Next Article in Journal
Complex AC Magnetic Susceptibility as a Tool for Exploring Nonlinear Magnetic Phenomena and Pinning Properties in Superconductors
Previous Article in Journal
Bio-Producing Bacterial Cellulose Filaments through Co-Designing with Biological Characteristics
 
 
Search for Articles:
Title / Keyword
Author / Affiliation / Email
Journal
Article Type
 
 
Advanced Search
 
Section
Special Issue
Volume
Issue
Number
Page
 
Journals
Materials
Volume 16
Issue 14
10.3390/ma16144894
materials-logo
Submit to this Journal Review for this Journal Propose a Special Issue
► Article Menu

Article Menu

share Share announcement Help format_quote Cite question_answer Discuss in SciProfiles thumb_up
...
Endorse textsms
...
Comment
first_page
settings
Order Article Reprints
Font Type:
Arial Georgia Verdana
Font Size:
Aa Aa Aa
Line Spacing:
Column Width:
Background:
Article

The Optical and Spectroscopic Properties of Fuchsite, Spodumene, and Lepidolite from Northern Scandinavia (Kautokeino, Kaustinen, Kolmozero)

by
Miłosz Huber
1,*,
Daniel M. Kamiński
2 and
Urszula Maciołek
3
1
Department of Geology, Soil Science and Geoinformacy, Faculty of Earth Science and Spatial Management, Maria Curie-Skłodowska University, 2d/107 Kraśnickie Rd., 20-718 Lublin, Poland
2
Faculty of Chemistry, Maria Curie-Skłodowska University, 2/508 Maria Curie-Skłodowska Sq., 20-031 Lublin, Poland
3
Analytical Laboratory, Institute of Chemical Sciences, Faculty of Chemistry, Maria Curie-Skłodowska University, 3/27 Maria Curie-Skłodowska Sq., 20-031 Lublin, Poland
*
Author to whom correspondence should be addressed.
Materials 2023, 16(14), 4894; https://doi.org/10.3390/ma16144894
Submission received: 27 April 2023 / Revised: 3 July 2023 / Accepted: 5 July 2023 / Published: 8 July 2023
Browse Figures
Review Reports Versions Notes

Abstract

:
Li-Ce-Ta (LCT) pegmatites containing lithium mineralization in the form of spodumene and lepidolite, as well as fuchsite, from the regions of northern Scandinavia (N Norway, N Finland, N Russia) were studied. Detailed analyses of the chemical compositions of these minerals were carried out, involving scanning electron microscopy (SEM) with energy-dispersive spectroscopy (EDS), Fourier transform infrared (FTIR) spectroscopy with attenuated total reflectance (ATR), and X-ray photoelectron spectroscopy (XPS) studies. Their crystal structures were confirmed with the X-ray diffraction technique. Studies involving microscopy were also carried out, indicating the optical features of these minerals. Based on the analyses carried out in the studied rocks, the characteristics of these minerals were determined, as well as the crystallization conditions. This research indicates that the N Scandinavian area is prospective and may lead to further discoveries of this type of pegmatite in the studied region.

1. Introduction

In northern Scandinavia, pegmatite veins containing rare lithium and schists with chromium minerals are found in the regions of northern Norway [1], Finland [2], and the Kola Peninsula in Russia [3], among rocks constituting the cratonic basement of the Northern Fennoscandia [4]. These rocks contain minerals such as mica (lepidolite, fuchsite, muscovite) and pyroxene (spodumene), which co-occur with quartz, plagioclase, orthoclase, and several ore minerals: oxides (e.g., columbite, tantalite, cassiterite, sillenite, clarkeite) and sulfides (pyrite, chalcopyrite). Their thickness reaches several meters, and they cut through their metamorphic host rocks [5]. The previous study of these rocks was mainly concerned with analyses for the needs of economic geology [6]. The purpose of this article is a detailed analysis of the mineralogy of these rocks and a discussion of the crystalline structure characteristics of spodumene, lepidolite, and fuchsite.

2. Study Area and Massifs Geology

The northern part of the Scandinavian Peninsula is part of the Fennoscandia (Figure 1). In this region, Archean and Proterozoic rocks are exposed, forming various types of gneisses that constitute the basement of the Baltic Shield [3,7,8,9,10,11,12,13,14]. In the Fennoscandia, numerous intrusions have been found, such as the Tonalite Trondheimite Granodiorites of Murmansk (3.75 Ga) [3] and Jergul (2.97 Ga) [15], Patchenvarek anorthosites (2.92 Ga) [16], and enderbites (2.83 Ga) [9], with layered Paleoproterozoic intrusions in Monchegorsk (2.50 Ga) [17]. These rocks metamorphosed in the amphibolite and granulite facies [18,19]. Alkaline metavolcanic rocks and granitoid intrusions occur in the vicinity of the discussed pegmatite sites [20,21,22]. This is the case in the Kaustinen and Kolmozero areas, where numerous pegmatite veins can be found in these rocks [23,24,25,26]. In the Kaustinen area (Finland) and the Kolmozero area, there are pegmatite veins with lithium–cesium–tantalum mineralization (LCT), which are up to several meters thick and 100 m or more in length. In the Kautokeino area, schists containing chromic mica are visible. The age of Kautokeino and Kaustinen rocks spans the range of 1.9–1.8 Ga [27,28,29]. These rocks are exposed on the surface or covered by Pleistocene sediments [30,31]. In these locations, high-relief landscapes have developed [32,33,34,35,36].

3. Materials and Methods

Rock samples were collected between 2018 and 2022. During this period, the discussed massifs were visited, and the geological documentation of the samples was also carried out. In Scandinavia, rock samples were taken from the site of their occurrence. The selected rocks were targeted for thin-section preparations. Subsequently, the minerals were subjected to analyses using a Leica DM2500P (Heerbrugg, Switzerland) polarizing optical microscope [38,39,40,41] and with a scanning electron microscope, a Hitachi SU6600 (Tokyo, Japan), equipped with energy-dispersive spectroscopy (EDS) [42,43]. The samples were analyzed under a low vacuum (10 Pa), 15 kV accelerating voltage, and beam diameter of 0.2 µm. A total of 525 analyses were performed using the microprobe (at Kautokeino, 72; at Kaustinen, 179; and at Kolmozero, 274). The selected minerals were separated and analyzed with single-crystal X-ray diffraction. Data were collected using a Rigaku diffractometer (Tokyo, Japan) [44] with CuKα radiation (λ = 1.54184 Å) at 293 K. Crystallographic refinement and data collection, as well as data reduction and analysis, were performed with a CrysAlisPro v42 [45]. The selected single crystals were mounted on the nylon loop with oil. The structures were determined by applying direct methods using the SHELXS-86 program and refined with SHELXL [46,47] in Olex2 software [48]. Table 1 provides the experimental details for the single crystals’ X-ray measurements. These samples were also examined with the Fourier transform infrared (FTIR) technique [49,50]. The samples were measured using a Nicolet 8700A Thermo Scientific Shimadzu FTIR spectrophotometer (Waltham, MA, USA) equipped with an attenuated total reflectance (ATR) accessory, a Smart Orbit™ diamond ATR QATR-S (Riyadh, Saudi Arabia) (wideband diamond crystal). Every spectrum was obtained from 256 records at a 4 cm−1 resolution ranging from 4000 to 400 cm−1. The elaboration of a spectrum was carried out using the OMNIC program. Optical and microscopic studies were performed at the Department of Geology, Soil Science, and Geoinformation of the Institute of Earth and Environmental Sciences, and crystal chemistry studies were performed at the Department of Crystallochemistry, Faculty of Chemistry, Maria Curie-Skłodowska University, in Lublin. The UHV multi-chamber system (Prevac, Poland) was used to carry out the X-ray photoelectron spectroscopy (XPS) measurements. Molybdenum mounts were used to hold the measured samples. The chamber pressure was 5 × 10−9 mbar during analysis. The mineral surface was excited with X-rays (Al Kα, 1486.6 eV) from a Scienta SAX-100 X-ray source equipped with an XM 650 X-ray monochromator. The hemispherical electron analyzer R 4000 (Scienta, Uppsala, Sweden) operating in sweep mode was used to detect photons arriving from the sample. The energy of the spectra was calibrated using the C1s aliphatic carbon peak, EB = 285 eV. The CasaXPS v2.3.23-PR1 software from Casa Software Ltd. (London, UK) was used to analyze the measured data. The full width at half maximum (FWHM) and relative peak shift were fixed in the fitting process [51,52].

4. Results

4.1. Host Rock Petrology

The examined lithologies are located in the Kolmozero–Voronya Greenstone Belt, Pohjanmaa Schist Belt (Kaustinen Pegmatites), and Kautokeino Greenstone Belt. The LCT pegmatites from the Kolmozero area are located in the Kolmozero–Voronya Greenstone Belt, separating the Murmansk block from the Kola block, composed of mixed metasediments and metavolcanites. These formations are intersected by numerous intrusions of alkaline and acidic rocks. The discussed LCT pegmatites intersect the alkaline rocks of the Patchemvarek anorthosite intrusion. This intrusion is located on the border of the Kolmozero block with the plagiogranites of the Murmansk block [53]. These rocks are in direct contact with biotite gneisses and amphibolites of the Kolmozero–Voronya Belt. There are fine-grained tourmaline-muscovite granites with pegmatite apophyses rich in tourmaline, garnet, and apatite. The studies of Kudrashov et al. [54] indicated that these are pegmatites of hydrothermal–metasomatic origin [55,56].
The Kaustinen pegmatite province is located in Western Finland. It is situated among supracrustal rocks belonging to the Pohjanmaa Schist Belt [57,58]. It is surrounded by the Vaasa granitoid complex to the west and Central Finland granitoides to the east [6]. The Pohjanmaa Schist Belt is composed of micaceous schists and gneisses, along with metavolcanic rocks. These rocks were metamorphosed under the amphibolite facies of 1.89–1.88 Ga [59]. The lithium-rich pegmatites from the Kaustinen province belong to the albite spodumene type according to the classification of Černy and Ercit [55]. They were formed during the metamorphism of the rocks of the Pohjanmaa belt. The pegmatites form a complex of veins cutting the rocks of the Pohjanmaa Käpyaho belt and others [60,61,62,63].
In the region of the Palaeoproterozoic Kautokeino Greenstone Belt, where muscovite-fuchsite and quartz-orthoclase schists are located between the gneissic Ráiseatnu Complex (1868–1828 Ma) to the west and the metaplutonic Jergul Complex to the east (tonalite–trondhjemite–granodiorite–granite plutonic rocks formed between 2975 and 2776 Ma). In the Kautokeino Greenstone Belt, metasedimentary–metavolcanic rocks are present, with numerous mafic intrusions [27]. The Masi Formation in the Archean basement is formed of a quartz-feldspar conglomerate with muscovite interbedding and ore mineralization composed of iron and copper sulfides (pyrite, chalcopyrite). It is intersected by the mafic sills of the Haaskalehto formation (2220 Ma age). [64] Among these formations are the discussed fuchsite-rich rocks, which may have formed as an alteration product of detrital chromite grains [65].

4.1.1. Kautokeino

The paleoproterozoic metamorphic formations classified as the Alta-Kautokeino Greenstone Belt are exposed in the Kautokeino region. Among these formations, there are mica schists [66] containing fuchsite (Figure 2A). This rock is an intense green-pink, characterized by layering resulting from a gneissic, streaky texture. The rock has a grano-lepidoblastic texture and is also characterized by a glomeroblastic, locally diablastic texture. Under an optical microscope, large quartz crystals are visible, forming irregular, hooked aggregates in contact with each other. Opaque minerals, such as pyrite and chalcopyrite, are visible between the muscovite and fuchsite. Close to the quartz crystals, microcline and Na-rich plagioclase are also present, forming leucocratic zones. In the interstices of plagioclase and microcline, small crystals of epidote are encountered. In addition to these zones are areas richer in femic minerals. They are represented by aggregates of biotite, which co-occur with fuchsite to form a streaky structure in the rock. These minerals form aggregates, resulting in interlaced streaks in the discussed rock. Opaque minerals can be observed, and zircon and apatite are woven into the biotite flakes. The detailed results of the phase studies in the micro-area are discussed below.

4.1.2. Kaustinen

In the Kaustinen area, pegmatites with a silicon-gray color, coarse crystalline structure, and compact, disordered texture are exposed among the gneisses. Their age was determined to be 1.79 Ga (U-Pb method) [67]. Under an optical microscope, the quartz crystals form large grains in contact with each other and closely interlocking. The quartz in the studied rock has wavy extinction. Alongside these are large orthoclase crystals adjacent to the quartz (Figure 2B). They are accompanied by much smaller tabular grains of Na-rich plagioclase, often between the orthoclase and quartz. Femic minerals are represented by muscovite forming large clusters of flakes, in the background of which fine zircon crystals are visible. Muscovite crystals are near the pyroxene. Biotite is also visible in the form of small flakes, usually between large pyroxene crystals. The pyroxenes in the discussed rock form large crystals, reaching several centimeters in size. They are represented by spodumene (and hypersthene). The spodumene forms compact crystals with jagged boundaries in which quartz and muscovite are visible. The hypersthene is anhedral. Opaque minerals (columbite-tantalite, sillenite) are visible in the form of small crystals close to the quartz, sometimes also forming solid inclusions, accompanying zircon. The detailed results of the micro-area phase studies are discussed below.

4.1.3. Kolmozero

In the area of the Kola Peninsula between the Kola and Murmansk blocks is the Archean Kolmozero–Voronya Greenstone Belt. Adjacent to the LCT pegmatites are Archean gabbro-anorthosites and granitic rocks. The analyzed pegmatites are dated to 1.90–1.86 Ga [68]. The pegmatites containing spodumene and lepidolite are cream-gray-colored rocks with a coarse crystalline texture and a compact, disorderly texture (Figure 2C). In thin sections, there are large crystals of quartz interlocking with each other. The quartz forms clumped aggregates in the space between the other phases. Alongside these minerals are visible crystals of Na-rich plagioclase. In the described rock, orthoclase, usually reaching a considerable size, is also visible near the other leucocratic minerals. Among the potassium feldspars, microcline usually forms small crystals. Alongside these minerals, flakes of biotite and muscovite can be identified, interspersed among the quartz and plagioclase. Biotite is much less abundant than muscovite, which predominates. In the pegmatites with lepidolite, this mineral accompanies muscovite, forming deformed flake aggregates of varying sizes. Large crystals of spodumene, reaching several centimeters in length, are visible alongside these minerals. They are surrounded by biotite, lepidolite, and plagioclase. In addition, small crystals of opaque minerals are visible near muscovite flakes occurring in interstices of quartz and feldspar. Zircon crystals are also visible within mica flakes. Accessory apatite forms small crystals co-occurring with femic minerals.

4.2. SEM-EDS Analyses

In the case of the Kautokeino rocks, the examined trioctahedral mica can mainly be classified as annite and siderophyllite [69,70,71] (Figure 3). These micas co-occur with fuchsite-forming overgrowths (Table A1).
Dioctahedral micas are represented by muscovite with fuchsite and lepidolite (Table A1). Muscovite usually shows a low Na+ content (up to 5 wt.%). In the rocks from Kautokeino, in addition to muscovite, it was found that all the chromic micas examined were fuchsites. Some of the examined chromium micas have a composition characteristic of paragonite (Figure 4). In addition, an admixture of clinozoisite and epidote (mainly in the Kaustinen pegmatites, Table A1) was found in the discussed rocks.
The examined pyroxenes are mainly represented by spodumene, with an Na content of up to 5 wt.%. In the examined samples, spodumene dominates, while admixtures of jade particles occur in small amounts (Table A2). Hypersthene was also found in the latter.
The accompanying leucocratic minerals are represented by quartz, usually with an admixture of up to 4% of aluminum oxide. The plagioclase is represented by albite with a small admixture of oligoclase (4%), as well as andesine (6%) and labradorite (6%). The labradorite is an admixture found mainly in the pegmatites from Kaustinen. Accessory minerals are represented by zircon and apatite. Zircon crystals are mainly found in close association with muscovite flakes. Phosphates are represented mainly by a variety of hydroxyapatites, with approximately 3% carboxy apatite and 2% fluoroapatite.
In addition, opaque minerals were found in the exanimated rocks. In the Kolmozero pegmatite, columbite ((Fe,Mn)Nb2O6) forms euhedral crystals, usually close to spodumene, quartz, and plagioclase [2]. Along with columbite, tantalite is visible. Tantalite ((Fe, Mn)Ta2O6) is replaced with bixbyite in the oxidation zone. Magnetite was also found. The sample also presents clarkeite (Na,Ca,Pb)2(UO2)2(O,OH)3 in the vicinity of apatite and sillenite Bi12SiO in the vicinity of femic minerals.
The opaque minerals in the investigated rocks are represented by multiple phases. In the case of the schists from Kautokeino, the opaque phases include cassiterite and pyrite. In the pegmatite from Kaustinen, the opaque phases include magnetite and ilmenite, accompanied by titanite. Trace or minor cassiterite was also found, as well as galena, sphalerite, and chalcopyrite, which, together with barite, form disseminations. Columbite and tantalite were also found, although in smaller amounts relative to the Kolmozero pegmatite.

4.3. Optical Properties of the Discussed Minerals

Spodumene forms large xenomorphic crystals, with sizes reaching several cm. This mineral usually has a light green color. Sometimes, it resembles plagioclase, which, when undergoing sericitization, also has a slight gray-green tint. In the microscopic image, it sometimes forms a diablastic texture according to the (100) miller index. It is usually found near micas represented by muscovite, lepidolite, and, less often, biotite (Figure 5). The schist is highly visible. Small admixtures of Fe-oxides can be seen along the schistosity of the rock. The straw color on the thin section has a clear, positive relief, with darkening extinction.
Lepidolite forms large lamellar aggregates, usually colored pearly pink. Macroscopically, this mineral forms flakes reaching up to 1 cm in size. It is usually quite visible in the rock due to its coloration and luster. In the microscopic image, it forms numerous adhesions of varying sizes. It is present with spodumene, near plagioclase and quartz. Between the mica flakes, rutile be observed. In the thin section, it is colorless, with a faint, negative relief. Under polarized light, it shows second-order interference colors, optically resembling biotite (Figure 6). Our microscopic observations of lepidolite showed some deformation of its lamellae due to dynamic processes.
Fuchsite forms fine, scaly accumulations, the size of which reaches several millimeters. Macroscopically, it is colored green and has a pearly luster. It is highly visible against the background of biotite and feldspar in the investigated rocks. Fine zircon grains are visible in the background of the fuchsite aggregates (Figure 7). In the microscopic image, they form polysynthetic adhesions with muscovite occurring between quartz and orthoclase. The sample shows pleochroism with a delicate greenish (β)-bluish (α) coloration. Under polarized light, it shows intense second-order interference colors, making it similar to muscovite.

4.4. Spectroscopic Properties of the Minerals under Investigation

Infrared studies carried out for spodumene showed some small oscillations at a wavelength of 3612 cm−1, which can be explained by the influence of water. Values in the vicinity of 1005 cm−1 may be related to stretching vibrations for silicon-oxygen tetrahedra [74]. Vibrations in the vicinity of 779 cm−1 can be correlated with Si-O stretching vibrations. Similarly, for lengths of 647 cm−1 to 448 cm−1, non-bridging bending vibrations for O-Si-O can be found with the participation of aluminum, which can also substitute the spodumene structure in an octahedral position (Figure 8). The latter oscillations are also affected by the position of lithium (448 cm−1), which, combined with oxygen, contributes to their modification. Through a comparison with the crystals of jadeite, it can be seen that substitution with Na cation with an ionic radius of 186 pm [75] in the M6 position shifts these vibrations to 455 cm−1. In comparison, magnesium enstatite, in the M6 position, has 447 cm−1 vibrations (enstatite [76] and bronzite [77]). Lithium is a much lighter element than sodium, as its molar mass is 6.941 (for sodium it is 22.989 [51,78] close parenthesis g/mol) and its ionic radius is 152 pm. The full width at half maximum of the 455 cm−1 vibrations suggests that these vibrations are partly derived from the sodium at this position.
In the case of the study micas (fuchsite and lepidolite, Figure 9), comparisons were made with muscovite [79]. In both cases, the absorbance characteristic of stretching vibrations of the OH groups in the vicinity of 3625 and 3608 cm−1 is visible (Figure 9). These are determined by vibrations between ions located in octahedral groups and their interaction with water [80,81]. These differences become apparent depending on the nature of the ions in the analyzed minerals (Li in lepidolite, Cr in fuchsite). There is also a slight increase in absorbance in the region of 1621 cm−1, which is more pronounced for lepidolite. Another oscillation in the region of 970 cm−1 and 960 cm−1 is related to deformations produced through connection between aluminum and the OH group in these minerals [82]. In the region of 796–799 cm−1, there are Si-O deformations in both mica, and those at 750 cm−1 are characteristic of O-Al-O stretching vibrations in the tetrahedral position. Similarly, in lepidolite, a band in the 523 cm−1 region was found that is characteristic of Al(Li)-O-Si vibrations. The last absorbance in the 464 cm−1 and 441 cm−1 is associated with vibrations in the Si-O-Si group [82].

4.5. Single Crystals and XPS Analysis Results

4.5.1. Fuchsite

The studied fuchsite crystals, like all minerals in this group, contain chromium [82,83]. This is visible in the results of the diffraction measurements for the monocrystals and XPS. The X-ray data indicate that the studied fuchsite crystal contains 0.4 ions of this element per elemental cell of the crystal in the Cr-Al layer (Figure 7). It is worth noting the staggered position of both the Al3+ and Cr3+ ions at a distance of 0.12(1) Å (Figure 10 and Figure 11). This spread is due to the difference in the ionic radii of these two elements. The diffraction data show that only one position in the lattice, where the Al3+ ions are present, is occupied by additional Cr3+ ions, while the other position is 100% occupied by Al3+ ions (Figure 10). In addition, the layer has a free space filled, in this case, with water or an OH- group in the amount of 0.1 molecule/ion per elementary cell. In this case, the OH- group can compensate for the positive charge of the cations. In the Si-K layer, no admixture of other ions is observed at the detection level of this technique. All cell parameters and compositions are within the typical limits for this type of mineral. The thermal vibration ellipsoids observed in the experiment at 296 K had small thermal vibration amplitudes of Uiso 0.02–0.03 (Figure 11). This indicates strong interactions between ions in the lattice.

4.5.2. Lepidolite

Diffraction studies of the lepidolite yielded its structure [84,85,86,87]. They confirmed that it is a mineral from the silicate cluster, classified as lithium micas with an admixture of Fe2+ or Mn2+ in one position. However, unequivocally determining which ion is in this position is impossible with this technique. Positively charged Li-K ions reside in the space between the negatively charged aluminosilicate layers. In addition, OH− group or water molecules in the amount of 0.1 per elementary cell of the crystal can be found in this crystal net space (Figure 12). In an elementary cell, there are three such layers in the direction of b. A richer atomic composition is provided by the data obtained through XPS measurements. This technique is more sensitive to heavier elements and allows for the unambiguous determination of their type. In contrast, lithium ions, which are difficult to determine via XPS, are visible in the monocrystalline structure. The ratio of K/Li ions is 2:1 in the structure. A close fit of the X-ray data with the model indicates that the lattice occupancy of Al3+ ions is 90 ± 5%. This indicates that aluminum shares this position with lighter ions, e.g., Mg and Na. However, (Figure 10), in this case, it is necessary to properly balance the charges in the lattice. Also, the occupancy of the Li position is less than 100%, which, in this case, may indicate the partial substitution of this position with water molecules. The low values of the Qizo parameters (0.02–0.03) for atoms at 296 K indicate strong interactions between atoms (Figure 13).

4.5.3. Spodumene

This is another studied mineral from the silicate cluster containing lithium [88,89,90,91]. In this case, the structural studies of the crystals indicated that the stoichiometric contents of Li and Al in the crystal lattice are within the error margin. Attempts to fit a crystal lattice model with a free occupancy parameter for Li indicated that the modeled electron density at this site is slightly higher than 1, at 1.06 (Figure 14). This may indicate a small content of a heavier element at this site, e.g., sodium, as suggested by the XPS and FTIR measurements. In the studied monocrystals, other ions were not visible in the crystal lattice (Figure 12). In the spodumene, silicate ions connect adjacent layers, so there is not enough space for additional ions between them, which explains the composition of this mineral. The compact lattice structure also contributes to strong interactions between atoms, which, in turn, manifests itself in the lowest Qizo values of all the minerals presented (0.006–0.017) and its highest relative hardness (Figure 15).

5. Discussion

The minerals included in rocks found in northern Scandinavia (within Norway, Finland, and Russia) [92,93,94,95,96,97] were studied. These are exposed in many places in the area under discussion. Due to their mineralization, they may be significant in terms of raw material development, although the relatively small size of these pegmatite veins makes their profitability highly dependent on raw material prices. The mineralization of these pegmatites is the result of the crystallization of residual melts, which contain many incompatible elements [55,98]. On the other hand, the presence of some elements is related to the chemistry of the host rocks. This is particularly evident in the case of fuchsite, in which the presence of chromium may be related to specific rock types. Such small occurrences of fuchsite have been found by the authors in vein rocks in the Monchepluton area (Russia). Lepidolite and spodumene, on the other hand, show small admixtures of sodium, manganese, and iron, which may also be related to the rocks near these pegmatites. This was confirmed by both micro-area studies and monocrystal and XPS analyses. The presence of water in the mica and even in the spodumene (found using FTIR) confirms the hydrothermal nature of the association between these minerals [99,100]. Their nature in the discussed rocks varies. Optical studies indicated that the spodumene in the analyzed pegmatites usually has hypidiomorphic crystals, which may indicate crystallization as an early silicate phase. The presence of small admixtures of sodium may indicate that the mineral originally formed at a great depth, where higher pressures prevail, and then tectonically dislocated with solutions to its present site of occurrence, where it was hydrothermally altered [53,54,57]. On the other hand, aggregates of fuchsite and lepidolite tend to be secondary, co-occurring with other micas and occupying a position in the interstices of existing minerals; moreover, lepidolite can probably be a secondary mineral, formed at the expense of spodumene, as evidenced by our observations of this mineral in pegmatites. It is noteworthy that in addition to these minerals, there are many accessory phases, such as apatite and zircon. Alongside these, opaque minerals are present in large numbers. The presence of tin minerals points to the granitoid association as the source material for the origin of the schists [101,102]. In the case of the LCT pegmatites found in the Kaustinen area, these include, in addition to the aforementioned cassiterite and barite, magnetite, ilmenite, and titanite, as well as galena, sphalerite, and chalcopyrite. The presence of these minerals may also be related to the granitoid products and the action of hydrothermal products. The mineralization of Kolmozero pegmatites is also associated with the action of hydrothermal formations. This is evidenced by the mutual relations of rock-forming minerals with the observed bixbite, clarkeite, and sillenite, which are also accompanied by magnetite. Columbite and tantalite were also found in the LCT pegmatites.

6. Conclusions

The studied minerals are from selected rocks that are exposed in northern Scandinavia. The studied mineralization indicates the hydrothermal nature of these components. The studied minerals, including spodumene, lepidolite, and fuchsite, were formed after residual crystallization. The small admixtures of sodium present in the spodumene may indicate that it was formed under high pressures and, together with the melt, reached its present location, where it was altered due to pressure from hydrothermal fluids. The occurring lepidolite crystallized at a later stage, at the expense of spodumene, as evidenced by the structure of this mineral in the rock and by association (the occurrence of relics of spodumene in the vicinity of lepidolite). Fuchsite, like lepidolite, crystallized in the final stage, co-occurring with muscovite and biotite. The presence of chromium ions in this fuchsite is probably due to the occurrence of chromium-containing rocks in the vicinity of the formation of intrusions from the residual melts in which the studied rocks crystallized. The presence of accessory and opaque minerals also attests to the granitoid association of the original solutions. The minerals present may be of economic importance. Thorough research may contribute to the discovery of new locations of this type of pegmatite in the discussed area.

Author Contributions

Conceptualization, M.H. and D.M.K.; methodology, M.H., D.M.K. and U.M.; validation, M.H., D.M.K. and U.M.; formal analysis, M.H.; investigation, resources, M.H.; data curation, M.H. and D.M.K.; writing—original draft preparation, M.H.; writing—review and editing, D.M.K.; visualization, M.H. and D.M.K. All authors have read and agreed to the published version of the manuscript.

Funding

We would like to thank EcoTech Complex in Lublin for providing the equipment for the X-ray diffraction measurements.

Conflicts of Interest

The authors declare no conflict of interest.

Appendix A

Table
Table A1. Results of the SEM-EDS analysis of the mica minerals (wt.%).
Table A1. Results of the SEM-EDS analysis of the mica minerals (wt.%).
Point *OFNaMgAlSiKTiCrFeMineral
Kautokeino(2)_pt938.47 5.786.1328.909.29 6.82biotite
Kautokeino(3)_pt240.41 1.2613.5030.6710.79 1.20biotite
Kautokeino(3)_pt339.56 1.1213.8530.6510.80 1.01biotite
Kautokeino(3)_pt1039.30 6.036.9433.309.03 3.66biotite
Kautokeino(3)_pt1138.96 5.567.5632.419.13 4.77biotite
Kautokeino(4)_pt739.52 6.697.1030.4410.85 3.54biotite
Kautokeino(4)_pt838.51 6.976.5730.1311.49 4.41biotite
Kautokeino(4)_pt938.67 7.138.0528.5610.28 5.04biotite
Kautokeino(4)_pt1037.87 7.317.6829.729.70 6.34biotite
Kautokeino(4)_pt1138.60 6.618.0728.2310.152.34 4.05biotite
Kautokeino(4)_pt1338.19 6.577.5929.199.72 7.07biotite
Kautokeino(2)_pt831.59 5.035.0724.086.89 4.6613.44fuchsite
Kautokeino(3)_pt139.04 0.9512.1529.829.90 5.99 fuchsite
Kautokeino(3)_pt438.06 0.9011.7428.5010.21 7.75 fuchsite
Kautokeino(3)_pt537.84 1.1012.4628.4610.10 6.51 fuchsite
Kautokeino(3)_pt638.17 1.1012.6629.359.94 5.9 fuchsite
Kautokeino(3)_pt737.021.31 1.0112.6526.9110.73 6.78 fuchsite
Kautokeino(3)_pt837.61 1.2012.4129.7710.08 6.36 fuchsite
Kautokeino(3)_pt938.06 1.0712.1331.389.01 6 fuchsite
Kautokeino(3)_pt1639.94 1.7746.382.21 6.43 fuchsite
Kautokeino(4)_pt1236.05 5.946.7024.059.142.133.9610.16fuchsite
Kautokeino(4)_pt1434.89 6.636.2726.517.25 5.9311.10fuchsite
Kautokeino(4)_pt1535.44 5.676.1827.838.58 5.429.02fuchsite
Kautokeino(4)_pt1636.18 2.5410.9427.549.90 5.146.18fuchsite
Kautokeino(5)_pt1236.14 0.73 8.6434.5813.82 4.5 fuchsite
Kautokeino(6)_pt437.66 0.61 7.7535.1612.63 4.54 fuchsite
Kautokeino(3)_pt1742.47 1.9950.462.88 muscovite
Kautokeino(3)_pt1842.54 1.8551.382.56 muscovite
Kolmozero(1)_pt139.02 0.83 17.3827.639.12 0.44muscovite
Kolmozero(1)_pt237.31 2.10 9.6834.9011.99 muscovite
Kolmozero(3)_pt137.17 15.6325.2511.08 muscovite
Kolmozero(3)_pt238.20 0.83 17.3923.4711.12 muscovite
Kolmozero(3)_pt338.89 0.72 18.1324.7712.08 muscovite
Kolmozero(3)_pt439.11 0.98 18.5724.7711.22 muscovite
Kolmozero(3)_pt539.22 0.85 18.0125.5511.69 muscovite
Kolmozero(3)_pt638.21 0.73 19.4326.5610.50 muscovite
Kolmozero(3)_pt739.77 18.7626.8410.23 muscovite
Kolmozero(4)_pt238.25 17.1726.6811.62 muscovite
Kolmozero(4)_pt338.44 17.6824.7810.67 muscovite
Kolmozero(5)_pt437.23 9.3932.7913.13 muscovite
Kolmozero(8)_pt939.78 15.2231.539.76 muscovite
Kolmozero(8)_pt1039.89 16.6131.139.80 muscovite
Kolmozero(8)_pt1141.80 9.4039.636.02 muscovite
Kaustinen(3)_pt139.27 13.1829.668.86 muscovite
Kaustinen(3)_pt441.17 16.2130.537.95 muscovite
Kaustinen(3)_pt540.52 16.3829.329.09 muscovite
Kaustinen(3)_pt641.54 0.47 17.4030.997.62 muscovite
Kaustinen(4)_pt239.23 13.4829.108.63 muscovite
Kaustinen(4)_pt339.95 14.0227.829.82 muscovite
Kaustinen(4)_pt440.15 13.1730.729.08 muscovite
Kaustinen(4)_pt540.33 14.3529.988.70 muscovite
Kaustinen2(2)_pt336.97 1.55 10.2532.1717.82 muscovite
Kaustinen2(2)_pt437.19 1.04 10.4732.3117.49 muscovite
Kolmozero(18)_pt140.37 18.8128.0111.61 muscovite
Kolmozero(18)_pt239.06 0.47 19.4827.3210.97 muscovite
Kolmozero(18)_pt339.58 19.9126.7711.55 muscovite
Kolmozero(18)_pt439.57 19.3726.4412.23 muscovite
Kolmozero(18)_pt539.48 20.4726.0411.26 muscovite
Kolmozero(18)_pt637.54 0.68 18.2025.4710.24 muscovite
Kolmozero(20)_pt540.13 15.5731.968.82 muscovite
Kolmozero(20)_pt640.33 15.6530.288.94 muscovite
Kolmozero(20)_pt839.69 0.1815.9430.0610.06 muscovite
Kaustinen(10)_pt841.26 17.8726.387.57 muscovite
Kaustinen(10)_pt941.38 16.2825.387.66 2.67 muscovite
Kolmozero2(4)_pt132.042.290.29 12.9623.217.85 lepidolite
Kolmozero2(4)_pt233.983.32 13.5724.758.64 lepidolite
Kolmozero2(4)_pt334.253.140.37 13.6425.038.52 lepidolite
Kolmozero2(4)_pt434.652.890.35 14.1125.938.68 lepidolite
Kolmozero2(4)_pt534.632.930.590.1214.4226.268.58 lepidolite
Kolmozero2(4)_pt635.523.76 15.2529.769.38 lepidolite
Kolmozero2(4)_pt735.473.340.49 15.1729.8210.43 lepidolite
Kolmozero2(4)_pt835.303.090.52 14.6329.409.66 lepidolite
Kolmozero2(4)_pt933.582.990.48 14.5127.449.17 lepidolite
Kolmozero2(4)_pt1034.993.47 0.4414.0527.388.28 lepidolite
Kolmozero2(4)_pt1133.490.220.62 10.5731.0012.48 lepidolite
Kolmozero2(4)_pt1232.110.510.44 10.5331.6113.20 lepidolite
Kolmozero2(4)_pt1334.310.510.30 10.8131.9612.31 lepidolite
Kolmozero2(4)_pt1433.980.68 11.2132.5913.15 lepidolite
Kolmozero2(4)_pt1535.653.42 14.9929.249.89 lepidolite
Kolmozero2(5)_pt133.592.55 13.5425.858.51 lepidolite
Kolmozero2(5)_pt234.153.54 13.2326.379.10 lepidolite
Kolmozero2(5)_pt333.723.680.30 14.2428.208.37 lepidolite
Kolmozero2(5)_pt434.713.62 14.5727.899.68 lepidolite
Kolmozero2(5)_pt534.305.37 11.9330.889.34 lepidolite
Kolmozero2(5)_pt634.420.92 11.4932.6813.07 lepidolite
Kolmozero2(5)_pt734.200.690.32 11.4432.6614.01 lepidolite
Kolmozero2(5)_pt834.693.76 15.6629.8610.63 lepidolite
Kolmozero2(5)_pt935.973.36 15.3530.0210.31 lepidolite
Kolmozero2(5)_pt1036.153.60 15.8330.3610.08 lepidolite
Kolmozero2(5)_pt1135.813.15 15.7430.5110.43 lepidolite
Kolmozero2(6)_pt441.350.520.83 15.9833.983.64 lepidolite
Kolmozero2(2)_pt536.38 0.71 12.9434.8314.26 lepidolite
Kolmozero2(1)_pt737.96 0.34 12.1535.6512.84 lepidolite
* In this analysis, there is no possibility of lithium indication.
Table
Table A2. Results of the SEM-EDS of spodumene (wt.%).
Table A2. Results of the SEM-EDS of spodumene (wt.%).
Point *COFNaMgAlSiMineral
Kaustinen(3)_pt142.6744.24 15.8237.26spodumene
Kaustinen(3)_pt152.8444.21 15.7937.15spodumene
Kaustinen(3)_pt162.4745.12 15.8636.55spodumene
Kolmozero(2)_pt16.7239.68 6.48 11.1735.95spodumene
Kolmozero(2)_pt25.7540.09 6.67 11.5335.96spodumene
Kolmozero(2)_pt42.8240.45 7.15 11.7937.78spodumene
Kolmozero(2)_pt53.4939.73 7.17 11.7437.86spodumene
Kolmozero(3)_pt82.6539.69 7.09 11.3537.51spodumene
Kolmozero(3)_pt93.7639.19 7.51 11.7236.94spodumene
Kolmozero(3)_pt103.1140.44 6.20 11.3437.27spodumene
Kolmozero(3)_pt113.5942.46 1.52 14.9236.26spodumene
Kolmozero(3)_pt124.3941.44 4.15 11.1838.84spodumene
Kolmozero(3)_pt135.0140.19 1.22 9.7937.67spodumene
Kolmozero(5)_pt34.8043.59 14.0737.54spodumene
Kolmozero(7)_pt47.6842.37 0.66 14.0235.27spodumene
Kolmozero(7)_pt55.8043.61 14.0736.52spodumene
Kolmozero(8)_pt114.4240.36 12.5732.66spodumene
Kolmozero(8)_pt216.2441.07 12.9429.75spodumene
Kolmozero(8)_pt66.9239.78 1.1952.11spodumene
Kolmozero(8)_pt74.7041.89 1.1752.24spodumene
Kolmozero(8)_pt82.6442.38 1.1353.84spodumene
Kolmozero(8)_pt122.6543.13 2.0152.21spodumene
Kolmozero(9)_pt117.2341.85 12.1028.81spodumene
Kolmozero(9)_pt210.6840.60 4.01 11.5133.19spodumene
Kolmozero(9)_pt39.6142.79 4.7142.89spodumene
Kolmozero(9)_pt47.7144.53 11.7536.01spodumene
Kolmozero(9)_pt555.0233.59 2.189.21spodumene
Kolmozero(11)_pt74.8942.72 1.77 14.7935.83spodumene
Kolmozero(11)_pt84.1640.72 6.32 11.1837.62spodumene
Kolmozero(11)_pt94.3041.67 7.35 11.3735.31spodumene
Kolmozero(11)_pt103.3041.02 7.36 11.5036.82spodumene
Kolmozero(11)_pt113.1539.99 8.01 11.2137.64spodumene
Kolmozero(12)_pt156.4739.50 7.58 10.9935.46spodumene
Kolmozero(12)_pt166.1639.91 7.36 11.3335.24spodumene
Kolmozero(12)_pt175.8939.88 7.46 10.2436.53spodumene
Kolmozero(13)_pt13.2540.25 8.04 10.3638.10spodumene
Kolmozero(14)_pt129.9241.91 13.1035.07spodumene
Kolmozero(14)_pt137.6140.92 0.55 2.3348.58spodumene
Kolmozero(14)_pt147.0841.82 1.8249.28spodumene
Kolmozero(16)_pt116.2640.72 13.2929.73spodumene
Kolmozero(16)_pt222.4538.80 10.9527.79spodumene
Kolmozero(16)_pt314.2942.10 13.2230.39spodumene
Kolmozero(16)_pt415.0840.91 12.6131.40spodumene
Kolmozero(16)_pt514.3539.36 12.1427.78spodumene
Kolmozero(16)_pt616.2241.32 13.2129.25spodumene
Kolmozero(16)_pt748.2933.01 4.6611.81spodumene
Kaustinen(2)_pt13.1044.54 14.1238.25spodumene
Kaustinen(2)_pt22.7844.26 15.3937.57spodumene
Kaustinen(2)_pt32.7343.36 14.1235.14spodumene
Kaustinen(2)_pt43.2545.14 13.7337.88spodumene
Kaustinen(2)_pt52.4045.10 14.3838.11spodumene
Kaustinen(2)_pt61.9842.98 4.0550.99spodumene
Kaustinen(1)_pt415.2239.54 0.7544.49spodumene
Kaustinen(1)_pt516.3939.16 41.13spodumene
Kaustinen(1)_pt616.9539.84 43.22spodumene
Kaustinen(1)_pt719.2438.76 0.5341.47spodumene
Kaustinen(1)_pt814.6740.34 0.6344.37spodumene
Kaustinen(1)_pt912.6740.84 46.48spodumene
Kaustinen(3)_pt210.3641.85 1.6743.23spodumene
Kaustinen(3)_pt312.0641.64 1.6944.61spodumene
Kaustinen(3)_pt72.8944.46 12.9139.75spodumene
Kaustinen(3)_pt83.1443.49 12.6940.68spodumene
Kaustinen(3)_pt103.8245.32 15.3935.47spodumene
Kaustinen(6)_pt62.2444.68 2.7250.35spodumene
Kaustinen(7)_pt12.3444.62 0.88 14.7337.43spodumene
Kaustinen(7)_pt22.4544.46 0.84 15.0137.25spodumene
Kaustinen(7)_pt32.6343.62 0.73 14.1538.87spodumene
Kaustinen(7)_pt43.7346.01 0.69 13.1036.48spodumene
Kaustinen(7)_pt82.8143.03 1.7052.46spodumene
Kaustinen(7)_pt93.8941.11 5.0344.12spodumene
Kolmozero(17)_pt116.8541.72 1.70 11.7228.01spodumene
Kolmozero(17)_pt217.9543.16 11.5027.39spodumene
Kolmozero(17)_pt313.6339.68 13.9730.33spodumene
Kolmozero(17)_pt47.1941.22 15.7435.84spodumene
Kolmozero(17)_pt54.6344.85 0.56 14.3935.58spodumene
Kolmozero(17)_pt64.6941.82 0.98 15.4237.09spodumene
Kolmozero(17)_pt72.6044.11 0.58 16.0236.70spodumene
Kolmozero(17)_pt82.6143.70 16.1937.50spodumene
Kolmozero(18)_pt154.1843.12 15.7536.95spodumene
Kolmozero(18)_pt162.2444.51 16.8036.44spodumene
Kolmozero(19)_pt37.1542.68 9.7228.44spodumene
Kolmozero(19)_pt42.5944.00 2.2751.14spodumene
Kolmozero(19)_pt55.5543.75 12.2838.41spodumene
Kolmozero(19)_pt65.5742.40 0.89 13.5937.54spodumene
Kolmozero(19)_pt82.4244.24 14.4838.86spodumene
Kolmozero(19)_pt95.1142.75 0.60 14.6836.87spodumene
Kolmozero(20)_pt94.9140.01 0.62 15.5729.61spodumene
Kolmozero(20)_pt105.4443.93 13.2336.00spodumene
Kolmozero(20)_pt113.9944.34 13.3636.58spodumene
Kolmozero(20)_pt124.3343.88 0.79 13.1136.20spodumene
Kaustinen(10)_pt26.6044.88 14.6133.90spodumene
Kaustinen(10)_pt34.5145.00 15.4935.00spodumene
Kaustinen(10)_pt44.8445.31 15.7134.14spodumene
Kaustinen(10)_pt55.3244.41 15.0535.22spodumene
Kaustinen(10)_pt65.2644.87 15.5634.32spodumene
Kaustinen(10)_pt74.6444.56 16.4734.32spodumene
Kaustinen(13)_pt26.0043.27 0.91 11.5334.39spodumene
Kaustinen(13)_pt35.6344.74 0.97 12.2436.42spodumene
Kaustinen(13)_pt84.0942.63 0.99 1.6750.63spodumene
* In this analysis there is no possibility of Lithium indicated.
Table
Table A3. Fractional atomic coordinates (×104) and equivalent isotropic displacement parameters (Å2 × 103) for fuchsite. Ueq is defined as 1/3 of the trace of the orthogonalized UIJ tensor.
Table A3. Fractional atomic coordinates (×104) and equivalent isotropic displacement parameters (Å2 × 103) for fuchsite. Ueq is defined as 1/3 of the trace of the orthogonalized UIJ tensor.
AtomxyzU(eq)
K150004023.4(14)750026.6(4)
Cr12370(20)5812(8)5015(5)6(3)
Al22577(9)5839(4)4992(2)13.2(16)
Si29645.9(19)5705.7(11)6358.7(5)12.0(4)
Si14518.5(19)7416.3(10)6358.9(5)11.8(4)
O23888(5)7483(2)5535.9(13)14.9(7)
O49591(5)5591(3)5537.9(13)14.7(6)
O69245(6)4067(3)6685.3(13)17.8(7)
O15445(6)5637(3)4491.4(13)16.4(6)
O512.457(5)6332(3)6690.0(13)18.0(7)
O37455(5)6852(3)6587.4(13)19.7(7)
O77500750050007(13)
Table
Table A4. Anisotropic displacement parameters (Å2 × 103) for fuchsite. The anisotropic displacement factor exponent takes the form: −2π2[h2a * 2U11 + 2hka * b * U12+…].
Table A4. Anisotropic displacement parameters (Å2 × 103) for fuchsite. The anisotropic displacement factor exponent takes the form: −2π2[h2a * 2U11 + 2hka * b * U12+…].
AtomU11U22U33U23U13U12
K127.8(8)26.1(8)25.7(7)02.3(5)0
Si213.5(7)8.8(6)13.6(6)−0.2(3)1.3(4)−0.2(3)
Si113.2(7)9.9(6)12.2(6)0.4(3)0.5(4)0.0(3)
O217.0(16)11.9(13)15.6(14)−1.9(8)0.3(11)−1.5(9)
O415.5(14)11.9(12)16.1(14)0.3(10)−0.5(9)−2.1(10)
O626.3(16)12.5(14)15.0(13)−0.9(9)4.0(11)−1.6(10)
O119.8(15)15.2(13)14.4(13)2.8(10)2.9(10)2.3(10)
O521.3(15)16.4(14)16.1(13)0.8(10)0.5(11)−4.8(11)
O319.3(15)20.3(15)18.9(13)−4.3(10)−0.7(10)4.4(11)
Table
Table A5. Bond lengths for fuchsite.
Table A5. Bond lengths for fuchsite.
AtomAtomLength/ÅAtomAtomLength/Å
K1Si1 13.7400(10)Cr1O1 101.943(10)
K1Si1 23.7400(10)Cr1O12.010(11)
K1O6 32.881(3)Al2Al2 102.946(9)
K1O6 43.269(3)Al2O21.928(5)
K1O6 53.269(3)Al2O2 91.962(5)
K1O62.881(3)Al2O4 101.960(5)
K1O5 42.885(3)Al2O4 52.004(6)
K1O5 63.261(3)Al2O11.893(5)
K1O5 73.261(3)Al2O1 101.924(5)
K1O5 52.885(3)Si2O41.646(3)
K1O3 62.912(3)Si2O61.643(3)
K1O3 72.912(3)Si2O51.648(3)
Cr1Cr1 82.87(2)Si2O31.642(3)
Cr1O21.960(9)Si1O21.650(3)
Cr1O2 91.970(9)Si1O6 111.643(2)
Cr1O4 51.882(11)Si1O5 51.644(3)
Cr1O4 101.911(9)Si1O31.635(3)
1 1/2-X,-1/2 + Y,3/2-Z; 2 1/2 + X,-1/2 + Y,+Z; 3 1-X,+Y,3/2-Z; 4 2-X,+Y,3/2-Z; 5 -1 + X,+Y,+Z; 6 -1/2 + X,-1/2 + Y,+Z; 7 3/2-X,-1/2 + Y,3/2-Z; 8 -X,1-Y,1-Z; 9 1/2-X,3/2-Y,1-Z; 10 1-X,1-Y,1-Z; 11 -1/2 + X,1/2 + Y,+Z.
Si1 1K1Si1 2134.23(4)O2Al2O4 10165.5(3)
O6 3K1Si1 224.63(5)O2 8Al2O4 595.7(2)
O6 4K1Si1 172.96(5)O4 10Al2Al2 1096.5(2)
O6 5K1Si1 1107.60(5)O4 5Al2Al2 10130.5(3)
O6K1Si1 124.63(5)O4 10Al2O2 892.7(2)
O6K1Si1 2156.87(6)O4 10Al2O4 577.6(2)
O6 3K1Si1 1156.87(6)O1Al2Al2 1039.88(14)
O6 5K1Si1 272.96(5)O1 10Al2Al2 1039.10(13)
O6 4K1Si1 2107.60(5)O1Al2O296.9(2)
O6 3K1O6178.45(11)O1Al2O2 894.2(2)
O6K1O6 5115.84(8)O1 10Al2O295.3(2)
O6 3K1O6 4115.84(8)O1 10Al2O2 8170.4(3)
O6 3K1O6 564.13(8)O1 10Al2O4 591.9(2)
O6K1O6 464.14(8)O1Al2O4 1095.3(2)
O6 4K1O6 5178.63(9)O1Al2O4 5168.0(2)
O6 3K1O5 588.48(7)O1 10Al2O4 1094.7(2)
O6K1O5 6130.96(7)O1Al2O1 1079.0(2)
O6 3K1O5 7130.96(8)K1 11Si2K187.18(2)
O6 3K1O5 650.56(7)K1 11Si2K1 1288.01(2)
O6K1O5 750.56(6)K1 12Si2K187.08(2)
O6 3K1O5 490.40(8)O4Si2K1 12130.69(10)
O6K1O5 590.40(8)O4Si2K1 11121.42(10)
O6K1O5 488.48(8)O4Si2K1128.79(10)
O6K1O3 788.89(7)O4Si2O5110.47(14)
O6 3K1O3 688.89(7)O6Si2K144.48(10)
O6 3K1O3 792.16(8)O6Si2K1 12118.54(10)
O6K1O3 692.16(8)O6Si2K1 1160.47(11)
O5 4K1Si1 1110.10(5)O6Si2O4110.57(14)
O5 5K1Si1 1102.68(5)O6Si2O5107.07(15)
O5 5K1Si1 2110.10(5)O5Si2K1 1259.61(10)
O5 7K1Si1 2108.51(6)O5Si2K1119.26(10)
O5 4K1Si1 2102.68(6)O5Si2K1 1146.85(10)
O5 6K1Si1 226.03(5)O3Si2K165.35(11)
O5 7K1Si1 126.03(5)O3Si2K1 11125.61(10)
O5 6K1Si1 1108.51(6)O3Si2K1 1247.15(9)
O5 6K1O6 498.47(7)O3Si2O4112.10(14)
O5 5K1O6 550.47(7)O3Si2O6109.83(15)
O5 7K1O6 482.56(6)O3Si2O5106.61(14)
O5 6K1O6 582.56(6)K112Si1K186.95(2)
O5 7K1O6 598.47(7)K1 13Si1K187.36(2)
O5 4K1O6 5128.25(7)K1 13Si1K1 1287.98(2)
O5 5K1O6 4128.25(8)O2Si1K1 13121.52(10)
O5 4K1O6 450.47(7)O2Si1K1 12130.93(10)
O5 5K1O5 7116.24(8)O2Si1K1128.47(9)
O5 5K1O5 6129.78(2)O6 13Si1K1 1346.95(10)
O5 4K1O5 7129.78(2)O6 13Si1K1 1259.88(11)
O5 4K1O5 587.22(11)O6 13Si1K1119.68(10)
O5 4K1O5 6116.24(8)O6 13Si1O2110.39(13)
O5 7K1O5 683.32(9)O6 13Si1O5 5107.19(15)
O5 5K1O3 788.88(8)O5 5Si1K144.35(10)
O5 4K1O3688.88(8)O5 5Si1K1 1360.49(10)
O5 4K1O3 7175.28(8)O5 5Si1K1 12118.17(10)
O5 5K1O3 6175.28(8)O5 5Si1O2110.66(13)
O3 6K1Si1 268.20(6)O3Si1K1 13125.45(10)
O3 7K1Si1 168.20(6)O3Si1K1 1247.06(10)
O3 7K1Si1 281.17(6)O3Si1K165.07(11)
O3 6K1Si1 181.17(6)O3Si1O2112.21(14)
O3 7K1O6 549.98(7)O3Si1O6 13106.78(15)
O3 6K1O6 449.98(7)O3Si1O5 5109.42(14)
O3 7K1O6 4131.24(7)Cr1O2Cr1 8102.2(3)
O3 6K1O6 5131.24(7)Cr1O2Al2 8101.2(4)
O3 6K1O5 768.39(7)Si1O2Cr1122.3(3)
O3 7K1O5 750.22(7)Si1O2Cr1 8127.6(3)
O3 6K1O5 650.22(7)Si1O2Al2124.06(18)
O3 7K1O5 668.39(8)Si1O2Al2 8126.55(19)
O3 7K1O3 695.13(11)Cr1 11O4Cr1 1098.3(4)
O2 8Cr1Cr1 998.8(6)Cr1 11O4Al2 110.8(4)
O2Cr1Cr1 9135.0(7)Cr1 10O4Al2 1199.0(4)
O2Cr1O2 877.8(3)Cr1 10O4Al2 103.4(4)
O2 8Cr1O190.4(4)Cr1 11O4Al2 10101.6(4)
O2Cr1O192.2(4)Si2O4Cr1 10125.1(3)
O4 5Cr1Cr1 941.3(3)Si2O4Cr1 11127.8(3)
O4 10Cr1Cr1 940.5(2)Si2O4Al2 10122.33(19)
O4 10Cr1O2170.2(6)Si2O4Al2 11127.0(2)
O4 10Cr1O2 893.9(5)K1O6K1 11115.84(8)
O4 5Cr1O2 899.5(5)Si2O6K1 1193.59(12)
O4 5Cr1O294.4(5)Si2O6K1111.96(13)
O4 5Cr1O4 1081.7(4)Si1 1O6K1108.42(13)
O4 10Cr1O193.0(4)Si1 1O6K11194.36(12)
O4 5Cr1O1169.1(5)Si1 1O6Si2129.97(17)
O4 10Cr1O1 1095.7(4)Cr1 10O1Cr1104.3(4)
O4 5Cr1O1 1095.1(4)K1 11O5K1 12116.24(8)
O1 10Cr1Cr1 997.1(4)Si2O5K1 1294.54(12)
O1Cr1Cr1 9132.8(6)Si2O5K1 11108.52(12)
O1 10Cr1O293.6(5)Si1 11O5K1 11112.18(13)
O1 10Cr1O2 8163.5(6)Si1 11O5K1 1293.48(11)
O1 10Cr1O175.7(4)Si1 11O5Si2129.33(16)
O2 8Al2Al2 10133.8(3)Si2O3K1 12108.42(12)
O2Al2Al2 1097.9(3)Si1O3K1 12108.66(13)
O2Al2O2 878.70(18)Si1O3Si2140.99(17)
O2Al2O4 591.6(2)
1 1/2 + X,-1/2 + Y,+Z; 2 1/2-X,-1/2 + Y,3/2-Z; 3 1-X,+Y,3/2-Z; 4 2-X,+Y,3/2-Z; 5 -1 + X,+Y,+Z; 6 3/2-X,-1/2 + Y,3/2-Z; 7 -1/2 + X,-1/2 + Y,+Z; 8 1/2-X,3/2-Y,1-Z; 9 -X,1-Y,1-Z; 10 1-X,1-Y,1-Z; 11 1 + X,+Y,+Z; 12 1/2 + X,1/2 + Y,+Z; 13 -1/2 + X,1/2 + Y,+Z.
Table
Table A6. Torsion angles for fuchsite.
Table A6. Torsion angles for fuchsite.
ABCDAngle/˚ABCDAngle/˚
K1 1Si2O4Cr1 1−41.6(4)O4Si2O6K1 1115.30(12)
K1Si2O4Cr1 1−156.3(3)O4Si2O6K1−124.95(13)
K1 2Si2O4Cr1 176.5(4)O4Si2O6Si1 416.6(3)
K1 2Si2O4Cr1 3−143.2(4)O4Si2O5K1 2126.00(11)
K1 1Si2O4Cr1 398.6(4)O4Si2O5K1 1−114.38(13)
K1Si2O4Cr1 3−16.0(4)O4Si2O5Si1 127.7(3)
K1 1Si2O4Al2 3101.0(2)O4Si2O3K1 2−125.67(13)
K1Si2O4Al2 3−13.7(3)O4Si2O3Si135.6(4)
K1 1Si2O4Al2 1−41.8(2)O6Si2O4Cr1 331.5(4)
K1 2Si2O4Al2 176.3(2)O6Si2O4Cr1 1−108.8(4)
K1 2Si2O4Al2 3−140.89(19)O6Si2O4Al2 333.8(3)
K1Si2O4Al2 1−156.50(17)O6Si2O4Al2 1−109.0(2)
K1Si2O6K1 1−119.75(13)O6Si2O5K1 2−113.54(12)
K1 1Si2O6K1119.75(13)O6Si2O5K1 16.08(16)
K1 2Si2O6K150.46(15)O6Si2O5Si1 1148.2(2)
K1 2Si2O6K1 1−69.29(10)O6Si2O3K1 2111.00(14)
K1 1Si2O6Si1 4−98.7(3)O6Si2O3Si1−87.7(3)
K1 2Si2O6Si1 4−168.03(18)O6 5Si1O2Cr1 6−5.9(5)
K1Si2O6Si1 4141.5(3)O6 5Si1O2Cr1−149.3(4)
K1Si2O5K1 2−66.66(9)O6 5Si1O2Al2−152.9(2)
K1 2Si2O5K1 1119.62(12)O6 5Si1O2Al2 6−10.3(3)
K1 1Si2O5K1 2−119.62(12)O6 5Si1O3K1 24.85(16)
K1Si2O5K1 152.96(14)O6 5Si1O3Si2−156.4(3)
K1 1Si2O5Si1 1142.1(3)O1 3Al2O1Al2 3−0.002(0)
K1Si2O5Si1 1−164.93(16)O5Si2O4Cr1 19.5(4)
K1 2Si2O5Si1 1−98.3(2)O5Si2O4Cr1 3149.8(4)
K1 1Si2O3K1 243.71(16)O5Si2O4Al2 19.3(3)
K1Si2O3K1 2110.44(11)O5Si2O4Al2 3152.1(2)
K1 1Si2O3Si1−155.0(2)O5Si2O6K1 1−5.10(14)
K1 2Si2O3Si1161.3(4)O5Si2O6K1114.65(14)
K1Si2O3Si1−88.3(3)O5Si2O6Si1 4−103.8(3)
K1Si1O2Cr116.7(5)O5Si2O3K1 2−4.67(16)
K1 5Si1O2Cr1 645.3(4)O5Si2O3Si1156.6(3)
K1 2Si1O2Cr1 6−73.2(4)O5 7Si1O2Cr1 6112.6(4)
K1 2Si1O2Cr1143.5(4)O5 7Si1O2Cr1−30.8(4)
K1 5Si1O2Cr1−98.1(4)O5 7Si1O2Al2−34.5(3)
K1Si1O2Cr1 6160.0(4)O5 7Si1O2Al2 6108.2(3)
K1 5Si1O2Al2−101.7(2)O5 7Si1O3K1 2−110.84(13)
K1 2Si1O2Al2 6−77.5(3)O5 7Si1O3Si287.9(3)
K1Si1O2Al26155.7(2)O3Si2O4Cr13−91.5(4)
K1Si1O2Al213.0(3)O3Si2O4Cr1 1128.3(3)
K1 2Si1O2Al2139.8(2)O3Si2O4Al2 1128.0(2)
K1 5Si1O2Al2 641.0(3)O3Si2O4Al2 3−89.1(2)
K1Si1O3K1 2−110.63(11)O3Si2O6K1 1−120.48(12)
K1 5Si1O3K1 2−43.80(16)O3Si2O6K1−0.72(18)
K1 2Si1O3Si2−161.2(4)O3Si2O6Si1 4140.8(2)
K1Si1O3Si288.1(3)O3Si2O5K1 23.97(14)
K1 5Si1O3Si2155.0(2)O3Si2O5K1 1123.59(13)
O2 6Al2O1Al2 3173.1(3)O3Si2O5Si1 1−94.3(2)
O2Al2O1Al2 394.0(2)O3Si1O2Cr1 6−124.9(4)
O2Si1O3K1 2125.92(12)O3Si1O2Cr191.8(4)
O2Si1O3Si2−35.3(3)O3Si1O2Al2 6−129.2(3)
O4 7Al2O1Al2 3−41.1(13)O3Si1O2Al288.1(3)
O4 3Al2O1Al2 3−93.8(2)
1 1 + X,+Y,+Z; 2 1/2 + X,1/2 + Y,+Z; 3 1-X,1-Y,1-Z; 4 1/2 + X,-1/2 + Y,+Z; 5 -1/2 + X,1/2 + Y,+Z; 6 1/2-X,3/2-Y,1-Z; 7 -1 + X,+Y,+Z.
Table
Table A7. Fractional atomic coordinates (×104) and equivalent isotropic displacement parameters (Å2 × 103) for lepidolite. Ueq is defined as 1/3 of the trace of the orthogonalized UIJ tensor.
Table A7. Fractional atomic coordinates (×104) and equivalent isotropic displacement parameters (Å2 × 103) for lepidolite. Ueq is defined as 1/3 of the trace of the orthogonalized UIJ tensor.
AtomxyzU(eq)
Si14541(3)7437(2)6337.3(9)15.6(6)
Si29635(4)5734(2)6336.5(9)15.2(6)
Al12536(5)9160(2)4999.5(13)24.9(7)
O74307(12)9092(5)6657(3)25.1(13)
O22405(10)6399(6)6666(3)24.5(12)
O37414(10)6827(6)6588(3)26.7(13)
O43978(10)7483(5)5527(2)20.5(11)
O59518(10)5644(6)5528(3)22.1(12)
O65476(10)5670(5)4510(2)19.7(11)
Li275007500500038(5)
Fe150004060.8(18)750020.3(8)
O14850(110)3850(60)7010(30)0(11)
Table
Table A8. Anisotropic displacement parameters (Å2 × 103) for lepidolite. The Anisotropic displacement factor exponent takes the form: −2π2[h2a * 2U11 + 2hka * b * U12+…].
Table A8. Anisotropic displacement parameters (Å2 × 103) for lepidolite. The Anisotropic displacement factor exponent takes the form: −2π2[h2a * 2U11 + 2hka * b * U12+…].
AtomU11U22U33U23U13U12
Si114.0(10)14.3(10)18.0(10)−0.8(6)−0.7(7)−0.6(7)
Si215.6(11)10.2(9)19.5(11)−2.0(6)0.2(8)−1.0(6)
Al124.9(13)20.3(13)29.1(14)−0.5(8)0.1(10)−1.2(8)
O737(3)13(3)25(3)−2.2(18)2(2)0(2)
O222(3)26(3)25(3)−1(2)1(2)−9(2)
O318(3)33(3)28(3)−8(2)−5(2)11(2)
O422(2)21(2)18(3)−0.8(19)−1(2)0(2)
O521(3)23(3)22(3)−4(2)2(2)−4(2)
O626(3)20(2)13(2)1.6(19)2(2)−7(2)
Li236(11)43(13)36(11)2(9)7(9)15(10)
Fe118.3(11)20.2(11)21.9(13)00.0(7)0
Table
Table A9. Bond lengths for lepidolite.
Table A9. Bond lengths for lepidolite.
AtomAtomLength/ÅAtomAtomLength/Å
Si1O71.636(5)Al1O4 31.946(5)
Si1O21.641(5)Al1O5 51.956(6)
Si1O31.628(5)Al1O5 61.944(6)
Si1O41.632(5)Al1O6 31.939(6)
Si2O7 11.633(5)Al1O6 61.943(6)
Si2O2 21.641(5)Al1Li22.986(2)
Si2O31.637(5)Al1Li2 63.014(2)
Si2O51.627(5)Al1Li2 73.019(2)
Al1Al1 32.997(4)O4Li22.205(5)
Al1Al1 42.979(5)O5Li22.196(5)
Al1O41.957(5)O6Li22.148(5)
1 1/2 + X,-1/2 + Y,+Z; 2 1 + X,+Y,+Z; 3 1/2-X,3/2-Y,1-Z; 4 1-X,2-Y,1-Z; 5 3/2-X,3/2-Y,1-Z; 6 -1/2 + X,1/2 + Y,+Z; 7 -1 + X,+Y,+Z.
Table
Table A10. Bond angles for lepidolite.
Table A10. Bond angles for lepidolite.
AtomAtomAtomAngle/˚AtomAtomAtomAngle/˚
O7Si1O2106.5(3)Si2O5Al1 1123.4(3)
O3Si1O7106.7(3)Si2O5Al1 7125.7(3)
O3Si1O2108.6(3)Si2O5Li2114.7(3)
O3Si1O4113.0(3)Al1 1O5Al1 799.6(2)
O4Si1O7111.0(3)Al1 1O5Li293.2(2)
O4Si1O2110.8(3)Al1 7O5Li291.8(2)
O7 1Si2O2 2107.0(3)Al1 4O6Al1 1103.3(2)
O7 1Si2O3108.7(3)Al1 4O6Li295.1(2)
O3Si2O2 2105.9(3)Al1 1O6Li294.8(2)
O5Si2O7 1110.9(3)Al1 7Li2Al1 4120.13(7)
O5Si2O2 2111.7(3)Al1 7Li2Al1180.0
O5Si2O3112.4(3)Al1 1Li2Al1 460.60(8)
Al1 3Al1Al1 4121.30(16)Al1 7Li2Al1 259.87(7)
Al1 3Al1Li260.70(8)Al1 7Li2Al1 3120.47(8)
Al1 3Al1Li2 559.77(7)Al1 4Li2Al1 2180.00(10)
Al1 3Al1Li2 6179.17(13)Al1Li2Al1 2120.13(7)
Al1 4Al1Li2 5178.93(14)Al1Li2Al1 359.53(8)
Al1 4Al1Li2 659.53(8)Al1Li2Al1 1120.47(8)
O4 4Al1Al1 3133.8(2)Al1 3Li2Al1 260.60(8)
O4Al1Al1 396.20(19)Al1 1Li2Al1 3180.0
O4Al1Al1 439.70(15)Al1 7Li2Al1 159.53(8)
O4 4Al1Al1 439.98(15)Al1 3Li2Al1 4119.40(8)
O4 4Al1O479.7(2)Al1Li2Al1 459.87(7)
O4 4Al1O5 794.0(2)Al1 1Li2Al1 2119.40(8)
O4 4Al1Li2 646.83(16)O4Li2Al1 7139.07(14)
O4Al1Li247.57(16)O4Li2Al1 189.93(14)
O4 4Al1Li285.56(17)O4 7Li2Al1 389.93(14)
O4Al1Li2 5140.81(18)O4Li2Al1 390.07(14)
O4Al1Li2 684.47(16)O4 7Li2Al1 740.93(14)
O4 4Al1Li2 5139.49(18)O4Li2Al1 2139.94(14)
O5 5Al1Al1 4134.0(2)O47Li2Al1 240.06(14)
O5 7Al1Al1 495.80(19)O4Li2Al1 440.06(14)
O5 7Al1Al1 340.06(16)O47Li2Al1139.07(14)
O5 5Al1Al1 340.35(16)O4Li2Al140.93(14)
O5 7Al1O494.9(2)O4 7Li2Al1 4139.94(14)
O5 5Al1O494.6(3)O4 7Li2Al1 190.07(14)
O5 5Al1O4 4171.7(3)O4 7Li2O4180.0
O5 5Al1O5 780.4(2)O5Li2Al1 3139.91(14)
O5 5Al1Li2 6139.15(19)O5 7Li2Al1 289.76(14)
O5 5Al1Li286.12(18)O5 7Li2Al1 7139.10(14)
O5 7Al1Li2 6140.44(18)O5 7Li2Al140.90(14)
O5 7Al1Li2 585.13(17)O5 7Li2Al1 490.24(14)
O5 7Al1Li247.32(17)O5Li2Al1 140.09(14)
O5 5Al1Li2 546.68(17)O5Li2Al1 489.76(14)
O6 5Al1Al1 394.37(19)O5Li2Al1139.10(14)
O6 4Al1Al1 3134.2(2)O5Li2Al1 740.90(14)
O6 4Al1Al1 493.91(19)O5Li2Al1 290.24(14)
O6 5Al1Al1 4134.0(2)O5 7Li2Al1 1139.91(14)
O6 4Al1O4 491.9(2)O5 7Li2Al1 340.09(14)
O6 4Al1O494.0(2)O5 7Li2O481.83(19)
O6 5Al1O4 494.7(2)O5 7Li2O4 798.17(19)
O6 5Al1O4169.2(3)O5Li2O498.17(19)
O6 5Al1O5 794.8(2)O5Li2O4 781.83(19)
O6 4Al1O5 594.5(2)O5Li2O5 7180.0
O6 5Al1O5 591.9(2)O6Li2Al1 3140.03(15)
O6 4Al1O5 7170.0(2)O6Li2Al1 439.77(14)
O6 4Al1O6 576.7(2)O6 7Li2Al1 339.97(15)
O6 5Al1Li2 545.25(16)O6Li2Al1 790.00(15)
O6 4Al1Li2 645.14(15)O6 7Li2Al1 239.77(14)
O6 5Al1Li2 684.95(17)O6 7Li2Al1 4140.23(14)
O6 4Al1Li2 585.14(16)O6Li2Al190.00(15)
O6 4Al1Li2141.39(18)O6Li2Al1 2140.23(14)
O6 5Al1Li2141.87(19)O6 7Li2Al190.00(15)
Li2Al1Al1 460.60(8)O6 7Li2Al1 1140.03(15)
Li2Al1Li2 6120.13(7)O6Li2Al1 139.97(15)
Li2 5Al1Li2 6119.40(8)O6 7Li2Al1 790.00(15)
Li2Al1Li2 5120.47(8)O6 7Li2O4 779.81(19)
Si2 5O7Si1131.2(4)O6 7Li2O4100.19(18)
Si1O2Si2 6130.4(3)O6Li2O479.81(19)
Si1O3Si2139.7(3)O6Li2O4 7100.19(18)
Si1O4Al1125.9(3)O6 7Li2O5 780.03(19)
Si1O4Al14123.4(3)O6Li2O580.03(19)
Si1O4Li2113.9(3)O6 7Li2O599.97(19)
Al1 4O4Al1100.3(2)O6Li2O5 799.97(19)
Al1 4O4Li293.1(2)O6 7Li2O6180.0
Al1O4Li291.5(2)
1 1/2 + X,-1/2+Y,+Z; 2 1 + X,+Y,+Z; 3 1-X,2-Y,1-Z; 4 1/2-X,3/2-Y,1-Z; 5 -1/2 + X,1/2 + Y,+Z; 6 -1 + X,+Y,+Z; 7 3/2-X,3/2-Y,1-Z.
Table
Table A11. Torsion angles for lepidolite.
Table A11. Torsion angles for lepidolite.
ABCDAngle/˚ABCDAngle/˚
O7Si1O2Si2 1107.0(5)O2 6Si2O5Al1 413.5(5)
O7Si1O3Si2−149.6(6)O2 6Si2O5Al1 3149.5(3)
O7Si1O4Al1 2−149.6(4)O2 6Si2O5Li2−98.4(3)
O7Si1O4Al1−11.7(5)O3Si1O7Si2 599.0(5)
O7Si1O4Li299.1(3)O3Si1O2Si2 1−138.5(4)
O7 3Si2O3Si1−95.5(6)O3Si1O4Al1 290.6(4)
O7 3Si2O5Al1 330.2(5)O3Si1O4Al1−131.5(4)
O7 3Si2O5Al1 4−105.8(4)O3Si1O4Li2−20.7(4)
O7 3Si2O5Li2142.3(3)O3Si2O5Al1 3−91.6(4)
O2Si1O7Si2 5−145.1(5)O3Si2O5Al1 4132.3(4)
O2Si1O3Si296.0(6)O3Si2O5Li220.5(4)
O2Si1O4Al1106.3(4)O4Si1O7Si2 5−24.5(6)
O2Si1O4Al1 2−31.5(4)O4Si1O2Si2 1−13.8(5)
O2Si1O4Li2−142.8(3)O4Si1O3Si2−27.4(7)
O2 6Si2O3Si1149.9(6)O5Si2O3Si127.6(7)
1 -1 + X,+Y,+Z; 2 1/2-X,3/2-Y,1-Z; 3 1/2 + X,-1/2 + Y,+Z; 4 3/2-X,3/2-Y,1-Z; 5 -1/2 + X,1/2 + Y,+Z; 6 1 + X,+Y,+Z.
Table
Table A12. Fractional Atomic Coordinates (×104) and Equivalent Isotropic Displacement Parameters (Å2 × 103) for Spodumene. Ueq is defined as 1/3 of the trace of the orthogonalized UIJ tensor.
Table A12. Fractional Atomic Coordinates (×104) and Equivalent Isotropic Displacement Parameters (Å2 × 103) for Spodumene. Ueq is defined as 1/3 of the trace of the orthogonalized UIJ tensor.
AtomxyzU(eq)
Si14619.7(9)4066.4(5)2058.8(5)6.4(3)
Al12500933.4(8)06.2(3)
O15308(2)4178.0(13)3901.6(13)7.6(3)
O34359(2)2331.2(14)1352.0(13)10.6(3)
O22022(2)5130.5(14)1434.8(12)10.3(3)
Li175002265(6)500017.0(9)
Table
Table A13. Anisotropic displacement parameters (Å2 × 103) for spodumene. The anisotropic displacement factor exponent takes the form: −2π2[h2a * 2U11 + 2hka * b * U12+…].
Table A13. Anisotropic displacement parameters (Å2 × 103) for spodumene. The anisotropic displacement factor exponent takes the form: −2π2[h2a * 2U11 + 2hka * b * U12+…].
AtomU11U22U33U23U13U12
Si16.6(4)6.9(4)5.8(3)−0.67(14)1.2(2)−0.20(15)
Al17.1(5)6.0(4)5.5(4)01.3(3)0
O18.6(6)8.1(7)6.3(6)−0.5(4)2.1(5)−0.2(4)
O312.6(7)8.5(7)10.3(6)−2.3(4)1.5(5)0.1(5)
O210.1(7)12.7(6)8.0(7)0.6(4)1.8(5)2.7(5)
Li119(2)17(2)15(2)03.9(18)0
Table
Table A14. Bond lengths for Spodumene.
Table A14. Bond lengths for Spodumene.
AtomAtomLength/ÅAtomAtomLength/Å
Si1O11.6404(12)Al1O1 61.9459(12)
Si1O31.5863(12)Al1O3 71.8219(12)
Si1O211.6294(12)Al1O31.8219(12)
Si1O21.6215(12)Al1Li1 53.079(5)
Si1Li122.8688(19)Al1Li1 33.017(2)
Si1Li13.159(2)Al1Li1 23.017(2)
Al1O1 31.9459(12)O1Li12.096(4)
Al1O1 41.9970(12)O3Li1 22.2767(14)
Al1O1 51.9970(12)O2Li1 82.262(4)
1 1/2 + X,1-Y,+Z; 2 3/2-X,1/2-Y,1/2-Z; 3 1/2-X,1/2-Y,1/2-Z; 4 1-X,-1/2 + Y,1/2-Z; 5 -1/2 + X,-1/2 + Y,-1/2 + Z; 6 +X,1/2-Y,-1/2 + Z; 7 1/2-X,+Y,-Z; 8 -1/2 + X,1/2 + Y,-1/2 + Z.
Table
Table A15. Bond angles for spodumene.
Table A15. Bond angles for spodumene.
AtomAtomAtomAngle/˚AtomAtomAtomAngle/˚
O1Si1Li137.00(8)Si1 1Li1Si181.615(18)
O1Si1Li1 1131.24(6)Si1 1Li1Al1 167.695(17)
O3Si1O1116.60(6)Si1 11Li1Al1 1140.37(3)
O3Si1O2 2104.13(7)Si1 1Li1Al1 8112.94(9)
O3Si1O2111.80(7)Si1 11Li1Al1 667.695(17)
O3Si1Li1 152.32(9)Si1 11Li1Al1 8112.94(9)
O3Si1Li183.56(9)Si1 1Li1Al1 6140.37(3)
O2Si1O1108.04(6)Al1 1Li1Si190.84(9)
O2 2Si1O1108.45(6)Al1 8Li1Si161.41(7)
O2Si1O2 2107.36(4)Al1 6Li1Si160.38(5)
O2 2Si1Li1 151.92(9)Al1 1Li1Al1 859.92(8)
O2Si1Li1 1120.16(6)Al1 1Li1Al1 6119.83(15)
O2Si1Li1140.39(5)Al1 6Li1Al1 859.92(8)
O2 2Si1Li1103.38(5)O1Li1Si128.10(3)
Li1 1Si1Li198.386(18)O1 12Li1Si198.58(15)
O1 3Al1O1 496.97(5)O1Li1Si1 1107.22(5)
O1 4Al1O1 584.90(7)O1Li1Si1 11107.51(6)
O1 6Al1O1 596.97(5)O1 12Li1Si1 1107.51(6)
O1 6Al1O1 478.91(5)O1 12Li1Si1 11107.22(5)
O1 3Al1O1 578.91(5)O1Li1Al1 840.01(9)
O1 3Al1O1 6174.49(7)O1 12Li1Al1 139.86(5)
O1 3Al1Li1 143.67(7)O1 12Li1Al1 689.99(13)
O1 4Al1Li1 442.45(3)O1Li1Al1 189.99(13)
O1 6Al1Li1 1140.49(6)O1 12Li1Al1 840.01(9)
O1 3Al1Li1 6140.49(6)O1Li1Al1 639.86(5)
O1 4Al1Li1 688.12(7)O1Li1O1 1280.03(18)
O1 5Al1Li1 188.12(7)O1 12Li1O3 176.18(10)
O1 3Al1Li1 487.25(4)O1Li1O3 1176.18(10)
O1 6Al1Li1 487.25(4)O1 12Li1O3 1190.64(12)
O1 6Al1Li1 643.67(7)O1Li1O3 190.64(12)
O1 4Al1Li1 1140.59(6)O1 12Li1O2 13116.63(4)
O1 5Al1Li1 6140.59(6)O1Li1O2 13139.93(5)
O1 5Al1Li1 442.45(3)O1 12Li1O2 5139.93(5)
O3 7Al1O1 488.42(5)O1Li1O2 5116.63(4)
O3Al1O1 4167.96(5)O3 1Li1Si1 133.47(4)
O3Al1O1 391.54(5)O3 11Li1Si1 1161.83(16)
O3 7Al1O1 392.00(5)O3 11Li1Si1 1133.47(4)
O3Al1O1 588.42(5)O3 1Li1Si174.82(6)
O3 7Al1O1 691.54(5)O3 11Li1Si196.87(8)
O3 7Al1O1 5167.96(5)O3 1Li1Si1 11161.83(16)
O3Al1O1 692.00(5)O3 11Li1Al1 637.04(5)
O3Al1O3 799.81(8)O3 1Li1Al1 881.45(12)
O3Al1Li1 4130.10(4)O3 11Li1Al1 1130.47(15)
O3 7Al1Li1 648.83(5)O3 1Li1Al1 137.04(5)
O3Al1Li1 148.83(5)O3 11Li1Al1 881.45(12)
O3 7Al1Li1 4130.10(4)O3 1Li1Al16130.47(15)
O3 7Al1Li1 190.72(7)O3 1Li1O3 11162.9(2)
O3Al1Li1 690.72(7)O2 13Li1Si1 1101.91(15)
Li1 1Al1Li1 6119.83(15)O2 13Li1Si1140.94(9)
Li1 6Al1Li1 4120.08(8)O2 5Li1Si188.95(3)
Li1 1Al1Li1 4120.08(8)O2 5Li1Si1 134.53(4)
Si1O1Al1 6119.89(7)O2 5Li1Si1 11101.91(15)
Si1O1Al1 8122.01(7)O2 13Li1Si1 1134.53(4)
Si1O1Li1114.90(8)O2 13Li1Al1 6101.20(4)
Al1 6O1Al1 8101.09(5)O2 5Li1Al1 6126.86(6)
Al1 8O1Li197.54(10)O2 5Li1Al1 8142.39(8)
Al1 6O1Li196.47(6)O2 13Li1Al1 8142.39(8)
Si1O3Al1148.44(8)O2 13Li1Al1 1126.86(6)
Si1O3Li1 194.21(13)O2 5Li1Al1 1101.20(4)
Al1O3Li1 194.13(9)O2 13Li1O3 1127.67(16)
Si1O2Si1 9138.97(8)O2 5Li1O3 11127.67(16)
Si1 9O2Li1 1093.55(8)O2 13Li1O3 1167.94(7)
Si1O2Li1 10116.79(7)O2 5Li1O3 167.94(7)
Si1 1Li1Si1 11134.13(17)O2 5Li1O2 1375.23(16)
Si1 11Li1Si1121.25(2)
1 3/2-X,1/2-Y,1/2-Z; 2 1/2 + X,1-Y,+Z; 3 +X,1/2-Y,-1/2 + Z; 4 -1/2 + X,-1/2+Y,-1/2 + Z; 5 1-X,-1/2 + Y,1/2-Z; 6 1/2-X,1/2-Y,1/2-Z; 7 1/2-X,+Y,-Z; 8 ½ + X,1/2 + Y,1/2+Z; 9 -1/2 + X,1-Y,+Z; 10 -1/2 + X,1/2 + Y,-1/2 + Z; 11 +X,1/2-Y,1/2 + Z; 12 3/2-X,+Y,1-Z; 13 1/2 + X,-1/2 + Y,1/2 + Z.
Table
Table A16. Torsion angles for spodumene.
Table A16. Torsion angles for spodumene.
ABCDAngle/˚ABCDAngle/˚
O1Si1O3Al1132.06(14)O2Si1O1Li1156.07(9)
O1Si1O3Li1 1−123.01(7)O2Si1O3Al17.07(17)
O1Si1O2Si1 2−16.87(14)O2 10Si1O3Al1−108.53(15)
O1Si1O2Li1 3116.44(10)O2 10Si1O3Li1 1−3.60(7)
O1 4Al1O3Si1114.97(15)O2Si1O3Li1 1112.00(7)
O1 5Al1O3Si1−166.17(15)O2 10Si1O2Si1 2−133.64(13)
O1 6Al1O3Si1−69.24(15)O2 10Si1O2Li1 3−0.34(12)
O1 7Al1O3Si1−109.9(3)Li1 1Si1O1Al1 6−146.96(11)
O1 4Al1O3Li1110.01(11)Li1 1Si1O1Al1 884.66(14)
O1 6Al1O3Li1 1−174.20(10)Li1Si1O1Al1 6−114.20(12)
O1 7Al1O3Li1 1145.1(3)Li1Si1O1Al1 8117.42(12)
O1 5Al1O3Li1 188.88(10)Li1 1Si1O1Li1−32.8(2)
O3Si1O1Al1 8146.63(7)Li1Si1O3Al1149.25(15)
O3Si1O1Al1 6−85.00(9)Li1 1Si1O3Al1−104.93(16)
O3Si1O1Li129.20(12)Li1Si1O3Li11−105.82(6)
O3Si1O2Si1 2112.74(12)Li1 1Si1O2Si1 2170.80(13)
O3Si1O2Li1 3−113.96(10)Li1Si1O2Si1 25.6(2)
O3 9Al1O3Si122.67(12)Li1Si1O2Li1 3138.95(19)
O3 9Al1O3Li1 1−82.29(10)Li1 1Si1O2Li1 3−55.89(18)
O2Si1O1Al1 8−86.50(9)Li1 1Al1O3Si1104.96(18)
O2 10Si1O1Al1 6157.94(7)Li1 7Al1O3Si1−157.33(12)
O2Si1O1Al1 641.87(9)Li1 6Al1O3Si1−25.58(15)
O2 10Si1O1Al1 829.57(9)Li1 7Al1O3Li1 197.71(10)
O2 10Si1O1Li1−87.86(10)Li1 6Al1O3Li1 1−130.53(14)
1 3/2-X,1/2-Y,1/2-Z; 2 -1/2 + X,1-Y,+Z; 3 -1/2 + X,1/2 + Y,-1/2 + Z; 4 +X,1/2-Y,-1/2 + Z; 5 1-X,-1/2 + Y,1/2-Z; 6 1/2-X,1/2-Y,1/2-Z; 7 -1/2 + X,-1/2 + Y,-1/2 + Z; 8 1/2 + X,1/2 + Y,1/2 + Z; 9 1/2-X,+Y,-Z; 10 1/2 + X,1-Y,+Z.

References

  1. Fisher, L.N. Characterization of the Mineralized Albitite Bodies at Biggejavri, Kautokeino Greenstone Belt, Finnmark, Northern Norway. Master’s Thesis, Colorado School of Mines, Golden, CO, USA, 2019; pp. 1–69. Available online: https://hdl.handle.net/11124/173977 (accessed on 26 April 2023).
  2. Huber, M.; Kamiński, D.; Maciołek, U. Columbite–Tantalite from Northern Scandinavia (Kaustinen, Kolmozero) Pegmatites: An Optical and Spectroscopic Properties. Crystals 2023, 13, 612. [Google Scholar] [CrossRef]
  3. Bayanova, T.B.; Kunakkuzin, E.L.; Serov, P.A.; Steshenko, E.; Borisenko, E.S.; Turkina, O. The Oldest Grey Gneisses and Tonalite-Trondhjemite Granodiorites in the Fennoscandian Shield: ID-TIMS and SHRIMP Data. Open J. Geol. 2020, 10, 2. [Google Scholar] [CrossRef] [Green Version]
  4. Lahtinen, R.; Garde, A.A.; Melezhik, V.A. Paleoproterozoic evolution of Fennoscandia and Greenland. Episodes 2008, 31, 20–28. [Google Scholar] [CrossRef] [PubMed] [Green Version]
  5. Hölttä, P.; Balagansky, V.; Garde, A.A.; Mertanen, S.; Peltonen, P.; Slabunov, A.; Sorjonen-Ward, P.; Whitehouse, M. Archean of Greenland and Fennoscandia. Episodes 2008, 31, 13–19. [Google Scholar] [CrossRef] [Green Version]
  6. Ahtola, T.; Kuusela, J.; Käpyaho, A.; Kontoniemi, O. Overview of lithium pegmatite exploration in the Kaustinen area in 2003–2012. Geological Survey of Finland. Rep. Investig. 2015, 220, 28. [Google Scholar]
  7. Bibikova, E.V.; Bogdanova, S.V.; Postnikov, A.V.; Popova, L.P.; Kirnozova, T.I.; Fugzan, M.M.; Glushchenko, V.V. Sarmatia–Volgo-Uralia Junction Zone: Isotopic–Geochronologic Characteristic of Supracrustal Rocks and Granitoids. Stratigr. Geol. Correl. 2009, 17, 561–573. [Google Scholar] [CrossRef]
  8. Glebovitsky, V.A. Early Precambrian of the Baltic Shield; Nauka: St Petersburg, Russia, 2005; p. 710. (In Russian) [Google Scholar]
  9. Pozhilienko, V.I.; Gavrilenko, B.V.; Zhirov, C.V.; Zhabin, S.V. Geology of Mineral Areas of the Murmansk Region; Kola Scientific Center, Russian Academy of Sciences: Apatity, Russia, 2002; p. 360. (In Russian) [Google Scholar]
  10. Andersson, J.; Möller, C.; Johansson, L. Zircon geochronology of migmatite gneisses along the Mylonite Zone (S Sweden): A major Sveconorwegian terrane boundary in the Baltic shield. Precambrian Res. 2002, 114, 121–147. [Google Scholar] [CrossRef]
  11. Bridgewater, D.; Scott, D.J.; Balagansky, V.V.; Timmerman, M.J.; Marker, M.; Bushmin, A.; Alexeyev, N.L.; Daly, J.S. Age and Provenance of Early Precambrian Metasidementary Rocks in the Lapland-Kola Belt, Russia: Evidence from Pb and Nd Isotopic Data. Terra Nova 2001, 13, 32–37. [Google Scholar] [CrossRef]
  12. Hölttä, P.; Heilimo, E.; Huhma, H.; Juopperi, H.; Kontinen, A.; Konnunaho, H.; Lauri, L.; Mikkola, P.; Paavola, J.; Sorjonen-Ward, P. Archaean Complexes of the Karelia Province in Finland. Geol. Surv. Finl. Spec. Pap. 2012, 54, 9–20. [Google Scholar]
  13. Timmerman, M.J.; Daly, S.J. Sm-Nd Evidence for Late Arhaean Crust Formation in the Lapland-Kola Mobile Belt, Kola Peninsula, Russia and Norway. Precambrian Res. 1995, 72, 97–107. [Google Scholar] [CrossRef]
  14. Huber, M.; Bayanova, T.B.; Serov, P.A.; Skupiński, S. Archean Gneisses of the Murmansk, Oleniegorsk Region, NE Fennoscandia, in the Light of the Petrographic and Geochemical Analysis; Sciences Publisher: Lublin, Poland, 2018; p. 181. (In Polish) [Google Scholar]
  15. Halla, J. The TTG-Amphibolite Terrains of Arctic Fennoscandia: Infinite Networks of Amphibolite Metatexite-Diatexite Transitions, Front. Earth Sci. Sec. Petrol. 2020, 8, 252. [Google Scholar] [CrossRef]
  16. Mokrushin, A.V.; Kudryashov, N.M.; Huber, M. First discovery of sperrylite in Archaean Patchemvarek gabbro-anorthosite (Kola region, Russia). In Proceedings of the Abstracts of the 12th International Platinum Symposium, Yekaterinburg, Russia, 11–14 August 2014; pp. 305–306. Available online: http://conf.uran.ru/12IPS/12%20IPS%20ABSTRACTS.pdf (accessed on 26 April 2023).
  17. Smol’kin, V.F.; Mokrushin, A.V. Paleoproterozoic Layered Intrusions of the Monchegorsk Ore District: Geochemistry and U–Pb, Sm–Nd, Re–Os Isotope Analysis. Minerals 2022, 12, 1432. [Google Scholar] [CrossRef]
  18. Petrovskaya, L.S.; Mitrofanov, F.P.; Bayanova, T.B.; Petrov, V.P.; Petrovski, M.N. Neoarchean Enderbites-Granulite Complex of the Puloziero-Polnek-Tundra Region, Central Kola Block: Stages and the Thermodynamic Regime of Evolution; Kola Scientific Center, Russian Academy of Sciences: Apatity, Russia, 2010; p. 78. (In Russian) [Google Scholar]
  19. Petrovskaya, L.S.; Mitrofanov, F.P.; Bayanova, T.B.; Serov, P.A. The Archean Pulozero–Polnek-Tundra Enderbite–Granulite Complex of the Central Kola Block: Stages and Formation Conditions (Kola Peninsula). Dokl. Akad. Nauk 2007, 416, 370–373. [Google Scholar] [CrossRef]
  20. Hałas, S.; Huber, M.; Piestrzynski, A. Petrology of gabbroides and isotope signature of sulfide mineralization from Fedorov-Pansky layered mafic intrusion, Kola peninsula, Russia. Geochronometria 2009, 33, 19–22. [Google Scholar] [CrossRef] [Green Version]
  21. Huber, M.A.; Hałas, S.; Neradovsky, Y.N.; Bayanova, T.B.; Mokrushin, A.W.; Lata, L. Stable isotope geochemistry of sulfides from intrusion in Monchegorsk, Northern part of baltic shield. Geochronometria 2016, 43, 96–101. [Google Scholar] [CrossRef] [Green Version]
  22. Huber, M.; Stępniewska, K. Application of the Fractal Dimension Calculation Technique to Determine the Shape of Selected Monchepluton Intrusion Crystals (NE Fennoscandia). Minerals 2021, 11, 1140. [Google Scholar] [CrossRef]
  23. Torske, T.; Bergh, S. The Caravarri Formation of the Kautokeino Greenstone Belt, Finnmark, North Norway; a Palaeoproterozoic foreland basin succession. NG U-BULL 2004, 442, 5–22. [Google Scholar]
  24. Morozova, L.N. Rare-metal pegmatites of the Soldat-Myl’k pegmatite field: Geology, geochemistry of rare elements. IOP Publ. 2020, 539, 012162. [Google Scholar] [CrossRef]
  25. Morozova, L.N.; Sokolova, E.N.; Smirnov, S.Z.; Balagansky, V.V.; Bazai, A.V. Spodumene from rare-metal pegmatites of the Kolmozero lithium world-class deposit on the Fennoscandian shield: Trace elements and crystal-rich fluid inclusions. Mineral. Mag. 2021, 85, 149–160. [Google Scholar] [CrossRef]
  26. Huber, M.; Kamiński, D.; Czernel, G.; Kozlov, E. Optical and Spectroscopic Properties of Lorenzenite, Loparite, Perovskite, Titanite, Apatite, Carbonates from the Khibiny, Lovozero, Kovdor, and Afrikanda Alkaline Intrusion of Kola Peninsula (NE Fennoscandia). Crystals 2022, 12, 224. [Google Scholar] [CrossRef]
  27. Bingen, B.; Solli, A.; Viola, G.; Torgersen, E.; Sandstad, J.S.; Whitehouse, M.J.; Nasuti, A. Geochronology of the Palaeoproterozoic Kautokeino Greenstone Belt, Finnmark, Norway: Tectonic implications in a Fennoscandia context. Nor. J. Geol. 2015, 95, 365–396. [Google Scholar] [CrossRef] [Green Version]
  28. Al-Ani, T.; Ahtola, T. Mineralogy of Spodumene Pegmatites, Kaustinen, Western Finland; Geological Survey of Finland Report; Southern Finland Office: Helsinki, Finland, 2008; Volume 19, pp. 1–48. Available online: https://tupa.gtk.fi/raportti/arkisto/m19_2323_2008_61.pdf (accessed on 26 April 2023).
  29. Morozova, L.N. The Kolmozero lithium deposit of rare metal pegmatites: New data on the rare element composition (Kola Peninsula). Lithosphere 2018, 18, 82–98. [Google Scholar] [CrossRef] [Green Version]
  30. Evzerov, V.Y. Glacier Deposits As Unique Formations in the Loose Cover of the Baltic Shield. Lithol. Miner. Resour. 2001, 36, 109–115. [Google Scholar] [CrossRef]
  31. Korsakova, O.P. Pleistocene marine deposits in the coastal areas of Kola Peninsula (Russia). Quat. Int. 2009, 206, 3–15. [Google Scholar] [CrossRef]
  32. Huber, M.; Rusek, A.; Menshakova, M.; Zhigunova, G.; Chmiel, S.; Iakovleva, O. Possibilities of Sustainable Development including Improvement in Air Quality for the City of Murmansk-Examples of Best Practice from Scandinavia. Climate 2022, 10, 15. [Google Scholar] [CrossRef]
  33. Huber, M.; Iakovleva, O. Tourism, Scientific, and Didactic Potential of the Ultrabasic-Alkaline Intrusion in Afrikanda with Perovskite Mineral (Kola Peninsula, N Russia) and of the Related Built Heritage. Heritage 2021, 4, 3892–3907. [Google Scholar] [CrossRef]
  34. Huber, M.; Zhigunova, G.; Menshakova, M.; Iakovleva, O.; Karimova, M. Geoheritage of the Monchegorsk Igneous Layered Paleoproterozoic Intrusion (Kola Peninsula, Arctic Russia): Evaluation and Geotourism Opportunities. Heritage 2021, 4, 3583–3610. [Google Scholar] [CrossRef]
  35. Huber, M.; Zhigunova, G.; Menshakova, M.; Gainanova, R.; Iakovleva, O. Geoheritage of the Kandalaksha region (Kola Peninsula, White Sea, Arctic Russia), Evaluation, and Geotourism Opportunities. Geoheritage 2022, 14, 112. [Google Scholar] [CrossRef]
  36. Huber, M.; Iakovleva, O.; Zhigunova, G.; Menshakova, M.; Gainanova, R. Can the Arctic be saved for the next generations? Study of examples and internships in Murmansk District. IOP Conf. Ser. Earth Environ. Sci. 2021, 678, 01203. [Google Scholar] [CrossRef]
  37. Smith, E.; Wang, W. Diamond with Concentric Inclusions. Gems Gemol. 2017, 53, 2. [Google Scholar]
  38. Bowers, D.G.; Binding, C.E. The optical properties of mineral suspended particles: A review and synthesis. Estuarine. Coast. Shelf Sci. 2006, 67, 219–230. [Google Scholar] [CrossRef]
  39. De Lima, A.F.; Souza, S.O.; Lalic, M.V. Electronic and optical properties of spodumene gemstone: A theoretical study. Opt. Mater. 2008, 30, 1048–1051. [Google Scholar] [CrossRef]
  40. Faye, G.H. The optical absorption spectra of certain transition metal ions in muscovite, lepidolite, and fuchsite. Can. J. Earth Sci. 1968, 5, 31–38. [Google Scholar] [CrossRef]
  41. Levinson, A.A. Studies in the mica group; relationship between polymorphism and composition in the muscovite-lepidolite series. Am. Mineral. J. Earth Planet. Mater. 1953, 38, 88–107. [Google Scholar]
  42. Gu, Y. Automated scanning electron microscope based mineral liberation analysis. J. Miner. Mater. Charact. Eng. 2003, 2, 33–41. [Google Scholar]
  43. Pirrie, D.; Power, M.R.; Rollinson, G.K.; Wiltshire, P.E.; Newberry, J.; Campbell, H.E. Automated SEM-EDS (QEMSCAN®) mineral analysis in forensic soil investigations: Testing instrumental reproducibility. In Criminal and Environmental Soil Forensics; Springer: Berlin, Germany, 2009; pp. 411–430. [Google Scholar]
  44. Rigaku. CRYSALIS Software System; Rigaku: Oxford, UK, 2016. [Google Scholar]
  45. Sheldrick, G.M. A short history of SHELX. Acta Crystallogr. 2008, A64, 112–122. [Google Scholar] [CrossRef] [Green Version]
  46. Sheldrick, G.M. SHELXT—Integrated space-group and crystal-structure determination. Acta Crystallogr. 2015, A71, 3–8. [Google Scholar] [CrossRef] [Green Version]
  47. Sheldrick, G.M. Crystal structure refinement with SHELXL. Acta Crystallogr. 2015, C71, 3–8. [Google Scholar]
  48. Dolomanov, O.V.; Bourhis, L.J.; Gildea, R.J.; Howard, J.A.K.; Puschmann, H.J. A Complete Structure Solution, Refinement and Analysis Program. Appl. Cryst. 2009, 42, 339–341. [Google Scholar] [CrossRef]
  49. Amarie, S.; Zaslansky, P.; Kajihara, Y.; Griesshaber, E.; Schmahl, W.W.; Keilmann, F. Nano-FTIR chemical mapping of minerals in biological materials. Beilstein J. Nanotechnol. 2012, 3, 312–323. [Google Scholar] [CrossRef]
  50. Pleshko, N.; Boskey, A.; Mendelsohn, R. Novel infrared spectroscopic method for the determination of crystallinity of hydroxyapatite minerals. Biophys. J. 1991, 60, 786–793. [Google Scholar] [CrossRef] [PubMed] [Green Version]
  51. Biesinger, M.C.; Hart, B.R.; Polack, R.; Kobe, B.A.; Smart, R.S.C. Analysis of mineral surface chemistry in flotation separation using imaging XPS. Miner. Eng. 2007, 20, 152–162. [Google Scholar] [CrossRef]
  52. Hochella, M.F., Jr.; Brown, G.E., Jr. Aspects of silicate surface and bulk structure analysis using X-ray photoelectron spectroscopy (XPS). Geochim. Cosmochim. Acta 1988, 52, 1641–1648. [Google Scholar] [CrossRef]
  53. Kudryashov, N.M.; Lyalina, L.M.; Apanasevich, E.A. Age of Rare-Metal Pegmatites from the Vasin-Myl’k Deposit (Kola Region): Evidence from U–Pb Geochronology of Microlite. Dokl. Earth Sci. 2015, 461, 321–3250. [Google Scholar] [CrossRef]
  54. Kudryashov, N.M.; Udoratina, O.V.; Coble, M.A.; Steshenko, E.N. Geochronological and Geochemical Study of Zircon from Tourmaline-Muscovite Granites of the Archaean Kolmozero–Voronya Greenstone Belt: Insights into Sources of the Rare-Metal Pegmatites. Minerals 2020, 10, 760. [Google Scholar] [CrossRef]
  55. Černý, P.; London, D.; Novák, M. Granitic Pegmatites as Refl ections of Their Sources. Elements 2012, 8, 289–294. [Google Scholar] [CrossRef]
  56. Linnen, R.L.; Lichtervelde, M.V.; Černý, P. Granitic Pegmatites as Sources of Strategic Metals. Elements 2012, 8, 275–280. [Google Scholar] [CrossRef]
  57. Alviola, R.; Mänttäri, I.; Mäkitie, H.; Vaasjoki, M. Svecofennian rare-element granitic pegmatites of the Ostrobothnia region western Finland: Their metamorphic environment and time of intrusion. In Svecofennian Granitic Pegmatites (1.86–1.79 Ga) and Quartz Monzonite (1.87 Ga), and Their Metamorphic Environment in the Seinäjoki Region, Western Finland; Mäkitie, H., Ed.; Special Paper; Geological Survey of Finland: Espoo, Finland, 2001; Volume 30, pp. 9–29. [Google Scholar]
  58. Vaasjoki, M.; Korsman, K.; Koistinen, T. Precambrian geology of Finland: Key to the evolution of the Fennoscandian Shield. Dev. Precambrian Geol. 2005, 14, 1–17. [Google Scholar]
  59. Mäkitie, H.; Kärkkäinen, N.; Lahti, S.I.; Alviola, R. Compositional variation of granitic pegmatites in relation to regional metamorphism in the Seinäjoki region, Western Finland. Geol. Surv. Finl. Spec. Pap. 2001, 30, 31–59. [Google Scholar]
  60. Käpyaho, A.; Sarapää, O.; Kaunismäki, J.; Lohva, J.; Ahtola, T.; Johansson, B.; Huhta, P. Research Report on the Li-Pegmatite Studies Carried out in the Years 2004 and 2005 in the Municipality of Kaustinen in the Catchment area Matoneva (Mining registration number 7882/1); Archive Report M06/2323/2007/10/78; Geological Research Center: Charleston, SC, USA, 2007. (In Finnish) [Google Scholar]
  61. Ahtola, T.; Kuusela, J.; Koistinen, E.; Seppänen, H.; Hatakka, T.; Lohva, J. Report of Investigations on the Leviäkangas Lithium Pegmatite Deposit in Kaustinen, Western Finland; Archive Report M19/2323/2010/32; Geological Survey of Finland: Espoo, Finland, 2010. [Google Scholar]
  62. Kuusela, J.; Ahtola, T.; Koistinen, E.; Seppänen, H.; Hatakka, T.; Lohva, J. Report of Investigations on the Rapasaaret Lithium Pegmatite Deposit In Kaustinen Kokkola, Western Finland; Archive Report 42/2011; Geological Survey of Finland: Espoo, Finland, 2011. [Google Scholar]
  63. Martikainen, A. Kaustisen–Ullavan Regional Geochemical Features and Source Granitoids of the Lithium Pegmatites of Kaustinen-Ullava. Master’s Thesis, University of Helsinki, Helsinki, Finland, 2012; p. 77. (in Finnish). [Google Scholar]
  64. Hanski, E.; Huhma, H.; Vuollo, J. SIMS zircon ages and Nd isotope systematics of the 2.2 Ga mafic intrusions in northern and eastern Finland. Bull. Geol. Soc. Finl. 2010, 82, 31–62. [Google Scholar] [CrossRef]
  65. Solli, A. Precambrian Stratigraphy in the Masi Area, Southwestern Finnmark, Norway. Norges geol. Unders. 1983, 380, 97–105. [Google Scholar]
  66. Henderson, I.H.; Viola, G.; Nasuti, A. A new tectonic model for the Palaeoproterozoic Kautokeino Greenstone Belt, northern Norway, based on high-resolution airborne magnetic data and field structural analysis and implications for mineral potential. Nor. J. Geol. 2015, 95, 339–363. [Google Scholar] [CrossRef] [Green Version]
  67. Steiner, B.M. Tools and workflows for grassroots Li–Cs–Ta (LCT) pegmatite exploration. Minerals 2019, 9, 499. [Google Scholar] [CrossRef] [Green Version]
  68. Vrevskii, A.B. Age and sources of the anorthosites of the Neoarchean Kolmozero-Voron’ya greenstone belt (Fennoscandian Shield). Petrology 2016, 24, 527–542. [Google Scholar] [CrossRef]
  69. Thompson, A.B. Calculation of muscovite-paragonite-alkali feldspar phase relations. Contrib. Mineral. Petrol. 1974, 44, 173–194. [Google Scholar] [CrossRef]
  70. Ambrosio, M.R.; Azzone, R.G. The Influence of Crystal and Melt Compositions On the Ree+y Partitioning Between Clinopyroxene and Basanitic/tephritic Melts of Cretaceous Alkaline Magmatism On the Southeastern Part of the South American Platform, Southeast Brazil. Can. Mineral. 2018, 56, 303–329. [Google Scholar] [CrossRef]
  71. Deer, W.A.; Howie, R.A.; Zussman, J. An Introduction to the Rock-Forming Minerals, 2nd ed.; Pearson: Harlow, UK, 1992. [Google Scholar]
  72. Schliestedt, M. Phasengleichgewichte in Hochdruckgesteinen von Sifnos, Griechenland. Ph.D. Thesis, Technische Universität Braunschweig, Braunschweig, Germany, 1980. [Google Scholar]
  73. Tappert, M.C.; Rivard, B.; Giles, D.; Tappert, R.; Mauger, A. The mineral chemistry, near-infrared, and mid-infrared reflectance spectroscopy of phengite from the Olympic Dam IOCG deposit, South Australia. Ore Geol. Rev. 2013, 53, 26–38. [Google Scholar] [CrossRef]
  74. Liu, W.; Zhang, S.; Wang, W.; Zhang, J.; Yan, W.; Deng, J.; Feng, Q.; Huang, Y. The effects of Ca (II) and Mg (II) ions on the flotation of spodumene using NaOL. Miner. Eng. 2015, 79, 40–46. [Google Scholar] [CrossRef]
  75. Ion Radius. Available online: http://www.chemmix.edu.pl/artnet/print.php?s1=03&s2=004&s3=000 (accessed on 20 February 2023).
  76. Bloise, A.; Pingitore, V.; Miriello, D.; Apollaro, C.; Armentano, D.; Barrese, E.; Oliva, A. Flux growth and characterization of Ti-and Ni-doped enstatite single crystals. J. Cryst. Growth 2011, 329, 86–91. [Google Scholar] [CrossRef]
  77. Bronzite IR spectra: Bronzite R040093, RRUFF Database: Raman, X-ray, Infrared, and Chemistry. Available online: https://rruff.info/bronzite/R040093 (accessed on 20 February 2023).
  78. Zhang, Y.; Shi, G. Origin of Blue-Water Jadeite Jades from Myanmar and Guatemala: Differentiation by Non-Destructive Spectroscopic Techniques. Crystals 2022, 12, 1448. [Google Scholar] [CrossRef]
  79. Muscovite IR Spectra. Available online: https://rruff.info/Muscovite/R040108 (accessed on 20 February 2023).
  80. Vieceli, N.; Nogueira, C.A.; Pereira, M.F.; Dias, A.P.S.; Durão, F.O.; Guimarães, C.; Margarido, F. Effects of mechanical activation on lithium extraction from a lepidolite ore concentrate. Miner. Eng. 2017, 102, 1–14. [Google Scholar] [CrossRef]
  81. Juchem, P.L.; de Brum, T.M.M.; Fischer, A.C.; Balzaretti, N.M.; Augustin, A.H. Fuchsite quartzite as an imitation of emerald. J. Gemmol. -Lond. 2006, 30, 207. [Google Scholar] [CrossRef]
  82. Navas, A.S.; Reddy, B.J.; Nieto, F. Spectroscopic study of chromium, iron, OH, fluid and mineral inclusions in uvarovite and fuchsite. Spectrochim. Acta Part A Mol. Biomol. Spectrosc. 2004, 60, 2261–2268. [Google Scholar] [CrossRef]
  83. Takasawa, K.; Sakae, T.; Tateyama, H. Nickeliferous fuchsite in the quartz-magnesite rock from the Setogawa Group. Japan. Clay Sci. 1976, 5, 57–65. [Google Scholar]
  84. Sartori, F.; Franzini, M.; Merlino, S. Crystal structure of a 2M2 lepidolite. Acta Crystallogr. Sect. B: Struct. Crystallogr. Cryst. Chem. 1973, 29, 573–578. [Google Scholar] [CrossRef]
  85. Sartori, F. The crystal structure of a 2 M 1 lepidolite. Tschermaks Mineral. Und Petrogr. Mitteilungen 1977, 24, 23–37. [Google Scholar] [CrossRef]
  86. Brown, B.E. The crystal structure of a 3lepidolite. Am. Mineral. 1978, 63, 332–336. [Google Scholar]
  87. Takeda, H.; Haga, N.; Sadanaga, R. Structural investigation of polymorphic transition between 2M2-, 1M-lepidolite and 2M1 muscovite. Mineral. J. 1971, 6, 203–215. [Google Scholar] [CrossRef] [Green Version]
  88. He, G.C.; Xiang, H.M.; Jiang, W.; Kang, Q.; Chen, J.H. First-principles theory on electronic structure and floatability of spodumene. Rare Met. 2014, 33, 742–748. [Google Scholar] [CrossRef]
  89. Moon, K.S.; Fuerstenau, D.W. Surface crystal chemistry in selective flotation of spodumene (LiAl [SiO3] 2) from other aluminosilicates. Int. J. Miner. Process. 2003, 72, 11–24. [Google Scholar] [CrossRef]
  90. Prewitt, C.T.; Burnham, C.W. The crystal structure of jadeite, NaAlSi2O6. Am. Mineral. J. Earth Planet. Mater. 1966, 51, 956–975. [Google Scholar]
  91. Nestola, F.; Tribaudino, M.; Boffa Ballaran, T.; Liebske, C.; Bruno, M. The crystal structure of pyroxenes along the jadeite–hedenbergite and jadeite–aegirine joins. Am. Mineral. 2007, 92, 1492–1501. [Google Scholar] [CrossRef]
  92. Pripachkin, P.V.; Kudryashov, N.M.; Rundkvist, T.V.; Morozova, L.N. Lithium in pegmatites of the Fennoscandian Shield and operation prospects for the Kolmozero deposit on the Kola Peninsula (Russia). Appl. Earth Sci. 2022, 131, 179–192. [Google Scholar] [CrossRef]
  93. Ghisler, M. Fuchsite and chrome-epidote from Fiskenæsset. Rapp. Grønlands Geol. Undersøgelse 1976, 73, 67–69. [Google Scholar] [CrossRef]
  94. Gordienko, V.V.; Gordienko, V.V.; Sergeev, A.S.; Levskii, L.K.; Lokhov, K.I.; Kapitonov, I.N.; Sergeev, S.A. First data in favor of the crystallization model of lithium isotope fractionation in the pegmatitic process. Dokl. Earth Sci. 2007, 413, 441. [Google Scholar] [CrossRef]
  95. Pekov, I.V.; Kononkova, N.N. Rubidium mineralization in rare-element granitic pegmatites of the Voron’i tundras, Kola Peninsula, Russia. Geochem. Int. 2010, 48, 695–713. [Google Scholar] [CrossRef]
  96. Mueller, M.; Peltonen, P.; Eilu, P.; Goldfarb, R.; Hanski, E. The Mustajärvi orogenic gold occurrence, Central Lapland Greenstone Belt, Finland: A telluride-dominant mineral system. Miner. Depos. 2020, 55, 1625–1646. [Google Scholar] [CrossRef]
  97. Ettner, D.C.; Bjørlykke, A.; Andersen, T. A fluid inclusion and stable isotope study of the Proterozoic Bidjovagge Au-Cu deposit, Finnmark, northern Norway. Miner. Depos. 1994, 29, 16–29. [Google Scholar] [CrossRef]
  98. Bradley, D.C.; McCauley, A. A Preliminary Deposit Model for Lithium-Cesium-Tantalum (LCT) Pegmatites; US Department of the Interior, US Geological Survey: Reston, VA, USA, 2013. [Google Scholar] [CrossRef]
  99. El-Enen, M.A.; Okrusch, M.; Will, T.M. Metapelitic assemblages in the Umm Zariq schists, central western Kid belt, Sinai Peninsula, Egypt. Neues Jahrb. Mineralogie. Abh. 2003, 178, 277–306. [Google Scholar] [CrossRef]
  100. Maxwell, P.; Mora, M. Lithium and Chile: Looking back and looking forward. Miner. Econ. 2020, 33, 57–71. [Google Scholar] [CrossRef]
  101. Beskin, S.M.; Marin, Y.B. Granite systems with rare-metal pegmatites. Geol. Ore Depos. 2020, 62, 554–563. [Google Scholar] [CrossRef]
  102. Kudryashov, N.M.; Petrovsky, M.N.; Mokrushin, A.V.; Elizarov, D.V. Neoarchean sanukitoid magmatism in the Kola region: Geological, petrochemical, geochronological, and isotopic-geochemical data. Petrology 2013, 21, 351–374. [Google Scholar] [CrossRef]
Materials 16 04894 g001 550
Figure 1. Simplified geological–tectonic map of N Scandinavia (after [37]) with the sample locations.
Figure 1. Simplified geological–tectonic map of N Scandinavia (after [37]) with the sample locations.
Materials 16 04894 g001
Materials 16 04894 g002 550
Figure 2. Macroscopic images of rocks under investigation. Schist with fuchsite from Kautokeino (A), pegmatite with lepidolite from Kaustinen (B), and pegmatite from Kolmozero with spodumene (C) and lepidolite (D). Abbreviations: fu—fuchsite, sp—spodumene, lp—lepidolite, qtz—quartz, mu—muscovie, pl—plagioclase, or—orthoclase.
Figure 2. Macroscopic images of rocks under investigation. Schist with fuchsite from Kautokeino (A), pegmatite with lepidolite from Kaustinen (B), and pegmatite from Kolmozero with spodumene (C) and lepidolite (D). Abbreviations: fu—fuchsite, sp—spodumene, lp—lepidolite, qtz—quartz, mu—muscovie, pl—plagioclase, or—orthoclase.
Materials 16 04894 g002
Materials 16 04894 g003 550
Figure 3. Mineral composition of trioctahedral micas from Kautokeino schists. The element content is expressed in wt.%. The yellow area represents the composition of the most frequent, naturally occurring biotites [71].
Figure 3. Mineral composition of trioctahedral micas from Kautokeino schists. The element content is expressed in wt.%. The yellow area represents the composition of the most frequent, naturally occurring biotites [71].
Materials 16 04894 g003
Materials 16 04894 g004 550
Figure 4. Type of dioctahedral micas examined in the discussed rocks (based on [72,73], modified by the authors). The element content is expressed in wt.%.
Figure 4. Type of dioctahedral micas examined in the discussed rocks (based on [72,73], modified by the authors). The element content is expressed in wt.%.
Materials 16 04894 g004
Materials 16 04894 g005 550
Figure 5. Microphotographs of spodumene (sp) from Kaustinen under transmitted light (A) and polarized light (B) accompanying quartz (qtz) and muscovite (mu) crystals.
Figure 5. Microphotographs of spodumene (sp) from Kaustinen under transmitted light (A) and polarized light (B) accompanying quartz (qtz) and muscovite (mu) crystals.
Materials 16 04894 g005
Materials 16 04894 g006 550
Figure 6. Microphotographs of lepidolite (lp) from Kolmozero under transmitted light (A) and polarized light (B) with quartz (qtz).
Figure 6. Microphotographs of lepidolite (lp) from Kolmozero under transmitted light (A) and polarized light (B) with quartz (qtz).
Materials 16 04894 g006
Materials 16 04894 g007 550
Figure 7. Microphotographs of fuchsite (fu) from Kautoteino under transmitted light (A) and polarized light (B) near biotite (bt) and quartz (qtz) crystals.
Figure 7. Microphotographs of fuchsite (fu) from Kautoteino under transmitted light (A) and polarized light (B) near biotite (bt) and quartz (qtz) crystals.
Materials 16 04894 g007
Materials 16 04894 g008 550
Figure 8. IR spectrum for the Kaustinen spodumene.
Figure 8. IR spectrum for the Kaustinen spodumene.
Materials 16 04894 g008
Materials 16 04894 g009 550
Figure 9. IR spectra for lepidolite (A) and fuchsite (B).
Figure 9. IR spectra for lepidolite (A) and fuchsite (B).
Materials 16 04894 g009
Materials 16 04894 g010 550
Figure 10. XPS spectrum for fuchsite.
Figure 10. XPS spectrum for fuchsite.
Materials 16 04894 g010
Materials 16 04894 g011 550
Figure 11. Crystal structure of the fuchsite from the analyzed rocks, as received by the authors (a, b, c—the main structural axes).
Figure 11. Crystal structure of the fuchsite from the analyzed rocks, as received by the authors (a, b, c—the main structural axes).
Materials 16 04894 g011
Materials 16 04894 g012 550
Figure 12. XPS spectra obtained for lepidolite from the studied rocks.
Figure 12. XPS spectra obtained for lepidolite from the studied rocks.
Materials 16 04894 g012
Materials 16 04894 g013 550
Figure 13. Crystal structure of lepidolite from the studied lithologies (a, b, c—the main structural axes).
Figure 13. Crystal structure of lepidolite from the studied lithologies (a, b, c—the main structural axes).
Materials 16 04894 g013
Materials 16 04894 g014 550
Figure 14. XPS spectra were obtained for spodumene from the studied rocks.
Figure 14. XPS spectra were obtained for spodumene from the studied rocks.
Materials 16 04894 g014
Materials 16 04894 g015 550
Figure 15. Crystal structure of spodumene (a, b, c—the main structural axes).
Figure 15. Crystal structure of spodumene (a, b, c—the main structural axes).
Materials 16 04894 g015
Table
Table 1. Single crystals’ X-ray diffraction results for all studied minerals.
Table 1. Single crystals’ X-ray diffraction results for all studied minerals.
MineralFuchsiteLepidoliteSpodumene
Empirical formulaAl1.63Cr0.37KSi4O12.1Al2Fe0.93H0.25LiSi4O12.12Al2Li2Si4O12
Temperature/K294294294
Crystal systemmonoclinicmonoclinicmonoclinic
Space groupC2/cC2/cI2/a
a/Å5.2149(1)5.2037(2)5.2204(1)
b/Å9.0505(2)9.0250(4)8.3947(2)
c/Å20.0457(5)20.1588(8)9.0993(2)
α/°909090
β/°95.78(1)95.52(1)102.40(1)
γ/°909090
Volume/Å3941.29(4)942.32(7)389.462(17)
Z442
ρcalcg/cm32.8812.9563.174
Crystal size/mm30.6 × 0.6 × 0.080.4 × 0.3 × 0.050.3 × 0.2 × 0.1
Data/restraints/parameters844/0/89854/0/98344/0/48
Goodness-of-fit on F21.0811.1111.113
Final R indexes [I ≥ 2σ (I)]R1 = 0.0530,
wR2 = 0.1444		R1 = 0.0712,
wR2 = 0.2039		R1 = 0.0184,
wR2 = 0.0553
Largest diff. peak/hole/e Å−30.88/−0.790.88/−1.400.28/−0.26
Disclaimer/Publisher’s Note: The statements, opinions and data contained in all publications are solely those of the individual author(s) and contributor(s) and not of MDPI and/or the editor(s). MDPI and/or the editor(s) disclaim responsibility for any injury to people or property resulting from any ideas, methods, instructions or products referred to in the content.

Share and Cite

MDPI and ACS Style

Huber, M.; Kamiński, D.M.; Maciołek, U. The Optical and Spectroscopic Properties of Fuchsite, Spodumene, and Lepidolite from Northern Scandinavia (Kautokeino, Kaustinen, Kolmozero). Materials 2023, 16, 4894. https://doi.org/10.3390/ma16144894

AMA Style

Huber M, Kamiński DM, Maciołek U. The Optical and Spectroscopic Properties of Fuchsite, Spodumene, and Lepidolite from Northern Scandinavia (Kautokeino, Kaustinen, Kolmozero). Materials. 2023; 16(14):4894. https://doi.org/10.3390/ma16144894

Chicago/Turabian Style

Huber, Miłosz, Daniel M. Kamiński, and Urszula Maciołek. 2023. "The Optical and Spectroscopic Properties of Fuchsite, Spodumene, and Lepidolite from Northern Scandinavia (Kautokeino, Kaustinen, Kolmozero)" Materials 16, no. 14: 4894. https://doi.org/10.3390/ma16144894

Note that from the first issue of 2016, this journal uses article numbers instead of page numbers. See further details here.

Article Metrics

Back to TopTop