Introduction

Deynekoite, Ca₉□Fe³⁺(PO₄)₇ (R3c, a = 10.3516(3) Å, c = 37.1599(17) Å, V = 3448.4(3) ų and Z = 6), a new mineral isostructural with merrillite, was found in the phosphide-bearing contact facies of diopside–anorthite–tridymite paralava of the Hatrurim Complex in Jordan. According to the cerite supergroup classification, deynekoite belongs to the merrillite subgroup. Together, the merrillite subgroup and the whitlockite subgroup form the merrillite group (Table 1; Atencio and Azzi, Reference Atencio and Azzi2020). The general formula of minerals of the merrillite group can be presented as follows: (A1₃A2₃A3₃)_Σ9XM(P1O₄)₃ (P2O₃Ø)₃(P3O3Ø), where A = Ca, Sr and Na; X = Na, Ca and vacancy (□); M = Mg, Fe^2+,3+ and Mn²⁺; P = P; Ø = O and OH. Deynekoite is the first mineral of the merrillite group whose composition includes Fe³⁺; it has a synthetic analogue (Lazoryak et al., Reference Lazoryak, Morozov, Belik, Khasanov and Shekhtman1996; Benarafaa et al., Reference Benarafaa, Kacimia, Gharbagea, Millet and Ziyada2000; Deyneko et al., Reference Deyneko, Aksenov, Morozov, Stefanovich, Dimitrova, Barishnikova and Lazoryak2014).

Table 1.

Minerals of the merrillite group.

* Hedegaardite was approved by the CNMNC-IMA in 2015, however a paper describing the mineral has not been published yet, so the most probable cation distribution among different sites is shown.

Minerals of the merrillite group (merrillite, Ca₉NaMg(PO₄)₇, keplerite, Ca₉(Ca_0.5□_0.5)Mg(PO₄)₇, and the potentially new mineral Ca₈Y□Mg(PO₄)₇, forming a solid solution) were found recently in hematite-bearing diopside paralava hosted by the rocks of the ‘olive unit’, in the Negev Desert, Hatrurim Basin, Israel (Galuskina et al., Reference Galuskina, Galuskin and Vapnik2016; Britvin et al., Reference Britvin, Galuskina, Vlasenko, Vereshchagin, Bocharov, Krzhizhanovskaya, Shilovskikh, Galuskin, Vapnik and Obolonskaya2021b).

Merrillite is one of the most common phosphates in meteorites of different types and forms a solid solution with ferro-merrillite, Ca₉NaFe²⁺(PO₄)₇, which is typical for Martian shergottites (Britvin et al., Reference Britvin, Krivovichev and Armbruster2016; Ward et al., Reference Ward, Bischoff, Roszjar, Berndt and Whitehouse2017). OH-bearing minerals of the merrillite group (whitlockite subgroup) occur only in terrestrial rocks (Frondel, Reference Frondel1943; Britvin et al., Reference Britvin, Pakhomovskii, Bogdanova and Skiba1991; Cooper et al., Reference Cooper, Hawthorne, Abdu, Ball, Ramik and Tait2013).

In this paper, we provide a description of a new mineral, deynekoite, and discuss common problems in the classification of the merrillite group. We also consider the mechanism and conditions of deynekoite formation in phosphide-bearing contact facies of paralava from Jordan. The mineral and its name (symbol Dnk) have been approved by the Commission on New Minerals, Nomenclature and Classification (CNMNC) of the International Mineralogical Association (IMA), as IMA 2020-108 (Galuskin et al., Reference Galuskin, Stachowicz, Galuskina, Woźniak, Vapnik, Murashko and Zieliński2022b). The name deynekoite is given in honour of Dr Dina V. Deyneko (born 1988) for her valuable contribution to the investigation of synthetic analogues of merrillite-group minerals (Deyneko et al., Reference Deyneko, Aksenov, Morozov, Stefanovich, Dimitrova, Barishnikova and Lazoryak2014). Type material was deposited in the mineralogical collection of the Fersman Mineralogical Museum, Leninskiy pr., 18/k. 2, 115162 Moscow, Russia, registration number: 5791/1.

Methods of investigation

The morphology and composition of deynekoite and associated minerals were studied using optical microscopy, scanning electron microscopes (Phenom XL and Quanta 250, Institute of Earth Sciences, Faculty of Natural Sciences, University of Silesia, Sosnowiec, Poland) and an electron microprobe analyser (Cameca SX100, Micro-Area Analysis Laboratory, Polish Geological Institute – National Research Institute, Warsaw, Poland). Chemical analyses were carried out in WDS-mode (wavelength-dispersive X-ray spectroscopy, settings: 15 keV, 20 nA and ~1 μm beam diameter) using the following lines and standards: NaKα – NaCl; CaKα and MgKα – diopside; AlKα and KKα – orthoclase; FeKα – Fe₂O₃; and VKα – V. Other chemical elements were below the detection limit.

The Raman spectra of deynekoite were recorded on a WITec alpha 300R Confocal Raman Microscope (Department of Earth Science, University of Silesia, Poland) equipped with an air-cooled solid laser (532 nm) and a CCD camera operating at –61°C. An air Zeiss LD EC Epiplan-Neofluan DIC-100/0.75NA objective was used. Raman scattered light was focused onto a multi-mode fibre and monochromator with a 600 mm^–1 grating. The power of the laser at the sample position was ~30 mW, and 15–20 scans with an integration time of 3–5 s were collected and averaged. The resolution was 3 cm^–1. The spectrometer monochromator was calibrated using the Raman scattering line of a silicon plate (520.7 cm^–1).

Single-crystal X-ray studies were carried out with a four-circle diffractometer SuperNova with AgKα radiation (λ = 0.56087 Å) (University of Warsaw Biological and Chemical Research Centre), equipped with an Eos CCD detector (Agilent). The detector-to-crystal distance was 63.2 mm. AgKα radiation was used at 65 kV and 0.6 mA. Crystals were attached to a non-diffracting Mitegen micromount support. A frame-width of 1° in ω scans and a frame time of 410 s were used for data collection. Information relevant to the data collection is summarised in Table 2. Reflection intensities were corrected for Lorentz, polarisation and absorption effects and converted to structure factors using CrysAlisPro 1.171.40.53 (Rigaku Oxford Diffraction, Reference Rigaku Oxford Diffraction2019) software.

Table 2.

Crystal data and structure refinement details for deynekoite.

*w = 1/[Σ²(F _o²) + (0.0236P)²], where P is [2Fc² + Fo²)]/3

Geological setting

Deynekoite was found in a small phosphorite prospecting quarry (31°22'01''N, 36°11'10''E) in the Daba-Siwaqa pyrometamorphic rock field, Hatrurim Complex, Jordan (Novikov et al., Reference Novikov, Vapnik and Safonova2013; Khoury et al., Reference Khoury, Sokol, Kokh, Seryotkin, Nigmatulina, Goryainov, Belogub and Clark2016). The Hatrurim Complex is distributed along the Dead Sea rift as a series of outcrops of pyrometamorphic rocks in the territories of Israel, Palestine and Jordan (Bentor, Reference Bentor1960; Gross, Reference Gross1977, Reference Gross1984; Vapnik et al., Reference Vapnik, Sharygin, Sokol and Shagam2007; Novikov et al., Reference Novikov, Vapnik and Safonova2013). The Hatrurim Complex is characterised by a wide diversity of rocks. Spurrite marble, larnite pseudoconglomerate and gehlenite hornfels dominate; however, there are also exotic rock types containing such rock-forming minerals as ye'elimite, Ca₄Al₆(SO₄)O₁₂; fluormayenite, Ca₁₂Al₁₄O₃₂F₂; nabimusaite, KCa₁₂(SiO₄)₄(SO₄)₂O₂F; ariegilatite, BaCa₁₂(SiO₄)₄(PO₄)₂F₂O; jasmundite, Ca₁₁(SiO₄)₄O₂S; ternesite, Ca₅(SiO₄)₂(SO₄); levantite, KCa₃Al₂(SiO₄)(Si₂O₇)(PO₄); silicocarnotite, Ca₅(PO₄)₂(SiO₄); oldhamite, CaS₂; khesinite, Ca₄(Mg₂Fe³⁺₁₀)O₄(Fe³⁺₂₀Si₂)O₃₆; and others (Galuskina et al., Reference Galuskina, Galuskin, Pakhomova, Widmer, Armbruster, Krüger, Grew, Vapnik, Dzierażanowski and Murashko2017a; Galuskin et al., Reference Galuskin, Galuskina, Gfeller, Krüger, Kusz, Vapnik, Dulski and Dzierżanowski2016, Reference Galuskin, Krüger, Galuskina, Krüger, Vapnik, Pauluhn and Olieric2019, Reference Galuskin, Galuskina, Krüger, Krüger, Vapnik, Krzątała, Środek and Zieliński2021, Reference Galuskin, Galuskina, Vapnik and Zieliński2023a). In the Hatrurim Complex, molten rocks that are diverse in composition form veins, lenses and oval bodies of paralavas and slag-like rocks from a few centimetres to tens of metres in size (Galuskin et al., Reference Galuskin, Gfeller, Galuskina, Pakhomova, Armbruster, Vapnik, Włodyka, Dzierżanowski and Murashko2015; Galuskina et al., Reference Galuskina, Galuskin, Pakhomova, Widmer, Armbruster, Krüger, Grew, Vapnik, Dzierażanowski and Murashko2017a, Reference Galuskina, Galuskin, Prusik, Vapnik, Juroszek, Jeżak and Murashko2017b, Reference Galuskina, Galuskin, Vapnik, Prusik, Stasiak, Dzierżanowski and Murashko2017c; Krzątała et al., Reference Krzątała, Krüger, Galuskina, Vapnik and Galuskin2020; Krüger et al., Reference Krüger, Galuskin, Galuskina, Krüger and Vapnik2021; Murashko et al., Reference Murashko, Britvin, Vapnik, Polekhovsky, Shilovskikh, Zaitsev and Vereshchagin2022). It is the paralavas, which feature relatively coarser-grained rocks compared to other types of pyrometamorphic rocks, that are associated with the discovery of a significant number of new minerals. One example is the diopside–anorthite–tridymite paralava which forms a body ~30 m in diameter in pyrometamorphically altered carbonate rock of the Muwaqqar Chalk–Marl Formation, Daba-Siwaqa, Jordan. Deynekoite and a series of new minerals presented by both reduced (phosphides) and oxidised (phosphates containing Fe³⁺) phases were discovered at the contact facies of this paralava. The phosphides discovered were transjordanite, Ni₂P; zuktamrurite, FeP₂; murashkoite, FeP; orishchinite, Ni₂P; and nickolayite, FeMoP. The phosphates were crocobelonite, CaFe³⁺(PO₄)O; moabite, NiFe³⁺(PO₄)O; yakubovichite, CaNi₂Fe³⁺(PO₄)₃; and nazarchukite, Ca₂NiFe³⁺₂(PO₄)₄ (Britvin et al., Reference Britvin, Murashko, Vapnik, Polekhovsky, Krivovichev, Vereshchagin, Vlasenko, Shilovskikh and Zaitsev2019a, Reference Britvin, Vapnik, Polekhovsky, Krivovichev, Krzhizhanovskaya, Gorelova, Vereshchagin, Shilovskikh and Zaitsev2019b, Reference Britvin, Murashko, Vapnik, Polekhovsky, Krivovichev, Krzhizhanovskaya, Vereshchagin, Shilovskikh and Vlasenko2020, Reference Britvin, Murashko, Krzhizhanovskaya, Vapnik, Vlasenko, Vereshchagin, Pankin and Vasiliev2021a, Reference Britvin, Galuskina, Vlasenko, Vereshchagin, Bocharov, Krzhizhanovskaya, Shilovskikh, Galuskin, Vapnik and Obolonskaya2021b, Reference Britvin, Murashko, Vapnik, Zaitsev, Shilovskikh, Krzhizhanovskaya, Gorelova, Vereshchagin, Vasilev and Vlasenko2022a, Reference Britvin, Murashko, Krzhizhanovskaya, Vereshchagin, Vlasenko, Vapnik and Bocharov2022b, Reference Britvin, Murashko, Krzhizhanovskaya, Vlasenko, Vereshchagin, Vapnik and Bocharov2023a, Reference Britvin, Murashko, Krzhizhanovskaya, Vapnik, Vlasenko, Vereshchagin, Pankin, Zaitsev and Zolotarev2023b; Murashko et al., Reference Murashko, Britvin, Vapnik, Polekhovsky, Shilovskikh, Zaitsev and Vereshchagin2022).

The genesis of the Hatrurim Complex rocks remains an unsolved problem. The early ‘classic hypothesis’ stated that pyrometamorphic rocks formed as a result of the spontaneous combustion of bitumen, which was contained in a sedimentary protolith (Kolodny and Gross, Reference Kolodny and Gross1974; Matthews and Gross, Reference Matthews and Gross1980; Geller et al., Reference Geller, Burg, Halicz and Kolodny2012). The relatively recent ‘mud volcano’ hypothesis suggests that deep anomalous pressure in the sedimentary sequence caused by the tectonic activity of the Dead Sea Rift affected the destruction of hydrocarbon collectors, inducing subsequent methane combustion in the vicinity of the surface (Sokol et al., Reference Sokol, Novikov, Zateeva, Vapnik, Shagam and Kozmenko2010; Novikov et al., Reference Novikov, Vapnik and Safonova2013). Our investigation shows that the reactions of combustion by-products (hot gases, fluids and melts) with the pyrometamorphic phases formed earlier sharply increased the mineral diversity of the rocks (Galuskin et al., Reference Galuskin, Galuskina, Gfeller, Krüger, Kusz, Vapnik, Dulski and Dzierżanowski2016, Reference Galuskin, Krüger, Galuskina, Krüger, Vapnik, Pauluhn and Olieric2019).

Deynekoite occurrence

The paralava studied presents a dense, fine-grained rock in which porous, pumice-like fragments are distributed in an undulating pattern (Fig. 1a). It consists of diopside with hedenbergite rims, wollastonite, anorthite, tridymite, fluorapatite and a small amount of glass (Fig. 1b). The presence of cristobalite with typical fissures showing a fish-scale texture indicates that tetragonal cristobalite is a product of phase transition and the primary crystallisation of the mineral was as a high-temperature cubic phase, growing on tridymite (Fig. 1c). In thin apophyses of paralava into the country rock, pseudomorphs of fluorapatite after fish bones were detected (Fig. 1d). Accessory minerals of the paralava include spinel of the magnesiochromite–chromite–magnetite–trevorite series, titanite and pyrrhotite.

Figure 1.

(a) Heterogeneous, porous basalt-like rock from a central part of the paralava body. (b) Paralava consisting of diopside, tridymite, anorthite and wollastonite. Back-scattered electron (BSE) image. (c) Cristobalite with fish-scale texture fissures overgrowing tridymite. BSE image. (d) Pseudomorph of fluorapatite after fish bone in the paralava. BSE image. An = anorthite, Crs = cristobalite, Di = diopside, Fap = fluorapatite, Hd = hedenbergite, Gls = glass, Mgt = magnetite, Trd = tridymite, Tnt = titanite, Wol = wollastonite.

Minerals of the merrillite group forming a solid solution of merrillite–keplerite–deynekoite–whitlockite occur in a thin dark zone on the boundary of paralava and altered country rock (Fig. 2a). A contact facies of paralava has been strongly altered by low-temperature processes. Here, prismatic diopside crystals with composition close to ideal and up to 1 cm in size are embedded in a low-temperature mineral matrix containing primarily calcite and zeolites, among which gismondine-Ca prevails (Fig. 2b–d). Locally, rocks are enriched in minerals of the tobermorite, ettringite groups and unidentified opal-like Ca-hydrosilicates–phosphates.

Figure 2.

(a) Contact of diopside paralava (I) and altered marl (II), black is a hematite-bearing zone. The white frame shows a fragment magnified in Fig. 2b. (b) Position of phosphate mineralisation at the contact zone of rocks: 1 – diopside paralava, 2 – zone enriched with phosphides (murashkoite, zuktamrurite), 3 – phosphate zone, 4 – hematite zone (developed after pyrrhotite), 5 – altered host rock (marl); diopside chondrules are shown by arrows. (c) Phosphate zone represented, mainly, by deynekoite. Diopside paralava is replaced intensively by calcite and gismondine-Ca; in unaltered diopside crystals, barringerite inclusions are noted. The white frame shows a fragment magnified in Fig. 2d; (d) One of the rare places where deynekoite forms almost monomineralic aggregates of elongated grains up to 50 μm in size. Bgr = barringerite, Dnk = deynekoite, Di = diopside, Fap = fluorapatite, Hem = hematite, Gsm = gismondine-Ca, Muh = murashkoite.

In the contact facies of the paralava, needle-like inclusions of 1–2 μm in thickness of barringerite (Fig. 1c) and oldhamite are observed in diopside crystals. Small cracks in the rock ~0.1 mm in thickness are filled with aggregates of phosphides of the barringerite–transjordanite series replaced by murashkoite. Rare grains of Ti-bearing pyrrhotite, daubréelite and blue Ti³⁺-bearing titanite were also noted.

A dark zone at the contact of the paralava with the altered country rock is characterised by zonation in the direction from paralava to country rock (Fig. 2b). The phosphide zone, where barringerite, transjordanite, murashkoite and zuktamrurite were identified, is gradually replaced by a phosphate zone. The phosphate zone consists mainly of minerals of the merrillite group and fluorapatite. Here, we identified graftonite-(Ca), CaFe²⁺₂(PO₄)₂; crocobelonite, CaFe³⁺₂(PO₄)₂O; Fe-analogue of stanfieldite, Ca₄MgFe²⁺₄(PO₄)₆; and β-Fe₂P₂O₇ – a high-temperature analogue of nabateaite, γ-Fe₂P₂O₇, discovered recently in phosphide-bearing paralava in Israel (Britvin et al., Reference Britvin, Murashko, Vapnik, Vlasenko, Vereshchagin, Krzhizhanovskaya and Bocharov2021c).

The phosphate zone is followed by a hematite zone, in which relics of Fe–Ni spinel and pyrrhotite are preserved, and on the boundary of which the country rock is transformed into chondrite-like rock (Fig. 2b). Individual diopside crystals are observed in all the described zones (Fig. 2b,c). Fe²⁺-bearing phosphates tend to occur next to phosphides, whereas Fe³⁺-bearing phosphates are usually in contact with hematite. Grained aggregates of deynekoite were found as intergrowths with hematite in several polished mounts. Typically, fluorapatite is intergrown with hematite (Fig. 2c,d). Small relics of Fe²⁺-bearing phosphates and berlinite, AlPO₄, occurring in deynekoite deserve attention. The morphology of the hematite, which has a lattice-like form, indicates that it formed after the pyrrhotite crystals (Fig. 2d).

Deynekoite forms aggregates with grains up to 30–40 μm in size. The grains are transparent and light-yellow and light-brown in colour. The streak is white with a yellowish tint. The microhardness is VHN₂₅ = 319(29), 253–331 (in kg/mm²), which corresponds to a Mohs hardness of 4.5. The mineral is brittle with a conchoidal fracture, and cleavage is not observed. Its density, calculated on the basis of the empirical composition and the structural data, is 3.09 g⋅cm^–3. Deynekoite is uniaxial (−), its refractive indices are ω = 1.658(3), ε = 1.652(3) (λ = 589 nm), and pleochroism was not observed.

Deynekoite has a relatively invariable chemical composition (Tables 1, 3), and it can be described by the mean empirical formula (Ca_8.90Na_0.11K_0.02)_Σ9.03(Fe³⁺_0.62Mg_0.30Al_0.05)_Σ0.97P_6.98V⁵⁺_0.05O_27.70(OH)_0.30, which can be simplified to Ca_9.00(Fe³⁺_0.70Mg_0.30)_Σ1.0[(PO₄)_6.70 (PO₃OH)_0.3]_Σ7, and the end-member formula Ca₉Fe³⁺(PO₄)₇.

Table 3.

Chemical composition of deynekoite.

* Water was calculated by charge balance; ** (OH) apfu; S.D. – standard deviation

Raman spectroscopy

In the Raman spectrum of deynekoite (Fig. 3) most of the bands are related to vibrations in (РО₄)^3– groups: bands in the range 1200–1000 cm^–1 are connected with vibrations ν₃(PO₄)^3–; 1000–900 cm^–1 with ν₁(PO₄)^3–; 550–630 cm^–1 with ν₄(PO₄)^3–; and 400–470 cm^–1 with ν₂(PO₄)^3–. Bands lower than 300 cm^–1 are ascribed to vibrations of Са–О and lattice vibrations. In the deynekoite spectrum there are two bands, at 934 cm^–1 and 880 cm^–1, which have low intensity but appear in all its spectra. These bands are not noted in merrillite and keplerite spectra (Britvin et al., Reference Britvin, Galuskina, Vlasenko, Vereshchagin, Bocharov, Krzhizhanovskaya, Shilovskikh, Galuskin, Vapnik and Obolonskaya2021b). The band at 934 cm^–1 is related to P–O vibrations in the PO₃OH group. The same band is observed in the spectrum of whitlockite (Jolliff et al., Reference Jolliff, Hughes, Freeman and Zeigler2006). The band at 880 cm^–1 is connected with the ν₁(VO₄)^3– vibration. As has been shown for the pyromorphite–vanadinite series, even for a low content, when V⁵⁺ substitutes for P⁵⁺ at the tetrahedra, bands from the stretching vibration of V–O in ν₁(VO₄)^3– are clearly visible in the Raman spectra (Solecka et al., Reference Solecka, Bajda, Topolska, Zelek-Pogudz and Manecki2018). The OH-group content in deynekoite is insignificant, so bands from O–H stretching vibrations within the characteristic range 3000–3700 cm^–1 are not observed (Fig. 3).

Figure 3.

Raman spectrum of deynekoite.

Deynekoite structure

The crystal structure of deynekoite was solved in the R3c space group with a dual-space algorithm implemented in Shelxt (Sheldrick, Reference Sheldrick2015a). The model was refined with least-squares minimisation using Shelxl (Sheldrick, Reference Sheldrick2015b), with Olex2 (Dolomanov et al., Reference Dolomanov, Bourhis, Gildea, Howard and Puschmann2009) as the graphical interface. Twinning by inversion was observed with two domains of 56:44 ratios. The occupancy of the M site in deynekoite was constrained to 1 and refined as Fe vs. Mg. Disorder in the ^{P 1}PO₄ tetrahedron was observed, where the P1 and O10 sites split into two parts, forming P1A, O10A and P1B, O10B groups of atoms. The occupancy of ^{P 1}PO₄ was constrained to 1 and the occupancies of the disordered atoms were refined as part 1 vs. part 2. The H10b atom was fixed at 0.96 Å from O10B in the direction of the O8 atom to form an H-bond interaction. The occupancy of H10b was refined together with P1B and O10B in the ‘part 2’ group of the disordered atoms. Experimental details and refinement data are summarised in Tables 2, 4–6. The crystallographic information file has been deposited with the Principal Editor of Mineralogical Magazine and is available as Supplementary material (see below). In the deynekoite structure a series of polyhedra are distinguished, parts of which are fully occupied by cations of one type. There are tetrahedrally coordinated phosphorus sites P2 and P3, eight-coordinated Ca sites (Ca1, Ca2 and Ca3) and a number of oxygen sites (Table 4). The M site in minerals of the merrillite structure is always fully occupied (Britvin et al., Reference Britvin, Galuskina, Vlasenko, Vereshchagin, Bocharov, Krzhizhanovskaya, Shilovskikh, Galuskin, Vapnik and Obolonskaya2021b). In the case of deynekoite, this site is occupied by Fe³⁺, Mg and Al. Refinement of the site occupation gave (Fe³⁺_0.58Mg_0.42), which yields a charge of +2.58 and 20.12 е ^–. Data from the microprobe analyses gave the occupation of the M site (Fe³⁺_0.62Mg_0.30Al_0.05), which yields a charge of +2.61 and 20.37 е ^–. Considering that it is impossible to separate Mg and Al during structure refinement, the data regarding the occupation of the M site are relevant to the microprobe analyses data, although it cannot be ruled out that the grain used for the structure refinement has a slightly lower Fe³⁺ content. The tetrahedral site P1 splits into sites P1A and P1B with refined occupation in a ratio of 0.73:0.27. The occupation ratio of the О10А and О10В sites is identical; the atoms are located at the top of the tetrahedra and oriented to the opposite sides. The bases of both tetrahedra are formed by oxygen О9–О9–О9. The tetrahedron ^{P 1A}PO₄ has the typical interatomic distances P1A–O9 = 1.534(4) Å and P1A–O10A = 1.526(14) Å (Table 6). The first variant of the structure refinement of deynekoite, submitted in the new-mineral proposal check-list, reported an anomalously large distance P1В–O10В = 1.78(5) Å and normal distances P1В–O9 = 1.517(6) Å×3. In whitlockite the distance P1В–(O10BH) ≈ 1.61 Å (Hughes et al., Reference Hughes, Jolliff and Rakovan2008). The anomalous bond length may be due to the presence of a very small amount of Na at the X site, which overlaps with the O10B position in deynekoite. We have taken into consideration the X site in the revised deynekoite structure model and have refined the Na content at this site equal to 0.1 atoms per formula unit (apfu). It may be that the X site has the lower occupation as it can contain K (Table 2). In the revised model, the distances in the ^{P 1В}PO₄ tetrahedron are P1В–O10В = 1.64(5) Å and P1В–O9 = 1.519(6) Å ×3 (Table 5). The increase in the P1В–O10В distance in comparison with P1А–O10А is connected with the partial protonation of O10B with the formation of strong hydrogen bond O10B⋅⋅⋅O8 with the distance d _O10B–O8 = 2.68(3)Å and ∠^{O–H⋅⋅⋅O} = 175.5° (see Fig. 5e). The deynekoite structure, which is formed by the intercalation of two types of layers, is shown in Fig. 4.

Figure 4.

Deynekoite structure. (a) Projection on (010). The structure can be presented as the intercalation of two types of layers (see Fig. 5) in the sequence ABA'B’A’’B”A. (b) Projection on (001). One slice of the A layer and two slices of B layers are shown. The Na site with lower occupation is not shown. Ca atoms – light-orange; Na atoms – yellow; ^P2PO₄ tetrahedron – dark-blue; ^P3PO₄ tetrahedron – blue; ^{P 1A}PO₄ tetrahedron – dark-green; ^{P 1B}PO₄ tetrahedron – light-green; МО₆ octahedron – brown; oxygen O10B – dark blue balls; oxygen O10A – blue balls; hydrogen – small pink balls.

Figure 5.

(a,b) Layers of two types (А, В see Fig. 4) in the structure of deynekoite, projection on (00$\bar{1}$). (a) In the B layer formed by six-membered rings building from Ca-polyhedra, three types of triangular empty occupation are shown as in the ideal structures of merrillite (1), deynekoite (2) and whitlockite (3). (b) The A layer is the same in merrillite, deynekoite and whitlockite, consisting of millwheel clusters M(^P2+P3PO₄)₆ linked with one another by triplets of Ca-polyhedra. (c–e) Atom arrangement near the P1 site in holotype deynekoite: c – merrillite type (10%); d – deynekoite type (63%); e – whitlockite type (27%). Ca-polyhedra – light-orange; ^P2PO₄ tetrahedron – dark-blue; ^P3PO₄ tetrahedron – blue; ^{P 1A}PO₄ tetrahedron – dark-green; ^{P 1B}PO₄ tetrahedron – light-green; truncated prism XO₆ – yellow; octahedron МО₆ – brown (Fe3+)/dark-orange (Mg); oxygen – blue balls; hydrogen – pink balls (hydrogen bonds are shown); empty circle – vacancy.

Table 4.

Fractional atomic coordinates and isotropic* or equivalent isotropic displacement parameters (Ų) for deynekoite.

Table 5.

Atomic displacement parameters (Ų) for deynekoite.

Table 6.

Selected bond lengths (Å) and bond-valence sum (BVS) calculation for deynekoite.

As deynekoite occurs only in tiny amounts and its crystals contain large amounts of inclusions of other phases, powder X-ray diffraction data were not collected, as it could be calculated more reliably from the results of single-crystal structure refinements. The calculated data are listed in Supplementary Table S1.

Structural aspects

The crystal structure of the merrillite-group minerals is formed by a framework of cation-centred polyhedra linked by common corners and edges. There are PO₄ tetrahedra, MO₆ octahedra, AO₈ polyhedra and XO₆ distorted trigonal prisms. The merrillite type structure is usually considered a combination of columns of different types along the Z axis (Britvin et al., Reference Britvin, Galuskina, Vlasenko, Vereshchagin, Bocharov, Krzhizhanovskaya, Shilovskikh, Galuskin, Vapnik and Obolonskaya2021b). It can also be described as an interlayering of corrugated layers (modules) of two types, nested within each other (Fig. 4, 5). This interpretation was applied, for example, in the description of the structure of Ca₉Y(VO₄)₇ (Lazoryak et al., Reference Lazoryak, Deyneko, Aksenov, Stefanovich, Fortalnova, Petrova, Baryshnikova, Kosmyna and Shekhovtsov2018).

The first type of layer (type B, Fig. 4) is presented by corrugated six-fold rings formed by the edge sharing ^ACaO₈ polyhedra. In the inside ring in the merrillite layer there is a truncated ^XNaO₆ prism, sharing common edges with Ca polyhedra (Fig. 5a). The prism also shares a top face with ^{P 1A}PO₄ tetrahedra and bottom corners with three other phosphate groups, which are linked to the Ca ring apically (Fig. 5c). In deynekoite, an Na(X) site has low occupation (0.1 apfu) and inside the ring there is a virtual trigonal bipyramid (Fig. 5a) which is formed by a disordered PO₄ tetrahedron oriented either down (^{Р 1A}PО₄) or up (^{Р 1B}PО₄) in the ratio 0.73:0.27 (Fig. 5d,e). As a rule, in minerals of the merrillite subgroup the ^{Р 1A}PО₄ tetrahedron is occupied (at the top of the truncate Na-prism), whereas in the whitlockite-subgroup minerals, the ^Р1BPО₄ tetrahedron is practically fully occupied (at the place of the missing Na-site) (Figs 5c, 6). In a synthetic phase, which is very close in composition to natural deynekoite (Deyneko et al., Reference Deyneko, Aksenov, Morozov, Stefanovich, Dimitrova, Barishnikova and Lazoryak2014), the tetrahedron-up ^{Р 1B}PО₄ is fully occupied as in whitlockite (Figs. 5e, 6). However, in whitlockite the tetrahedron-down ^{Р 1A}PО₄ can have a low phosphorus content (Fig. 6d). The second type of structural layer (А type, Fig. 4) repeats without changes in all minerals of the merrillite group and features M(PO₄)₆ clusters. The clusters are linked to each other by Ca-polyhedra (CaO₈) triplets (Fig. 5b).

Figure 6.

Comparison of deynekoite [(a), Na site lower occupied is not shown] and its synthetic analogue [(b), crystal structure data from Deyneko et al., Reference Deyneko, Aksenov, Morozov, Stefanovich, Dimitrova, Barishnikova and Lazoryak2014], merrillite [(c), crystal structure data from Xie et al., Reference Xie, Yang, Gu and Downs2015] and whitlockite [(d), crystal structure data from Hughes et al., 2008], projection on (010). Са – light-orange balls; ^P2PO₄ tetrahedron – dark blue; ^P3PO₄ tetrahedron – blue; ^{P 1A}PO₄ tetrahedron – dark-green; ^{P 1B}PO₄ tetrahedron – light-green; truncate prism XO₆ – yellow; МО₆ octahedron – brown (Fe)/light-green (Mg); hydrogen – pink balls. The numerals show tetrahedral site occupation in percent.

Deynekoite is the first mineral of the merrillite group with a formally vacant X (Na) site (Na pfu ≤ 0.1). Natural deynekoite, ~Ca₉(□_0.9Na_0.1)[Fe³⁺_0.58(Mg,Al)_0.42)(P O₄)_6.73(PO₃OH)_0.27, has a synthetic analogue with close composition – Ca₉(Fe³⁺_0.63Mg_0.37)(PO₄)_6.63(PO₃OH)_0.37 (Deyneko et al., Reference Deyneko, Aksenov, Morozov, Stefanovich, Dimitrova, Barishnikova and Lazoryak2014). In the synthetic analogue the tetrahedron-up ^{Р 1B}PО₄ with apical oxygen, which is partially (0.37) protonated, is fully occupied (Fig. 6b). In deynekoite the tetrahedron-down ^{Р 1А}PО₄ has 0.73 occupation, vs. 0.27 for the tetrahedron-up ^{Р 1B}PО₄ (Fig. 6a). The apical oxygen ^O10BO of ^{Р 1B}PО₄ forms an OH group, where ^H10BH is disordered between three symmetrically equivalent positions. The distance ^{P 1B}P–^O10BO = 1.64 Å is increased compared to the distance ^{P 1B}P–^O10BO = 1.53 Å (Table 6) and close to the distance ^{P 1B}P–^O10BO = 1.614 Å in whitlockite (Hughes et al., Reference Hughes, Jolliff and Rakovan2008).

The iron valence in deynekoite was not determined by the direct method because of the limited amount of material and very small grain size. The yellow-to-brown colour of deynekoite, totals from microprobe analyses close to 100% and the significant decrease of the mean M–O = 2.041 Å in comparison with other minerals of the merrillite group (which have the distance M–O = 2.08 Å) all indicate that iron in deynekoite is trivalent. This is confirmed by the bond-valence sum (BVS) calculation (Table 5), which shows that the trivalent cation predominates at the M site.

The differences in the occupation of the ^{Р 1}(PО₄)^3– sites in deynekoite and synthetic analogues can be explained by the peculiar features of deynekoite's origin. Initially, in high-temperature and reduced conditions, ferromerrillite, NaCa₉(Fe²⁺,Mg)(PO₄)₇, forming a solid solution with keplerite, Ca_0.5Ca₉(Fe²⁺,Mg)(PO₄)₇, crystallises. As the temperature decreases and oxygen activity increases, ferromerrillite is replaced by deynekoite with the removal of Na from the structure. Deynekoite inherits the characteristics of the ferromerrillite structure – the ^{P 1А}PO₄ tetrahedron preserves significant occupation, though a small part of the phosphorus changes its position and occupies the ^P1BPO₄ site, accompanied by the protonation of the ^O10BO apical oxygen.

Genesis

Diopside–anorthite–tridymite paralava, on the contact of which deynekoite was found, was generated at the near-surface combustion focus. This was a continuous and relatively long-lasting combustion phenomenon that determined the anomalous high temperature of the generated melt (~1500°С). One indicator of the super-high combustion temperature is cristobalite with a fish-scale or ballen structure (Fig. 1c), which reflects volume shrinkage upon the inversion of β-cristobalite to α-cristobalite (Schmieder et al., Reference Schmieder, Buchner and Kröchert2009).

The genesis of phosphides and phosphates on the boundary of the diopside–anorthite–tridymite paralava was connected with the interaction of the paralava and country rocks, which were a source of reductant (altered bitumen) and also phosphorus and iron. These probably came from the phosphorite-bearing rocks of the Muwaqqar formation, the so-called Р–Fe–C (± Si) series analogous to the rocks of the lower part of the Ghareb formation, Israel (Shahar et al., Reference Shahar, Yaacov and Yair1989). A find of fluorapatite pseudomorphs after fish bones in the paralava confirms the presence of phosphorite inclusions in the carbonate protolith (Fig. 1d). Accessory fluorapatite in the paralava was stable on the contact of paralava with the country rocks and cannot be a source of phosphorus. The genesis of phosphides is related to carbothermal reductive reactions on the boundary of paralava and country rocks. These reactions were considered by us in the frame of the phosphide genesis model defined for the contact of gehlenite paralava and fragments of country rocks in breccia of the Hatrurim Basin in the Negev Desert, Israel: Fe₂O₃ + 3C → 2Fe(lq) + 3CO(g); 8Ca₅(PO4)₃F [fluorapatite from phosphorite with (OH)^– and (CO₃)^2– impurities] + 22SiO₂ + 20Al₂O₃ + 60C = 12P₂(g) + 60CO(g) + 20Ca₂Al₂O₇ + 2SiF₄(g); nFe(lq) + ½P₂(g) = FenP, n = 1,2,3 (Galuskin et al., Reference Galuskin, Galuskina, Kamenetsky, Vapnik, Kusz and Zieliński2022a, Reference Galuskin, Kusz, Galuskina, Książek, Vapnik and Zieliński2023b). The crystallisation of phosphides took place in the context of the increasing activity of P that is reflected in the crystallisation sequence of Fe₂P (barringerite) – FeP (murashkoite) – FeP₂ (zuktamrurite) (Britvin et al., Reference Britvin, Murashko, Vapnik, Polekhovsky, Krivovichev, Vereshchagin, Vlasenko, Shilovskikh and Zaitsev2019a, Reference Britvin, Vapnik, Polekhovsky, Krivovichev, Krzhizhanovskaya, Gorelova, Vereshchagin, Shilovskikh and Zaitsev2019b). The temperature of phosphide formation from a melt was higher than 1300°C (the temperature of barringerite crystallisation is 1350°C), which is similar to the temperature at which troilite (pyrrhotite) crystallises from sulfide melt. With the further decrease in temperature and increasing influence of atmospheric oxygen (processes occurring at near-surface conditions), phosphides were replaced by Fe²⁺-bearing phosphates, which were changed by association of Fe³⁺-bearing phosphates. Our investigations of phosphide-bearing rocks from Jordan and Israel show that other minerals of the merrillite group (merrillite, keplerite, ferromerrillite and possibly matyhite), also appear in them. These minerals contain Fe²⁺ and crystallise from the locally generated phosphate melt at high temperatures (~1200°C). Deynekoite, which contains Fe³⁺ (substituting Fe²⁺-phosphates) and a small amount of water (see below), was formed at lower temperatures (600–800°C). Most likely, when the early associations were replaced by later ones, metasomatic mechanisms of the replacement of minerals in the quasi-solid state and with the participation of intergranular melt and active gases were realised.