Grzegorz Gil | University of Warsaw (original) (raw)
Papers by Grzegorz Gil
Ore Geology Reviews
The Gilów deposit is located in the Góry Sowie Massif of the Central Sudetes (NE Bohemian Massif,... more The Gilów deposit is located in the Góry Sowie Massif of the Central Sudetes (NE Bohemian Massif, SW Poland). Talcose rocks are associated with serpentinite bodies hosted by country migmatitic paragneiss, in an area where paragneiss also hosts amphibolitized eclogite bodies and granitic pegmatite veins. The talcose rocks and wall rocks were subjected to petrographic examination, electron microprobe study of minerals (including monazite Th-U-total Pb chemical dating), bulk rock chemical examination, as well as stable O, H and Cl isotope analysis. The talcose rocks can be used as a carving material and in ceramics, although the presence of tremolite and anthophyllite, and high Cr and Ni contents, preclude application in pharmacy and cosmetics. High Cr (2121.0–2148.4 ppm), Ni (1079–1561 ppm) and Co (57.4–84.8 ppm) contents, low ΣREE (2.13–13.81 ppm), as well as isotopic composition of O and H, classify the talcose rocks as a serpentinite-hosted type of deposit. Location in the strongly folded metamorphic unit, in the intimate vicinity of several faults and mylonitic zones, implies classification along the thrust-bound and fold-related metamorphogenic deposits. The talcose rocks are separated from serpentinites by the metasomatic chlorite schist, which contains two generations of monazite yielding two, different Th-U-total Pb dates. Older (389.8 ± 11.4 Ma) probably dates serpentinites juxtaposition with country paragneiss and chlorite formation. Younger (365.0 ± 18.2 Ma) likely dates amphiboles and talc formation, as overlaps the ages of amphibolite facies, country paragneiss migmatitization and intrusions of granitic pegmatites, and the talcose rocks contain talc-tremolite-anthophyllite assemblage indicative of the low-pressure mid-amphibolite facies. High MgO (24.27–27.21 wt%), Fe2O3 (5.06–5.12 wt%), Cr, Ni and Co contents are inherited from serpentinites. On the other hand, SiO2 (57.30–60.46 wt%), CaO (0.86–4.39 wt%), Al2O3 (1.38–3.04 wt%), TiO2 (0.02–0.04 wt%) and F (197–337 ppm) contents in the talcose rocks are higher than in host-serpentinites, likely due to a metasomatic introduction by fluids derived from migmatitic paragneisses or intruding pegmatites. Introduction of these elements is evidenced by a negative δ37Cl and elevated δ18O of the talcose rocks relative to host-serpentinites that are typical effects of interaction with a felsic crustal material. Interaction with paragneiss- and pegmatite-derived fluids is further evidenced by REE and trace elements patterns of the talcose rocks. The LREE/HREE enrichment, negative Sr and Ti anomalies, and positive Nb-La and Zr-Hf-Sm slopes, of the talcose rocks patterns, are similar as in paragneiss and pegmatite. Serpentinite bodies transformation into the talcose rocks was gradual and associated with increase of δ18O, and decrease of a Cl content, δD and δ37Cl. Pseudomorphic serpentinite, similar to abyssal serpentinites in terms of an isotopic composition (δ18O = +5.7‰, δD = –64‰, δ37Cl = +2.0‰), recrystallized into non-pseudomorphic serpentinite (δ18O = +7.1‰, δD = –48‰, δ37Cl = –0.1‰), which, in turn, was replaced by the talcose rock (δ18O = +8.3‰ to +8.7‰, δD = –52‰ to –48‰, δ37Cl = –2.6‰ to –0.1‰). Moreover, paragneiss- and pegmatite-derived fluids might have interacted with eclogite bodies during amphibolite facies-retrogression. Amphibolitized eclogite has Cl-rich amphibole rims, and negative δ37Cl (–0.5‰) consistent with a Cl-rich crustal fluid.
Ore Geology Reviews, 2022
The Gilów deposit is located in the Góry Sowie Massif of the Central Sudetes (NE Bohemian Massif,... more The Gilów deposit is located in the Góry Sowie Massif of the Central Sudetes (NE Bohemian Massif, SW Poland). Talcose rocks are associated with serpentinite bodies hosted by country migmatitic paragneiss, in an area where paragneiss also hosts amphibolitized eclogite bodies and granitic pegmatite veins. The talcose rocks and wall rocks were subjected to petrographic examination, electron microprobe study of minerals (including monazite Th-U-total Pb chemical dating), bulk rock chemical examination, as well as stable O, H and Cl isotope analysis. The talcose rocks can be used as a carving material and in ceramics, although the presence of tremolite and anthophyllite, and high Cr and Ni contents, preclude application in pharmacy and cosmetics. High Cr (2121.0–2148.4 ppm), Ni (1079–1561 ppm) and Co (57.4–84.8 ppm) contents, low ΣREE (2.13–13.81 ppm), as well as isotopic composition of O and H, classify the talcose rocks as a serpentinite-hosted type of deposit. Location in the strongly folded metamorphic unit, in the intimate vicinity of several faults and mylonitic zones, implies classification along the thrust-bound and fold-related metamorphogenic deposits. The talcose rocks are separated from serpentinites by the metasomatic chlorite schist, which contains two generations of monazite yielding two, different Th-U-total Pb dates. Older (389.8 ± 11.4 Ma) probably dates serpentinites juxtaposition with country paragneiss and chlorite formation. Younger (365.0 ± 18.2 Ma) likely dates amphiboles and talc formation, as overlaps the ages of amphibolite facies, country paragneiss migmatitization and intrusions of granitic pegmatites, and the talcose rocks contain talc-tremolite-anthophyllite assemblage indicative of the low-pressure mid-amphibolite facies. High MgO (24.27–27.21 wt%), Fe2O3 (5.06–5.12 wt%), Cr, Ni and Co contents are inherited from serpentinites. On the other hand, SiO2 (57.30–60.46 wt%), CaO (0.86–4.39 wt%), Al2O3 (1.38–3.04 wt%), TiO2 (0.02–0.04 wt%) and F (197–337 ppm) contents in the talcose rocks are higher than in host-serpentinites, likely due to a metasomatic introduction by fluids derived from migmatitic paragneisses or intruding pegmatites. Introduction of these elements is evidenced by a negative δ37Cl and elevated δ18O of the talcose rocks relative to host-serpentinites that are typical effects of interaction with a felsic crustal material. Interaction with paragneiss- and pegmatite-derived fluids is further evidenced by REE and trace elements patterns of the talcose rocks. The LREE/HREE enrichment, negative Sr and Ti anomalies, and positive Nb-La and Zr-Hf-Sm slopes, of the talcose rocks patterns, are similar as in paragneiss and pegmatite. Serpentinite bodies transformation into the talcose rocks was gradual and associated with increase of δ18O, and decrease of a Cl content, δD and δ37Cl. Pseudomorphic serpentinite, similar to abyssal serpentinites in terms of an isotopic composition (δ18O = +5.7‰, δD = –64‰, δ37Cl = +2.0‰), recrystallized into non-pseudomorphic serpentinite (δ18O = +7.1‰, δD = –48‰, δ37Cl = –0.1‰), which, in turn, was replaced by the talcose rock (δ18O = +8.3‰ to +8.7‰, δD = –52‰ to –48‰, δ37Cl = –2.6‰ to –0.1‰). Moreover, paragneiss- and pegmatite-derived fluids might have interacted with eclogite bodies during amphibolite facies-retrogression. Amphibolitized eclogite has Cl-rich amphibole rims, and negative δ37Cl (–0.5‰) consistent with a Cl-rich crustal fluid.
Ore Geology Reviews, 2022
Ore Geology Reviews, 2020
Abstract Nephrites belonging to both the dolomite-related and serpentinite-related genetic types,... more Abstract Nephrites belonging to both the dolomite-related and serpentinite-related genetic types, from the Zloty Stok deposit, and Jordanow Śląski and Naslawice prospects in the Śleza Ophiolite, respectively, were analyzed for Fe and Sr isotope compositions. These deposits in the Central Sudetes (SW Poland), are unusually situated relatively close to each other. This study is a first attempt to perform combined Fe and Sr isotope study of nephrites. Our results show that Fe in the Fe-As-Au-bearing skarn samples from Zloty Stok (2.77-7.00 wt.% Fe, δ56Fe +0.07 to +0.14‰, and δ57Fe +0.12 to +0.21‰), to which the dolomite-related nephrite belongs, is not inherited from the host dolomitic marbles (ca. 0.4 wt.% Fe; δ56Fe -0.08 to -0.07‰, and δ57Fe -0.12 to -0.09‰), but derived from the nearby, ca. 340 Ma granite intrusion (2.64-5.64 wt.% Fe). In contrast, iron in the serpentinite-related nephrites (2.06-3.88 wt.% Fe, δ56Fe +0.41 to +0.45‰, and δ57Fe +0.59 to +0.66‰) was likely inherited from host serpentinites (5.27-4.81 wt.% Fe), rather than metasomatically derived from adjacent granite intrusions (0.13-0.45 wt.% Fe). Moreover, both the marble transformation into a dolomite-related nephrite (and Fe-As-Au-bearing skarn), and the abyssal serpentinite – through ophiolite – towards serpentinite-related nephrite transformation, are accompanied by a progressive increase of δ56Fe and δ57Fe. This increase is regardless of changes in the bulk Fe content, increasing during the dolomite-related nephrite formation, and decreasing during serpentinite-related nephrite formation. This phenomena may be caused by one of the below listed factors, or combinations: a) preferential incorporation of heavy iron by tremolite and diopside; b) preferential incorporation of the heavy iron in the Fe3+-bearing phases, crystallizing during nephrite formation; c) preferential incorporation of the heavy Fe from migrating granite-derived fluids (positive fractionation between aqueous Fe-bearing fluid, and tremolite/diopside); d) positive isotope fractionation between dolomite/antigorite precursor, and newly formed amphibole/clinopyroxene; e) change of the Fe oxidation state. Furthermore, Fe in the rock-forming tremolite from the serpentinite-related nephrites is isotopically heavier than Fe in tremolite from the dolomite-related ones. In contrast to the iron, the isotopic composition of strontium, combined with its content and structural evidence, suggest multiple sources for this element. In the case of the dolomite-related nephrite (ca. 3-4 ppm Sr; initial 87Sr/86Sr = 0.7085), Sr inheritance from the host-dolomitic marble (ca. 90 ppm Sr; initial 87Sr/86Sr = 0.7081), as well as its derivation from intrusions of both the syn- to late-tectonic, ca. 340 Ma granites (ca. 400-440 ppm Sr), and post-tectonic ∼305 Ma granites (86.4 ppm Sr), is suggested. In the case of the serpentinite-related nephrite (6.3-61.7 ppm Sr; initial 87Sr/86Sr 0.7037 to 0.7081), the situation is similar, i.e., Sr in the most primitive samples tends to be sourced from ophiolitic rocks (up to 2.4 ppm Sr in serpentinite), whereas in the more evolved types, it was likely delivered from the adjacent, ca. 340 Ma (8.8-102.6 ppm Sr) partially rodingitized granites, as well as ∼305 Ma granites (ca. 80 ppm Sr). Moreover, these granites caused the fluid-flow, responsible for Sr-bearing clinozoisite vein formation; these veins are likely related with nephrite formation, and with a metallic mineralization.
Minerals, 2019
The Kletno deposit in the Śnieżnik Massif (Central Sudetes, SW Poland), mined for Fe, U, Ag, Cu, ... more The Kletno deposit in the Śnieżnik Massif (Central Sudetes, SW Poland), mined for Fe, U, Ag, Cu, fluorite, and marble through the ages, developed at the contact of marbles and orthogneiss. Here, we present a new Fe-Ti-V-ore (containing up to 14.07 wt.% Fe, 2.05 wt.% Ti, and 2055 ppm V in bulk rock) and ornamental- to gem-quality talc prospect at the southwest margin of this deposit. This newly documented Fe-Ti-V mineralization is hosted in hornblendites, dolomite veins, and chlorite schists, which, along with talc, envelopes a tectonic slice of serpentinite. Hornblendites are interpreted as metamorphosed ferrogabbros, derived from the same mafic melts as adjacent barren metagabbros. The oxygen and carbon isotope compositions of metabasites and dolomite veins (amphibole δ18O values = 8.8–9.3‰; carbonate δ18O values = 12.8–16.0‰, and δ13C values = −8.3‰ to −7.2‰), in combination with those of the country marbles (carbonate δ18O and δ13C values = 23.2‰ and +0.1‰, respectively), suggest...
Journal of Molecular Structure, 2018
Abstract Raman and infrared spectroscopy are fast, simple and useful methods of identifying and d... more Abstract Raman and infrared spectroscopy are fast, simple and useful methods of identifying and distinguishing between different rock samples, which often originate from different sources. We analyzed nephrite samples from Polish deposits (Zloty Stok in the Sudetes and Jordanow Śląski in the Fore-Sudetic Block). Studied nephrites amphiboles, with the general formula (Ca2(Mg,Fe)5Si8O22(OH)2), magnesium and iron contents, in terms of Fe/(Fe+Mg) per formula unit, are as follows: Jordanow Śląski (0.06–0.10), Zloty Stok type 1 (0.10–0.20) and Zloty Stok type 2 (0.04–0.18). Our spectroscopic study is consistent with results of previous petrographic microscopy, scanning electron microscopy and chemical composition of constituting minerals, measured by the electron microprobe; which methods were applied to the same nephrite deposits. Results of Jordanow and Zloty Stok nephrites studies were compared with data available in literature, which confirmed petrographic composition of studied samples. In addition, in case of actinolite nephrite samples (Fe/(Fe+Mg) > 0.10), qualification of the studied minerals to actinolite with content of Fe ion below 15% and 30% in sample from Jordanow Śląski and Zloty Stok, respectively, is possible based solely on applied spectroscopic methods. Spectroscopic studies also allowed to note the relationship between the obtained results and the genetic origin (serpentinite-related or dolomite-related) of the studied nephrites. Findings confirmed that spectroscopic methods are not only applicable and useful, but, which is very important in gemological and archaeometric practice, also non-destructive.
The Canadian Mineralogist, 2015
The Zloty Stok Au-As deposit (SW Poland) hosts two distinct nephrite varieties: ‘type 1’ – a gray... more The Zloty Stok Au-As deposit (SW Poland) hosts two distinct nephrite varieties: ‘type 1’ – a grayish green or pale green, translucent, with waxy to greasy luster nephrite composed of actinolite and abundant lollingite; ‘type 2’ – a deep or intense green, less-translucent, with sub-vitreous to dull luster nephrite composed of tremolite and actinolite, with rare lollingite and arsenopyrite. ‘Nephrite type 1’ shows evidence for more intense metasomatism and recrystallization than ‘type 2’, e.g. , more abundant arsenide, sulfosalt, and tungstate minerals, and higher Fe, As, and Co concentrations. The tremolite and actinolite in both types formed at the expense of dolomite—either directly from dolomite or through diopside formation. Calcite is a byproduct of the amphiboles' formation directly from dolomite. Amphiboles have Cr2O3 and NiO concentrations of 0.00–0.04 wt.% and 0.00 wt.%, respectively, typical of dolomite-related nephrites. Diopside composition (up to 51 Wo, 0.00–0.05 wt.% Cr2O3 and 0.00–0.09 wt.% NiO) is similar to other dolomite-related nephrite compositions. Bulk-rock Cr and Ni (<30 ppm and <40 ppm, respectively) and Co, which is less affected by ore mineralization (<10 ppm), are similar to the values in dolomite-related nephrite. Yellow cathodoluminescent diopside is similar to that in other metasomatized dolomitic marbles. Nephrite has δ18O values ranging from +8.3 to +10.4‰ (precision = ±0.1‰), higher than in other typical dolomite-related nephrite. δD values range from –77 to –75‰, similar to the dolomite-related type. Based on these observations, we interpret the Zloty Stok nephrite deposit to have formed as a metasomatic replacement of dolomitic marble. This is the third documented case of a dolomite-related origin (para-nephrite) for nephrite in Europe. Furthermore, the dolomite-related nephrite adds the Lower Silesian Sudetes and its Foreland to rare areas like Wyoming, southern Siberia, China, Korea, and the Alps, where both dolomite-related and serpentinite-related nephrites occur. The Zloty Stok nephrite formed via at least two crystallization events. In the first event, quartz veins and nephrite formed, and the paragenesis included quartz, tremolite, Fe-poor actinolite, Fe-poor diopside and, probably, arsenopyrite. In the second event, Si-depleted actinolite, Fe-enriched diopside, and lollingite formed, and the earlier arsenopyrite was replaced by calcite. The crystallization path reflects progressive metamorphism ( i.e. , temperature rise) or change in the saturation conditions, e.g. , silica and sulfur activity in the fluid. The nephrite formation can be linked with the emplacement and cooling of the neighboring Variscan Klodzko-Zloty Stok granite at ca. 340–298 Ma.
Geological Quarterly., 2015
Geological Quarterly, 2014
![Research paper thumbnail of Detailed descriptions of the possible source regions in the Swiss Alps and in the Bohemian Massif [in square brackets: short description of the once (bulk-rock chemically) measured ˮnephriteˮ sample from the given site]](https://attachments.academia-assets.com/84055260/thumbnails/1.jpg)
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Lower Silesia hosts im por tant Eu ro pean neph rite de pos its of Jordanów and less-known of Zot... more Lower Silesia hosts im por tant Eu ro pean neph rite de pos its of Jordanów and less-known of Zoty Stok. Neph rite ar ti facts were dis cov ered in ar chae o log i cal sites dated back to the Neo lithic pe riod, across Eur asia. Es pe cially ar ti facts found in Po land, It-aly and Bul garia may orig i nate from Pol ish nephrites. Now a days, only one ar ti fact is pre cisely linked to Jordanów. Petrographic study of nephrites and chem i cal anal y ses of con stit u ents by means of EMPA al low ac cu rate iden ti fi ca tion of the nephrites. The char ac ter is tic phases of Jordanów tremolite neph rite are ro tated and cataclased di op side porphyroblasts with pres sure shad ows, chlorite lay ers and nests with in ter lock ing non-pseudomorphic tex ture and prehnite veins. The pres ence of hydrogrossular, grossular, ti tan ite, ap a tite with monazite in clu sions, and zir con with pleochroic haloe is typ i cal. Chlorites are usu ally rep re sented by penninite, and mi nor clinochlo...
The As-bearing minerals from the contact aureole of K odzko-Z oty Stok granitoid Intrusion Unit (... more The As-bearing minerals from the contact aureole of K odzko-Z oty Stok granitoid Intrusion Unit (Sudetes Mts) are known since medieval ages. The main As-ore bearing minerals in this deposit are arsenopyrite and lollingite (J !drzejewska, Sa aci "ski 1997). Nephrite occurs there occasionally, forming thin veins within pyroxenites. The microprobe study of the As-ore minerals from the Z oty Stok nephrites was the main goal of this research. After the field sampling, the conventional petrographic studies were made and some samples were marked out for microprobe analysis . The 18 electron microprobe analyses of the As-ore bearing minerals were carried out using the Cameca SX 100 microprobe analyzer in the Microscopy and Microprobe Laboratory at the Warsaw University,. The obtained results showed that the As-ore bearing minerals from Z oty Stok
Fe and Sr isotopic data of nephrite, clinopyroxenite and dolomitic marble.
Nephrite is mainly known in prehistoric context as raw material for polished stone tools. It is p... more Nephrite is mainly known in prehistoric context as raw material for polished stone tools. It is present among archaeological finds in Hungary only in a few numbers. They are known mostly from Transdanubian archaeological sites. The general aim of our investigations is the detailed petrographic and geochemical examination of the nephrite artefacts found on Hungarian sites, and locating the origin of the raw materials. The material was basically investigated by non-destructive methods (PGAA, non-destructive SEM-EDX) to avoid invasive analyses on the complete artefacts. In this study, preliminary results are presented. Based on their chemical composition, most of the artefacts measured so far belong to the S-type (serpentiniterelated) nephrite deposits. On the basis of their microscopic and mineral-chemical features, the artefacts investigated so far can be divided into five raw material types: (1) almost pure tremolite-nephrite with only a few fine grained magnetite or ilmenite grains...
9th International Conference Mineralogy and Museums, 2021
Nephrite artefacts are rare discoveries in archeological sites dated back to early Neolithic. Pre... more Nephrite artefacts are rare discoveries in archeological sites dated back to early Neolithic. Precise identification of the raw material source provides valuable information about the past mining activity, as well as migration and trade routes due to rarity of nephrite deposits. Serpentinite-related nephrite occurrences from Jordanów Śląski and Nasławice in the Ślęża Ophiolite, and dolomite-related nephrite from the Złoty Stok deposit in the Śnieżnik Massif, were selected for investigation focused at documentation of unique features, allowing unequivocal identification of the raw material source. Both nephrite deposits are located relatively close each other, in the Central Sudetes terrane (SW Poland) of the European Variscan Belt.
Ore Geology Reviews
The Gilów deposit is located in the Góry Sowie Massif of the Central Sudetes (NE Bohemian Massif,... more The Gilów deposit is located in the Góry Sowie Massif of the Central Sudetes (NE Bohemian Massif, SW Poland). Talcose rocks are associated with serpentinite bodies hosted by country migmatitic paragneiss, in an area where paragneiss also hosts amphibolitized eclogite bodies and granitic pegmatite veins. The talcose rocks and wall rocks were subjected to petrographic examination, electron microprobe study of minerals (including monazite Th-U-total Pb chemical dating), bulk rock chemical examination, as well as stable O, H and Cl isotope analysis. The talcose rocks can be used as a carving material and in ceramics, although the presence of tremolite and anthophyllite, and high Cr and Ni contents, preclude application in pharmacy and cosmetics. High Cr (2121.0–2148.4 ppm), Ni (1079–1561 ppm) and Co (57.4–84.8 ppm) contents, low ΣREE (2.13–13.81 ppm), as well as isotopic composition of O and H, classify the talcose rocks as a serpentinite-hosted type of deposit. Location in the strongly folded metamorphic unit, in the intimate vicinity of several faults and mylonitic zones, implies classification along the thrust-bound and fold-related metamorphogenic deposits. The talcose rocks are separated from serpentinites by the metasomatic chlorite schist, which contains two generations of monazite yielding two, different Th-U-total Pb dates. Older (389.8 ± 11.4 Ma) probably dates serpentinites juxtaposition with country paragneiss and chlorite formation. Younger (365.0 ± 18.2 Ma) likely dates amphiboles and talc formation, as overlaps the ages of amphibolite facies, country paragneiss migmatitization and intrusions of granitic pegmatites, and the talcose rocks contain talc-tremolite-anthophyllite assemblage indicative of the low-pressure mid-amphibolite facies. High MgO (24.27–27.21 wt%), Fe2O3 (5.06–5.12 wt%), Cr, Ni and Co contents are inherited from serpentinites. On the other hand, SiO2 (57.30–60.46 wt%), CaO (0.86–4.39 wt%), Al2O3 (1.38–3.04 wt%), TiO2 (0.02–0.04 wt%) and F (197–337 ppm) contents in the talcose rocks are higher than in host-serpentinites, likely due to a metasomatic introduction by fluids derived from migmatitic paragneisses or intruding pegmatites. Introduction of these elements is evidenced by a negative δ37Cl and elevated δ18O of the talcose rocks relative to host-serpentinites that are typical effects of interaction with a felsic crustal material. Interaction with paragneiss- and pegmatite-derived fluids is further evidenced by REE and trace elements patterns of the talcose rocks. The LREE/HREE enrichment, negative Sr and Ti anomalies, and positive Nb-La and Zr-Hf-Sm slopes, of the talcose rocks patterns, are similar as in paragneiss and pegmatite. Serpentinite bodies transformation into the talcose rocks was gradual and associated with increase of δ18O, and decrease of a Cl content, δD and δ37Cl. Pseudomorphic serpentinite, similar to abyssal serpentinites in terms of an isotopic composition (δ18O = +5.7‰, δD = –64‰, δ37Cl = +2.0‰), recrystallized into non-pseudomorphic serpentinite (δ18O = +7.1‰, δD = –48‰, δ37Cl = –0.1‰), which, in turn, was replaced by the talcose rock (δ18O = +8.3‰ to +8.7‰, δD = –52‰ to –48‰, δ37Cl = –2.6‰ to –0.1‰). Moreover, paragneiss- and pegmatite-derived fluids might have interacted with eclogite bodies during amphibolite facies-retrogression. Amphibolitized eclogite has Cl-rich amphibole rims, and negative δ37Cl (–0.5‰) consistent with a Cl-rich crustal fluid.
Ore Geology Reviews, 2022
The Gilów deposit is located in the Góry Sowie Massif of the Central Sudetes (NE Bohemian Massif,... more The Gilów deposit is located in the Góry Sowie Massif of the Central Sudetes (NE Bohemian Massif, SW Poland). Talcose rocks are associated with serpentinite bodies hosted by country migmatitic paragneiss, in an area where paragneiss also hosts amphibolitized eclogite bodies and granitic pegmatite veins. The talcose rocks and wall rocks were subjected to petrographic examination, electron microprobe study of minerals (including monazite Th-U-total Pb chemical dating), bulk rock chemical examination, as well as stable O, H and Cl isotope analysis. The talcose rocks can be used as a carving material and in ceramics, although the presence of tremolite and anthophyllite, and high Cr and Ni contents, preclude application in pharmacy and cosmetics. High Cr (2121.0–2148.4 ppm), Ni (1079–1561 ppm) and Co (57.4–84.8 ppm) contents, low ΣREE (2.13–13.81 ppm), as well as isotopic composition of O and H, classify the talcose rocks as a serpentinite-hosted type of deposit. Location in the strongly folded metamorphic unit, in the intimate vicinity of several faults and mylonitic zones, implies classification along the thrust-bound and fold-related metamorphogenic deposits. The talcose rocks are separated from serpentinites by the metasomatic chlorite schist, which contains two generations of monazite yielding two, different Th-U-total Pb dates. Older (389.8 ± 11.4 Ma) probably dates serpentinites juxtaposition with country paragneiss and chlorite formation. Younger (365.0 ± 18.2 Ma) likely dates amphiboles and talc formation, as overlaps the ages of amphibolite facies, country paragneiss migmatitization and intrusions of granitic pegmatites, and the talcose rocks contain talc-tremolite-anthophyllite assemblage indicative of the low-pressure mid-amphibolite facies. High MgO (24.27–27.21 wt%), Fe2O3 (5.06–5.12 wt%), Cr, Ni and Co contents are inherited from serpentinites. On the other hand, SiO2 (57.30–60.46 wt%), CaO (0.86–4.39 wt%), Al2O3 (1.38–3.04 wt%), TiO2 (0.02–0.04 wt%) and F (197–337 ppm) contents in the talcose rocks are higher than in host-serpentinites, likely due to a metasomatic introduction by fluids derived from migmatitic paragneisses or intruding pegmatites. Introduction of these elements is evidenced by a negative δ37Cl and elevated δ18O of the talcose rocks relative to host-serpentinites that are typical effects of interaction with a felsic crustal material. Interaction with paragneiss- and pegmatite-derived fluids is further evidenced by REE and trace elements patterns of the talcose rocks. The LREE/HREE enrichment, negative Sr and Ti anomalies, and positive Nb-La and Zr-Hf-Sm slopes, of the talcose rocks patterns, are similar as in paragneiss and pegmatite. Serpentinite bodies transformation into the talcose rocks was gradual and associated with increase of δ18O, and decrease of a Cl content, δD and δ37Cl. Pseudomorphic serpentinite, similar to abyssal serpentinites in terms of an isotopic composition (δ18O = +5.7‰, δD = –64‰, δ37Cl = +2.0‰), recrystallized into non-pseudomorphic serpentinite (δ18O = +7.1‰, δD = –48‰, δ37Cl = –0.1‰), which, in turn, was replaced by the talcose rock (δ18O = +8.3‰ to +8.7‰, δD = –52‰ to –48‰, δ37Cl = –2.6‰ to –0.1‰). Moreover, paragneiss- and pegmatite-derived fluids might have interacted with eclogite bodies during amphibolite facies-retrogression. Amphibolitized eclogite has Cl-rich amphibole rims, and negative δ37Cl (–0.5‰) consistent with a Cl-rich crustal fluid.
Ore Geology Reviews, 2022
Ore Geology Reviews, 2020
Abstract Nephrites belonging to both the dolomite-related and serpentinite-related genetic types,... more Abstract Nephrites belonging to both the dolomite-related and serpentinite-related genetic types, from the Zloty Stok deposit, and Jordanow Śląski and Naslawice prospects in the Śleza Ophiolite, respectively, were analyzed for Fe and Sr isotope compositions. These deposits in the Central Sudetes (SW Poland), are unusually situated relatively close to each other. This study is a first attempt to perform combined Fe and Sr isotope study of nephrites. Our results show that Fe in the Fe-As-Au-bearing skarn samples from Zloty Stok (2.77-7.00 wt.% Fe, δ56Fe +0.07 to +0.14‰, and δ57Fe +0.12 to +0.21‰), to which the dolomite-related nephrite belongs, is not inherited from the host dolomitic marbles (ca. 0.4 wt.% Fe; δ56Fe -0.08 to -0.07‰, and δ57Fe -0.12 to -0.09‰), but derived from the nearby, ca. 340 Ma granite intrusion (2.64-5.64 wt.% Fe). In contrast, iron in the serpentinite-related nephrites (2.06-3.88 wt.% Fe, δ56Fe +0.41 to +0.45‰, and δ57Fe +0.59 to +0.66‰) was likely inherited from host serpentinites (5.27-4.81 wt.% Fe), rather than metasomatically derived from adjacent granite intrusions (0.13-0.45 wt.% Fe). Moreover, both the marble transformation into a dolomite-related nephrite (and Fe-As-Au-bearing skarn), and the abyssal serpentinite – through ophiolite – towards serpentinite-related nephrite transformation, are accompanied by a progressive increase of δ56Fe and δ57Fe. This increase is regardless of changes in the bulk Fe content, increasing during the dolomite-related nephrite formation, and decreasing during serpentinite-related nephrite formation. This phenomena may be caused by one of the below listed factors, or combinations: a) preferential incorporation of heavy iron by tremolite and diopside; b) preferential incorporation of the heavy iron in the Fe3+-bearing phases, crystallizing during nephrite formation; c) preferential incorporation of the heavy Fe from migrating granite-derived fluids (positive fractionation between aqueous Fe-bearing fluid, and tremolite/diopside); d) positive isotope fractionation between dolomite/antigorite precursor, and newly formed amphibole/clinopyroxene; e) change of the Fe oxidation state. Furthermore, Fe in the rock-forming tremolite from the serpentinite-related nephrites is isotopically heavier than Fe in tremolite from the dolomite-related ones. In contrast to the iron, the isotopic composition of strontium, combined with its content and structural evidence, suggest multiple sources for this element. In the case of the dolomite-related nephrite (ca. 3-4 ppm Sr; initial 87Sr/86Sr = 0.7085), Sr inheritance from the host-dolomitic marble (ca. 90 ppm Sr; initial 87Sr/86Sr = 0.7081), as well as its derivation from intrusions of both the syn- to late-tectonic, ca. 340 Ma granites (ca. 400-440 ppm Sr), and post-tectonic ∼305 Ma granites (86.4 ppm Sr), is suggested. In the case of the serpentinite-related nephrite (6.3-61.7 ppm Sr; initial 87Sr/86Sr 0.7037 to 0.7081), the situation is similar, i.e., Sr in the most primitive samples tends to be sourced from ophiolitic rocks (up to 2.4 ppm Sr in serpentinite), whereas in the more evolved types, it was likely delivered from the adjacent, ca. 340 Ma (8.8-102.6 ppm Sr) partially rodingitized granites, as well as ∼305 Ma granites (ca. 80 ppm Sr). Moreover, these granites caused the fluid-flow, responsible for Sr-bearing clinozoisite vein formation; these veins are likely related with nephrite formation, and with a metallic mineralization.
Minerals, 2019
The Kletno deposit in the Śnieżnik Massif (Central Sudetes, SW Poland), mined for Fe, U, Ag, Cu, ... more The Kletno deposit in the Śnieżnik Massif (Central Sudetes, SW Poland), mined for Fe, U, Ag, Cu, fluorite, and marble through the ages, developed at the contact of marbles and orthogneiss. Here, we present a new Fe-Ti-V-ore (containing up to 14.07 wt.% Fe, 2.05 wt.% Ti, and 2055 ppm V in bulk rock) and ornamental- to gem-quality talc prospect at the southwest margin of this deposit. This newly documented Fe-Ti-V mineralization is hosted in hornblendites, dolomite veins, and chlorite schists, which, along with talc, envelopes a tectonic slice of serpentinite. Hornblendites are interpreted as metamorphosed ferrogabbros, derived from the same mafic melts as adjacent barren metagabbros. The oxygen and carbon isotope compositions of metabasites and dolomite veins (amphibole δ18O values = 8.8–9.3‰; carbonate δ18O values = 12.8–16.0‰, and δ13C values = −8.3‰ to −7.2‰), in combination with those of the country marbles (carbonate δ18O and δ13C values = 23.2‰ and +0.1‰, respectively), suggest...
Journal of Molecular Structure, 2018
Abstract Raman and infrared spectroscopy are fast, simple and useful methods of identifying and d... more Abstract Raman and infrared spectroscopy are fast, simple and useful methods of identifying and distinguishing between different rock samples, which often originate from different sources. We analyzed nephrite samples from Polish deposits (Zloty Stok in the Sudetes and Jordanow Śląski in the Fore-Sudetic Block). Studied nephrites amphiboles, with the general formula (Ca2(Mg,Fe)5Si8O22(OH)2), magnesium and iron contents, in terms of Fe/(Fe+Mg) per formula unit, are as follows: Jordanow Śląski (0.06–0.10), Zloty Stok type 1 (0.10–0.20) and Zloty Stok type 2 (0.04–0.18). Our spectroscopic study is consistent with results of previous petrographic microscopy, scanning electron microscopy and chemical composition of constituting minerals, measured by the electron microprobe; which methods were applied to the same nephrite deposits. Results of Jordanow and Zloty Stok nephrites studies were compared with data available in literature, which confirmed petrographic composition of studied samples. In addition, in case of actinolite nephrite samples (Fe/(Fe+Mg) > 0.10), qualification of the studied minerals to actinolite with content of Fe ion below 15% and 30% in sample from Jordanow Śląski and Zloty Stok, respectively, is possible based solely on applied spectroscopic methods. Spectroscopic studies also allowed to note the relationship between the obtained results and the genetic origin (serpentinite-related or dolomite-related) of the studied nephrites. Findings confirmed that spectroscopic methods are not only applicable and useful, but, which is very important in gemological and archaeometric practice, also non-destructive.
The Canadian Mineralogist, 2015
The Zloty Stok Au-As deposit (SW Poland) hosts two distinct nephrite varieties: ‘type 1’ – a gray... more The Zloty Stok Au-As deposit (SW Poland) hosts two distinct nephrite varieties: ‘type 1’ – a grayish green or pale green, translucent, with waxy to greasy luster nephrite composed of actinolite and abundant lollingite; ‘type 2’ – a deep or intense green, less-translucent, with sub-vitreous to dull luster nephrite composed of tremolite and actinolite, with rare lollingite and arsenopyrite. ‘Nephrite type 1’ shows evidence for more intense metasomatism and recrystallization than ‘type 2’, e.g. , more abundant arsenide, sulfosalt, and tungstate minerals, and higher Fe, As, and Co concentrations. The tremolite and actinolite in both types formed at the expense of dolomite—either directly from dolomite or through diopside formation. Calcite is a byproduct of the amphiboles' formation directly from dolomite. Amphiboles have Cr2O3 and NiO concentrations of 0.00–0.04 wt.% and 0.00 wt.%, respectively, typical of dolomite-related nephrites. Diopside composition (up to 51 Wo, 0.00–0.05 wt.% Cr2O3 and 0.00–0.09 wt.% NiO) is similar to other dolomite-related nephrite compositions. Bulk-rock Cr and Ni (<30 ppm and <40 ppm, respectively) and Co, which is less affected by ore mineralization (<10 ppm), are similar to the values in dolomite-related nephrite. Yellow cathodoluminescent diopside is similar to that in other metasomatized dolomitic marbles. Nephrite has δ18O values ranging from +8.3 to +10.4‰ (precision = ±0.1‰), higher than in other typical dolomite-related nephrite. δD values range from –77 to –75‰, similar to the dolomite-related type. Based on these observations, we interpret the Zloty Stok nephrite deposit to have formed as a metasomatic replacement of dolomitic marble. This is the third documented case of a dolomite-related origin (para-nephrite) for nephrite in Europe. Furthermore, the dolomite-related nephrite adds the Lower Silesian Sudetes and its Foreland to rare areas like Wyoming, southern Siberia, China, Korea, and the Alps, where both dolomite-related and serpentinite-related nephrites occur. The Zloty Stok nephrite formed via at least two crystallization events. In the first event, quartz veins and nephrite formed, and the paragenesis included quartz, tremolite, Fe-poor actinolite, Fe-poor diopside and, probably, arsenopyrite. In the second event, Si-depleted actinolite, Fe-enriched diopside, and lollingite formed, and the earlier arsenopyrite was replaced by calcite. The crystallization path reflects progressive metamorphism ( i.e. , temperature rise) or change in the saturation conditions, e.g. , silica and sulfur activity in the fluid. The nephrite formation can be linked with the emplacement and cooling of the neighboring Variscan Klodzko-Zloty Stok granite at ca. 340–298 Ma.
Geological Quarterly., 2015
Geological Quarterly, 2014
Lower Silesia hosts im por tant Eu ro pean neph rite de pos its of Jordanów and less-known of Zot... more Lower Silesia hosts im por tant Eu ro pean neph rite de pos its of Jordanów and less-known of Zoty Stok. Neph rite ar ti facts were dis cov ered in ar chae o log i cal sites dated back to the Neo lithic pe riod, across Eur asia. Es pe cially ar ti facts found in Po land, It-aly and Bul garia may orig i nate from Pol ish nephrites. Now a days, only one ar ti fact is pre cisely linked to Jordanów. Petrographic study of nephrites and chem i cal anal y ses of con stit u ents by means of EMPA al low ac cu rate iden ti fi ca tion of the nephrites. The char ac ter is tic phases of Jordanów tremolite neph rite are ro tated and cataclased di op side porphyroblasts with pres sure shad ows, chlorite lay ers and nests with in ter lock ing non-pseudomorphic tex ture and prehnite veins. The pres ence of hydrogrossular, grossular, ti tan ite, ap a tite with monazite in clu sions, and zir con with pleochroic haloe is typ i cal. Chlorites are usu ally rep re sented by penninite, and mi nor clinochlo...
The As-bearing minerals from the contact aureole of K odzko-Z oty Stok granitoid Intrusion Unit (... more The As-bearing minerals from the contact aureole of K odzko-Z oty Stok granitoid Intrusion Unit (Sudetes Mts) are known since medieval ages. The main As-ore bearing minerals in this deposit are arsenopyrite and lollingite (J !drzejewska, Sa aci "ski 1997). Nephrite occurs there occasionally, forming thin veins within pyroxenites. The microprobe study of the As-ore minerals from the Z oty Stok nephrites was the main goal of this research. After the field sampling, the conventional petrographic studies were made and some samples were marked out for microprobe analysis . The 18 electron microprobe analyses of the As-ore bearing minerals were carried out using the Cameca SX 100 microprobe analyzer in the Microscopy and Microprobe Laboratory at the Warsaw University,. The obtained results showed that the As-ore bearing minerals from Z oty Stok
Fe and Sr isotopic data of nephrite, clinopyroxenite and dolomitic marble.
Nephrite is mainly known in prehistoric context as raw material for polished stone tools. It is p... more Nephrite is mainly known in prehistoric context as raw material for polished stone tools. It is present among archaeological finds in Hungary only in a few numbers. They are known mostly from Transdanubian archaeological sites. The general aim of our investigations is the detailed petrographic and geochemical examination of the nephrite artefacts found on Hungarian sites, and locating the origin of the raw materials. The material was basically investigated by non-destructive methods (PGAA, non-destructive SEM-EDX) to avoid invasive analyses on the complete artefacts. In this study, preliminary results are presented. Based on their chemical composition, most of the artefacts measured so far belong to the S-type (serpentiniterelated) nephrite deposits. On the basis of their microscopic and mineral-chemical features, the artefacts investigated so far can be divided into five raw material types: (1) almost pure tremolite-nephrite with only a few fine grained magnetite or ilmenite grains...
9th International Conference Mineralogy and Museums, 2021
Nephrite artefacts are rare discoveries in archeological sites dated back to early Neolithic. Pre... more Nephrite artefacts are rare discoveries in archeological sites dated back to early Neolithic. Precise identification of the raw material source provides valuable information about the past mining activity, as well as migration and trade routes due to rarity of nephrite deposits. Serpentinite-related nephrite occurrences from Jordanów Śląski and Nasławice in the Ślęża Ophiolite, and dolomite-related nephrite from the Złoty Stok deposit in the Śnieżnik Massif, were selected for investigation focused at documentation of unique features, allowing unequivocal identification of the raw material source. Both nephrite deposits are located relatively close each other, in the Central Sudetes terrane (SW Poland) of the European Variscan Belt.