Mechanism of kaolinite dissolution at room temperature and pressure Part II: kinetic study

Huertas, F. Javier; Chou, Lei; Wollast, Roland

doi:10.1016/s0016-7037(99)00249-5

Cited by 198 publications

(111 citation statements)

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“…2, the rate of kaolinite dissolution in acetic acid was dependent upon the pH value of the solution, in the range of pH 2.5-5.5, and the logarithm of the rate of kaolinite dissolution was linearly dependent upon the solution pH. The reaction order with respect to n H + of the proton-promoted dissolution reaction is 0.28, approximately close to previous reports [2,13,15,36]. Then, the dissolution of kaolinite enhanced only by protons could be described by following equation:…”

Section: Discussionsupporting

confidence: 86%

“…The rate of kaolinite dissolution obtained in acetic acid in this paper is larger than that reported by several researchers at the same pH [2,15,21], and it relates to the larger surface of kaolinite in our experiment than that used by Wieland and Stumm [15], Huertas et al [2], and Welch and Ullman [21]. Hradil and Hostomský [30] observed that acid weathering rates of kaolinite increased with their structural disorder, and the solubility of kaolinite is related to its composition and physical properties.…”

Section: Discussioncontrasting

confidence: 65%

“…Its dissolution and precipitation are of fundamental importance for genesis and degradation of the soils and the maintenance of soils fertility [2].…”

Section: Introductionmentioning

confidence: 99%

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Dissolution of kaolinite induced by citric, oxalic, and malic acids

Wang

Hu³

et al. 2005

Journal of Colloid and Interface Science

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Section: Discussionsupporting

confidence: 86%

Section: Discussioncontrasting

confidence: 65%

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Dissolution of kaolinite induced by citric, oxalic, and malic acids

Wang

Hu³

et al. 2005

Journal of Colloid and Interface Science

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“…The reactivity of 123 6 smectite surfaces has already been investigated using AFM techniques (e.g., Metz et al 124 2005). It was shown that basal plane dissolution may contribute to phyllosilicate bulk 125 dissolution rates (Blum, 1994;Huertas et al, 1999;Cama et al, 2002;Brandt et al, 2003; 126 Ganor et al, 2003), but the dissolution process is dominated by the chemical attack on edge 127 sites (Metz et al 2005). 128…”

mentioning

confidence: 99%

Towards a link between the energetic heterogeneities of the edge faces of smectites and their stability in the context of metallic corrosion

Perronnet

Villièras

Jullien

et al. 2007

Geochimica et Cosmochimica Acta

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… From a geometrical point of view, it is thought that clay destabilization is mainly 36 controlled by phenomena starting at the edge faces of the particles. 37In the present work, the rates of the smectite-Fe(0) reaction at 80°C was assessed by XRD, 38 Mössbauer and CEC analyses for three smectites. The investigations show marked 39 differences in the degree of stability, which can not be explained by the crystal-chemistry 40 rules established in previous studies. Therefore, the Fe(0)-smectite interactions were studied 41 in view of textural and energetic surface quantitative analyses. The studied smectites have 42 equivalent nitrogen BET specific surface areas, equivalent argon edge surface areas and 43 slightly different basal surface areas. This similarity in particle shape indicates that the edge 44 surface area can not be accounted for when explaining the observed differences in reactivity. 45However, a correlation is obtained between smectite reactivity and the energetic 46 heterogeneity of its edge faces. This is interpreted in terms of a multiplication of the number 47 of sites on the edge faces, where the electron transfer between Fe(0) and the smectite 48 structure can occur. 49 3 50 INTRODUCTION 51 52Iron-clay reactions are of great importance in soils and in sedimentary and diagenetic 53 processes. In soils, the evolution of clay minerals is mainly controlled by oxidation-reduction 54 reactions. Kaolinite is very reactive in media under varying redox conditions, but Fe-rich 55 TOT clay minerals are even more reactive, and great changes in their properties may occur 56 (e.g. Favre et al. 2002). Low temperature, iron-rich, clayey environments are also described 57 in sedimentary verdine facies (Bailey 1988; Odin 1988; Odin 1990), in diagenetic oolitic 58 ironstones (Bhattacharyya 1983; Bhattacharyya 1986) and in sandstones (Hornibrook and 59 Longstaffe 1996;Aagaard et al. 2000; Hillier and Velde 1992;Hillier 1994). In these natural 60 systems, iron is present as iron oxides and/ or hydroxides (e.g. Odin 1988;Buatier et al. 1989; 61 Walker and Thompson 1990;Hornibrook and Longstaffe 1996), although metallic iron, 62Fe(0), has only been identified in contact with clay in extraterrestrial materials, such as CM 63 carbonaceous chondrites. In this case, when heating of the asteroid induces fusion of accreted 64 ice, cronstedtite, a Fe-rich 7Å mineral, is formed by interaction between olivine and FeNi 65 metal (Zolensky and McSween 1988;Brearley 1997;Zega and Buseck. 2003 Other possible controlling parameters, which were not analyzed in Lantenois' work, are those 95 describing the surface properties. Indeed, phyllosilicate surfaces have strong differential 96 reactivity because of the extreme anisotropy of their structure (Cases et al., 1986; Bickmore 97 et al., 2001), the irregular surface topography (e.g., kinks, edges and adatoms) and the 98 5 presence of defects (Metz et al., 2005). For example, concerning the alkaline dissolution of 99 smectites (Sato et al. 2003), it has been confirmed t...

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“…Kaolinite (Al 2 Si 2 O 5 (OH) 4 , (Grim, 1968) is commonly found in sediments and soils 48 around nuclear sites (Huertas et al, 1999), and has a simple 1:1 sheet silicate 49 structure (Bauer et al, 1998 …”

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confidence: 99%