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The minerals of the kröhnkite supergroup: structural relations and chemical compositions

Published online by Cambridge University Press:  21 January 2025

Frank C. Hawthorne Open the ORCID record for Frank C. Hawthorne [Opens in a new window]
Frank C. Hawthorne*
Affiliation:
Department of Earth Sciences, University of Manitoba, Winnipeg, MB, Canada
*
Email: frank.hawthorne@umanitoba.ca
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Abstract

The minerals of the kröhnkite, talmessite and fairfieldite groups plus dondoellite, general formula X2M2+(TO4)2(H2O)2 where X = Na, Ca; M2+ = Mg, Fe, Mn, Co, Ni, Zn, Cu; and T = S, P, As; have been consolidated into the IMA-approved kröhnkite supergroup. The cell dimensions and space-group symmetries of the minerals in these three groups and dondoellite are distinct but the structures of these minerals are strongly related as they have topologically identical structural units. Differences in structure between the different groups involve the disposition of adjacent [M2+(TO4)2(H2O)2] chains and the stereochemical details of the hydrogen bonds that link adjacent [M2+(TO4)2(H2O)2] chains. The ions that form the interstitial complex of a mineral and the structural unit must satisfy the principle of correspondence of Lewis acidity–basicity whereby stable structures will form where the Lewis acidity of the structural unit closely matches the Lewis basicity of the interstitial complex. For pentavalent T cations (P5+or As5+), the Lewis acidity of Ca2+ shows the closest match of all cations to the Lewis basicity of the structural unit. For hexavalent T cations (S6+), the Lewis acidity of Na+ shows the closest match of all cations to the Lewis basicity of the structural unit.

Keywords

kröhnkite supergroupkröhnkitetalmessite and fairfieldite groupsstructural relationsLewis acidity–basicitychemical composition

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Mineralogical Magazine , First View , pp. 1 - 5
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This is an Open Access article, distributed under the terms of the Creative Commons Attribution licence (http://creativecommons.org/licenses/by/4.0), which permits unrestricted re-use, distribution and reproduction, provided the original article is properly cited.
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© The Author(s), 2025. Published by Cambridge University Press on behalf of The Mineralogical Society of the United Kingdom and Ireland.

Introduction

A mineral supergroup consists of two or more groups that have essentially the same structure and are composed of chemically similar elements (Mills et al., Reference Mills, Hatert, Nickel and Ferraris2009). The minerals of the kröhnkite, talmessite and fairfieldite groups have the general formula

\begin{equation*}{{\text{X}}_{\text{2}}}{{\text{M}}^{{\text{2+}}}}{( {{\text{T}}{{\text{O}}_{\text{4}}}} )_{\text{2}}}{( {{{\text{H}}_{\text{2}}}{\text{O}}})_{\text{2}}}\end{equation*}

where X = Na or Ca; M2+ = Mg, Fe, Mn, Co, Ni, Zn or Cu; and T = S, P or As. There are currently 17 IMA-approved minerals in these three groups (Table 1) plus a single mineral, dondoellite, with a structure different from but related to the structures of the minerals of these three groups. The Commission on New Minerals, Nomenclature and Classification of the International Mineralogical Association (IMA–CNMNC) has approved the creation of the kröhnkite supergroup (Bosi et al., Reference Bosi, Hatert, Pasero and Mills2024). The details of the minerals in the supergroup and their division into three groups are shown in Fig. 1. The currently named kröhnkite, talmessite and fairfieldite groups are retained, and belong to the kröhnkite supergroup. Dondoellite is an isolated structure within the kröhnkite supergroup but cannot form a group until an isotypic mineral is approved whereupon a new group can be proposed.

Figure 1. The classification of the minerals of the kröhnkite supergroup.

Table 1. Minerals of the kröhnkite supergroup

* Dondoellite falls within the kröhnkite supergroup but not within the kröhnkite, talmessite and fairfieldite groups; it does not (as yet) have any isostructural minerals and hence cannot form a group, but it is likely that this will happen in due course.

Structure

All minerals in the kröhnkite supergroup are either monoclinic or triclinic. The cell dimensions and associated space-group symmetries of the minerals in these three groups and dondoellite are distinct (Table 2), but the structures of these minerals are strongly related as they have topologically identical structural units (Lima-de-Faria et al., Reference Lima-de-Faria, Hellner, Liebau, Makovicky and Parthé1990) that define the c-dimension of each group (Fig. 2). The structural unit is an [M(TO4)2Φ2] chain (Hawthorne, Reference Hawthorne1985) as shown idealised in Fig. 2a and as in the structure of brandtite in Fig. 2b. As noted by Hawthorne (Reference Hawthorne1983), the linkage between polyhedra in Fig. 2 maximises the accord with the valence-sum rule (Brown, Reference Brown2016; Hawthorne, Reference Hawthorne2012, Reference Hawthorne2015) for linkage of isolated octahedra and isolated tetrahedra into a chain without octahedron–octahedron or tetrahedron–tetrahedron linkages.

Figure 2. The [M(TO4)2Φ2] chain (Φ = unspecified anion) that forms the structural unit in the minerals of the kröhnkite supergroup; (a) the generalized chain (modified from Hawthorne, Reference Hawthorne1985); and (b) the [Mn2+(PO4)2(H2O)2] chain in brandtite. Drawn using ATOMS V6.4 (Dowty, Reference Dowty2016).

Table 2. Crystallographic properties of kröhnkite, brandtite, collinsite, fairfieldite and dondoellite

* References: (1) Hawthorne and Ferguson (Reference Hawthorne and Ferguson1975); (2) Herwig and Hawthorne (Reference Herwig and Hawthorne2006); (3) Catti et al. (Reference Catti, Ferraris and Ivaldi1977); (4) Yang et al. (Reference Yang, Gibbs, Mcglasson, Jenkins and Downs2022).

Differences in structure between the different groups involve the disposition of adjacent [M2+(TO4)2(H2O)2] chains and the details of the hydrogen bonds that link adjacent [M2+(TO4)2(H2O)2] chains. As indicated by the red arrows in Fig. 3, in the structures of the kröhnkite-group minerals (Fig. 3a), the octahedra of the structural units point alternately northeast and northwest in adjacent chains; in the structures of the talmessite-group minerals (Fig. 3b), the octahedra of the structural units point southwest in adjacent chains; in the structures of the fairfieldite-group minerals (Fig. 3c), the octahedra of the structural units point northeast in adjacent chains; and in the structure of dondoellite (Fig. 3d), the octahedra of the structural units point southwest in adjacent chains.

Figure 3. The crystal structures of (a) brandtite; (b) collinsite; (c) fairfieldite; and (d) dondoellite, projected onto (100). M octahedra are yellow, T tetrahedra are green, and H are small red circles; solid black lines: Odonor–H bonds; red dotted lines: hydrogen bonds; small blue circles: Oacceptor anions. The red arrows show the relative attitude of octahedra in adjacent chains. Drawn using ATOMS V6.4 (Dowty, Reference Dowty2016).

In the structures of the minerals of all groups, one H atom of the (H2O) group hydrogen-bonds to a (TO4) oxygen of the same chain and the other H atom of the (H2O) group hydrogen-bonds to a (TO4) oxygen of an adjacent chain. As indicated in Fig. 3a, in the kröhnkite-group structures, only two chains are involved in this mutual linkage of opposing (H2O) groups. In the collinsite-group structures, the fairfieldite-group structures, and in dondoellite, four chains are involved in this mutual linkage of opposing (H2O) groups (Fig. 3b,c,d).

There is no apparent sorting of structure type by cation radii and there are several compositions that occur as polymorphs that belong to different groups: brandtite–parabrandtite–fairfieldite; roselite–roselite-β; wendwilsonite–talmessite; zincroselite–gaitite; and messelite–dondoellite.

The bond-valence tables for kröhnkite and brandtite are shown in Tables 3 and 4, respectively. The bond topology of the two structures is the same and hence they have a similar pattern of bond valences. The coordination numbers of the anions, omitting the hydrogen bonds, is the same: O(1) = [3], O(2) = [4], O(3) = [2], O(4) = [3], OW = [2], and an unusual feature of each structure is the fact that the OW (H2O) group has significant incident bond-valence: 0.667 and 0.660 valence units (vu) and hence the associated hydrogen bonds are stronger than usual for bonded (H2O) groups in minerals. These strong hydrogen bonds compensate for the variation in coordination number of the anions and ensure that the valence-matching principle is satisfied (Tables 3 and 4). The incident bond-valence at the OW (H2O) group is the same in both kröhnkite and brandtite (∼0.67 vu) and yet the oxidation states of the coordinating cations are 1+ and 2+ in kröhnkite and 2+ and 2+ in brandtite; how can the same incident bond-valence be maintained in these two minerals? The key to this issue is the fact that the divalent cation in kröhnkite is Cu2+. Octahedrally coordinated Cu2+ is Jahn-Teller active (Burns and Hawthorne, Reference Burns and Hawthorne1996) and typically shows four short meridional bonds and two long apical bonds (Eby and Hawthorne, Reference Eby and Hawthorne1993; Gagné and Hawthorne, Reference Gagné and F.C2020). This is the case in kröhnkite. As the OW (H2O) group in kröhnkite is a meridional anion, it has a very strong bond incident from Cu2+ which compensates for the weaker Na–OW bond in kröhnkite (Table 3) compared to the stronger Ca–OW bond in brandtite (Table 4). This accounts for the absence of mineral compositions with the general formula Na2[6]M2+(SO4)2(H2O)2 other than kröhnkite with M2+ = Cu2+.

Table 3. Bond-valence (vu) table * for kröhnkite**

* Bond-valence curves from Gagné and Hawthorne (Reference Gagné and F.C2015);

** O(1) and O(3) have been interchanged to make the site labels consistent in kröhnkite and brandtite.

Table 4. Bond-valence (vu) table * for brandtite

* Bond-valence curves from Gagné and Hawthorne (Reference Gagné and F.C2015).

Controls on chemical composition in kröhnkite-supergroup structures

The general formula for the kröhnkite-supergroup minerals is X2M2+(TO4)2(H2O)2. What ions are possible in this topological structure-type at the various sites in the structure? Inspection of Table 1 shows that X = Na+ or Ca2+; M2+ = Mg, Fe, Mn, Co, Ni, Zn or Cu; and T = S6+, P5+ and As5+. What other ions can feasibly enter a crystal structure with the kröhnkite bond topology? In regard to this question, there has been considerable work on synthetic analogues of these minerals (e.g. Fleck et al., Reference Fleck, Kolitsch and Hertweck2002; Fleck and Kolitsch, Reference Fleck and Kolitsch2003; Kolitsch and Fleck, Reference Kolitsch and Fleck2005, Reference Kolitsch and Fleck2006; Wildner and Stoilova, Reference Wildner and Stoilova2003) as they show potential for industrial applications.

To approach this question, we use binary representation (Schindler and Hawthorne, Reference Schindler and Hawthorne2001; Hawthorne and Schindler, Reference Hawthorne and Schindler2008) whereby a structure is divided into a structural unit and an interstitial complex. The ions that form the interstitial complex of a mineral and the structural unit must satisfy the principle of correspondence of Lewis acidity–basicity (Hawthorne, Reference Hawthorne2012, Reference Hawthorne2015; Hawthorne and Schindler, Reference Hawthorne and Schindler2008), a mean-field version of the valence-matching principle (Brown, Reference Brown, O’Keeffe and Navrotsky1981; Hawthorne, Reference Hawthorne1994) whereby stable structures will form when the Lewis acid strength of the cation closely matches the Lewis base strength of the anion. Thus an ion may enter a structure with the kröhnkite bond topology if the resultant structure accords with the principle of correspondence of Lewis acidity–basicity.

The structural unit with the kröhnkite bond topology may be written as follows:

\begin{equation*}[^\text{[6]}{\text{M}{^\text{2+}}(^\text{[4]}\text{T}{^\textit{n}{^\textrm{+}}}\text{O}_\text{4})_\text{2}({^\text{[2]}{\text{H}_\text{2}\text{O})_{\text{2}}}}]}\end{equation*}

The number of bonds in the structural unit = 1 × [6] + 2 × [4] + 4 × [2] = 22. Note that although two of the hydrogen bonds exit the structural unit, they bond to anions in adjacent structural units and the two exident hydrogen-bonds are balanced by the two incident hydrogen-bonds from adjacent structural units. The number of bonds needed for [4]-coordination of all simple anions and [3]-coordination of (H2O) = 8 × [4] × 2 × [3] = 38. The number of additional bonds to the structural unit to achieve this coordination = 38 – 22 = 16 and hence the structural unit needs 16 bonds from the interstitial complex.

The charge on the structural unit [[6]M2+([4]Tn+O4)2([2]H2O)2] = 2+ + 2 × n + + 4 × 1+ – 2– × 10 = 6 + 2n – 20 = 2n – 14. The Lewis basicity of the structural unit = charge/bonds = (2n – 14)/14 vu.

For n = 5+ (P5+, As5+), the Lewis basicity of the structural unit = 4/16 = 0.250 vu. The Lewis basicity of Ca2+ = 0.264 vu (Gagné and Hawthorne, Reference Gagné and F.C2017) is the closest match with the Lewis basicity of the structural unit containing pentavalent cations. The Lewis basicity of Pb2+ = 0.266 vu but no Pb-bearing species occur; this may be a steric effect due to the large size of [8]Pb2+ (2.697 Å) compared to that of [8]Ca2+ (2.498 Å) (values from Hawthorne and Gagné, Reference Hawthorne and O.C2024).

For n = 6+ (S6+), the Lewis basicity of the structural unit = 2/16 = 0.125 vu. The Lewis basicity of Na+ is 0.159 vu but the coordination of Na+ in kröhnkite is [7] (Table 3) which reduces the effective Lewis acidity to 1/7 = 0.143 vu. The Lewis basicity of K+ is 0.108 vu (Gagné and Hawthorne, Reference Gagné and F.C2017). K-bearing kröhnkite-supergroup minerals have not been found but K-bearing synthetics have been synthesised with a view to their use in alkali-metal batteries (e.g. Barpanda et al., Reference Barpanda, Oyama, Ling and Yamada2014; Marinova et al., Reference Marinova, Kostov, Nikolova, Kukeva, Zhecheva, Sendova-Vasileva and Stoyanova2015; Watcharatharapong et al., Reference Watcharatharapong, Thienprasert, Barpanda, Ahuja and Chakraborty2017) and various possible optical applications (e.g. de Oliveira Neto et al., Reference de Oliveira Neto, Lang, Rodrigues, Gutiérrez, Murillo, de Sousa, Filho and dos Santos2022).

Acknowledgements

I thank Aaron Lussier and two anonymous reviewers for their comments on this paper.

Financial statement

This work was supported by a Discovery Grant from the Natural Sciences and Engineering Research Council of Canada.

Competing interests

The author declares none.

Footnotes

Associate Editor: Anthony R. Kampf

This paper is part of a collection in tribute to the work of Edward Grew at 80

References

Barpanda, P., Oyama, G., Ling, C.D. and Yamada, A (2014) Krohnkite-type Na2Fe(SO4)2.2H2O as a novel 3.25 V insertion compound for Na-ion batteries. Chemistry of Materials, 26, 1297–1299.Google Scholar
Bosi, F., Hatert, F., Pasero, M. and Mills, S.J. (2024) IMA Commission on New Minerals, Nomenclature and Classification (CNMNC) – Newsletter 80. European Journal of Mineralogy, 36, 599–604.Google Scholar
Brotherton, P.D., Maslen, E.N., Pryce, M.W. and White, A.H. (1974) Crystal structure of collinsite. Australian Journal of Chemistry, 27, 653–656.Google Scholar
Brown, I.D. (1981) The bond-valence method: an empirical approach to chemical structure and Bonding. pp. 1–30 in: Structure and Bonding in Crystals II (O’Keeffe, M. and Navrotsky, A., editors). Academic Press, New York.Google Scholar
Brown, I.D. (2016) The Chemical Bond in Inorganic Chemistry: The Bond Valence Model. Oxford University Press, UK.Google Scholar
Burns, P.C. and Hawthorne, F.C. (1996) Static and dynamic Jahn-Teller effects in Cu2+-oxysalt minerals. The Canadian Mineralogist, 34, 1089–1105.Google Scholar
Catti, M., Ferraris, G. and Ivaldi, G. (1977) Hydrogen bonding in the crystalline state. Structure of talmessite, Ca2(Mg,Co)(AsO4)2∙2(H2O), and the crystal chemistry of related minerals. Bulletin de la Société Française de Minéralogie et de Crystallographie, 100, 230–236.Google Scholar
Chukanov, N.V., Mukhanova, A.A., Möckel, S., Belakovsky, D.I. and Levitskaya, L.A. (2020) Nickeltalmessite, Ca2Ni(AsO4)2·2H2O, a new mineral species of the fairfieldite group, Bou Azzer, Morocco. Geology of Ore Deposits, 52, 606–611.Google Scholar
Dahlman, B. (1951) The crystal structures of kröhnkite, CuNa2(SO4)2·2H2O and brandtite, MnCa2(AsO4)2·2H2O. Arkiv för Mineralogi och Geologi, 1, 339–366.Google Scholar
de Oliveira Neto, J.G., Lang, R., Rodrigues, J.A.O., Gutiérrez, C.E.O., Murillo, M.A.R., de Sousa, F.F., Filho, J.G.S. and dos Santos, A.O. (2022) Kröhnkite-type K2Mn(SO4)2(H2O)2 double salt: synthesis, structure, and properties. Journal of Materials Science, 57, 8195–8210.Google Scholar
Dowty, E. (2016) ATOMS (Version 6.5.0). Shape Software, Kingsport, Tennessee, USA.Google Scholar
Dunn, P.J., Sturman, D.B. and Nelen, J.A. (1987) Wendwilsonite, the Mg analoge of roselite, from Morocco, New Jersey, and Mexico, and new data on roselite. American Mineralogist, 72, 217–221.Google Scholar
Eby, R.K. and Hawthorne, F.C. (1993) Structural relations in copper oxysalt minerals. I. Structural hierarchy. Acta Crystallographica, B49, 28–56.Google Scholar
Fanfani, L., Nunzi, A. and Zanazzi, P.F. (1970) The crystal structure of fairfieldite. Acta Crystallographica, B26, 640–645.Google Scholar
Fleck, M. and Kolitsch, U. (2003) Natural and synthetic compounds with kroehnkite-type chains. An update. Zeitschrift für Kristallographie, 218, 553–567.Google Scholar
Fleck, M., Kolitsch, U. and Hertweck, B. (2002) Natural and synthetic compounds with kröhnkite-type chains: an update. Zeitschrift für Kristallographie, 217, 435–443.Google Scholar
Frondel, C. (1955) Neomesselite and beta-roselite: two new members of the fairfieldite group. American Mineralogist, 40, 828–833.Google Scholar
Gagné, O.C. and F.C, Hawthorne. (2015) Comprehensive derivation of bond-valence parameters for ion pairs involving oxygen. Acta Crystallographica, B71, 562–578.Google Scholar
Gagné, O.C. and F.C, Hawthorne. (2017) Empirical Lewis-acid strengths for 135 cations bonded to oxygen. Acta Crystallographica, B73, 956–961.Google Scholar
Gagné, O.C. and F.C, Hawthorne. (2020) Bond-length distributions for ions bonded to oxygen: Results for the transition metals and quantification of the factors underlying bond-length variation in inorganic solids. IUCrJ, 7, 581–629.Google Scholar
Hawthorne, F.C. (1983) Graphical enumeration of polyhedral clusters. Acta Crystallographica, A39, 724–736.Google Scholar
Hawthorne, F.C. (1985) Towards a structural classification of minerals: The VIMIVT2φn minerals. American Mineralogist, 70, 455–473.Google Scholar
Hawthorne, F.C. (1994) Structural aspects of oxides and oxysalt crystals. Acta Crystallographica, B50, 481–510.Google Scholar
Hawthorne, F.C. (2012) A bond-topological approach to theoretical mineralogy: crystal structure, chemical composition and chemical reactions. Physics and Chemistry of Minerals, 39, 841–874.Google Scholar
Hawthorne, F.C. (2015) Toward theoretical mineralogy: a bond-topological approach. American Mineralogist, 100, 696–713.Google Scholar
Hawthorne, F.C. and Ferguson, R.B. (1975) Refinement of the crystal structure of kröhnkite. Acta Crystallographica, B31, 1753–1755.Google Scholar
Hawthorne, F.C. and Ferguson, R.B. (1977) The crystal structure of roselite. The Canadian Mineralogist, 15, 36–42.Google Scholar
Hawthorne, F.C. and O.C, Gagné. (2024) New ion radii for oxides and oxysalts, fluorides, chlorides and nitrides. Acta Crystallographica, B80, 326–339.Google Scholar
Hawthorne, F.C. and Schindler, M. (2008) Understanding the weakly bonded constituents in oxysalt minerals. Zeitschrift für Kristallographie, 223, 41–68.Google Scholar
Herwig, S. and Hawthorne, F.C. (2006) The topology of hydrogen bonding in minerals of the brandtite, collinsite and fairfieldite groups. The Canadian Mineralogist, 44, 1181–1196.Google Scholar
Keller, P., Lissner, F. and Schleid, T. (2004) The crystal structures of zincroselite and gaitite: Two natural polymorphs of Ca2Zn[AsO4]2·2H2O from Tsumeb, Namibia. European Journal of Mineralogy, 16, 353–359.Google Scholar
Kolitsch, U. and Fleck, M. (2005) Second update on compounds with kröhnkite-type chains. Zeitschrift für Kristallographie, 220, 31–41.Google Scholar
Kolitsch, U. and Fleck, M. (2006) Third update on compounds with kröhnkite-type chains: the crystal structure of wendwilsonite [Ca2Mg(AsO4)2·2H2O] and the new triclinic structure types of synthetic AgSc(CrO4)2·2H2O and M2Cu(Cr2O7)2·2H2O (M = Rb, Cs). European Journal of Mineralogy, 18, 471–482.Google Scholar
Lima-de-Faria, J., Hellner, E., Liebau, F., Makovicky, E. and Parthé, E. (1990) Nomenclature of Inorganic Structure Types. Report of the International Union of Crystallography Commission on Crystallographic Nomenclature Subcommittee on the Nomenclature of Inorganic Structure Types. Acta Crystallographica, A46, 1–11.Google Scholar
Marinova, D., Kostov, V., Nikolova, R., Kukeva, R., Zhecheva, E., Sendova-Vasileva, M., Stoyanova, R. (2015) From kröhnkite- to alluaudite-type of structure: novel method of synthesis of sodium manganese sulfates with electrochemical properties in alkali-metal ion batteries. Journal of Materials Chemistry, 3A, 22287–22299.Google Scholar
Mills, S.J., Hatert, F., Nickel, E H. and Ferraris, G. (2009) The standardisation of mineral group hierarchies: application to recent nomenclature proposals. European Journal of Mineralogy, 21, 1073–1080.Google Scholar
Schindler, M. and Hawthorne, F.C. (2001) A bond-valence approach to the structure, chemistry and paragenesis of hydroxy-hydrated oxysalt minerals: I. Theory. The Canadian Mineralogist, 39, 1225–1242.Google Scholar
Sejkora, J., Števko, M., Škoda, R., Víšková, E., Toman, J., Hreus, S., Plášil, J. and Dolníček, Z. (2021) Dobšináite, Ca2Ca(AsO4)2·2H2O, a new member of the roselite group from Dobšiná (Slovak Republic). Journal of Geosciences, 66, 127–135.Google Scholar
Watcharatharapong, T., Thienprasert, J., Barpanda, P., Ahuja, R. and Chakraborty, S. (2017) Mechanistic study of Na-ion diffusion and small polaron formation in kröhnkite Na2Fe(SO4)2.2H2O based cathode materials. Journal of Materials Chemistry, A5, 21726–21739.Google Scholar
White, J.S. Jr., Henderson, E.P. and Mason, B. (1967) Secondary minerals produced by weathering of the Wolf Creek meteorite. American Mineralogist, 52, 1190–1197.Google Scholar
Wildner, M. and Stoilova, D. (2003) Crystal structures and crystal chemical relationships of kröhnkite- and collinsite-type compounds Na2Me 2+(XO4)2.2H2O (X = S, Me = Mn, Cd; and X = Se, Me = Mn, Co, Ni, Zn, Cd) and K2Co(SeO4)2.2H2O. Zeitschrift für Kristallographie, 218, 201–209.Google Scholar
Yakubovich, O.V., Massa, W., Liferovich, R.P., Gavrilenko, P.G., Bogdanova, A.N. and Tuisku, P. (2003) Hillite, a new member of the fairfieldite group: its description and crystal structure. The Canadian Mineralogist, 41, 981–988.Google Scholar
Yang, H., Jenkins, R.A., Downs, R.T. and Evans, S.H. (2011) Rruffite, Ca2Cu(AsO4)2·2H2O, a new member of the roselite group, from Tierra Amarilla, Chile. The Canadian Mineralogist, 49, 877–884.Google Scholar
Yang, H., Gibbs, R.B., Mcglasson, J.A., Jenkins, R.A. and Downs, R.T. (2022) Dondoellite, Ca2Fe(PO4)2.2H2O, a new mineral species polymorphic with messelite, from Rapid Creek, Yukon, Canada. The Canadian Mineralogist, 60, 837–847.Google Scholar
Figure 0

Figure 1. The classification of the minerals of the kröhnkite supergroup.

Figure 1

Table 1. Minerals of the kröhnkite supergroup

Figure 2

Figure 2. The [M(TO4)2Φ2] chain (Φ = unspecified anion) that forms the structural unit in the minerals of the kröhnkite supergroup; (a) the generalized chain (modified from Hawthorne, 1985); and (b) the [Mn2+(PO4)2(H2O)2] chain in brandtite. Drawn using ATOMS V6.4 (Dowty, 2016).

Figure 3

Table 2. Crystallographic properties of kröhnkite, brandtite, collinsite, fairfieldite and dondoellite

Figure 4

Figure 3. The crystal structures of (a) brandtite; (b) collinsite; (c) fairfieldite; and (d) dondoellite, projected onto (100). M octahedra are yellow, T tetrahedra are green, and H are small red circles; solid black lines: Odonor–H bonds; red dotted lines: hydrogen bonds; small blue circles: Oacceptor anions. The red arrows show the relative attitude of octahedra in adjacent chains. Drawn using ATOMS V6.4 (Dowty, 2016).

Figure 5

Table 3. Bond-valence (vu) table * for kröhnkite**

Figure 6

Table 4. Bond-valence (vu) table * for brandtite