Fibrous Platinum-Group Minerals in “Floating Chromitites” from the Loma Larga Ni-Laterite Deposit, Dominican Republic

1. Introduction

The platinum-group elements (PGE) are a group of precious metals (Os, Ir, Ru, Rh, Pt, and Pd) which are referred to strategic metals because of their extreme scarcity within the Earth’s crust combined with the increasing need for PGE in advanced technologies (e.g., autocatalyst industries; electronics) and jewellery [1]. Currently, the vast majority (~80%) of the worldwide PGE demand is supplied by magmatic ore deposits located in only two countries, i.e., South Africa and Russia [2]. This supply situation has motivated the search for alternative sources of PGE, and large oxidized ore deposits associated with near surface modification of ultramafic rocks, such as ophiolite-related Ni-laterites, have been considered as worthy exploration targets for future unconventional PGE ore deposits [3]. In general, total PGE contents found in Ni-laterites around the world are in the range of <100 ppb to up to a few hundred ppb, however lateritic crust with 2 ppm PGE was reported from Western Australia [4] as well as >4 ppm PGE from Burundi [5].

Ni-laterites from the northern Caribbean are systematically enriched in the limonite and reach values of up to 0.6 ppm total PGE [6]. These increasing PGE contents toward the surface are mainly explained by residual accumulations of PGE-bearing minerals. However, the results of detailed mineralogical surveys also provide convincing morphological and chemical evidence for in situ neoformation of platinum-group minerals (PGM) within Ni-laterites by bioreduction and/or electrochemical accretion [7,8]. Hence, accumulations of what are most likely biogenic mediated in situ growths of PGM nanoparticles are believed to contribute to PGE anomalies in Ni-laterites. The recent verification of the biological role of PGM transformations in supergene environments by [9] has marked the beginning of a new period of PGE-related investigation and exploration.

The presented contribution reports on the observation of enigmatic fibrous PGM found close to the surface in Ni-laterites from the Dominican Republic and aims (i) to give a general overview of the prevailing features of fibrous PGM; (ii) to provide detailed textural as well as mineralogical data of one characteristic fibrous PGM and (iii) to discuss a possible origin of fibrous PGM.

2. Sample Material and Methods

Samples were collected in the ophiolite-related Loma Larga Ni-laterite ore deposit which forms part of the Falcondo mining area located in the central part of the Dominican Republic (Figure 1). The Falcondo mining area is currently known as the largest hydrous Mg-silicate type Ni-laterite deposit of the Caribbean, with measured and indicated Ni resources of 67.8 Mt at a grade of 1.5% Ni plus 4.9 Mt at 1.4% Ni inferred [10].

The Ni-laterite at Falcondo developed over the so-called Loma Caribe peridotite which occurs as a serpentinized belt of ultramafic rocks approximately 4–5 km wide and 95 km long in the northwest of Santo Domingo (Figure 1). Detailed information of the local geology and formation history of the Ni-laterites can be found elsewhere (e.g., [11] and references therein). In general, the weathering profile of the Falcondo mining area is divided into: (i) serpentinized protolith (harzburgite > dunite > lherzolite) at the bottom followed by (ii) saprolite with hydrous Mg-silicate dominated mineralogy (beneath the Mg-discontinuity) and (iii) limonite with Fe-oxide(s) dominated mineralogy at the top (above the Mg-discontinuity) [11,12,13,14].

Small, rare, and hence uneconomic chromitite occurrences are scattered within given horizons of the lateritic profile [15,16]. Within the Ni-laterite profile of the Loma Larga ore deposit a highly weathered chromitite body of approximately 0.5 m × 0.5 m is included in limonite (“floating chromitite”) (Figure 1). This chromitite is characterized by extremely high PGE contents up to 17.5 ppm total PGE [7].

Approximately 100 g of homogenized “floating chromitite” sample was carefully disaggregated, milled, and hand-sieved before being processed by means of hydroseparation (HS) techniques at the HS laboratory in Barcelona, Spain ([8] and reference therein). Heavy mineral concentrates were mounted as loose (unpolished) grains on a metallic cylinder (diameter 2.5 cm) and/or as polished monolayer resin blocks and were subsequently investigated by stereomicroscopy, optical reflected light microscopy, and by scanning electron microscopy (SEM) using a Quanta 200 FEI XTE 325/D8395 (FEI, Hillsboro, OR, USA) as well as a field emission scanning electron microscope (FE-SEM) Jeol JSM-7100 (JEOL, Tokyo, Japan) at the Serveis Científics i Tecnòlogics, University of Barcelona, Spain.

At the same institution, quantitative electron microprobe analyses (EMPA) were obtained with a JEOL JXA-8230 electron microprobe (JEOL, Tokyo, Japan) operating in wavelength-dispersive spectroscopy (WDS) mode with an accelerating voltage of 20 kV, a beam current of 10 nA, and a beam diameter of 1 μm. Pure metals were used as standards for Os, Ir, Ru, Rh, Pt, Pd, Co, and Sb as well as chromite (Al, Fe), periclase (Mg), NiO (Ni), S (S), GaAs (As), and wollastonite (Si). The following interferences RuLβ → RhLα, RhLβ → PdLα, RuLβ → PdLα, and RhLα → PtLα were online-corrected. The same instrument was used for element distribution maps (WDS mode) with an accelerating voltage of 20 kV and a beam current of 128.8 nA. Maps were collected by beam scanning with dwell times of 60 ms/pixel. For each element, the background map was subtracted from the corresponding peak map.

One fibrous PGM was investigated by single-crystal X-ray diffraction (XRD, Bruker, Billerica, MA, USA) analysis at the same institution. The X-ray intensity data were measured on a D8 Venture system equipped with a multilayer monochromator and a Mo microfocus (λ = 0.71073 Å). The sample was analyzed at a distance of 34 mm. The angles of the goniometer were 2theta = 0°, omega = 360°, and chi = 90°, and the sample was spun 360°. The measuring time was 60 s per step. Subsequent results were processed with Bruker software [19] which was used to subtract the background of the patterns, to detect the peaks, and to assign minerals and their corresponding d_hkl to each peak.

3. Mineralogy of Fibrous PGM

Approximately 300 grains of PGM in the size range of <10 µm to ~125 µm in diameter and with either Ru-, Ir-, or Pt-dominated mineralogy were detected in heavy mineral concentrates. Ru-dominated and Fe-rich alloys (e.g., ruthenian hexaferrum) are the most abundant PGM (>90%), followed by lower quantities of Ir- and Pt-bearing Fe-Ni alloys ([7,20] respectively). Careful examination of all PGM via FE-SEM led to the observation of a rarely occurring (~1%), Ru-dominated subgroup which is characterized by fibrous textures (Figure 2). These textures are explained by grain-forming fibers which are significantly longer (1–5 µm) than they are wide (~100 nm). Due to their nanometric diameters, these fibers were defined as nanofibers. In general they occur as <5 µm thick layers of nanofiber-bundles which are oriented orthogonal to the grains’ surfaces (Figure 2B,E). Fibrous PGM show diverse morphologies that range from subhedral to anhedral grains (e.g., Figure 2C,I, respectively) and elongated fibrous PGM occur in addition (Figure 2G). Interestingly, some grains contain rounded voids from where nanofiber-bundles propagate radially (Figure 2D,E,I). Energy-dispersive spectroscopy (EDS) analyses (spot diameter of 1 µm) suggest that fibrous PGM contain mainly Ru and Fe with minor contents of Os and Ir. However, small but clear peaks of Si are also observed.

3.1. Detailed Investigation of One Fibrous PGM

3.1.1. Field Emission Scanning Electron Microscopy (FE-SEM)

One fibrous PGM was separated and investigated in detail. The unpolished grain has an isometric morphology with approximately 75 µm long axes and is characterized by a subhedral shape with damaged corners and a broken central part (Figure 3A). A detailed survey by means of FE-SEM revealed numerous features on the surface of the grain which, to the best of the authors’ knowledge, have not been described for PGM before:

• the structure of the grain suggests an interdependency of PGM nanoparticles and nanofiber-bundles which are oriented orthogonal to the grain’s surface (Figure 3A,B,G,H);
• nanofibers occur within layers of nanofiber-bundles as well as within open spaces suggesting either in situ growth (“healing of cracks”) or misalignments (Figure 3C,D);
• comparison of BSE images and secondary electron (SE) images suggests that elements of high atomic number (PGE) are present in the central part of the nanofibers (bright in BSE images), whereas the outer part of the nanofibers appears to consist of elements with lower atomic numbers (e.g., Si) (Figure 3E,F);
• at the endings of nanofiber-bundles, a thin layer of a homogenous film occurs that host PGM nanoparticles (Figure 3G–J);
• within the central part of the grain a Si-rich, crater-like texture is present which occurs dark in BSE images (Figure 3A). This “crater” measures approximately 5 µm × 7 µm in diameter and hosts a great number of homogenously distributed PGM nanoparticles. At its periphery an Ir-rich accumulation (~1 µm in diameter) with a rather irregular shape is observed (Figure 3K);
• around the crater-like texture, PGM nanoparticles occur, which are characterized by ragged morphologies resembling sponge spicules. Interestingly, the Si-rich crater-like texture hosts smaller PGM nanoparticles than its Si-depleted immediate vicinity (Figure 3K);
• on plain walls at the upper part of the grain (Figure 3A), which represent the backside of nanofiber-bundles and therefore most likely film material, oval forms (~500 nm at the long axes) with included PGM nanoparticles occur, resembling observations by [21] in experiments with PGE reducing bacteria (Figure 3L).

3.1.2. X-ray Diffraction (XRD)

The same grain as shown in Figure 3A, revealing metallic luster under the stereomicroscope (Figure 4A), was studied using a single-crystal X-ray diffractometer. The obtained diffraction pattern displayed characteristic concentric, well defined, and homogeneous Debye rings, indicating that the grain is constituted by a randomly oriented polycrystalline assemblage (Figure 4B). Integration of the intensity data at constant steps of 2θ gives a conventional one dimensional powder diffraction pattern (Figure 4C).

A comparison with literature data for chemically related mineral phases (Os-group minerals) revealed that the fibrous PGM has rather identical X-ray line intensities and observed d-spacings as ruthenian hexaferrum [20] (

Table 1. Powder X-ray data for the fibrous platinum-group mineral (PGM) shown in Figure 3A and comparison with chemically related phases.

Fibrous PGM			Ruthenian Hexaferrum 1			Hexaferrum (PDF 54-0704)			Ruthenium (PDF 00-06-0663)			Osmium (PDF 00-041-0601)
Imeas	dmeas(Å)	hkl	Imeas	dmeas(Å)	hkl	Imeas	dmeas(Å)	hkl	Imeas	dmeas(Å)	hkl	Imeas	dmeas(Å)	hkl
20	2.3097	100	20	2.3068	100	50	2.28	100	40	2.343	100	80	2.363	100
25	2.1181	002	20	2.1250	002	60	2.10	002	35	2.142	002	30	2.166	002
100	2.0279	101	100	2.0274	101	100	2.006	101	100	2.056	101	100	2.071	101
30	1.5611	102	25	1.5629	102	30	1.549	102	25	1.5808	102	40	1.594	102
35	1.3335	110	40	1.3318	110	30	1.316	110	25	1.3530	110	60	1.364	110
40	1.2047	103	50	1.2072	103	30	1.195	103	25	1.2189	103	20	1.232	103
			10	1.1534	200				6	1.1715	200	10	1.180	200
50	1.1285	112	60	1.1285	112	20	1.118	112	25	1.1434	112	50	1.153	112
35	1.1142	201	40	1.1131	201	20	1.108	201	20	1.1299	201	40	1.039	201
									4	1.0705	004	1	1.080	004
									5	1.0278	202	10	1.035	202
									6	0.9738	104	5	0.9835	104
									16	0.9056	203	40	0.9135	203
									6	0.8857	210	10	0.8929	210
									25	0.8673	211	50	0.8737	211
									18	0.8395	114	20	0.8472	114
									10	0.8185	212	20	0.8252	212
									16	0.8043	105	20	0.8123	105
												5	0.7974	204
												10	0.7866	300

¹ [20].

). On this basis, the X-ray powder pattern for the fibrous PGM was indexed, leading to the refined unit-cell dimensions: a 2.6670 (13) Å, c 4.2361 (18) Å, V: 26.095 (27) ų, Z = 2 (

Table 2. Comparative data for chemically related phases including the fibrous PGM.

	Fibrous PGM	Ruthenian hexaferrum 1	Hexaferrum 2	Ruthenium 3	Osmium 4	Garutiite 5
Chem. Formula	(Ru,Os,Ir,Fe,Si,Al,Mn)	Ru0.4(Os,Ir)0.1Fe0.5	(Fe,Os,Ru,Ir)	(Ru,Ir,Os)	(Os,Ir,Ru)	(Ni,Fe,Ir)
Crystal System	Hexagonal	Hexagonal	Hexagonal	Hexagonal	Hexagonal	Hexagonal
Group Unit cell	P63/mmc	P63/mmc	P63/mmc	P63/mmc	P63/mmc	P63/mmc
a	2.6670 (13)	2.664 (1)	2.64 (1)	2726	2726	2.6939 (5)
c (Å)	4.2361 (18)	4.250 (2)	4.20 (2)	4326	4326	4.2732 (6)
V (Å3)	26.095 (27)	26.12 (3)	25.35	27.84	27.84	26.86 (1)
Z	2	2	2	2	2	2

¹ [20]; ² [22]; ³ [23]; ⁴ [24]; ⁵ [25].

).

3.1.3. Electron Microprobe Analysis (EMPA)

In continuation, the same grain as shown in Figure 3A was included in epoxy and polished for quantitative analyses as well as for element mappings. Polishing of the fibrous PGM led to a general loss of textures, providing evidence that observed complex textures occur exclusively associated with the surface of fibrous PGM. BSE images of the polished fibrous PGM reveal rather homogenous and bright zones, which are crosscut by a slightly darker, Si-bearing belt of varying thickness (Figure 5A). A close-up image of the Si-bearing belt displays the presence of PGE-bearing nanofibers (Figure 5B).

EMP analyses of four points (indicated in Figure 5A) are given in

Table 3. Composition of the fibrous PGM analyzed by electron microprobe (EMP).

wt %
	S	As	Os	Ir	Ru	Rh	Pt	Pd	Fe	Ni	Cu	Co	Si	Al	Mg	Sb	Mn	Total
1	0.04	0.15	17.95	5.32	42.96	bdl	bdl	bdl	16.64	0.33	0.09	0.13	0.54	0.62	0.05	bdl	0.59	85.54
2	0.12	0.15	17.78	5.04	40.94	0.12	bdl	bdl	11.36	0.17	0.09	0.07	0.82	0.44	0.03	0.15	0.86	78.14
3	0.06	0.10	16.34	7.78	43.03	bdl	bdl	bdl	14.59	0.29	0.06	0.14	0.47	0.59	0.06	bdl	0.76	84.29
4	0.03	0.09	17.31	7.81	41.56	bdl	bdl	bdl	16.50	0.36	0.10	0.10	0.47	0.60	0.04	bdl	0.58	85.55
at %
	S	As	Os	Ir	Ru	Rh	Pt	Pd	Fe	Ni	Cu	Co	Si	Al	Mg	Sb	Mn
1	0.14	0.22	10.33	3.03	46.54	0.00	0.00	0.00	32.63	0.62	0.16	0.25	2.11	2.50	0.23	0.00	1.17
2	0.47	0.25	11.62	3.26	50.35	0.14	0.00	0.00	25.29	0.35	0.18	0.15	3.63	2.05	0.16	0.15	1.94
3	0.20	0.15	9.76	4.60	48.38	0.00	0.00	0.00	29.69	0.56	0.10	0.28	1.92	2.49	0.29	0.00	1.57
4	0.10	0.13	10.10	4.51	45.63	0.00	0.00	0.00	32.79	0.69	0.17	0.18	1.85	2.48	0.19	0.00	1.18

bdl = below detection limit.

and confirm the dominance of Ru, Os, Fe, and Ir relative to other elements including trace amounts (<1 wt %) of Mn, Si, Al, and Ni. Low totals (<85.55 wt %) are mainly attributed to the fine-grained nature of the grain and maybe also to the possible occurrence of O or OH within the nanofibers. Element mappings of the area indicated in Figure 5A confirm the above-mentioned dominance of Fe-rich, Ru-Os-Ir compositions (Figure 5C). However, within the Si-rich area, lower Fe and Ni contents are observed, Os reveals an elongated zone of slightly higher contents, whereas Ru does not show visible compositional variations (Figure 5C).

4. Discussion

The nature and origin of fibrous PGM found in the Loma Larga ore deposit are enigmatic. Radial-fibrous internal textures of secondary PGM derived from the in situ alteration of magmatic laurite at low temperatures were reported from ophiolite-related chromitite samples from Greece [26], and similar secondary grains were also described by [27] from Turkish ophiolites. The latter authors demonstrated that dark zones in BSE images contain significant contents of Si and Mg (up to 9 and 10 at %, respectively), which accounted for sub-microscopic particles of chlorite or serpentine. Such secondary PGM grains with intimate intergrowths of Mg-silicates, believed to form during stages of serpentinization, occur in the study area ([8] and reference therein).

Recent studies have suggested that these Mg-silicates are not stable at higher levels of the Ni-laterite profile (close to the Mg-discontinuity) and are replaced by secondary Fe oxide(s) [20]. The observation of subsequent Fe-incorporation into secondary Ru-Os-Ir alloys via abiotic and/or biological processes has been used as an evidence for a supergene origin of ruthenian hexaferrum found in Ni-laterites from the Dominican Republic [20]. Here, the presented XRD data of one characteristic fibrous PGM with an isometric morphology suggest that such a PGM transformation from primary laurite toward ruthenian hexaferrum has occurred (Figure 3A; Table 1 and Table 2). However, PGE-bearing nanofibers have not been observed in ruthenian hexaferrum grains from the study area before.

Complex textures such as PGM nanoparticles within film material (Figure 3I,J), as well as ragged morphologies of PGM nanoparticles resembling sponge spicules and an Ir-rich accumulation with a rather irregular shape (Figure 3K), point to continuous in situ neoformation on the surface of ruthenian hexaferrum grains (Figure 3). Unfortunately, the nature of PGE-bearing nanofibers could not be determined in the present study and more analytical work is necessary to understand how associated PGM nanoparticles are formed. However, considering a starting material of secondary Ru-Os-Ir alloy hosting sub-microscopic fibrous serpentine minerals, it can be speculated that (bio-)weathering of these incorporated Mg-silicate remnants drives (i) the transformation of fibrous Mg-silicates into PGE-bearing nanofibers and (ii) the formation of PGM nanoparticles of different morphologies on the surface of the grain (Figure 3).

5. Conclusions

The PGM-rich “floating chromitite” found within the highest levels of the Loma Larga ore deposit is a suitable natural laboratory which can provide important new insights helping (i) to explain PGE mobilization in the surface environment; (ii) to understand transformation processes of hypogene PGM related to supergene (bio-)weathering and (iii) to find convincing evidence for supergene PGM neoformation and processes involved.