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Fourier transform infrared spectroscopy and thermal analyses of kaolinitic clays from South Africa and Cameroon.

1. introduction

Kaolin [[Al.sub.2][Si.sub.2][O.sub.2][O.sub.5][(OH).sub.4]] is a common phyllosilicate mineral, widely employed as raw material in ceramics, paper filling and coating, refractory, fiberglass, cement, rubber and plastics, paint, catalyst, pharmaceutics and agriculture (Ekosse, 2010; Diko et al., 2011). The minerals of the kaolin group comprises kaolinite, dickite, nacrite, and halloysite with kaolinite being the most common (Murray, 2007). Structurally they consist of the so-called 1:1 layers of combined silicate sheets (Si[O.sub.2][O.sub.5]) bonded to aluminium oxide/hydroxide [[Al.sub.2] [(OH).sub.4]] layers, which are continuous in the a- and b-axis directions and are stacked one above the other in the c-axis direction. Generally, the differences in kaolin minerals are related to the number of unit layers and manner in which they are stacked above each other (Murray, 2007; Vaculikova et al., 2011).

South Africa and Cameroon are two countries from Southern and West Africa respectively with significantly rich kaolin potential (Ekosse, 2010). As developing economies, the contribution of kaolin resources towards economic growth and sustainability of both nations is of paramount importance, however very few deposits have been sufficiently characterized for industrial purpose (Horn and Strydom, 1998; Njoya et al., 2006; Kamsue et al., 2007; Nkoumbou et al., 2009; Diko and Ekosse, 2012; Diko, 2012; Diko and Ekosse, 2014). Current exploitation of most kaolin deposits or occurrences in South Africa and Cameroon are limited to the manufacture of structural ceramic products such as bricks and roofing tiles. The selected kaolin deposits in this study (i.e. Zebediela and Duthuni kaolins in Limpopo Province, north of South Africa) are currently being exploited for bricks, while those from Cameroon (i.e. Moko and Ediki kaolins situated in the Southwest Region) are yet to be exploited for any industrial purpose. These respective deposits have been geologically, physico-chemically and mineralogically characterised in other studies (Diko and Ekosse, 2012; Diko, 2012; Diko and Ekosse, 2014). Genetically, Zebediela, Moko and Ediki deposits were classified as secondary kaolins, while Duthuni as primary (Diko, 2012). Kaolinite was identified as the predominant kaolin mineral in all four deposits, associated with quartz as major constituent, while mica (illite/muscovite) + k-feldspar (as microcline) [+ or -] goethite [+ or -] hematite [+ or -] anatase [+ or -] rutile [+ or -] ilmenite occurred in minor to trace quantities (Diko and Ekosse, 2012; Diko, 2012; Diko and Ekosse, 2014). The aforementioned mineralogical data was obtained through X-Ray diffraction analysis (XRD). Powder XRD for bulk samples were carried out using a Philips PW 1710 XRD unit operated at 40 Kv and 30 mA with a Cu-Ka radiation. The samples were mounted on sample holders with little pressure, using a blade to minimize preferred orientation of the kaolinite particles and scanned scanned for from 3[degree]20 to 60[degree] 20 at a counting time of one second. A graphite monochromator with a PW 1877 Automated Power Diffraction, X'PERT Data Collector soft-ware package was employed qualitative identification of the minerals Diko and Ekosse (2012). Diko (2012) further observed that end products from the studied South African deposits are often characterized by defects such as warping, cracking, exploding and peeling during firing which tends to impact on finished product quality. Therefore, in order to optimally exploit these kaolin resources, there is need for in-depth appraisal of the raw material properties.

Although other factors may account for defects in ceramic ware (e.g. inappropriate thermal treatment or percentage mixture of different proportions of the raw material prior to firing) the aforementioned defects in calcined kaolins may be attributed in part to the mineralogical assemblage, structural order and thermal stability of the raw material. An understanding of the degree of crystallinity, thermal behaviour and reaction dynamics during calcination are vital in characterizing kaolin for optimal exploitation (Madejova, 2003; Ekosse and Mulaba, 2008; Vaculikova et al., 2011). In this study, Fourier transform infrared (FTIR) spectroscopy, differential scanning calorimetry (DSC) and thermogravimetry (TGA) are used as complementary techniques to investigate structural order and phase transformation associated with thermal decomposition of the selected kaolins from South Africa and Cameroon in order to appraise their industrial suitability. In order to ascertain kaolinite structural order based on FTIR spectroscopy, Vaculikova et al (2011) recommended two approaches: (1) an empirical approach based on the resolution and relative intensities of OH stretching and bending vibrations of structural water in kaolinite, and (2) a numerical approach based on crystallinity indices (CI) calculated from the intensities of selected vibrational modes of structural OH bands. However in this study, only preliminary findings based on the empirical approach are reported. A more detailed study on kaolinite structural order involving comparison of the numerical approach with kaolinite CI (i.e. Hinkcley and Stoch Indices) calculated from XRD diffractograms is still on-going. In addition, thermal behaviour of the studied kaolins are compared against other kaolins with similar mineralogical assemblage and exploited for structural ceramics and refractories (e.g. Makoro and Kgwakwe kaolins, Botswana; Mayououm kaolin, Cameroon; and Mavaiela kaolins, Angola). It is anticipated that findings from this study will contribute towards improvement in end-product quality for the South African kaolinitic clays and give impetus for development of a ceramic plant in Southwest Region, Cameroon.

2. MATERIAL AND METHODS

2.1. SAMPLES

A total of four representative bulk kaolin samples from South Africa (denoted ZEB 1 and ZEB 2 from Zebediela and DUT 1 and DUT 2 from Duthuni) and four from Cameroon (denoted MK 1 and MK 2 from Moko, and ED 1 and ED 2 from Ediki) were obtained for FTIR, DSC and TGA analyses. Representativity was ensured by collecting the samples from two main heterogeneous kaolin bearing layers within the respective excavation pits. Heterogeneity between layers was defined by differences in colour, texture and mineralogy (Diko, 2012). However, in some instances the main difference was texturally driven, as in Ediki kaolin where two facies type; sand-rich and sand-poor kaolin have been identified (Diko and Ekosse, 2012). Within each distinct kaolin-bearing layer across all four deposits studied, four sub-samples were collected at variable intervals and mixed into a single homogenous sample.

2.2. EXPERIMENTAL

The IR spectra for bulk kaolin were acquired using a Perkin Elmer System 2000 FTIR spectrophotometer at a resolution of 4 [cm.sup.-1]. About 5 g of dried powdered samples were homogenized in spectrophotometric grade KBr in an agate mortar and pressed to 3 mm pellets with a hand press (Ekosse and Mulaba, 2008). In order not to distort the crystallinity of kaolinite in the samples, the mixing was set to 3 min allowing for minimal grinding as suggested by Tan (1996). Peaks were reported based on percentage transmittance to given wavelengths. Thermal analysis was conducted with a TA instrument SDT Q600 TGA-DSC analyser. Calcined [Al.sub.2][O.sub.3] served as the insert standard, while measurements were performed with 20 mg of samples, heated in air at 10 [degree]C/min, from 25 [degree]C to 1100 [degree]C as discussed in Njoya et al. (2006).

3. RESULTS AND DISCUSSION

3.1. FTIR SPECTROSCOPY

The structural order of kaolinites can be detected by differences in position and relative intensity of OH stretching and bending bands in IR spectrum (Madejova, 2003). The OH bands in kaolin typically display four sharp stretching bands between 3600 and 3700 [cm.sup.-1] namely; 3697, 3670, 3652/50 and 3620 [cm.sup.-1] (Ekosse and Mulaba, 2008; Ekosse, 2008; Saikia and Parthasarathy, 2010; Kiros et al., 2013; Djomgoue and Njopwouo, 2013). The strong band at 3697 [cm.sup.-1] arises from surface hydroxyls and produces an in-phase vibration perpendicular to the 1:1 layers (Ece et al., 2003). The two bands at 3670 [cm.sup.-1] and 3652 [cm.sup.-1] arise from stretching vibrations that are sub-parallel to the 1:1 layers whereas the low frequency 3620 [cm.sup.-1] is assigned to the fourth OH inner group. On the basis of resolution and relative intensities of the bands in the OH stretching and bending regions, Vaculikova et al. (2011) proposed the following classification schemes for kaolinite structural order:

* Ordered; if the OH stretching and bending bands are clearly resolved.

* Partially ordered; if the individual OH bands at 3670 [cm.sup.-1], 3650 [cm.sup.-1] and 938 [cm.sup.-1] had low intensities but could be identified.

* Poorly ordered; if only one band near 3660 [cm.sup.-1] or inflexions near 3670 [cm.sup.-1], 3650 [cm.sup.-1] and 938 [cm.sup.-1] were observed in the spectra.

The positions and assignments of the transmittance bands of representative samples from South Africa and Cameroon compared against that of theoretical kaolinite is summarized in Table 1. Three characteristic peaks at 3688/3687 [cm.sup.-1], 3651/3652[degree]C[degree]C cm[degree]C -1 and 3690/3692 [cm.sup.-1] were observed in ZEB 1, ZEB 2, DUT 1 and DUT 2 (Fig. 1 (a - d), a weak doublet between 3620 [cm.sup.-1] and 3700 [cm.sup.-1] was present in MK 1 and MK 2 (Fig. 2 a and b) whereas only a single clearly resolved 3619 [cm.sup.-1] peak with very weak inflexion at 3686 [cm.sup.-1] characterized ED 1 and ED 4 (Fig. 2c and d). Low frequency peaks at 3620 [cm.sup.-1] and 3619 [cm.sup.-1] were prominent in all the samples. Single broad bands at 3650/3651 [cm.sup.-1], were observed in samples ED 1 and 2, indicative of poor structural order (Saikia and Parthasarathy, 2010; Kiros et al., 2013; Djomgoue and Njopwouo, 2013). Muscovite + quartz interference was identified in all the samples whereas iron oxides were prominent in ZEB 2, DUT 1, DUT 2, MK 1 and MK 2 but absent in ED 1 and ED 2. According to Saikia and Parthasarathy (2010) broad H-O-H bands at 3450 [cm.sup.-1] and weak peaks at 1633 [cm.sup.-1] in DUT 6, DUT 13, MK 1, MK 2, ED 1 and ED4 may contribute significantly towards mass loss during calcination. The IR spectrum infers the following increasing structural order; ED 2 < ED 1< MK 2 < MK 1 < ZEB 2 < ZEB 1, with ED 2 having the least and ZEB 1 the most.

3.2. THERMAL ANALYSIS

The DSC curves show endothermic and exothermic reactions during calcination, such as desorption of surface water (H2O), dehydroxy lation (structural OH-groups) and the transformation to mullite and cristobalite, with resultant temperature effects of dehydroxylation and polymorphic transformation strongly dependent on kaolinite structural order (Ece et al., 2003; Ekosse, 2008).

Kaolin group minerals are characterised by two major endothermic peaks and one exothermic peak. The exothermic peak corresponds to the destruction of the 1:1 kaolinite structure and is typically observed between 943 [degree]C and 968 [degree]C (Ece et al., 2003; Ekosse, 2008). The dehydroxylation temperature of most kaolinites ranges from 498 [degree]C to 605 [degree]C, whereas the dehydroxylation of dickite and nacrite occurs at 680 [degree]C. According to Ece et al. (2003) and Saviano et al. (2005) well-ordered kaolinites have broad endothermic peaks at approximately 590 [degree]C however, Njoya et al. (2006) reported endothermic peaks for well-ordered kaolinites from Mayouom at 520 522 [degree]C. Conversely, major weight losses during TG experiments are typically observed between 400 and 600 [degree]C (Saviano et al., 2005).

[FIGURE 1 OMITTED]

[FIGURE 2 OMITTED]

[FIGURE 3 OMITTED]

The DSC--TG curves of DUT 1 and DUT 2, ED 1 and ED 2, and MK 1 and MK 2 were not significantly different hence only one of each has been presented. With the exception of ZEB 1 (Fig. 3), low temperature endothermic peak observed between 85 [degree]C to 110 [degrees]C was recorded in the rest of the samples (Figs. 4 - 7). A second endothermic peak observed between 295 [degree]C and 350 [degree]C in ZEB 2, DUT 1 and MK 2 (Figs. 4, 5 and 7 respectively) was attributed to dehydroxylation reactions of goethite ([alpha]-FeO.OH) resulting in the formation of hematite as represented by the equation below:
2 [alpha]-FeO.OH [right arrow] [alpha]-[Fe.sub.2][O.sub.3] +
                                       [H.sub.2]O (1)
  Goethite                             hematite


The DSC scans also portrayed samples having endothermic peaks between 500 [degree]C to 560 [degree]C, corresponding to dehydroxylation and transformation of kaolinite to metakaolinite as indicated below:
[Al.sub.2][Si.sub.2][O.sub.5][(OH).sub.4] [right arrow] [Al.sub.2]
                                          [Si.sub.2][O.sub.7] +
                                          [H.sub.2]O (2)
Kaolinite                                     metakaolinite


Exothermic temperature peaks between 930 [degree]C and 1000 [degree]C were attributed to the temperature range for mullite formation from metakaolinite (Ekosse, 2008) as per the following equation:
3[Al.sub.2][Si      [right arrow]      [Al.sub.6][Si.sub.2]
.sub.2][O.sub.7]                     [O.sub.13] + 4Si[O.sub.2] (3)

Metakaolinite                                   mullite


In addition, differential mass losses ranging from 6.5 % to 19.4 % accompanied the endothermic reactions of the studied kaolins (Figs. 3 - 7). Dehydration reactions involving loss of adsorbed water and destruction of structural OH during kaolinite dehydroxylation is considered to have accounted for the observed mass losses. The high values reported for DUT 1, DUT 2, MK 1 and MK 2 corroborates with the presence of broad H-O-H bands whereas the comparatively lower mass loss in Ediki samples (Fig. 6) is attributed to minor kaolinite content and weak H-O-H bands. The lack of symmetry displayed by the DSC curves, kaolinite dehydroxylation temperatures (500 - 650 [degree]C) together with goethite dehydroxylation reactions observed in the studied kaolins, suggests moderate degrees of crystallinity (Saviano et al., 2005). According to Ekosse (2008), oxides and other associated clay minerals (e.g mica and smectite) may equally have influenced the reaction dynamics.

[FIGURE 4 OMITTED]

In order to further assess the industrial suitability potentials, thermal stability and reaction dynamics of the studied kaolins were compared against those of selected kaolins exploited for a range of industrial applications (Table 2). The endothermic peak temperatures and main reactions of the studied kaolins were similar to those reported for Makoro and Kgwakwe kaolins (Botswana) widely employed in the manufacture of ceramics (Ekosse, 2000; 2001). In contrast, exothermic peak temperatures of the studied kaolins were lower than those for Makoro and Kgwakgwe. Compared to Mayouom kaolins, utilised for white firing ceramics and refractories (Njoya et al., 2006; Nkoumbou et al., 2009), exothermic temperatures for MK 1 and 2 were much lower whereas the rest of the samples recorded comparatively higher values (Table 2). With the exception of MK 1 and MK 2, exothermic temperatures of the studied samples were close to that of Mavaiela kaolins, used for bricks, tile and paper (Saviano et al., 2005; Ekosse, 2010). Apart from MK 1 and MK 2 with higher mass loss (14.4 - 19.4 wt. %), values for the other samples were consistent with those reported for Mayouom, Mavaiela, Makoro and Kgwakgwe kaolins (Table 2).

[FIGURE 5 OMITTED]

4. CONCLUSION

Selected kaolins from South Africa (ZEB 1, ZEB 2, DUT 1 and DUT 2) and Cameroon (MK 1, MK 2, ED 1 and ED 2) have been characterised by FTIR and simultaneous DSC - TG analyses in order to elucidate on their structural order and thermal stability. Kaolinite order was determined based on empirical analysis of the resolution and relative intensity of the OH stretching and bending vibrations of structural water. In terms of kaolinite finger prints, three characteristic peaks at 3688/3687 [cm.sup.-1], 3651/3652 [cm.sup.-1] and 3690/3692 [cm.sup.-1] were observed in the South African clays. A weak doublet between 3620 [cm.sup.-1] and 3700 [cm.sup.-1] was present in MK 1 and MK 2 whereas only a single clearly resolved peak at 3619 [cm.sup.-1], single broad band at 3650/3651 [cm.sup.-1] with very weak inflexion at 3686 [cm.sup.-1] characterized ED 1 and ED 2. Low frequency peaks at 3620 [cm.sup.-1] and 3619 [cm.sup.-1] were prominent in all the samples. Based on changes in relative intensities of OH stretching and bending vibrations the following kaolinite structural order was inferred; ED 2 < ED 1< MK 2 < MK 1 < ZEB 2 < ZEB 1, with ED 2 having the least order and ZEB 1 the most. In addition to the Al-OH functional group, the IR spectra equally inferred muscovite + quartz interference, and iron oxide enrichment in the samples. The mineralogical phases identified from IR study were found to be consistent with previously reported XRD data.

[FIGURE 6 OMTTED]

Thermal behaviour was ascertained from decomposition peak temperatures, mineralogical phase transformations and cumulative mass loss, inferred from the DSC - TG curves. The following endothermic and exothermic reactions were observed; dehydration of adsorbed water (85 - 110 [degree]C), goethite dehydroxy lation (295 - 350 [degree]C), kao linite dehydroxylation (500 - 560 [degree]C), and kaolinite recry stallization (930 - 1002 [degree]C). In addition, differential mass losses ranging from 6.5 % to 19.4 % were attributed to loss of adsorbed water and destruction of structural OH during kaolinite dehydroxylation. The characteristic kaolinite dehydroxylation temperatures (500 - 560 [degree]C), mass loss (6.5 to 19.4 %) coupled with a lack of observable symmetry from the DSC curves displayed by the studied kaolins corroborates with suggested poor to partially ordered kaolinite structures. Based on comparison of thermal behaviour against other commercial kaolins, the samples show moderate to good potentials for use in structural ceramics and refractories. However, additional technological appraisal is recommended in order to substantiate current findings.

[FIGURE 7 OMTTED]

DOI: 10.13168/AGG.2015.0052

ARTICLE INFO

Article history:

Received 31 August 2015

Accepted 11 November 2015

Available online 12 December 2015

ACKNOWLEDGEMENTS

Funding from UNESCO/IUGS/IGCP 545 Project on Clays and Clay Minerals in Africa is acknowledged.

REFERENCES

Diko, M.L. and Ekosse, G.E.: 2012, Physico-chemical and mineralogical considerations of Ediki sandstone-hosted kaolin occurrence, South West Cameroon. International Journal of Physical Science, 7, No. 3, 501-507. DOI: 10.5897/UPS1U506

Diko, M.L. and Ekosse, G.E.: 2014, Soil ingestion and associated health implications: a physicochemical and mineralogical appraisal of geophagic soils from Moko, Cameroon. Studies on Ethno-medicine, 8, No. 1, 8388.

Diko, M.L., Ekosse, G.E., Ayonghe. S.N. and Ntasin, E.: 2011, Physical characterization of clayey materials from Tertiary volcanic cones in Limbe (Cameroon) for ceramic applications. Applied Clay Science, No. 51, 380-384. D0I:10.1016/j.clay.2010.11.034

Diko, M.L.: 2012, Genesis and ceramic applications of selected kaolin occurrences from Limpopo Province, South Africa and South West Region, Cameroon. PhD thesis, University of Limpopo, South Africa, 239 pp.

Djomgoue, P. and Njopwouo, D.: 2013, FT-IR Spectroscopy applied for surface clays characterization. Journal of Surface Engineered Materials and Advanced Technology, 3, 275-282. DOI: http://dx.doi.org/10.4236/jsemat.2013.34037

Ece, O.I., Nakagawa, Z. and Schroed, P.: 2003, Alteration of volcanic rocks and genesis of kaolin deposits in the Sile region, Northern Istanbul, Turkey. Clay Mineralogy. Clays and Clay Minerals, 51, No. 6, 675688. DOI: 10.1346/CCMN.2003.0510610

Ekosse, G.E. and Mulaba, A.: 2008, Mineral thermochemistry of bentonite and kaolinite related to their possible application in the ceramic industry. Journal of Applied Sciences 8, No. 22, 4145-4151. DOI: 10.3923/jas.2008.4145.4151

Ekosse, G.E.: 2000, The Makoro kaolin deposit, southeastern Botswana: its genesis and possible industrial applications. Applied Clay Science, 16, 301-320. DOI: 10.1016/S0169-1317(99)00059-9

Ekosse, G.E.: 2001, Provenance of the Kgwakgwe kaolin deposit in southeastern Botswana and its possible utilization. Applied Clay Science, 20, 137-152. DOI:10.1016/S0169-1317(01)00064-3

Ekosse, G.E.: 2008, Thermoanalytical characterization, stable isotope and paleoenvironmental considerations of kaolinite from two genetic sources. Fresenius Environmental Bulletin, 17, No. 1, 29-42.

Ekosse, G.E.: 2010, Kaolin deposits and occurrences in Africa: Geology, mineralogy and utilization. Applied Clay Science, 50, No. 2, 212-236. DOI:10.1016/j.clay.2010.08.003

Horn, G.F. and Strydom, J.H.: 1998, Clay. In: Wilson M.G. and Anhaeusser C.R., (Eds.): The Mineral Resources of South Africa. Council for Geoscience, 16, 106-135. Kamsue, E., Leonelli, C., Boccaccini, D. N., Veronesi, P., Miselli, P., Giancarlo, P. and Chinje Melo, U.: 2007, Characterisation of porcelain compositions using two china clays from Cameroon. Ceramics International, 33, 851-857. DOI: 10.5897/IJPS12.714

Kiros, A., Gholap, A. and Gigante, G.E.: 2013, Fourier transform infrared spectroscopic characterization of clay minerals from rocks of Lalibela churches, Ethiopia. International Journal of Physical Sciences, 8, No 3, 109-119. DOI: 10.5897/IJPS12.714

Madejova, J.: 2003, FTIR techniques in clay mineral studies. Vibrational Spectroscopy, 31, 1-10. DOI: 10.1016/S0924-2031(02)00065-6

Murray, H.H.: 2007, Applied clay mineralogy. occurrences, processing and application of kaolins, bentonites, palygorskite-Sepiolite and common clays. Developments in Clay Science, No. 2, 179 pp.

Njoya, A., Nkoumbou, C., Grosbois, C., Njopwouo, D., Njoya, D., Courtin-Nomade, A., Yvon, J. and Martin, F.: 2006, Genesis of Mayouom kaolin deposit (western Cameroon). Applied Clay Science, 32, 125140. DOI: 10.1016/j.clay.2005.11.005.

Nkoumbou, C., Njoya, A., Njoya, D., Grosbois, C., Njopwouo, D., Yvon, J. and Martin, F.: 2009, Kaolin from Mayouom (Western Cameroon): Industrial suitability evaluation. Applied Clay Science, 43, 118124. DOI:10.1016/j.clay.2008.07.019

Saikia, B. and Parthasarathy, G.: 2010, Fourier Transform Infrared Spectroscopic Characterization of kaolinite from Assam and Meghalaya, Northeastern India. Journal of Modern Physics, 1, 206-210.

DOI: 10.4236/jmp.2010.14031 Saviano, G., Maurizio, V., Umberto, P. and Emidio, T.L.: 2005, Kaolin deposits from the northern sector of Cunene Anorthosite Complex (Southern Angola). Clays and Clay Minerals, 53, No. 6, 674-685. DOI: 10.1346/CCMN.2005.0530613

Tan, K.H.: 1996, Soil sampling preparation and analysis. Marcel Dekker Inc. New York,

Vaculikova, L., Plevova, E., Vallova, S. and Koutnik, I.: 2011, Characterization and differentiation of kaolinites from selected Czech deposits using infrared spectroscopy and differential thermal analysis. Acta Geodyn. Geomater., 8, No. 161, 59-67.

Makia DIKO (1) *, Georges EKOSSE (2) and Jason OGOLA (3)

(1) Geology Division, University of Limpopo, Sovenga, P/B XU06 Limpopo Province, 0727 South Africa

(2) Directorate of Research and Innovation, University of Venda, P/B X5050 Limpopo Province, 0950 South Africa

(3) Department of Mining and Environmental Geology, University of Venda, P/B X5050 Limpopo Province, 0950 South Africa

* Corresponding author's e-mail: dikom73@gmail.com
Table 1 Assignments and infrared band positions of selected kaolin
samples from South Africa, Cameroon and theoretical kaolinite.

                         Wavenumber ([cm.sup.-1])

Theoretical    ZEB 1   ZEB 2   DUT 1   DUT 2   ED 1   ED 2
kaolinite

3670 - 56      3688    3687    3692    3690    3686    --
               3650    3650    3651    3652     --     --

3645           3619    3619    3619    3624    3619   3619

                --      --     3404    3368    3410   3410
-               --      --      --      --     1397   1404

-               --     1648    1653    1649    1640   1641

1117 - 05      1113    1113    1111    1112    1113    --

1035 - 30
               1039    1023    1025    1024     --     --

1019 - 05       993     996     999     996    981    978

918 - 09        907     908     908     908    907    908

                828     --      --      --      --    828
800 - 784       795     789     793     789    796    797
                749     750             748    751

700 - 686       687     683     686     679    684    690

542 - 35        521     523     524     522    518    519

475 - 68        454     455     459     455    455    455

430             423     --      419     414    410     --
                403     403     403     --     403    402
                --      --      398     --      --    399

                Wavenumber
               ([cm.sup.-1])

Theoretical    MK 1   MK 2   Assignment
kaolinite

3670 - 56      3693   3700   Al---O-H
                --     --    stretching of inner-surface hydroxyls

                             Al---O-H
3645           3621   3624   stretching of inner hydroxyls

               3398   3411   H-O-H stretching
-               --    1417   (absorbed water)

                             H-O-H bending;
-              1642   1636   possibly smectite interference

1117 - 05       --     --    Si--O stretching

1035 - 30                    Si--O stretching;
                --     --    muscovite interference

1019 - 05      1000   979    Si--O quartz

918 - 09       909    907    OH deformation

                --     --    OH deformation
800 - 784      797    797    linked to [Al.sup.3-], [Mg.sup.2-]
               749    778

700 - 686      682    691    Si - O quartz

542 - 35       523    515    * Fe-O, [Fe.sub.2][O.sub.3]; Si--O--Al
                             stretching

475 - 68       459    450    Si--O--Si bending

430            415    422    Si--O deformation
               407    406
                --     --

Values for theoretical kaolinite (Vaculikova et al., 2011); * Fe-O,
[Fe.sub.2][O.sub.3] not present in theoretical kaolinite; (--),
very weak intensity or not detected.

Table 2 DSC-DTG endothermic and exothermic peak temperatures and
main reactions of representative samples from South Africa and
Cameroon compared against Mayouom, Mavaiela, Makoro and Kgwakgwe
kaolins.

ZEB 1    ZEB 2   DUT 1   DUT 2   ED 1   ED 2   MK 1   MK 2

                    Endothermic peaks ([degrees]C)

-         85      90      85      95     95    105    110

-         350     300     295     --     --    305     --

530       560     530     535    560    560    500    505

6.5      10.4    16.2    10.5     8     9.2    19.4   14.4

                    Exothermic peaks ([degrees]C)

1000      970     955     945    1002   930    960    980

Mayouom    Mavaiela   Makoro   Kgwakgwe   Main reaction

              Endothermic peaks ([degrees]C)

--         100-105      --       120      Dehydration of
                                          adsorbed water

--            --       350        --      Goethite
                                          dehyroxylation

520 -522   550-540     605       610      Kaolinite
                                          dehydroxylation

12-13         --      12-16      6-13     Mass loss
                                          (Wt. %)

               Exothermic peaks ([degrees]C)

980-975      1000      1000      1020     Recrystallization
                                          of kaolinite

Values for Mayououm, Mavaiela, Makoro and Kgwakgwe obtained from
Njoya et al. (2006), Saviano et al (2005); and Ekosse,
2000; 2001 respectively.
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Title Annotation:Original paper
Author:Diko, Makia; Ekosse, Georges; Ogola, Jason
Publication:Acta Geodynamica et Geromaterialia
Article Type:Report
Geographic Code:6CAME
Date:Apr 1, 2016
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