzib, Pizette, Zaitan and Benzina2019). Clay minerals are aluminosilicates that are able to exchange cations. The great variety of clay types allows a wide range of uses. The physicochemical properties of clay minerals have been investigated for possible application in many fields including cosmetics (Khiari et al. Reference Khiari, Mefteh, Sánchez-Espejo, Cerezo, Aguzzi, López-Galindo, Jamoussi and Viseras Iborra2014), pharmacology (Mefteh et al. Reference Mefteh, Khiyari, Sanchez-Espejo, Aguzzi, Lopez Galindo, Jamoussi and Viseras2014), environmental application (Ghrab et al. Reference Ghrab, Boujelben, Medhioub and Jamoussi2014; Ghnainia et al. Reference Ghnainia, Eloussaief, Zouari and Abbes2016), ceramics (Jemaï et al. Reference Jemaï, Sdiri, Ben Salah, Ben Aissa, Bouaziz and Duplay2017), and fluid refining (Ashraf et al. Reference Ashraf, Hussain, Rasheed, Iqbal, Riaz and Arif2017). The use of clay minerals has evolved with technological developments in such fields as adsorption of terpenic compounds for the synthesis of an insecticidal formulation (Ghrab et al. Reference Ghrab, Eloussaief, Lambert, Bouaziz and Benzina2017).
Tunisia has significant reserves of clay materials and several studies have focused on them. For instance, the reserves of kaolin in the Numidian Flysch in Sidi El Bader were investigated by Felhi et al. (Reference Felhi, Tlili, Gaied and Montacer2008) and Hafez et al. (Reference Hafez, Naser, Ibrahim, Abou El-magd and Hashem2016). Another reserve of smectite in the Coniacian–Santonien Aleg formation was studied by Jarraya et al. (Reference Jarraya, Fourmentin, Benzina and Bouaziz2011).
The Eocene deposit reveals a variety of facies extending from continental deposits in the south to deep marine deposits in the north. This paleogeographic dissimilarity is due to the compressive Triassic halokinetic events along the tectonic fault corridors and folds of the Atlassic domain (Bédir Reference Bédir1995; Boukadi and Bédir Reference Boukadi and Bédir1996). The continental facies are located in two different areas: around Kasserine Island (Burollet Reference Burollet1956; Zouari Reference Zouari1984) and Jeffara Island which were formed at the end of the Upper Cretaceous in the south of Tunisia. The presence of palygorskite deposits, sometimes including sepiolite, has been described by Kadri et al. (Reference Kadri, Matmati, Ben Ayed and Ben Haj Ali1986), Abdeljaoued (Reference Abdeljaoued1991, Reference Abdeljaoued1997), and Jamoussi et al. (Reference Jamoussi, Bédir, Boukadi, Kharbachi, Zargouni, López-Galindo and Paquet2003), who studied the mineralogy and geochemistry of Eocene sequences in many localities around the two islands. The identification of the continental Eocene in central Tunisia was investigated in Jebel Chaambi and the presence of continental facies on the southeastern flank of the Jebel Kebar was revealed (Sassi et al. Reference Sassi, Triat, Truc and Millot1984). Similarly, the continental Eocene facies were detected by Kadri et al. Reference Kadri, Matmati, Ben Ayed and Ben Haj Ali1986 in the Lessouda and Koumine mountains. The same facies were studied in the Chamsi mountain by Jamousssi et al. (Reference Jamoussi, Abbès, Fakhfakh, Bédir, Kharbachi, Soussi, Zargouni and López-Galindo2001) while Abdeljaoued (Reference Abdeljaoued1983, Reference Abdeljaoued1997) determined the continental Bouloufa formation which dated from Lower Eocene in the northern “Chain of Chotts.”
The current study aimed to characterize the continental Eocene deposit at the southern end of the northern axis of Tunisia, the Khanguet Rheouis in the Sidi Bouzid region. Significant reserves of clay minerals of Eocene age were observed. This Eocene deposit in Khanguet Rheouis constitutes the Cherahil formation. Cherahil sediments were deposited on the limestone of the Abiod formation and are surmounted by the Quaternary deposits of the Segui formation.
The Eocene dolomite in central Tunisia has been studied by a number of researchers who explained the occurrence of Eocene dolomite which contains considerable quantities of two fibrous clays (palygorskite and sepiolite). These clays are enriched with other detrital aluminosilicates (illte, smectite, and kaolonite), quartz, and lesser quantities of gypsum and halite. The present study focused on the Eocene dolomite associated with palygorskite in Khanguet Rheouis. The Eocene deposit in the Khaguet Rheouis region of Tunisia has been little studied, but is of fundamental importance for a more complete understanding of the mineralogy of this region.
The mineralogy and geochemical characteristics of the Eocene deposits in Khanguet Rheouis are of great interest. In fact, the homogeneity and the distribution of palygorskite through the dolomitic sequence were evaluated in this study. Finding out whether this clay represents a real economic potential for Tunisia is important. Similarly, can the deposits of primary materials be used widely by the medical and pharmaceutical industries?
GEOLOGICAL SETTING
The outcrops of the Eocene clays in Khanguet Rheouis are located at the junction zone between Jebel Rheouis and Jebel Boudinar (Fig. 1). This area constitutes the southern end of the north–south axis in Tunisia and presents a complex diapiric structure (Abdeljaoued Reference Abdeljaoued1991).
Fig. 1. Location and simplified geological map of Khanguet Rheouis.
The Eocene clays are limited at the southern end of Jebel Rheouis by a narrow strike corridor, marked by two major fractures trending NW–SE. An east–west section of the Khanguet Rheouis region shows that the Eocene clay is limited by two faults: (1) an overlapping inverse fault (FI) trending NNE–SSW in direction; and (2) a strike fault (FD) trending NNW–SSE in direction, disturbed by Triassic evaporite activity (Fig. 1).
The CA and CB sections were made at the joint area of Jebel Meloussi at Khanguet Rheouis. Because the two sections have the same lithostratigraphic succession, a single lithostratigraphic log is presented (Fig. 2). This log reveals the lithostratigraphic succession and details of the sampling from the base to the top. The white chalky limestones and the green clays of the Abiod and El Haria formations were covered by the Cherahil formation of Eocene age. The Cherahil formation consists mainly of clay alternating with dolomitic banks.
Fig. 2. Lithological description of Khanguet Rheouis.
Materials and Methods
Sampling
In the section studied was the Eocene outcrop represented by the Cherahil formation (75 m). The clay strata alternate with thin dolomite ones. The clay strata become thicker towards the top. The observations of mineral samples from the outcrop show three distinct clay facies: Green clay localized at the base of the geological section, red clay in the middle, and green clay at the top. To determine the mineralogy of the Cherahil samples, nine specimens were analyzed (Fig. 2).
Chemical Analysis
Chemical analysis of the raw samples was performed by dissolving 1 g of dried sample in 25 mL of HNO3 and 25 mL of HCl. The mixture was evaporated to dryness, then bidistilled water was added to eliminate the remaining traces of acid, and the suspension was filtered with an ashless filter paper (Whatman®) (Eloussaief et al. Reference Eloussaief, Bouaziz, Kallel and Benzina2013a). Finally, the chemical composition was determined by atomic adsorption spectrophotometry (ICP-AES). The residue, consisting of insoluble silica (SiO2), was estimated by gravimetry (Benzina Reference Benzina1990) after calcination at 900°C for 1 h. Loss on ignition (LOI) was considered to be the weight percent difference between samples heated at 100 and 1000°C.
Mineralogical Analysis
X-ray diffraction (XRD) data were obtained using a Philips® X-Pert (Philips Analytical, Almelo, The Netherlands) PW 1710 diffractometer equipped with a CuKα radiation source operating at 40 kV and 40 mA. All XRD data were collected under the same experimental conditions, i.e. over the angular range of 3–45°2θ with an analysis time of 30 min. Natural samples of rock and clay fraction were used to identify the mineralogical associations. The ≤2 μm fraction was separated by sedimentation and centrifugation at 2500 rpm (1540×g) for 20 min (Sdiri et al. Reference Sdiri, Higashi, Hatta, Jamoussi and Norio2010; Eloussaief et al. Reference Eloussaief, Sdiri and Benzina2013b). The diffraction data were analyzed using the X’Pert HighScore Plus® software (Martin-Ramos Reference Martín-Ramos2004).
Textural Analysis
The textural analysis was performed only for the representative sample AR6 from the Cherahil formation. The specific surface area was determined by the adsorption-desorption isotherms of nitrogen (BET-Specific Surface area and Porosity Analyzer 2020, Micromeritics, Merignac, France).
FTIR Spectroscopy
The Fourier-transform infrared spectrometry (FTIR) was recorded in the 4000–400 cm–1 range using a Bruker Equinox 55 spectrometer (Bruker, Kennewick, Washington, USA). The samples were prepared using the KBr pellet method. All the samples were studied under the same hydration conditions, kept over H2SO4 solutions (relative humidity RH = 45%). The clay mixtures and dried KBr (ratio 1:200) were subjected to a pressure of 785 MPa. Statistical treatment of the data was carried out using the SPSS 10.0 program.
Morphology Analysis
The morphology of the raw sample was examined using scanning electron microscopy (SEM - Philips® 30 SEM, Philips Electron Optics, Ottoway, Australia) and microanalysis was conducted by associated energy-dispersive X-ray spectroscopy (EDX). The raw sample fragments were coated with gold prior to analysis (Eloussaief et al. Reference Eloussaief, Kallel, Yaacoubi and Benzina2011). The SEM images were obtained using a secondary electron detector.
RESULTS AND DISCUSSION
Chemical Analysis
Chemical analysis of the Cherahil formation samples (Table 1) showed that the clay fractions have significant SiO2 and Al2O3 contents, ranging between 15 and 35.3 wt.% for SiO2 and between 2.5 and 6 wt.% for Al2O3. All of the samples displayed a large MgO content ranging from 5 to 12 wt.%, except for the middle samples. The large MgO content is related to dolomite (Zhu et al. Reference Zhu, Chen, Liu, Xu and Xie2016). Further, Mg2+ may be incorporated in the octahedral sheet of phyllosilicates (Tlili et al. Reference Tlili, Felhi and Montacer2010). The Fe2O3 content varied from 0.7 to 3.45 wt.%. The clays are impure and heterogeneous. The iron deficiency is associated with the reduced depositional environment. The remaining Fe is the iron oxide which was already obtained from the clay.
Table 1 Chemical composition (wt.%) of samples.
On the other hand, the alkaline cation contents of the samples revealed that the amounts of K2O and Na2O do not vary significantly. The small K2O contents are due to the trace amounts of potassic clay minerals, probably illite (Felhi et al. Reference Felhi, Tlili, Gaied and Montacer2008). The AR2 sample, located below the gypsum layer, is an exception as it contains 0.11 wt.% of Na2O. This richness in Na2O is associated with the alteration of the gypsum member. The largest LOI, determined by calcination, was attributed to the evaporation of physically bound water, the dehydroxylation of clay minerals, and the decomposition of carbonate minerals.
A negative correlation was observed between Al and Mg (Fig. 3), which means that Al belongs to clay minerals and Mg belongs mostly to dolomite in the lower part of the Cherahil formation. Al and Mg belong to both the clay and non-clay fractions of the collected samples. Another negative correlation was found between Al and Mg, indicating that Ca belongs mostly to dolomite. The calcium does not belong to the fibrous structures. It can be derived from the impurities associated with the clay minerals. The curves show correlations between Al2O3/Na2O and Al2O3/K2O. Potassium and sodium, therefore, are incorporated into the interlayer space of the clay minerals and the positive correlation with Al2O/Fe2O3 confirms that Fe occupies the octahedral site of the clay mineral. It may also be present in the form of Fe (oxyhydr)oxide.
Fig. 3. Chemical composition correlated with the locations of the samples collected.
Mineralogical Analysis
The XRD pattern of sample AR6 was considered to be representative because that sample contained a large percentage of palygorskite (Fig. 4) as indicated by the reflections at 10 Å (Zha et al. Reference Zha, Huang, Wang, Chang, Ding and Ma2013). The palygorskite is associated with dolomite and quartz which were detected by the (104) reflection at 2.88 Å and the (101) reflection at 3.34 Å.
Fig. 4. XRD patterns of total rock (TR) and oriented aggregates: normal (N), glycolated (G) and heated, at 550°C (H), of representative sample (AR6)
The mineralogical compositions of all the samples (Table 2) show that the base of the Cherahil formation is moderately rich in palygorskite associated with dolomite. The findings obtained were correlated with the chemical analysis which confirmed the presence of carbonate and magnesium elements. Toward the middle level of the Cherahil formation, the dominant palygorskite is related to a decrease in carbonate and magnesium in samples AR5, AR6, and AR7.
Table 2 Mineralogical composition of samples.
For some levels, the palygorskite was associated more with dolomite and siliceous crystals which reach up to 80 wt.%. Palygorskite alternates with dolomite levels, especially toward the lowest and upper most parts of the Cherahil formation. Further, the association palygorskite/dolomite is a result of the trapped clay between the dolomite blocks.
Overall, the results of mineralogical analyses of the samples collected from the Cherahil formation show a lateral homogeneity of the Eocene deposit clay from east (CA) to west (CB) (Fig. 5).
Fig. 5. Mineralogical variation of Cherahil formation samples in the CA and CB sections.
Textural Analysis
The nitrogen adsorption-desorption isotherms of the representative sample AR6 (Fig. 6) together with the BET specific surface area (Table 3) were classified as type III behavior by the classification of Brunauer, Deming, Deming, and Teller (BDDT) (Brunauer et al. Reference Brunauer, Deming, Deming and Teller1940). The curves of AR6 had different hysteresis loops compared with those of smectite (Park et al. Reference Park, Godwin, Ayoko and Frost2011; Affouri et al. Reference Affouri, Eloussaief, Kallel and Benzina2015). The saturation of AR6 by N2 was not completed. This analysis revealed that the AR6 structure consists of smaller fibers which build up bundles of developed pore channels.
Fig. 6. N2 adsorption/desorption isotherms of sample AR6 from the Cherahil formation.
Table 3 Specific surface area (S BET), pore volume (V p), and pore diameter (P s) of representative sample AR6.
The main textural constants are summarized in Table 3. The BET specific surface area was estimated to be 61 m2/g.
FTIR Spectroscopy
The FTIR spectra revealed important peaks (Fig. 7). Firstly, the band at 3543 cm–1 was assigned to coordinated water; a contribution of the OH-stretching mode in Al–Mg–OH, Fe–Mg–OH, and Fe–OH groups was also considered. The peak observed in sample AR6 agreed well with this observation because it is rich in magnesium. The lowest wavenumbers occurred between 1200 and 500 cm–1, characteristic of Si–O groups in the tetrahedral sheet. Frost et al. (Reference Frost, Locos, Ruan and Kloprogge2001) assigned the absorption bands found between 990 and 615 cm–1 to M–OH deformation. For the sample studied here, the peak located at 1190 cm–1 was regarded as characteristic of palygorskite. The presence of small quantities of impurities can easily be detected in the FTIR spectra (Fig. 7). Calcite or dolomite was detected in the AR6 sample by the characteristic band at 1433 cm–1 and a shoulder at 876 cm–1. As for quartz, it was detected at 728 and 615 cm–1.
Fig. 7. FTIR spectra of representative sample AR6.
Morphology
Representative samples of the basal level (AR1, AR3), middle level (AR6), and top level (AR7) were chosen for SEM analysis (Fig. 8); the results reflected the compositions determined by XRD (Table 4).
Fig. 8. SEM images (D: Dolomite, P: Palygorskite) showing the morphology of the samples collected from the Cherahil formation.
Table 4 EDX microanalyses of samples AR1, AR3, AR6, and AR7′.
The SEM image of the AR1 sample (Fig. 8) showed that the bottom of the Cherahil formation consists of an abundance of well developed rhombohedral crystals which correspond to dolomite. The presence of dolomite in AR3 was confirmed by EDX analysis. This analysis revealed a Mg content of 9% and average contents of Al and K of 4 and 0.4%. All the samples showed a smaller K content. These results are in total agreement with the chemical and mineralogical analyses.
The AR6 sample was made up of rod-like particles of variable thicknesses and lengths packed densely in a randomly oriented network (Xu et al. Reference Xu, Wang and Wang2014). The presence of palygorskite increases toward the middle of the Cherahil formation. Palygorskite is associated with dolomite crystals along this formation (AR3), indicating that the dolomitization process began during early diagenesis. Moreover, the mineral impurities reduce the size and crystallinity of the fibrous clay from the clay deposits in the lower part of the Cherahil formation. The characteristic morphology correlates with some other studies including those of Yuan et al. (Reference Yuan, Li, Guan, Liu, Xiao and Zhang2007) and Qiu et al. (Reference Qiu, Xie, Liu, Chen, Xie and Li2015). The presence of palygorskite was confirmed by a Mg content of between 6.3 and 9.72%.
On the other hand, the density of crystallized palygorskite in sample AR7 was low. The rod-like particles were in parallel orientation and packed densely, with impurities. Palygorskite exhibits that same fibrous texture and appears most commonly as chaotic arrangements of short fibers, i.e. of <2 μm. The crystal lattice has the structure of a hollow brick the cavities of which are filled with water (Zhang et al. Reference Zhang, Wang, Zhang, Liu and Wang2015).
In terms of other palygorskites from Saudi Arabia, New Zealand, Senegal, and the United Arab Emirates described in previous studies (Cagatay Reference Cagatay1990; Soong Reference Soong1992; Garcia-Romero et al. Reference Garcia-Romero, Suarez, Santaren and Alvarez2007; Draidia et al. Reference Draidia, El Ouahabi, Daoudi, Havenith and Fagel2016), the geochemical and textural results observed here indicate that the genesis of this type of clay was probably by direct precipitation from Ca-, Mg-, Al-, Fe-, and Si-rich solutions or recrystallization of smectite. The morphology of palygorskite resembles that of a 2:1 fibrous phyllosilicate with isolated fibers and associated with dolomite and small quantities of quartz (Cagatay Reference Cagatay1990; Soong Reference Soong1992; Garcia-Romero et al. Reference Garcia-Romero, Suarez, Santaren and Alvarez2007; Draidia et al. Reference Draidia, El Ouahabi, Daoudi, Havenith and Fagel2016). The palygorskite contains mainly Mg, Al, Si, and Fe with a significant Mg content. The Mg concentrations combined with the presence of dolomite were sufficient to generate the palygorskite material.
The formation of deposits of the palygorskite in the present study zone occurred during evaporative oxidizing conditions and took place during Eocene, Oligocene, and Mio-Pliocene times (Cagatay Reference Cagatay1990; Soong Reference Soong1992; Garcia-Romero et al. Reference Garcia-Romero, Suarez, Santaren and Alvarez2007; Draidia et al. Reference Draidia, El Ouahabi, Daoudi, Havenith and Fagel2016). The formation of palygorskite required specific conditions such as alkaline pH and large amounts of Mg. The chemical changes were probably due to climatic fluctuations and/or gypsum precipitation. The amount of Mg may have led to the various generations of dolomite and to the appearance of palygorskite.
Conclusions
The mineralogy and physiochemical characterization of Cherahil-formation material revealed the presence of Mg-rich clay and dolomite crystallization increasing towards the top of the formation. Palygorskite deposits of Eocene age showed a lateral homogeneity in the Cherahil formation from east (CA) and west (CB). This material represents a very important reserve of palygorskite (80%) and should be investigated for use in the pharmaceutical industry, e.g. as a hydrated adsorbent (gel) or a dehydryated adsorbent, and (following slight purification) as an anti-diarrheal product, and in cosmetics products. It could also be a valuable resource in other industries, e.g. in the separation of fluids, in agriculture as a suspended fertilizer, in environmental applications as an adsorbent in photo-catalysis, and also in drilling technologies.
ACKNOWLEDGMENTS
The authors are grateful to Prof. Abdelmajid Dammak for his checking of the English in the manuscript.
Compliance with Ethical Standards
CONFLICT OF INTEREST
We confirm that there are no known conflicts of interest associated with this publication and there has been no significant financial support for this work that could have influenced its outcome.
