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Review

Provenance and Paleoenvironmental Studies of Cretaceous African and South American Kaolins: Similarities and Differences

by
Olaonipekun Oyebanjo
1,2,
Nenita Bukalo
1,* and
Georges-Ivo Ekosse
1
1
Directorate of Research and Innovation, University of Venda, Thohoyandou 0950, South Africa
2
Natural History Museum, Obafemi Awolowo University, Ile-Ife 220282, Nigeria
*
Author to whom correspondence should be addressed.
Minerals 2021, 11(10), 1074; https://doi.org/10.3390/min11101074
Submission received: 17 August 2021 / Revised: 22 September 2021 / Accepted: 27 September 2021 / Published: 30 September 2021
(This article belongs to the Section Clays and Engineered Mineral Materials)
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Abstract

:
The African and South American continents are of great interest in continental drift studies. Hence, this study assesses the possible correlations in the provenance and paleoenvironment of selected Cretaceous Nigerian and Cameroonian (in Africa), and Argentine and Brazilian (in South America) kaolins through an analysis of their mineralogical and geochemical characteristics. On the basis of their mineralogical composition, the Nigerian Lakiri and Brazilian soft Capim River kaolins are predominantly characterised as pure kaolins, whereas the kaolins from Cameroon (except for Yatchika) and Argentina are mainly considered as sandy kaolins. The present study revealed that the Brazilian soft Capim River kaolin had the highest kaolinite structural order, whilst the Argentine Santa Cruz kaolin had the least. The kaolins from Nigeria, Cameroon, and Argentina were dominated by subhedral to anhedral kaolinite crystals relative to the Brazilian kaolin, which possess more euhedral kaolinite crystals. The kaolins were formed by the intense weathering of intermediate to felsic rocks under anoxic conditions, which is consistent with the structural framework of the basins. The average paleotemperatures obtained for the kaolins (except for the one from Santa Cruz) indicates that the paleoweathering took place under tropical climates.

1. Introduction

The continental drift hypothesis supported by German meteorologist and geophysicist Alfred Wegener in 1912 was revitalised in the 1960s with the emergence of the plate tectonic theory and the discovery of seafloor spreading [1]. The emergence demonstrated that the separation of continental masses with the subsequent formation of ocean basins cannot be simply considered as a hypothesis lacking geological mechanism to explain the drifting of the continents [2], but a fact [3]. During the Early Cretaceous (approximately 130 Ma), the South American plate began to drift westwards from the African plate, which allowed for the opening of the South Atlantic Ocean [4]. Complementary shapes along the margin of the continents were first recognised by Dutch scientist Ortelius in 1596 [5]. These striking similarities in their coastlines in the South Atlantic Ocean have stimulated several scientific, geological, and geochronological research to validate the fact that their similarities are more than mere coincidence [4,5,6,7,8,9,10].
Comparative quantitative tests have been made between the two continental masses with the advent of radiometric dating [11,12,13,14]. Hurley et al. [11] substantiated the geochronological evolution of the similarities between basement rocks in Liberia and Sierra Leone in West Africa and analogous rocks in Venezuela, Guyana, and Surinam in South America. This is attributed to a major episode of orogeny in the middle Precambrian called Eburnean in Africa and Transamazonian in South America, which was later corroborated by Tugarinov [15]. Furthermore, the induced granitisation processes associated with these orogenies, which led to the formation of granitic rocks of different types in both regions, were later identified as a means for pre-drift reconstruction, such as pegmatitic provinces or tin (Sn) mineralisation in both continents, despite the structural trends and geochronological line of evidence [16]. The Paraná Basin in South America and Karoo Basin in Southern Africa have been correlated on the basis of geological, paleontological, and palaeoecological studies. Extensive continental glaciations covering both parts and sedimentary sequences in the two basins have been easily correlated due to very similar faunistic and floristic assemblages [8]. Margin basins from prolific hydrocarbon provinces with oil habitats have been correlated as indicated by paleogeographic ties [17]. More than five predicted matches have been validated between West African basins from Rio Muni (in Equatorial Guinea) to Angola and their Brazilian conjugate basins from Recȏncavo to Santos, on the basis of oil geochemical family characterisation [18].
Most studies carried out to establish the pre-drift geological correlations between the two continents have been on the basis of the rock associations, tectonic links, geochronological data, mineralisation, and structural patterns, which are traceable on both continents [2,3,5,10,19,20,21,22,23,24]. None of these studies considered the use of continental argillaceous sediments, such as kaolins, in pre-drift reconstructions, despite kaolins being good paleo-climatic and paleoenvironmental indicators [25], with the exception of Petschnick et al. [26], which was limited to marine argillaceous sediments of the South Atlantic. Considering the enormous thick clay deposits, particularly kaolin deposits, occurring on both continents [27,28], it is imperative to also correlate the clay deposits on both continents. Hitherto, there has never been any formal attempt to correlate these deposits, despite South America and Africa being joined until their breakup into separate continents during the Cretaceous period. Hence, there is still much uncertainty in correlations between the two continents as far as clay and clay minerals are concerned [10,29]. Africa and South America occupy strategic places in the global tectonic understanding and have attracted geoscientific interest since the beginning of studies on continental drift [2]. Therefore, the integration of available data will allow the re-evaluation of the geological framework of the two domains and provide new insights for correlations between them. This review is a comparative study on the mineralogical and geochemical characteristics of some West African and South American kaolins vis-à-vis their provenance and the paleoenvironmental conditions under which they were formed.

2. Geologic Setting of the Selected Cretaceous Kaolin Deposits

The studied Cretaceous deposits are the Lakiri and Eruku kaolins in Nigeria, the Logbaba and Yatchika kaolins in Cameroon, the soft Capim River kaolin in Brazil, and the Santa Cruz kaolin in Argentina. Their detailed geological characteristics are described in Oyebanjo et al. [30,31] for the Nigerian kaolins; Bukalo et al. [32,33] for the Cameroonian kaolins; Santos and Rossetti [34], and Sousa et al. [35] for the Brazilian kaolin; and Dominguez et al. [36,37], and Dondi et al. [38] for the Argentine kaolin. The Cretaceous kaolin deposits from Nigeria (Lakiri and Eruku) are located within the Ise Formation (Abeokuta Group) of the Eastern Dahomey Basin (Figure 1a). The Ise Formation overlying the Basement Complex consists of continental sands, grits, and siltstones with interbeds of kaolinitic clays as high as several metres in some places [30]. Furthermore, the Logbaba Formation of the Douala Sub-basin hosts the Logbaba and Yatchika kaolin deposits from Cameroon (Figure 1b). The Logbaba Formation is composed of sandstones and clays with intercalations of sands and the rare occurrence of limestones [32]. On the South American side, the soft Capim River kaolin deposit of the Cametá Sub-basin occurs within the Ipixuna Formation (Figure 1c), which consists of strongly deferruginised, kaolinised sandstones, and intercalated kaolinitic argillites [34]. The Santa Cruz kaolin deposits in Argentina occur within the Baquero Formation belonging to the Deseado Basin (Figure 1d). The Baquero Formation is a sequence of conglomerates and sandstones covered by dark grey clay (composed of kaolinite, quartz, and expandable clay minerals) with abundant inorganic carbon [37].

3. Materials and Methods

The mineralogical and geochemical data used in this study were obtained from 12 articles (Table 1). The list of selected Cretaceous kaolins from Africa and South America, and the various methods of analyses as stated by the respective authors are shown in Table 1. The various Cretaceous deposits were selected on the basis of their proximities to the continental margins, detrital origins, and availability of data.

4. Results and Discussion

4.1. Mineralogical Considerations

4.1.1. XRD Studies

The Lakiri and soft Capim River kaolins contained greater amounts of kaolinite (averages of 99 wt% and 98 wt%, respectively) and less quartz (average of 1 wt% for both), relative to other selected kaolins from Cameroon and Argentina (Table 2). However, the Logbaba, Yatchika, and Santa Cruz kaolin deposits had other clay minerals, such as illite/illite–smectite interstratified and smectite, occurring in them. In addition, titania and iron oxide minerals were present in all the kaolins in trace-to-minor percentages (Table 2).
The mineralogical characteristics of these kaolins will affect their potential industrial uses [49]. A plot of the average percentages of minerals present in each of the deposits is shown in the ternary diagram for the general mineralogical classification of economic kaolin deposits, which categorises the deposits according to kaolin types (Figure 2). The Lakiri and soft Capim River kaolins present higher average kaolinite abundances, plotted in the region of pure kaolin, whereas other kaolins (except Yatchika) have lower average kaolinite and higher quartz contents, plotted in the region of sandy kaolins.
The Hinckley index (HI) average values of 0.98 (Eruku kaolin), 0.99 (Lakiri kaolin), and 1.11 (soft Capim River kaolin) indicate a moderate kaolinite structural order, whereas the value of 0.40 for the Santa Cruz kaolin deposits indicates a poor kaolinite structural order. From the HI averages (Table 2), kaolins can be classified, in increasing order of kaolinite structural order, as follows: Santa Cruz kaolin (with the least orderliness) < Eruku kaolin < Lakiri kaolin < soft Capim River kaolin (with the best orderliness).

4.1.2. Kaolinite Crystal Habit

The SEM images display the various crystal habits of the selected Cretaceous kaolins (Figure 3, Figure 4 and Figure 5). Figure 3 and Figure 4 show that all the studied kaolins have kaolinite crystals occurring as thin platy particles and pseudohexagonal plates (Figure 5).
In addition, the Nigerian and Cameroonian kaolins appear to have less microporosity between grains than what can be observed between grains in the Brazilian soft Capim River kaolins. This could be attributed to the coarser kaolinite with paucity of ultra-fine (<0.1 μm) particles in the matrix between the stacks in the soft Capim River kaolin. The kaolinite plates in the Nigerian, Cameroonian, and Argentine kaolins have subhedral–anhedral external forms with irregular edges, whereas the soft Capim River kaolinite crystals are euhedral with smooth edges.

4.2. Geochemical Considerations

The average SiO2 and Al2O3 contents showed variation among the kaolins as result of their kaolinite and quartz contents. The high SiO2/Al2O3 ratios for Eruku, Logbaba, Yatchika, and Santa Cruz kaolins relative to typical kaolinite (1.17) could be attributed to their higher percentages of quartz. The average TiO2 and Fe2O3 values for Nigerian and Cameroonian kaolins were higher than those obtained from Brazil and Argentina. Other oxides (MnO, MgO, CaO, Na2O, K2O, and P2O5) occur as minor constituents (Table 3).
In assessing the paleoweathering conditions, the average chemical index of alteration (CIA) value of the soft Capim River kaolin (99.75) was the highest, whereas the Yatchika (96.30) had the lowest value (Table 3). The Al2O3 − (CaO* + Na2O) − K2O (A−CN−K) ternary plot with CIA shows that the source rocks experienced intense chemical weathering under tropical climatic conditions, with all plotting in/close to the kaolinite field with high CIA values (Figure 6). The variations in the geochemical features, despite having similarly high CIA values, indicate the high maturity of the Cretaceous kaolins, with their parent rock characteristics playing a more significant role than the degree of weathering [51].
The provenance of the kaolins was predominantly from intermediate to felsic rocks on the basis of Roser and Korsch [52] discrimination diagrams (Figure 7). The higher ratios of K2O/Na2O in the kaolins further depict the dominance of K-feldspar over plagioclase feldspar (albite) in their respective source rocks (except for the soft Capim River kaolin), assuming that no post-depositional modifications had occurred. In addition, all kaolins were formed under passive continental tectonic settings (Figure 8).
In evaluating the paleoredox conditions under which the kaolins were formed, Ni/Co ratios greater than five represent suboxic and anoxic environments, whereas ratios less than five suggest oxic environments [55]. Gross [56] and Landergreen and Manhem [57] obtained V/Cr ratios of 1.1 and 0.75, respectively, for anoxic recent marine sediments to brackish-water sediments and higher values between 2 and 10 for oxic environments. The average Ni/Co ratios obtained for the Cretaceous kaolins suggests that they were deposited in anoxic environments (except for the Logbaba and Santa Cruz kaolins, which were deposited in oxic environments) (Table 3).
This is also confirmed by the V/Cr ratios, which indicated deposition in anoxic environments for all kaolins, except for the Santa Cruz kaolin, which was deposited in an oxic environment (Table 3). The observation that some of the kaolins were formed in a restricted oxygen-poor (anoxic) depositional environment is consistent with the horst-and-graben structural systems for the Eastern Dahomey Basin [58,59] in Nigeria, the Kribi-Campo Sub-basin [60] in Cameroon, and the Cametá Sub-basin [35] in Brazil.

4.3. Hydrogen and Oxygen Stable Isotopic Considerations

The average hydrogen and oxygen compositions of the selected Cretaceous kaolins from Nigeria, Cameroon, Brazil, and Argentina are presented in Table 4 and plotted in Figure 9. The average δ18O values obtained for all studied Cretaceous kaolins were within the +19 and +23‰ values for kaolinites of sedimentary origin, except for the Brazil soft Capim River kaolin that presented a value of 15.65‰, which corresponds to kaolinites from residual deposits with δ18O values between +15 and +19‰ [62] (Table 4). dos Santos et al. [48] attributed the low δ18O of the soft Capim River kaolin to mineralogical contaminations from framework grains, rather than post-formational modifications due to interactions with meteoric waters depleted in δ18O. They further concluded that the δ18O values reflect a low isotopic composition of the parent minerals, such as feldspars and micas with variable rates of replacements by kaolinites.
The Nigerian kaolins had the highest average δD values followed by the Cameroonian kaolins relative to the Brazilian soft Capim River and the Argentine kaolins. This suggests that the isotopic composition of meteoric water during the formation of the Nigerian kaolins was heavier, whereas the other kaolins might have interacted with paleometeoric waters with lesser levels of δ18O and δD [63]. Figure 9 shows that the average δ18O and δD values of the selected Cretaceous kaolins are plotted between the kaolinite line (KL) of Savin and Epstein [64] and the supergene–hypogene line (SHL) of Sheppard et al. [65], except for the Santa Cruz kaolin deposits, which are plotted to the right of the KL. The position of the Santa Cruz kaolin deposits below the KL is suggestive of post-formational modifications of the isotopic compositions of the Argentine kaolinites [66,67]. The plot of (Ba + Sr) versus (Ce + Y + La) [68] also indicates supergene kaolinisation mechanisms for the kaolins (Figure 10).
The calculated average temperatures of kaolinisation (Tc) for the selected Cretaceous kaolins using the Clauer et al. [69] and Galan et al. [70] equations are given in Table 4. The average Tc for the Nigerian and Cameroonian kaolins was lower than the values obtained for the Brazilian soft Capim River kaolin. However, the average Tc values obtained for both the Nigerian and Brazilian kaolins suggest that the kaolins were formed under warm conditions, whereas the average Tc of 21.85 °C of the Cameroonian kaolins suggests formation under cooler conditions. The low/inaccurate Tc for the Argentine kaolin could be attributed to the post-formational modifications of the isotopic compositions of the kaolinite due to their interaction with meteoric water depleted in δ18O and δD [63,67]. It is noteworthy that the Tc values below 50 °C do not relate kaolinisation with a low-temperature hydrothermal event [69]. The average paleotemperatures obtained for the Nigerian, Cameroonian, and Brazilian kaolins were characteristic of paleoweathering formation under tropical climates. Previous work by Scotese [71] concluded that the three countries had identical tropical climates during the Cretaceous Period.

5. Conclusions

Selected Cretaceous African (Lakiri and Eruku in Nigeria, and Logbaba and Yatchika in Cameroon) and South American (soft Capim River in Brazil and Santa Cruz in Argentina) kaolins were studied to determine similarities and differences in their provenance and paleoenvironment. On the basis of their mineral phases, Lakiri and soft Capim River kaolins were pure, showing moderate kaolinite structural order, unlike the other kaolins. Morphologically, kaolinite crystals in all the kaolin samples generally occurred as thin platy particles and pseudohexagonal plates, although the African kaolins contained less microporosity between their crystals. From their geochemical characteristics, all the kaolins displayed the extreme silicate weathering of intermediate to felsic rocks that are formed under passive continental tectonic settings. The Nigerian, Cameroonian, and Brazilian kaolins were formed under anoxic paleoredox conditions, whereas the Argentine kaolin was formed under oxic paleoredox conditions. However, all the kaolins were formed under supergene conditions in a tropical climate. This review shows that there are more similarities between Cretaceous African and South American kaolins than previously considered, thereby positively correlating the two continental masses.

Author Contributions

Conceptualisation, O.O., N.B. and G.-I.E.; formal analysis, O.O., N.B. and G.-I.E.; funding acquisition, G.-I.E.; investigation, O.O. and N.B.; writing–original draft preparation, O.O. and N.B.; writing–review and editing, G.-I.E.; supervision, G.-I.E. All authors have read and agreed to the published version of the manuscript.

Funding

This research was funded by the NATIONAL RESEARCH FOUNDATION (South Africa), grant number UID 91559, 2014–2016. The APC was funded by the University of Venda.

Acknowledgments

In this section, you can acknowledge any support given which is not covered by the author contribution or funding sections. This may include administrative and technical support, or donations in kind (e.g., materials used for experiments).

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 1. Generalised lithostratigraphy of (a) Eastern Dahomey Basin (modified from Olabode and Mohammed [39]), (b) Douala Sub-basin (after Anoh and Petters [40]), (c) Cameta Sub-basin (after Santos and Rossetti [34]), and (d) Deseado Basin (after Paredes et al. [41]).
Figure 1. Generalised lithostratigraphy of (a) Eastern Dahomey Basin (modified from Olabode and Mohammed [39]), (b) Douala Sub-basin (after Anoh and Petters [40]), (c) Cameta Sub-basin (after Santos and Rossetti [34]), and (d) Deseado Basin (after Paredes et al. [41]).
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Figure 2. Mineralogical classification by kaolin type for the selected Cretaceous kaolins (fields after Pruett [49]).
Figure 2. Mineralogical classification by kaolin type for the selected Cretaceous kaolins (fields after Pruett [49]).
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Figure 3. SEM micrographs of Cretaceous Eruku (a,b) and Lakiri kaolins (c,d) in Nigeria [42,44].
Figure 3. SEM micrographs of Cretaceous Eruku (a,b) and Lakiri kaolins (c,d) in Nigeria [42,44].
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Figure 4. SEM micrographs of Cretaceous Logbaba (a,b) and Yatchika kaolins (c,d) in Cameroon [45].
Figure 4. SEM micrographs of Cretaceous Logbaba (a,b) and Yatchika kaolins (c,d) in Cameroon [45].
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Figure 5. SEM micrographs of Cretaceous soft Capim River (a,b) and Santa Cruz kaolins (c–e) in Brazil [49] and Argentina [36], respectively.
Figure 5. SEM micrographs of Cretaceous soft Capim River (a,b) and Santa Cruz kaolins (c–e) in Brazil [49] and Argentina [36], respectively.
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Figure 6. A−CN−K (Al2O3 − CaO* + Na2O − K2O) ternary diagram of the selected Cretaceous kaolins combined with CIA (fields after Nesbitt and Young [53], and Hofer et al. [54]).
Figure 6. A−CN−K (Al2O3 − CaO* + Na2O − K2O) ternary diagram of the selected Cretaceous kaolins combined with CIA (fields after Nesbitt and Young [53], and Hofer et al. [54]).
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Figure 7. Discrimination diagrams for the provenance of the studied Cretaceous kaolin deposits using (a) raw major oxide concentrations—DFI = 0.445 TiO2 + 0.070 Al2O3 − 0.250 Fe2O3 − 1.142 MgO + 0.438 CaO + 1.475 Na2O + 1.426 K2O − 6.861 and DFII = − 1.773 TiO2 + 0.607 Al2O3 + 0.760 Fe2O3 − 1.500 MgO + 0.616 CaO + 0.509 Na2O − 1.224 K2O − 9.090; and (b) ratios of major oxides to Al2O3—DFI = 56.500 TiO2/Al2O3 − 10.879 Fe2O3/Al2O3 + 30.875 MgO/Al2O3 − 5.404 Na2O/Al2O3 + 11.112 K2O/Al2O3 − 3.89 and DFII = 30.638 TiO2/Al2O3 − 12.541 Fe2O3/Al2O3 + 7.329 MgO/Al2O3 + 12.031 Na2O/Al2O3 + 35.402 K2O/Al2O3 − 6.382 (fields after Roser and Korsch [52]).
Figure 7. Discrimination diagrams for the provenance of the studied Cretaceous kaolin deposits using (a) raw major oxide concentrations—DFI = 0.445 TiO2 + 0.070 Al2O3 − 0.250 Fe2O3 − 1.142 MgO + 0.438 CaO + 1.475 Na2O + 1.426 K2O − 6.861 and DFII = − 1.773 TiO2 + 0.607 Al2O3 + 0.760 Fe2O3 − 1.500 MgO + 0.616 CaO + 0.509 Na2O − 1.224 K2O − 9.090; and (b) ratios of major oxides to Al2O3—DFI = 56.500 TiO2/Al2O3 − 10.879 Fe2O3/Al2O3 + 30.875 MgO/Al2O3 − 5.404 Na2O/Al2O3 + 11.112 K2O/Al2O3 − 3.89 and DFII = 30.638 TiO2/Al2O3 − 12.541 Fe2O3/Al2O3 + 7.329 MgO/Al2O3 + 12.031 Na2O/Al2O3 + 35.402 K2O/Al2O3 − 6.382 (fields after Roser and Korsch [52]).
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Figure 8. Discrimination function diagram for sedimentary tectonic settings of the <2 μm fractions of the studied kaolin deposits (fields after Bhatia [61]). DFI = −0.0447SiO2 − 0.972TiO2 + 0.008Al2O3 − 0.267Fe2O3 + 0.208FeO − 3.082MnO + 0.140MgO + 0.195CaO + 0.719Na2O − 0.032K2O + 7.510P2O5 + 0.303 and DFII = −0.421SiO2 + 1.998TiO2 − 0.526Al2O3 − 0.551Fe2O3 − 1.610FeO + 2.720MnO + 0.881MgO − 0.907CaO − 0.177Na2O − 1.840K2O + 7.244P2O5 + 43.57.
Figure 8. Discrimination function diagram for sedimentary tectonic settings of the <2 μm fractions of the studied kaolin deposits (fields after Bhatia [61]). DFI = −0.0447SiO2 − 0.972TiO2 + 0.008Al2O3 − 0.267Fe2O3 + 0.208FeO − 3.082MnO + 0.140MgO + 0.195CaO + 0.719Na2O − 0.032K2O + 7.510P2O5 + 0.303 and DFII = −0.421SiO2 + 1.998TiO2 − 0.526Al2O3 − 0.551Fe2O3 − 1.610FeO + 2.720MnO + 0.881MgO − 0.907CaO − 0.177Na2O − 1.840K2O + 7.244P2O5 + 43.57.
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Figure 9. Average δD versus δ18O isotopic composition diagram of the selected Cretaceous kaolins.
Figure 9. Average δD versus δ18O isotopic composition diagram of the selected Cretaceous kaolins.
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Figure 10. Ba + Sr versus Ce + Y + La binary discrimination diagram of the selected Cretaceous kaolins (fields after Dill et al. [68]).
Figure 10. Ba + Sr versus Ce + Y + La binary discrimination diagram of the selected Cretaceous kaolins (fields after Dill et al. [68]).
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Table
Table 1. Selected Cretaceous kaolin deposits and summary of analytical methods used to determine their mineralogy and geochemistry.
Table 1. Selected Cretaceous kaolin deposits and summary of analytical methods used to determine their mineralogy and geochemistry.
CountryDepositsMethodsReferences
Major/Trace ElementsMineral Phases/MorphologyO/H Isotope
NigeriaLakiri ErukuXRF 1/LAICPMS 2XRD 3/SEM 4FDXPMS 5[30,42,43,44]
CameroonLogbaba
Yatchika		XRF 1/ICPMS 6XRD 3/SEM 4FDXPMS 5[45,46,47]
ArgentinaSanta CruzXRF 1/INAA 7/ICPOES 8XRD 3/SEM 4SVGID 9/SS 10[36,37]
BrazilSoft Capim RiverICPAES 11/ICPMS 7XRD 3/SEM 4FMTDMS 12/
TFTCEA 13		[35,48,49]
1 X-ray Fluorescence Spectroscopy, 2 Laser Ablation Inductively Coupled Plasma Mass Spectrometry, 3 X-ray Diffraction, 4 Scanning Electron Microscopy, 5 Finnegan DeltaXP mass spectrometry, 6 Inductively Coupled Plasma Mass Spectrometry, 7 Instrumental Neutron Activation Analysis, 8 Inductively-Coupled Plasma Optical Emission Spectrometry, 9 SIRA II-VG Isotech device, 10 SIRA II spectrometry, 11 Inductively Coupled Plasma Atomic Emission Spectroscopy, 12 a Finnigan-MAT DELTA mass spectrometry, 13 Thermo-Finnigan Thermal Conversion Elemental Analysis.
Table
Table 2. Average mineralogical compositions (wt%) of the selected Cretaceous kaolin deposits. Ka: kaolinite; Qz: quartz; I/S: illite and illite–smectite interstratified; Sm: smectite; M: mica; Fd: feldspar; Ac: titania and iron oxide minerals; HI: Hinckley index.
Table 2. Average mineralogical compositions (wt%) of the selected Cretaceous kaolin deposits. Ka: kaolinite; Qz: quartz; I/S: illite and illite–smectite interstratified; Sm: smectite; M: mica; Fd: feldspar; Ac: titania and iron oxide minerals; HI: Hinckley index.
CountryDepositKaQzI/SSmMFdAcHI
NigeriaLakiri 1991----trace0.99 a
Eruku 17816--4-20.98 a
CameroonLogbaba 2484125--4-
Yatchika 24234514--5-
ArgentinaSanta Cruz 3503564-230.40
BrazilSoft Capim River 4981----11.11 b
1 Oyebanjo et al. [44]; 2 Bukalo et al. [47]; 3 Dominguez et al. [36]; 4 Pruett [49]; a Oyebanjo et al. [30]; b dos Santos et al. [50]. (-): Not detected.
Table
Table 3. Average concentrations of major element oxides (wt%), CIA, and trace elemental ratios of the selected Cretaceous kaolin deposits.
Table 3. Average concentrations of major element oxides (wt%), CIA, and trace elemental ratios of the selected Cretaceous kaolin deposits.
NigeriaCameroonArgentinaBrazil
Lakiri 1Eruku 1Logbaba 2Yatchika 2Santa Cruz 3Soft Capim River 4
SiO249.6456.8261.3851.6664.3544.3
TiO21.602.102.351.700.550.44
Al2O335.5528.2529.6528.2122.5139.35
Fe2O31.092.561.047.750.990.66
CaO0.020.020.040.030.25<0.02
MgO-0.040.080.700.240.04
MnO0.010.01--0.01-
Na2O0.020.020.020.060.09<0.06
K2O0.410.200.180.990.690.02
P2O50.060.110.180.120.03<0.09
LOI12.5710.004.769.0210.1114.15
CIA99.2298.3899.1896.3096.8599.75
SiO2/Al2O31.402.012.071.832.861.13
K2O/Na2O20.5010.009.0016.507.67-
V/Cr1.040.960.901.382.971.04
Ni/Co7.885.522.957.211.978.37
1 Oyebanjo [42], 2 Bukalo et al. [47], 3 Dominguez et al. [36], 4 dos Santos et al. [50]. (-): Not detected.
Table
Table 4. Average δ18O and δD values (in ‰) and calculated temperature of kaolinisation (in °C) for the selected Cretaceous kaolins.
Table 4. Average δ18O and δD values (in ‰) and calculated temperature of kaolinisation (in °C) for the selected Cretaceous kaolins.
CountryDepositδ18OδDTemperature
NigeriaEruku 119.2−5331.2
Lakiri 119.7−5229.9
CameroonLogbaba 220.2−6420.82
Yatchika 219.4−6622.88
ArgentinaSanta Cruz 319.6−1034.87
Brazilsoft Capim River 415.7−6938.4
1 Oyebanjo et al. [43]; 2 Bukalo et al. [46]; 3 Dominguez et al. [37]; 4 dos Santos et al. [48].
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Oyebanjo, O.; Bukalo, N.; Ekosse, G.-I. Provenance and Paleoenvironmental Studies of Cretaceous African and South American Kaolins: Similarities and Differences. Minerals 2021, 11, 1074. https://doi.org/10.3390/min11101074

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Oyebanjo O, Bukalo N, Ekosse G-I. Provenance and Paleoenvironmental Studies of Cretaceous African and South American Kaolins: Similarities and Differences. Minerals. 2021; 11(10):1074. https://doi.org/10.3390/min11101074

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Oyebanjo, Olaonipekun, Nenita Bukalo, and Georges-Ivo Ekosse. 2021. "Provenance and Paleoenvironmental Studies of Cretaceous African and South American Kaolins: Similarities and Differences" Minerals 11, no. 10: 1074. https://doi.org/10.3390/min11101074

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